doi 101098rsta20010964 767-802360 2002 Phil Trans R Soc Lond A
CHRIS S M TURNEYSIWAN M DAVIES NICHOLAS P BRANCH J JOHN LOWE and Holoceneframework for Termination 1 and the Early Towards a European tephrochronological
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101098rsta20010964
Towards a European tephrochronologicalframework for Termination 1 and
the Early Holocene
By Siwan M Davies Nicholas P BranchJ John Low e a n d Chris S M Turneyy
Centre for Quaternary Research Department of GeographyRoyal Holloway University of London EghamSurrey TW20 0EX UK (smdaviesrhulacuk)
Published online 19 March 2002
The record of deposition of tephras in Europe and the North Atlantic during theperiod 18580 14C ka BP (the Last Termination and Early Holocene) is reviewedAltogether 34 tephras originating from four main volcanic provinces (Iceland theEifel district the Massif Central and Italy) have been identishy ed so far in geologicalsequences spanning this time-interval Most of the records have been based untilvery recently on observations of visible layers of tephras Here we report on thepotential for extending the areas over which some of the tephras can be traced bythe search for layers of micro-tephra which are not visible to the naked eye andon the use of geochemical methods to correlate them with known tephra horizonsThis approach has greatly extended the area in Northern Europe over which theVedde Ash can be traced The same potential exists in southern Europe which isdemonstrated for the shy rst time by the discovery of a distinct layer of micro-tephraof the Neapolitan Yellow Tunot in a site in the Northern Apennines in Italy far tothe north of the occurrences of visible records of this tephra The paper closes byconsidering the potential for developing a robust European tephrostratigraphy tounderpin the chronology of records of the Last Termination and Early Holocenethereby promoting a better understanding of the nature timing and environmentalenotects of the abrupt climatic changes that characterized this period
Keywords non-visible tephra layers electron microprobeabrupt climate change Late Glacial period
1 Introduction
A series of abrupt high-amplitude climatic changes characterizes Termination 1 andthe Early Holocene (shy gure 1) especially during the transition between the last coldstage and the present interglacial usually termed the `Late Glacialrsquo (ca 1390 14C kaBP or 14790 GRIP ice-core ka BP) (due to signishy cant dinoterences in the time-scalesderived from ice-core radiocarbon and varve dating the basis of all age estimatesquoted in this paper are specishy ed thus 14C = radiocarbon years (uncalibrated)
y Present address School of Archaeology and Palaeoecology Queenrsquo s University Belfast BelfastBT7 1NN UK
Phil Trans R Soc Lond A (2002) 360 767802
767
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768 S M Davies and others
- 42 - 40 - 38 - 36 - 34
Holocene
Greenland stadial 1
Greenland interstadial 1
Greenland stadial 2
GI-1aGI-1b
GI-1c
GI-1d
GI-1e
GR
IP ic
e co
re (
year
s B
P)
18O permil (SMOW)d
11 000
12 000
13 000
14 000
15 000
16 000
17 000
18 000
19 000
20 000
Figure 1 The Greenland event stratigraphy scheme based on the macr 18 O record (SMOW) andstratigraphic terminology for the Last Termination and Early Holocene (after Bjorck et al 1998 Walker et al 1999)
cal = calibrated radiocarbon years GRIP ice-core yrs refers to the GRIP ss08c time-scale) (Walker 1995 Lowe et al 1999) The most pronounced features in the climaticrecords for this period are abrupt warmings at the start of Greenland Interstadial 1(the GI-1e thermal maximum) and at the onset of the Holocene and a short periodof severely cold conditions corresponding to the `Younger Dryasrsquo stadial or theGS-1 event (Greenland Stadial 1) in the proposed Greenland stratotype sequence(see Bjorck et al 1998 Walker et al 1999)
A broadly similar pattern of climatic changes has been inferred from records of theLast TerminationEarly Holocene obtained from widely scattered localities through-out the North Atlantic region and which have been derived from a wide range ofproxy data These include for example macr 18O and snow-accumulation records fromthe Greenland ice cores (Alley et al 1993 Dansgaard et al 1993) fossil beetle andchironomid assemblages from the British Isles (Atkinson et al 1987 Coope et al 1998 Lowe et al 1999 Brooks et al 1997) greyscale variations reregecting ratesof sediment accumulation in laminated deposits of the tropical Atlantic (Hughenet al 1996 1998) and macr 18O variations in Swiss German and Dutch lake sediment
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 769
sequences (Lotter et al 1992 von Grafenstein et al 1999 Hoek amp Bohncke 2001)A question that is pivotal to understanding the climate-driving mechanisms in theNorth Atlantic region is whether the abrupt events as well as the environmentalresponses to them were synchronous within the continental marine and polar icerealms or whether there were signishy cant `leadsrsquo and `lagsrsquo between them
The Greenland ice-core records suggest that some of the climatic transitions duringthe Last Termination took place within only a few decades (Mayewski et al 1997)while the short-lived cooling events within GI-1 lasted some 100300 ice-core yr atmost Determining the precise timing and duration of equivalent events representedin the ocean and continental records is extremely dimacr cult at present because of theuncertainties associated with the dating methods employed Age estimates obtainedusing the most widely adopted method radiocarbon dating have error ranges at 1frac14that are rarely better than sect50 14C yr and which frequently exceed sect100 14C yror more Interpretations of radiocarbon ages are complicated still further by uncer-tain calibration procedures and the distorting inreguences of radiocarbon `plateauxrsquo|episodes of near-constant radiocarbon age (see Lowe amp Walker 2000) Radiocarbondates obtained from marine sequences of Last Termination age are particularly sus-pect due to the inreguences of marine reservoir errors (Sikes et al 2000 Waelbroecket al 2001) There are equally wide uncertainties associated with other methodssuch as varve counting while the ice-core records themselves in the segment ofthe records that span the Last Termination may have systematic errors exceeding200 years (Stuiver amp Grootes 2000) A further problem is that some of the climatechanges at this time may have been time-transgressive (Coope et al 1998 Witteet al 1998) signishy cantly undermining the use of conventional approaches such asclimatostratigraphy and biostratigraphy for correlating the records It is evidentthen that conventional approaches to the dating and correlation of events duringthe Last Termination are inadequate for testing the hypothesis that abrupt climaticchanges during this period were truly synchronous at the continental or global scale
The problems of dating and correlating sequences that span the Last Terminationhave been reviewed through a series of workshops organized by the INTIMATE group(INTegration of Ice core MArine and TErrestrial records of the Last Termination|a core programme of the International Quaternary Union (INQUA) Palaeocli-mate Commission (httpwwwgeoguunlfgpalaeoclimateintimate)) (Bjorck etal 2001) which has recommended a set of proposals for improved precision in thefuture (Lowe et al 2001) Central to these proposals is the application of correlationtools that can provide independent tests of the age estimates and correlations basedon radiocarbon dating varve chronology and ice-layer counting
One of the approaches recommended by the INTIMATE and COTAV (INQUACommission on Tephrochronology and Volcanism) groups is tephrochronology forthere is growing evidence to suggest that this technique has the potential to resolvesome of the pressing geochronological issues while some tephras may be detectableover much wider geographical areas than appreciated hitherto Here we examine thepotential for developing a tephrostratigraphical and tephrochronological frameworkfor Europe for the period 18580 14C ka BP (encompassing the Last Terminationand the Early Holocene) It is argued that such a scheme will provide a rigorousunderpinning structure for geochronological models for this period and hence leadto improved understanding of the mechanisms timing and environmental enotects ofabrupt climatic changes during the Last Termination
Phil Trans R Soc Lond A (2002)
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770 S M Davies and others
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European tephrochronological framework for Termination 1 771
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772 S M Davies and others
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den
Bogaard
ampS
chm
inck
e(1
985)
19
Fri
edri
chet
al
(1999)
20
Bra
uer
eta
l(1
999)
21
Etl
ich
eret
al
(1987)
22
Tu
rney
etal
(1997)
23
Pate
rne
et
al
(1986)
24
Kel
ler
(1980)
25
Eir
parasup3kss
on
etal
(2000)
26
Hadeg
idaso
net
al
(2000)
27
Ale
ssio
etal
(1976)
28
Vez
zoli
(1991)
29
San
tacr
oce
(1987)
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 773
Tab
le1
(Con
t)
GR
IPage
tep
hra
age
(ss0
8c
volc
an
ich
ori
zon
(14C
yrs
)ti
me-
scale
)n
SiO
2T
iO2
Al 2
O3
FeO
Mn
OM
gO
CaO
Na
2O
K2O
P2O
5to
tal
EP
MA
sou
rce
ref
La
Nu
gmicroere
ca11
400
12
549
922
9160
470
002
324
454
744
538
972
4W
DS
La
Nu
gmicroere
6
21
(MC
)
Nea
poli
tan
ca12
000
17
588
104
2177
631
901
006
525
940
686
9
962
8W
DS
Cam
pi
1Y
ello
w(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(0
78)
Fle
gre
i
Tu
reg(I
T)
568
106
0194
448
7
17
451
938
75
5
100
ED
S
596
804
9192
940
3
06
435
034
588
9
100
ED
S2
14
619
403
1196
329
9
02
019
943
485
7
100
ED
S
Borr
ob
ol
ca12
300
18
733
601
1122
914
700
601
207
635
837
6
955
1W
DS
Hek
la22
(IC
)(0
35)
(00
2)
(01
8)
(00
9)
(00
2)
(00
2)
(00
3)
(01
4)
(00
9)
(0
47)
un
kn
ow
n14
650
sect200
(Ca
pea
k)
(17458
m)
un
kn
ow
n14
650
sect200
(C
ap
eak)
(17506
m)
E-2
P
oll
ara
ca13
000
766
302
7138
810
8
01
015
025
239
7
100
ED
SA
eoli
an
2
23
24
pu
mic
e(I
T)
Isla
nd
s
KO
L-G
S-2
13
400
18
490
910
6148
8100
702
184
9126
521
400
902
8989
6W
DS
25
(IC
)
GS
-2B
AS
-113
400
3497
417
0132
7124
402
266
6118
124
802
103
4988
7W
DS
26
(IC
)
Ref
eren
ces
1
this
stu
dy
2
Pate
rne
etal
(1988)
3
Narc
isi
(1996)
4
All
enet
al
(1999)
5
An
dro
nic
oet
al
(1995)
6
Ju
vig
nparae
et
al
(1996)
7
Bir
ks
et
al
(1996)
8
Bjo
rck
ampW
ast
egordma
rd(1
999)
9
Du
gm
ore
ampN
ewto
n(1
998)
10
Bjo
rck
et
al
(1992)
11
Kva
mm
eet
al
(1989)
12
Zoli
tsch
ka
etal
(1995)
13
Ju
vig
nparae
ampG
ewel
t(1
987)
14
Di
Vit
oet
al
(1999)
15
Del
ibri
as
etal
(1979)
16
Ju
vig
nparae
etal
(1987)
17
Dav
ies
et
al
(2001)
18
van
den
Bogaard
ampS
chm
inck
e(1
985)
19
Fri
edri
chet
al
(1999)
20
Bra
uer
eta
l(1
999)
21
Etl
ich
eret
al
(1987)
22
Tu
rney
etal
(1997)
23
Pate
rne
et
al
(1986)
24
Kel
ler
(1980)
25
Eir
parasup3kss
on
etal
(2000)
26
Hadeg
idaso
net
al
(2000)
27
Ale
ssio
etal
(1976)
28
Vez
zoli
(1991)
29
San
tacr
oce
(1987)
Phil Trans R Soc Lond A (2002)
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774 S M Davies and others
Tab
le1
(Con
t)
(Th
evarv
eage
for
the
Gre
enis
h(I
T)rsquo
row
is17
560
yea
rs)
GR
IPage
tep
hra
age
(ss0
8c
volc
an
ich
ori
zon
(14C
yrs
)ti
me-
scale
)n
SiO
2T
iO2
Al 2
O3
FeO
Mn
OM
gO
CaO
Na
2O
K2O
P2O
5to
tal
EP
MA
sou
rce
ref
GS
-2B
AS
-213
400
6497
933
2122
4147
902
445
389
829
905
205
4979
4W
DS
26
(IC
)
GS
-2B
AS
-313
400
2538
529
9125
7131
203
132
174
729
507
707
7980
1W
DS
26
(IC
)
GS
-2B
AS
-414
000
7503
617
4145
1113
202
155
3100
528
010
5
975
7W
DS
26
(IC
)
Un
ita
dei
ca14
000
5648
804
7184
625
901
602
217
432
679
302
8100
ED
SP
hle
gre
an
3
27
Tef
ra(0
53
)(0
13
)(0
25)
(07
4)
(01
4)
(01
6)
(01
6)
(03
4)
(06
6)
(01
6)
Fie
lds
Su
per
iori
(IT
)
Y-1
(IT
)ca
14
000
16
600
413
7169
555
502
218
242
262
229
306
8100
ED
SE
tna
28
Bla
ck17
000
sect300
Fea
ther
(17890
m)
Gre
enis
hca
15
000
9618
704
190
731
601
804
328
531
586
202
6100
ED
SV
esu
viu
s3
4
(IT
)(0
70
)(0
08
)(0
45)
(06
8)
(01
0)
(01
0)
(05
9)
(05
3)
(05
8)
(01
6)
29
L9
(IT
)ca
16
000
15
626
704
4188
630
401
103
329
429
683
402
7100
ED
SV
esu
viu
s3
15
17
000
(14
2)
(01
4)
(07
2)
(11
1)
(00
9)
(02
4)
(06
6)
(04
8)
(06
5)
(01
8)
St
2-1
85
18
500
7504
015
1145
5112
002
466
9114
525
206
6
992
2W
DS
26
(IC
)
Ref
eren
ces
1
this
stu
dy
2
Pate
rne
etal
(1988)
3
Narc
isi
(1996)
4
All
enet
al
(1999)
5
An
dro
nic
oet
al
(1995)
6
Ju
vig
nparae
et
al
(1996)
7
Bir
ks
et
al
(1996)
8
Bjo
rck
ampW
ast
egordma
rd(1
999)
9
Du
gm
ore
ampN
ewto
n(1
998)
10
Bjo
rck
et
al
(1992)
11
Kva
mm
eet
al
(1989)
12
Zoli
tsch
ka
etal
(1995)
13
Ju
vig
nparae
ampG
ewel
t(1
987)
14
Di
Vit
oet
al
(1999)
15
Del
ibri
as
etal
(1979)
16
Ju
vig
nparae
etal
(1987)
17
Dav
ies
et
al
(2001)
18
van
den
Bogaard
ampS
chm
inck
e(1
985)
19
Fri
edri
chet
al
(1999)
20
Bra
uer
eta
l(1
999)
21
Etl
ich
eret
al
(1987)
22
Tu
rney
etal
(1997)
23
Pate
rne
et
al
(1986)
24
Kel
ler
(1980)
25
Eir
parasup3kss
on
etal
(2000)
26
Hadeg
idaso
net
al
(2000)
27
Ale
ssio
etal
(1976)
28
Vez
zoli
(1991)
29
San
tacr
oce
(1987)
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European tephrochronological framework for Termination 1 775
Altogether 34 tephra layers have been reported from sediment sequences in Europeand the NE Atlantic region which date to the period between 185 and 80 14C ka BP(table 1) Because tephra layers are deposited virtually instantaneously (in geologicalterms) they enotectively represent time-parallel marker horizons within stratigraphicalsequences (Westgate amp Gorton 1981 Sarna-Wojcicki 2000 Turney amp Lowe 2001) Intheory therefore all 34 tephras could prove valuable for correlation purposes eitherin a local context or in those cases where the ash deposits have been widely dispersedbetween regional sequences In practice however very little is known about the fullgeographical dispersal of the majority of the ash layers listed in table 1 Furthermorecorrelation by tephrostratigraphy will only work if the various ash layers have wellcharacterized geochemical signatures While some geochemical data are available forthe majority of the tephras listed in table 1 the collective data are far from robustand no geochemical data have yet been published for some
Nonetheless there is mounting evidence to show that some of the tephra depositslisted in table 1 are not only geochemically distinct but are also much more widelydispersed across Europe than was initially realized Stratigraphic records of thebetter-known tephras were initially limited to observations of visible tephra layersThe development of a technique that enables detection of tephra layers that are invis-ible to the naked eye (micro-tephra) in Late Glacial sequences has greatly extendedthe area over which some of the ashes can be traced (Lowe amp Turney 1997 Turneyet al 1997 Turney 1998 Wastegard et al 1998 2000a b) Most of this research sofar has focused on micro-tephra layers originating from Icelandic centres distributedthroughout northern Europe Here we report on further development of this line ofresearch with new evidence for the occurrence of micro-tephra layers in a site insouthern Europe The results suggest that there is great potential for tracing someash layers that originated from Italian volcanic complexes over much larger tracts ofsouthern and central Europe than records of visible tephra deposits allow This inturn greatly enhances the scope for making precise correlations not only betweenparts of southern Europe but also between continental and marine (MediterraneanSea) sequences
2 Micro-tephra extraction techniques
Micro-tephra horizons are composed of glass shards that are generally between 80and 24 m m (long axis) in size and that are present in such low concentration insedimentary sequences that they can only be detected by the use of a particle sep-aration technique Several factors inreguence the concentration of shards such as dis-tance from the volcanic source precipitation patterns during the eruption and sub-sequent tephra dispersal and sedimentary processes within the catchment In someterrestrial sequences micro-tephra horizons with a peak concentration (peak con-centration tends to coincide with the shy rst occurrence of glass shards in a sedimentsequence which is then taken to mark the time of maximum ash deposition) as lowas 10 shards cmiexcl3 has been conshy rmed whereas other sites have recorded as muchas 8000 shards cmiexcl3 (Turney et al 1997) In complete contrast tephra horizons inthe GRIP ice core have been identishy ed based on a single glass shard only (Gronvoldet al 1995)
Enotective separation techniques for the detection and isolation of tephra particlesfrom sedimentary sequences have been developed These include ashing of organic
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776 S M Davies and others
matter (Pilcher amp Hall 1992) digestion of biogenic and opaline silica (Rose et al 1996) the use of magnetic properties of ash layers (see for example Oldshy eld et al 1980 van den Bogaard et al 1994 Pawse et al 1998) X-ray analysis (Dugmore ampNewton 1992) and a density separation (regotation) technique (Turney 1998) Den-sity separation has proved exceedingly useful for the detection of small glass shardspresent in low concentrations in mineral-rich Late Glacial sediments This involvesthe separation and concentration of particles of predetermined specishy c gravity withthe use of a heavy liquid and subsequent identishy cation of glass shards with the useof a polarizing light microscope (for further details see Turney (1998)) This methodhas been particularly successful in the detection of tephras of rhyolitic compositionthat have a specishy c density of 2325 g cmiexcl3 (Lowe amp Turney 1997 Turney et al 1997 2001 Turney 1998 Wastegard et al 1998 2000a b) It is this technique thathas resulted in the wider recognition of micro-tephras in Europe as discussed below
3 Geochemical ` ngerprintingrsquo of tephra layers
The 34 tephras listed in table 1 have originated from four major volcanic complexesIceland the Massif Central in central France the Eifel district near Bonn and threevolcanic centres in Italy (the Campanian group Etna and the Aeolian Islands (seeshy gure 2)) An important matter to resolve is the extent to which the various magmasand ashes generated by these volcanic complexes can be geochemically shy ngerprintedThis is especially important in the case of tephras which have originated from thesame volcanic centre in which there may have been limited geochemical evolution ofmagmas over time In this section we summarize the approach generally adopted todetermine the geochemical character of visible and micro-tephras as background tothe geochemical data summarized in table 1 In the subsequent section of the paperwe review the present state of knowledge concerning all 34 tephras listed in table 1
Glass shards formed during the rapid cooling of magma are thought to have acomposition that is representative of the bulk geochemistry of the magma (Barker1983) hence widely dispersed glass particles are regarded as the most appropriateconstituents of pyroclastic material for geochemical analysis If a tephra deposit canbe shown to have a distinct geochemical signature then it can be used to correlatethe stratigraphic units in which it occurs (tephrostratigraphy) as well as to datethese units (tephrochronology) if the ages of the tephras are known (Westgate ampGorton 1981) A key element of building a tephrostratigraphical framework there-fore is to establish as rigorously as possible the geochemical composition of theindividual tephras used in its construction Robust and directly comparable geo-chemical datasets are dimacr cult to assemble for glass however because it is highlyunstable material particularly prone to sodium mobilization
The technique most widely employed to establish the geochemical signature of atephra is electron probe micro-analysis (EPMA) This enables grain-discrete determi-nations of the major elements within an individual glass shard which is of particularbeneshy t in the analysis of micro-tephra layers which generally contain glass particlesin low concentration The glass surface is bombarded with an electron beam and theX-ray energy produced is unique to each element while the intensity of the signalemitted is proportional to the amount of that element in the glass shard (Hunt amp Hill1993) Measurement can be by either energy dispersive spectrometry (EDS) or wave-length dispersive spectrometry (WDS) EDS has a lower precision mainly because
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European tephrochronological framework for Termination 1 777
N
0 500 km
Confirmed records of Vedde Ash (visible occurrences)
New records of Vedde Ash from flotation method
Extended area of Vedde Ash detection (micro-tephra)
Known area of Laacher See Tephra (visible occurrences)
Confirmed records of Neapolitan Yellow Tuff (visible occurrences)
New record of Neapolitan Yellow Tuff from flotation method
Known area of Neapolitan Yellow Tuff
Volcanic centres of particular relevance to this study
Other major volcanic centres in Europe
Figure 2 Location of the principal volcanic centres that were active during Termination 1 andthe Early Holocene The known distribution of the Vedde Ash (VA) Laacher See (LST) andNeapolitan Yellow Tureg (NYT) are shown
the behaviour of each element cannot be monitored independently during measure-ment and so this approach fails to detect for example any signishy cant mobilizationof sodium during the bombardment process (Hunt amp Hill 1993) Although WDSrequires a higher beam current and a longer counting time than EDS the formeronoters the distinct advantage of sequential acquisition of elemental data so that thedegree of sodium loss can be tracked The morphology of individual glass shards canalso distort EDS data a problem that is reduced when using WDS because for thisprocedure glass shards are mounted in an epoxy resin and polished to provide aregat surface for analysis Hence data should always be obtained using WDS whereverpossible
Even when WDS is used as a common tool for determining the geochemical spectraof samples aberrant results can arise that inreguence data comparisons For examplesome glass shards may contain tiny crystalline inclusions of feldspar and these shouldbe avoided when selecting surface points for analysis (Hunt amp Hill 2001) Hunt amp Hill
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778 S M Davies and others
6
4
2
40 50 60 70 80
K2O
(
)
SiO2 ()
Laacher See
Iceland
Veidivoumltn-Dyngjufjoumlll
Katla (basalt)
Grimsvoumltn-Kverkfjoumlll
Hekla
Katla (rhyolitic)
0
Icelandic volcanic centres8
10
Massif Central
Etna
Campanian
Figure 3 Bi-plot of SiO2 and K2 O concentrations in tephras derived from the main Europeanash provinces (modimacred after Mangerud et al 1984) The Campanian Massif Central and Etnaconcentrations are based on the data presented in table 1
(2001) have concluded that small variations in the laboratory procedures employedto determine glass chemistry can lead to misidentishy cation of sources for glass shardsand give an example of shards with a Jan Mayen provenance wrongly attributedto an Icelandic source Clearly there is a need for standardization of laboratoryprocedures and while a number of recommendations have recently been advocated(Froggatt 1992 Hunt amp Hill 1993 Hunt et al 1998) there is still some variation inlaboratory and operator practice (Hunt amp Hill 1996) Standardization is also requiredin the form in which results are presented to ensure comparability Normalizationof the data to 100 a practice employed by some researchers can obscure poorresults and hence lead to incorrect comparisons (Hunt amp Hill 1993) However othersargue that it may actually facilitate comparisons between samples by removing thedistorting enotects of the water component contained in glass shards (see for exampleFroggatt 1992) The majority of the published Italian and some of the Eifel datahave been normalized while those from other parts of Europe have not and hencedata comparisons are not always straightforward
Table 1 provides mean values and standard deviations for major oxide concentra-tions obtained from those tephras for which data are presently available The tableincludes previously unpublished WDS results for the Neapolitan Yellow Tunot (NYTdiscussed in x 4 below) and for the Mercato Tephra While individual tephra layersmay be geochemically distinct the geochemical envelopes representing the collectivedata obtained from all of the tephras assigned to each major volcanic province showsignishy cant overlaps as is illustrated in the bi-plots and ternary plots (shy gures 3 and 4)of selected oxide concentration data It is clear therefore that measurement of majoroxide concentrations does not satisfactorily discriminate between some tephras orig-inating from dinoterent volcanic centres (as noted by van den Bogaard amp Schmincke(1985) and Frezzotti amp Narcisi (1996) with respect to Eifel and Italian tephras)nor of tephras of dinoterent age originating from the same volcanic centre (Bond et
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European tephrochronological framework for Termination 1 779
40 50 60 70 80
K2O
(
)
SiO2 ()
shyshyshyshy
shy
shyshy
shyshyshy
shy
shy
shy
shy
reg
reg regreg
regregregregreg regregregregreg
FF
F
ll
l
l
4 8 12 16
reg
regreg
regreg
regregreg
regreg
regregreg
shy
F
l shyshyshyshyshy shyshyshyshyshyshy
F
F
l
ll
FeO ()
TiO
2 (
)
reg
l
Iceland
Eifel
F
shy ItalyMassif Central
100
80
60
40
20
100
80
60
40
20
100 80 60 40 20
CaO
FeO
K2O
regregreg
reg
reg
reg
reg
reg
reg
regregreg
shyF
F
F
regreg
l
lllshy
shyshyshy
shyshyshy
l
0
2
4
6
8
10
0
1
2
3
4
5
regreg
regreg
regreg
regreg
regreg
reg
reg
regreg
l
l
ll
shy
shyshy
shyshy
shy
shyshy
FF
F
100
80
60
40
20
100
80
60
40
20
100 80 60 40 20
K2ONa2O
CaO
(c) (d)
(a)
(b)
Figure 4 Plots of selected geochemical data obtained from tephras of Termination 1 age (seetable 1) (a) Bi-plot of mean SiO2 and K2 O values (b) Bi-plot of mean FeO and TiO2 values(c) Ternary plot indicating variations in the proportions of FeO CaO and K2 O (d) Ternaryplot indicating variations in the proportion of CaO Na2 O and K2 O
al 2001) Individual tephra layers are presently assigned to a particular volcanicevent on the basis of a combination of criteria usually including examination of thephysical properties (eg refractive index and surface detail of the glass shards) thestratigraphic position of the layer and independent assessment of the age of the layeras well as any geochemical data that may be available The construction of a tephro-stratigraphical scheme would clearly beneshy t from the application of a more diagnostic
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780 S M Davies and others
geochemical tool One approach that has promise is the analysis of trace and rareearth elements using an ultraviolet laser ablation inductively coupled plasma massspectrometer (UV-LA-ICP-MS) (Pearce et al 1996 1999 Eastwood et al 1999)This approach has been applied successfully to analysis of tephras of Mid-Holoceneage but not yet to tephras that fall within the period of interest here
4 Tephra layers in Europe and the North Atlantic regiondated to between 185 and 80 14C ka
(a) Icelandic province
The Icelandic volcanic systems are divided into three main groups based on theirgeochemical characteristics tholeiitic basalts transitional alkali basalts and alkaliolivine basalts (Jakobsson 1979) Collectively magmas from the Icelandic provincespan a wide geochemical spectrum although individual volcanic centres have tightgeochemical distributions (shy gure 3) for four of the main centres Grimsvotn-Kverfjolland Veidvotn-Dyngjufoll which form part of the northern (tholeiitic) volcanic zoneand Hekla and Katla which fall within the eastern (alkali olivine basalt and transi-tional alkali basalt) volcanic zone (Haregidason et al 2000) These appear to be thekey centres for the tephras listed in table 1 that have been assigned an Icelandicorigin
One of the best-known and most widely dispersed tephra horizons in northernEurope that has an Icelandic origin is the Vedde Ash (VA) which was depositedca 103 14C ka BP (Birks et al 1996 Wastegard et al 1998) within the GS-1Younger Dryas chronozone This ash is believed to originate from the Katla complexwithin the transitional alkali basalt province (Mangerud et al 1984 Lacasse et al 1995) in the south of the island The ash has a bimodal geochemical composition (rhy-olitic and basaltic) which is thought to reregect derivation from two separate magmachambers Studies of recent volcanic events in Iceland have shown that the mostexplosive eruptions generating the largest amounts of tephra occur in this tran-sitional alkali basalt province (Haregidason et al 2000) It is also believed that thewidespread distribution of this ash was caused by the development of co-ignimbriteash plumes during an ignimbrite-forming eruption (Lacasse et al 1995)
Layers of VA that are visible to the naked eye have been found in lake sediments inwestern Norway (Mangerud et al 1984) and the Inner Hebrides Scotland (Davies etal 2001) and in marine cores throughout the NE Atlantic (see for example Kvammeet al 1989 Lacasse et al 1995) in the northern North Sea (Long amp Morton 1987)on the Iceland plateau (Ruddiman amp McIntyre 1981 Sejrup et al 1989) and on theeast Greenland continental margin (Stein et al 1996) The distribution of the VAin North Atlantic marine sequences is characterized by an arcuate lobe extendingsouthwest from the Denmark Strait and curving eastwards to mid-latitudes in theNorth Atlantic (Lacasse et al 1995) This strongly suggests deposition from raftedice which was displaced to the southwest and south in a circulating counterclockwisegyre (Ruddiman amp Glover 1972) This may well reregect Katlarsquos close proximity tothe southern coast of Iceland with the Vedde tephra being deposited on ice thatcalved directly into the North Atlantic (Haregidason et al 2000) However depositionvia the atmosphere almost certainly took place as well as is indicated by the recentdiscoveries of rhyolitic VA in micro-tephra form in several sites in Scotland (Turneyet al 1997) southern Sweden (Wastegard et al 1998 2000a) and western Russia
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(Wastegard et al 2000b) A more recent discovery of a relatively high concentrationof rhyolitic VA glass shards in the northern Netherlands indicates that the ash maywell have been dispersed much further south than previously thought (S M Davies2002 unpublished work) Finally glass shards assigned to the VA have also beendiscovered in the GRIP ice core and dated to 11 980 sect 80 GRIP yr BP (Gronvold etal 1995) This discovery is extremely important for it indicates that the VA maywell provide a reliable time-parallel marker horizon between ice-core marine andterrestrial records
Two other important Icelandic ash layers the Borrobol and Saksunarvatn Tephraswere deposited near the beginning and end of the Last TerminationEarly Holoceneinterval respectively The Borrobol Tephra was discovered for the shy rst time in lakesediments in several sites in Scotland and as yet is known only in micro-tephra formIt has been dated in Scottish sites to ca 123 14C ka BP (Turney et al 1997) Whatis thought to be a contemporaneous tephra has been detected in marine sedimentson the North Icelandic shelf (Eirplusmn ksson et al 2000) This certainly has a very similargeochemical composition to those reported from Scotland but the horizon in whichit was discovered on the North Iceland plateau has been dated to 134 14C ka Theage discrepancy between the Scottish and Icelandic Borrobol Tephra layers may wellreregect the inreguence of a marine reservoir error although the possibility that severaltephras with similar geochemical composition were erupted over a period exceeding1000 yr cannot be ruled out (Larsen 2000)
The Saksunarvatn Ash appears to have been one of the largest Holocene eruptionsin Iceland It has a tholeiitic basaltic composition which is considered to indicate anorigin in the Grimsvotn or Kverfjoll complex (shy gure 3) (Mangerud et al 1986) Layersof this ash have been identishy ed in sites on the Faroe Islands (Mangerud et al 1986Dugmore amp Newton 1998 Wastegard et al 2001) the Shetland Isles (Bennet et al 1992) northern Germany (Merkt et al 1993) western Norway (micro-tephra) (Birkset al 1996) and in the GRIP (Gronvold et al 1995) and NordGRIP ice cores (S MDavies 2002 unpublished work) It has been dated to between 9060 and 8930 14C kaBP (Birks et al 1996) in Norway and to ca 10 240 sect 30 GRIP yr BP in the GRIPice core (Gronvold et al 1995) The Saksunarvatn Ash may thus provide a secondimportant widespread time-parallel marker between ice-core marine and terrestrialrecords
Other Icelandic tephras of rhyolitic amacr nity are less well known in terms of theirdistribution and geochemical variation The Hogstorpsmossen Tephra reported fromSweden (Bjorck amp Wastegard 1999) and the L3754 tephra discovered in the FaroeIslands (Dugmore amp Newton 1998) are known from single sites only and so theirpotential for tephrostratigraphy is uncertain at present Furthermore the geochem-ical spectrum of the Hogstorpsmossen Tephra is based on a small dataset with lowanalytical totals
A number of tephras of basaltic composition have originated from Iceland buttheir distributions are largely conshy ned to Iceland or to marine cores collected fromclose to the Iceland coast or in the North Atlantic These include the tephras listedas 1-THOL-1 1-THOL-2 KOL-GS-2 GS-2BAS-1 GS-2BAS-2 GS-2BAS-3 andGS-2BAS-4 in table 1 (Kvamme et al 1989 Bjorck et al 1992 Eirplusmn ksson et al 2000 Haregidason et al 2000) The shy rst two in this list are tholeiitic basaltic tephrasassociated with the VA in a complex series of tephras collectively termed NorthAtlantic Ash Zone 1 (NAAZ1) which has been detected in numerous marine cores
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782 S M Davies and others
from the North Atlantic Initially thought to represent a single eruption analysisof high-resolution sediment sequences from Lake Torfadalsvatn in northern Iceland(Bjorck et al 1992) the Hebridean Shelf near NW Scotland (Austin amp Kroon 1996)the St Kilda Basin (Hunt et al 1995) and the open North Atlantic (Bond et al 2001)has demonstrated that NAAZ1 comprises a series of distinct ashes that probablyreregect separate eruption events 1-THOL-1 is thought to originate from Veidivotn(shy gure 3) while Grimsvotn may have been the source of 1-THOL-2 (Kvamme et al 1989)
KOL-GS-2 is also of tholeiitic basaltic composition but is thought to originatefrom the Kolbeinsey Ridge system (Eirplusmn ksson et al 2000) To date this tephra hasbeen detected in one marine core only within the same record on the North Ice-landic shelf as that from which the correlative of the Borrobol Tephra was alsoreported (Eirplusmn ksson et al 2000) GS-2BAS-1 to GS-2BAS-4 are of uncertain ori-gin but are thought to have been deposited at roughly the same time as KOL-GS-2(ca 134 14C ka BP (Haregidason et al 2000))
The limited distribution of these basaltic tephras a feature that is not unique toIcelandic basaltic material may reregect two factors the relative magnitude of the vol-canic eruptions from which they were derived and the limited aerial transportationof basaltic glass which is denser than rhyolitic material However a rather surpris-ing recent discovery is that of visible basaltic VA in a site on the Isle of Skye inthe Inner Hebrides Scotland (shy gure 5) (Davies et al 2001) All other occurrencesof VA in Scotland are exclusively of rhyolitic material and in micro-tephra formonly (Turney et al 1997 Turney 1998) Clearly basaltic tephra must have beentransported subaerially as far south as Skye and the reason why it has not beendetected at other sites in Scotland is puzzling We suspect that this partly reregectsthe laboratory methods employed to separate glass shards present in low concentra-tion within a micro-tephra layer from the host sediment The technique used is adensity-separation (regotation) procedure (Turney 1998) and as basaltic shards havea specishy c density similar to quartz one of the most abundant minerals in lake sedi-ments of Late Glacial age basaltic material is dimacr cult to detect using this methodThis hypothesis is currently under investigation and alternative detection methodsare being explored including magnetic separation (Mackie et al 2002)
Several other events listed in table 1 that are of probable Icelandic origin includetephras recorded in the GRIP ice core including visible (eg the `Black Featherrsquo)tephras as well as uncertain tephras inferred from distinct Ca peaks (S Johnsen2001 personal communication) No glass shards have yet been detected in the latterbut a volcanic origin is assumed because high Ca peaks are associated with knowntephras in other Greenland ice cores (S Johnsen 2001 personal communication)These are referred to as `unknownrsquo in table 1 No geochemical analyses are availablefrom these horizons so their origin must remain speculative but a possible source isIceland in view of its proximity to the Greenland ice sheet and assumed atmosphericcirculation patterns
(b) Eifel province
There are two prominent tephra events dated to the Termination 1Early Holocenetime-span that originated from the Eifel province the Laacher See Tephra (LST)and the Ulmener Maar Tephra (UMT) Visible occurrences of the LST indicate that
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European tephrochronological framework for Termination 1 783
Vedde Ash
615 625 635 645 655depth (cm)
organic lake mudsHolocene
silty clayGS-1Younger Dryas
organic lake mudsGI-1Alleroslashd
100 microm
(a)
(b)
Figure 5 (a) Photograph of the visible VA layer discovered at Loch Ashik Isle of Skye InnerHebrides Scotland (b) Light microscope photograph showing the rich content of basaltic shards(examples are indicated by the arrows) within this layer (8024 m m size fraction)
this ash was dispersed over much of central Europe (van den Bogaard amp Schmincke1985 Friedrich et al 1999 Litt amp Stebich 1999) The LST is dated by radiocarbonto ca 110 14C ka BP (van den Bogaard amp Schmincke 1985) and to 11 063sect12 14C BP(Friedrich et al 1999) by varve chronology to 1288 varve ka BP (Brauer et al 1999Litt et al 2001) and by ArAr dating to 129 ka cal BP (van den Bogaard 1995) Ithas a phonolitic composition and is thought to have originated from a plinian andphreatomagmatic eruption with the distal ash being carried in three distinct plumesone to the northeast towards Poland one to the west and the third to the southcovering the Jura Mountains and north Italy (van den Bogaard amp Schmincke 1985Juvigne et al 1995 Bossuet et al 1997) This pattern is thought to reregect altitu-dinal variations in the predominant wind direction Sedimentary sequences near thevolcanic source indicate that the LST consists of three main layers which represent
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784 S M Davies and others
dinoterent eruption phases These are grouped together as the Laacher See TephraFormation but the three individual units can be traced within and between a seriesof depositional fans The geochemical data obtained from these three LST layersshow signishy cant variations as reregected in the ternary plots (shy gure 4)
The Early Holocene Ulmener Maar Tephra (UMT) is of rhyolitic composition andappears to be restricted to sites in Germany though this conclusion is also based onrecords of visible tephras only It is dated to ca 956 14C ka BP and to 110 varve ka(Zolitschka et al 1995 Litt et al 2001)
(c) Massif Central province
The Massif Central tephras are mainly of basaltic trachyandesitic compositionwhich is distinct from the other ash provinces (shy gures 3 and 4) and their known dis-tributions are mostly conshy ned to the Massif Central region The ages of the MassifCentral tephras are based on radiocarbon dates obtained from mire and lake sedi-ments which `bracketrsquo the tephras The La Nugsup3ere Tephra with an age of 114 14C kaBP is the oldest Massif Central tephra identishy ed so far within the time-span of inter-est (Etlicher et al 1987 Juvigne et al 1996) The two Godivelle Tephras (5 and 4)are close in age but extensive radiocarbon dating suggests distinct ages of 107and 103 14C ka BP respectively (Juvigne et al 1996) The age of the Puy de DomeTephra is less certain as the estimate is based on only one radiocarbon date froma site in the southern Chaplusmn ne des Puys (table 1) This tephra is thought to havea trachyte composition (Juvigne 1993) although no major element concentrationshave yet been published
The ChopineKilianVasset tephras are thought to be derived from three separateEarly Holocene eruptions although the stratigraphic succession is not known atpresent These trachytic tephras have been radiocarbon dated to ca 854sect150 14C kaBP but are thought to have erupted separately within ca 260 yr (Juvigne et al 1996) This series of tephras is considerably more widespread than the others fromthe region having been identishy ed as far east as the Jura Mountains (Martini amp Duret1965 Martini 1970) Some other ash falls that originated from the Chaplusmn ne des Puysappear to be of local importance only (Vernet et al 1998 Vernet amp Raynal 2001)Geochemical data are currently available for only three of the Massif Central tephrasand so far as is known no attempt has yet been made to identify these tephras inmicro-tephra form
(d ) Italian provinces
The Italian tephras from this period can be assigned to three main volcanic com-plexes the Campanian volcanic shy elds around Naples Etna on Sicily and the AeolianIslands The Campanian complex which includes the Phlegrean Fields Vesuviusand Ischia is mainly trachytic in composition with a geochemical spectrum that isquite distinct from those of the Etna complex and of the Aeolian Islands (shy gure 3)Tephras originating from one or more of these three complexes have been detectedin marine cores from the Tyrrhenian and Adriatic seas as well as other parts of theMediterranean Sea (Keller et al 1978 Paterne et al 1986 1988 1990 Langone etal 1996) and in lake sequences in southern Italy such as Lago Grande di Monticchio(Newton amp Dugmore 1993 Narcisi 1996 Allen et al 1999) and central Italy such asLago Albano near Rome (Calanchi et al 1996) Some work has also been conducted
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European tephrochronological framework for Termination 1 785
in or close to the volcanic source areas in an attempt to establish the full sequenceof volcanic eruptions during the Late Quaternary (see for example Di Vito et al 1999) There are nine Italian tephras reported from marine and lake sequences thatdate from the period between 185 and 80 14C ka BP In all instances the recordsare of visible layers of tephra The ages of some of these are poorly established atpresent with conregicting data obtained from dinoterent sites The ages suggested intable 1 are those favoured in the most recent publications but these may requirere-assessment in the light of future research
The two oldest known tephras in the time-period of interest are the L9 and Green-ish Tephras both recorded as separate features within the annually laminated Lagodi Monticchio maar sequence The lowest of the two L9 is considered to be the cor-relative of the `basalrsquo plinian eruption of Vesuvius (Narcisi 1996) Age estimates ofa palaeosol that underlies the Vesuvius tephra sequence are ca 1617 14C ka BP forthis event (Delibrias et al 1979) L9 has a trachytic composition very similar to theGreenish Tephra (table 1) However L9 which is also a product of Vesuvius is foundstratigraphically below the Greenish Tephra in the Lago di Monticchio core TheGreenish Tephra is dated in the Monticchio sequence to 17 560 varve yr BP (Allenet al 1999) and has a calibrated radiocarbon age estimate of 17 830 sect 300 cal BP(Andronico et al 1995) Both tephras have a dominantly eastwards dispersal basedon the occurrences of visible layers (Santacroce 1987 Narcisi 1996) Both tephrasalso have a trachytic composition and as can be seen from table 1 the reportedgeochemical spectra are very close indeed with the standard deviations overlappingfor almost every major element This could present problems for tephrostratigra-phy where only one of the tephras is evident in a sediment sequence in particularbecause they are so close in age This is a good example of where an analysis oftrace and rare earth elements might be required to make a clear distinction betweentephras with very similar major oxide concentrations
The Y-1 Tephra also termed the Biancavilla Montalto Ignimbrite (Vezzoli 1991)is a product of Etna and has been identishy ed as a visible benmoritic tephra horizonthroughout the central Mediterranean (Paterne et al 1988) including central Italyand the Adriatic Sea (Vezzoli 1991 Narcisi 1993 Calanchi et al 1996) It has anestimated age of ca 140 14C ka BP The Unita dei Tefra Superiori tephra which hasbeen detected as far east as Lago di Monticchio in south-central Italy (Narcisi 1996)is also dated to ca 140 14C ka BP (Alessio et al 1976) but it is thought that thesource of this tephra lies in the Phlegrean Fields No geochemical data are availablefrom the presumed source region|the data reported in table 1 were obtained fromthe Lago di Monticchio record (Narcisi 1996)
The NYT which is equivalent to the C-2 tephra reported from various marinesequences has also been traced throughout central Italy and the Adriatic Sea (Pat-erne et al 1988 Calanchi et al 1996 Di Vito et al 1999) (shy gure 2) In the centralApennines region it formed the parent material for a soil that started to developat the beginning of the Holocene period (Frezzotti amp Narcisi 1996) Also originatingfrom the Campi Flegrei caldera it is dated to ca 120 14C ka BP (Di Vito et al 1999) Published geochemical data based on EDS indicate three dinoterent geochemicalpopulations varying from latite to phonotrachyte in composition (Orsi et al 1992Paterne et al 1988) (table 1) We report in x 4 of this paper on new data obtainedfrom the NYT by WDS and it is the mean of these new data that is included intable 1 Comparisons with the previously published EDS data are provided (table 1)
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786 S M Davies and others
The new data indicate clearly that the NYT originated from the Campanian volcaniccentre
In the interval between the dispersal of the NYT (ca 120 14C ka BP) and 95 14Cka BP there appear to have been as many as 34 eruptions in the Campi Flegrei caldera(Di Vito et al 1999) Of these only one appears to have been detected widely in theregion the Pomici Principali (also termed the Agnano Formation or C-1 tephra inmarine records (Paterne et al 1988) This was the product of the highest magnitudeeruption from this epoch and is dated to between 976 sect 300 and 1032 sect 50 14C kaBP (Delibrias et al 1979 Di Vito et al 1999) or to 122 varve ka BP based on theMonticchio varve chronology (Allen et al 1999) It is trachytic in composition andappears to have had a mainly eastwards dispersal
The Mercato Tephra dated to ca 80 14C ka BP and originally analysed usingEDS has a phonolitic composition and is believed to have been generated by Vesu-vius (Paterne et al 1988) New WDS data obtained from reference samples col-lected from an exposure to the west of Naples support these conclusions (table 1 andAppendix A) The silica content of the WDS analyses are ca 3 lower than thoseobtained using EDS (table 1) which may reregect the fact that the EDS data werenormalized
The only tephra listed in table 1 that is thought to have originated from the AeolianIslands is the Pollara pumice also referred to as the E2 tephra in marine sequences(Paterne et al 1986 1988) The limited geochemical data available so far suggest itto be the only Italian tephra listed in table 1 that is rhyolitic in composition Littlemore is known about this ash which has not been recorded extensively except thatits age is estimated to be ca 130 14C ka BP (Keller 1980)
5 Extending the known distributions of European tephras
Figure 2 summarizes schematically the known distributions of three of the tephrasreferred to in the preceding section the VA the LST and the NYT Following theintroduction of a laboratory method that enables the detection of micro-tephra parti-cles in mineral-rich sediment the VA has been traced to sites that are located muchfarther south (into The Netherlands) and east (as far as St Petersburg) than thedistribution limits based on occurrences of visible layers of the ash As a result con-tinental sequences over a much larger area in northern Europe can now be correlateddirectly with marine and ice-core records using the VA as a time-parallel marker
This suggests therefore that other prominent ash layers such as the LST andNYT should also be detectable over larger tracts of Europe than is presently thecase if suitable sites are examined for the presence of micro-tephra horizons To testthis assertion we examined lake sediment deposits of Last Termination age froma site in the northern Apennines in order to establish whether the NYT could bedetected in micro-tephra form The site selected Prato Spilla `Crsquo lies well to thenorth of the localities in central and southern Italy and in the Adriatic Sea fromwhich visible records of the NYT have been reported Prato Spilla `Crsquo lies at an alti-tude of ca 1350 m in the Appennino Parmense ca 60 km south of Parma and 15 kmeast of Pontremoli The site contains a continuous sediment sequence spanning theLast Termination and most of the Holocene Detailed pollen and coleopteran strati-graphical records which have been radiocarbon dated have been published for thissite (Lowe 1992 Ponel amp Lowe 1992 Lowe amp Watson 1993)
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Figure 6 Light microscope photograph of an NYT glass shard from Prato Spilla Crsquosequence assigned on geochemical grounds to the NYT
The methods adopted for sub-sampling of the Prato Spilla `Crsquo sequence for thequantishy cation of glass shard concentrations and for subsequent electron microprobeanalysis of selected glass shards followed those described elsewhere (Turney 1998)In summary contiguous samples of 1 cm stratigraphic interval were extracted fromthe sequence to establish presenceabsence of glass shards Each of the 1 cm3 blocksin which tephra particles was detected was then examined with more care andshard concentrations were quantishy ed for each sub-sample Micro-tephra particleswere detected in shy ve samples (shy gure 6) but were predominantly clustered around500 cm in the part of the sequence assigned on pollen-stratigraphic grounds to theLate Glacial Interstadial or the `Allerfrac12drsquo|indeed the part of the succession in whichthe NYT would be expected to occur Peak concentrations of micro-tephra particlesreach 225 shards cmiexcl3 and are conshy ned to a single 1 cm thick sample in the sequencewhich probably represents the time of maximum deposition of the ash
Electron microprobe measurements based on WDS were obtained from the surfacesof 21 separate glass shards extracted from the sample with peak shard concentrations(Appendix A) Since only EDS measurements were available for the NYT prior to thepresent study we also obtained WDS measurements from 17 shards extracted fromthe visible layer of NYT that is exposed on Procida Island which lies in the type-locality for the NYT close to the city of Naples (Appendix A) The results providenot only a more comprehensive geochemical dataset for the NYT than was previ-ously available but also a consistent basis for comparison with the Prato Spilla `Crsquodataset All of the WDS data reported here (Appendix A) were measured at the samelaboratory (Tephrochronology Analytical Unit University of Edinburgh) using thesame sample pretreatment and preparation protocol The WDS results for the NYTdinoter to a minor degree from the EDS results (table 1 and Appendix A) especiallywith respect to the amounts of silica aluminium and calcium measured The EDS
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788 S M Davies and others
4 8FeO ()
TiO
2 (
) Neapolitan Yellow Tuff(Procida)Neapolitan Yellow Tuff(Prato Spilla lsquoCrsquo)
0
1
2
3
40 50 60 70
MgO
(
)
SiO2 ()
K2O
(
)
40 50 60 70
0
04
08
4
8
12
SiO2 ()
(a)(b)
(c)
Figure 7 Bi-plots of SiO2 K2 O SiO2 MgO and FeOTiO2 for the WDS analyses obtainedfrom glass shards of the NYT from Procida (Naples) and Prato Spilla Crsquo Means and standarddeviations are shown
results show a higher degree of statistical scatter than the WDS measurements whichmay reregect the fact that the data were normalized combined with the inreguence ofvariation in water content between shards
There is a very close correspondence between the WDS data for the Prato Spilla `Crsquomicro-tephra shards and those obtained from the type-material near Naples (shy g-ure 7) The geochemical data strongly suggest therefore that the NYT is representedat the Prato Spilla `Crsquo site by a discrete layer of micro-tephra particles This conclu-sion is compatible with the pollen-stratigraphic data from the site and accords withage estimates for the NYT (ca 120 14C ka BP) obtained from other sites (Paterneet al 1990)
These results encourage us to believe that many if not all of the tephras listedin table 1 will be detectable over much larger tracts of Europe than is presently thecase if appropriate research is undertaken to detect layers of micro-tephra particlesin selected sites The authors are presently engaged in a major continent-wide pro-gramme of research in collaboration with a number of European research groupsdesigned to test this hypothesis The focus in this research is on those parts of Europewhere we expect to shy nd overlapping `apronsrsquo of tephra deposition originating fromthe Italian Eifel Massif Central and Icelandic provinces For example a number ofsites in parts of southern France northern Italy and perhaps western Switzerlandmay have received inreguxes of micro-tephra originating from the Italian and Eifelprovinces and perhaps also from the Massif Central Sites in parts of Germany Den-mark and southern Sweden for example may in turn have received tephra depositsfrom both of the Icelandic and Eifel provinces If this proves to be the case then thestage will be set for the construction of a tephrostratigraphical framework for Europewhich will enable Last Termination sequences to be correlated on a continent-widebasis using micro- and visible tephra layers as time-parallel stratigraphic markersFurthermore there is also the possibility that other tephras remain to be discovered
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European tephrochronological framework for Termination 1 789
those which either because of the magnitude or nature of some volcanic eruptionswere distributed over parts of Europe in micro-tephra form only
6 European tephrostratigraphy and the chronology of eventsduring the Last Termination and Early Holocene
One of the crucial issues in Late Quaternary palaeoenvironmental research thatremains to be resolved is the degree to which climatic events inferred from oceanicterrestrial and ice-core records were synchronous during the Last Termination andEarly Holocene If the ice-core records provide realistic estimates of the rates anddurations of climatic events during this period then comparisons between individ-ual records have to be enotected with at least a decadal precision The problem thispresents and the role that tephrostratigraphy can play in resolving some of thedimacr culties involved are put into perspective in shy gure 8
Figure 8 shows some of the data used to calibrate radiocarbon dates (the LakeSuigetsu and Cariaco Basin datasets) plotted against the GRIP ss08c ice-core recordof macr 18O variations The latter has been selected by the INTIMATE group as an arbi-trary and temporary standard for this period and used to deshy ne an event stratig-raphy scheme (shy gure 1) for the Last Termination (see Bjorck et al 1998 Walker etal 2001) As has been alluded to in earlier sections of this paper the uncertaintiesassociated with all of the dating methods currently employed preclude precise com-parisons of ice-core marine and terrestrial records Oceanic and terrestrial recordsmostly rely upon radiocarbon dating locally supplemented in a few cases by varvechronology Imprecisions in radiocarbon dates can arise through site-specishy c fac-tors (eg hard-water or mineral carbon errors in freshwater sequences and reservoirerrors in marine sequences) sample selection laboratory measurements of 14C activ-ity and other factors (Lowe amp Walker 2000) Further imprecision may be introducedby the calibration of radiocarbon dates since the uncertainties in the dataset usedto calibrate pre-Holocene radiocarbon dates INTCAL98 are far higher than forthe Holocene which is based on dendro-calibration (Stuiver et al 1998) There arealso uncertainties anotecting varve chronologies while the ss08c ice-core chronologyfor the Last Termination dinoters signishy cantly from the GISP2 record and indeedfrom other models of the GRIP record (Lowe et al 2001) Published comparisonsbetween ice-core marine and terrestrial records for the Last Termination seldom takeinto account the true magnitude of the dating uncertainties involved and frequentlyemploy circular reasoning
Figure 8 shows the positions on the radiocarbon time-scale of 20 of the tephrasdiscussed earlier in this paper these being the ones for which reasonably conshy dentradiocarbon age estimates can be made (though these will be subject to revised esti-mates in the future) A high number of these occur in the period 14080 14C kaBP but we conshy dently anticipate the discovery in the future of additional tephras(perhaps in micro-tephra form only) which will date to the period 185140 14C kaBP Tephras detected in the GRIP ice core over the same time-interval are plottedon the calendar time-scale in shy gure 8 By providing key `time-linesrsquo between recordstephrostratigraphy can help to resolve some of the dating uncertainties referredto earlier by for example enabling direct comparisons of discrepant age estimatesobtained using dinoterent methods (cf Litt et al 2001) It can also provide estimatesof the magnitudes of the reservoir errors that anotected various marine sectors at dif-
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790 S M Davies and others
-44
-40
-36
-32
cale
ndar
yea
rs B
P
8000
9000
10 0
00
11 0
00
12 0
00
13 0
00
14 0
00
15 0
00
16 0
00
17 0
00
18 0
00
14C age (BP)
VA
SA
Un
Un
Un
Un
Un
BF
Hol
ocen
eG
S-1
GI-
1aG
I-1b
GI-
1cG
I-1d
GI-
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S-2
aG
S-2
bG
S-
2c
Bor
robo
l
La
Nug
egravere
Laa
cher
See
God
ivel
le 5
amp I
-TH
OL
-2
Puy
de D
ocircme
I-T
HO
L-1
Saks
unar
vatn
Houmlg
stor
psm
osse
nU
lmen
er M
aar
amp L
3574
radiocarbon dated European tephra horizons
Cho
pine
Kili
an V
asse
tM
erca
to
God
ivel
le 4
Pom
ici P
rinc
ipal
i amp V
edde
Polla
ra p
umic
eK
OL
-GS-
2 amp
GS
-2B
AS-
12
3
GS
-2B
AS-
4 U
nita
dei
Tef
raSu
peri
ori amp
laye
r Y
-1
Gre
enis
h
L9
20 0
0018
000
16 0
0014
000
12 0
0010
000
-44
-40
-36
-32
800
600
400
200 0
GISP2 volcanicsulphate conc (ppb)
1000
Nea
polit
an Y
ello
w T
uff
GISP2 18O (permil) dGRIP 18O (permil) d
Figure 8 For description see opposite
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European tephrochronological framework for Termination 1 791
ferent times through a comparison of radiocarbon dates obtained from marine andterrestrial horizons in which the same tephra has been detected (see for exampleAustin et al 1995 Bondevik et al 2001 Haregidason et al 2000) Tephrostratigraphymay provide an independent test of suggestions that some of the climatic changesduring the Last Termination were time-transgressive as illustrated for some appar-ently contrasting climatic trends in Iceland Britain and NW Russia (Lowe 2001) Ofparticular importance as far as establishing `leadsrsquo and `lagsrsquo in climatic changes isconcerned are the tephra records from the Greenland ice cores The discovery of theVedde and Saksunarvatn ashes in the GRIP record (Gronvold et al 1995) alreadyprovides a basis for making direct comparisons between marine terrestrial and ice-core records It is a matter of some urgency that the incidence of tephra depositsin the Greenland ice cores be more fully explored in the hope that this will lead tothe recognition of additional time-parallel links between the ice-core records on theone hand and oceanic and terrestrial records on the other An investigation of thenew NordGRIP record for this purpose is currently in progress (S M Davies 2002unpublished data)
Finally a fuller and more reshy ned tephrostratigraphical scheme for Europe will alsohave other applications It will provide an important database for those investigatingthe timing and frequency of volcanic eruptions in Europe during the past 20 000 yror so as well as of the geochemical evolution of the dinoterent volcanic centres overthat period A fuller record of the distribution of micro-tephras may also provideinformation on atmospheric circulation patterns during the dispersal and depositionperiods as well as on the nature and altitude of the eruption columns which mayin turn provide inferences about magma viscosity
This paper is a contribution to the INTIMATE project of the INQUA Palaeoclimate Com-mission and the work is supported by a Leverhulme Trust Research project (grant allocationnumber F07537C) entitled Testing hypotheses of rapid climate change using tephrochronol-ogyrsquo SMDrsquo s contribution was completed during possession of a NERC PhD studentship(GT 0499ES162) We are extremely grateful to Dr Peter G Hill for his assistance withthe EPMA analyses at the Tephrochronology Analytical Unit University of Edinburgh We alsothank Dr G Mastrolorenzo (Vesuvius Observatory) and Miss G Swindle for assistance duringthe macreld investigations in Naples Thanks are also expressed to two anonymous reviewers forcomments on an earlier draft
Appendix A
Table 2 shows the major oxide concentrations of NYT glass shards from Procidaand Prato Spilla `Crsquo and of the Mercato Tephra from the Naples area (see x 4 forsite context) All oxides are shown as weight and total iron is expressed as FeO
Figure 8 Radiocarbon calibration curve for Termination 1 and the Early Holocene compared with theGRIP macr 18 O event stratigraphy the GRIP ss08c and GISP2 macr 18 O records (wwwngdcnoaagov) andknown tephra horizons from this period The shaded areas represent the cooler climatic episodes andare labelled with the Greenland stratotype terminology (Bjorck et al 1998) Where radiocarbon agesare reported in table 1 as a range the mean is given here Abbreviations for GRIP horizons are asfollows Un unknown (approximate positions are given (S Johnsen 2001 personal communication))SA Saksunarvatn Ash VA Vedde Ash BF Black Feather Sulphate concentrations from the GISP2record are also shown (Zielinski et al 1996) Open circles denote radiocarbon calibration data fromLake Suigetsu (Kitagawa amp van der Plicht 2000) Filled circles denote radiocarbon calibration data fromCariaco Basin assuming a marine reservoir age of 420 14 C yr (Hughen et al 1998)
Phil Trans R Soc Lond A (2002)
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792 S M Davies and others
Tab
le2
Majo
roxi
de
con
cen
trati
on
sof
NY
Tgl
ass
shard
sfr
om
Pro
cida
an
dP
rato
Spil
laC
rsquoan
dof
the
Mer
cato
Tep
hra
from
the
Naple
sare
a(s
eex4
for
site
con
text
)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
roci
da)
1584
204
0177
634
201
106
828
635
197
5969
1W
DS
2598
603
9178
027
101
204
924
244
583
4965
8W
DS
3586
604
5173
631
100
805
924
342
183
0951
9W
DS
4583
903
9177
933
000
906
924
540
486
9958
3W
DS
5605
106
8179
126
901
204
923
243
086
1976
4W
DS
6591
704
5177
332
801
006
425
740
887
8968
0W
DS
7581
804
1178
031
501
107
125
640
086
9956
1W
DS
8589
504
2179
533
701
506
926
740
987
5970
4W
DS
9592
003
9178
135
101
007
026
443
585
7972
7W
DS
10
591
404
2174
631
601
105
723
442
482
6957
0W
DS
11
593
403
6177
131
301
506
726
439
188
5967
6W
DS
12
588
103
8176
128
100
505
525
141
583
4952
1W
DS
13
577
003
8176
533
500
807
228
140
384
8952
0W
DS
14
586
004
7179
735
300
706
827
842
984
6968
5W
DS
15
588
104
2180
629
400
505
924
937
993
0964
5W
DS
16
579
603
9178
536
501
308
228
836
087
1959
9W
DS
17
580
103
9177
631
500
907
327
039
488
9956
6W
DS
mea
n588
104
2177
631
901
006
525
940
686
9962
8
sd
(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(07
8)
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 793
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
rato
Spil
laC
rsquo)
1552
105
4177
247
401
914
38
735
578
9951
1W
DS
2557
305
7179
845
701
512
640
136
581
5960
6W
DS
3595
004
4173
724
302
003
117
652
877
8950
7W
DS
4575
704
2179
433
001
406
627
043
083
6953
7W
DS
5599
904
0178
826
401
304
421
841
688
4966
5W
DS
6591
103
8177
826
601
105
022
443
888
8960
2W
DS
7565
304
5180
939
501
410
532
535
791
8962
1W
DS
8597
606
9180
826
501
604
821
546
684
6970
7W
DS
9571
805
6179
939
801
109
932
240
883
6964
7W
DS
10
588
603
7176
527
601
104
721
042
487
7953
3W
DS
11
559
404
9180
544
501
812
339
435
878
6957
2W
DS
12
594
704
0181
328
301
705
522
144
785
6967
9W
DS
13
611
103
7187
016
900
802
419
938
195
9975
8W
DS
14
599
204
4181
128
601
404
620
844
986
6971
6W
DS
15
601
204
4177
328
302
004
722
446
385
5972
1W
DS
16
595
104
5176
428
801
504
722
744
884
3962
8W
DS
17
603
704
1177
825
101
503
520
348
181
2965
3W
DS
18
558
704
5179
647
401
813
139
836
879
0960
7W
DS
19
589
602
8178
830
901
606
622
436
091
8960
5W
DS
20
553
606
3178
647
401
913
840
136
978
0956
6W
DS
21
579
004
0175
739
000
708
328
338
286
7959
9W
DS
mea
n582
804
6179
033
401
507
427
341
484
8962
1
sd
(1
87)
(01
0)
(02
7)
(09
2)
(00
4)
(03
9)
(08
0)
(04
9)
(05
0)
(07
0)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
794 S M Davies and others
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)
1575
202
7194
219
701
101
016
374
766
9951
8W
DS
2575
802
9194
523
902
201
520
273
564
5959
0W
DS
3574
301
4205
219
101
100
416
481
266
1965
2W
DS
4575
500
7206
018
002
000
415
181
669
3968
6W
DS
5580
000
9208
018
601
300
515
883
367
1975
5W
DS
6571
001
0206
016
101
600
515
078
967
1957
2W
DS
7577
501
1201
117
101
500
620
675
655
4950
5W
DS
8573
700
9212
717
101
900
815
187
564
2973
9W
DS
9580
301
3208
715
801
400
824
81
754
1968
1W
DS
10
574
400
6211
18
402
00
516
480
567
8971
6W
DS
11
577
200
7214
212
501
200
829
879
247
962
6W
DS
12
572
200
9211
217
301
501
15
980
465
9966
3W
DS
13
571
800
7210
417
402
201
16
184
467
2971
2W
DS
14
567
300
9208
916
901
400
917
383
262
5959
3W
DS
15
568
600
8205
918
202
101
414
682
666
6960
8W
DS
16
572
501
1211
318
202
01
215
884
364
5970
9W
DS
17
572
901
2212
916
502
101
215
883
667
2973
4W
DS
18
573
01
4211
716
301
801
416
83
365
5970
4W
DS
19
569
201
1207
418
602
101
414
982
964
961
6W
DS
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
3)
(04
2)
(01
3)
(00
1)
(00
2)
(01
)(0
39)
(01
1)
(02
5)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
References
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Delibrias G Di Paola G M Rosi M amp Santacroce R 1979 La storia eruttiva del complessovulcanico Somma Vesuvio ricostruita dalle successini piroclastiche del Monte Somma RendSoc It Mineral Petrolog 35 411438
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Hoek W Z amp Bohncke S J P 2001 Oxygen isotope wiggle matching as a tool for synchronisingice-core and terrestrial records over Termination 1 Quat Sci Rev 20 12511264
Hughen K A Overpeck J T Peterson L C amp Trumbore S 1996 Rapid climate changes inthe tropical Atlantic region during the last deglaciation Nature 380 5153
Hughen K A Overpeck J T amp Lehman J 1998 A new 14 C calibration data set for the LastDeglaciation Radiocarbon 39 483494
Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
Hunt J B amp Hill P G 1996 An inter-laboratory comparison of the electron probe microanalysisof glass geochemistry Quat Int 3436 229241
Hunt J B amp Hill P G 2001 Tephrological implications of beam sizesample size ereg ects inelectron microprobe analysis of glass shards J Quat Sci 16 105117
Hunt J B Fannin N G T Hill P G amp Peacock J D 1995 The tephrochronology andradiocarbon dating of North Atlantic Late Quaternary sediments an example from the StKilda Basin In The tectonics sedimentation and palaeoceanography of the North Atlanticregion (ed R A Scrutton M S Stoker G B Shimmield amp A W Tudhope) vol 90pp 227248 Geological Society of London Special Publication
Hunt J B Clift P D Lacasse C Vallier T L amp Werner R 1998 Standardisation ofelectron probe microanalysis of glass geochemistry In Proc ODP Scientimacrc Results vol 152pp 8591 College Station TX Ocean Drilling Program
Jakobsson S P 1979 Outline of the petrology of Iceland Jokull 29 5773
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Juvignparae E amp Gewelt M 1987 La Narse drsquo Ampoix comme tparaephrostratotype dans la Chasup3 ne desPuys mparaeridionale (France) Bull Ass Fr Etud Quat 29 3749
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Larsen G 2000 Holocene volcanism in Iceland and tephrochronology as a tool in volcanologyIn Iceland 2000 modern processes and past environments Keele University UK
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 799
Litt T amp Stebich M 1999 Bio- and chronostratigraphy of the Lateglacial in the Eifel regionGermany Quat Int 61 516
Litt T Brauer A Goslar T Merkt J Balaga K Muller H Ralska-Jasiewiczowa MStebich M amp Negendank J F W 2001 Correlation and synchronisation of Lateglacialcontinental sequences in northern Central Europe based on annually laminated lacustrinesediments Quat Sci Rev 20 12331249
Long D amp Morton A C 1987 An ash fall within the Loch Lomond stadial J Quat Sci 297101
Lotter A F Eicher U Siegenthaler U amp Birks H J B 1992 Lateglacial climatic oscillationsas recorded in Swiss lake sediments J Quat Sci 7 187204
Lowe J J 1992 Lateglacial and Early Holocene lake sediments from the Northern ApenninesItaly|pollen stratigraphy and radiocarbon dating Boreas 21 193208
Lowe J J 2001 Abrupt climatic changes in Europe during the last glacialinterglacial tran-sition the potential for testing hypotheses on the synchroneity of climatic events usingtephrochronology Global Planet Change 603 7384
Lowe J J amp Turney C S M 1997 Vedde Ash layer discovered in a small lake basin on theScottish mainland J Geol Soc Lond 154 605612
Lowe J J amp Walker M J C 2000 Radiocarbon dating the last glacialinterglacial transition(ca 14914 C ka BP) in terrestrial and marine records the need for new quality assuranceprotocols Radiocarbon 42 5368
Lowe J J amp Watson C 1993 Lateglacial and Early Holocene pollen stratigraphy of the northernApennines Italy Quat Sci Rev 12 727738
Lowe J J Birks H H Brooks S J Coope G R Harkness D D Mayle F E SheldrickC Turney C S M amp Walker M J C 1999 The chronology of palaeoenvironmental changesduring the Last GlacialHolocene transition towards an event stratigraphy for the BritishIsles J Geol Soc Lond 156 397410
Lowe J J Hoek W Z amp INTIMATE group 2001 Inter-regional correlation of palaeoclimaticrecords for the Last GlacialInterglacial transition a protocol for improved precision recom-mended by the INTIMATE project group Quat Sci Rev 20 11751187
Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
Mangerud J Lie S E Furnes H Kristiansen I L amp Liquest mo L 1984 A Younger Dryas ashbed in western Norway and its possible correlation with tephra beds from the Norwegian Seaand North Atlantic Quat Res 21 85104
Mangerud J Furnes H amp Jparaohansen J 1986 A 9000 year-old ash bed on the Faroe IslandsQuat Res 26 262265
Martini J 1970 Recherche de retombparaees volcaniques dans le sud-est de la France et la Suisseoccidentale Arch Sci 23 641674
Martini J amp Duret J J 1965 Note preliminaire sur la presence drsquo un niveau de cendres vol-caniques dans des sparaediments post-glaciaires des environs de Genmicroeve Arch Sci 18 587588
Mayewski P A Meeker L D Twickler M S Whitlow S Yang Q Lyons W B amp Pren-tice M 1997 Major features and forcing of high latitudes Northern Hemisphere atmosphericcirculation using a 110 000 year long glaciochemical series J Geophys Res 102 345365
Merkt J Muller H Knabe W Muller P amp Weiser T 1993 The Early Holocene Saksunarvatntephra found in lake sediments in NW Germany Boreas 22 93100
Narcisi B 1993 Segnalazione di un livello piroclastico di provenienza etnea nellrsquo area del Fucino(Italia Centrale) Quaternario 6 8792
Narcisi B 1996 Tephrochronology of a Late Quaternary lacustrine record from the Monticchiomaar (Vulture volcano southern Italy) Quat Sci Rev 15 155165
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Newton A J amp Dugmore A J 1993 Tephrochronology of Core C from Lago Grande di Mon-ticchio In Paleolimnology of European Maar Lakes (ed J F W Negendank amp B Zolitschka)Lecture Notes in Earth Science vol 49 333348 Springer
Oldmacreld F Appleby P G amp Thompson R 1980 Palaeoecological studies of lakes in theHighlands of Papua New Guinea J Ecol 68 457477
Orsi G Drsquo Antonio M de Vita S amp Gallo G 1992 The Neapolitan Yellow Tureg a large mag-nitude trachytic phreatoplinian eruption eruptive dynamics magma withdrawal and calderacollapse J Volcanol Geotherm Res 53 275287
Paterne M Guichard F Labeyrie J Gillot P Y amp Duplessy J C 1986 Tyrrhenian Seatephrochronology of the oxygen isotope record for the past 60 000 years Mar Geol 72259285
Paterne M Guichard F amp Labeyrie J 1988 Explosive activity of the south Italian volca-noes during the past 80 000 years as determined by marine tephrochronology J VolcanolGeotherm Res 34 153172
Paterne M Labeyrie J Guichard F Mazaud A amp Maitre F 1990 Fluctuations of the Cam-panian explosive volcanic activity (south Italy) during the past 190 000 years as determinedby marine tephrochronology Earth Planet Sci Lett 98 166174
Pawse A Beske-Diehl S amp Marshall S A 1998 Use of magnetic hysteresis properties andelectron spin resonance spectroscopy for the identimacrcation of volcanic ash a preliminary studyGeophys J Int 132 712720
Pearce N J G Westgate J A amp Perkins W T 1996 Developments in the analysis of singleglass shards in volcanic deposits by laser ablation ICP-MS quantitative and single internalstandard multi-element methods Quat Int 3436 213227
Pearce N J G Westgate J A Perkins W T Eastwood W J amp Shane P 1999 Theapplication of laser ablation ICP-MS to the analysis of volcanic glass shards from tephradeposits bulk glass and single shard analysis Global Planet Change 21 151171
Pilcher J R amp Hall V A 1992 Towards a tephrochronology for the Holocene of the north ofIreland Holocene 2 255259
Ponel P amp Lowe J J 1992 Coleopteran pollen and radiocarbon evidence from the Prato Spillarsquo Drsquo succession N Italy C R Acad Sci Paris Sparaer II 315 14251431
Rose N L Golding P N E amp Battarbee R W 1996 Selective concentration and enumerationof tephra shards from lake sediment cores Holocene 6 243246
Ruddiman W F amp Glover L K 1972 Vertical mixing of ice rafted volcanic ash in NorthAtlantic sediments Geol Soc Am Bull 83 28172836
Ruddiman W amp McIntyre A 1981 The North Atlantic Ocean during the last deglaciationPalaeogeogr Palaeoclimatol Palaeoecol 35 145214
Santacroce R 1987 Somma Vesuvius Quad Ric Sci 114 252
Sarna-Wojcicki A 2000 Tephrochronology In Quaternary geochronology methods and applica-tions (ed J S Noller J M Sowers amp W R Lettis) AGU Reference shelf vol 4 pp 357377Washington DC American Geophysical Union
Sejrup H P Sjiquest holm J Furnes H Beyer I Eide L Jansen E amp Mangerud J 1989Quaternary tephrochronology on the Iceland Plateau north of Iceland J Quat Sci 4 109114
Sikes E L Samson C R Guilderson T P amp Howard W R 2000 Old radiocarbon agesin the southwest Pacimacrc Ocean during the last glacial period and deglaciation Nature 405555558
Stein R Nam S-I Grobe H amp Hubbersten H 1996 Late Quaternary glacial history andshort term ice rafted debris deg uctuations along the East Greenland continental marine In LateQuaternary palaeoceanography of the North Atlantic margins (ed J T Andrews W E NAustin H Bergsten amp A E Jennings) pp 135151 Geological Society London SpecialPublication
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on September 20 2011rstaroyalsocietypublishingorgDownloaded from
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Stuiver M amp Grootes P M 2000 GISP2 oxygen isotope ratios Quat Res 53 277284
Stuiver M Reimer P J Bard E Beck J W Burr G S Hughen K A Kromer BMcCormac G Van der Plicht J amp Spurk M 1998 INTCAL 98 radiocarbon age calibration24 0000 cal BP Radiocarbon 40 10411083
Sweatman T R amp Long J V P 1969 Quantitative electron microprobe analysis of rock formingminerals J Petrol 7 332379
Turney C S M 1998 Extraction of rhyolitic ash from minerogenic lake sediments J Paleolim-nol 19 199206
Turney C S M amp Lowe J J 2001 Tephrochronology In Tracking environmental changes inlake sediments physical and chemical techniques (ed W M Last amp J P Smol) DordrechtKluwer Academic
Turney C S M Harkness D D amp Lowe J J 1997 The use of microtephra horizons tocorrelate Lateglacial lake sediments successions in Scotland J Quat Sci 12 525531
Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
van den Bogaard P amp Schmincke H 1985 A widespread isochronous Late Quaternary tephralayer in central and northern Europe Geol Soc Am Bull 96 15541571
van den Bogaard B Dordeg er W Sandgren P amp Schmincke H-U 1994 Correlating theHolocene records Icelandic tephra found in Schleswig-Holstein (northern Germany) Natur-wissenschaften 81 554556
Vernet G amp Raynal J-P 2001 Tephrostratigraphy of the Limagne revisited Implications forLateglacial and Holocene Prehistory In Tephras chronology archaeology (ed E Juvignparae ampJ-P Raynal) pp 111116 Dossiers de lrsquo ArchparaeoLogis no 1 France
Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
Vezzoli L 1991 Tephra layers in Bannock Basin (eastern Mediterranean) Mar Geol 1002134
von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
Walker M J C Bjorck S Lowe J J Cwynar L C Johnsen S Knudsen K-L WohlfarthB amp INTIMATE Group 1999 Isotopic events in the GRIP ice core a stratotype for the LatePleistocene Quat Sci Rev 18 11431150
Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
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802 S M Davies and others
Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
101098rsta20010964
Towards a European tephrochronologicalframework for Termination 1 and
the Early Holocene
By Siwan M Davies Nicholas P BranchJ John Low e a n d Chris S M Turneyy
Centre for Quaternary Research Department of GeographyRoyal Holloway University of London EghamSurrey TW20 0EX UK (smdaviesrhulacuk)
Published online 19 March 2002
The record of deposition of tephras in Europe and the North Atlantic during theperiod 18580 14C ka BP (the Last Termination and Early Holocene) is reviewedAltogether 34 tephras originating from four main volcanic provinces (Iceland theEifel district the Massif Central and Italy) have been identishy ed so far in geologicalsequences spanning this time-interval Most of the records have been based untilvery recently on observations of visible layers of tephras Here we report on thepotential for extending the areas over which some of the tephras can be traced bythe search for layers of micro-tephra which are not visible to the naked eye andon the use of geochemical methods to correlate them with known tephra horizonsThis approach has greatly extended the area in Northern Europe over which theVedde Ash can be traced The same potential exists in southern Europe which isdemonstrated for the shy rst time by the discovery of a distinct layer of micro-tephraof the Neapolitan Yellow Tunot in a site in the Northern Apennines in Italy far tothe north of the occurrences of visible records of this tephra The paper closes byconsidering the potential for developing a robust European tephrostratigraphy tounderpin the chronology of records of the Last Termination and Early Holocenethereby promoting a better understanding of the nature timing and environmentalenotects of the abrupt climatic changes that characterized this period
Keywords non-visible tephra layers electron microprobeabrupt climate change Late Glacial period
1 Introduction
A series of abrupt high-amplitude climatic changes characterizes Termination 1 andthe Early Holocene (shy gure 1) especially during the transition between the last coldstage and the present interglacial usually termed the `Late Glacialrsquo (ca 1390 14C kaBP or 14790 GRIP ice-core ka BP) (due to signishy cant dinoterences in the time-scalesderived from ice-core radiocarbon and varve dating the basis of all age estimatesquoted in this paper are specishy ed thus 14C = radiocarbon years (uncalibrated)
y Present address School of Archaeology and Palaeoecology Queenrsquo s University Belfast BelfastBT7 1NN UK
Phil Trans R Soc Lond A (2002) 360 767802
767
creg 2002 The Royal Society
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768 S M Davies and others
- 42 - 40 - 38 - 36 - 34
Holocene
Greenland stadial 1
Greenland interstadial 1
Greenland stadial 2
GI-1aGI-1b
GI-1c
GI-1d
GI-1e
GR
IP ic
e co
re (
year
s B
P)
18O permil (SMOW)d
11 000
12 000
13 000
14 000
15 000
16 000
17 000
18 000
19 000
20 000
Figure 1 The Greenland event stratigraphy scheme based on the macr 18 O record (SMOW) andstratigraphic terminology for the Last Termination and Early Holocene (after Bjorck et al 1998 Walker et al 1999)
cal = calibrated radiocarbon years GRIP ice-core yrs refers to the GRIP ss08c time-scale) (Walker 1995 Lowe et al 1999) The most pronounced features in the climaticrecords for this period are abrupt warmings at the start of Greenland Interstadial 1(the GI-1e thermal maximum) and at the onset of the Holocene and a short periodof severely cold conditions corresponding to the `Younger Dryasrsquo stadial or theGS-1 event (Greenland Stadial 1) in the proposed Greenland stratotype sequence(see Bjorck et al 1998 Walker et al 1999)
A broadly similar pattern of climatic changes has been inferred from records of theLast TerminationEarly Holocene obtained from widely scattered localities through-out the North Atlantic region and which have been derived from a wide range ofproxy data These include for example macr 18O and snow-accumulation records fromthe Greenland ice cores (Alley et al 1993 Dansgaard et al 1993) fossil beetle andchironomid assemblages from the British Isles (Atkinson et al 1987 Coope et al 1998 Lowe et al 1999 Brooks et al 1997) greyscale variations reregecting ratesof sediment accumulation in laminated deposits of the tropical Atlantic (Hughenet al 1996 1998) and macr 18O variations in Swiss German and Dutch lake sediment
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 769
sequences (Lotter et al 1992 von Grafenstein et al 1999 Hoek amp Bohncke 2001)A question that is pivotal to understanding the climate-driving mechanisms in theNorth Atlantic region is whether the abrupt events as well as the environmentalresponses to them were synchronous within the continental marine and polar icerealms or whether there were signishy cant `leadsrsquo and `lagsrsquo between them
The Greenland ice-core records suggest that some of the climatic transitions duringthe Last Termination took place within only a few decades (Mayewski et al 1997)while the short-lived cooling events within GI-1 lasted some 100300 ice-core yr atmost Determining the precise timing and duration of equivalent events representedin the ocean and continental records is extremely dimacr cult at present because of theuncertainties associated with the dating methods employed Age estimates obtainedusing the most widely adopted method radiocarbon dating have error ranges at 1frac14that are rarely better than sect50 14C yr and which frequently exceed sect100 14C yror more Interpretations of radiocarbon ages are complicated still further by uncer-tain calibration procedures and the distorting inreguences of radiocarbon `plateauxrsquo|episodes of near-constant radiocarbon age (see Lowe amp Walker 2000) Radiocarbondates obtained from marine sequences of Last Termination age are particularly sus-pect due to the inreguences of marine reservoir errors (Sikes et al 2000 Waelbroecket al 2001) There are equally wide uncertainties associated with other methodssuch as varve counting while the ice-core records themselves in the segment ofthe records that span the Last Termination may have systematic errors exceeding200 years (Stuiver amp Grootes 2000) A further problem is that some of the climatechanges at this time may have been time-transgressive (Coope et al 1998 Witteet al 1998) signishy cantly undermining the use of conventional approaches such asclimatostratigraphy and biostratigraphy for correlating the records It is evidentthen that conventional approaches to the dating and correlation of events duringthe Last Termination are inadequate for testing the hypothesis that abrupt climaticchanges during this period were truly synchronous at the continental or global scale
The problems of dating and correlating sequences that span the Last Terminationhave been reviewed through a series of workshops organized by the INTIMATE group(INTegration of Ice core MArine and TErrestrial records of the Last Termination|a core programme of the International Quaternary Union (INQUA) Palaeocli-mate Commission (httpwwwgeoguunlfgpalaeoclimateintimate)) (Bjorck etal 2001) which has recommended a set of proposals for improved precision in thefuture (Lowe et al 2001) Central to these proposals is the application of correlationtools that can provide independent tests of the age estimates and correlations basedon radiocarbon dating varve chronology and ice-layer counting
One of the approaches recommended by the INTIMATE and COTAV (INQUACommission on Tephrochronology and Volcanism) groups is tephrochronology forthere is growing evidence to suggest that this technique has the potential to resolvesome of the pressing geochronological issues while some tephras may be detectableover much wider geographical areas than appreciated hitherto Here we examine thepotential for developing a tephrostratigraphical and tephrochronological frameworkfor Europe for the period 18580 14C ka BP (encompassing the Last Terminationand the Early Holocene) It is argued that such a scheme will provide a rigorousunderpinning structure for geochronological models for this period and hence leadto improved understanding of the mechanisms timing and environmental enotects ofabrupt climatic changes during the Last Termination
Phil Trans R Soc Lond A (2002)
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770 S M Davies and others
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Ref
eren
ces
1
this
stu
dy
2
Pate
rne
etal
(1988)
3
Narc
isi
(1996)
4
All
enet
al
(1999)
5
An
dro
nic
oet
al
(1995)
6
Ju
vig
nparae
et
al
(1996)
7
Bir
ks
et
al
(1996)
8
Bjo
rck
ampW
ast
egordma
rd(1
999)
9
Du
gm
ore
ampN
ewto
n(1
998)
10
Bjo
rck
et
al
(1992)
11
Kva
mm
eet
al
(1989)
12
Zoli
tsch
ka
etal
(1995)
13
Ju
vig
nparae
ampG
ewel
t(1
987)
14
Di
Vit
oet
al
(1999)
15
Del
ibri
as
etal
(1979)
16
Ju
vig
nparae
etal
(1987)
17
Dav
ies
et
al
(2001)
18
van
den
Bogaard
ampS
chm
inck
e(1
985)
19
Fri
edri
chet
al
(1999)
20
Bra
uer
eta
l(1
999)
21
Etl
ich
eret
al
(1987)
22
Tu
rney
etal
(1997)
23
Pate
rne
et
al
(1986)
24
Kel
ler
(1980)
25
Eir
parasup3kss
on
etal
(2000)
26
Hadeg
idaso
net
al
(2000)
27
Ale
ssio
etal
(1976)
28
Vez
zoli
(1991)
29
San
tacr
oce
(1987)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 771
Tab
le1
(Con
t)
(Th
eva
rve
ages
for
the
Ulm
ener
Maar
(E)rsquo
row
an
dth
eP
om
ici
Pri
nci
pali
(IT
)rsquoro
ware
11
000
an
d12
180
yea
rs
resp
ecti
vel
y)
GR
IPage
tep
hra
age
(ss0
8c
volc
an
ic
hori
zon
(14C
yrs
)ti
me-
scale
)n
SiO
2T
iO2
Al 2
O3
FeO
Mn
OM
gO
CaO
Na
2O
K2O
P2O
5to
tal
EP
MA
sou
rce
ref
IT
HO
L-1
9200
7493
612
2144
7101
001
987
1136
819
701
1
998
1W
DS
Vei
div
otn
10
11
(IC
)(0
45
)(0
08
)(0
15)
(01
)(0
08
)(0
25)
(02
7)
(01
4)
(00
6)
Ulm
ener
956
0
12
Maar
(E)
Pu
yd
e97
90
sect1
75
P
uy
de
6
13
Dom
eD
om
e
(MC
)
Pom
ici
976
0sect
300
605
205
1179
539
0
09
432
033
286
7100
ED
SP
hle
gre
an
2
4
Pri
nci
pali
10
32
0sect
50
Fie
lds
14
15
(IT
)
God
ivel
le1
030
010
557
516
2204
553
2
18
261
445
243
3
999
5W
DS
Lac
Ch
au
vet
6
16
4(M
C)
Lac
drsquoe
nH
au
tP
uy
de
Tart
are
tL
ac
de
laF
age
Ved
de
10
31
0sect
50
11
98
0sect
60
11
704
602
9129
536
301
702
013
846
433
4
970
6W
DS
Katl
a7
Ash
(IC
)(1
63
95
5m
)(0
92
)(0
03
)(0
22)
(02
9)
(00
8)
(00
3)
(00
9)
(04
0)
(01
1)
(1
22
)
20
464
845
1125
8145
502
049
896
230
307
4
967
0W
DS
Katl
a17
(01
8)
(01
1)
(01
5)
(01
7)
(00
2)
(00
7)
(01
9)
(00
6)
(00
4)
(0
42
)
Ref
eren
ces
1
this
stu
dy
2
Pate
rne
etal
(1988)
3
Narc
isi
(1996)
4
All
enet
al
(1999)
5
An
dro
nic
oet
al
(1995)
6
Ju
vig
nparae
et
al
(1996)
7
Bir
ks
et
al
(1996)
8
Bjo
rck
ampW
ast
egordma
rd(1
999)
9
Du
gm
ore
ampN
ewto
n(1
998)
10
Bjo
rck
et
al
(1992)
11
Kva
mm
eet
al
(1989)
12
Zoli
tsch
ka
etal
(1995)
13
Ju
vig
nparae
ampG
ewel
t(1
987)
14
Di
Vit
oet
al
(1999)
15
Del
ibri
as
etal
(1979)
16
Ju
vig
nparae
etal
(1987)
17
Dav
ies
et
al
(2001)
18
van
den
Bogaard
ampS
chm
inck
e(1
985)
19
Fri
edri
chet
al
(1999)
20
Bra
uer
eta
l(1
999)
21
Etl
ich
eret
al
(1987)
22
Tu
rney
etal
(1997)
23
Pate
rne
et
al
(1986)
24
Kel
ler
(1980)
25
Eir
parasup3kss
on
etal
(2000)
26
Hadeg
idaso
net
al
(2000)
27
Ale
ssio
etal
(1976)
28
Vez
zoli
(1991)
29
San
tacr
oce
(1987)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
772 S M Davies and others
Tab
le1
(Con
t)
(Th
eva
rve
age
for
the
Laach
erS
ee(E
)rsquoro
wis
12
880
yea
rs)
GR
IPage
tep
hra
age
(ss0
8c
volc
an
ich
ori
zon
(14C
yrs
)ti
me-
scale
)n
SiO
2T
iO2
Al 2
O3
FeO
Mn
OM
gO
CaO
Na
2O
K2O
P2O
5to
tal
EP
MA
sou
rce
ref
IT
HO
L-2
10
70
0
13
470
727
7152
9132
002
364
7110
928
104
6
994
0W
DS
Gri
msv
otn
10
11
(IC
)1
080
0(0
95)
(03
)(0
38
)(0
5)
(00
6)
(08
6)
(07
4)
(02
6)
(00
6)
un
kn
own
12
385
sect6
0
(Ca
pea
k)
(16
530
m)
God
ivel
leca
1
070
010
523
723
192
867
419
831
977
736
326
9
999
5W
DS
Lac
Ch
au
vet
6
16
5(M
C)
Lac
drsquoe
nH
au
tP
uy
de
Tart
are
tL
ac
de
laF
age
Laach
er11
000
sect50
39
578
4
228
515
604
5
03
2113
553
7
100
ED
SL
aach
erS
ee1820
See
(E)
11
063
sect12
(06
9)
(0
26
)(0
07)
(00
5)
(0
03
)(0
75
)(0
33)
29
595
501
0214
818
200
700
210
485
969
9
100
ED
S(0
70)
(00
7)
(02
8)
(01
4)
(00
8)
(00
5)
(01
3)
(09
7)
(04
2)
27
604
801
8210
019
200
200
614
174
272
1
100
ED
S(0
55)
(00
7)
(01
7)
(02
3)
(00
5)
(00
9)
(02
7)
(06
4)
(04
7)
30
598
604
3201
823
300
102
018
071
578
0
100
ED
S
(07
7)
(02
3)
(04
6)
(03
3)
(00
4)
(02
5)
(06
1)
(08
)(0
46)
un
kn
own
12
820
sect60
(C
ap
eak)
(16684
m)
Ref
eren
ces
1
this
stu
dy
2
Pate
rne
etal
(1988)
3
Narc
isi
(1996)
4
All
enet
al
(1999)
5
An
dro
nic
oet
al
(1995)
6
Ju
vig
nparae
et
al
(1996)
7
Bir
ks
et
al
(1996)
8
Bjo
rck
ampW
ast
egordma
rd(1
999)
9
Du
gm
ore
ampN
ewto
n(1
998)
10
Bjo
rck
et
al
(1992)
11
Kva
mm
eet
al
(1989)
12
Zoli
tsch
ka
etal
(1995)
13
Ju
vig
nparae
ampG
ewel
t(1
987)
14
Di
Vit
oet
al
(1999)
15
Del
ibri
as
etal
(1979)
16
Ju
vig
nparae
etal
(1987)
17
Dav
ies
et
al
(2001)
18
van
den
Bogaard
ampS
chm
inck
e(1
985)
19
Fri
edri
chet
al
(1999)
20
Bra
uer
eta
l(1
999)
21
Etl
ich
eret
al
(1987)
22
Tu
rney
etal
(1997)
23
Pate
rne
et
al
(1986)
24
Kel
ler
(1980)
25
Eir
parasup3kss
on
etal
(2000)
26
Hadeg
idaso
net
al
(2000)
27
Ale
ssio
etal
(1976)
28
Vez
zoli
(1991)
29
San
tacr
oce
(1987)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 773
Tab
le1
(Con
t)
GR
IPage
tep
hra
age
(ss0
8c
volc
an
ich
ori
zon
(14C
yrs
)ti
me-
scale
)n
SiO
2T
iO2
Al 2
O3
FeO
Mn
OM
gO
CaO
Na
2O
K2O
P2O
5to
tal
EP
MA
sou
rce
ref
La
Nu
gmicroere
ca11
400
12
549
922
9160
470
002
324
454
744
538
972
4W
DS
La
Nu
gmicroere
6
21
(MC
)
Nea
poli
tan
ca12
000
17
588
104
2177
631
901
006
525
940
686
9
962
8W
DS
Cam
pi
1Y
ello
w(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(0
78)
Fle
gre
i
Tu
reg(I
T)
568
106
0194
448
7
17
451
938
75
5
100
ED
S
596
804
9192
940
3
06
435
034
588
9
100
ED
S2
14
619
403
1196
329
9
02
019
943
485
7
100
ED
S
Borr
ob
ol
ca12
300
18
733
601
1122
914
700
601
207
635
837
6
955
1W
DS
Hek
la22
(IC
)(0
35)
(00
2)
(01
8)
(00
9)
(00
2)
(00
2)
(00
3)
(01
4)
(00
9)
(0
47)
un
kn
ow
n14
650
sect200
(Ca
pea
k)
(17458
m)
un
kn
ow
n14
650
sect200
(C
ap
eak)
(17506
m)
E-2
P
oll
ara
ca13
000
766
302
7138
810
8
01
015
025
239
7
100
ED
SA
eoli
an
2
23
24
pu
mic
e(I
T)
Isla
nd
s
KO
L-G
S-2
13
400
18
490
910
6148
8100
702
184
9126
521
400
902
8989
6W
DS
25
(IC
)
GS
-2B
AS
-113
400
3497
417
0132
7124
402
266
6118
124
802
103
4988
7W
DS
26
(IC
)
Ref
eren
ces
1
this
stu
dy
2
Pate
rne
etal
(1988)
3
Narc
isi
(1996)
4
All
enet
al
(1999)
5
An
dro
nic
oet
al
(1995)
6
Ju
vig
nparae
et
al
(1996)
7
Bir
ks
et
al
(1996)
8
Bjo
rck
ampW
ast
egordma
rd(1
999)
9
Du
gm
ore
ampN
ewto
n(1
998)
10
Bjo
rck
et
al
(1992)
11
Kva
mm
eet
al
(1989)
12
Zoli
tsch
ka
etal
(1995)
13
Ju
vig
nparae
ampG
ewel
t(1
987)
14
Di
Vit
oet
al
(1999)
15
Del
ibri
as
etal
(1979)
16
Ju
vig
nparae
etal
(1987)
17
Dav
ies
et
al
(2001)
18
van
den
Bogaard
ampS
chm
inck
e(1
985)
19
Fri
edri
chet
al
(1999)
20
Bra
uer
eta
l(1
999)
21
Etl
ich
eret
al
(1987)
22
Tu
rney
etal
(1997)
23
Pate
rne
et
al
(1986)
24
Kel
ler
(1980)
25
Eir
parasup3kss
on
etal
(2000)
26
Hadeg
idaso
net
al
(2000)
27
Ale
ssio
etal
(1976)
28
Vez
zoli
(1991)
29
San
tacr
oce
(1987)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
774 S M Davies and others
Tab
le1
(Con
t)
(Th
evarv
eage
for
the
Gre
enis
h(I
T)rsquo
row
is17
560
yea
rs)
GR
IPage
tep
hra
age
(ss0
8c
volc
an
ich
ori
zon
(14C
yrs
)ti
me-
scale
)n
SiO
2T
iO2
Al 2
O3
FeO
Mn
OM
gO
CaO
Na
2O
K2O
P2O
5to
tal
EP
MA
sou
rce
ref
GS
-2B
AS
-213
400
6497
933
2122
4147
902
445
389
829
905
205
4979
4W
DS
26
(IC
)
GS
-2B
AS
-313
400
2538
529
9125
7131
203
132
174
729
507
707
7980
1W
DS
26
(IC
)
GS
-2B
AS
-414
000
7503
617
4145
1113
202
155
3100
528
010
5
975
7W
DS
26
(IC
)
Un
ita
dei
ca14
000
5648
804
7184
625
901
602
217
432
679
302
8100
ED
SP
hle
gre
an
3
27
Tef
ra(0
53
)(0
13
)(0
25)
(07
4)
(01
4)
(01
6)
(01
6)
(03
4)
(06
6)
(01
6)
Fie
lds
Su
per
iori
(IT
)
Y-1
(IT
)ca
14
000
16
600
413
7169
555
502
218
242
262
229
306
8100
ED
SE
tna
28
Bla
ck17
000
sect300
Fea
ther
(17890
m)
Gre
enis
hca
15
000
9618
704
190
731
601
804
328
531
586
202
6100
ED
SV
esu
viu
s3
4
(IT
)(0
70
)(0
08
)(0
45)
(06
8)
(01
0)
(01
0)
(05
9)
(05
3)
(05
8)
(01
6)
29
L9
(IT
)ca
16
000
15
626
704
4188
630
401
103
329
429
683
402
7100
ED
SV
esu
viu
s3
15
17
000
(14
2)
(01
4)
(07
2)
(11
1)
(00
9)
(02
4)
(06
6)
(04
8)
(06
5)
(01
8)
St
2-1
85
18
500
7504
015
1145
5112
002
466
9114
525
206
6
992
2W
DS
26
(IC
)
Ref
eren
ces
1
this
stu
dy
2
Pate
rne
etal
(1988)
3
Narc
isi
(1996)
4
All
enet
al
(1999)
5
An
dro
nic
oet
al
(1995)
6
Ju
vig
nparae
et
al
(1996)
7
Bir
ks
et
al
(1996)
8
Bjo
rck
ampW
ast
egordma
rd(1
999)
9
Du
gm
ore
ampN
ewto
n(1
998)
10
Bjo
rck
et
al
(1992)
11
Kva
mm
eet
al
(1989)
12
Zoli
tsch
ka
etal
(1995)
13
Ju
vig
nparae
ampG
ewel
t(1
987)
14
Di
Vit
oet
al
(1999)
15
Del
ibri
as
etal
(1979)
16
Ju
vig
nparae
etal
(1987)
17
Dav
ies
et
al
(2001)
18
van
den
Bogaard
ampS
chm
inck
e(1
985)
19
Fri
edri
chet
al
(1999)
20
Bra
uer
eta
l(1
999)
21
Etl
ich
eret
al
(1987)
22
Tu
rney
etal
(1997)
23
Pate
rne
et
al
(1986)
24
Kel
ler
(1980)
25
Eir
parasup3kss
on
etal
(2000)
26
Hadeg
idaso
net
al
(2000)
27
Ale
ssio
etal
(1976)
28
Vez
zoli
(1991)
29
San
tacr
oce
(1987)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 775
Altogether 34 tephra layers have been reported from sediment sequences in Europeand the NE Atlantic region which date to the period between 185 and 80 14C ka BP(table 1) Because tephra layers are deposited virtually instantaneously (in geologicalterms) they enotectively represent time-parallel marker horizons within stratigraphicalsequences (Westgate amp Gorton 1981 Sarna-Wojcicki 2000 Turney amp Lowe 2001) Intheory therefore all 34 tephras could prove valuable for correlation purposes eitherin a local context or in those cases where the ash deposits have been widely dispersedbetween regional sequences In practice however very little is known about the fullgeographical dispersal of the majority of the ash layers listed in table 1 Furthermorecorrelation by tephrostratigraphy will only work if the various ash layers have wellcharacterized geochemical signatures While some geochemical data are available forthe majority of the tephras listed in table 1 the collective data are far from robustand no geochemical data have yet been published for some
Nonetheless there is mounting evidence to show that some of the tephra depositslisted in table 1 are not only geochemically distinct but are also much more widelydispersed across Europe than was initially realized Stratigraphic records of thebetter-known tephras were initially limited to observations of visible tephra layersThe development of a technique that enables detection of tephra layers that are invis-ible to the naked eye (micro-tephra) in Late Glacial sequences has greatly extendedthe area over which some of the ashes can be traced (Lowe amp Turney 1997 Turneyet al 1997 Turney 1998 Wastegard et al 1998 2000a b) Most of this research sofar has focused on micro-tephra layers originating from Icelandic centres distributedthroughout northern Europe Here we report on further development of this line ofresearch with new evidence for the occurrence of micro-tephra layers in a site insouthern Europe The results suggest that there is great potential for tracing someash layers that originated from Italian volcanic complexes over much larger tracts ofsouthern and central Europe than records of visible tephra deposits allow This inturn greatly enhances the scope for making precise correlations not only betweenparts of southern Europe but also between continental and marine (MediterraneanSea) sequences
2 Micro-tephra extraction techniques
Micro-tephra horizons are composed of glass shards that are generally between 80and 24 m m (long axis) in size and that are present in such low concentration insedimentary sequences that they can only be detected by the use of a particle sep-aration technique Several factors inreguence the concentration of shards such as dis-tance from the volcanic source precipitation patterns during the eruption and sub-sequent tephra dispersal and sedimentary processes within the catchment In someterrestrial sequences micro-tephra horizons with a peak concentration (peak con-centration tends to coincide with the shy rst occurrence of glass shards in a sedimentsequence which is then taken to mark the time of maximum ash deposition) as lowas 10 shards cmiexcl3 has been conshy rmed whereas other sites have recorded as muchas 8000 shards cmiexcl3 (Turney et al 1997) In complete contrast tephra horizons inthe GRIP ice core have been identishy ed based on a single glass shard only (Gronvoldet al 1995)
Enotective separation techniques for the detection and isolation of tephra particlesfrom sedimentary sequences have been developed These include ashing of organic
Phil Trans R Soc Lond A (2002)
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776 S M Davies and others
matter (Pilcher amp Hall 1992) digestion of biogenic and opaline silica (Rose et al 1996) the use of magnetic properties of ash layers (see for example Oldshy eld et al 1980 van den Bogaard et al 1994 Pawse et al 1998) X-ray analysis (Dugmore ampNewton 1992) and a density separation (regotation) technique (Turney 1998) Den-sity separation has proved exceedingly useful for the detection of small glass shardspresent in low concentrations in mineral-rich Late Glacial sediments This involvesthe separation and concentration of particles of predetermined specishy c gravity withthe use of a heavy liquid and subsequent identishy cation of glass shards with the useof a polarizing light microscope (for further details see Turney (1998)) This methodhas been particularly successful in the detection of tephras of rhyolitic compositionthat have a specishy c density of 2325 g cmiexcl3 (Lowe amp Turney 1997 Turney et al 1997 2001 Turney 1998 Wastegard et al 1998 2000a b) It is this technique thathas resulted in the wider recognition of micro-tephras in Europe as discussed below
3 Geochemical ` ngerprintingrsquo of tephra layers
The 34 tephras listed in table 1 have originated from four major volcanic complexesIceland the Massif Central in central France the Eifel district near Bonn and threevolcanic centres in Italy (the Campanian group Etna and the Aeolian Islands (seeshy gure 2)) An important matter to resolve is the extent to which the various magmasand ashes generated by these volcanic complexes can be geochemically shy ngerprintedThis is especially important in the case of tephras which have originated from thesame volcanic centre in which there may have been limited geochemical evolution ofmagmas over time In this section we summarize the approach generally adopted todetermine the geochemical character of visible and micro-tephras as background tothe geochemical data summarized in table 1 In the subsequent section of the paperwe review the present state of knowledge concerning all 34 tephras listed in table 1
Glass shards formed during the rapid cooling of magma are thought to have acomposition that is representative of the bulk geochemistry of the magma (Barker1983) hence widely dispersed glass particles are regarded as the most appropriateconstituents of pyroclastic material for geochemical analysis If a tephra deposit canbe shown to have a distinct geochemical signature then it can be used to correlatethe stratigraphic units in which it occurs (tephrostratigraphy) as well as to datethese units (tephrochronology) if the ages of the tephras are known (Westgate ampGorton 1981) A key element of building a tephrostratigraphical framework there-fore is to establish as rigorously as possible the geochemical composition of theindividual tephras used in its construction Robust and directly comparable geo-chemical datasets are dimacr cult to assemble for glass however because it is highlyunstable material particularly prone to sodium mobilization
The technique most widely employed to establish the geochemical signature of atephra is electron probe micro-analysis (EPMA) This enables grain-discrete determi-nations of the major elements within an individual glass shard which is of particularbeneshy t in the analysis of micro-tephra layers which generally contain glass particlesin low concentration The glass surface is bombarded with an electron beam and theX-ray energy produced is unique to each element while the intensity of the signalemitted is proportional to the amount of that element in the glass shard (Hunt amp Hill1993) Measurement can be by either energy dispersive spectrometry (EDS) or wave-length dispersive spectrometry (WDS) EDS has a lower precision mainly because
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N
0 500 km
Confirmed records of Vedde Ash (visible occurrences)
New records of Vedde Ash from flotation method
Extended area of Vedde Ash detection (micro-tephra)
Known area of Laacher See Tephra (visible occurrences)
Confirmed records of Neapolitan Yellow Tuff (visible occurrences)
New record of Neapolitan Yellow Tuff from flotation method
Known area of Neapolitan Yellow Tuff
Volcanic centres of particular relevance to this study
Other major volcanic centres in Europe
Figure 2 Location of the principal volcanic centres that were active during Termination 1 andthe Early Holocene The known distribution of the Vedde Ash (VA) Laacher See (LST) andNeapolitan Yellow Tureg (NYT) are shown
the behaviour of each element cannot be monitored independently during measure-ment and so this approach fails to detect for example any signishy cant mobilizationof sodium during the bombardment process (Hunt amp Hill 1993) Although WDSrequires a higher beam current and a longer counting time than EDS the formeronoters the distinct advantage of sequential acquisition of elemental data so that thedegree of sodium loss can be tracked The morphology of individual glass shards canalso distort EDS data a problem that is reduced when using WDS because for thisprocedure glass shards are mounted in an epoxy resin and polished to provide aregat surface for analysis Hence data should always be obtained using WDS whereverpossible
Even when WDS is used as a common tool for determining the geochemical spectraof samples aberrant results can arise that inreguence data comparisons For examplesome glass shards may contain tiny crystalline inclusions of feldspar and these shouldbe avoided when selecting surface points for analysis (Hunt amp Hill 2001) Hunt amp Hill
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778 S M Davies and others
6
4
2
40 50 60 70 80
K2O
(
)
SiO2 ()
Laacher See
Iceland
Veidivoumltn-Dyngjufjoumlll
Katla (basalt)
Grimsvoumltn-Kverkfjoumlll
Hekla
Katla (rhyolitic)
0
Icelandic volcanic centres8
10
Massif Central
Etna
Campanian
Figure 3 Bi-plot of SiO2 and K2 O concentrations in tephras derived from the main Europeanash provinces (modimacred after Mangerud et al 1984) The Campanian Massif Central and Etnaconcentrations are based on the data presented in table 1
(2001) have concluded that small variations in the laboratory procedures employedto determine glass chemistry can lead to misidentishy cation of sources for glass shardsand give an example of shards with a Jan Mayen provenance wrongly attributedto an Icelandic source Clearly there is a need for standardization of laboratoryprocedures and while a number of recommendations have recently been advocated(Froggatt 1992 Hunt amp Hill 1993 Hunt et al 1998) there is still some variation inlaboratory and operator practice (Hunt amp Hill 1996) Standardization is also requiredin the form in which results are presented to ensure comparability Normalizationof the data to 100 a practice employed by some researchers can obscure poorresults and hence lead to incorrect comparisons (Hunt amp Hill 1993) However othersargue that it may actually facilitate comparisons between samples by removing thedistorting enotects of the water component contained in glass shards (see for exampleFroggatt 1992) The majority of the published Italian and some of the Eifel datahave been normalized while those from other parts of Europe have not and hencedata comparisons are not always straightforward
Table 1 provides mean values and standard deviations for major oxide concentra-tions obtained from those tephras for which data are presently available The tableincludes previously unpublished WDS results for the Neapolitan Yellow Tunot (NYTdiscussed in x 4 below) and for the Mercato Tephra While individual tephra layersmay be geochemically distinct the geochemical envelopes representing the collectivedata obtained from all of the tephras assigned to each major volcanic province showsignishy cant overlaps as is illustrated in the bi-plots and ternary plots (shy gures 3 and 4)of selected oxide concentration data It is clear therefore that measurement of majoroxide concentrations does not satisfactorily discriminate between some tephras orig-inating from dinoterent volcanic centres (as noted by van den Bogaard amp Schmincke(1985) and Frezzotti amp Narcisi (1996) with respect to Eifel and Italian tephras)nor of tephras of dinoterent age originating from the same volcanic centre (Bond et
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European tephrochronological framework for Termination 1 779
40 50 60 70 80
K2O
(
)
SiO2 ()
shyshyshyshy
shy
shyshy
shyshyshy
shy
shy
shy
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reg
reg regreg
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FF
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4 8 12 16
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l shyshyshyshyshy shyshyshyshyshyshy
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ll
FeO ()
TiO
2 (
)
reg
l
Iceland
Eifel
F
shy ItalyMassif Central
100
80
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100 80 60 40 20
CaO
FeO
K2O
regregreg
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K2ONa2O
CaO
(c) (d)
(a)
(b)
Figure 4 Plots of selected geochemical data obtained from tephras of Termination 1 age (seetable 1) (a) Bi-plot of mean SiO2 and K2 O values (b) Bi-plot of mean FeO and TiO2 values(c) Ternary plot indicating variations in the proportions of FeO CaO and K2 O (d) Ternaryplot indicating variations in the proportion of CaO Na2 O and K2 O
al 2001) Individual tephra layers are presently assigned to a particular volcanicevent on the basis of a combination of criteria usually including examination of thephysical properties (eg refractive index and surface detail of the glass shards) thestratigraphic position of the layer and independent assessment of the age of the layeras well as any geochemical data that may be available The construction of a tephro-stratigraphical scheme would clearly beneshy t from the application of a more diagnostic
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780 S M Davies and others
geochemical tool One approach that has promise is the analysis of trace and rareearth elements using an ultraviolet laser ablation inductively coupled plasma massspectrometer (UV-LA-ICP-MS) (Pearce et al 1996 1999 Eastwood et al 1999)This approach has been applied successfully to analysis of tephras of Mid-Holoceneage but not yet to tephras that fall within the period of interest here
4 Tephra layers in Europe and the North Atlantic regiondated to between 185 and 80 14C ka
(a) Icelandic province
The Icelandic volcanic systems are divided into three main groups based on theirgeochemical characteristics tholeiitic basalts transitional alkali basalts and alkaliolivine basalts (Jakobsson 1979) Collectively magmas from the Icelandic provincespan a wide geochemical spectrum although individual volcanic centres have tightgeochemical distributions (shy gure 3) for four of the main centres Grimsvotn-Kverfjolland Veidvotn-Dyngjufoll which form part of the northern (tholeiitic) volcanic zoneand Hekla and Katla which fall within the eastern (alkali olivine basalt and transi-tional alkali basalt) volcanic zone (Haregidason et al 2000) These appear to be thekey centres for the tephras listed in table 1 that have been assigned an Icelandicorigin
One of the best-known and most widely dispersed tephra horizons in northernEurope that has an Icelandic origin is the Vedde Ash (VA) which was depositedca 103 14C ka BP (Birks et al 1996 Wastegard et al 1998) within the GS-1Younger Dryas chronozone This ash is believed to originate from the Katla complexwithin the transitional alkali basalt province (Mangerud et al 1984 Lacasse et al 1995) in the south of the island The ash has a bimodal geochemical composition (rhy-olitic and basaltic) which is thought to reregect derivation from two separate magmachambers Studies of recent volcanic events in Iceland have shown that the mostexplosive eruptions generating the largest amounts of tephra occur in this tran-sitional alkali basalt province (Haregidason et al 2000) It is also believed that thewidespread distribution of this ash was caused by the development of co-ignimbriteash plumes during an ignimbrite-forming eruption (Lacasse et al 1995)
Layers of VA that are visible to the naked eye have been found in lake sediments inwestern Norway (Mangerud et al 1984) and the Inner Hebrides Scotland (Davies etal 2001) and in marine cores throughout the NE Atlantic (see for example Kvammeet al 1989 Lacasse et al 1995) in the northern North Sea (Long amp Morton 1987)on the Iceland plateau (Ruddiman amp McIntyre 1981 Sejrup et al 1989) and on theeast Greenland continental margin (Stein et al 1996) The distribution of the VAin North Atlantic marine sequences is characterized by an arcuate lobe extendingsouthwest from the Denmark Strait and curving eastwards to mid-latitudes in theNorth Atlantic (Lacasse et al 1995) This strongly suggests deposition from raftedice which was displaced to the southwest and south in a circulating counterclockwisegyre (Ruddiman amp Glover 1972) This may well reregect Katlarsquos close proximity tothe southern coast of Iceland with the Vedde tephra being deposited on ice thatcalved directly into the North Atlantic (Haregidason et al 2000) However depositionvia the atmosphere almost certainly took place as well as is indicated by the recentdiscoveries of rhyolitic VA in micro-tephra form in several sites in Scotland (Turneyet al 1997) southern Sweden (Wastegard et al 1998 2000a) and western Russia
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(Wastegard et al 2000b) A more recent discovery of a relatively high concentrationof rhyolitic VA glass shards in the northern Netherlands indicates that the ash maywell have been dispersed much further south than previously thought (S M Davies2002 unpublished work) Finally glass shards assigned to the VA have also beendiscovered in the GRIP ice core and dated to 11 980 sect 80 GRIP yr BP (Gronvold etal 1995) This discovery is extremely important for it indicates that the VA maywell provide a reliable time-parallel marker horizon between ice-core marine andterrestrial records
Two other important Icelandic ash layers the Borrobol and Saksunarvatn Tephraswere deposited near the beginning and end of the Last TerminationEarly Holoceneinterval respectively The Borrobol Tephra was discovered for the shy rst time in lakesediments in several sites in Scotland and as yet is known only in micro-tephra formIt has been dated in Scottish sites to ca 123 14C ka BP (Turney et al 1997) Whatis thought to be a contemporaneous tephra has been detected in marine sedimentson the North Icelandic shelf (Eirplusmn ksson et al 2000) This certainly has a very similargeochemical composition to those reported from Scotland but the horizon in whichit was discovered on the North Iceland plateau has been dated to 134 14C ka Theage discrepancy between the Scottish and Icelandic Borrobol Tephra layers may wellreregect the inreguence of a marine reservoir error although the possibility that severaltephras with similar geochemical composition were erupted over a period exceeding1000 yr cannot be ruled out (Larsen 2000)
The Saksunarvatn Ash appears to have been one of the largest Holocene eruptionsin Iceland It has a tholeiitic basaltic composition which is considered to indicate anorigin in the Grimsvotn or Kverfjoll complex (shy gure 3) (Mangerud et al 1986) Layersof this ash have been identishy ed in sites on the Faroe Islands (Mangerud et al 1986Dugmore amp Newton 1998 Wastegard et al 2001) the Shetland Isles (Bennet et al 1992) northern Germany (Merkt et al 1993) western Norway (micro-tephra) (Birkset al 1996) and in the GRIP (Gronvold et al 1995) and NordGRIP ice cores (S MDavies 2002 unpublished work) It has been dated to between 9060 and 8930 14C kaBP (Birks et al 1996) in Norway and to ca 10 240 sect 30 GRIP yr BP in the GRIPice core (Gronvold et al 1995) The Saksunarvatn Ash may thus provide a secondimportant widespread time-parallel marker between ice-core marine and terrestrialrecords
Other Icelandic tephras of rhyolitic amacr nity are less well known in terms of theirdistribution and geochemical variation The Hogstorpsmossen Tephra reported fromSweden (Bjorck amp Wastegard 1999) and the L3754 tephra discovered in the FaroeIslands (Dugmore amp Newton 1998) are known from single sites only and so theirpotential for tephrostratigraphy is uncertain at present Furthermore the geochem-ical spectrum of the Hogstorpsmossen Tephra is based on a small dataset with lowanalytical totals
A number of tephras of basaltic composition have originated from Iceland buttheir distributions are largely conshy ned to Iceland or to marine cores collected fromclose to the Iceland coast or in the North Atlantic These include the tephras listedas 1-THOL-1 1-THOL-2 KOL-GS-2 GS-2BAS-1 GS-2BAS-2 GS-2BAS-3 andGS-2BAS-4 in table 1 (Kvamme et al 1989 Bjorck et al 1992 Eirplusmn ksson et al 2000 Haregidason et al 2000) The shy rst two in this list are tholeiitic basaltic tephrasassociated with the VA in a complex series of tephras collectively termed NorthAtlantic Ash Zone 1 (NAAZ1) which has been detected in numerous marine cores
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from the North Atlantic Initially thought to represent a single eruption analysisof high-resolution sediment sequences from Lake Torfadalsvatn in northern Iceland(Bjorck et al 1992) the Hebridean Shelf near NW Scotland (Austin amp Kroon 1996)the St Kilda Basin (Hunt et al 1995) and the open North Atlantic (Bond et al 2001)has demonstrated that NAAZ1 comprises a series of distinct ashes that probablyreregect separate eruption events 1-THOL-1 is thought to originate from Veidivotn(shy gure 3) while Grimsvotn may have been the source of 1-THOL-2 (Kvamme et al 1989)
KOL-GS-2 is also of tholeiitic basaltic composition but is thought to originatefrom the Kolbeinsey Ridge system (Eirplusmn ksson et al 2000) To date this tephra hasbeen detected in one marine core only within the same record on the North Ice-landic shelf as that from which the correlative of the Borrobol Tephra was alsoreported (Eirplusmn ksson et al 2000) GS-2BAS-1 to GS-2BAS-4 are of uncertain ori-gin but are thought to have been deposited at roughly the same time as KOL-GS-2(ca 134 14C ka BP (Haregidason et al 2000))
The limited distribution of these basaltic tephras a feature that is not unique toIcelandic basaltic material may reregect two factors the relative magnitude of the vol-canic eruptions from which they were derived and the limited aerial transportationof basaltic glass which is denser than rhyolitic material However a rather surpris-ing recent discovery is that of visible basaltic VA in a site on the Isle of Skye inthe Inner Hebrides Scotland (shy gure 5) (Davies et al 2001) All other occurrencesof VA in Scotland are exclusively of rhyolitic material and in micro-tephra formonly (Turney et al 1997 Turney 1998) Clearly basaltic tephra must have beentransported subaerially as far south as Skye and the reason why it has not beendetected at other sites in Scotland is puzzling We suspect that this partly reregectsthe laboratory methods employed to separate glass shards present in low concentra-tion within a micro-tephra layer from the host sediment The technique used is adensity-separation (regotation) procedure (Turney 1998) and as basaltic shards havea specishy c density similar to quartz one of the most abundant minerals in lake sedi-ments of Late Glacial age basaltic material is dimacr cult to detect using this methodThis hypothesis is currently under investigation and alternative detection methodsare being explored including magnetic separation (Mackie et al 2002)
Several other events listed in table 1 that are of probable Icelandic origin includetephras recorded in the GRIP ice core including visible (eg the `Black Featherrsquo)tephras as well as uncertain tephras inferred from distinct Ca peaks (S Johnsen2001 personal communication) No glass shards have yet been detected in the latterbut a volcanic origin is assumed because high Ca peaks are associated with knowntephras in other Greenland ice cores (S Johnsen 2001 personal communication)These are referred to as `unknownrsquo in table 1 No geochemical analyses are availablefrom these horizons so their origin must remain speculative but a possible source isIceland in view of its proximity to the Greenland ice sheet and assumed atmosphericcirculation patterns
(b) Eifel province
There are two prominent tephra events dated to the Termination 1Early Holocenetime-span that originated from the Eifel province the Laacher See Tephra (LST)and the Ulmener Maar Tephra (UMT) Visible occurrences of the LST indicate that
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Vedde Ash
615 625 635 645 655depth (cm)
organic lake mudsHolocene
silty clayGS-1Younger Dryas
organic lake mudsGI-1Alleroslashd
100 microm
(a)
(b)
Figure 5 (a) Photograph of the visible VA layer discovered at Loch Ashik Isle of Skye InnerHebrides Scotland (b) Light microscope photograph showing the rich content of basaltic shards(examples are indicated by the arrows) within this layer (8024 m m size fraction)
this ash was dispersed over much of central Europe (van den Bogaard amp Schmincke1985 Friedrich et al 1999 Litt amp Stebich 1999) The LST is dated by radiocarbonto ca 110 14C ka BP (van den Bogaard amp Schmincke 1985) and to 11 063sect12 14C BP(Friedrich et al 1999) by varve chronology to 1288 varve ka BP (Brauer et al 1999Litt et al 2001) and by ArAr dating to 129 ka cal BP (van den Bogaard 1995) Ithas a phonolitic composition and is thought to have originated from a plinian andphreatomagmatic eruption with the distal ash being carried in three distinct plumesone to the northeast towards Poland one to the west and the third to the southcovering the Jura Mountains and north Italy (van den Bogaard amp Schmincke 1985Juvigne et al 1995 Bossuet et al 1997) This pattern is thought to reregect altitu-dinal variations in the predominant wind direction Sedimentary sequences near thevolcanic source indicate that the LST consists of three main layers which represent
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dinoterent eruption phases These are grouped together as the Laacher See TephraFormation but the three individual units can be traced within and between a seriesof depositional fans The geochemical data obtained from these three LST layersshow signishy cant variations as reregected in the ternary plots (shy gure 4)
The Early Holocene Ulmener Maar Tephra (UMT) is of rhyolitic composition andappears to be restricted to sites in Germany though this conclusion is also based onrecords of visible tephras only It is dated to ca 956 14C ka BP and to 110 varve ka(Zolitschka et al 1995 Litt et al 2001)
(c) Massif Central province
The Massif Central tephras are mainly of basaltic trachyandesitic compositionwhich is distinct from the other ash provinces (shy gures 3 and 4) and their known dis-tributions are mostly conshy ned to the Massif Central region The ages of the MassifCentral tephras are based on radiocarbon dates obtained from mire and lake sedi-ments which `bracketrsquo the tephras The La Nugsup3ere Tephra with an age of 114 14C kaBP is the oldest Massif Central tephra identishy ed so far within the time-span of inter-est (Etlicher et al 1987 Juvigne et al 1996) The two Godivelle Tephras (5 and 4)are close in age but extensive radiocarbon dating suggests distinct ages of 107and 103 14C ka BP respectively (Juvigne et al 1996) The age of the Puy de DomeTephra is less certain as the estimate is based on only one radiocarbon date froma site in the southern Chaplusmn ne des Puys (table 1) This tephra is thought to havea trachyte composition (Juvigne 1993) although no major element concentrationshave yet been published
The ChopineKilianVasset tephras are thought to be derived from three separateEarly Holocene eruptions although the stratigraphic succession is not known atpresent These trachytic tephras have been radiocarbon dated to ca 854sect150 14C kaBP but are thought to have erupted separately within ca 260 yr (Juvigne et al 1996) This series of tephras is considerably more widespread than the others fromthe region having been identishy ed as far east as the Jura Mountains (Martini amp Duret1965 Martini 1970) Some other ash falls that originated from the Chaplusmn ne des Puysappear to be of local importance only (Vernet et al 1998 Vernet amp Raynal 2001)Geochemical data are currently available for only three of the Massif Central tephrasand so far as is known no attempt has yet been made to identify these tephras inmicro-tephra form
(d ) Italian provinces
The Italian tephras from this period can be assigned to three main volcanic com-plexes the Campanian volcanic shy elds around Naples Etna on Sicily and the AeolianIslands The Campanian complex which includes the Phlegrean Fields Vesuviusand Ischia is mainly trachytic in composition with a geochemical spectrum that isquite distinct from those of the Etna complex and of the Aeolian Islands (shy gure 3)Tephras originating from one or more of these three complexes have been detectedin marine cores from the Tyrrhenian and Adriatic seas as well as other parts of theMediterranean Sea (Keller et al 1978 Paterne et al 1986 1988 1990 Langone etal 1996) and in lake sequences in southern Italy such as Lago Grande di Monticchio(Newton amp Dugmore 1993 Narcisi 1996 Allen et al 1999) and central Italy such asLago Albano near Rome (Calanchi et al 1996) Some work has also been conducted
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in or close to the volcanic source areas in an attempt to establish the full sequenceof volcanic eruptions during the Late Quaternary (see for example Di Vito et al 1999) There are nine Italian tephras reported from marine and lake sequences thatdate from the period between 185 and 80 14C ka BP In all instances the recordsare of visible layers of tephra The ages of some of these are poorly established atpresent with conregicting data obtained from dinoterent sites The ages suggested intable 1 are those favoured in the most recent publications but these may requirere-assessment in the light of future research
The two oldest known tephras in the time-period of interest are the L9 and Green-ish Tephras both recorded as separate features within the annually laminated Lagodi Monticchio maar sequence The lowest of the two L9 is considered to be the cor-relative of the `basalrsquo plinian eruption of Vesuvius (Narcisi 1996) Age estimates ofa palaeosol that underlies the Vesuvius tephra sequence are ca 1617 14C ka BP forthis event (Delibrias et al 1979) L9 has a trachytic composition very similar to theGreenish Tephra (table 1) However L9 which is also a product of Vesuvius is foundstratigraphically below the Greenish Tephra in the Lago di Monticchio core TheGreenish Tephra is dated in the Monticchio sequence to 17 560 varve yr BP (Allenet al 1999) and has a calibrated radiocarbon age estimate of 17 830 sect 300 cal BP(Andronico et al 1995) Both tephras have a dominantly eastwards dispersal basedon the occurrences of visible layers (Santacroce 1987 Narcisi 1996) Both tephrasalso have a trachytic composition and as can be seen from table 1 the reportedgeochemical spectra are very close indeed with the standard deviations overlappingfor almost every major element This could present problems for tephrostratigra-phy where only one of the tephras is evident in a sediment sequence in particularbecause they are so close in age This is a good example of where an analysis oftrace and rare earth elements might be required to make a clear distinction betweentephras with very similar major oxide concentrations
The Y-1 Tephra also termed the Biancavilla Montalto Ignimbrite (Vezzoli 1991)is a product of Etna and has been identishy ed as a visible benmoritic tephra horizonthroughout the central Mediterranean (Paterne et al 1988) including central Italyand the Adriatic Sea (Vezzoli 1991 Narcisi 1993 Calanchi et al 1996) It has anestimated age of ca 140 14C ka BP The Unita dei Tefra Superiori tephra which hasbeen detected as far east as Lago di Monticchio in south-central Italy (Narcisi 1996)is also dated to ca 140 14C ka BP (Alessio et al 1976) but it is thought that thesource of this tephra lies in the Phlegrean Fields No geochemical data are availablefrom the presumed source region|the data reported in table 1 were obtained fromthe Lago di Monticchio record (Narcisi 1996)
The NYT which is equivalent to the C-2 tephra reported from various marinesequences has also been traced throughout central Italy and the Adriatic Sea (Pat-erne et al 1988 Calanchi et al 1996 Di Vito et al 1999) (shy gure 2) In the centralApennines region it formed the parent material for a soil that started to developat the beginning of the Holocene period (Frezzotti amp Narcisi 1996) Also originatingfrom the Campi Flegrei caldera it is dated to ca 120 14C ka BP (Di Vito et al 1999) Published geochemical data based on EDS indicate three dinoterent geochemicalpopulations varying from latite to phonotrachyte in composition (Orsi et al 1992Paterne et al 1988) (table 1) We report in x 4 of this paper on new data obtainedfrom the NYT by WDS and it is the mean of these new data that is included intable 1 Comparisons with the previously published EDS data are provided (table 1)
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The new data indicate clearly that the NYT originated from the Campanian volcaniccentre
In the interval between the dispersal of the NYT (ca 120 14C ka BP) and 95 14Cka BP there appear to have been as many as 34 eruptions in the Campi Flegrei caldera(Di Vito et al 1999) Of these only one appears to have been detected widely in theregion the Pomici Principali (also termed the Agnano Formation or C-1 tephra inmarine records (Paterne et al 1988) This was the product of the highest magnitudeeruption from this epoch and is dated to between 976 sect 300 and 1032 sect 50 14C kaBP (Delibrias et al 1979 Di Vito et al 1999) or to 122 varve ka BP based on theMonticchio varve chronology (Allen et al 1999) It is trachytic in composition andappears to have had a mainly eastwards dispersal
The Mercato Tephra dated to ca 80 14C ka BP and originally analysed usingEDS has a phonolitic composition and is believed to have been generated by Vesu-vius (Paterne et al 1988) New WDS data obtained from reference samples col-lected from an exposure to the west of Naples support these conclusions (table 1 andAppendix A) The silica content of the WDS analyses are ca 3 lower than thoseobtained using EDS (table 1) which may reregect the fact that the EDS data werenormalized
The only tephra listed in table 1 that is thought to have originated from the AeolianIslands is the Pollara pumice also referred to as the E2 tephra in marine sequences(Paterne et al 1986 1988) The limited geochemical data available so far suggest itto be the only Italian tephra listed in table 1 that is rhyolitic in composition Littlemore is known about this ash which has not been recorded extensively except thatits age is estimated to be ca 130 14C ka BP (Keller 1980)
5 Extending the known distributions of European tephras
Figure 2 summarizes schematically the known distributions of three of the tephrasreferred to in the preceding section the VA the LST and the NYT Following theintroduction of a laboratory method that enables the detection of micro-tephra parti-cles in mineral-rich sediment the VA has been traced to sites that are located muchfarther south (into The Netherlands) and east (as far as St Petersburg) than thedistribution limits based on occurrences of visible layers of the ash As a result con-tinental sequences over a much larger area in northern Europe can now be correlateddirectly with marine and ice-core records using the VA as a time-parallel marker
This suggests therefore that other prominent ash layers such as the LST andNYT should also be detectable over larger tracts of Europe than is presently thecase if suitable sites are examined for the presence of micro-tephra horizons To testthis assertion we examined lake sediment deposits of Last Termination age froma site in the northern Apennines in order to establish whether the NYT could bedetected in micro-tephra form The site selected Prato Spilla `Crsquo lies well to thenorth of the localities in central and southern Italy and in the Adriatic Sea fromwhich visible records of the NYT have been reported Prato Spilla `Crsquo lies at an alti-tude of ca 1350 m in the Appennino Parmense ca 60 km south of Parma and 15 kmeast of Pontremoli The site contains a continuous sediment sequence spanning theLast Termination and most of the Holocene Detailed pollen and coleopteran strati-graphical records which have been radiocarbon dated have been published for thissite (Lowe 1992 Ponel amp Lowe 1992 Lowe amp Watson 1993)
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European tephrochronological framework for Termination 1 787
Figure 6 Light microscope photograph of an NYT glass shard from Prato Spilla Crsquosequence assigned on geochemical grounds to the NYT
The methods adopted for sub-sampling of the Prato Spilla `Crsquo sequence for thequantishy cation of glass shard concentrations and for subsequent electron microprobeanalysis of selected glass shards followed those described elsewhere (Turney 1998)In summary contiguous samples of 1 cm stratigraphic interval were extracted fromthe sequence to establish presenceabsence of glass shards Each of the 1 cm3 blocksin which tephra particles was detected was then examined with more care andshard concentrations were quantishy ed for each sub-sample Micro-tephra particleswere detected in shy ve samples (shy gure 6) but were predominantly clustered around500 cm in the part of the sequence assigned on pollen-stratigraphic grounds to theLate Glacial Interstadial or the `Allerfrac12drsquo|indeed the part of the succession in whichthe NYT would be expected to occur Peak concentrations of micro-tephra particlesreach 225 shards cmiexcl3 and are conshy ned to a single 1 cm thick sample in the sequencewhich probably represents the time of maximum deposition of the ash
Electron microprobe measurements based on WDS were obtained from the surfacesof 21 separate glass shards extracted from the sample with peak shard concentrations(Appendix A) Since only EDS measurements were available for the NYT prior to thepresent study we also obtained WDS measurements from 17 shards extracted fromthe visible layer of NYT that is exposed on Procida Island which lies in the type-locality for the NYT close to the city of Naples (Appendix A) The results providenot only a more comprehensive geochemical dataset for the NYT than was previ-ously available but also a consistent basis for comparison with the Prato Spilla `Crsquodataset All of the WDS data reported here (Appendix A) were measured at the samelaboratory (Tephrochronology Analytical Unit University of Edinburgh) using thesame sample pretreatment and preparation protocol The WDS results for the NYTdinoter to a minor degree from the EDS results (table 1 and Appendix A) especiallywith respect to the amounts of silica aluminium and calcium measured The EDS
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788 S M Davies and others
4 8FeO ()
TiO
2 (
) Neapolitan Yellow Tuff(Procida)Neapolitan Yellow Tuff(Prato Spilla lsquoCrsquo)
0
1
2
3
40 50 60 70
MgO
(
)
SiO2 ()
K2O
(
)
40 50 60 70
0
04
08
4
8
12
SiO2 ()
(a)(b)
(c)
Figure 7 Bi-plots of SiO2 K2 O SiO2 MgO and FeOTiO2 for the WDS analyses obtainedfrom glass shards of the NYT from Procida (Naples) and Prato Spilla Crsquo Means and standarddeviations are shown
results show a higher degree of statistical scatter than the WDS measurements whichmay reregect the fact that the data were normalized combined with the inreguence ofvariation in water content between shards
There is a very close correspondence between the WDS data for the Prato Spilla `Crsquomicro-tephra shards and those obtained from the type-material near Naples (shy g-ure 7) The geochemical data strongly suggest therefore that the NYT is representedat the Prato Spilla `Crsquo site by a discrete layer of micro-tephra particles This conclu-sion is compatible with the pollen-stratigraphic data from the site and accords withage estimates for the NYT (ca 120 14C ka BP) obtained from other sites (Paterneet al 1990)
These results encourage us to believe that many if not all of the tephras listedin table 1 will be detectable over much larger tracts of Europe than is presently thecase if appropriate research is undertaken to detect layers of micro-tephra particlesin selected sites The authors are presently engaged in a major continent-wide pro-gramme of research in collaboration with a number of European research groupsdesigned to test this hypothesis The focus in this research is on those parts of Europewhere we expect to shy nd overlapping `apronsrsquo of tephra deposition originating fromthe Italian Eifel Massif Central and Icelandic provinces For example a number ofsites in parts of southern France northern Italy and perhaps western Switzerlandmay have received inreguxes of micro-tephra originating from the Italian and Eifelprovinces and perhaps also from the Massif Central Sites in parts of Germany Den-mark and southern Sweden for example may in turn have received tephra depositsfrom both of the Icelandic and Eifel provinces If this proves to be the case then thestage will be set for the construction of a tephrostratigraphical framework for Europewhich will enable Last Termination sequences to be correlated on a continent-widebasis using micro- and visible tephra layers as time-parallel stratigraphic markersFurthermore there is also the possibility that other tephras remain to be discovered
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European tephrochronological framework for Termination 1 789
those which either because of the magnitude or nature of some volcanic eruptionswere distributed over parts of Europe in micro-tephra form only
6 European tephrostratigraphy and the chronology of eventsduring the Last Termination and Early Holocene
One of the crucial issues in Late Quaternary palaeoenvironmental research thatremains to be resolved is the degree to which climatic events inferred from oceanicterrestrial and ice-core records were synchronous during the Last Termination andEarly Holocene If the ice-core records provide realistic estimates of the rates anddurations of climatic events during this period then comparisons between individ-ual records have to be enotected with at least a decadal precision The problem thispresents and the role that tephrostratigraphy can play in resolving some of thedimacr culties involved are put into perspective in shy gure 8
Figure 8 shows some of the data used to calibrate radiocarbon dates (the LakeSuigetsu and Cariaco Basin datasets) plotted against the GRIP ss08c ice-core recordof macr 18O variations The latter has been selected by the INTIMATE group as an arbi-trary and temporary standard for this period and used to deshy ne an event stratig-raphy scheme (shy gure 1) for the Last Termination (see Bjorck et al 1998 Walker etal 2001) As has been alluded to in earlier sections of this paper the uncertaintiesassociated with all of the dating methods currently employed preclude precise com-parisons of ice-core marine and terrestrial records Oceanic and terrestrial recordsmostly rely upon radiocarbon dating locally supplemented in a few cases by varvechronology Imprecisions in radiocarbon dates can arise through site-specishy c fac-tors (eg hard-water or mineral carbon errors in freshwater sequences and reservoirerrors in marine sequences) sample selection laboratory measurements of 14C activ-ity and other factors (Lowe amp Walker 2000) Further imprecision may be introducedby the calibration of radiocarbon dates since the uncertainties in the dataset usedto calibrate pre-Holocene radiocarbon dates INTCAL98 are far higher than forthe Holocene which is based on dendro-calibration (Stuiver et al 1998) There arealso uncertainties anotecting varve chronologies while the ss08c ice-core chronologyfor the Last Termination dinoters signishy cantly from the GISP2 record and indeedfrom other models of the GRIP record (Lowe et al 2001) Published comparisonsbetween ice-core marine and terrestrial records for the Last Termination seldom takeinto account the true magnitude of the dating uncertainties involved and frequentlyemploy circular reasoning
Figure 8 shows the positions on the radiocarbon time-scale of 20 of the tephrasdiscussed earlier in this paper these being the ones for which reasonably conshy dentradiocarbon age estimates can be made (though these will be subject to revised esti-mates in the future) A high number of these occur in the period 14080 14C kaBP but we conshy dently anticipate the discovery in the future of additional tephras(perhaps in micro-tephra form only) which will date to the period 185140 14C kaBP Tephras detected in the GRIP ice core over the same time-interval are plottedon the calendar time-scale in shy gure 8 By providing key `time-linesrsquo between recordstephrostratigraphy can help to resolve some of the dating uncertainties referredto earlier by for example enabling direct comparisons of discrepant age estimatesobtained using dinoterent methods (cf Litt et al 2001) It can also provide estimatesof the magnitudes of the reservoir errors that anotected various marine sectors at dif-
Phil Trans R Soc Lond A (2002)
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790 S M Davies and others
-44
-40
-36
-32
cale
ndar
yea
rs B
P
8000
9000
10 0
00
11 0
00
12 0
00
13 0
00
14 0
00
15 0
00
16 0
00
17 0
00
18 0
00
14C age (BP)
VA
SA
Un
Un
Un
Un
Un
BF
Hol
ocen
eG
S-1
GI-
1aG
I-1b
GI-
1cG
I-1d
GI-
1eG
S-2
aG
S-2
bG
S-
2c
Bor
robo
l
La
Nug
egravere
Laa
cher
See
God
ivel
le 5
amp I
-TH
OL
-2
Puy
de D
ocircme
I-T
HO
L-1
Saks
unar
vatn
Houmlg
stor
psm
osse
nU
lmen
er M
aar
amp L
3574
radiocarbon dated European tephra horizons
Cho
pine
Kili
an V
asse
tM
erca
to
God
ivel
le 4
Pom
ici P
rinc
ipal
i amp V
edde
Polla
ra p
umic
eK
OL
-GS-
2 amp
GS
-2B
AS-
12
3
GS
-2B
AS-
4 U
nita
dei
Tef
raSu
peri
ori amp
laye
r Y
-1
Gre
enis
h
L9
20 0
0018
000
16 0
0014
000
12 0
0010
000
-44
-40
-36
-32
800
600
400
200 0
GISP2 volcanicsulphate conc (ppb)
1000
Nea
polit
an Y
ello
w T
uff
GISP2 18O (permil) dGRIP 18O (permil) d
Figure 8 For description see opposite
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European tephrochronological framework for Termination 1 791
ferent times through a comparison of radiocarbon dates obtained from marine andterrestrial horizons in which the same tephra has been detected (see for exampleAustin et al 1995 Bondevik et al 2001 Haregidason et al 2000) Tephrostratigraphymay provide an independent test of suggestions that some of the climatic changesduring the Last Termination were time-transgressive as illustrated for some appar-ently contrasting climatic trends in Iceland Britain and NW Russia (Lowe 2001) Ofparticular importance as far as establishing `leadsrsquo and `lagsrsquo in climatic changes isconcerned are the tephra records from the Greenland ice cores The discovery of theVedde and Saksunarvatn ashes in the GRIP record (Gronvold et al 1995) alreadyprovides a basis for making direct comparisons between marine terrestrial and ice-core records It is a matter of some urgency that the incidence of tephra depositsin the Greenland ice cores be more fully explored in the hope that this will lead tothe recognition of additional time-parallel links between the ice-core records on theone hand and oceanic and terrestrial records on the other An investigation of thenew NordGRIP record for this purpose is currently in progress (S M Davies 2002unpublished data)
Finally a fuller and more reshy ned tephrostratigraphical scheme for Europe will alsohave other applications It will provide an important database for those investigatingthe timing and frequency of volcanic eruptions in Europe during the past 20 000 yror so as well as of the geochemical evolution of the dinoterent volcanic centres overthat period A fuller record of the distribution of micro-tephras may also provideinformation on atmospheric circulation patterns during the dispersal and depositionperiods as well as on the nature and altitude of the eruption columns which mayin turn provide inferences about magma viscosity
This paper is a contribution to the INTIMATE project of the INQUA Palaeoclimate Com-mission and the work is supported by a Leverhulme Trust Research project (grant allocationnumber F07537C) entitled Testing hypotheses of rapid climate change using tephrochronol-ogyrsquo SMDrsquo s contribution was completed during possession of a NERC PhD studentship(GT 0499ES162) We are extremely grateful to Dr Peter G Hill for his assistance withthe EPMA analyses at the Tephrochronology Analytical Unit University of Edinburgh We alsothank Dr G Mastrolorenzo (Vesuvius Observatory) and Miss G Swindle for assistance duringthe macreld investigations in Naples Thanks are also expressed to two anonymous reviewers forcomments on an earlier draft
Appendix A
Table 2 shows the major oxide concentrations of NYT glass shards from Procidaand Prato Spilla `Crsquo and of the Mercato Tephra from the Naples area (see x 4 forsite context) All oxides are shown as weight and total iron is expressed as FeO
Figure 8 Radiocarbon calibration curve for Termination 1 and the Early Holocene compared with theGRIP macr 18 O event stratigraphy the GRIP ss08c and GISP2 macr 18 O records (wwwngdcnoaagov) andknown tephra horizons from this period The shaded areas represent the cooler climatic episodes andare labelled with the Greenland stratotype terminology (Bjorck et al 1998) Where radiocarbon agesare reported in table 1 as a range the mean is given here Abbreviations for GRIP horizons are asfollows Un unknown (approximate positions are given (S Johnsen 2001 personal communication))SA Saksunarvatn Ash VA Vedde Ash BF Black Feather Sulphate concentrations from the GISP2record are also shown (Zielinski et al 1996) Open circles denote radiocarbon calibration data fromLake Suigetsu (Kitagawa amp van der Plicht 2000) Filled circles denote radiocarbon calibration data fromCariaco Basin assuming a marine reservoir age of 420 14 C yr (Hughen et al 1998)
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792 S M Davies and others
Tab
le2
Majo
roxi
de
con
cen
trati
on
sof
NY
Tgl
ass
shard
sfr
om
Pro
cida
an
dP
rato
Spil
laC
rsquoan
dof
the
Mer
cato
Tep
hra
from
the
Naple
sare
a(s
eex4
for
site
con
text
)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
roci
da)
1584
204
0177
634
201
106
828
635
197
5969
1W
DS
2598
603
9178
027
101
204
924
244
583
4965
8W
DS
3586
604
5173
631
100
805
924
342
183
0951
9W
DS
4583
903
9177
933
000
906
924
540
486
9958
3W
DS
5605
106
8179
126
901
204
923
243
086
1976
4W
DS
6591
704
5177
332
801
006
425
740
887
8968
0W
DS
7581
804
1178
031
501
107
125
640
086
9956
1W
DS
8589
504
2179
533
701
506
926
740
987
5970
4W
DS
9592
003
9178
135
101
007
026
443
585
7972
7W
DS
10
591
404
2174
631
601
105
723
442
482
6957
0W
DS
11
593
403
6177
131
301
506
726
439
188
5967
6W
DS
12
588
103
8176
128
100
505
525
141
583
4952
1W
DS
13
577
003
8176
533
500
807
228
140
384
8952
0W
DS
14
586
004
7179
735
300
706
827
842
984
6968
5W
DS
15
588
104
2180
629
400
505
924
937
993
0964
5W
DS
16
579
603
9178
536
501
308
228
836
087
1959
9W
DS
17
580
103
9177
631
500
907
327
039
488
9956
6W
DS
mea
n588
104
2177
631
901
006
525
940
686
9962
8
sd
(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(07
8)
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 793
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
rato
Spil
laC
rsquo)
1552
105
4177
247
401
914
38
735
578
9951
1W
DS
2557
305
7179
845
701
512
640
136
581
5960
6W
DS
3595
004
4173
724
302
003
117
652
877
8950
7W
DS
4575
704
2179
433
001
406
627
043
083
6953
7W
DS
5599
904
0178
826
401
304
421
841
688
4966
5W
DS
6591
103
8177
826
601
105
022
443
888
8960
2W
DS
7565
304
5180
939
501
410
532
535
791
8962
1W
DS
8597
606
9180
826
501
604
821
546
684
6970
7W
DS
9571
805
6179
939
801
109
932
240
883
6964
7W
DS
10
588
603
7176
527
601
104
721
042
487
7953
3W
DS
11
559
404
9180
544
501
812
339
435
878
6957
2W
DS
12
594
704
0181
328
301
705
522
144
785
6967
9W
DS
13
611
103
7187
016
900
802
419
938
195
9975
8W
DS
14
599
204
4181
128
601
404
620
844
986
6971
6W
DS
15
601
204
4177
328
302
004
722
446
385
5972
1W
DS
16
595
104
5176
428
801
504
722
744
884
3962
8W
DS
17
603
704
1177
825
101
503
520
348
181
2965
3W
DS
18
558
704
5179
647
401
813
139
836
879
0960
7W
DS
19
589
602
8178
830
901
606
622
436
091
8960
5W
DS
20
553
606
3178
647
401
913
840
136
978
0956
6W
DS
21
579
004
0175
739
000
708
328
338
286
7959
9W
DS
mea
n582
804
6179
033
401
507
427
341
484
8962
1
sd
(1
87)
(01
0)
(02
7)
(09
2)
(00
4)
(03
9)
(08
0)
(04
9)
(05
0)
(07
0)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
794 S M Davies and others
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)
1575
202
7194
219
701
101
016
374
766
9951
8W
DS
2575
802
9194
523
902
201
520
273
564
5959
0W
DS
3574
301
4205
219
101
100
416
481
266
1965
2W
DS
4575
500
7206
018
002
000
415
181
669
3968
6W
DS
5580
000
9208
018
601
300
515
883
367
1975
5W
DS
6571
001
0206
016
101
600
515
078
967
1957
2W
DS
7577
501
1201
117
101
500
620
675
655
4950
5W
DS
8573
700
9212
717
101
900
815
187
564
2973
9W
DS
9580
301
3208
715
801
400
824
81
754
1968
1W
DS
10
574
400
6211
18
402
00
516
480
567
8971
6W
DS
11
577
200
7214
212
501
200
829
879
247
962
6W
DS
12
572
200
9211
217
301
501
15
980
465
9966
3W
DS
13
571
800
7210
417
402
201
16
184
467
2971
2W
DS
14
567
300
9208
916
901
400
917
383
262
5959
3W
DS
15
568
600
8205
918
202
101
414
682
666
6960
8W
DS
16
572
501
1211
318
202
01
215
884
364
5970
9W
DS
17
572
901
2212
916
502
101
215
883
667
2973
4W
DS
18
573
01
4211
716
301
801
416
83
365
5970
4W
DS
19
569
201
1207
418
602
101
414
982
964
961
6W
DS
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
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(04
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(00
1)
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1)
(02
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Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
References
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Bond G C Mandeville C amp Horeg man S 2001 Were rhyolitic glasses in the Vedde Ash andin the North Atlanticrsquo s Ash zone 1 produced by the same volcanic eruption Quat Sci Rev20 11891199
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Delibrias G Di Paola G M Rosi M amp Santacroce R 1979 La storia eruttiva del complessovulcanico Somma Vesuvio ricostruita dalle successini piroclastiche del Monte Somma RendSoc It Mineral Petrolog 35 411438
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Frezzotti M amp Narcisi B 1996 Late Quaternary Tephra derived paleosols in central Italyrsquo scarbonate Apennine range stratigraphical and paleoclimatological implications Quat Int3436 147153
Friedrich M Kromer B Spurk M Hofmann J amp Kaiser K F 1999 Paleoenvironment andradiocarbon calibration as derived from LateglacialEarly Holocene tree-ring chronologiesQuat Int 61 2739
Froggatt P C 1992 Standardisation of the chemical analysis of tephra deposits Report of theICCT working group Quat Int 1314 9396
Gronvold K Oskarsson N Johnsen S J Clausen H B Hammer C U Bond G amp Bard E1995 Ash layers from Iceland in the GRIP ice core correlated with oceanic and land sedimentsEarth Planet Sci Lett 135 149155
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Hadeg idason H Eirpara sup3 ksson J amp van Kreveld S 2000 The tephrochronology of Iceland and theNorth Atlantic region during the Middle and Late Quaternary a review J Quat Sci 15322
Hoek W Z amp Bohncke S J P 2001 Oxygen isotope wiggle matching as a tool for synchronisingice-core and terrestrial records over Termination 1 Quat Sci Rev 20 12511264
Hughen K A Overpeck J T Peterson L C amp Trumbore S 1996 Rapid climate changes inthe tropical Atlantic region during the last deglaciation Nature 380 5153
Hughen K A Overpeck J T amp Lehman J 1998 A new 14 C calibration data set for the LastDeglaciation Radiocarbon 39 483494
Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
Hunt J B amp Hill P G 1996 An inter-laboratory comparison of the electron probe microanalysisof glass geochemistry Quat Int 3436 229241
Hunt J B amp Hill P G 2001 Tephrological implications of beam sizesample size ereg ects inelectron microprobe analysis of glass shards J Quat Sci 16 105117
Hunt J B Fannin N G T Hill P G amp Peacock J D 1995 The tephrochronology andradiocarbon dating of North Atlantic Late Quaternary sediments an example from the StKilda Basin In The tectonics sedimentation and palaeoceanography of the North Atlanticregion (ed R A Scrutton M S Stoker G B Shimmield amp A W Tudhope) vol 90pp 227248 Geological Society of London Special Publication
Hunt J B Clift P D Lacasse C Vallier T L amp Werner R 1998 Standardisation ofelectron probe microanalysis of glass geochemistry In Proc ODP Scientimacrc Results vol 152pp 8591 College Station TX Ocean Drilling Program
Jakobsson S P 1979 Outline of the petrology of Iceland Jokull 29 5773
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Juvignparae E 1993 Contribution microa la tparaephrostratigraphie du Quaternaire et son application microa lagparaeomorphologie Mparaem Serv Explicat Cartes Gparaeol Min Belg 36 166
Juvignparae E amp Gewelt M 1987 La Narse drsquo Ampoix comme tparaephrostratotype dans la Chasup3 ne desPuys mparaeridionale (France) Bull Ass Fr Etud Quat 29 3749
Juvignparae E Kozarski S amp Nowaczyk B 1995 The occurrence of Laacher See Tephra in Pomera-nia NW Poland Boreas 24 225231
Juvignparae E Bastin B Delibrias G Evin J Gewelt M Gilot E amp Streel M 1996 Acomprehensive pollen and tephra based chronostratigraphic model for the Lateglacial andHolocene period in the French Massif Central Quat Int 3436 113120
Keller J 1980 The island of Vulcano Rend Soc It Mineral Petrolog 36 369414
Keller J Ryan W B F Ninkovich D amp Altherr R 1978 Explosive volcanic activity in theMediterranean over the past 200 000 years as recorded in deep sea sediments Geol Soc AmBull 89 591604
Kitagawa H amp van der Plicht J 2000 Atmospheric radiocarbon calibration beyond 11 900 calBP from Lake Suigetsu laminated sediments Radiocarbon 42 369380
Kvamme T Mangerud J Furnes H amp Ruddiman W F 1989 Geochemistry of Pleistoceneash zones in cores from the North Atlantic Norsk Geol Tids 69 251272
Lacasse C Sigurdsson H Johannesson H Paterne M amp Carey S 1995 Source of Ash zone 1in the North Atlantic Bull Volcanol 57 1832
Langone L Asioli A Corregiari A amp Trincardi F 1996 Age depth modelling through theLate-Quaternary deposits of the central Adriatic Basin In Palaeoenvironmental analysis ofItalian crater lake and Adriatic sediments (ed F Oldmacreld amp P Guilizzoni) vol 55 pp 177196 Memorie dellrsquo Instituto Italiano di Idrobiologia
Larsen G 2000 Holocene volcanism in Iceland and tephrochronology as a tool in volcanologyIn Iceland 2000 modern processes and past environments Keele University UK
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European tephrochronological framework for Termination 1 799
Litt T amp Stebich M 1999 Bio- and chronostratigraphy of the Lateglacial in the Eifel regionGermany Quat Int 61 516
Litt T Brauer A Goslar T Merkt J Balaga K Muller H Ralska-Jasiewiczowa MStebich M amp Negendank J F W 2001 Correlation and synchronisation of Lateglacialcontinental sequences in northern Central Europe based on annually laminated lacustrinesediments Quat Sci Rev 20 12331249
Long D amp Morton A C 1987 An ash fall within the Loch Lomond stadial J Quat Sci 297101
Lotter A F Eicher U Siegenthaler U amp Birks H J B 1992 Lateglacial climatic oscillationsas recorded in Swiss lake sediments J Quat Sci 7 187204
Lowe J J 1992 Lateglacial and Early Holocene lake sediments from the Northern ApenninesItaly|pollen stratigraphy and radiocarbon dating Boreas 21 193208
Lowe J J 2001 Abrupt climatic changes in Europe during the last glacialinterglacial tran-sition the potential for testing hypotheses on the synchroneity of climatic events usingtephrochronology Global Planet Change 603 7384
Lowe J J amp Turney C S M 1997 Vedde Ash layer discovered in a small lake basin on theScottish mainland J Geol Soc Lond 154 605612
Lowe J J amp Walker M J C 2000 Radiocarbon dating the last glacialinterglacial transition(ca 14914 C ka BP) in terrestrial and marine records the need for new quality assuranceprotocols Radiocarbon 42 5368
Lowe J J amp Watson C 1993 Lateglacial and Early Holocene pollen stratigraphy of the northernApennines Italy Quat Sci Rev 12 727738
Lowe J J Birks H H Brooks S J Coope G R Harkness D D Mayle F E SheldrickC Turney C S M amp Walker M J C 1999 The chronology of palaeoenvironmental changesduring the Last GlacialHolocene transition towards an event stratigraphy for the BritishIsles J Geol Soc Lond 156 397410
Lowe J J Hoek W Z amp INTIMATE group 2001 Inter-regional correlation of palaeoclimaticrecords for the Last GlacialInterglacial transition a protocol for improved precision recom-mended by the INTIMATE project group Quat Sci Rev 20 11751187
Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
Mangerud J Lie S E Furnes H Kristiansen I L amp Liquest mo L 1984 A Younger Dryas ashbed in western Norway and its possible correlation with tephra beds from the Norwegian Seaand North Atlantic Quat Res 21 85104
Mangerud J Furnes H amp Jparaohansen J 1986 A 9000 year-old ash bed on the Faroe IslandsQuat Res 26 262265
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Martini J amp Duret J J 1965 Note preliminaire sur la presence drsquo un niveau de cendres vol-caniques dans des sparaediments post-glaciaires des environs de Genmicroeve Arch Sci 18 587588
Mayewski P A Meeker L D Twickler M S Whitlow S Yang Q Lyons W B amp Pren-tice M 1997 Major features and forcing of high latitudes Northern Hemisphere atmosphericcirculation using a 110 000 year long glaciochemical series J Geophys Res 102 345365
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Orsi G Drsquo Antonio M de Vita S amp Gallo G 1992 The Neapolitan Yellow Tureg a large mag-nitude trachytic phreatoplinian eruption eruptive dynamics magma withdrawal and calderacollapse J Volcanol Geotherm Res 53 275287
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European tephrochronological framework for Termination 1 801
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Turney C S M amp Lowe J J 2001 Tephrochronology In Tracking environmental changes inlake sediments physical and chemical techniques (ed W M Last amp J P Smol) DordrechtKluwer Academic
Turney C S M Harkness D D amp Lowe J J 1997 The use of microtephra horizons tocorrelate Lateglacial lake sediments successions in Scotland J Quat Sci 12 525531
Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
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van den Bogaard B Dordeg er W Sandgren P amp Schmincke H-U 1994 Correlating theHolocene records Icelandic tephra found in Schleswig-Holstein (northern Germany) Natur-wissenschaften 81 554556
Vernet G amp Raynal J-P 2001 Tephrostratigraphy of the Limagne revisited Implications forLateglacial and Holocene Prehistory In Tephras chronology archaeology (ed E Juvignparae ampJ-P Raynal) pp 111116 Dossiers de lrsquo ArchparaeoLogis no 1 France
Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
Vezzoli L 1991 Tephra layers in Bannock Basin (eastern Mediterranean) Mar Geol 1002134
von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
Walker M J C Bjorck S Lowe J J Cwynar L C Johnsen S Knudsen K-L WohlfarthB amp INTIMATE Group 1999 Isotopic events in the GRIP ice core a stratotype for the LatePleistocene Quat Sci Rev 18 11431150
Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
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Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
Phil Trans R Soc Lond A (2002)
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768 S M Davies and others
- 42 - 40 - 38 - 36 - 34
Holocene
Greenland stadial 1
Greenland interstadial 1
Greenland stadial 2
GI-1aGI-1b
GI-1c
GI-1d
GI-1e
GR
IP ic
e co
re (
year
s B
P)
18O permil (SMOW)d
11 000
12 000
13 000
14 000
15 000
16 000
17 000
18 000
19 000
20 000
Figure 1 The Greenland event stratigraphy scheme based on the macr 18 O record (SMOW) andstratigraphic terminology for the Last Termination and Early Holocene (after Bjorck et al 1998 Walker et al 1999)
cal = calibrated radiocarbon years GRIP ice-core yrs refers to the GRIP ss08c time-scale) (Walker 1995 Lowe et al 1999) The most pronounced features in the climaticrecords for this period are abrupt warmings at the start of Greenland Interstadial 1(the GI-1e thermal maximum) and at the onset of the Holocene and a short periodof severely cold conditions corresponding to the `Younger Dryasrsquo stadial or theGS-1 event (Greenland Stadial 1) in the proposed Greenland stratotype sequence(see Bjorck et al 1998 Walker et al 1999)
A broadly similar pattern of climatic changes has been inferred from records of theLast TerminationEarly Holocene obtained from widely scattered localities through-out the North Atlantic region and which have been derived from a wide range ofproxy data These include for example macr 18O and snow-accumulation records fromthe Greenland ice cores (Alley et al 1993 Dansgaard et al 1993) fossil beetle andchironomid assemblages from the British Isles (Atkinson et al 1987 Coope et al 1998 Lowe et al 1999 Brooks et al 1997) greyscale variations reregecting ratesof sediment accumulation in laminated deposits of the tropical Atlantic (Hughenet al 1996 1998) and macr 18O variations in Swiss German and Dutch lake sediment
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 769
sequences (Lotter et al 1992 von Grafenstein et al 1999 Hoek amp Bohncke 2001)A question that is pivotal to understanding the climate-driving mechanisms in theNorth Atlantic region is whether the abrupt events as well as the environmentalresponses to them were synchronous within the continental marine and polar icerealms or whether there were signishy cant `leadsrsquo and `lagsrsquo between them
The Greenland ice-core records suggest that some of the climatic transitions duringthe Last Termination took place within only a few decades (Mayewski et al 1997)while the short-lived cooling events within GI-1 lasted some 100300 ice-core yr atmost Determining the precise timing and duration of equivalent events representedin the ocean and continental records is extremely dimacr cult at present because of theuncertainties associated with the dating methods employed Age estimates obtainedusing the most widely adopted method radiocarbon dating have error ranges at 1frac14that are rarely better than sect50 14C yr and which frequently exceed sect100 14C yror more Interpretations of radiocarbon ages are complicated still further by uncer-tain calibration procedures and the distorting inreguences of radiocarbon `plateauxrsquo|episodes of near-constant radiocarbon age (see Lowe amp Walker 2000) Radiocarbondates obtained from marine sequences of Last Termination age are particularly sus-pect due to the inreguences of marine reservoir errors (Sikes et al 2000 Waelbroecket al 2001) There are equally wide uncertainties associated with other methodssuch as varve counting while the ice-core records themselves in the segment ofthe records that span the Last Termination may have systematic errors exceeding200 years (Stuiver amp Grootes 2000) A further problem is that some of the climatechanges at this time may have been time-transgressive (Coope et al 1998 Witteet al 1998) signishy cantly undermining the use of conventional approaches such asclimatostratigraphy and biostratigraphy for correlating the records It is evidentthen that conventional approaches to the dating and correlation of events duringthe Last Termination are inadequate for testing the hypothesis that abrupt climaticchanges during this period were truly synchronous at the continental or global scale
The problems of dating and correlating sequences that span the Last Terminationhave been reviewed through a series of workshops organized by the INTIMATE group(INTegration of Ice core MArine and TErrestrial records of the Last Termination|a core programme of the International Quaternary Union (INQUA) Palaeocli-mate Commission (httpwwwgeoguunlfgpalaeoclimateintimate)) (Bjorck etal 2001) which has recommended a set of proposals for improved precision in thefuture (Lowe et al 2001) Central to these proposals is the application of correlationtools that can provide independent tests of the age estimates and correlations basedon radiocarbon dating varve chronology and ice-layer counting
One of the approaches recommended by the INTIMATE and COTAV (INQUACommission on Tephrochronology and Volcanism) groups is tephrochronology forthere is growing evidence to suggest that this technique has the potential to resolvesome of the pressing geochronological issues while some tephras may be detectableover much wider geographical areas than appreciated hitherto Here we examine thepotential for developing a tephrostratigraphical and tephrochronological frameworkfor Europe for the period 18580 14C ka BP (encompassing the Last Terminationand the Early Holocene) It is argued that such a scheme will provide a rigorousunderpinning structure for geochronological models for this period and hence leadto improved understanding of the mechanisms timing and environmental enotects ofabrupt climatic changes during the Last Termination
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
770 S M Davies and others
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Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 771
Tab
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Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
772 S M Davies and others
Tab
le1
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t)
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idaso
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ssio
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zoli
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tacr
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Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 773
Tab
le1
(Con
t)
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yrs
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)
Ref
eren
ces
1
this
stu
dy
2
Pate
rne
etal
(1988)
3
Narc
isi
(1996)
4
All
enet
al
(1999)
5
An
dro
nic
oet
al
(1995)
6
Ju
vig
nparae
et
al
(1996)
7
Bir
ks
et
al
(1996)
8
Bjo
rck
ampW
ast
egordma
rd(1
999)
9
Du
gm
ore
ampN
ewto
n(1
998)
10
Bjo
rck
et
al
(1992)
11
Kva
mm
eet
al
(1989)
12
Zoli
tsch
ka
etal
(1995)
13
Ju
vig
nparae
ampG
ewel
t(1
987)
14
Di
Vit
oet
al
(1999)
15
Del
ibri
as
etal
(1979)
16
Ju
vig
nparae
etal
(1987)
17
Dav
ies
et
al
(2001)
18
van
den
Bogaard
ampS
chm
inck
e(1
985)
19
Fri
edri
chet
al
(1999)
20
Bra
uer
eta
l(1
999)
21
Etl
ich
eret
al
(1987)
22
Tu
rney
etal
(1997)
23
Pate
rne
et
al
(1986)
24
Kel
ler
(1980)
25
Eir
parasup3kss
on
etal
(2000)
26
Hadeg
idaso
net
al
(2000)
27
Ale
ssio
etal
(1976)
28
Vez
zoli
(1991)
29
San
tacr
oce
(1987)
Phil Trans R Soc Lond A (2002)
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774 S M Davies and others
Tab
le1
(Con
t)
(Th
evarv
eage
for
the
Gre
enis
h(I
T)rsquo
row
is17
560
yea
rs)
GR
IPage
tep
hra
age
(ss0
8c
volc
an
ich
ori
zon
(14C
yrs
)ti
me-
scale
)n
SiO
2T
iO2
Al 2
O3
FeO
Mn
OM
gO
CaO
Na
2O
K2O
P2O
5to
tal
EP
MA
sou
rce
ref
GS
-2B
AS
-213
400
6497
933
2122
4147
902
445
389
829
905
205
4979
4W
DS
26
(IC
)
GS
-2B
AS
-313
400
2538
529
9125
7131
203
132
174
729
507
707
7980
1W
DS
26
(IC
)
GS
-2B
AS
-414
000
7503
617
4145
1113
202
155
3100
528
010
5
975
7W
DS
26
(IC
)
Un
ita
dei
ca14
000
5648
804
7184
625
901
602
217
432
679
302
8100
ED
SP
hle
gre
an
3
27
Tef
ra(0
53
)(0
13
)(0
25)
(07
4)
(01
4)
(01
6)
(01
6)
(03
4)
(06
6)
(01
6)
Fie
lds
Su
per
iori
(IT
)
Y-1
(IT
)ca
14
000
16
600
413
7169
555
502
218
242
262
229
306
8100
ED
SE
tna
28
Bla
ck17
000
sect300
Fea
ther
(17890
m)
Gre
enis
hca
15
000
9618
704
190
731
601
804
328
531
586
202
6100
ED
SV
esu
viu
s3
4
(IT
)(0
70
)(0
08
)(0
45)
(06
8)
(01
0)
(01
0)
(05
9)
(05
3)
(05
8)
(01
6)
29
L9
(IT
)ca
16
000
15
626
704
4188
630
401
103
329
429
683
402
7100
ED
SV
esu
viu
s3
15
17
000
(14
2)
(01
4)
(07
2)
(11
1)
(00
9)
(02
4)
(06
6)
(04
8)
(06
5)
(01
8)
St
2-1
85
18
500
7504
015
1145
5112
002
466
9114
525
206
6
992
2W
DS
26
(IC
)
Ref
eren
ces
1
this
stu
dy
2
Pate
rne
etal
(1988)
3
Narc
isi
(1996)
4
All
enet
al
(1999)
5
An
dro
nic
oet
al
(1995)
6
Ju
vig
nparae
et
al
(1996)
7
Bir
ks
et
al
(1996)
8
Bjo
rck
ampW
ast
egordma
rd(1
999)
9
Du
gm
ore
ampN
ewto
n(1
998)
10
Bjo
rck
et
al
(1992)
11
Kva
mm
eet
al
(1989)
12
Zoli
tsch
ka
etal
(1995)
13
Ju
vig
nparae
ampG
ewel
t(1
987)
14
Di
Vit
oet
al
(1999)
15
Del
ibri
as
etal
(1979)
16
Ju
vig
nparae
etal
(1987)
17
Dav
ies
et
al
(2001)
18
van
den
Bogaard
ampS
chm
inck
e(1
985)
19
Fri
edri
chet
al
(1999)
20
Bra
uer
eta
l(1
999)
21
Etl
ich
eret
al
(1987)
22
Tu
rney
etal
(1997)
23
Pate
rne
et
al
(1986)
24
Kel
ler
(1980)
25
Eir
parasup3kss
on
etal
(2000)
26
Hadeg
idaso
net
al
(2000)
27
Ale
ssio
etal
(1976)
28
Vez
zoli
(1991)
29
San
tacr
oce
(1987)
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Altogether 34 tephra layers have been reported from sediment sequences in Europeand the NE Atlantic region which date to the period between 185 and 80 14C ka BP(table 1) Because tephra layers are deposited virtually instantaneously (in geologicalterms) they enotectively represent time-parallel marker horizons within stratigraphicalsequences (Westgate amp Gorton 1981 Sarna-Wojcicki 2000 Turney amp Lowe 2001) Intheory therefore all 34 tephras could prove valuable for correlation purposes eitherin a local context or in those cases where the ash deposits have been widely dispersedbetween regional sequences In practice however very little is known about the fullgeographical dispersal of the majority of the ash layers listed in table 1 Furthermorecorrelation by tephrostratigraphy will only work if the various ash layers have wellcharacterized geochemical signatures While some geochemical data are available forthe majority of the tephras listed in table 1 the collective data are far from robustand no geochemical data have yet been published for some
Nonetheless there is mounting evidence to show that some of the tephra depositslisted in table 1 are not only geochemically distinct but are also much more widelydispersed across Europe than was initially realized Stratigraphic records of thebetter-known tephras were initially limited to observations of visible tephra layersThe development of a technique that enables detection of tephra layers that are invis-ible to the naked eye (micro-tephra) in Late Glacial sequences has greatly extendedthe area over which some of the ashes can be traced (Lowe amp Turney 1997 Turneyet al 1997 Turney 1998 Wastegard et al 1998 2000a b) Most of this research sofar has focused on micro-tephra layers originating from Icelandic centres distributedthroughout northern Europe Here we report on further development of this line ofresearch with new evidence for the occurrence of micro-tephra layers in a site insouthern Europe The results suggest that there is great potential for tracing someash layers that originated from Italian volcanic complexes over much larger tracts ofsouthern and central Europe than records of visible tephra deposits allow This inturn greatly enhances the scope for making precise correlations not only betweenparts of southern Europe but also between continental and marine (MediterraneanSea) sequences
2 Micro-tephra extraction techniques
Micro-tephra horizons are composed of glass shards that are generally between 80and 24 m m (long axis) in size and that are present in such low concentration insedimentary sequences that they can only be detected by the use of a particle sep-aration technique Several factors inreguence the concentration of shards such as dis-tance from the volcanic source precipitation patterns during the eruption and sub-sequent tephra dispersal and sedimentary processes within the catchment In someterrestrial sequences micro-tephra horizons with a peak concentration (peak con-centration tends to coincide with the shy rst occurrence of glass shards in a sedimentsequence which is then taken to mark the time of maximum ash deposition) as lowas 10 shards cmiexcl3 has been conshy rmed whereas other sites have recorded as muchas 8000 shards cmiexcl3 (Turney et al 1997) In complete contrast tephra horizons inthe GRIP ice core have been identishy ed based on a single glass shard only (Gronvoldet al 1995)
Enotective separation techniques for the detection and isolation of tephra particlesfrom sedimentary sequences have been developed These include ashing of organic
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776 S M Davies and others
matter (Pilcher amp Hall 1992) digestion of biogenic and opaline silica (Rose et al 1996) the use of magnetic properties of ash layers (see for example Oldshy eld et al 1980 van den Bogaard et al 1994 Pawse et al 1998) X-ray analysis (Dugmore ampNewton 1992) and a density separation (regotation) technique (Turney 1998) Den-sity separation has proved exceedingly useful for the detection of small glass shardspresent in low concentrations in mineral-rich Late Glacial sediments This involvesthe separation and concentration of particles of predetermined specishy c gravity withthe use of a heavy liquid and subsequent identishy cation of glass shards with the useof a polarizing light microscope (for further details see Turney (1998)) This methodhas been particularly successful in the detection of tephras of rhyolitic compositionthat have a specishy c density of 2325 g cmiexcl3 (Lowe amp Turney 1997 Turney et al 1997 2001 Turney 1998 Wastegard et al 1998 2000a b) It is this technique thathas resulted in the wider recognition of micro-tephras in Europe as discussed below
3 Geochemical ` ngerprintingrsquo of tephra layers
The 34 tephras listed in table 1 have originated from four major volcanic complexesIceland the Massif Central in central France the Eifel district near Bonn and threevolcanic centres in Italy (the Campanian group Etna and the Aeolian Islands (seeshy gure 2)) An important matter to resolve is the extent to which the various magmasand ashes generated by these volcanic complexes can be geochemically shy ngerprintedThis is especially important in the case of tephras which have originated from thesame volcanic centre in which there may have been limited geochemical evolution ofmagmas over time In this section we summarize the approach generally adopted todetermine the geochemical character of visible and micro-tephras as background tothe geochemical data summarized in table 1 In the subsequent section of the paperwe review the present state of knowledge concerning all 34 tephras listed in table 1
Glass shards formed during the rapid cooling of magma are thought to have acomposition that is representative of the bulk geochemistry of the magma (Barker1983) hence widely dispersed glass particles are regarded as the most appropriateconstituents of pyroclastic material for geochemical analysis If a tephra deposit canbe shown to have a distinct geochemical signature then it can be used to correlatethe stratigraphic units in which it occurs (tephrostratigraphy) as well as to datethese units (tephrochronology) if the ages of the tephras are known (Westgate ampGorton 1981) A key element of building a tephrostratigraphical framework there-fore is to establish as rigorously as possible the geochemical composition of theindividual tephras used in its construction Robust and directly comparable geo-chemical datasets are dimacr cult to assemble for glass however because it is highlyunstable material particularly prone to sodium mobilization
The technique most widely employed to establish the geochemical signature of atephra is electron probe micro-analysis (EPMA) This enables grain-discrete determi-nations of the major elements within an individual glass shard which is of particularbeneshy t in the analysis of micro-tephra layers which generally contain glass particlesin low concentration The glass surface is bombarded with an electron beam and theX-ray energy produced is unique to each element while the intensity of the signalemitted is proportional to the amount of that element in the glass shard (Hunt amp Hill1993) Measurement can be by either energy dispersive spectrometry (EDS) or wave-length dispersive spectrometry (WDS) EDS has a lower precision mainly because
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European tephrochronological framework for Termination 1 777
N
0 500 km
Confirmed records of Vedde Ash (visible occurrences)
New records of Vedde Ash from flotation method
Extended area of Vedde Ash detection (micro-tephra)
Known area of Laacher See Tephra (visible occurrences)
Confirmed records of Neapolitan Yellow Tuff (visible occurrences)
New record of Neapolitan Yellow Tuff from flotation method
Known area of Neapolitan Yellow Tuff
Volcanic centres of particular relevance to this study
Other major volcanic centres in Europe
Figure 2 Location of the principal volcanic centres that were active during Termination 1 andthe Early Holocene The known distribution of the Vedde Ash (VA) Laacher See (LST) andNeapolitan Yellow Tureg (NYT) are shown
the behaviour of each element cannot be monitored independently during measure-ment and so this approach fails to detect for example any signishy cant mobilizationof sodium during the bombardment process (Hunt amp Hill 1993) Although WDSrequires a higher beam current and a longer counting time than EDS the formeronoters the distinct advantage of sequential acquisition of elemental data so that thedegree of sodium loss can be tracked The morphology of individual glass shards canalso distort EDS data a problem that is reduced when using WDS because for thisprocedure glass shards are mounted in an epoxy resin and polished to provide aregat surface for analysis Hence data should always be obtained using WDS whereverpossible
Even when WDS is used as a common tool for determining the geochemical spectraof samples aberrant results can arise that inreguence data comparisons For examplesome glass shards may contain tiny crystalline inclusions of feldspar and these shouldbe avoided when selecting surface points for analysis (Hunt amp Hill 2001) Hunt amp Hill
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778 S M Davies and others
6
4
2
40 50 60 70 80
K2O
(
)
SiO2 ()
Laacher See
Iceland
Veidivoumltn-Dyngjufjoumlll
Katla (basalt)
Grimsvoumltn-Kverkfjoumlll
Hekla
Katla (rhyolitic)
0
Icelandic volcanic centres8
10
Massif Central
Etna
Campanian
Figure 3 Bi-plot of SiO2 and K2 O concentrations in tephras derived from the main Europeanash provinces (modimacred after Mangerud et al 1984) The Campanian Massif Central and Etnaconcentrations are based on the data presented in table 1
(2001) have concluded that small variations in the laboratory procedures employedto determine glass chemistry can lead to misidentishy cation of sources for glass shardsand give an example of shards with a Jan Mayen provenance wrongly attributedto an Icelandic source Clearly there is a need for standardization of laboratoryprocedures and while a number of recommendations have recently been advocated(Froggatt 1992 Hunt amp Hill 1993 Hunt et al 1998) there is still some variation inlaboratory and operator practice (Hunt amp Hill 1996) Standardization is also requiredin the form in which results are presented to ensure comparability Normalizationof the data to 100 a practice employed by some researchers can obscure poorresults and hence lead to incorrect comparisons (Hunt amp Hill 1993) However othersargue that it may actually facilitate comparisons between samples by removing thedistorting enotects of the water component contained in glass shards (see for exampleFroggatt 1992) The majority of the published Italian and some of the Eifel datahave been normalized while those from other parts of Europe have not and hencedata comparisons are not always straightforward
Table 1 provides mean values and standard deviations for major oxide concentra-tions obtained from those tephras for which data are presently available The tableincludes previously unpublished WDS results for the Neapolitan Yellow Tunot (NYTdiscussed in x 4 below) and for the Mercato Tephra While individual tephra layersmay be geochemically distinct the geochemical envelopes representing the collectivedata obtained from all of the tephras assigned to each major volcanic province showsignishy cant overlaps as is illustrated in the bi-plots and ternary plots (shy gures 3 and 4)of selected oxide concentration data It is clear therefore that measurement of majoroxide concentrations does not satisfactorily discriminate between some tephras orig-inating from dinoterent volcanic centres (as noted by van den Bogaard amp Schmincke(1985) and Frezzotti amp Narcisi (1996) with respect to Eifel and Italian tephras)nor of tephras of dinoterent age originating from the same volcanic centre (Bond et
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European tephrochronological framework for Termination 1 779
40 50 60 70 80
K2O
(
)
SiO2 ()
shyshyshyshy
shy
shyshy
shyshyshy
shy
shy
shy
shy
reg
reg regreg
regregregregreg regregregregreg
FF
F
ll
l
l
4 8 12 16
reg
regreg
regreg
regregreg
regreg
regregreg
shy
F
l shyshyshyshyshy shyshyshyshyshyshy
F
F
l
ll
FeO ()
TiO
2 (
)
reg
l
Iceland
Eifel
F
shy ItalyMassif Central
100
80
60
40
20
100
80
60
40
20
100 80 60 40 20
CaO
FeO
K2O
regregreg
reg
reg
reg
reg
reg
reg
regregreg
shyF
F
F
regreg
l
lllshy
shyshyshy
shyshyshy
l
0
2
4
6
8
10
0
1
2
3
4
5
regreg
regreg
regreg
regreg
regreg
reg
reg
regreg
l
l
ll
shy
shyshy
shyshy
shy
shyshy
FF
F
100
80
60
40
20
100
80
60
40
20
100 80 60 40 20
K2ONa2O
CaO
(c) (d)
(a)
(b)
Figure 4 Plots of selected geochemical data obtained from tephras of Termination 1 age (seetable 1) (a) Bi-plot of mean SiO2 and K2 O values (b) Bi-plot of mean FeO and TiO2 values(c) Ternary plot indicating variations in the proportions of FeO CaO and K2 O (d) Ternaryplot indicating variations in the proportion of CaO Na2 O and K2 O
al 2001) Individual tephra layers are presently assigned to a particular volcanicevent on the basis of a combination of criteria usually including examination of thephysical properties (eg refractive index and surface detail of the glass shards) thestratigraphic position of the layer and independent assessment of the age of the layeras well as any geochemical data that may be available The construction of a tephro-stratigraphical scheme would clearly beneshy t from the application of a more diagnostic
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780 S M Davies and others
geochemical tool One approach that has promise is the analysis of trace and rareearth elements using an ultraviolet laser ablation inductively coupled plasma massspectrometer (UV-LA-ICP-MS) (Pearce et al 1996 1999 Eastwood et al 1999)This approach has been applied successfully to analysis of tephras of Mid-Holoceneage but not yet to tephras that fall within the period of interest here
4 Tephra layers in Europe and the North Atlantic regiondated to between 185 and 80 14C ka
(a) Icelandic province
The Icelandic volcanic systems are divided into three main groups based on theirgeochemical characteristics tholeiitic basalts transitional alkali basalts and alkaliolivine basalts (Jakobsson 1979) Collectively magmas from the Icelandic provincespan a wide geochemical spectrum although individual volcanic centres have tightgeochemical distributions (shy gure 3) for four of the main centres Grimsvotn-Kverfjolland Veidvotn-Dyngjufoll which form part of the northern (tholeiitic) volcanic zoneand Hekla and Katla which fall within the eastern (alkali olivine basalt and transi-tional alkali basalt) volcanic zone (Haregidason et al 2000) These appear to be thekey centres for the tephras listed in table 1 that have been assigned an Icelandicorigin
One of the best-known and most widely dispersed tephra horizons in northernEurope that has an Icelandic origin is the Vedde Ash (VA) which was depositedca 103 14C ka BP (Birks et al 1996 Wastegard et al 1998) within the GS-1Younger Dryas chronozone This ash is believed to originate from the Katla complexwithin the transitional alkali basalt province (Mangerud et al 1984 Lacasse et al 1995) in the south of the island The ash has a bimodal geochemical composition (rhy-olitic and basaltic) which is thought to reregect derivation from two separate magmachambers Studies of recent volcanic events in Iceland have shown that the mostexplosive eruptions generating the largest amounts of tephra occur in this tran-sitional alkali basalt province (Haregidason et al 2000) It is also believed that thewidespread distribution of this ash was caused by the development of co-ignimbriteash plumes during an ignimbrite-forming eruption (Lacasse et al 1995)
Layers of VA that are visible to the naked eye have been found in lake sediments inwestern Norway (Mangerud et al 1984) and the Inner Hebrides Scotland (Davies etal 2001) and in marine cores throughout the NE Atlantic (see for example Kvammeet al 1989 Lacasse et al 1995) in the northern North Sea (Long amp Morton 1987)on the Iceland plateau (Ruddiman amp McIntyre 1981 Sejrup et al 1989) and on theeast Greenland continental margin (Stein et al 1996) The distribution of the VAin North Atlantic marine sequences is characterized by an arcuate lobe extendingsouthwest from the Denmark Strait and curving eastwards to mid-latitudes in theNorth Atlantic (Lacasse et al 1995) This strongly suggests deposition from raftedice which was displaced to the southwest and south in a circulating counterclockwisegyre (Ruddiman amp Glover 1972) This may well reregect Katlarsquos close proximity tothe southern coast of Iceland with the Vedde tephra being deposited on ice thatcalved directly into the North Atlantic (Haregidason et al 2000) However depositionvia the atmosphere almost certainly took place as well as is indicated by the recentdiscoveries of rhyolitic VA in micro-tephra form in several sites in Scotland (Turneyet al 1997) southern Sweden (Wastegard et al 1998 2000a) and western Russia
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European tephrochronological framework for Termination 1 781
(Wastegard et al 2000b) A more recent discovery of a relatively high concentrationof rhyolitic VA glass shards in the northern Netherlands indicates that the ash maywell have been dispersed much further south than previously thought (S M Davies2002 unpublished work) Finally glass shards assigned to the VA have also beendiscovered in the GRIP ice core and dated to 11 980 sect 80 GRIP yr BP (Gronvold etal 1995) This discovery is extremely important for it indicates that the VA maywell provide a reliable time-parallel marker horizon between ice-core marine andterrestrial records
Two other important Icelandic ash layers the Borrobol and Saksunarvatn Tephraswere deposited near the beginning and end of the Last TerminationEarly Holoceneinterval respectively The Borrobol Tephra was discovered for the shy rst time in lakesediments in several sites in Scotland and as yet is known only in micro-tephra formIt has been dated in Scottish sites to ca 123 14C ka BP (Turney et al 1997) Whatis thought to be a contemporaneous tephra has been detected in marine sedimentson the North Icelandic shelf (Eirplusmn ksson et al 2000) This certainly has a very similargeochemical composition to those reported from Scotland but the horizon in whichit was discovered on the North Iceland plateau has been dated to 134 14C ka Theage discrepancy between the Scottish and Icelandic Borrobol Tephra layers may wellreregect the inreguence of a marine reservoir error although the possibility that severaltephras with similar geochemical composition were erupted over a period exceeding1000 yr cannot be ruled out (Larsen 2000)
The Saksunarvatn Ash appears to have been one of the largest Holocene eruptionsin Iceland It has a tholeiitic basaltic composition which is considered to indicate anorigin in the Grimsvotn or Kverfjoll complex (shy gure 3) (Mangerud et al 1986) Layersof this ash have been identishy ed in sites on the Faroe Islands (Mangerud et al 1986Dugmore amp Newton 1998 Wastegard et al 2001) the Shetland Isles (Bennet et al 1992) northern Germany (Merkt et al 1993) western Norway (micro-tephra) (Birkset al 1996) and in the GRIP (Gronvold et al 1995) and NordGRIP ice cores (S MDavies 2002 unpublished work) It has been dated to between 9060 and 8930 14C kaBP (Birks et al 1996) in Norway and to ca 10 240 sect 30 GRIP yr BP in the GRIPice core (Gronvold et al 1995) The Saksunarvatn Ash may thus provide a secondimportant widespread time-parallel marker between ice-core marine and terrestrialrecords
Other Icelandic tephras of rhyolitic amacr nity are less well known in terms of theirdistribution and geochemical variation The Hogstorpsmossen Tephra reported fromSweden (Bjorck amp Wastegard 1999) and the L3754 tephra discovered in the FaroeIslands (Dugmore amp Newton 1998) are known from single sites only and so theirpotential for tephrostratigraphy is uncertain at present Furthermore the geochem-ical spectrum of the Hogstorpsmossen Tephra is based on a small dataset with lowanalytical totals
A number of tephras of basaltic composition have originated from Iceland buttheir distributions are largely conshy ned to Iceland or to marine cores collected fromclose to the Iceland coast or in the North Atlantic These include the tephras listedas 1-THOL-1 1-THOL-2 KOL-GS-2 GS-2BAS-1 GS-2BAS-2 GS-2BAS-3 andGS-2BAS-4 in table 1 (Kvamme et al 1989 Bjorck et al 1992 Eirplusmn ksson et al 2000 Haregidason et al 2000) The shy rst two in this list are tholeiitic basaltic tephrasassociated with the VA in a complex series of tephras collectively termed NorthAtlantic Ash Zone 1 (NAAZ1) which has been detected in numerous marine cores
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from the North Atlantic Initially thought to represent a single eruption analysisof high-resolution sediment sequences from Lake Torfadalsvatn in northern Iceland(Bjorck et al 1992) the Hebridean Shelf near NW Scotland (Austin amp Kroon 1996)the St Kilda Basin (Hunt et al 1995) and the open North Atlantic (Bond et al 2001)has demonstrated that NAAZ1 comprises a series of distinct ashes that probablyreregect separate eruption events 1-THOL-1 is thought to originate from Veidivotn(shy gure 3) while Grimsvotn may have been the source of 1-THOL-2 (Kvamme et al 1989)
KOL-GS-2 is also of tholeiitic basaltic composition but is thought to originatefrom the Kolbeinsey Ridge system (Eirplusmn ksson et al 2000) To date this tephra hasbeen detected in one marine core only within the same record on the North Ice-landic shelf as that from which the correlative of the Borrobol Tephra was alsoreported (Eirplusmn ksson et al 2000) GS-2BAS-1 to GS-2BAS-4 are of uncertain ori-gin but are thought to have been deposited at roughly the same time as KOL-GS-2(ca 134 14C ka BP (Haregidason et al 2000))
The limited distribution of these basaltic tephras a feature that is not unique toIcelandic basaltic material may reregect two factors the relative magnitude of the vol-canic eruptions from which they were derived and the limited aerial transportationof basaltic glass which is denser than rhyolitic material However a rather surpris-ing recent discovery is that of visible basaltic VA in a site on the Isle of Skye inthe Inner Hebrides Scotland (shy gure 5) (Davies et al 2001) All other occurrencesof VA in Scotland are exclusively of rhyolitic material and in micro-tephra formonly (Turney et al 1997 Turney 1998) Clearly basaltic tephra must have beentransported subaerially as far south as Skye and the reason why it has not beendetected at other sites in Scotland is puzzling We suspect that this partly reregectsthe laboratory methods employed to separate glass shards present in low concentra-tion within a micro-tephra layer from the host sediment The technique used is adensity-separation (regotation) procedure (Turney 1998) and as basaltic shards havea specishy c density similar to quartz one of the most abundant minerals in lake sedi-ments of Late Glacial age basaltic material is dimacr cult to detect using this methodThis hypothesis is currently under investigation and alternative detection methodsare being explored including magnetic separation (Mackie et al 2002)
Several other events listed in table 1 that are of probable Icelandic origin includetephras recorded in the GRIP ice core including visible (eg the `Black Featherrsquo)tephras as well as uncertain tephras inferred from distinct Ca peaks (S Johnsen2001 personal communication) No glass shards have yet been detected in the latterbut a volcanic origin is assumed because high Ca peaks are associated with knowntephras in other Greenland ice cores (S Johnsen 2001 personal communication)These are referred to as `unknownrsquo in table 1 No geochemical analyses are availablefrom these horizons so their origin must remain speculative but a possible source isIceland in view of its proximity to the Greenland ice sheet and assumed atmosphericcirculation patterns
(b) Eifel province
There are two prominent tephra events dated to the Termination 1Early Holocenetime-span that originated from the Eifel province the Laacher See Tephra (LST)and the Ulmener Maar Tephra (UMT) Visible occurrences of the LST indicate that
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European tephrochronological framework for Termination 1 783
Vedde Ash
615 625 635 645 655depth (cm)
organic lake mudsHolocene
silty clayGS-1Younger Dryas
organic lake mudsGI-1Alleroslashd
100 microm
(a)
(b)
Figure 5 (a) Photograph of the visible VA layer discovered at Loch Ashik Isle of Skye InnerHebrides Scotland (b) Light microscope photograph showing the rich content of basaltic shards(examples are indicated by the arrows) within this layer (8024 m m size fraction)
this ash was dispersed over much of central Europe (van den Bogaard amp Schmincke1985 Friedrich et al 1999 Litt amp Stebich 1999) The LST is dated by radiocarbonto ca 110 14C ka BP (van den Bogaard amp Schmincke 1985) and to 11 063sect12 14C BP(Friedrich et al 1999) by varve chronology to 1288 varve ka BP (Brauer et al 1999Litt et al 2001) and by ArAr dating to 129 ka cal BP (van den Bogaard 1995) Ithas a phonolitic composition and is thought to have originated from a plinian andphreatomagmatic eruption with the distal ash being carried in three distinct plumesone to the northeast towards Poland one to the west and the third to the southcovering the Jura Mountains and north Italy (van den Bogaard amp Schmincke 1985Juvigne et al 1995 Bossuet et al 1997) This pattern is thought to reregect altitu-dinal variations in the predominant wind direction Sedimentary sequences near thevolcanic source indicate that the LST consists of three main layers which represent
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784 S M Davies and others
dinoterent eruption phases These are grouped together as the Laacher See TephraFormation but the three individual units can be traced within and between a seriesof depositional fans The geochemical data obtained from these three LST layersshow signishy cant variations as reregected in the ternary plots (shy gure 4)
The Early Holocene Ulmener Maar Tephra (UMT) is of rhyolitic composition andappears to be restricted to sites in Germany though this conclusion is also based onrecords of visible tephras only It is dated to ca 956 14C ka BP and to 110 varve ka(Zolitschka et al 1995 Litt et al 2001)
(c) Massif Central province
The Massif Central tephras are mainly of basaltic trachyandesitic compositionwhich is distinct from the other ash provinces (shy gures 3 and 4) and their known dis-tributions are mostly conshy ned to the Massif Central region The ages of the MassifCentral tephras are based on radiocarbon dates obtained from mire and lake sedi-ments which `bracketrsquo the tephras The La Nugsup3ere Tephra with an age of 114 14C kaBP is the oldest Massif Central tephra identishy ed so far within the time-span of inter-est (Etlicher et al 1987 Juvigne et al 1996) The two Godivelle Tephras (5 and 4)are close in age but extensive radiocarbon dating suggests distinct ages of 107and 103 14C ka BP respectively (Juvigne et al 1996) The age of the Puy de DomeTephra is less certain as the estimate is based on only one radiocarbon date froma site in the southern Chaplusmn ne des Puys (table 1) This tephra is thought to havea trachyte composition (Juvigne 1993) although no major element concentrationshave yet been published
The ChopineKilianVasset tephras are thought to be derived from three separateEarly Holocene eruptions although the stratigraphic succession is not known atpresent These trachytic tephras have been radiocarbon dated to ca 854sect150 14C kaBP but are thought to have erupted separately within ca 260 yr (Juvigne et al 1996) This series of tephras is considerably more widespread than the others fromthe region having been identishy ed as far east as the Jura Mountains (Martini amp Duret1965 Martini 1970) Some other ash falls that originated from the Chaplusmn ne des Puysappear to be of local importance only (Vernet et al 1998 Vernet amp Raynal 2001)Geochemical data are currently available for only three of the Massif Central tephrasand so far as is known no attempt has yet been made to identify these tephras inmicro-tephra form
(d ) Italian provinces
The Italian tephras from this period can be assigned to three main volcanic com-plexes the Campanian volcanic shy elds around Naples Etna on Sicily and the AeolianIslands The Campanian complex which includes the Phlegrean Fields Vesuviusand Ischia is mainly trachytic in composition with a geochemical spectrum that isquite distinct from those of the Etna complex and of the Aeolian Islands (shy gure 3)Tephras originating from one or more of these three complexes have been detectedin marine cores from the Tyrrhenian and Adriatic seas as well as other parts of theMediterranean Sea (Keller et al 1978 Paterne et al 1986 1988 1990 Langone etal 1996) and in lake sequences in southern Italy such as Lago Grande di Monticchio(Newton amp Dugmore 1993 Narcisi 1996 Allen et al 1999) and central Italy such asLago Albano near Rome (Calanchi et al 1996) Some work has also been conducted
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European tephrochronological framework for Termination 1 785
in or close to the volcanic source areas in an attempt to establish the full sequenceof volcanic eruptions during the Late Quaternary (see for example Di Vito et al 1999) There are nine Italian tephras reported from marine and lake sequences thatdate from the period between 185 and 80 14C ka BP In all instances the recordsare of visible layers of tephra The ages of some of these are poorly established atpresent with conregicting data obtained from dinoterent sites The ages suggested intable 1 are those favoured in the most recent publications but these may requirere-assessment in the light of future research
The two oldest known tephras in the time-period of interest are the L9 and Green-ish Tephras both recorded as separate features within the annually laminated Lagodi Monticchio maar sequence The lowest of the two L9 is considered to be the cor-relative of the `basalrsquo plinian eruption of Vesuvius (Narcisi 1996) Age estimates ofa palaeosol that underlies the Vesuvius tephra sequence are ca 1617 14C ka BP forthis event (Delibrias et al 1979) L9 has a trachytic composition very similar to theGreenish Tephra (table 1) However L9 which is also a product of Vesuvius is foundstratigraphically below the Greenish Tephra in the Lago di Monticchio core TheGreenish Tephra is dated in the Monticchio sequence to 17 560 varve yr BP (Allenet al 1999) and has a calibrated radiocarbon age estimate of 17 830 sect 300 cal BP(Andronico et al 1995) Both tephras have a dominantly eastwards dispersal basedon the occurrences of visible layers (Santacroce 1987 Narcisi 1996) Both tephrasalso have a trachytic composition and as can be seen from table 1 the reportedgeochemical spectra are very close indeed with the standard deviations overlappingfor almost every major element This could present problems for tephrostratigra-phy where only one of the tephras is evident in a sediment sequence in particularbecause they are so close in age This is a good example of where an analysis oftrace and rare earth elements might be required to make a clear distinction betweentephras with very similar major oxide concentrations
The Y-1 Tephra also termed the Biancavilla Montalto Ignimbrite (Vezzoli 1991)is a product of Etna and has been identishy ed as a visible benmoritic tephra horizonthroughout the central Mediterranean (Paterne et al 1988) including central Italyand the Adriatic Sea (Vezzoli 1991 Narcisi 1993 Calanchi et al 1996) It has anestimated age of ca 140 14C ka BP The Unita dei Tefra Superiori tephra which hasbeen detected as far east as Lago di Monticchio in south-central Italy (Narcisi 1996)is also dated to ca 140 14C ka BP (Alessio et al 1976) but it is thought that thesource of this tephra lies in the Phlegrean Fields No geochemical data are availablefrom the presumed source region|the data reported in table 1 were obtained fromthe Lago di Monticchio record (Narcisi 1996)
The NYT which is equivalent to the C-2 tephra reported from various marinesequences has also been traced throughout central Italy and the Adriatic Sea (Pat-erne et al 1988 Calanchi et al 1996 Di Vito et al 1999) (shy gure 2) In the centralApennines region it formed the parent material for a soil that started to developat the beginning of the Holocene period (Frezzotti amp Narcisi 1996) Also originatingfrom the Campi Flegrei caldera it is dated to ca 120 14C ka BP (Di Vito et al 1999) Published geochemical data based on EDS indicate three dinoterent geochemicalpopulations varying from latite to phonotrachyte in composition (Orsi et al 1992Paterne et al 1988) (table 1) We report in x 4 of this paper on new data obtainedfrom the NYT by WDS and it is the mean of these new data that is included intable 1 Comparisons with the previously published EDS data are provided (table 1)
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786 S M Davies and others
The new data indicate clearly that the NYT originated from the Campanian volcaniccentre
In the interval between the dispersal of the NYT (ca 120 14C ka BP) and 95 14Cka BP there appear to have been as many as 34 eruptions in the Campi Flegrei caldera(Di Vito et al 1999) Of these only one appears to have been detected widely in theregion the Pomici Principali (also termed the Agnano Formation or C-1 tephra inmarine records (Paterne et al 1988) This was the product of the highest magnitudeeruption from this epoch and is dated to between 976 sect 300 and 1032 sect 50 14C kaBP (Delibrias et al 1979 Di Vito et al 1999) or to 122 varve ka BP based on theMonticchio varve chronology (Allen et al 1999) It is trachytic in composition andappears to have had a mainly eastwards dispersal
The Mercato Tephra dated to ca 80 14C ka BP and originally analysed usingEDS has a phonolitic composition and is believed to have been generated by Vesu-vius (Paterne et al 1988) New WDS data obtained from reference samples col-lected from an exposure to the west of Naples support these conclusions (table 1 andAppendix A) The silica content of the WDS analyses are ca 3 lower than thoseobtained using EDS (table 1) which may reregect the fact that the EDS data werenormalized
The only tephra listed in table 1 that is thought to have originated from the AeolianIslands is the Pollara pumice also referred to as the E2 tephra in marine sequences(Paterne et al 1986 1988) The limited geochemical data available so far suggest itto be the only Italian tephra listed in table 1 that is rhyolitic in composition Littlemore is known about this ash which has not been recorded extensively except thatits age is estimated to be ca 130 14C ka BP (Keller 1980)
5 Extending the known distributions of European tephras
Figure 2 summarizes schematically the known distributions of three of the tephrasreferred to in the preceding section the VA the LST and the NYT Following theintroduction of a laboratory method that enables the detection of micro-tephra parti-cles in mineral-rich sediment the VA has been traced to sites that are located muchfarther south (into The Netherlands) and east (as far as St Petersburg) than thedistribution limits based on occurrences of visible layers of the ash As a result con-tinental sequences over a much larger area in northern Europe can now be correlateddirectly with marine and ice-core records using the VA as a time-parallel marker
This suggests therefore that other prominent ash layers such as the LST andNYT should also be detectable over larger tracts of Europe than is presently thecase if suitable sites are examined for the presence of micro-tephra horizons To testthis assertion we examined lake sediment deposits of Last Termination age froma site in the northern Apennines in order to establish whether the NYT could bedetected in micro-tephra form The site selected Prato Spilla `Crsquo lies well to thenorth of the localities in central and southern Italy and in the Adriatic Sea fromwhich visible records of the NYT have been reported Prato Spilla `Crsquo lies at an alti-tude of ca 1350 m in the Appennino Parmense ca 60 km south of Parma and 15 kmeast of Pontremoli The site contains a continuous sediment sequence spanning theLast Termination and most of the Holocene Detailed pollen and coleopteran strati-graphical records which have been radiocarbon dated have been published for thissite (Lowe 1992 Ponel amp Lowe 1992 Lowe amp Watson 1993)
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European tephrochronological framework for Termination 1 787
Figure 6 Light microscope photograph of an NYT glass shard from Prato Spilla Crsquosequence assigned on geochemical grounds to the NYT
The methods adopted for sub-sampling of the Prato Spilla `Crsquo sequence for thequantishy cation of glass shard concentrations and for subsequent electron microprobeanalysis of selected glass shards followed those described elsewhere (Turney 1998)In summary contiguous samples of 1 cm stratigraphic interval were extracted fromthe sequence to establish presenceabsence of glass shards Each of the 1 cm3 blocksin which tephra particles was detected was then examined with more care andshard concentrations were quantishy ed for each sub-sample Micro-tephra particleswere detected in shy ve samples (shy gure 6) but were predominantly clustered around500 cm in the part of the sequence assigned on pollen-stratigraphic grounds to theLate Glacial Interstadial or the `Allerfrac12drsquo|indeed the part of the succession in whichthe NYT would be expected to occur Peak concentrations of micro-tephra particlesreach 225 shards cmiexcl3 and are conshy ned to a single 1 cm thick sample in the sequencewhich probably represents the time of maximum deposition of the ash
Electron microprobe measurements based on WDS were obtained from the surfacesof 21 separate glass shards extracted from the sample with peak shard concentrations(Appendix A) Since only EDS measurements were available for the NYT prior to thepresent study we also obtained WDS measurements from 17 shards extracted fromthe visible layer of NYT that is exposed on Procida Island which lies in the type-locality for the NYT close to the city of Naples (Appendix A) The results providenot only a more comprehensive geochemical dataset for the NYT than was previ-ously available but also a consistent basis for comparison with the Prato Spilla `Crsquodataset All of the WDS data reported here (Appendix A) were measured at the samelaboratory (Tephrochronology Analytical Unit University of Edinburgh) using thesame sample pretreatment and preparation protocol The WDS results for the NYTdinoter to a minor degree from the EDS results (table 1 and Appendix A) especiallywith respect to the amounts of silica aluminium and calcium measured The EDS
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788 S M Davies and others
4 8FeO ()
TiO
2 (
) Neapolitan Yellow Tuff(Procida)Neapolitan Yellow Tuff(Prato Spilla lsquoCrsquo)
0
1
2
3
40 50 60 70
MgO
(
)
SiO2 ()
K2O
(
)
40 50 60 70
0
04
08
4
8
12
SiO2 ()
(a)(b)
(c)
Figure 7 Bi-plots of SiO2 K2 O SiO2 MgO and FeOTiO2 for the WDS analyses obtainedfrom glass shards of the NYT from Procida (Naples) and Prato Spilla Crsquo Means and standarddeviations are shown
results show a higher degree of statistical scatter than the WDS measurements whichmay reregect the fact that the data were normalized combined with the inreguence ofvariation in water content between shards
There is a very close correspondence between the WDS data for the Prato Spilla `Crsquomicro-tephra shards and those obtained from the type-material near Naples (shy g-ure 7) The geochemical data strongly suggest therefore that the NYT is representedat the Prato Spilla `Crsquo site by a discrete layer of micro-tephra particles This conclu-sion is compatible with the pollen-stratigraphic data from the site and accords withage estimates for the NYT (ca 120 14C ka BP) obtained from other sites (Paterneet al 1990)
These results encourage us to believe that many if not all of the tephras listedin table 1 will be detectable over much larger tracts of Europe than is presently thecase if appropriate research is undertaken to detect layers of micro-tephra particlesin selected sites The authors are presently engaged in a major continent-wide pro-gramme of research in collaboration with a number of European research groupsdesigned to test this hypothesis The focus in this research is on those parts of Europewhere we expect to shy nd overlapping `apronsrsquo of tephra deposition originating fromthe Italian Eifel Massif Central and Icelandic provinces For example a number ofsites in parts of southern France northern Italy and perhaps western Switzerlandmay have received inreguxes of micro-tephra originating from the Italian and Eifelprovinces and perhaps also from the Massif Central Sites in parts of Germany Den-mark and southern Sweden for example may in turn have received tephra depositsfrom both of the Icelandic and Eifel provinces If this proves to be the case then thestage will be set for the construction of a tephrostratigraphical framework for Europewhich will enable Last Termination sequences to be correlated on a continent-widebasis using micro- and visible tephra layers as time-parallel stratigraphic markersFurthermore there is also the possibility that other tephras remain to be discovered
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European tephrochronological framework for Termination 1 789
those which either because of the magnitude or nature of some volcanic eruptionswere distributed over parts of Europe in micro-tephra form only
6 European tephrostratigraphy and the chronology of eventsduring the Last Termination and Early Holocene
One of the crucial issues in Late Quaternary palaeoenvironmental research thatremains to be resolved is the degree to which climatic events inferred from oceanicterrestrial and ice-core records were synchronous during the Last Termination andEarly Holocene If the ice-core records provide realistic estimates of the rates anddurations of climatic events during this period then comparisons between individ-ual records have to be enotected with at least a decadal precision The problem thispresents and the role that tephrostratigraphy can play in resolving some of thedimacr culties involved are put into perspective in shy gure 8
Figure 8 shows some of the data used to calibrate radiocarbon dates (the LakeSuigetsu and Cariaco Basin datasets) plotted against the GRIP ss08c ice-core recordof macr 18O variations The latter has been selected by the INTIMATE group as an arbi-trary and temporary standard for this period and used to deshy ne an event stratig-raphy scheme (shy gure 1) for the Last Termination (see Bjorck et al 1998 Walker etal 2001) As has been alluded to in earlier sections of this paper the uncertaintiesassociated with all of the dating methods currently employed preclude precise com-parisons of ice-core marine and terrestrial records Oceanic and terrestrial recordsmostly rely upon radiocarbon dating locally supplemented in a few cases by varvechronology Imprecisions in radiocarbon dates can arise through site-specishy c fac-tors (eg hard-water or mineral carbon errors in freshwater sequences and reservoirerrors in marine sequences) sample selection laboratory measurements of 14C activ-ity and other factors (Lowe amp Walker 2000) Further imprecision may be introducedby the calibration of radiocarbon dates since the uncertainties in the dataset usedto calibrate pre-Holocene radiocarbon dates INTCAL98 are far higher than forthe Holocene which is based on dendro-calibration (Stuiver et al 1998) There arealso uncertainties anotecting varve chronologies while the ss08c ice-core chronologyfor the Last Termination dinoters signishy cantly from the GISP2 record and indeedfrom other models of the GRIP record (Lowe et al 2001) Published comparisonsbetween ice-core marine and terrestrial records for the Last Termination seldom takeinto account the true magnitude of the dating uncertainties involved and frequentlyemploy circular reasoning
Figure 8 shows the positions on the radiocarbon time-scale of 20 of the tephrasdiscussed earlier in this paper these being the ones for which reasonably conshy dentradiocarbon age estimates can be made (though these will be subject to revised esti-mates in the future) A high number of these occur in the period 14080 14C kaBP but we conshy dently anticipate the discovery in the future of additional tephras(perhaps in micro-tephra form only) which will date to the period 185140 14C kaBP Tephras detected in the GRIP ice core over the same time-interval are plottedon the calendar time-scale in shy gure 8 By providing key `time-linesrsquo between recordstephrostratigraphy can help to resolve some of the dating uncertainties referredto earlier by for example enabling direct comparisons of discrepant age estimatesobtained using dinoterent methods (cf Litt et al 2001) It can also provide estimatesof the magnitudes of the reservoir errors that anotected various marine sectors at dif-
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790 S M Davies and others
-44
-40
-36
-32
cale
ndar
yea
rs B
P
8000
9000
10 0
00
11 0
00
12 0
00
13 0
00
14 0
00
15 0
00
16 0
00
17 0
00
18 0
00
14C age (BP)
VA
SA
Un
Un
Un
Un
Un
BF
Hol
ocen
eG
S-1
GI-
1aG
I-1b
GI-
1cG
I-1d
GI-
1eG
S-2
aG
S-2
bG
S-
2c
Bor
robo
l
La
Nug
egravere
Laa
cher
See
God
ivel
le 5
amp I
-TH
OL
-2
Puy
de D
ocircme
I-T
HO
L-1
Saks
unar
vatn
Houmlg
stor
psm
osse
nU
lmen
er M
aar
amp L
3574
radiocarbon dated European tephra horizons
Cho
pine
Kili
an V
asse
tM
erca
to
God
ivel
le 4
Pom
ici P
rinc
ipal
i amp V
edde
Polla
ra p
umic
eK
OL
-GS-
2 amp
GS
-2B
AS-
12
3
GS
-2B
AS-
4 U
nita
dei
Tef
raSu
peri
ori amp
laye
r Y
-1
Gre
enis
h
L9
20 0
0018
000
16 0
0014
000
12 0
0010
000
-44
-40
-36
-32
800
600
400
200 0
GISP2 volcanicsulphate conc (ppb)
1000
Nea
polit
an Y
ello
w T
uff
GISP2 18O (permil) dGRIP 18O (permil) d
Figure 8 For description see opposite
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European tephrochronological framework for Termination 1 791
ferent times through a comparison of radiocarbon dates obtained from marine andterrestrial horizons in which the same tephra has been detected (see for exampleAustin et al 1995 Bondevik et al 2001 Haregidason et al 2000) Tephrostratigraphymay provide an independent test of suggestions that some of the climatic changesduring the Last Termination were time-transgressive as illustrated for some appar-ently contrasting climatic trends in Iceland Britain and NW Russia (Lowe 2001) Ofparticular importance as far as establishing `leadsrsquo and `lagsrsquo in climatic changes isconcerned are the tephra records from the Greenland ice cores The discovery of theVedde and Saksunarvatn ashes in the GRIP record (Gronvold et al 1995) alreadyprovides a basis for making direct comparisons between marine terrestrial and ice-core records It is a matter of some urgency that the incidence of tephra depositsin the Greenland ice cores be more fully explored in the hope that this will lead tothe recognition of additional time-parallel links between the ice-core records on theone hand and oceanic and terrestrial records on the other An investigation of thenew NordGRIP record for this purpose is currently in progress (S M Davies 2002unpublished data)
Finally a fuller and more reshy ned tephrostratigraphical scheme for Europe will alsohave other applications It will provide an important database for those investigatingthe timing and frequency of volcanic eruptions in Europe during the past 20 000 yror so as well as of the geochemical evolution of the dinoterent volcanic centres overthat period A fuller record of the distribution of micro-tephras may also provideinformation on atmospheric circulation patterns during the dispersal and depositionperiods as well as on the nature and altitude of the eruption columns which mayin turn provide inferences about magma viscosity
This paper is a contribution to the INTIMATE project of the INQUA Palaeoclimate Com-mission and the work is supported by a Leverhulme Trust Research project (grant allocationnumber F07537C) entitled Testing hypotheses of rapid climate change using tephrochronol-ogyrsquo SMDrsquo s contribution was completed during possession of a NERC PhD studentship(GT 0499ES162) We are extremely grateful to Dr Peter G Hill for his assistance withthe EPMA analyses at the Tephrochronology Analytical Unit University of Edinburgh We alsothank Dr G Mastrolorenzo (Vesuvius Observatory) and Miss G Swindle for assistance duringthe macreld investigations in Naples Thanks are also expressed to two anonymous reviewers forcomments on an earlier draft
Appendix A
Table 2 shows the major oxide concentrations of NYT glass shards from Procidaand Prato Spilla `Crsquo and of the Mercato Tephra from the Naples area (see x 4 forsite context) All oxides are shown as weight and total iron is expressed as FeO
Figure 8 Radiocarbon calibration curve for Termination 1 and the Early Holocene compared with theGRIP macr 18 O event stratigraphy the GRIP ss08c and GISP2 macr 18 O records (wwwngdcnoaagov) andknown tephra horizons from this period The shaded areas represent the cooler climatic episodes andare labelled with the Greenland stratotype terminology (Bjorck et al 1998) Where radiocarbon agesare reported in table 1 as a range the mean is given here Abbreviations for GRIP horizons are asfollows Un unknown (approximate positions are given (S Johnsen 2001 personal communication))SA Saksunarvatn Ash VA Vedde Ash BF Black Feather Sulphate concentrations from the GISP2record are also shown (Zielinski et al 1996) Open circles denote radiocarbon calibration data fromLake Suigetsu (Kitagawa amp van der Plicht 2000) Filled circles denote radiocarbon calibration data fromCariaco Basin assuming a marine reservoir age of 420 14 C yr (Hughen et al 1998)
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792 S M Davies and others
Tab
le2
Majo
roxi
de
con
cen
trati
on
sof
NY
Tgl
ass
shard
sfr
om
Pro
cida
an
dP
rato
Spil
laC
rsquoan
dof
the
Mer
cato
Tep
hra
from
the
Naple
sare
a(s
eex4
for
site
con
text
)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
roci
da)
1584
204
0177
634
201
106
828
635
197
5969
1W
DS
2598
603
9178
027
101
204
924
244
583
4965
8W
DS
3586
604
5173
631
100
805
924
342
183
0951
9W
DS
4583
903
9177
933
000
906
924
540
486
9958
3W
DS
5605
106
8179
126
901
204
923
243
086
1976
4W
DS
6591
704
5177
332
801
006
425
740
887
8968
0W
DS
7581
804
1178
031
501
107
125
640
086
9956
1W
DS
8589
504
2179
533
701
506
926
740
987
5970
4W
DS
9592
003
9178
135
101
007
026
443
585
7972
7W
DS
10
591
404
2174
631
601
105
723
442
482
6957
0W
DS
11
593
403
6177
131
301
506
726
439
188
5967
6W
DS
12
588
103
8176
128
100
505
525
141
583
4952
1W
DS
13
577
003
8176
533
500
807
228
140
384
8952
0W
DS
14
586
004
7179
735
300
706
827
842
984
6968
5W
DS
15
588
104
2180
629
400
505
924
937
993
0964
5W
DS
16
579
603
9178
536
501
308
228
836
087
1959
9W
DS
17
580
103
9177
631
500
907
327
039
488
9956
6W
DS
mea
n588
104
2177
631
901
006
525
940
686
9962
8
sd
(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(07
8)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 793
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
rato
Spil
laC
rsquo)
1552
105
4177
247
401
914
38
735
578
9951
1W
DS
2557
305
7179
845
701
512
640
136
581
5960
6W
DS
3595
004
4173
724
302
003
117
652
877
8950
7W
DS
4575
704
2179
433
001
406
627
043
083
6953
7W
DS
5599
904
0178
826
401
304
421
841
688
4966
5W
DS
6591
103
8177
826
601
105
022
443
888
8960
2W
DS
7565
304
5180
939
501
410
532
535
791
8962
1W
DS
8597
606
9180
826
501
604
821
546
684
6970
7W
DS
9571
805
6179
939
801
109
932
240
883
6964
7W
DS
10
588
603
7176
527
601
104
721
042
487
7953
3W
DS
11
559
404
9180
544
501
812
339
435
878
6957
2W
DS
12
594
704
0181
328
301
705
522
144
785
6967
9W
DS
13
611
103
7187
016
900
802
419
938
195
9975
8W
DS
14
599
204
4181
128
601
404
620
844
986
6971
6W
DS
15
601
204
4177
328
302
004
722
446
385
5972
1W
DS
16
595
104
5176
428
801
504
722
744
884
3962
8W
DS
17
603
704
1177
825
101
503
520
348
181
2965
3W
DS
18
558
704
5179
647
401
813
139
836
879
0960
7W
DS
19
589
602
8178
830
901
606
622
436
091
8960
5W
DS
20
553
606
3178
647
401
913
840
136
978
0956
6W
DS
21
579
004
0175
739
000
708
328
338
286
7959
9W
DS
mea
n582
804
6179
033
401
507
427
341
484
8962
1
sd
(1
87)
(01
0)
(02
7)
(09
2)
(00
4)
(03
9)
(08
0)
(04
9)
(05
0)
(07
0)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
794 S M Davies and others
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)
1575
202
7194
219
701
101
016
374
766
9951
8W
DS
2575
802
9194
523
902
201
520
273
564
5959
0W
DS
3574
301
4205
219
101
100
416
481
266
1965
2W
DS
4575
500
7206
018
002
000
415
181
669
3968
6W
DS
5580
000
9208
018
601
300
515
883
367
1975
5W
DS
6571
001
0206
016
101
600
515
078
967
1957
2W
DS
7577
501
1201
117
101
500
620
675
655
4950
5W
DS
8573
700
9212
717
101
900
815
187
564
2973
9W
DS
9580
301
3208
715
801
400
824
81
754
1968
1W
DS
10
574
400
6211
18
402
00
516
480
567
8971
6W
DS
11
577
200
7214
212
501
200
829
879
247
962
6W
DS
12
572
200
9211
217
301
501
15
980
465
9966
3W
DS
13
571
800
7210
417
402
201
16
184
467
2971
2W
DS
14
567
300
9208
916
901
400
917
383
262
5959
3W
DS
15
568
600
8205
918
202
101
414
682
666
6960
8W
DS
16
572
501
1211
318
202
01
215
884
364
5970
9W
DS
17
572
901
2212
916
502
101
215
883
667
2973
4W
DS
18
573
01
4211
716
301
801
416
83
365
5970
4W
DS
19
569
201
1207
418
602
101
414
982
964
961
6W
DS
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
3)
(04
2)
(01
3)
(00
1)
(00
2)
(01
)(0
39)
(01
1)
(02
5)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
References
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Di Vito M A Isaia R Orsi G Southon J de Vita S Drsquo Antonio M Pappalardo L ampPiochi M 1999 Volcanism and deformation since 12 000 years at the Campi Flegrei caldera(Italy) J Volcanol Geophys Res 91 221246
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Dugmore A J amp Newton A J 1998 Holocene tephra layers in the Faroe Islands Frodskaparrit46 191204
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Frezzotti M amp Narcisi B 1996 Late Quaternary Tephra derived paleosols in central Italyrsquo scarbonate Apennine range stratigraphical and paleoclimatological implications Quat Int3436 147153
Friedrich M Kromer B Spurk M Hofmann J amp Kaiser K F 1999 Paleoenvironment andradiocarbon calibration as derived from LateglacialEarly Holocene tree-ring chronologiesQuat Int 61 2739
Froggatt P C 1992 Standardisation of the chemical analysis of tephra deposits Report of theICCT working group Quat Int 1314 9396
Gronvold K Oskarsson N Johnsen S J Clausen H B Hammer C U Bond G amp Bard E1995 Ash layers from Iceland in the GRIP ice core correlated with oceanic and land sedimentsEarth Planet Sci Lett 135 149155
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798 S M Davies and others
Hadeg idason H Eirpara sup3 ksson J amp van Kreveld S 2000 The tephrochronology of Iceland and theNorth Atlantic region during the Middle and Late Quaternary a review J Quat Sci 15322
Hoek W Z amp Bohncke S J P 2001 Oxygen isotope wiggle matching as a tool for synchronisingice-core and terrestrial records over Termination 1 Quat Sci Rev 20 12511264
Hughen K A Overpeck J T Peterson L C amp Trumbore S 1996 Rapid climate changes inthe tropical Atlantic region during the last deglaciation Nature 380 5153
Hughen K A Overpeck J T amp Lehman J 1998 A new 14 C calibration data set for the LastDeglaciation Radiocarbon 39 483494
Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
Hunt J B amp Hill P G 1996 An inter-laboratory comparison of the electron probe microanalysisof glass geochemistry Quat Int 3436 229241
Hunt J B amp Hill P G 2001 Tephrological implications of beam sizesample size ereg ects inelectron microprobe analysis of glass shards J Quat Sci 16 105117
Hunt J B Fannin N G T Hill P G amp Peacock J D 1995 The tephrochronology andradiocarbon dating of North Atlantic Late Quaternary sediments an example from the StKilda Basin In The tectonics sedimentation and palaeoceanography of the North Atlanticregion (ed R A Scrutton M S Stoker G B Shimmield amp A W Tudhope) vol 90pp 227248 Geological Society of London Special Publication
Hunt J B Clift P D Lacasse C Vallier T L amp Werner R 1998 Standardisation ofelectron probe microanalysis of glass geochemistry In Proc ODP Scientimacrc Results vol 152pp 8591 College Station TX Ocean Drilling Program
Jakobsson S P 1979 Outline of the petrology of Iceland Jokull 29 5773
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Juvignparae E 1993 Contribution microa la tparaephrostratigraphie du Quaternaire et son application microa lagparaeomorphologie Mparaem Serv Explicat Cartes Gparaeol Min Belg 36 166
Juvignparae E amp Gewelt M 1987 La Narse drsquo Ampoix comme tparaephrostratotype dans la Chasup3 ne desPuys mparaeridionale (France) Bull Ass Fr Etud Quat 29 3749
Juvignparae E Kozarski S amp Nowaczyk B 1995 The occurrence of Laacher See Tephra in Pomera-nia NW Poland Boreas 24 225231
Juvignparae E Bastin B Delibrias G Evin J Gewelt M Gilot E amp Streel M 1996 Acomprehensive pollen and tephra based chronostratigraphic model for the Lateglacial andHolocene period in the French Massif Central Quat Int 3436 113120
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Keller J Ryan W B F Ninkovich D amp Altherr R 1978 Explosive volcanic activity in theMediterranean over the past 200 000 years as recorded in deep sea sediments Geol Soc AmBull 89 591604
Kitagawa H amp van der Plicht J 2000 Atmospheric radiocarbon calibration beyond 11 900 calBP from Lake Suigetsu laminated sediments Radiocarbon 42 369380
Kvamme T Mangerud J Furnes H amp Ruddiman W F 1989 Geochemistry of Pleistoceneash zones in cores from the North Atlantic Norsk Geol Tids 69 251272
Lacasse C Sigurdsson H Johannesson H Paterne M amp Carey S 1995 Source of Ash zone 1in the North Atlantic Bull Volcanol 57 1832
Langone L Asioli A Corregiari A amp Trincardi F 1996 Age depth modelling through theLate-Quaternary deposits of the central Adriatic Basin In Palaeoenvironmental analysis ofItalian crater lake and Adriatic sediments (ed F Oldmacreld amp P Guilizzoni) vol 55 pp 177196 Memorie dellrsquo Instituto Italiano di Idrobiologia
Larsen G 2000 Holocene volcanism in Iceland and tephrochronology as a tool in volcanologyIn Iceland 2000 modern processes and past environments Keele University UK
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European tephrochronological framework for Termination 1 799
Litt T amp Stebich M 1999 Bio- and chronostratigraphy of the Lateglacial in the Eifel regionGermany Quat Int 61 516
Litt T Brauer A Goslar T Merkt J Balaga K Muller H Ralska-Jasiewiczowa MStebich M amp Negendank J F W 2001 Correlation and synchronisation of Lateglacialcontinental sequences in northern Central Europe based on annually laminated lacustrinesediments Quat Sci Rev 20 12331249
Long D amp Morton A C 1987 An ash fall within the Loch Lomond stadial J Quat Sci 297101
Lotter A F Eicher U Siegenthaler U amp Birks H J B 1992 Lateglacial climatic oscillationsas recorded in Swiss lake sediments J Quat Sci 7 187204
Lowe J J 1992 Lateglacial and Early Holocene lake sediments from the Northern ApenninesItaly|pollen stratigraphy and radiocarbon dating Boreas 21 193208
Lowe J J 2001 Abrupt climatic changes in Europe during the last glacialinterglacial tran-sition the potential for testing hypotheses on the synchroneity of climatic events usingtephrochronology Global Planet Change 603 7384
Lowe J J amp Turney C S M 1997 Vedde Ash layer discovered in a small lake basin on theScottish mainland J Geol Soc Lond 154 605612
Lowe J J amp Walker M J C 2000 Radiocarbon dating the last glacialinterglacial transition(ca 14914 C ka BP) in terrestrial and marine records the need for new quality assuranceprotocols Radiocarbon 42 5368
Lowe J J amp Watson C 1993 Lateglacial and Early Holocene pollen stratigraphy of the northernApennines Italy Quat Sci Rev 12 727738
Lowe J J Birks H H Brooks S J Coope G R Harkness D D Mayle F E SheldrickC Turney C S M amp Walker M J C 1999 The chronology of palaeoenvironmental changesduring the Last GlacialHolocene transition towards an event stratigraphy for the BritishIsles J Geol Soc Lond 156 397410
Lowe J J Hoek W Z amp INTIMATE group 2001 Inter-regional correlation of palaeoclimaticrecords for the Last GlacialInterglacial transition a protocol for improved precision recom-mended by the INTIMATE project group Quat Sci Rev 20 11751187
Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
Mangerud J Lie S E Furnes H Kristiansen I L amp Liquest mo L 1984 A Younger Dryas ashbed in western Norway and its possible correlation with tephra beds from the Norwegian Seaand North Atlantic Quat Res 21 85104
Mangerud J Furnes H amp Jparaohansen J 1986 A 9000 year-old ash bed on the Faroe IslandsQuat Res 26 262265
Martini J 1970 Recherche de retombparaees volcaniques dans le sud-est de la France et la Suisseoccidentale Arch Sci 23 641674
Martini J amp Duret J J 1965 Note preliminaire sur la presence drsquo un niveau de cendres vol-caniques dans des sparaediments post-glaciaires des environs de Genmicroeve Arch Sci 18 587588
Mayewski P A Meeker L D Twickler M S Whitlow S Yang Q Lyons W B amp Pren-tice M 1997 Major features and forcing of high latitudes Northern Hemisphere atmosphericcirculation using a 110 000 year long glaciochemical series J Geophys Res 102 345365
Merkt J Muller H Knabe W Muller P amp Weiser T 1993 The Early Holocene Saksunarvatntephra found in lake sediments in NW Germany Boreas 22 93100
Narcisi B 1993 Segnalazione di un livello piroclastico di provenienza etnea nellrsquo area del Fucino(Italia Centrale) Quaternario 6 8792
Narcisi B 1996 Tephrochronology of a Late Quaternary lacustrine record from the Monticchiomaar (Vulture volcano southern Italy) Quat Sci Rev 15 155165
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800 S M Davies and others
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Oldmacreld F Appleby P G amp Thompson R 1980 Palaeoecological studies of lakes in theHighlands of Papua New Guinea J Ecol 68 457477
Orsi G Drsquo Antonio M de Vita S amp Gallo G 1992 The Neapolitan Yellow Tureg a large mag-nitude trachytic phreatoplinian eruption eruptive dynamics magma withdrawal and calderacollapse J Volcanol Geotherm Res 53 275287
Paterne M Guichard F Labeyrie J Gillot P Y amp Duplessy J C 1986 Tyrrhenian Seatephrochronology of the oxygen isotope record for the past 60 000 years Mar Geol 72259285
Paterne M Guichard F amp Labeyrie J 1988 Explosive activity of the south Italian volca-noes during the past 80 000 years as determined by marine tephrochronology J VolcanolGeotherm Res 34 153172
Paterne M Labeyrie J Guichard F Mazaud A amp Maitre F 1990 Fluctuations of the Cam-panian explosive volcanic activity (south Italy) during the past 190 000 years as determinedby marine tephrochronology Earth Planet Sci Lett 98 166174
Pawse A Beske-Diehl S amp Marshall S A 1998 Use of magnetic hysteresis properties andelectron spin resonance spectroscopy for the identimacrcation of volcanic ash a preliminary studyGeophys J Int 132 712720
Pearce N J G Westgate J A amp Perkins W T 1996 Developments in the analysis of singleglass shards in volcanic deposits by laser ablation ICP-MS quantitative and single internalstandard multi-element methods Quat Int 3436 213227
Pearce N J G Westgate J A Perkins W T Eastwood W J amp Shane P 1999 Theapplication of laser ablation ICP-MS to the analysis of volcanic glass shards from tephradeposits bulk glass and single shard analysis Global Planet Change 21 151171
Pilcher J R amp Hall V A 1992 Towards a tephrochronology for the Holocene of the north ofIreland Holocene 2 255259
Ponel P amp Lowe J J 1992 Coleopteran pollen and radiocarbon evidence from the Prato Spillarsquo Drsquo succession N Italy C R Acad Sci Paris Sparaer II 315 14251431
Rose N L Golding P N E amp Battarbee R W 1996 Selective concentration and enumerationof tephra shards from lake sediment cores Holocene 6 243246
Ruddiman W F amp Glover L K 1972 Vertical mixing of ice rafted volcanic ash in NorthAtlantic sediments Geol Soc Am Bull 83 28172836
Ruddiman W amp McIntyre A 1981 The North Atlantic Ocean during the last deglaciationPalaeogeogr Palaeoclimatol Palaeoecol 35 145214
Santacroce R 1987 Somma Vesuvius Quad Ric Sci 114 252
Sarna-Wojcicki A 2000 Tephrochronology In Quaternary geochronology methods and applica-tions (ed J S Noller J M Sowers amp W R Lettis) AGU Reference shelf vol 4 pp 357377Washington DC American Geophysical Union
Sejrup H P Sjiquest holm J Furnes H Beyer I Eide L Jansen E amp Mangerud J 1989Quaternary tephrochronology on the Iceland Plateau north of Iceland J Quat Sci 4 109114
Sikes E L Samson C R Guilderson T P amp Howard W R 2000 Old radiocarbon agesin the southwest Pacimacrc Ocean during the last glacial period and deglaciation Nature 405555558
Stein R Nam S-I Grobe H amp Hubbersten H 1996 Late Quaternary glacial history andshort term ice rafted debris deg uctuations along the East Greenland continental marine In LateQuaternary palaeoceanography of the North Atlantic margins (ed J T Andrews W E NAustin H Bergsten amp A E Jennings) pp 135151 Geological Society London SpecialPublication
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 801
Stuiver M amp Grootes P M 2000 GISP2 oxygen isotope ratios Quat Res 53 277284
Stuiver M Reimer P J Bard E Beck J W Burr G S Hughen K A Kromer BMcCormac G Van der Plicht J amp Spurk M 1998 INTCAL 98 radiocarbon age calibration24 0000 cal BP Radiocarbon 40 10411083
Sweatman T R amp Long J V P 1969 Quantitative electron microprobe analysis of rock formingminerals J Petrol 7 332379
Turney C S M 1998 Extraction of rhyolitic ash from minerogenic lake sediments J Paleolim-nol 19 199206
Turney C S M amp Lowe J J 2001 Tephrochronology In Tracking environmental changes inlake sediments physical and chemical techniques (ed W M Last amp J P Smol) DordrechtKluwer Academic
Turney C S M Harkness D D amp Lowe J J 1997 The use of microtephra horizons tocorrelate Lateglacial lake sediments successions in Scotland J Quat Sci 12 525531
Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
van den Bogaard P amp Schmincke H 1985 A widespread isochronous Late Quaternary tephralayer in central and northern Europe Geol Soc Am Bull 96 15541571
van den Bogaard B Dordeg er W Sandgren P amp Schmincke H-U 1994 Correlating theHolocene records Icelandic tephra found in Schleswig-Holstein (northern Germany) Natur-wissenschaften 81 554556
Vernet G amp Raynal J-P 2001 Tephrostratigraphy of the Limagne revisited Implications forLateglacial and Holocene Prehistory In Tephras chronology archaeology (ed E Juvignparae ampJ-P Raynal) pp 111116 Dossiers de lrsquo ArchparaeoLogis no 1 France
Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
Vezzoli L 1991 Tephra layers in Bannock Basin (eastern Mediterranean) Mar Geol 1002134
von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
Walker M J C Bjorck S Lowe J J Cwynar L C Johnsen S Knudsen K-L WohlfarthB amp INTIMATE Group 1999 Isotopic events in the GRIP ice core a stratotype for the LatePleistocene Quat Sci Rev 18 11431150
Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
802 S M Davies and others
Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 769
sequences (Lotter et al 1992 von Grafenstein et al 1999 Hoek amp Bohncke 2001)A question that is pivotal to understanding the climate-driving mechanisms in theNorth Atlantic region is whether the abrupt events as well as the environmentalresponses to them were synchronous within the continental marine and polar icerealms or whether there were signishy cant `leadsrsquo and `lagsrsquo between them
The Greenland ice-core records suggest that some of the climatic transitions duringthe Last Termination took place within only a few decades (Mayewski et al 1997)while the short-lived cooling events within GI-1 lasted some 100300 ice-core yr atmost Determining the precise timing and duration of equivalent events representedin the ocean and continental records is extremely dimacr cult at present because of theuncertainties associated with the dating methods employed Age estimates obtainedusing the most widely adopted method radiocarbon dating have error ranges at 1frac14that are rarely better than sect50 14C yr and which frequently exceed sect100 14C yror more Interpretations of radiocarbon ages are complicated still further by uncer-tain calibration procedures and the distorting inreguences of radiocarbon `plateauxrsquo|episodes of near-constant radiocarbon age (see Lowe amp Walker 2000) Radiocarbondates obtained from marine sequences of Last Termination age are particularly sus-pect due to the inreguences of marine reservoir errors (Sikes et al 2000 Waelbroecket al 2001) There are equally wide uncertainties associated with other methodssuch as varve counting while the ice-core records themselves in the segment ofthe records that span the Last Termination may have systematic errors exceeding200 years (Stuiver amp Grootes 2000) A further problem is that some of the climatechanges at this time may have been time-transgressive (Coope et al 1998 Witteet al 1998) signishy cantly undermining the use of conventional approaches such asclimatostratigraphy and biostratigraphy for correlating the records It is evidentthen that conventional approaches to the dating and correlation of events duringthe Last Termination are inadequate for testing the hypothesis that abrupt climaticchanges during this period were truly synchronous at the continental or global scale
The problems of dating and correlating sequences that span the Last Terminationhave been reviewed through a series of workshops organized by the INTIMATE group(INTegration of Ice core MArine and TErrestrial records of the Last Termination|a core programme of the International Quaternary Union (INQUA) Palaeocli-mate Commission (httpwwwgeoguunlfgpalaeoclimateintimate)) (Bjorck etal 2001) which has recommended a set of proposals for improved precision in thefuture (Lowe et al 2001) Central to these proposals is the application of correlationtools that can provide independent tests of the age estimates and correlations basedon radiocarbon dating varve chronology and ice-layer counting
One of the approaches recommended by the INTIMATE and COTAV (INQUACommission on Tephrochronology and Volcanism) groups is tephrochronology forthere is growing evidence to suggest that this technique has the potential to resolvesome of the pressing geochronological issues while some tephras may be detectableover much wider geographical areas than appreciated hitherto Here we examine thepotential for developing a tephrostratigraphical and tephrochronological frameworkfor Europe for the period 18580 14C ka BP (encompassing the Last Terminationand the Early Holocene) It is argued that such a scheme will provide a rigorousunderpinning structure for geochronological models for this period and hence leadto improved understanding of the mechanisms timing and environmental enotects ofabrupt climatic changes during the Last Termination
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
770 S M Davies and others
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Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 771
Tab
le1
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Ref
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4
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9
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rck
et
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11
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13
Ju
vig
nparae
ampG
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t(1
987)
14
Di
Vit
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(1999)
15
Del
ibri
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(1979)
16
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vig
nparae
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Bra
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21
Etl
ich
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ler
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parasup3kss
on
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(2000)
26
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idaso
net
al
(2000)
27
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ssio
etal
(1976)
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Vez
zoli
(1991)
29
San
tacr
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(1987)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
772 S M Davies and others
Tab
le1
(Con
t)
(Th
eva
rve
age
for
the
Laach
erS
ee(E
)rsquoro
wis
12
880
yea
rs)
GR
IPage
tep
hra
age
(ss0
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volc
an
ich
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zon
(14C
yrs
)ti
me-
scale
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SiO
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O3
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Mn
OM
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5to
tal
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sou
rce
ref
IT
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7152
9132
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364
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104
6
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6)
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6)
un
kn
own
12
385
sect6
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(Ca
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SL
aach
erS
ee1820
See
(E)
11
063
sect12
(06
9)
(0
26
)(0
07)
(00
5)
(0
03
)(0
75
)(0
33)
29
595
501
0214
818
200
700
210
485
969
9
100
ED
S(0
70)
(00
7)
(02
8)
(01
4)
(00
8)
(00
5)
(01
3)
(09
7)
(04
2)
27
604
801
8210
019
200
200
614
174
272
1
100
ED
S(0
55)
(00
7)
(01
7)
(02
3)
(00
5)
(00
9)
(02
7)
(06
4)
(04
7)
30
598
604
3201
823
300
102
018
071
578
0
100
ED
S
(07
7)
(02
3)
(04
6)
(03
3)
(00
4)
(02
5)
(06
1)
(08
)(0
46)
un
kn
own
12
820
sect60
(C
ap
eak)
(16684
m)
Ref
eren
ces
1
this
stu
dy
2
Pate
rne
etal
(1988)
3
Narc
isi
(1996)
4
All
enet
al
(1999)
5
An
dro
nic
oet
al
(1995)
6
Ju
vig
nparae
et
al
(1996)
7
Bir
ks
et
al
(1996)
8
Bjo
rck
ampW
ast
egordma
rd(1
999)
9
Du
gm
ore
ampN
ewto
n(1
998)
10
Bjo
rck
et
al
(1992)
11
Kva
mm
eet
al
(1989)
12
Zoli
tsch
ka
etal
(1995)
13
Ju
vig
nparae
ampG
ewel
t(1
987)
14
Di
Vit
oet
al
(1999)
15
Del
ibri
as
etal
(1979)
16
Ju
vig
nparae
etal
(1987)
17
Dav
ies
et
al
(2001)
18
van
den
Bogaard
ampS
chm
inck
e(1
985)
19
Fri
edri
chet
al
(1999)
20
Bra
uer
eta
l(1
999)
21
Etl
ich
eret
al
(1987)
22
Tu
rney
etal
(1997)
23
Pate
rne
et
al
(1986)
24
Kel
ler
(1980)
25
Eir
parasup3kss
on
etal
(2000)
26
Hadeg
idaso
net
al
(2000)
27
Ale
ssio
etal
(1976)
28
Vez
zoli
(1991)
29
San
tacr
oce
(1987)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 773
Tab
le1
(Con
t)
GR
IPage
tep
hra
age
(ss0
8c
volc
an
ich
ori
zon
(14C
yrs
)ti
me-
scale
)n
SiO
2T
iO2
Al 2
O3
FeO
Mn
OM
gO
CaO
Na
2O
K2O
P2O
5to
tal
EP
MA
sou
rce
ref
La
Nu
gmicroere
ca11
400
12
549
922
9160
470
002
324
454
744
538
972
4W
DS
La
Nu
gmicroere
6
21
(MC
)
Nea
poli
tan
ca12
000
17
588
104
2177
631
901
006
525
940
686
9
962
8W
DS
Cam
pi
1Y
ello
w(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(0
78)
Fle
gre
i
Tu
reg(I
T)
568
106
0194
448
7
17
451
938
75
5
100
ED
S
596
804
9192
940
3
06
435
034
588
9
100
ED
S2
14
619
403
1196
329
9
02
019
943
485
7
100
ED
S
Borr
ob
ol
ca12
300
18
733
601
1122
914
700
601
207
635
837
6
955
1W
DS
Hek
la22
(IC
)(0
35)
(00
2)
(01
8)
(00
9)
(00
2)
(00
2)
(00
3)
(01
4)
(00
9)
(0
47)
un
kn
ow
n14
650
sect200
(Ca
pea
k)
(17458
m)
un
kn
ow
n14
650
sect200
(C
ap
eak)
(17506
m)
E-2
P
oll
ara
ca13
000
766
302
7138
810
8
01
015
025
239
7
100
ED
SA
eoli
an
2
23
24
pu
mic
e(I
T)
Isla
nd
s
KO
L-G
S-2
13
400
18
490
910
6148
8100
702
184
9126
521
400
902
8989
6W
DS
25
(IC
)
GS
-2B
AS
-113
400
3497
417
0132
7124
402
266
6118
124
802
103
4988
7W
DS
26
(IC
)
Ref
eren
ces
1
this
stu
dy
2
Pate
rne
etal
(1988)
3
Narc
isi
(1996)
4
All
enet
al
(1999)
5
An
dro
nic
oet
al
(1995)
6
Ju
vig
nparae
et
al
(1996)
7
Bir
ks
et
al
(1996)
8
Bjo
rck
ampW
ast
egordma
rd(1
999)
9
Du
gm
ore
ampN
ewto
n(1
998)
10
Bjo
rck
et
al
(1992)
11
Kva
mm
eet
al
(1989)
12
Zoli
tsch
ka
etal
(1995)
13
Ju
vig
nparae
ampG
ewel
t(1
987)
14
Di
Vit
oet
al
(1999)
15
Del
ibri
as
etal
(1979)
16
Ju
vig
nparae
etal
(1987)
17
Dav
ies
et
al
(2001)
18
van
den
Bogaard
ampS
chm
inck
e(1
985)
19
Fri
edri
chet
al
(1999)
20
Bra
uer
eta
l(1
999)
21
Etl
ich
eret
al
(1987)
22
Tu
rney
etal
(1997)
23
Pate
rne
et
al
(1986)
24
Kel
ler
(1980)
25
Eir
parasup3kss
on
etal
(2000)
26
Hadeg
idaso
net
al
(2000)
27
Ale
ssio
etal
(1976)
28
Vez
zoli
(1991)
29
San
tacr
oce
(1987)
Phil Trans R Soc Lond A (2002)
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774 S M Davies and others
Tab
le1
(Con
t)
(Th
evarv
eage
for
the
Gre
enis
h(I
T)rsquo
row
is17
560
yea
rs)
GR
IPage
tep
hra
age
(ss0
8c
volc
an
ich
ori
zon
(14C
yrs
)ti
me-
scale
)n
SiO
2T
iO2
Al 2
O3
FeO
Mn
OM
gO
CaO
Na
2O
K2O
P2O
5to
tal
EP
MA
sou
rce
ref
GS
-2B
AS
-213
400
6497
933
2122
4147
902
445
389
829
905
205
4979
4W
DS
26
(IC
)
GS
-2B
AS
-313
400
2538
529
9125
7131
203
132
174
729
507
707
7980
1W
DS
26
(IC
)
GS
-2B
AS
-414
000
7503
617
4145
1113
202
155
3100
528
010
5
975
7W
DS
26
(IC
)
Un
ita
dei
ca14
000
5648
804
7184
625
901
602
217
432
679
302
8100
ED
SP
hle
gre
an
3
27
Tef
ra(0
53
)(0
13
)(0
25)
(07
4)
(01
4)
(01
6)
(01
6)
(03
4)
(06
6)
(01
6)
Fie
lds
Su
per
iori
(IT
)
Y-1
(IT
)ca
14
000
16
600
413
7169
555
502
218
242
262
229
306
8100
ED
SE
tna
28
Bla
ck17
000
sect300
Fea
ther
(17890
m)
Gre
enis
hca
15
000
9618
704
190
731
601
804
328
531
586
202
6100
ED
SV
esu
viu
s3
4
(IT
)(0
70
)(0
08
)(0
45)
(06
8)
(01
0)
(01
0)
(05
9)
(05
3)
(05
8)
(01
6)
29
L9
(IT
)ca
16
000
15
626
704
4188
630
401
103
329
429
683
402
7100
ED
SV
esu
viu
s3
15
17
000
(14
2)
(01
4)
(07
2)
(11
1)
(00
9)
(02
4)
(06
6)
(04
8)
(06
5)
(01
8)
St
2-1
85
18
500
7504
015
1145
5112
002
466
9114
525
206
6
992
2W
DS
26
(IC
)
Ref
eren
ces
1
this
stu
dy
2
Pate
rne
etal
(1988)
3
Narc
isi
(1996)
4
All
enet
al
(1999)
5
An
dro
nic
oet
al
(1995)
6
Ju
vig
nparae
et
al
(1996)
7
Bir
ks
et
al
(1996)
8
Bjo
rck
ampW
ast
egordma
rd(1
999)
9
Du
gm
ore
ampN
ewto
n(1
998)
10
Bjo
rck
et
al
(1992)
11
Kva
mm
eet
al
(1989)
12
Zoli
tsch
ka
etal
(1995)
13
Ju
vig
nparae
ampG
ewel
t(1
987)
14
Di
Vit
oet
al
(1999)
15
Del
ibri
as
etal
(1979)
16
Ju
vig
nparae
etal
(1987)
17
Dav
ies
et
al
(2001)
18
van
den
Bogaard
ampS
chm
inck
e(1
985)
19
Fri
edri
chet
al
(1999)
20
Bra
uer
eta
l(1
999)
21
Etl
ich
eret
al
(1987)
22
Tu
rney
etal
(1997)
23
Pate
rne
et
al
(1986)
24
Kel
ler
(1980)
25
Eir
parasup3kss
on
etal
(2000)
26
Hadeg
idaso
net
al
(2000)
27
Ale
ssio
etal
(1976)
28
Vez
zoli
(1991)
29
San
tacr
oce
(1987)
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 775
Altogether 34 tephra layers have been reported from sediment sequences in Europeand the NE Atlantic region which date to the period between 185 and 80 14C ka BP(table 1) Because tephra layers are deposited virtually instantaneously (in geologicalterms) they enotectively represent time-parallel marker horizons within stratigraphicalsequences (Westgate amp Gorton 1981 Sarna-Wojcicki 2000 Turney amp Lowe 2001) Intheory therefore all 34 tephras could prove valuable for correlation purposes eitherin a local context or in those cases where the ash deposits have been widely dispersedbetween regional sequences In practice however very little is known about the fullgeographical dispersal of the majority of the ash layers listed in table 1 Furthermorecorrelation by tephrostratigraphy will only work if the various ash layers have wellcharacterized geochemical signatures While some geochemical data are available forthe majority of the tephras listed in table 1 the collective data are far from robustand no geochemical data have yet been published for some
Nonetheless there is mounting evidence to show that some of the tephra depositslisted in table 1 are not only geochemically distinct but are also much more widelydispersed across Europe than was initially realized Stratigraphic records of thebetter-known tephras were initially limited to observations of visible tephra layersThe development of a technique that enables detection of tephra layers that are invis-ible to the naked eye (micro-tephra) in Late Glacial sequences has greatly extendedthe area over which some of the ashes can be traced (Lowe amp Turney 1997 Turneyet al 1997 Turney 1998 Wastegard et al 1998 2000a b) Most of this research sofar has focused on micro-tephra layers originating from Icelandic centres distributedthroughout northern Europe Here we report on further development of this line ofresearch with new evidence for the occurrence of micro-tephra layers in a site insouthern Europe The results suggest that there is great potential for tracing someash layers that originated from Italian volcanic complexes over much larger tracts ofsouthern and central Europe than records of visible tephra deposits allow This inturn greatly enhances the scope for making precise correlations not only betweenparts of southern Europe but also between continental and marine (MediterraneanSea) sequences
2 Micro-tephra extraction techniques
Micro-tephra horizons are composed of glass shards that are generally between 80and 24 m m (long axis) in size and that are present in such low concentration insedimentary sequences that they can only be detected by the use of a particle sep-aration technique Several factors inreguence the concentration of shards such as dis-tance from the volcanic source precipitation patterns during the eruption and sub-sequent tephra dispersal and sedimentary processes within the catchment In someterrestrial sequences micro-tephra horizons with a peak concentration (peak con-centration tends to coincide with the shy rst occurrence of glass shards in a sedimentsequence which is then taken to mark the time of maximum ash deposition) as lowas 10 shards cmiexcl3 has been conshy rmed whereas other sites have recorded as muchas 8000 shards cmiexcl3 (Turney et al 1997) In complete contrast tephra horizons inthe GRIP ice core have been identishy ed based on a single glass shard only (Gronvoldet al 1995)
Enotective separation techniques for the detection and isolation of tephra particlesfrom sedimentary sequences have been developed These include ashing of organic
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776 S M Davies and others
matter (Pilcher amp Hall 1992) digestion of biogenic and opaline silica (Rose et al 1996) the use of magnetic properties of ash layers (see for example Oldshy eld et al 1980 van den Bogaard et al 1994 Pawse et al 1998) X-ray analysis (Dugmore ampNewton 1992) and a density separation (regotation) technique (Turney 1998) Den-sity separation has proved exceedingly useful for the detection of small glass shardspresent in low concentrations in mineral-rich Late Glacial sediments This involvesthe separation and concentration of particles of predetermined specishy c gravity withthe use of a heavy liquid and subsequent identishy cation of glass shards with the useof a polarizing light microscope (for further details see Turney (1998)) This methodhas been particularly successful in the detection of tephras of rhyolitic compositionthat have a specishy c density of 2325 g cmiexcl3 (Lowe amp Turney 1997 Turney et al 1997 2001 Turney 1998 Wastegard et al 1998 2000a b) It is this technique thathas resulted in the wider recognition of micro-tephras in Europe as discussed below
3 Geochemical ` ngerprintingrsquo of tephra layers
The 34 tephras listed in table 1 have originated from four major volcanic complexesIceland the Massif Central in central France the Eifel district near Bonn and threevolcanic centres in Italy (the Campanian group Etna and the Aeolian Islands (seeshy gure 2)) An important matter to resolve is the extent to which the various magmasand ashes generated by these volcanic complexes can be geochemically shy ngerprintedThis is especially important in the case of tephras which have originated from thesame volcanic centre in which there may have been limited geochemical evolution ofmagmas over time In this section we summarize the approach generally adopted todetermine the geochemical character of visible and micro-tephras as background tothe geochemical data summarized in table 1 In the subsequent section of the paperwe review the present state of knowledge concerning all 34 tephras listed in table 1
Glass shards formed during the rapid cooling of magma are thought to have acomposition that is representative of the bulk geochemistry of the magma (Barker1983) hence widely dispersed glass particles are regarded as the most appropriateconstituents of pyroclastic material for geochemical analysis If a tephra deposit canbe shown to have a distinct geochemical signature then it can be used to correlatethe stratigraphic units in which it occurs (tephrostratigraphy) as well as to datethese units (tephrochronology) if the ages of the tephras are known (Westgate ampGorton 1981) A key element of building a tephrostratigraphical framework there-fore is to establish as rigorously as possible the geochemical composition of theindividual tephras used in its construction Robust and directly comparable geo-chemical datasets are dimacr cult to assemble for glass however because it is highlyunstable material particularly prone to sodium mobilization
The technique most widely employed to establish the geochemical signature of atephra is electron probe micro-analysis (EPMA) This enables grain-discrete determi-nations of the major elements within an individual glass shard which is of particularbeneshy t in the analysis of micro-tephra layers which generally contain glass particlesin low concentration The glass surface is bombarded with an electron beam and theX-ray energy produced is unique to each element while the intensity of the signalemitted is proportional to the amount of that element in the glass shard (Hunt amp Hill1993) Measurement can be by either energy dispersive spectrometry (EDS) or wave-length dispersive spectrometry (WDS) EDS has a lower precision mainly because
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European tephrochronological framework for Termination 1 777
N
0 500 km
Confirmed records of Vedde Ash (visible occurrences)
New records of Vedde Ash from flotation method
Extended area of Vedde Ash detection (micro-tephra)
Known area of Laacher See Tephra (visible occurrences)
Confirmed records of Neapolitan Yellow Tuff (visible occurrences)
New record of Neapolitan Yellow Tuff from flotation method
Known area of Neapolitan Yellow Tuff
Volcanic centres of particular relevance to this study
Other major volcanic centres in Europe
Figure 2 Location of the principal volcanic centres that were active during Termination 1 andthe Early Holocene The known distribution of the Vedde Ash (VA) Laacher See (LST) andNeapolitan Yellow Tureg (NYT) are shown
the behaviour of each element cannot be monitored independently during measure-ment and so this approach fails to detect for example any signishy cant mobilizationof sodium during the bombardment process (Hunt amp Hill 1993) Although WDSrequires a higher beam current and a longer counting time than EDS the formeronoters the distinct advantage of sequential acquisition of elemental data so that thedegree of sodium loss can be tracked The morphology of individual glass shards canalso distort EDS data a problem that is reduced when using WDS because for thisprocedure glass shards are mounted in an epoxy resin and polished to provide aregat surface for analysis Hence data should always be obtained using WDS whereverpossible
Even when WDS is used as a common tool for determining the geochemical spectraof samples aberrant results can arise that inreguence data comparisons For examplesome glass shards may contain tiny crystalline inclusions of feldspar and these shouldbe avoided when selecting surface points for analysis (Hunt amp Hill 2001) Hunt amp Hill
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778 S M Davies and others
6
4
2
40 50 60 70 80
K2O
(
)
SiO2 ()
Laacher See
Iceland
Veidivoumltn-Dyngjufjoumlll
Katla (basalt)
Grimsvoumltn-Kverkfjoumlll
Hekla
Katla (rhyolitic)
0
Icelandic volcanic centres8
10
Massif Central
Etna
Campanian
Figure 3 Bi-plot of SiO2 and K2 O concentrations in tephras derived from the main Europeanash provinces (modimacred after Mangerud et al 1984) The Campanian Massif Central and Etnaconcentrations are based on the data presented in table 1
(2001) have concluded that small variations in the laboratory procedures employedto determine glass chemistry can lead to misidentishy cation of sources for glass shardsand give an example of shards with a Jan Mayen provenance wrongly attributedto an Icelandic source Clearly there is a need for standardization of laboratoryprocedures and while a number of recommendations have recently been advocated(Froggatt 1992 Hunt amp Hill 1993 Hunt et al 1998) there is still some variation inlaboratory and operator practice (Hunt amp Hill 1996) Standardization is also requiredin the form in which results are presented to ensure comparability Normalizationof the data to 100 a practice employed by some researchers can obscure poorresults and hence lead to incorrect comparisons (Hunt amp Hill 1993) However othersargue that it may actually facilitate comparisons between samples by removing thedistorting enotects of the water component contained in glass shards (see for exampleFroggatt 1992) The majority of the published Italian and some of the Eifel datahave been normalized while those from other parts of Europe have not and hencedata comparisons are not always straightforward
Table 1 provides mean values and standard deviations for major oxide concentra-tions obtained from those tephras for which data are presently available The tableincludes previously unpublished WDS results for the Neapolitan Yellow Tunot (NYTdiscussed in x 4 below) and for the Mercato Tephra While individual tephra layersmay be geochemically distinct the geochemical envelopes representing the collectivedata obtained from all of the tephras assigned to each major volcanic province showsignishy cant overlaps as is illustrated in the bi-plots and ternary plots (shy gures 3 and 4)of selected oxide concentration data It is clear therefore that measurement of majoroxide concentrations does not satisfactorily discriminate between some tephras orig-inating from dinoterent volcanic centres (as noted by van den Bogaard amp Schmincke(1985) and Frezzotti amp Narcisi (1996) with respect to Eifel and Italian tephras)nor of tephras of dinoterent age originating from the same volcanic centre (Bond et
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European tephrochronological framework for Termination 1 779
40 50 60 70 80
K2O
(
)
SiO2 ()
shyshyshyshy
shy
shyshy
shyshyshy
shy
shy
shy
shy
reg
reg regreg
regregregregreg regregregregreg
FF
F
ll
l
l
4 8 12 16
reg
regreg
regreg
regregreg
regreg
regregreg
shy
F
l shyshyshyshyshy shyshyshyshyshyshy
F
F
l
ll
FeO ()
TiO
2 (
)
reg
l
Iceland
Eifel
F
shy ItalyMassif Central
100
80
60
40
20
100
80
60
40
20
100 80 60 40 20
CaO
FeO
K2O
regregreg
reg
reg
reg
reg
reg
reg
regregreg
shyF
F
F
regreg
l
lllshy
shyshyshy
shyshyshy
l
0
2
4
6
8
10
0
1
2
3
4
5
regreg
regreg
regreg
regreg
regreg
reg
reg
regreg
l
l
ll
shy
shyshy
shyshy
shy
shyshy
FF
F
100
80
60
40
20
100
80
60
40
20
100 80 60 40 20
K2ONa2O
CaO
(c) (d)
(a)
(b)
Figure 4 Plots of selected geochemical data obtained from tephras of Termination 1 age (seetable 1) (a) Bi-plot of mean SiO2 and K2 O values (b) Bi-plot of mean FeO and TiO2 values(c) Ternary plot indicating variations in the proportions of FeO CaO and K2 O (d) Ternaryplot indicating variations in the proportion of CaO Na2 O and K2 O
al 2001) Individual tephra layers are presently assigned to a particular volcanicevent on the basis of a combination of criteria usually including examination of thephysical properties (eg refractive index and surface detail of the glass shards) thestratigraphic position of the layer and independent assessment of the age of the layeras well as any geochemical data that may be available The construction of a tephro-stratigraphical scheme would clearly beneshy t from the application of a more diagnostic
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780 S M Davies and others
geochemical tool One approach that has promise is the analysis of trace and rareearth elements using an ultraviolet laser ablation inductively coupled plasma massspectrometer (UV-LA-ICP-MS) (Pearce et al 1996 1999 Eastwood et al 1999)This approach has been applied successfully to analysis of tephras of Mid-Holoceneage but not yet to tephras that fall within the period of interest here
4 Tephra layers in Europe and the North Atlantic regiondated to between 185 and 80 14C ka
(a) Icelandic province
The Icelandic volcanic systems are divided into three main groups based on theirgeochemical characteristics tholeiitic basalts transitional alkali basalts and alkaliolivine basalts (Jakobsson 1979) Collectively magmas from the Icelandic provincespan a wide geochemical spectrum although individual volcanic centres have tightgeochemical distributions (shy gure 3) for four of the main centres Grimsvotn-Kverfjolland Veidvotn-Dyngjufoll which form part of the northern (tholeiitic) volcanic zoneand Hekla and Katla which fall within the eastern (alkali olivine basalt and transi-tional alkali basalt) volcanic zone (Haregidason et al 2000) These appear to be thekey centres for the tephras listed in table 1 that have been assigned an Icelandicorigin
One of the best-known and most widely dispersed tephra horizons in northernEurope that has an Icelandic origin is the Vedde Ash (VA) which was depositedca 103 14C ka BP (Birks et al 1996 Wastegard et al 1998) within the GS-1Younger Dryas chronozone This ash is believed to originate from the Katla complexwithin the transitional alkali basalt province (Mangerud et al 1984 Lacasse et al 1995) in the south of the island The ash has a bimodal geochemical composition (rhy-olitic and basaltic) which is thought to reregect derivation from two separate magmachambers Studies of recent volcanic events in Iceland have shown that the mostexplosive eruptions generating the largest amounts of tephra occur in this tran-sitional alkali basalt province (Haregidason et al 2000) It is also believed that thewidespread distribution of this ash was caused by the development of co-ignimbriteash plumes during an ignimbrite-forming eruption (Lacasse et al 1995)
Layers of VA that are visible to the naked eye have been found in lake sediments inwestern Norway (Mangerud et al 1984) and the Inner Hebrides Scotland (Davies etal 2001) and in marine cores throughout the NE Atlantic (see for example Kvammeet al 1989 Lacasse et al 1995) in the northern North Sea (Long amp Morton 1987)on the Iceland plateau (Ruddiman amp McIntyre 1981 Sejrup et al 1989) and on theeast Greenland continental margin (Stein et al 1996) The distribution of the VAin North Atlantic marine sequences is characterized by an arcuate lobe extendingsouthwest from the Denmark Strait and curving eastwards to mid-latitudes in theNorth Atlantic (Lacasse et al 1995) This strongly suggests deposition from raftedice which was displaced to the southwest and south in a circulating counterclockwisegyre (Ruddiman amp Glover 1972) This may well reregect Katlarsquos close proximity tothe southern coast of Iceland with the Vedde tephra being deposited on ice thatcalved directly into the North Atlantic (Haregidason et al 2000) However depositionvia the atmosphere almost certainly took place as well as is indicated by the recentdiscoveries of rhyolitic VA in micro-tephra form in several sites in Scotland (Turneyet al 1997) southern Sweden (Wastegard et al 1998 2000a) and western Russia
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(Wastegard et al 2000b) A more recent discovery of a relatively high concentrationof rhyolitic VA glass shards in the northern Netherlands indicates that the ash maywell have been dispersed much further south than previously thought (S M Davies2002 unpublished work) Finally glass shards assigned to the VA have also beendiscovered in the GRIP ice core and dated to 11 980 sect 80 GRIP yr BP (Gronvold etal 1995) This discovery is extremely important for it indicates that the VA maywell provide a reliable time-parallel marker horizon between ice-core marine andterrestrial records
Two other important Icelandic ash layers the Borrobol and Saksunarvatn Tephraswere deposited near the beginning and end of the Last TerminationEarly Holoceneinterval respectively The Borrobol Tephra was discovered for the shy rst time in lakesediments in several sites in Scotland and as yet is known only in micro-tephra formIt has been dated in Scottish sites to ca 123 14C ka BP (Turney et al 1997) Whatis thought to be a contemporaneous tephra has been detected in marine sedimentson the North Icelandic shelf (Eirplusmn ksson et al 2000) This certainly has a very similargeochemical composition to those reported from Scotland but the horizon in whichit was discovered on the North Iceland plateau has been dated to 134 14C ka Theage discrepancy between the Scottish and Icelandic Borrobol Tephra layers may wellreregect the inreguence of a marine reservoir error although the possibility that severaltephras with similar geochemical composition were erupted over a period exceeding1000 yr cannot be ruled out (Larsen 2000)
The Saksunarvatn Ash appears to have been one of the largest Holocene eruptionsin Iceland It has a tholeiitic basaltic composition which is considered to indicate anorigin in the Grimsvotn or Kverfjoll complex (shy gure 3) (Mangerud et al 1986) Layersof this ash have been identishy ed in sites on the Faroe Islands (Mangerud et al 1986Dugmore amp Newton 1998 Wastegard et al 2001) the Shetland Isles (Bennet et al 1992) northern Germany (Merkt et al 1993) western Norway (micro-tephra) (Birkset al 1996) and in the GRIP (Gronvold et al 1995) and NordGRIP ice cores (S MDavies 2002 unpublished work) It has been dated to between 9060 and 8930 14C kaBP (Birks et al 1996) in Norway and to ca 10 240 sect 30 GRIP yr BP in the GRIPice core (Gronvold et al 1995) The Saksunarvatn Ash may thus provide a secondimportant widespread time-parallel marker between ice-core marine and terrestrialrecords
Other Icelandic tephras of rhyolitic amacr nity are less well known in terms of theirdistribution and geochemical variation The Hogstorpsmossen Tephra reported fromSweden (Bjorck amp Wastegard 1999) and the L3754 tephra discovered in the FaroeIslands (Dugmore amp Newton 1998) are known from single sites only and so theirpotential for tephrostratigraphy is uncertain at present Furthermore the geochem-ical spectrum of the Hogstorpsmossen Tephra is based on a small dataset with lowanalytical totals
A number of tephras of basaltic composition have originated from Iceland buttheir distributions are largely conshy ned to Iceland or to marine cores collected fromclose to the Iceland coast or in the North Atlantic These include the tephras listedas 1-THOL-1 1-THOL-2 KOL-GS-2 GS-2BAS-1 GS-2BAS-2 GS-2BAS-3 andGS-2BAS-4 in table 1 (Kvamme et al 1989 Bjorck et al 1992 Eirplusmn ksson et al 2000 Haregidason et al 2000) The shy rst two in this list are tholeiitic basaltic tephrasassociated with the VA in a complex series of tephras collectively termed NorthAtlantic Ash Zone 1 (NAAZ1) which has been detected in numerous marine cores
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782 S M Davies and others
from the North Atlantic Initially thought to represent a single eruption analysisof high-resolution sediment sequences from Lake Torfadalsvatn in northern Iceland(Bjorck et al 1992) the Hebridean Shelf near NW Scotland (Austin amp Kroon 1996)the St Kilda Basin (Hunt et al 1995) and the open North Atlantic (Bond et al 2001)has demonstrated that NAAZ1 comprises a series of distinct ashes that probablyreregect separate eruption events 1-THOL-1 is thought to originate from Veidivotn(shy gure 3) while Grimsvotn may have been the source of 1-THOL-2 (Kvamme et al 1989)
KOL-GS-2 is also of tholeiitic basaltic composition but is thought to originatefrom the Kolbeinsey Ridge system (Eirplusmn ksson et al 2000) To date this tephra hasbeen detected in one marine core only within the same record on the North Ice-landic shelf as that from which the correlative of the Borrobol Tephra was alsoreported (Eirplusmn ksson et al 2000) GS-2BAS-1 to GS-2BAS-4 are of uncertain ori-gin but are thought to have been deposited at roughly the same time as KOL-GS-2(ca 134 14C ka BP (Haregidason et al 2000))
The limited distribution of these basaltic tephras a feature that is not unique toIcelandic basaltic material may reregect two factors the relative magnitude of the vol-canic eruptions from which they were derived and the limited aerial transportationof basaltic glass which is denser than rhyolitic material However a rather surpris-ing recent discovery is that of visible basaltic VA in a site on the Isle of Skye inthe Inner Hebrides Scotland (shy gure 5) (Davies et al 2001) All other occurrencesof VA in Scotland are exclusively of rhyolitic material and in micro-tephra formonly (Turney et al 1997 Turney 1998) Clearly basaltic tephra must have beentransported subaerially as far south as Skye and the reason why it has not beendetected at other sites in Scotland is puzzling We suspect that this partly reregectsthe laboratory methods employed to separate glass shards present in low concentra-tion within a micro-tephra layer from the host sediment The technique used is adensity-separation (regotation) procedure (Turney 1998) and as basaltic shards havea specishy c density similar to quartz one of the most abundant minerals in lake sedi-ments of Late Glacial age basaltic material is dimacr cult to detect using this methodThis hypothesis is currently under investigation and alternative detection methodsare being explored including magnetic separation (Mackie et al 2002)
Several other events listed in table 1 that are of probable Icelandic origin includetephras recorded in the GRIP ice core including visible (eg the `Black Featherrsquo)tephras as well as uncertain tephras inferred from distinct Ca peaks (S Johnsen2001 personal communication) No glass shards have yet been detected in the latterbut a volcanic origin is assumed because high Ca peaks are associated with knowntephras in other Greenland ice cores (S Johnsen 2001 personal communication)These are referred to as `unknownrsquo in table 1 No geochemical analyses are availablefrom these horizons so their origin must remain speculative but a possible source isIceland in view of its proximity to the Greenland ice sheet and assumed atmosphericcirculation patterns
(b) Eifel province
There are two prominent tephra events dated to the Termination 1Early Holocenetime-span that originated from the Eifel province the Laacher See Tephra (LST)and the Ulmener Maar Tephra (UMT) Visible occurrences of the LST indicate that
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European tephrochronological framework for Termination 1 783
Vedde Ash
615 625 635 645 655depth (cm)
organic lake mudsHolocene
silty clayGS-1Younger Dryas
organic lake mudsGI-1Alleroslashd
100 microm
(a)
(b)
Figure 5 (a) Photograph of the visible VA layer discovered at Loch Ashik Isle of Skye InnerHebrides Scotland (b) Light microscope photograph showing the rich content of basaltic shards(examples are indicated by the arrows) within this layer (8024 m m size fraction)
this ash was dispersed over much of central Europe (van den Bogaard amp Schmincke1985 Friedrich et al 1999 Litt amp Stebich 1999) The LST is dated by radiocarbonto ca 110 14C ka BP (van den Bogaard amp Schmincke 1985) and to 11 063sect12 14C BP(Friedrich et al 1999) by varve chronology to 1288 varve ka BP (Brauer et al 1999Litt et al 2001) and by ArAr dating to 129 ka cal BP (van den Bogaard 1995) Ithas a phonolitic composition and is thought to have originated from a plinian andphreatomagmatic eruption with the distal ash being carried in three distinct plumesone to the northeast towards Poland one to the west and the third to the southcovering the Jura Mountains and north Italy (van den Bogaard amp Schmincke 1985Juvigne et al 1995 Bossuet et al 1997) This pattern is thought to reregect altitu-dinal variations in the predominant wind direction Sedimentary sequences near thevolcanic source indicate that the LST consists of three main layers which represent
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784 S M Davies and others
dinoterent eruption phases These are grouped together as the Laacher See TephraFormation but the three individual units can be traced within and between a seriesof depositional fans The geochemical data obtained from these three LST layersshow signishy cant variations as reregected in the ternary plots (shy gure 4)
The Early Holocene Ulmener Maar Tephra (UMT) is of rhyolitic composition andappears to be restricted to sites in Germany though this conclusion is also based onrecords of visible tephras only It is dated to ca 956 14C ka BP and to 110 varve ka(Zolitschka et al 1995 Litt et al 2001)
(c) Massif Central province
The Massif Central tephras are mainly of basaltic trachyandesitic compositionwhich is distinct from the other ash provinces (shy gures 3 and 4) and their known dis-tributions are mostly conshy ned to the Massif Central region The ages of the MassifCentral tephras are based on radiocarbon dates obtained from mire and lake sedi-ments which `bracketrsquo the tephras The La Nugsup3ere Tephra with an age of 114 14C kaBP is the oldest Massif Central tephra identishy ed so far within the time-span of inter-est (Etlicher et al 1987 Juvigne et al 1996) The two Godivelle Tephras (5 and 4)are close in age but extensive radiocarbon dating suggests distinct ages of 107and 103 14C ka BP respectively (Juvigne et al 1996) The age of the Puy de DomeTephra is less certain as the estimate is based on only one radiocarbon date froma site in the southern Chaplusmn ne des Puys (table 1) This tephra is thought to havea trachyte composition (Juvigne 1993) although no major element concentrationshave yet been published
The ChopineKilianVasset tephras are thought to be derived from three separateEarly Holocene eruptions although the stratigraphic succession is not known atpresent These trachytic tephras have been radiocarbon dated to ca 854sect150 14C kaBP but are thought to have erupted separately within ca 260 yr (Juvigne et al 1996) This series of tephras is considerably more widespread than the others fromthe region having been identishy ed as far east as the Jura Mountains (Martini amp Duret1965 Martini 1970) Some other ash falls that originated from the Chaplusmn ne des Puysappear to be of local importance only (Vernet et al 1998 Vernet amp Raynal 2001)Geochemical data are currently available for only three of the Massif Central tephrasand so far as is known no attempt has yet been made to identify these tephras inmicro-tephra form
(d ) Italian provinces
The Italian tephras from this period can be assigned to three main volcanic com-plexes the Campanian volcanic shy elds around Naples Etna on Sicily and the AeolianIslands The Campanian complex which includes the Phlegrean Fields Vesuviusand Ischia is mainly trachytic in composition with a geochemical spectrum that isquite distinct from those of the Etna complex and of the Aeolian Islands (shy gure 3)Tephras originating from one or more of these three complexes have been detectedin marine cores from the Tyrrhenian and Adriatic seas as well as other parts of theMediterranean Sea (Keller et al 1978 Paterne et al 1986 1988 1990 Langone etal 1996) and in lake sequences in southern Italy such as Lago Grande di Monticchio(Newton amp Dugmore 1993 Narcisi 1996 Allen et al 1999) and central Italy such asLago Albano near Rome (Calanchi et al 1996) Some work has also been conducted
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European tephrochronological framework for Termination 1 785
in or close to the volcanic source areas in an attempt to establish the full sequenceof volcanic eruptions during the Late Quaternary (see for example Di Vito et al 1999) There are nine Italian tephras reported from marine and lake sequences thatdate from the period between 185 and 80 14C ka BP In all instances the recordsare of visible layers of tephra The ages of some of these are poorly established atpresent with conregicting data obtained from dinoterent sites The ages suggested intable 1 are those favoured in the most recent publications but these may requirere-assessment in the light of future research
The two oldest known tephras in the time-period of interest are the L9 and Green-ish Tephras both recorded as separate features within the annually laminated Lagodi Monticchio maar sequence The lowest of the two L9 is considered to be the cor-relative of the `basalrsquo plinian eruption of Vesuvius (Narcisi 1996) Age estimates ofa palaeosol that underlies the Vesuvius tephra sequence are ca 1617 14C ka BP forthis event (Delibrias et al 1979) L9 has a trachytic composition very similar to theGreenish Tephra (table 1) However L9 which is also a product of Vesuvius is foundstratigraphically below the Greenish Tephra in the Lago di Monticchio core TheGreenish Tephra is dated in the Monticchio sequence to 17 560 varve yr BP (Allenet al 1999) and has a calibrated radiocarbon age estimate of 17 830 sect 300 cal BP(Andronico et al 1995) Both tephras have a dominantly eastwards dispersal basedon the occurrences of visible layers (Santacroce 1987 Narcisi 1996) Both tephrasalso have a trachytic composition and as can be seen from table 1 the reportedgeochemical spectra are very close indeed with the standard deviations overlappingfor almost every major element This could present problems for tephrostratigra-phy where only one of the tephras is evident in a sediment sequence in particularbecause they are so close in age This is a good example of where an analysis oftrace and rare earth elements might be required to make a clear distinction betweentephras with very similar major oxide concentrations
The Y-1 Tephra also termed the Biancavilla Montalto Ignimbrite (Vezzoli 1991)is a product of Etna and has been identishy ed as a visible benmoritic tephra horizonthroughout the central Mediterranean (Paterne et al 1988) including central Italyand the Adriatic Sea (Vezzoli 1991 Narcisi 1993 Calanchi et al 1996) It has anestimated age of ca 140 14C ka BP The Unita dei Tefra Superiori tephra which hasbeen detected as far east as Lago di Monticchio in south-central Italy (Narcisi 1996)is also dated to ca 140 14C ka BP (Alessio et al 1976) but it is thought that thesource of this tephra lies in the Phlegrean Fields No geochemical data are availablefrom the presumed source region|the data reported in table 1 were obtained fromthe Lago di Monticchio record (Narcisi 1996)
The NYT which is equivalent to the C-2 tephra reported from various marinesequences has also been traced throughout central Italy and the Adriatic Sea (Pat-erne et al 1988 Calanchi et al 1996 Di Vito et al 1999) (shy gure 2) In the centralApennines region it formed the parent material for a soil that started to developat the beginning of the Holocene period (Frezzotti amp Narcisi 1996) Also originatingfrom the Campi Flegrei caldera it is dated to ca 120 14C ka BP (Di Vito et al 1999) Published geochemical data based on EDS indicate three dinoterent geochemicalpopulations varying from latite to phonotrachyte in composition (Orsi et al 1992Paterne et al 1988) (table 1) We report in x 4 of this paper on new data obtainedfrom the NYT by WDS and it is the mean of these new data that is included intable 1 Comparisons with the previously published EDS data are provided (table 1)
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786 S M Davies and others
The new data indicate clearly that the NYT originated from the Campanian volcaniccentre
In the interval between the dispersal of the NYT (ca 120 14C ka BP) and 95 14Cka BP there appear to have been as many as 34 eruptions in the Campi Flegrei caldera(Di Vito et al 1999) Of these only one appears to have been detected widely in theregion the Pomici Principali (also termed the Agnano Formation or C-1 tephra inmarine records (Paterne et al 1988) This was the product of the highest magnitudeeruption from this epoch and is dated to between 976 sect 300 and 1032 sect 50 14C kaBP (Delibrias et al 1979 Di Vito et al 1999) or to 122 varve ka BP based on theMonticchio varve chronology (Allen et al 1999) It is trachytic in composition andappears to have had a mainly eastwards dispersal
The Mercato Tephra dated to ca 80 14C ka BP and originally analysed usingEDS has a phonolitic composition and is believed to have been generated by Vesu-vius (Paterne et al 1988) New WDS data obtained from reference samples col-lected from an exposure to the west of Naples support these conclusions (table 1 andAppendix A) The silica content of the WDS analyses are ca 3 lower than thoseobtained using EDS (table 1) which may reregect the fact that the EDS data werenormalized
The only tephra listed in table 1 that is thought to have originated from the AeolianIslands is the Pollara pumice also referred to as the E2 tephra in marine sequences(Paterne et al 1986 1988) The limited geochemical data available so far suggest itto be the only Italian tephra listed in table 1 that is rhyolitic in composition Littlemore is known about this ash which has not been recorded extensively except thatits age is estimated to be ca 130 14C ka BP (Keller 1980)
5 Extending the known distributions of European tephras
Figure 2 summarizes schematically the known distributions of three of the tephrasreferred to in the preceding section the VA the LST and the NYT Following theintroduction of a laboratory method that enables the detection of micro-tephra parti-cles in mineral-rich sediment the VA has been traced to sites that are located muchfarther south (into The Netherlands) and east (as far as St Petersburg) than thedistribution limits based on occurrences of visible layers of the ash As a result con-tinental sequences over a much larger area in northern Europe can now be correlateddirectly with marine and ice-core records using the VA as a time-parallel marker
This suggests therefore that other prominent ash layers such as the LST andNYT should also be detectable over larger tracts of Europe than is presently thecase if suitable sites are examined for the presence of micro-tephra horizons To testthis assertion we examined lake sediment deposits of Last Termination age froma site in the northern Apennines in order to establish whether the NYT could bedetected in micro-tephra form The site selected Prato Spilla `Crsquo lies well to thenorth of the localities in central and southern Italy and in the Adriatic Sea fromwhich visible records of the NYT have been reported Prato Spilla `Crsquo lies at an alti-tude of ca 1350 m in the Appennino Parmense ca 60 km south of Parma and 15 kmeast of Pontremoli The site contains a continuous sediment sequence spanning theLast Termination and most of the Holocene Detailed pollen and coleopteran strati-graphical records which have been radiocarbon dated have been published for thissite (Lowe 1992 Ponel amp Lowe 1992 Lowe amp Watson 1993)
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Figure 6 Light microscope photograph of an NYT glass shard from Prato Spilla Crsquosequence assigned on geochemical grounds to the NYT
The methods adopted for sub-sampling of the Prato Spilla `Crsquo sequence for thequantishy cation of glass shard concentrations and for subsequent electron microprobeanalysis of selected glass shards followed those described elsewhere (Turney 1998)In summary contiguous samples of 1 cm stratigraphic interval were extracted fromthe sequence to establish presenceabsence of glass shards Each of the 1 cm3 blocksin which tephra particles was detected was then examined with more care andshard concentrations were quantishy ed for each sub-sample Micro-tephra particleswere detected in shy ve samples (shy gure 6) but were predominantly clustered around500 cm in the part of the sequence assigned on pollen-stratigraphic grounds to theLate Glacial Interstadial or the `Allerfrac12drsquo|indeed the part of the succession in whichthe NYT would be expected to occur Peak concentrations of micro-tephra particlesreach 225 shards cmiexcl3 and are conshy ned to a single 1 cm thick sample in the sequencewhich probably represents the time of maximum deposition of the ash
Electron microprobe measurements based on WDS were obtained from the surfacesof 21 separate glass shards extracted from the sample with peak shard concentrations(Appendix A) Since only EDS measurements were available for the NYT prior to thepresent study we also obtained WDS measurements from 17 shards extracted fromthe visible layer of NYT that is exposed on Procida Island which lies in the type-locality for the NYT close to the city of Naples (Appendix A) The results providenot only a more comprehensive geochemical dataset for the NYT than was previ-ously available but also a consistent basis for comparison with the Prato Spilla `Crsquodataset All of the WDS data reported here (Appendix A) were measured at the samelaboratory (Tephrochronology Analytical Unit University of Edinburgh) using thesame sample pretreatment and preparation protocol The WDS results for the NYTdinoter to a minor degree from the EDS results (table 1 and Appendix A) especiallywith respect to the amounts of silica aluminium and calcium measured The EDS
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788 S M Davies and others
4 8FeO ()
TiO
2 (
) Neapolitan Yellow Tuff(Procida)Neapolitan Yellow Tuff(Prato Spilla lsquoCrsquo)
0
1
2
3
40 50 60 70
MgO
(
)
SiO2 ()
K2O
(
)
40 50 60 70
0
04
08
4
8
12
SiO2 ()
(a)(b)
(c)
Figure 7 Bi-plots of SiO2 K2 O SiO2 MgO and FeOTiO2 for the WDS analyses obtainedfrom glass shards of the NYT from Procida (Naples) and Prato Spilla Crsquo Means and standarddeviations are shown
results show a higher degree of statistical scatter than the WDS measurements whichmay reregect the fact that the data were normalized combined with the inreguence ofvariation in water content between shards
There is a very close correspondence between the WDS data for the Prato Spilla `Crsquomicro-tephra shards and those obtained from the type-material near Naples (shy g-ure 7) The geochemical data strongly suggest therefore that the NYT is representedat the Prato Spilla `Crsquo site by a discrete layer of micro-tephra particles This conclu-sion is compatible with the pollen-stratigraphic data from the site and accords withage estimates for the NYT (ca 120 14C ka BP) obtained from other sites (Paterneet al 1990)
These results encourage us to believe that many if not all of the tephras listedin table 1 will be detectable over much larger tracts of Europe than is presently thecase if appropriate research is undertaken to detect layers of micro-tephra particlesin selected sites The authors are presently engaged in a major continent-wide pro-gramme of research in collaboration with a number of European research groupsdesigned to test this hypothesis The focus in this research is on those parts of Europewhere we expect to shy nd overlapping `apronsrsquo of tephra deposition originating fromthe Italian Eifel Massif Central and Icelandic provinces For example a number ofsites in parts of southern France northern Italy and perhaps western Switzerlandmay have received inreguxes of micro-tephra originating from the Italian and Eifelprovinces and perhaps also from the Massif Central Sites in parts of Germany Den-mark and southern Sweden for example may in turn have received tephra depositsfrom both of the Icelandic and Eifel provinces If this proves to be the case then thestage will be set for the construction of a tephrostratigraphical framework for Europewhich will enable Last Termination sequences to be correlated on a continent-widebasis using micro- and visible tephra layers as time-parallel stratigraphic markersFurthermore there is also the possibility that other tephras remain to be discovered
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European tephrochronological framework for Termination 1 789
those which either because of the magnitude or nature of some volcanic eruptionswere distributed over parts of Europe in micro-tephra form only
6 European tephrostratigraphy and the chronology of eventsduring the Last Termination and Early Holocene
One of the crucial issues in Late Quaternary palaeoenvironmental research thatremains to be resolved is the degree to which climatic events inferred from oceanicterrestrial and ice-core records were synchronous during the Last Termination andEarly Holocene If the ice-core records provide realistic estimates of the rates anddurations of climatic events during this period then comparisons between individ-ual records have to be enotected with at least a decadal precision The problem thispresents and the role that tephrostratigraphy can play in resolving some of thedimacr culties involved are put into perspective in shy gure 8
Figure 8 shows some of the data used to calibrate radiocarbon dates (the LakeSuigetsu and Cariaco Basin datasets) plotted against the GRIP ss08c ice-core recordof macr 18O variations The latter has been selected by the INTIMATE group as an arbi-trary and temporary standard for this period and used to deshy ne an event stratig-raphy scheme (shy gure 1) for the Last Termination (see Bjorck et al 1998 Walker etal 2001) As has been alluded to in earlier sections of this paper the uncertaintiesassociated with all of the dating methods currently employed preclude precise com-parisons of ice-core marine and terrestrial records Oceanic and terrestrial recordsmostly rely upon radiocarbon dating locally supplemented in a few cases by varvechronology Imprecisions in radiocarbon dates can arise through site-specishy c fac-tors (eg hard-water or mineral carbon errors in freshwater sequences and reservoirerrors in marine sequences) sample selection laboratory measurements of 14C activ-ity and other factors (Lowe amp Walker 2000) Further imprecision may be introducedby the calibration of radiocarbon dates since the uncertainties in the dataset usedto calibrate pre-Holocene radiocarbon dates INTCAL98 are far higher than forthe Holocene which is based on dendro-calibration (Stuiver et al 1998) There arealso uncertainties anotecting varve chronologies while the ss08c ice-core chronologyfor the Last Termination dinoters signishy cantly from the GISP2 record and indeedfrom other models of the GRIP record (Lowe et al 2001) Published comparisonsbetween ice-core marine and terrestrial records for the Last Termination seldom takeinto account the true magnitude of the dating uncertainties involved and frequentlyemploy circular reasoning
Figure 8 shows the positions on the radiocarbon time-scale of 20 of the tephrasdiscussed earlier in this paper these being the ones for which reasonably conshy dentradiocarbon age estimates can be made (though these will be subject to revised esti-mates in the future) A high number of these occur in the period 14080 14C kaBP but we conshy dently anticipate the discovery in the future of additional tephras(perhaps in micro-tephra form only) which will date to the period 185140 14C kaBP Tephras detected in the GRIP ice core over the same time-interval are plottedon the calendar time-scale in shy gure 8 By providing key `time-linesrsquo between recordstephrostratigraphy can help to resolve some of the dating uncertainties referredto earlier by for example enabling direct comparisons of discrepant age estimatesobtained using dinoterent methods (cf Litt et al 2001) It can also provide estimatesof the magnitudes of the reservoir errors that anotected various marine sectors at dif-
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790 S M Davies and others
-44
-40
-36
-32
cale
ndar
yea
rs B
P
8000
9000
10 0
00
11 0
00
12 0
00
13 0
00
14 0
00
15 0
00
16 0
00
17 0
00
18 0
00
14C age (BP)
VA
SA
Un
Un
Un
Un
Un
BF
Hol
ocen
eG
S-1
GI-
1aG
I-1b
GI-
1cG
I-1d
GI-
1eG
S-2
aG
S-2
bG
S-
2c
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cher
See
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ivel
le 5
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de D
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Saks
unar
vatn
Houmlg
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nU
lmen
er M
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3574
radiocarbon dated European tephra horizons
Cho
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Kili
an V
asse
tM
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to
God
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le 4
Pom
ici P
rinc
ipal
i amp V
edde
Polla
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-GS-
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-2B
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AS-
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raSu
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laye
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Gre
enis
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20 0
0018
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16 0
0014
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12 0
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800
600
400
200 0
GISP2 volcanicsulphate conc (ppb)
1000
Nea
polit
an Y
ello
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uff
GISP2 18O (permil) dGRIP 18O (permil) d
Figure 8 For description see opposite
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 791
ferent times through a comparison of radiocarbon dates obtained from marine andterrestrial horizons in which the same tephra has been detected (see for exampleAustin et al 1995 Bondevik et al 2001 Haregidason et al 2000) Tephrostratigraphymay provide an independent test of suggestions that some of the climatic changesduring the Last Termination were time-transgressive as illustrated for some appar-ently contrasting climatic trends in Iceland Britain and NW Russia (Lowe 2001) Ofparticular importance as far as establishing `leadsrsquo and `lagsrsquo in climatic changes isconcerned are the tephra records from the Greenland ice cores The discovery of theVedde and Saksunarvatn ashes in the GRIP record (Gronvold et al 1995) alreadyprovides a basis for making direct comparisons between marine terrestrial and ice-core records It is a matter of some urgency that the incidence of tephra depositsin the Greenland ice cores be more fully explored in the hope that this will lead tothe recognition of additional time-parallel links between the ice-core records on theone hand and oceanic and terrestrial records on the other An investigation of thenew NordGRIP record for this purpose is currently in progress (S M Davies 2002unpublished data)
Finally a fuller and more reshy ned tephrostratigraphical scheme for Europe will alsohave other applications It will provide an important database for those investigatingthe timing and frequency of volcanic eruptions in Europe during the past 20 000 yror so as well as of the geochemical evolution of the dinoterent volcanic centres overthat period A fuller record of the distribution of micro-tephras may also provideinformation on atmospheric circulation patterns during the dispersal and depositionperiods as well as on the nature and altitude of the eruption columns which mayin turn provide inferences about magma viscosity
This paper is a contribution to the INTIMATE project of the INQUA Palaeoclimate Com-mission and the work is supported by a Leverhulme Trust Research project (grant allocationnumber F07537C) entitled Testing hypotheses of rapid climate change using tephrochronol-ogyrsquo SMDrsquo s contribution was completed during possession of a NERC PhD studentship(GT 0499ES162) We are extremely grateful to Dr Peter G Hill for his assistance withthe EPMA analyses at the Tephrochronology Analytical Unit University of Edinburgh We alsothank Dr G Mastrolorenzo (Vesuvius Observatory) and Miss G Swindle for assistance duringthe macreld investigations in Naples Thanks are also expressed to two anonymous reviewers forcomments on an earlier draft
Appendix A
Table 2 shows the major oxide concentrations of NYT glass shards from Procidaand Prato Spilla `Crsquo and of the Mercato Tephra from the Naples area (see x 4 forsite context) All oxides are shown as weight and total iron is expressed as FeO
Figure 8 Radiocarbon calibration curve for Termination 1 and the Early Holocene compared with theGRIP macr 18 O event stratigraphy the GRIP ss08c and GISP2 macr 18 O records (wwwngdcnoaagov) andknown tephra horizons from this period The shaded areas represent the cooler climatic episodes andare labelled with the Greenland stratotype terminology (Bjorck et al 1998) Where radiocarbon agesare reported in table 1 as a range the mean is given here Abbreviations for GRIP horizons are asfollows Un unknown (approximate positions are given (S Johnsen 2001 personal communication))SA Saksunarvatn Ash VA Vedde Ash BF Black Feather Sulphate concentrations from the GISP2record are also shown (Zielinski et al 1996) Open circles denote radiocarbon calibration data fromLake Suigetsu (Kitagawa amp van der Plicht 2000) Filled circles denote radiocarbon calibration data fromCariaco Basin assuming a marine reservoir age of 420 14 C yr (Hughen et al 1998)
Phil Trans R Soc Lond A (2002)
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792 S M Davies and others
Tab
le2
Majo
roxi
de
con
cen
trati
on
sof
NY
Tgl
ass
shard
sfr
om
Pro
cida
an
dP
rato
Spil
laC
rsquoan
dof
the
Mer
cato
Tep
hra
from
the
Naple
sare
a(s
eex4
for
site
con
text
)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
roci
da)
1584
204
0177
634
201
106
828
635
197
5969
1W
DS
2598
603
9178
027
101
204
924
244
583
4965
8W
DS
3586
604
5173
631
100
805
924
342
183
0951
9W
DS
4583
903
9177
933
000
906
924
540
486
9958
3W
DS
5605
106
8179
126
901
204
923
243
086
1976
4W
DS
6591
704
5177
332
801
006
425
740
887
8968
0W
DS
7581
804
1178
031
501
107
125
640
086
9956
1W
DS
8589
504
2179
533
701
506
926
740
987
5970
4W
DS
9592
003
9178
135
101
007
026
443
585
7972
7W
DS
10
591
404
2174
631
601
105
723
442
482
6957
0W
DS
11
593
403
6177
131
301
506
726
439
188
5967
6W
DS
12
588
103
8176
128
100
505
525
141
583
4952
1W
DS
13
577
003
8176
533
500
807
228
140
384
8952
0W
DS
14
586
004
7179
735
300
706
827
842
984
6968
5W
DS
15
588
104
2180
629
400
505
924
937
993
0964
5W
DS
16
579
603
9178
536
501
308
228
836
087
1959
9W
DS
17
580
103
9177
631
500
907
327
039
488
9956
6W
DS
mea
n588
104
2177
631
901
006
525
940
686
9962
8
sd
(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(07
8)
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 793
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
rato
Spil
laC
rsquo)
1552
105
4177
247
401
914
38
735
578
9951
1W
DS
2557
305
7179
845
701
512
640
136
581
5960
6W
DS
3595
004
4173
724
302
003
117
652
877
8950
7W
DS
4575
704
2179
433
001
406
627
043
083
6953
7W
DS
5599
904
0178
826
401
304
421
841
688
4966
5W
DS
6591
103
8177
826
601
105
022
443
888
8960
2W
DS
7565
304
5180
939
501
410
532
535
791
8962
1W
DS
8597
606
9180
826
501
604
821
546
684
6970
7W
DS
9571
805
6179
939
801
109
932
240
883
6964
7W
DS
10
588
603
7176
527
601
104
721
042
487
7953
3W
DS
11
559
404
9180
544
501
812
339
435
878
6957
2W
DS
12
594
704
0181
328
301
705
522
144
785
6967
9W
DS
13
611
103
7187
016
900
802
419
938
195
9975
8W
DS
14
599
204
4181
128
601
404
620
844
986
6971
6W
DS
15
601
204
4177
328
302
004
722
446
385
5972
1W
DS
16
595
104
5176
428
801
504
722
744
884
3962
8W
DS
17
603
704
1177
825
101
503
520
348
181
2965
3W
DS
18
558
704
5179
647
401
813
139
836
879
0960
7W
DS
19
589
602
8178
830
901
606
622
436
091
8960
5W
DS
20
553
606
3178
647
401
913
840
136
978
0956
6W
DS
21
579
004
0175
739
000
708
328
338
286
7959
9W
DS
mea
n582
804
6179
033
401
507
427
341
484
8962
1
sd
(1
87)
(01
0)
(02
7)
(09
2)
(00
4)
(03
9)
(08
0)
(04
9)
(05
0)
(07
0)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
794 S M Davies and others
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)
1575
202
7194
219
701
101
016
374
766
9951
8W
DS
2575
802
9194
523
902
201
520
273
564
5959
0W
DS
3574
301
4205
219
101
100
416
481
266
1965
2W
DS
4575
500
7206
018
002
000
415
181
669
3968
6W
DS
5580
000
9208
018
601
300
515
883
367
1975
5W
DS
6571
001
0206
016
101
600
515
078
967
1957
2W
DS
7577
501
1201
117
101
500
620
675
655
4950
5W
DS
8573
700
9212
717
101
900
815
187
564
2973
9W
DS
9580
301
3208
715
801
400
824
81
754
1968
1W
DS
10
574
400
6211
18
402
00
516
480
567
8971
6W
DS
11
577
200
7214
212
501
200
829
879
247
962
6W
DS
12
572
200
9211
217
301
501
15
980
465
9966
3W
DS
13
571
800
7210
417
402
201
16
184
467
2971
2W
DS
14
567
300
9208
916
901
400
917
383
262
5959
3W
DS
15
568
600
8205
918
202
101
414
682
666
6960
8W
DS
16
572
501
1211
318
202
01
215
884
364
5970
9W
DS
17
572
901
2212
916
502
101
215
883
667
2973
4W
DS
18
573
01
4211
716
301
801
416
83
365
5970
4W
DS
19
569
201
1207
418
602
101
414
982
964
961
6W
DS
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
3)
(04
2)
(01
3)
(00
1)
(00
2)
(01
)(0
39)
(01
1)
(02
5)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
References
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Dugmore A J amp Newton A J 1998 Holocene tephra layers in the Faroe Islands Frodskaparrit46 191204
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Froggatt P C 1992 Standardisation of the chemical analysis of tephra deposits Report of theICCT working group Quat Int 1314 9396
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Hoek W Z amp Bohncke S J P 2001 Oxygen isotope wiggle matching as a tool for synchronisingice-core and terrestrial records over Termination 1 Quat Sci Rev 20 12511264
Hughen K A Overpeck J T Peterson L C amp Trumbore S 1996 Rapid climate changes inthe tropical Atlantic region during the last deglaciation Nature 380 5153
Hughen K A Overpeck J T amp Lehman J 1998 A new 14 C calibration data set for the LastDeglaciation Radiocarbon 39 483494
Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
Hunt J B amp Hill P G 1996 An inter-laboratory comparison of the electron probe microanalysisof glass geochemistry Quat Int 3436 229241
Hunt J B amp Hill P G 2001 Tephrological implications of beam sizesample size ereg ects inelectron microprobe analysis of glass shards J Quat Sci 16 105117
Hunt J B Fannin N G T Hill P G amp Peacock J D 1995 The tephrochronology andradiocarbon dating of North Atlantic Late Quaternary sediments an example from the StKilda Basin In The tectonics sedimentation and palaeoceanography of the North Atlanticregion (ed R A Scrutton M S Stoker G B Shimmield amp A W Tudhope) vol 90pp 227248 Geological Society of London Special Publication
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Jakobsson S P 1979 Outline of the petrology of Iceland Jokull 29 5773
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Juvignparae E 1993 Contribution microa la tparaephrostratigraphie du Quaternaire et son application microa lagparaeomorphologie Mparaem Serv Explicat Cartes Gparaeol Min Belg 36 166
Juvignparae E amp Gewelt M 1987 La Narse drsquo Ampoix comme tparaephrostratotype dans la Chasup3 ne desPuys mparaeridionale (France) Bull Ass Fr Etud Quat 29 3749
Juvignparae E Kozarski S amp Nowaczyk B 1995 The occurrence of Laacher See Tephra in Pomera-nia NW Poland Boreas 24 225231
Juvignparae E Bastin B Delibrias G Evin J Gewelt M Gilot E amp Streel M 1996 Acomprehensive pollen and tephra based chronostratigraphic model for the Lateglacial andHolocene period in the French Massif Central Quat Int 3436 113120
Keller J 1980 The island of Vulcano Rend Soc It Mineral Petrolog 36 369414
Keller J Ryan W B F Ninkovich D amp Altherr R 1978 Explosive volcanic activity in theMediterranean over the past 200 000 years as recorded in deep sea sediments Geol Soc AmBull 89 591604
Kitagawa H amp van der Plicht J 2000 Atmospheric radiocarbon calibration beyond 11 900 calBP from Lake Suigetsu laminated sediments Radiocarbon 42 369380
Kvamme T Mangerud J Furnes H amp Ruddiman W F 1989 Geochemistry of Pleistoceneash zones in cores from the North Atlantic Norsk Geol Tids 69 251272
Lacasse C Sigurdsson H Johannesson H Paterne M amp Carey S 1995 Source of Ash zone 1in the North Atlantic Bull Volcanol 57 1832
Langone L Asioli A Corregiari A amp Trincardi F 1996 Age depth modelling through theLate-Quaternary deposits of the central Adriatic Basin In Palaeoenvironmental analysis ofItalian crater lake and Adriatic sediments (ed F Oldmacreld amp P Guilizzoni) vol 55 pp 177196 Memorie dellrsquo Instituto Italiano di Idrobiologia
Larsen G 2000 Holocene volcanism in Iceland and tephrochronology as a tool in volcanologyIn Iceland 2000 modern processes and past environments Keele University UK
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 799
Litt T amp Stebich M 1999 Bio- and chronostratigraphy of the Lateglacial in the Eifel regionGermany Quat Int 61 516
Litt T Brauer A Goslar T Merkt J Balaga K Muller H Ralska-Jasiewiczowa MStebich M amp Negendank J F W 2001 Correlation and synchronisation of Lateglacialcontinental sequences in northern Central Europe based on annually laminated lacustrinesediments Quat Sci Rev 20 12331249
Long D amp Morton A C 1987 An ash fall within the Loch Lomond stadial J Quat Sci 297101
Lotter A F Eicher U Siegenthaler U amp Birks H J B 1992 Lateglacial climatic oscillationsas recorded in Swiss lake sediments J Quat Sci 7 187204
Lowe J J 1992 Lateglacial and Early Holocene lake sediments from the Northern ApenninesItaly|pollen stratigraphy and radiocarbon dating Boreas 21 193208
Lowe J J 2001 Abrupt climatic changes in Europe during the last glacialinterglacial tran-sition the potential for testing hypotheses on the synchroneity of climatic events usingtephrochronology Global Planet Change 603 7384
Lowe J J amp Turney C S M 1997 Vedde Ash layer discovered in a small lake basin on theScottish mainland J Geol Soc Lond 154 605612
Lowe J J amp Walker M J C 2000 Radiocarbon dating the last glacialinterglacial transition(ca 14914 C ka BP) in terrestrial and marine records the need for new quality assuranceprotocols Radiocarbon 42 5368
Lowe J J amp Watson C 1993 Lateglacial and Early Holocene pollen stratigraphy of the northernApennines Italy Quat Sci Rev 12 727738
Lowe J J Birks H H Brooks S J Coope G R Harkness D D Mayle F E SheldrickC Turney C S M amp Walker M J C 1999 The chronology of palaeoenvironmental changesduring the Last GlacialHolocene transition towards an event stratigraphy for the BritishIsles J Geol Soc Lond 156 397410
Lowe J J Hoek W Z amp INTIMATE group 2001 Inter-regional correlation of palaeoclimaticrecords for the Last GlacialInterglacial transition a protocol for improved precision recom-mended by the INTIMATE project group Quat Sci Rev 20 11751187
Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
Mangerud J Lie S E Furnes H Kristiansen I L amp Liquest mo L 1984 A Younger Dryas ashbed in western Norway and its possible correlation with tephra beds from the Norwegian Seaand North Atlantic Quat Res 21 85104
Mangerud J Furnes H amp Jparaohansen J 1986 A 9000 year-old ash bed on the Faroe IslandsQuat Res 26 262265
Martini J 1970 Recherche de retombparaees volcaniques dans le sud-est de la France et la Suisseoccidentale Arch Sci 23 641674
Martini J amp Duret J J 1965 Note preliminaire sur la presence drsquo un niveau de cendres vol-caniques dans des sparaediments post-glaciaires des environs de Genmicroeve Arch Sci 18 587588
Mayewski P A Meeker L D Twickler M S Whitlow S Yang Q Lyons W B amp Pren-tice M 1997 Major features and forcing of high latitudes Northern Hemisphere atmosphericcirculation using a 110 000 year long glaciochemical series J Geophys Res 102 345365
Merkt J Muller H Knabe W Muller P amp Weiser T 1993 The Early Holocene Saksunarvatntephra found in lake sediments in NW Germany Boreas 22 93100
Narcisi B 1993 Segnalazione di un livello piroclastico di provenienza etnea nellrsquo area del Fucino(Italia Centrale) Quaternario 6 8792
Narcisi B 1996 Tephrochronology of a Late Quaternary lacustrine record from the Monticchiomaar (Vulture volcano southern Italy) Quat Sci Rev 15 155165
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
800 S M Davies and others
Newton A J amp Dugmore A J 1993 Tephrochronology of Core C from Lago Grande di Mon-ticchio In Paleolimnology of European Maar Lakes (ed J F W Negendank amp B Zolitschka)Lecture Notes in Earth Science vol 49 333348 Springer
Oldmacreld F Appleby P G amp Thompson R 1980 Palaeoecological studies of lakes in theHighlands of Papua New Guinea J Ecol 68 457477
Orsi G Drsquo Antonio M de Vita S amp Gallo G 1992 The Neapolitan Yellow Tureg a large mag-nitude trachytic phreatoplinian eruption eruptive dynamics magma withdrawal and calderacollapse J Volcanol Geotherm Res 53 275287
Paterne M Guichard F Labeyrie J Gillot P Y amp Duplessy J C 1986 Tyrrhenian Seatephrochronology of the oxygen isotope record for the past 60 000 years Mar Geol 72259285
Paterne M Guichard F amp Labeyrie J 1988 Explosive activity of the south Italian volca-noes during the past 80 000 years as determined by marine tephrochronology J VolcanolGeotherm Res 34 153172
Paterne M Labeyrie J Guichard F Mazaud A amp Maitre F 1990 Fluctuations of the Cam-panian explosive volcanic activity (south Italy) during the past 190 000 years as determinedby marine tephrochronology Earth Planet Sci Lett 98 166174
Pawse A Beske-Diehl S amp Marshall S A 1998 Use of magnetic hysteresis properties andelectron spin resonance spectroscopy for the identimacrcation of volcanic ash a preliminary studyGeophys J Int 132 712720
Pearce N J G Westgate J A amp Perkins W T 1996 Developments in the analysis of singleglass shards in volcanic deposits by laser ablation ICP-MS quantitative and single internalstandard multi-element methods Quat Int 3436 213227
Pearce N J G Westgate J A Perkins W T Eastwood W J amp Shane P 1999 Theapplication of laser ablation ICP-MS to the analysis of volcanic glass shards from tephradeposits bulk glass and single shard analysis Global Planet Change 21 151171
Pilcher J R amp Hall V A 1992 Towards a tephrochronology for the Holocene of the north ofIreland Holocene 2 255259
Ponel P amp Lowe J J 1992 Coleopteran pollen and radiocarbon evidence from the Prato Spillarsquo Drsquo succession N Italy C R Acad Sci Paris Sparaer II 315 14251431
Rose N L Golding P N E amp Battarbee R W 1996 Selective concentration and enumerationof tephra shards from lake sediment cores Holocene 6 243246
Ruddiman W F amp Glover L K 1972 Vertical mixing of ice rafted volcanic ash in NorthAtlantic sediments Geol Soc Am Bull 83 28172836
Ruddiman W amp McIntyre A 1981 The North Atlantic Ocean during the last deglaciationPalaeogeogr Palaeoclimatol Palaeoecol 35 145214
Santacroce R 1987 Somma Vesuvius Quad Ric Sci 114 252
Sarna-Wojcicki A 2000 Tephrochronology In Quaternary geochronology methods and applica-tions (ed J S Noller J M Sowers amp W R Lettis) AGU Reference shelf vol 4 pp 357377Washington DC American Geophysical Union
Sejrup H P Sjiquest holm J Furnes H Beyer I Eide L Jansen E amp Mangerud J 1989Quaternary tephrochronology on the Iceland Plateau north of Iceland J Quat Sci 4 109114
Sikes E L Samson C R Guilderson T P amp Howard W R 2000 Old radiocarbon agesin the southwest Pacimacrc Ocean during the last glacial period and deglaciation Nature 405555558
Stein R Nam S-I Grobe H amp Hubbersten H 1996 Late Quaternary glacial history andshort term ice rafted debris deg uctuations along the East Greenland continental marine In LateQuaternary palaeoceanography of the North Atlantic margins (ed J T Andrews W E NAustin H Bergsten amp A E Jennings) pp 135151 Geological Society London SpecialPublication
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 801
Stuiver M amp Grootes P M 2000 GISP2 oxygen isotope ratios Quat Res 53 277284
Stuiver M Reimer P J Bard E Beck J W Burr G S Hughen K A Kromer BMcCormac G Van der Plicht J amp Spurk M 1998 INTCAL 98 radiocarbon age calibration24 0000 cal BP Radiocarbon 40 10411083
Sweatman T R amp Long J V P 1969 Quantitative electron microprobe analysis of rock formingminerals J Petrol 7 332379
Turney C S M 1998 Extraction of rhyolitic ash from minerogenic lake sediments J Paleolim-nol 19 199206
Turney C S M amp Lowe J J 2001 Tephrochronology In Tracking environmental changes inlake sediments physical and chemical techniques (ed W M Last amp J P Smol) DordrechtKluwer Academic
Turney C S M Harkness D D amp Lowe J J 1997 The use of microtephra horizons tocorrelate Lateglacial lake sediments successions in Scotland J Quat Sci 12 525531
Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
van den Bogaard P amp Schmincke H 1985 A widespread isochronous Late Quaternary tephralayer in central and northern Europe Geol Soc Am Bull 96 15541571
van den Bogaard B Dordeg er W Sandgren P amp Schmincke H-U 1994 Correlating theHolocene records Icelandic tephra found in Schleswig-Holstein (northern Germany) Natur-wissenschaften 81 554556
Vernet G amp Raynal J-P 2001 Tephrostratigraphy of the Limagne revisited Implications forLateglacial and Holocene Prehistory In Tephras chronology archaeology (ed E Juvignparae ampJ-P Raynal) pp 111116 Dossiers de lrsquo ArchparaeoLogis no 1 France
Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
Vezzoli L 1991 Tephra layers in Bannock Basin (eastern Mediterranean) Mar Geol 1002134
von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
Walker M J C Bjorck S Lowe J J Cwynar L C Johnsen S Knudsen K-L WohlfarthB amp INTIMATE Group 1999 Isotopic events in the GRIP ice core a stratotype for the LatePleistocene Quat Sci Rev 18 11431150
Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
802 S M Davies and others
Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
770 S M Davies and others
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Ref
eren
ces
1
this
stu
dy
2
Pate
rne
etal
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3
Narc
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4
All
enet
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5
An
dro
nic
oet
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6
Ju
vig
nparae
et
al
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7
Bir
ks
et
al
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8
Bjo
rck
ampW
ast
egordma
rd(1
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9
Du
gm
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ampN
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n(1
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10
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rck
et
al
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mm
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t(1
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14
Di
Vit
oet
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15
Del
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as
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(1979)
16
Ju
vig
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etal
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17
Dav
ies
et
al
(2001)
18
van
den
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chm
inck
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19
Fri
edri
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20
Bra
uer
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21
Etl
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22
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rney
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Pate
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Eir
parasup3kss
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26
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(2000)
27
Ale
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etal
(1976)
28
Vez
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(1991)
29
San
tacr
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(1987)
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European tephrochronological framework for Termination 1 771
Tab
le1
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9
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ewel
t(1
987)
14
Di
Vit
oet
al
(1999)
15
Del
ibri
as
etal
(1979)
16
Ju
vig
nparae
etal
(1987)
17
Dav
ies
et
al
(2001)
18
van
den
Bogaard
ampS
chm
inck
e(1
985)
19
Fri
edri
chet
al
(1999)
20
Bra
uer
eta
l(1
999)
21
Etl
ich
eret
al
(1987)
22
Tu
rney
etal
(1997)
23
Pate
rne
et
al
(1986)
24
Kel
ler
(1980)
25
Eir
parasup3kss
on
etal
(2000)
26
Hadeg
idaso
net
al
(2000)
27
Ale
ssio
etal
(1976)
28
Vez
zoli
(1991)
29
San
tacr
oce
(1987)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
772 S M Davies and others
Tab
le1
(Con
t)
(Th
eva
rve
age
for
the
Laach
erS
ee(E
)rsquoro
wis
12
880
yea
rs)
GR
IPage
tep
hra
age
(ss0
8c
volc
an
ich
ori
zon
(14C
yrs
)ti
me-
scale
)n
SiO
2T
iO2
Al 2
O3
FeO
Mn
OM
gO
CaO
Na
2O
K2O
P2O
5to
tal
EP
MA
sou
rce
ref
IT
HO
L-2
10
70
0
13
470
727
7152
9132
002
364
7110
928
104
6
994
0W
DS
Gri
msv
otn
10
11
(IC
)1
080
0(0
95)
(03
)(0
38
)(0
5)
(00
6)
(08
6)
(07
4)
(02
6)
(00
6)
un
kn
own
12
385
sect6
0
(Ca
pea
k)
(16
530
m)
God
ivel
leca
1
070
010
523
723
192
867
419
831
977
736
326
9
999
5W
DS
Lac
Ch
au
vet
6
16
5(M
C)
Lac
drsquoe
nH
au
tP
uy
de
Tart
are
tL
ac
de
laF
age
Laach
er11
000
sect50
39
578
4
228
515
604
5
03
2113
553
7
100
ED
SL
aach
erS
ee1820
See
(E)
11
063
sect12
(06
9)
(0
26
)(0
07)
(00
5)
(0
03
)(0
75
)(0
33)
29
595
501
0214
818
200
700
210
485
969
9
100
ED
S(0
70)
(00
7)
(02
8)
(01
4)
(00
8)
(00
5)
(01
3)
(09
7)
(04
2)
27
604
801
8210
019
200
200
614
174
272
1
100
ED
S(0
55)
(00
7)
(01
7)
(02
3)
(00
5)
(00
9)
(02
7)
(06
4)
(04
7)
30
598
604
3201
823
300
102
018
071
578
0
100
ED
S
(07
7)
(02
3)
(04
6)
(03
3)
(00
4)
(02
5)
(06
1)
(08
)(0
46)
un
kn
own
12
820
sect60
(C
ap
eak)
(16684
m)
Ref
eren
ces
1
this
stu
dy
2
Pate
rne
etal
(1988)
3
Narc
isi
(1996)
4
All
enet
al
(1999)
5
An
dro
nic
oet
al
(1995)
6
Ju
vig
nparae
et
al
(1996)
7
Bir
ks
et
al
(1996)
8
Bjo
rck
ampW
ast
egordma
rd(1
999)
9
Du
gm
ore
ampN
ewto
n(1
998)
10
Bjo
rck
et
al
(1992)
11
Kva
mm
eet
al
(1989)
12
Zoli
tsch
ka
etal
(1995)
13
Ju
vig
nparae
ampG
ewel
t(1
987)
14
Di
Vit
oet
al
(1999)
15
Del
ibri
as
etal
(1979)
16
Ju
vig
nparae
etal
(1987)
17
Dav
ies
et
al
(2001)
18
van
den
Bogaard
ampS
chm
inck
e(1
985)
19
Fri
edri
chet
al
(1999)
20
Bra
uer
eta
l(1
999)
21
Etl
ich
eret
al
(1987)
22
Tu
rney
etal
(1997)
23
Pate
rne
et
al
(1986)
24
Kel
ler
(1980)
25
Eir
parasup3kss
on
etal
(2000)
26
Hadeg
idaso
net
al
(2000)
27
Ale
ssio
etal
(1976)
28
Vez
zoli
(1991)
29
San
tacr
oce
(1987)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 773
Tab
le1
(Con
t)
GR
IPage
tep
hra
age
(ss0
8c
volc
an
ich
ori
zon
(14C
yrs
)ti
me-
scale
)n
SiO
2T
iO2
Al 2
O3
FeO
Mn
OM
gO
CaO
Na
2O
K2O
P2O
5to
tal
EP
MA
sou
rce
ref
La
Nu
gmicroere
ca11
400
12
549
922
9160
470
002
324
454
744
538
972
4W
DS
La
Nu
gmicroere
6
21
(MC
)
Nea
poli
tan
ca12
000
17
588
104
2177
631
901
006
525
940
686
9
962
8W
DS
Cam
pi
1Y
ello
w(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(0
78)
Fle
gre
i
Tu
reg(I
T)
568
106
0194
448
7
17
451
938
75
5
100
ED
S
596
804
9192
940
3
06
435
034
588
9
100
ED
S2
14
619
403
1196
329
9
02
019
943
485
7
100
ED
S
Borr
ob
ol
ca12
300
18
733
601
1122
914
700
601
207
635
837
6
955
1W
DS
Hek
la22
(IC
)(0
35)
(00
2)
(01
8)
(00
9)
(00
2)
(00
2)
(00
3)
(01
4)
(00
9)
(0
47)
un
kn
ow
n14
650
sect200
(Ca
pea
k)
(17458
m)
un
kn
ow
n14
650
sect200
(C
ap
eak)
(17506
m)
E-2
P
oll
ara
ca13
000
766
302
7138
810
8
01
015
025
239
7
100
ED
SA
eoli
an
2
23
24
pu
mic
e(I
T)
Isla
nd
s
KO
L-G
S-2
13
400
18
490
910
6148
8100
702
184
9126
521
400
902
8989
6W
DS
25
(IC
)
GS
-2B
AS
-113
400
3497
417
0132
7124
402
266
6118
124
802
103
4988
7W
DS
26
(IC
)
Ref
eren
ces
1
this
stu
dy
2
Pate
rne
etal
(1988)
3
Narc
isi
(1996)
4
All
enet
al
(1999)
5
An
dro
nic
oet
al
(1995)
6
Ju
vig
nparae
et
al
(1996)
7
Bir
ks
et
al
(1996)
8
Bjo
rck
ampW
ast
egordma
rd(1
999)
9
Du
gm
ore
ampN
ewto
n(1
998)
10
Bjo
rck
et
al
(1992)
11
Kva
mm
eet
al
(1989)
12
Zoli
tsch
ka
etal
(1995)
13
Ju
vig
nparae
ampG
ewel
t(1
987)
14
Di
Vit
oet
al
(1999)
15
Del
ibri
as
etal
(1979)
16
Ju
vig
nparae
etal
(1987)
17
Dav
ies
et
al
(2001)
18
van
den
Bogaard
ampS
chm
inck
e(1
985)
19
Fri
edri
chet
al
(1999)
20
Bra
uer
eta
l(1
999)
21
Etl
ich
eret
al
(1987)
22
Tu
rney
etal
(1997)
23
Pate
rne
et
al
(1986)
24
Kel
ler
(1980)
25
Eir
parasup3kss
on
etal
(2000)
26
Hadeg
idaso
net
al
(2000)
27
Ale
ssio
etal
(1976)
28
Vez
zoli
(1991)
29
San
tacr
oce
(1987)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
774 S M Davies and others
Tab
le1
(Con
t)
(Th
evarv
eage
for
the
Gre
enis
h(I
T)rsquo
row
is17
560
yea
rs)
GR
IPage
tep
hra
age
(ss0
8c
volc
an
ich
ori
zon
(14C
yrs
)ti
me-
scale
)n
SiO
2T
iO2
Al 2
O3
FeO
Mn
OM
gO
CaO
Na
2O
K2O
P2O
5to
tal
EP
MA
sou
rce
ref
GS
-2B
AS
-213
400
6497
933
2122
4147
902
445
389
829
905
205
4979
4W
DS
26
(IC
)
GS
-2B
AS
-313
400
2538
529
9125
7131
203
132
174
729
507
707
7980
1W
DS
26
(IC
)
GS
-2B
AS
-414
000
7503
617
4145
1113
202
155
3100
528
010
5
975
7W
DS
26
(IC
)
Un
ita
dei
ca14
000
5648
804
7184
625
901
602
217
432
679
302
8100
ED
SP
hle
gre
an
3
27
Tef
ra(0
53
)(0
13
)(0
25)
(07
4)
(01
4)
(01
6)
(01
6)
(03
4)
(06
6)
(01
6)
Fie
lds
Su
per
iori
(IT
)
Y-1
(IT
)ca
14
000
16
600
413
7169
555
502
218
242
262
229
306
8100
ED
SE
tna
28
Bla
ck17
000
sect300
Fea
ther
(17890
m)
Gre
enis
hca
15
000
9618
704
190
731
601
804
328
531
586
202
6100
ED
SV
esu
viu
s3
4
(IT
)(0
70
)(0
08
)(0
45)
(06
8)
(01
0)
(01
0)
(05
9)
(05
3)
(05
8)
(01
6)
29
L9
(IT
)ca
16
000
15
626
704
4188
630
401
103
329
429
683
402
7100
ED
SV
esu
viu
s3
15
17
000
(14
2)
(01
4)
(07
2)
(11
1)
(00
9)
(02
4)
(06
6)
(04
8)
(06
5)
(01
8)
St
2-1
85
18
500
7504
015
1145
5112
002
466
9114
525
206
6
992
2W
DS
26
(IC
)
Ref
eren
ces
1
this
stu
dy
2
Pate
rne
etal
(1988)
3
Narc
isi
(1996)
4
All
enet
al
(1999)
5
An
dro
nic
oet
al
(1995)
6
Ju
vig
nparae
et
al
(1996)
7
Bir
ks
et
al
(1996)
8
Bjo
rck
ampW
ast
egordma
rd(1
999)
9
Du
gm
ore
ampN
ewto
n(1
998)
10
Bjo
rck
et
al
(1992)
11
Kva
mm
eet
al
(1989)
12
Zoli
tsch
ka
etal
(1995)
13
Ju
vig
nparae
ampG
ewel
t(1
987)
14
Di
Vit
oet
al
(1999)
15
Del
ibri
as
etal
(1979)
16
Ju
vig
nparae
etal
(1987)
17
Dav
ies
et
al
(2001)
18
van
den
Bogaard
ampS
chm
inck
e(1
985)
19
Fri
edri
chet
al
(1999)
20
Bra
uer
eta
l(1
999)
21
Etl
ich
eret
al
(1987)
22
Tu
rney
etal
(1997)
23
Pate
rne
et
al
(1986)
24
Kel
ler
(1980)
25
Eir
parasup3kss
on
etal
(2000)
26
Hadeg
idaso
net
al
(2000)
27
Ale
ssio
etal
(1976)
28
Vez
zoli
(1991)
29
San
tacr
oce
(1987)
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 775
Altogether 34 tephra layers have been reported from sediment sequences in Europeand the NE Atlantic region which date to the period between 185 and 80 14C ka BP(table 1) Because tephra layers are deposited virtually instantaneously (in geologicalterms) they enotectively represent time-parallel marker horizons within stratigraphicalsequences (Westgate amp Gorton 1981 Sarna-Wojcicki 2000 Turney amp Lowe 2001) Intheory therefore all 34 tephras could prove valuable for correlation purposes eitherin a local context or in those cases where the ash deposits have been widely dispersedbetween regional sequences In practice however very little is known about the fullgeographical dispersal of the majority of the ash layers listed in table 1 Furthermorecorrelation by tephrostratigraphy will only work if the various ash layers have wellcharacterized geochemical signatures While some geochemical data are available forthe majority of the tephras listed in table 1 the collective data are far from robustand no geochemical data have yet been published for some
Nonetheless there is mounting evidence to show that some of the tephra depositslisted in table 1 are not only geochemically distinct but are also much more widelydispersed across Europe than was initially realized Stratigraphic records of thebetter-known tephras were initially limited to observations of visible tephra layersThe development of a technique that enables detection of tephra layers that are invis-ible to the naked eye (micro-tephra) in Late Glacial sequences has greatly extendedthe area over which some of the ashes can be traced (Lowe amp Turney 1997 Turneyet al 1997 Turney 1998 Wastegard et al 1998 2000a b) Most of this research sofar has focused on micro-tephra layers originating from Icelandic centres distributedthroughout northern Europe Here we report on further development of this line ofresearch with new evidence for the occurrence of micro-tephra layers in a site insouthern Europe The results suggest that there is great potential for tracing someash layers that originated from Italian volcanic complexes over much larger tracts ofsouthern and central Europe than records of visible tephra deposits allow This inturn greatly enhances the scope for making precise correlations not only betweenparts of southern Europe but also between continental and marine (MediterraneanSea) sequences
2 Micro-tephra extraction techniques
Micro-tephra horizons are composed of glass shards that are generally between 80and 24 m m (long axis) in size and that are present in such low concentration insedimentary sequences that they can only be detected by the use of a particle sep-aration technique Several factors inreguence the concentration of shards such as dis-tance from the volcanic source precipitation patterns during the eruption and sub-sequent tephra dispersal and sedimentary processes within the catchment In someterrestrial sequences micro-tephra horizons with a peak concentration (peak con-centration tends to coincide with the shy rst occurrence of glass shards in a sedimentsequence which is then taken to mark the time of maximum ash deposition) as lowas 10 shards cmiexcl3 has been conshy rmed whereas other sites have recorded as muchas 8000 shards cmiexcl3 (Turney et al 1997) In complete contrast tephra horizons inthe GRIP ice core have been identishy ed based on a single glass shard only (Gronvoldet al 1995)
Enotective separation techniques for the detection and isolation of tephra particlesfrom sedimentary sequences have been developed These include ashing of organic
Phil Trans R Soc Lond A (2002)
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776 S M Davies and others
matter (Pilcher amp Hall 1992) digestion of biogenic and opaline silica (Rose et al 1996) the use of magnetic properties of ash layers (see for example Oldshy eld et al 1980 van den Bogaard et al 1994 Pawse et al 1998) X-ray analysis (Dugmore ampNewton 1992) and a density separation (regotation) technique (Turney 1998) Den-sity separation has proved exceedingly useful for the detection of small glass shardspresent in low concentrations in mineral-rich Late Glacial sediments This involvesthe separation and concentration of particles of predetermined specishy c gravity withthe use of a heavy liquid and subsequent identishy cation of glass shards with the useof a polarizing light microscope (for further details see Turney (1998)) This methodhas been particularly successful in the detection of tephras of rhyolitic compositionthat have a specishy c density of 2325 g cmiexcl3 (Lowe amp Turney 1997 Turney et al 1997 2001 Turney 1998 Wastegard et al 1998 2000a b) It is this technique thathas resulted in the wider recognition of micro-tephras in Europe as discussed below
3 Geochemical ` ngerprintingrsquo of tephra layers
The 34 tephras listed in table 1 have originated from four major volcanic complexesIceland the Massif Central in central France the Eifel district near Bonn and threevolcanic centres in Italy (the Campanian group Etna and the Aeolian Islands (seeshy gure 2)) An important matter to resolve is the extent to which the various magmasand ashes generated by these volcanic complexes can be geochemically shy ngerprintedThis is especially important in the case of tephras which have originated from thesame volcanic centre in which there may have been limited geochemical evolution ofmagmas over time In this section we summarize the approach generally adopted todetermine the geochemical character of visible and micro-tephras as background tothe geochemical data summarized in table 1 In the subsequent section of the paperwe review the present state of knowledge concerning all 34 tephras listed in table 1
Glass shards formed during the rapid cooling of magma are thought to have acomposition that is representative of the bulk geochemistry of the magma (Barker1983) hence widely dispersed glass particles are regarded as the most appropriateconstituents of pyroclastic material for geochemical analysis If a tephra deposit canbe shown to have a distinct geochemical signature then it can be used to correlatethe stratigraphic units in which it occurs (tephrostratigraphy) as well as to datethese units (tephrochronology) if the ages of the tephras are known (Westgate ampGorton 1981) A key element of building a tephrostratigraphical framework there-fore is to establish as rigorously as possible the geochemical composition of theindividual tephras used in its construction Robust and directly comparable geo-chemical datasets are dimacr cult to assemble for glass however because it is highlyunstable material particularly prone to sodium mobilization
The technique most widely employed to establish the geochemical signature of atephra is electron probe micro-analysis (EPMA) This enables grain-discrete determi-nations of the major elements within an individual glass shard which is of particularbeneshy t in the analysis of micro-tephra layers which generally contain glass particlesin low concentration The glass surface is bombarded with an electron beam and theX-ray energy produced is unique to each element while the intensity of the signalemitted is proportional to the amount of that element in the glass shard (Hunt amp Hill1993) Measurement can be by either energy dispersive spectrometry (EDS) or wave-length dispersive spectrometry (WDS) EDS has a lower precision mainly because
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 777
N
0 500 km
Confirmed records of Vedde Ash (visible occurrences)
New records of Vedde Ash from flotation method
Extended area of Vedde Ash detection (micro-tephra)
Known area of Laacher See Tephra (visible occurrences)
Confirmed records of Neapolitan Yellow Tuff (visible occurrences)
New record of Neapolitan Yellow Tuff from flotation method
Known area of Neapolitan Yellow Tuff
Volcanic centres of particular relevance to this study
Other major volcanic centres in Europe
Figure 2 Location of the principal volcanic centres that were active during Termination 1 andthe Early Holocene The known distribution of the Vedde Ash (VA) Laacher See (LST) andNeapolitan Yellow Tureg (NYT) are shown
the behaviour of each element cannot be monitored independently during measure-ment and so this approach fails to detect for example any signishy cant mobilizationof sodium during the bombardment process (Hunt amp Hill 1993) Although WDSrequires a higher beam current and a longer counting time than EDS the formeronoters the distinct advantage of sequential acquisition of elemental data so that thedegree of sodium loss can be tracked The morphology of individual glass shards canalso distort EDS data a problem that is reduced when using WDS because for thisprocedure glass shards are mounted in an epoxy resin and polished to provide aregat surface for analysis Hence data should always be obtained using WDS whereverpossible
Even when WDS is used as a common tool for determining the geochemical spectraof samples aberrant results can arise that inreguence data comparisons For examplesome glass shards may contain tiny crystalline inclusions of feldspar and these shouldbe avoided when selecting surface points for analysis (Hunt amp Hill 2001) Hunt amp Hill
Phil Trans R Soc Lond A (2002)
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778 S M Davies and others
6
4
2
40 50 60 70 80
K2O
(
)
SiO2 ()
Laacher See
Iceland
Veidivoumltn-Dyngjufjoumlll
Katla (basalt)
Grimsvoumltn-Kverkfjoumlll
Hekla
Katla (rhyolitic)
0
Icelandic volcanic centres8
10
Massif Central
Etna
Campanian
Figure 3 Bi-plot of SiO2 and K2 O concentrations in tephras derived from the main Europeanash provinces (modimacred after Mangerud et al 1984) The Campanian Massif Central and Etnaconcentrations are based on the data presented in table 1
(2001) have concluded that small variations in the laboratory procedures employedto determine glass chemistry can lead to misidentishy cation of sources for glass shardsand give an example of shards with a Jan Mayen provenance wrongly attributedto an Icelandic source Clearly there is a need for standardization of laboratoryprocedures and while a number of recommendations have recently been advocated(Froggatt 1992 Hunt amp Hill 1993 Hunt et al 1998) there is still some variation inlaboratory and operator practice (Hunt amp Hill 1996) Standardization is also requiredin the form in which results are presented to ensure comparability Normalizationof the data to 100 a practice employed by some researchers can obscure poorresults and hence lead to incorrect comparisons (Hunt amp Hill 1993) However othersargue that it may actually facilitate comparisons between samples by removing thedistorting enotects of the water component contained in glass shards (see for exampleFroggatt 1992) The majority of the published Italian and some of the Eifel datahave been normalized while those from other parts of Europe have not and hencedata comparisons are not always straightforward
Table 1 provides mean values and standard deviations for major oxide concentra-tions obtained from those tephras for which data are presently available The tableincludes previously unpublished WDS results for the Neapolitan Yellow Tunot (NYTdiscussed in x 4 below) and for the Mercato Tephra While individual tephra layersmay be geochemically distinct the geochemical envelopes representing the collectivedata obtained from all of the tephras assigned to each major volcanic province showsignishy cant overlaps as is illustrated in the bi-plots and ternary plots (shy gures 3 and 4)of selected oxide concentration data It is clear therefore that measurement of majoroxide concentrations does not satisfactorily discriminate between some tephras orig-inating from dinoterent volcanic centres (as noted by van den Bogaard amp Schmincke(1985) and Frezzotti amp Narcisi (1996) with respect to Eifel and Italian tephras)nor of tephras of dinoterent age originating from the same volcanic centre (Bond et
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European tephrochronological framework for Termination 1 779
40 50 60 70 80
K2O
(
)
SiO2 ()
shyshyshyshy
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shyshy
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shy
shy
shy
shy
reg
reg regreg
regregregregreg regregregregreg
FF
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4 8 12 16
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l shyshyshyshyshy shyshyshyshyshyshy
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F
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ll
FeO ()
TiO
2 (
)
reg
l
Iceland
Eifel
F
shy ItalyMassif Central
100
80
60
40
20
100
80
60
40
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100 80 60 40 20
CaO
FeO
K2O
regregreg
reg
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lllshy
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0
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regreg
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FF
F
100
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60
40
20
100
80
60
40
20
100 80 60 40 20
K2ONa2O
CaO
(c) (d)
(a)
(b)
Figure 4 Plots of selected geochemical data obtained from tephras of Termination 1 age (seetable 1) (a) Bi-plot of mean SiO2 and K2 O values (b) Bi-plot of mean FeO and TiO2 values(c) Ternary plot indicating variations in the proportions of FeO CaO and K2 O (d) Ternaryplot indicating variations in the proportion of CaO Na2 O and K2 O
al 2001) Individual tephra layers are presently assigned to a particular volcanicevent on the basis of a combination of criteria usually including examination of thephysical properties (eg refractive index and surface detail of the glass shards) thestratigraphic position of the layer and independent assessment of the age of the layeras well as any geochemical data that may be available The construction of a tephro-stratigraphical scheme would clearly beneshy t from the application of a more diagnostic
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780 S M Davies and others
geochemical tool One approach that has promise is the analysis of trace and rareearth elements using an ultraviolet laser ablation inductively coupled plasma massspectrometer (UV-LA-ICP-MS) (Pearce et al 1996 1999 Eastwood et al 1999)This approach has been applied successfully to analysis of tephras of Mid-Holoceneage but not yet to tephras that fall within the period of interest here
4 Tephra layers in Europe and the North Atlantic regiondated to between 185 and 80 14C ka
(a) Icelandic province
The Icelandic volcanic systems are divided into three main groups based on theirgeochemical characteristics tholeiitic basalts transitional alkali basalts and alkaliolivine basalts (Jakobsson 1979) Collectively magmas from the Icelandic provincespan a wide geochemical spectrum although individual volcanic centres have tightgeochemical distributions (shy gure 3) for four of the main centres Grimsvotn-Kverfjolland Veidvotn-Dyngjufoll which form part of the northern (tholeiitic) volcanic zoneand Hekla and Katla which fall within the eastern (alkali olivine basalt and transi-tional alkali basalt) volcanic zone (Haregidason et al 2000) These appear to be thekey centres for the tephras listed in table 1 that have been assigned an Icelandicorigin
One of the best-known and most widely dispersed tephra horizons in northernEurope that has an Icelandic origin is the Vedde Ash (VA) which was depositedca 103 14C ka BP (Birks et al 1996 Wastegard et al 1998) within the GS-1Younger Dryas chronozone This ash is believed to originate from the Katla complexwithin the transitional alkali basalt province (Mangerud et al 1984 Lacasse et al 1995) in the south of the island The ash has a bimodal geochemical composition (rhy-olitic and basaltic) which is thought to reregect derivation from two separate magmachambers Studies of recent volcanic events in Iceland have shown that the mostexplosive eruptions generating the largest amounts of tephra occur in this tran-sitional alkali basalt province (Haregidason et al 2000) It is also believed that thewidespread distribution of this ash was caused by the development of co-ignimbriteash plumes during an ignimbrite-forming eruption (Lacasse et al 1995)
Layers of VA that are visible to the naked eye have been found in lake sediments inwestern Norway (Mangerud et al 1984) and the Inner Hebrides Scotland (Davies etal 2001) and in marine cores throughout the NE Atlantic (see for example Kvammeet al 1989 Lacasse et al 1995) in the northern North Sea (Long amp Morton 1987)on the Iceland plateau (Ruddiman amp McIntyre 1981 Sejrup et al 1989) and on theeast Greenland continental margin (Stein et al 1996) The distribution of the VAin North Atlantic marine sequences is characterized by an arcuate lobe extendingsouthwest from the Denmark Strait and curving eastwards to mid-latitudes in theNorth Atlantic (Lacasse et al 1995) This strongly suggests deposition from raftedice which was displaced to the southwest and south in a circulating counterclockwisegyre (Ruddiman amp Glover 1972) This may well reregect Katlarsquos close proximity tothe southern coast of Iceland with the Vedde tephra being deposited on ice thatcalved directly into the North Atlantic (Haregidason et al 2000) However depositionvia the atmosphere almost certainly took place as well as is indicated by the recentdiscoveries of rhyolitic VA in micro-tephra form in several sites in Scotland (Turneyet al 1997) southern Sweden (Wastegard et al 1998 2000a) and western Russia
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European tephrochronological framework for Termination 1 781
(Wastegard et al 2000b) A more recent discovery of a relatively high concentrationof rhyolitic VA glass shards in the northern Netherlands indicates that the ash maywell have been dispersed much further south than previously thought (S M Davies2002 unpublished work) Finally glass shards assigned to the VA have also beendiscovered in the GRIP ice core and dated to 11 980 sect 80 GRIP yr BP (Gronvold etal 1995) This discovery is extremely important for it indicates that the VA maywell provide a reliable time-parallel marker horizon between ice-core marine andterrestrial records
Two other important Icelandic ash layers the Borrobol and Saksunarvatn Tephraswere deposited near the beginning and end of the Last TerminationEarly Holoceneinterval respectively The Borrobol Tephra was discovered for the shy rst time in lakesediments in several sites in Scotland and as yet is known only in micro-tephra formIt has been dated in Scottish sites to ca 123 14C ka BP (Turney et al 1997) Whatis thought to be a contemporaneous tephra has been detected in marine sedimentson the North Icelandic shelf (Eirplusmn ksson et al 2000) This certainly has a very similargeochemical composition to those reported from Scotland but the horizon in whichit was discovered on the North Iceland plateau has been dated to 134 14C ka Theage discrepancy between the Scottish and Icelandic Borrobol Tephra layers may wellreregect the inreguence of a marine reservoir error although the possibility that severaltephras with similar geochemical composition were erupted over a period exceeding1000 yr cannot be ruled out (Larsen 2000)
The Saksunarvatn Ash appears to have been one of the largest Holocene eruptionsin Iceland It has a tholeiitic basaltic composition which is considered to indicate anorigin in the Grimsvotn or Kverfjoll complex (shy gure 3) (Mangerud et al 1986) Layersof this ash have been identishy ed in sites on the Faroe Islands (Mangerud et al 1986Dugmore amp Newton 1998 Wastegard et al 2001) the Shetland Isles (Bennet et al 1992) northern Germany (Merkt et al 1993) western Norway (micro-tephra) (Birkset al 1996) and in the GRIP (Gronvold et al 1995) and NordGRIP ice cores (S MDavies 2002 unpublished work) It has been dated to between 9060 and 8930 14C kaBP (Birks et al 1996) in Norway and to ca 10 240 sect 30 GRIP yr BP in the GRIPice core (Gronvold et al 1995) The Saksunarvatn Ash may thus provide a secondimportant widespread time-parallel marker between ice-core marine and terrestrialrecords
Other Icelandic tephras of rhyolitic amacr nity are less well known in terms of theirdistribution and geochemical variation The Hogstorpsmossen Tephra reported fromSweden (Bjorck amp Wastegard 1999) and the L3754 tephra discovered in the FaroeIslands (Dugmore amp Newton 1998) are known from single sites only and so theirpotential for tephrostratigraphy is uncertain at present Furthermore the geochem-ical spectrum of the Hogstorpsmossen Tephra is based on a small dataset with lowanalytical totals
A number of tephras of basaltic composition have originated from Iceland buttheir distributions are largely conshy ned to Iceland or to marine cores collected fromclose to the Iceland coast or in the North Atlantic These include the tephras listedas 1-THOL-1 1-THOL-2 KOL-GS-2 GS-2BAS-1 GS-2BAS-2 GS-2BAS-3 andGS-2BAS-4 in table 1 (Kvamme et al 1989 Bjorck et al 1992 Eirplusmn ksson et al 2000 Haregidason et al 2000) The shy rst two in this list are tholeiitic basaltic tephrasassociated with the VA in a complex series of tephras collectively termed NorthAtlantic Ash Zone 1 (NAAZ1) which has been detected in numerous marine cores
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782 S M Davies and others
from the North Atlantic Initially thought to represent a single eruption analysisof high-resolution sediment sequences from Lake Torfadalsvatn in northern Iceland(Bjorck et al 1992) the Hebridean Shelf near NW Scotland (Austin amp Kroon 1996)the St Kilda Basin (Hunt et al 1995) and the open North Atlantic (Bond et al 2001)has demonstrated that NAAZ1 comprises a series of distinct ashes that probablyreregect separate eruption events 1-THOL-1 is thought to originate from Veidivotn(shy gure 3) while Grimsvotn may have been the source of 1-THOL-2 (Kvamme et al 1989)
KOL-GS-2 is also of tholeiitic basaltic composition but is thought to originatefrom the Kolbeinsey Ridge system (Eirplusmn ksson et al 2000) To date this tephra hasbeen detected in one marine core only within the same record on the North Ice-landic shelf as that from which the correlative of the Borrobol Tephra was alsoreported (Eirplusmn ksson et al 2000) GS-2BAS-1 to GS-2BAS-4 are of uncertain ori-gin but are thought to have been deposited at roughly the same time as KOL-GS-2(ca 134 14C ka BP (Haregidason et al 2000))
The limited distribution of these basaltic tephras a feature that is not unique toIcelandic basaltic material may reregect two factors the relative magnitude of the vol-canic eruptions from which they were derived and the limited aerial transportationof basaltic glass which is denser than rhyolitic material However a rather surpris-ing recent discovery is that of visible basaltic VA in a site on the Isle of Skye inthe Inner Hebrides Scotland (shy gure 5) (Davies et al 2001) All other occurrencesof VA in Scotland are exclusively of rhyolitic material and in micro-tephra formonly (Turney et al 1997 Turney 1998) Clearly basaltic tephra must have beentransported subaerially as far south as Skye and the reason why it has not beendetected at other sites in Scotland is puzzling We suspect that this partly reregectsthe laboratory methods employed to separate glass shards present in low concentra-tion within a micro-tephra layer from the host sediment The technique used is adensity-separation (regotation) procedure (Turney 1998) and as basaltic shards havea specishy c density similar to quartz one of the most abundant minerals in lake sedi-ments of Late Glacial age basaltic material is dimacr cult to detect using this methodThis hypothesis is currently under investigation and alternative detection methodsare being explored including magnetic separation (Mackie et al 2002)
Several other events listed in table 1 that are of probable Icelandic origin includetephras recorded in the GRIP ice core including visible (eg the `Black Featherrsquo)tephras as well as uncertain tephras inferred from distinct Ca peaks (S Johnsen2001 personal communication) No glass shards have yet been detected in the latterbut a volcanic origin is assumed because high Ca peaks are associated with knowntephras in other Greenland ice cores (S Johnsen 2001 personal communication)These are referred to as `unknownrsquo in table 1 No geochemical analyses are availablefrom these horizons so their origin must remain speculative but a possible source isIceland in view of its proximity to the Greenland ice sheet and assumed atmosphericcirculation patterns
(b) Eifel province
There are two prominent tephra events dated to the Termination 1Early Holocenetime-span that originated from the Eifel province the Laacher See Tephra (LST)and the Ulmener Maar Tephra (UMT) Visible occurrences of the LST indicate that
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European tephrochronological framework for Termination 1 783
Vedde Ash
615 625 635 645 655depth (cm)
organic lake mudsHolocene
silty clayGS-1Younger Dryas
organic lake mudsGI-1Alleroslashd
100 microm
(a)
(b)
Figure 5 (a) Photograph of the visible VA layer discovered at Loch Ashik Isle of Skye InnerHebrides Scotland (b) Light microscope photograph showing the rich content of basaltic shards(examples are indicated by the arrows) within this layer (8024 m m size fraction)
this ash was dispersed over much of central Europe (van den Bogaard amp Schmincke1985 Friedrich et al 1999 Litt amp Stebich 1999) The LST is dated by radiocarbonto ca 110 14C ka BP (van den Bogaard amp Schmincke 1985) and to 11 063sect12 14C BP(Friedrich et al 1999) by varve chronology to 1288 varve ka BP (Brauer et al 1999Litt et al 2001) and by ArAr dating to 129 ka cal BP (van den Bogaard 1995) Ithas a phonolitic composition and is thought to have originated from a plinian andphreatomagmatic eruption with the distal ash being carried in three distinct plumesone to the northeast towards Poland one to the west and the third to the southcovering the Jura Mountains and north Italy (van den Bogaard amp Schmincke 1985Juvigne et al 1995 Bossuet et al 1997) This pattern is thought to reregect altitu-dinal variations in the predominant wind direction Sedimentary sequences near thevolcanic source indicate that the LST consists of three main layers which represent
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784 S M Davies and others
dinoterent eruption phases These are grouped together as the Laacher See TephraFormation but the three individual units can be traced within and between a seriesof depositional fans The geochemical data obtained from these three LST layersshow signishy cant variations as reregected in the ternary plots (shy gure 4)
The Early Holocene Ulmener Maar Tephra (UMT) is of rhyolitic composition andappears to be restricted to sites in Germany though this conclusion is also based onrecords of visible tephras only It is dated to ca 956 14C ka BP and to 110 varve ka(Zolitschka et al 1995 Litt et al 2001)
(c) Massif Central province
The Massif Central tephras are mainly of basaltic trachyandesitic compositionwhich is distinct from the other ash provinces (shy gures 3 and 4) and their known dis-tributions are mostly conshy ned to the Massif Central region The ages of the MassifCentral tephras are based on radiocarbon dates obtained from mire and lake sedi-ments which `bracketrsquo the tephras The La Nugsup3ere Tephra with an age of 114 14C kaBP is the oldest Massif Central tephra identishy ed so far within the time-span of inter-est (Etlicher et al 1987 Juvigne et al 1996) The two Godivelle Tephras (5 and 4)are close in age but extensive radiocarbon dating suggests distinct ages of 107and 103 14C ka BP respectively (Juvigne et al 1996) The age of the Puy de DomeTephra is less certain as the estimate is based on only one radiocarbon date froma site in the southern Chaplusmn ne des Puys (table 1) This tephra is thought to havea trachyte composition (Juvigne 1993) although no major element concentrationshave yet been published
The ChopineKilianVasset tephras are thought to be derived from three separateEarly Holocene eruptions although the stratigraphic succession is not known atpresent These trachytic tephras have been radiocarbon dated to ca 854sect150 14C kaBP but are thought to have erupted separately within ca 260 yr (Juvigne et al 1996) This series of tephras is considerably more widespread than the others fromthe region having been identishy ed as far east as the Jura Mountains (Martini amp Duret1965 Martini 1970) Some other ash falls that originated from the Chaplusmn ne des Puysappear to be of local importance only (Vernet et al 1998 Vernet amp Raynal 2001)Geochemical data are currently available for only three of the Massif Central tephrasand so far as is known no attempt has yet been made to identify these tephras inmicro-tephra form
(d ) Italian provinces
The Italian tephras from this period can be assigned to three main volcanic com-plexes the Campanian volcanic shy elds around Naples Etna on Sicily and the AeolianIslands The Campanian complex which includes the Phlegrean Fields Vesuviusand Ischia is mainly trachytic in composition with a geochemical spectrum that isquite distinct from those of the Etna complex and of the Aeolian Islands (shy gure 3)Tephras originating from one or more of these three complexes have been detectedin marine cores from the Tyrrhenian and Adriatic seas as well as other parts of theMediterranean Sea (Keller et al 1978 Paterne et al 1986 1988 1990 Langone etal 1996) and in lake sequences in southern Italy such as Lago Grande di Monticchio(Newton amp Dugmore 1993 Narcisi 1996 Allen et al 1999) and central Italy such asLago Albano near Rome (Calanchi et al 1996) Some work has also been conducted
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European tephrochronological framework for Termination 1 785
in or close to the volcanic source areas in an attempt to establish the full sequenceof volcanic eruptions during the Late Quaternary (see for example Di Vito et al 1999) There are nine Italian tephras reported from marine and lake sequences thatdate from the period between 185 and 80 14C ka BP In all instances the recordsare of visible layers of tephra The ages of some of these are poorly established atpresent with conregicting data obtained from dinoterent sites The ages suggested intable 1 are those favoured in the most recent publications but these may requirere-assessment in the light of future research
The two oldest known tephras in the time-period of interest are the L9 and Green-ish Tephras both recorded as separate features within the annually laminated Lagodi Monticchio maar sequence The lowest of the two L9 is considered to be the cor-relative of the `basalrsquo plinian eruption of Vesuvius (Narcisi 1996) Age estimates ofa palaeosol that underlies the Vesuvius tephra sequence are ca 1617 14C ka BP forthis event (Delibrias et al 1979) L9 has a trachytic composition very similar to theGreenish Tephra (table 1) However L9 which is also a product of Vesuvius is foundstratigraphically below the Greenish Tephra in the Lago di Monticchio core TheGreenish Tephra is dated in the Monticchio sequence to 17 560 varve yr BP (Allenet al 1999) and has a calibrated radiocarbon age estimate of 17 830 sect 300 cal BP(Andronico et al 1995) Both tephras have a dominantly eastwards dispersal basedon the occurrences of visible layers (Santacroce 1987 Narcisi 1996) Both tephrasalso have a trachytic composition and as can be seen from table 1 the reportedgeochemical spectra are very close indeed with the standard deviations overlappingfor almost every major element This could present problems for tephrostratigra-phy where only one of the tephras is evident in a sediment sequence in particularbecause they are so close in age This is a good example of where an analysis oftrace and rare earth elements might be required to make a clear distinction betweentephras with very similar major oxide concentrations
The Y-1 Tephra also termed the Biancavilla Montalto Ignimbrite (Vezzoli 1991)is a product of Etna and has been identishy ed as a visible benmoritic tephra horizonthroughout the central Mediterranean (Paterne et al 1988) including central Italyand the Adriatic Sea (Vezzoli 1991 Narcisi 1993 Calanchi et al 1996) It has anestimated age of ca 140 14C ka BP The Unita dei Tefra Superiori tephra which hasbeen detected as far east as Lago di Monticchio in south-central Italy (Narcisi 1996)is also dated to ca 140 14C ka BP (Alessio et al 1976) but it is thought that thesource of this tephra lies in the Phlegrean Fields No geochemical data are availablefrom the presumed source region|the data reported in table 1 were obtained fromthe Lago di Monticchio record (Narcisi 1996)
The NYT which is equivalent to the C-2 tephra reported from various marinesequences has also been traced throughout central Italy and the Adriatic Sea (Pat-erne et al 1988 Calanchi et al 1996 Di Vito et al 1999) (shy gure 2) In the centralApennines region it formed the parent material for a soil that started to developat the beginning of the Holocene period (Frezzotti amp Narcisi 1996) Also originatingfrom the Campi Flegrei caldera it is dated to ca 120 14C ka BP (Di Vito et al 1999) Published geochemical data based on EDS indicate three dinoterent geochemicalpopulations varying from latite to phonotrachyte in composition (Orsi et al 1992Paterne et al 1988) (table 1) We report in x 4 of this paper on new data obtainedfrom the NYT by WDS and it is the mean of these new data that is included intable 1 Comparisons with the previously published EDS data are provided (table 1)
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786 S M Davies and others
The new data indicate clearly that the NYT originated from the Campanian volcaniccentre
In the interval between the dispersal of the NYT (ca 120 14C ka BP) and 95 14Cka BP there appear to have been as many as 34 eruptions in the Campi Flegrei caldera(Di Vito et al 1999) Of these only one appears to have been detected widely in theregion the Pomici Principali (also termed the Agnano Formation or C-1 tephra inmarine records (Paterne et al 1988) This was the product of the highest magnitudeeruption from this epoch and is dated to between 976 sect 300 and 1032 sect 50 14C kaBP (Delibrias et al 1979 Di Vito et al 1999) or to 122 varve ka BP based on theMonticchio varve chronology (Allen et al 1999) It is trachytic in composition andappears to have had a mainly eastwards dispersal
The Mercato Tephra dated to ca 80 14C ka BP and originally analysed usingEDS has a phonolitic composition and is believed to have been generated by Vesu-vius (Paterne et al 1988) New WDS data obtained from reference samples col-lected from an exposure to the west of Naples support these conclusions (table 1 andAppendix A) The silica content of the WDS analyses are ca 3 lower than thoseobtained using EDS (table 1) which may reregect the fact that the EDS data werenormalized
The only tephra listed in table 1 that is thought to have originated from the AeolianIslands is the Pollara pumice also referred to as the E2 tephra in marine sequences(Paterne et al 1986 1988) The limited geochemical data available so far suggest itto be the only Italian tephra listed in table 1 that is rhyolitic in composition Littlemore is known about this ash which has not been recorded extensively except thatits age is estimated to be ca 130 14C ka BP (Keller 1980)
5 Extending the known distributions of European tephras
Figure 2 summarizes schematically the known distributions of three of the tephrasreferred to in the preceding section the VA the LST and the NYT Following theintroduction of a laboratory method that enables the detection of micro-tephra parti-cles in mineral-rich sediment the VA has been traced to sites that are located muchfarther south (into The Netherlands) and east (as far as St Petersburg) than thedistribution limits based on occurrences of visible layers of the ash As a result con-tinental sequences over a much larger area in northern Europe can now be correlateddirectly with marine and ice-core records using the VA as a time-parallel marker
This suggests therefore that other prominent ash layers such as the LST andNYT should also be detectable over larger tracts of Europe than is presently thecase if suitable sites are examined for the presence of micro-tephra horizons To testthis assertion we examined lake sediment deposits of Last Termination age froma site in the northern Apennines in order to establish whether the NYT could bedetected in micro-tephra form The site selected Prato Spilla `Crsquo lies well to thenorth of the localities in central and southern Italy and in the Adriatic Sea fromwhich visible records of the NYT have been reported Prato Spilla `Crsquo lies at an alti-tude of ca 1350 m in the Appennino Parmense ca 60 km south of Parma and 15 kmeast of Pontremoli The site contains a continuous sediment sequence spanning theLast Termination and most of the Holocene Detailed pollen and coleopteran strati-graphical records which have been radiocarbon dated have been published for thissite (Lowe 1992 Ponel amp Lowe 1992 Lowe amp Watson 1993)
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European tephrochronological framework for Termination 1 787
Figure 6 Light microscope photograph of an NYT glass shard from Prato Spilla Crsquosequence assigned on geochemical grounds to the NYT
The methods adopted for sub-sampling of the Prato Spilla `Crsquo sequence for thequantishy cation of glass shard concentrations and for subsequent electron microprobeanalysis of selected glass shards followed those described elsewhere (Turney 1998)In summary contiguous samples of 1 cm stratigraphic interval were extracted fromthe sequence to establish presenceabsence of glass shards Each of the 1 cm3 blocksin which tephra particles was detected was then examined with more care andshard concentrations were quantishy ed for each sub-sample Micro-tephra particleswere detected in shy ve samples (shy gure 6) but were predominantly clustered around500 cm in the part of the sequence assigned on pollen-stratigraphic grounds to theLate Glacial Interstadial or the `Allerfrac12drsquo|indeed the part of the succession in whichthe NYT would be expected to occur Peak concentrations of micro-tephra particlesreach 225 shards cmiexcl3 and are conshy ned to a single 1 cm thick sample in the sequencewhich probably represents the time of maximum deposition of the ash
Electron microprobe measurements based on WDS were obtained from the surfacesof 21 separate glass shards extracted from the sample with peak shard concentrations(Appendix A) Since only EDS measurements were available for the NYT prior to thepresent study we also obtained WDS measurements from 17 shards extracted fromthe visible layer of NYT that is exposed on Procida Island which lies in the type-locality for the NYT close to the city of Naples (Appendix A) The results providenot only a more comprehensive geochemical dataset for the NYT than was previ-ously available but also a consistent basis for comparison with the Prato Spilla `Crsquodataset All of the WDS data reported here (Appendix A) were measured at the samelaboratory (Tephrochronology Analytical Unit University of Edinburgh) using thesame sample pretreatment and preparation protocol The WDS results for the NYTdinoter to a minor degree from the EDS results (table 1 and Appendix A) especiallywith respect to the amounts of silica aluminium and calcium measured The EDS
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788 S M Davies and others
4 8FeO ()
TiO
2 (
) Neapolitan Yellow Tuff(Procida)Neapolitan Yellow Tuff(Prato Spilla lsquoCrsquo)
0
1
2
3
40 50 60 70
MgO
(
)
SiO2 ()
K2O
(
)
40 50 60 70
0
04
08
4
8
12
SiO2 ()
(a)(b)
(c)
Figure 7 Bi-plots of SiO2 K2 O SiO2 MgO and FeOTiO2 for the WDS analyses obtainedfrom glass shards of the NYT from Procida (Naples) and Prato Spilla Crsquo Means and standarddeviations are shown
results show a higher degree of statistical scatter than the WDS measurements whichmay reregect the fact that the data were normalized combined with the inreguence ofvariation in water content between shards
There is a very close correspondence between the WDS data for the Prato Spilla `Crsquomicro-tephra shards and those obtained from the type-material near Naples (shy g-ure 7) The geochemical data strongly suggest therefore that the NYT is representedat the Prato Spilla `Crsquo site by a discrete layer of micro-tephra particles This conclu-sion is compatible with the pollen-stratigraphic data from the site and accords withage estimates for the NYT (ca 120 14C ka BP) obtained from other sites (Paterneet al 1990)
These results encourage us to believe that many if not all of the tephras listedin table 1 will be detectable over much larger tracts of Europe than is presently thecase if appropriate research is undertaken to detect layers of micro-tephra particlesin selected sites The authors are presently engaged in a major continent-wide pro-gramme of research in collaboration with a number of European research groupsdesigned to test this hypothesis The focus in this research is on those parts of Europewhere we expect to shy nd overlapping `apronsrsquo of tephra deposition originating fromthe Italian Eifel Massif Central and Icelandic provinces For example a number ofsites in parts of southern France northern Italy and perhaps western Switzerlandmay have received inreguxes of micro-tephra originating from the Italian and Eifelprovinces and perhaps also from the Massif Central Sites in parts of Germany Den-mark and southern Sweden for example may in turn have received tephra depositsfrom both of the Icelandic and Eifel provinces If this proves to be the case then thestage will be set for the construction of a tephrostratigraphical framework for Europewhich will enable Last Termination sequences to be correlated on a continent-widebasis using micro- and visible tephra layers as time-parallel stratigraphic markersFurthermore there is also the possibility that other tephras remain to be discovered
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 789
those which either because of the magnitude or nature of some volcanic eruptionswere distributed over parts of Europe in micro-tephra form only
6 European tephrostratigraphy and the chronology of eventsduring the Last Termination and Early Holocene
One of the crucial issues in Late Quaternary palaeoenvironmental research thatremains to be resolved is the degree to which climatic events inferred from oceanicterrestrial and ice-core records were synchronous during the Last Termination andEarly Holocene If the ice-core records provide realistic estimates of the rates anddurations of climatic events during this period then comparisons between individ-ual records have to be enotected with at least a decadal precision The problem thispresents and the role that tephrostratigraphy can play in resolving some of thedimacr culties involved are put into perspective in shy gure 8
Figure 8 shows some of the data used to calibrate radiocarbon dates (the LakeSuigetsu and Cariaco Basin datasets) plotted against the GRIP ss08c ice-core recordof macr 18O variations The latter has been selected by the INTIMATE group as an arbi-trary and temporary standard for this period and used to deshy ne an event stratig-raphy scheme (shy gure 1) for the Last Termination (see Bjorck et al 1998 Walker etal 2001) As has been alluded to in earlier sections of this paper the uncertaintiesassociated with all of the dating methods currently employed preclude precise com-parisons of ice-core marine and terrestrial records Oceanic and terrestrial recordsmostly rely upon radiocarbon dating locally supplemented in a few cases by varvechronology Imprecisions in radiocarbon dates can arise through site-specishy c fac-tors (eg hard-water or mineral carbon errors in freshwater sequences and reservoirerrors in marine sequences) sample selection laboratory measurements of 14C activ-ity and other factors (Lowe amp Walker 2000) Further imprecision may be introducedby the calibration of radiocarbon dates since the uncertainties in the dataset usedto calibrate pre-Holocene radiocarbon dates INTCAL98 are far higher than forthe Holocene which is based on dendro-calibration (Stuiver et al 1998) There arealso uncertainties anotecting varve chronologies while the ss08c ice-core chronologyfor the Last Termination dinoters signishy cantly from the GISP2 record and indeedfrom other models of the GRIP record (Lowe et al 2001) Published comparisonsbetween ice-core marine and terrestrial records for the Last Termination seldom takeinto account the true magnitude of the dating uncertainties involved and frequentlyemploy circular reasoning
Figure 8 shows the positions on the radiocarbon time-scale of 20 of the tephrasdiscussed earlier in this paper these being the ones for which reasonably conshy dentradiocarbon age estimates can be made (though these will be subject to revised esti-mates in the future) A high number of these occur in the period 14080 14C kaBP but we conshy dently anticipate the discovery in the future of additional tephras(perhaps in micro-tephra form only) which will date to the period 185140 14C kaBP Tephras detected in the GRIP ice core over the same time-interval are plottedon the calendar time-scale in shy gure 8 By providing key `time-linesrsquo between recordstephrostratigraphy can help to resolve some of the dating uncertainties referredto earlier by for example enabling direct comparisons of discrepant age estimatesobtained using dinoterent methods (cf Litt et al 2001) It can also provide estimatesof the magnitudes of the reservoir errors that anotected various marine sectors at dif-
Phil Trans R Soc Lond A (2002)
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790 S M Davies and others
-44
-40
-36
-32
cale
ndar
yea
rs B
P
8000
9000
10 0
00
11 0
00
12 0
00
13 0
00
14 0
00
15 0
00
16 0
00
17 0
00
18 0
00
14C age (BP)
VA
SA
Un
Un
Un
Un
Un
BF
Hol
ocen
eG
S-1
GI-
1aG
I-1b
GI-
1cG
I-1d
GI-
1eG
S-2
aG
S-2
bG
S-
2c
Bor
robo
l
La
Nug
egravere
Laa
cher
See
God
ivel
le 5
amp I
-TH
OL
-2
Puy
de D
ocircme
I-T
HO
L-1
Saks
unar
vatn
Houmlg
stor
psm
osse
nU
lmen
er M
aar
amp L
3574
radiocarbon dated European tephra horizons
Cho
pine
Kili
an V
asse
tM
erca
to
God
ivel
le 4
Pom
ici P
rinc
ipal
i amp V
edde
Polla
ra p
umic
eK
OL
-GS-
2 amp
GS
-2B
AS-
12
3
GS
-2B
AS-
4 U
nita
dei
Tef
raSu
peri
ori amp
laye
r Y
-1
Gre
enis
h
L9
20 0
0018
000
16 0
0014
000
12 0
0010
000
-44
-40
-36
-32
800
600
400
200 0
GISP2 volcanicsulphate conc (ppb)
1000
Nea
polit
an Y
ello
w T
uff
GISP2 18O (permil) dGRIP 18O (permil) d
Figure 8 For description see opposite
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 791
ferent times through a comparison of radiocarbon dates obtained from marine andterrestrial horizons in which the same tephra has been detected (see for exampleAustin et al 1995 Bondevik et al 2001 Haregidason et al 2000) Tephrostratigraphymay provide an independent test of suggestions that some of the climatic changesduring the Last Termination were time-transgressive as illustrated for some appar-ently contrasting climatic trends in Iceland Britain and NW Russia (Lowe 2001) Ofparticular importance as far as establishing `leadsrsquo and `lagsrsquo in climatic changes isconcerned are the tephra records from the Greenland ice cores The discovery of theVedde and Saksunarvatn ashes in the GRIP record (Gronvold et al 1995) alreadyprovides a basis for making direct comparisons between marine terrestrial and ice-core records It is a matter of some urgency that the incidence of tephra depositsin the Greenland ice cores be more fully explored in the hope that this will lead tothe recognition of additional time-parallel links between the ice-core records on theone hand and oceanic and terrestrial records on the other An investigation of thenew NordGRIP record for this purpose is currently in progress (S M Davies 2002unpublished data)
Finally a fuller and more reshy ned tephrostratigraphical scheme for Europe will alsohave other applications It will provide an important database for those investigatingthe timing and frequency of volcanic eruptions in Europe during the past 20 000 yror so as well as of the geochemical evolution of the dinoterent volcanic centres overthat period A fuller record of the distribution of micro-tephras may also provideinformation on atmospheric circulation patterns during the dispersal and depositionperiods as well as on the nature and altitude of the eruption columns which mayin turn provide inferences about magma viscosity
This paper is a contribution to the INTIMATE project of the INQUA Palaeoclimate Com-mission and the work is supported by a Leverhulme Trust Research project (grant allocationnumber F07537C) entitled Testing hypotheses of rapid climate change using tephrochronol-ogyrsquo SMDrsquo s contribution was completed during possession of a NERC PhD studentship(GT 0499ES162) We are extremely grateful to Dr Peter G Hill for his assistance withthe EPMA analyses at the Tephrochronology Analytical Unit University of Edinburgh We alsothank Dr G Mastrolorenzo (Vesuvius Observatory) and Miss G Swindle for assistance duringthe macreld investigations in Naples Thanks are also expressed to two anonymous reviewers forcomments on an earlier draft
Appendix A
Table 2 shows the major oxide concentrations of NYT glass shards from Procidaand Prato Spilla `Crsquo and of the Mercato Tephra from the Naples area (see x 4 forsite context) All oxides are shown as weight and total iron is expressed as FeO
Figure 8 Radiocarbon calibration curve for Termination 1 and the Early Holocene compared with theGRIP macr 18 O event stratigraphy the GRIP ss08c and GISP2 macr 18 O records (wwwngdcnoaagov) andknown tephra horizons from this period The shaded areas represent the cooler climatic episodes andare labelled with the Greenland stratotype terminology (Bjorck et al 1998) Where radiocarbon agesare reported in table 1 as a range the mean is given here Abbreviations for GRIP horizons are asfollows Un unknown (approximate positions are given (S Johnsen 2001 personal communication))SA Saksunarvatn Ash VA Vedde Ash BF Black Feather Sulphate concentrations from the GISP2record are also shown (Zielinski et al 1996) Open circles denote radiocarbon calibration data fromLake Suigetsu (Kitagawa amp van der Plicht 2000) Filled circles denote radiocarbon calibration data fromCariaco Basin assuming a marine reservoir age of 420 14 C yr (Hughen et al 1998)
Phil Trans R Soc Lond A (2002)
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792 S M Davies and others
Tab
le2
Majo
roxi
de
con
cen
trati
on
sof
NY
Tgl
ass
shard
sfr
om
Pro
cida
an
dP
rato
Spil
laC
rsquoan
dof
the
Mer
cato
Tep
hra
from
the
Naple
sare
a(s
eex4
for
site
con
text
)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
roci
da)
1584
204
0177
634
201
106
828
635
197
5969
1W
DS
2598
603
9178
027
101
204
924
244
583
4965
8W
DS
3586
604
5173
631
100
805
924
342
183
0951
9W
DS
4583
903
9177
933
000
906
924
540
486
9958
3W
DS
5605
106
8179
126
901
204
923
243
086
1976
4W
DS
6591
704
5177
332
801
006
425
740
887
8968
0W
DS
7581
804
1178
031
501
107
125
640
086
9956
1W
DS
8589
504
2179
533
701
506
926
740
987
5970
4W
DS
9592
003
9178
135
101
007
026
443
585
7972
7W
DS
10
591
404
2174
631
601
105
723
442
482
6957
0W
DS
11
593
403
6177
131
301
506
726
439
188
5967
6W
DS
12
588
103
8176
128
100
505
525
141
583
4952
1W
DS
13
577
003
8176
533
500
807
228
140
384
8952
0W
DS
14
586
004
7179
735
300
706
827
842
984
6968
5W
DS
15
588
104
2180
629
400
505
924
937
993
0964
5W
DS
16
579
603
9178
536
501
308
228
836
087
1959
9W
DS
17
580
103
9177
631
500
907
327
039
488
9956
6W
DS
mea
n588
104
2177
631
901
006
525
940
686
9962
8
sd
(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(07
8)
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 793
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
rato
Spil
laC
rsquo)
1552
105
4177
247
401
914
38
735
578
9951
1W
DS
2557
305
7179
845
701
512
640
136
581
5960
6W
DS
3595
004
4173
724
302
003
117
652
877
8950
7W
DS
4575
704
2179
433
001
406
627
043
083
6953
7W
DS
5599
904
0178
826
401
304
421
841
688
4966
5W
DS
6591
103
8177
826
601
105
022
443
888
8960
2W
DS
7565
304
5180
939
501
410
532
535
791
8962
1W
DS
8597
606
9180
826
501
604
821
546
684
6970
7W
DS
9571
805
6179
939
801
109
932
240
883
6964
7W
DS
10
588
603
7176
527
601
104
721
042
487
7953
3W
DS
11
559
404
9180
544
501
812
339
435
878
6957
2W
DS
12
594
704
0181
328
301
705
522
144
785
6967
9W
DS
13
611
103
7187
016
900
802
419
938
195
9975
8W
DS
14
599
204
4181
128
601
404
620
844
986
6971
6W
DS
15
601
204
4177
328
302
004
722
446
385
5972
1W
DS
16
595
104
5176
428
801
504
722
744
884
3962
8W
DS
17
603
704
1177
825
101
503
520
348
181
2965
3W
DS
18
558
704
5179
647
401
813
139
836
879
0960
7W
DS
19
589
602
8178
830
901
606
622
436
091
8960
5W
DS
20
553
606
3178
647
401
913
840
136
978
0956
6W
DS
21
579
004
0175
739
000
708
328
338
286
7959
9W
DS
mea
n582
804
6179
033
401
507
427
341
484
8962
1
sd
(1
87)
(01
0)
(02
7)
(09
2)
(00
4)
(03
9)
(08
0)
(04
9)
(05
0)
(07
0)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
794 S M Davies and others
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)
1575
202
7194
219
701
101
016
374
766
9951
8W
DS
2575
802
9194
523
902
201
520
273
564
5959
0W
DS
3574
301
4205
219
101
100
416
481
266
1965
2W
DS
4575
500
7206
018
002
000
415
181
669
3968
6W
DS
5580
000
9208
018
601
300
515
883
367
1975
5W
DS
6571
001
0206
016
101
600
515
078
967
1957
2W
DS
7577
501
1201
117
101
500
620
675
655
4950
5W
DS
8573
700
9212
717
101
900
815
187
564
2973
9W
DS
9580
301
3208
715
801
400
824
81
754
1968
1W
DS
10
574
400
6211
18
402
00
516
480
567
8971
6W
DS
11
577
200
7214
212
501
200
829
879
247
962
6W
DS
12
572
200
9211
217
301
501
15
980
465
9966
3W
DS
13
571
800
7210
417
402
201
16
184
467
2971
2W
DS
14
567
300
9208
916
901
400
917
383
262
5959
3W
DS
15
568
600
8205
918
202
101
414
682
666
6960
8W
DS
16
572
501
1211
318
202
01
215
884
364
5970
9W
DS
17
572
901
2212
916
502
101
215
883
667
2973
4W
DS
18
573
01
4211
716
301
801
416
83
365
5970
4W
DS
19
569
201
1207
418
602
101
414
982
964
961
6W
DS
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
3)
(04
2)
(01
3)
(00
1)
(00
2)
(01
)(0
39)
(01
1)
(02
5)
Phil Trans R Soc Lond A (2002)
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796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
References
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European tephrochronological framework for Termination 1 797
Bondevik S Mangerud J amp Gulliksen S 2001 The marine 1 4 C age of the Vedde Ash Bedalong the west coast of Norway J Quat Sci 16 37
Bossuet G Richard H Magny M amp Rossy M 1997 A new occurrence of Laacher See Tephrain the central Jura (France) The mire of Le Lautrey C R Acad Sci Paris Sparaer IIa 3254348
Brauer A Endres C Gunter C Litt T Stebich M amp Negendank J F W 1999 Highresolution sediment and vegetation responses to Younger Dryas climate change in varved lakesediments from Meerfelder Maar Germany Quat Sci Rev 18 321329
Brooks S J Mayle F E amp Lowe J J 1997 Chironomid based Lateglacial climatic recon-struction for southeast Scotland J Quat Sci 12 161167
Calanchi N Dinelli E Gasparatto G amp Lucchini F 1996 Etnean tephra layer in Albanolake and Adriatic Sea cores new macrndings of Y-1 layer in the central Mediterranean area ActaVulcan 8 713
Coope G R Lemdahl G Lowe J J amp Walkling A 1998 Temperature gradients in northernEurope during the last glacialHolocene transition (149 ka BP) interpreted from coleopternassemblages J Quat Sci 13 419433
Dansgaard W (and 10 others) 1993 Evidence for general instability of past climate from a250 kyr ice-core record Nature 363 218220
Davies S M Turney C S M amp Lowe J J 2001 Identimacrcation and signimacrcance of a visiblebasalt-rich Vedde Ash layer in a Late-glacial sequence on the Isle of Skye Inner HebridesScotland J Quat Sci 16 99104
Delibrias G Di Paola G M Rosi M amp Santacroce R 1979 La storia eruttiva del complessovulcanico Somma Vesuvio ricostruita dalle successini piroclastiche del Monte Somma RendSoc It Mineral Petrolog 35 411438
Di Vito M A Isaia R Orsi G Southon J de Vita S Drsquo Antonio M Pappalardo L ampPiochi M 1999 Volcanism and deformation since 12 000 years at the Campi Flegrei caldera(Italy) J Volcanol Geophys Res 91 221246
Dugmore A J amp Newton A J 1992 Thin tephra layers in peat revealed by X-radiography JArchaeol Sci 19 163170
Dugmore A J amp Newton A J 1998 Holocene tephra layers in the Faroe Islands Frodskaparrit46 191204
Eastwood A J Pearce N J G Westgate J A Perkins W T Lamb H F amp RobertsN 1999 Geochemistry of Santorini tephra in lake sediments from southwest Turkey GlobalPlanet Change 21 1729
Eirpara sup3 ksson J Knudsen K L Hadeg idason H amp Henriksen P 2000 Lateglacial and Holocenepalaeoceanography of the North Icelandic shelf J Quat Sci 15 2342
Etlicher B Janssen C R Juvignparae E amp Van Leeuwen J F N 1987 Le Haut Forez (MassifCentral France) aprmicroes le Plparaeniglaciaire Wurmien environnement et tparaephra du volcan de LaNugmicroere Bull Ass Fr Etud Quat 4 229239
Frezzotti M amp Narcisi B 1996 Late Quaternary Tephra derived paleosols in central Italyrsquo scarbonate Apennine range stratigraphical and paleoclimatological implications Quat Int3436 147153
Friedrich M Kromer B Spurk M Hofmann J amp Kaiser K F 1999 Paleoenvironment andradiocarbon calibration as derived from LateglacialEarly Holocene tree-ring chronologiesQuat Int 61 2739
Froggatt P C 1992 Standardisation of the chemical analysis of tephra deposits Report of theICCT working group Quat Int 1314 9396
Gronvold K Oskarsson N Johnsen S J Clausen H B Hammer C U Bond G amp Bard E1995 Ash layers from Iceland in the GRIP ice core correlated with oceanic and land sedimentsEarth Planet Sci Lett 135 149155
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
798 S M Davies and others
Hadeg idason H Eirpara sup3 ksson J amp van Kreveld S 2000 The tephrochronology of Iceland and theNorth Atlantic region during the Middle and Late Quaternary a review J Quat Sci 15322
Hoek W Z amp Bohncke S J P 2001 Oxygen isotope wiggle matching as a tool for synchronisingice-core and terrestrial records over Termination 1 Quat Sci Rev 20 12511264
Hughen K A Overpeck J T Peterson L C amp Trumbore S 1996 Rapid climate changes inthe tropical Atlantic region during the last deglaciation Nature 380 5153
Hughen K A Overpeck J T amp Lehman J 1998 A new 14 C calibration data set for the LastDeglaciation Radiocarbon 39 483494
Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
Hunt J B amp Hill P G 1996 An inter-laboratory comparison of the electron probe microanalysisof glass geochemistry Quat Int 3436 229241
Hunt J B amp Hill P G 2001 Tephrological implications of beam sizesample size ereg ects inelectron microprobe analysis of glass shards J Quat Sci 16 105117
Hunt J B Fannin N G T Hill P G amp Peacock J D 1995 The tephrochronology andradiocarbon dating of North Atlantic Late Quaternary sediments an example from the StKilda Basin In The tectonics sedimentation and palaeoceanography of the North Atlanticregion (ed R A Scrutton M S Stoker G B Shimmield amp A W Tudhope) vol 90pp 227248 Geological Society of London Special Publication
Hunt J B Clift P D Lacasse C Vallier T L amp Werner R 1998 Standardisation ofelectron probe microanalysis of glass geochemistry In Proc ODP Scientimacrc Results vol 152pp 8591 College Station TX Ocean Drilling Program
Jakobsson S P 1979 Outline of the petrology of Iceland Jokull 29 5773
Juvignparae E 1987 Deux retombparaees volcaniques tardiglaciaires dans le Cparaezallier (Massif CentralFrance) Bull Ass Fr Etud Quat 13 37
Juvignparae E 1993 Contribution microa la tparaephrostratigraphie du Quaternaire et son application microa lagparaeomorphologie Mparaem Serv Explicat Cartes Gparaeol Min Belg 36 166
Juvignparae E amp Gewelt M 1987 La Narse drsquo Ampoix comme tparaephrostratotype dans la Chasup3 ne desPuys mparaeridionale (France) Bull Ass Fr Etud Quat 29 3749
Juvignparae E Kozarski S amp Nowaczyk B 1995 The occurrence of Laacher See Tephra in Pomera-nia NW Poland Boreas 24 225231
Juvignparae E Bastin B Delibrias G Evin J Gewelt M Gilot E amp Streel M 1996 Acomprehensive pollen and tephra based chronostratigraphic model for the Lateglacial andHolocene period in the French Massif Central Quat Int 3436 113120
Keller J 1980 The island of Vulcano Rend Soc It Mineral Petrolog 36 369414
Keller J Ryan W B F Ninkovich D amp Altherr R 1978 Explosive volcanic activity in theMediterranean over the past 200 000 years as recorded in deep sea sediments Geol Soc AmBull 89 591604
Kitagawa H amp van der Plicht J 2000 Atmospheric radiocarbon calibration beyond 11 900 calBP from Lake Suigetsu laminated sediments Radiocarbon 42 369380
Kvamme T Mangerud J Furnes H amp Ruddiman W F 1989 Geochemistry of Pleistoceneash zones in cores from the North Atlantic Norsk Geol Tids 69 251272
Lacasse C Sigurdsson H Johannesson H Paterne M amp Carey S 1995 Source of Ash zone 1in the North Atlantic Bull Volcanol 57 1832
Langone L Asioli A Corregiari A amp Trincardi F 1996 Age depth modelling through theLate-Quaternary deposits of the central Adriatic Basin In Palaeoenvironmental analysis ofItalian crater lake and Adriatic sediments (ed F Oldmacreld amp P Guilizzoni) vol 55 pp 177196 Memorie dellrsquo Instituto Italiano di Idrobiologia
Larsen G 2000 Holocene volcanism in Iceland and tephrochronology as a tool in volcanologyIn Iceland 2000 modern processes and past environments Keele University UK
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 799
Litt T amp Stebich M 1999 Bio- and chronostratigraphy of the Lateglacial in the Eifel regionGermany Quat Int 61 516
Litt T Brauer A Goslar T Merkt J Balaga K Muller H Ralska-Jasiewiczowa MStebich M amp Negendank J F W 2001 Correlation and synchronisation of Lateglacialcontinental sequences in northern Central Europe based on annually laminated lacustrinesediments Quat Sci Rev 20 12331249
Long D amp Morton A C 1987 An ash fall within the Loch Lomond stadial J Quat Sci 297101
Lotter A F Eicher U Siegenthaler U amp Birks H J B 1992 Lateglacial climatic oscillationsas recorded in Swiss lake sediments J Quat Sci 7 187204
Lowe J J 1992 Lateglacial and Early Holocene lake sediments from the Northern ApenninesItaly|pollen stratigraphy and radiocarbon dating Boreas 21 193208
Lowe J J 2001 Abrupt climatic changes in Europe during the last glacialinterglacial tran-sition the potential for testing hypotheses on the synchroneity of climatic events usingtephrochronology Global Planet Change 603 7384
Lowe J J amp Turney C S M 1997 Vedde Ash layer discovered in a small lake basin on theScottish mainland J Geol Soc Lond 154 605612
Lowe J J amp Walker M J C 2000 Radiocarbon dating the last glacialinterglacial transition(ca 14914 C ka BP) in terrestrial and marine records the need for new quality assuranceprotocols Radiocarbon 42 5368
Lowe J J amp Watson C 1993 Lateglacial and Early Holocene pollen stratigraphy of the northernApennines Italy Quat Sci Rev 12 727738
Lowe J J Birks H H Brooks S J Coope G R Harkness D D Mayle F E SheldrickC Turney C S M amp Walker M J C 1999 The chronology of palaeoenvironmental changesduring the Last GlacialHolocene transition towards an event stratigraphy for the BritishIsles J Geol Soc Lond 156 397410
Lowe J J Hoek W Z amp INTIMATE group 2001 Inter-regional correlation of palaeoclimaticrecords for the Last GlacialInterglacial transition a protocol for improved precision recom-mended by the INTIMATE project group Quat Sci Rev 20 11751187
Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
Mangerud J Lie S E Furnes H Kristiansen I L amp Liquest mo L 1984 A Younger Dryas ashbed in western Norway and its possible correlation with tephra beds from the Norwegian Seaand North Atlantic Quat Res 21 85104
Mangerud J Furnes H amp Jparaohansen J 1986 A 9000 year-old ash bed on the Faroe IslandsQuat Res 26 262265
Martini J 1970 Recherche de retombparaees volcaniques dans le sud-est de la France et la Suisseoccidentale Arch Sci 23 641674
Martini J amp Duret J J 1965 Note preliminaire sur la presence drsquo un niveau de cendres vol-caniques dans des sparaediments post-glaciaires des environs de Genmicroeve Arch Sci 18 587588
Mayewski P A Meeker L D Twickler M S Whitlow S Yang Q Lyons W B amp Pren-tice M 1997 Major features and forcing of high latitudes Northern Hemisphere atmosphericcirculation using a 110 000 year long glaciochemical series J Geophys Res 102 345365
Merkt J Muller H Knabe W Muller P amp Weiser T 1993 The Early Holocene Saksunarvatntephra found in lake sediments in NW Germany Boreas 22 93100
Narcisi B 1993 Segnalazione di un livello piroclastico di provenienza etnea nellrsquo area del Fucino(Italia Centrale) Quaternario 6 8792
Narcisi B 1996 Tephrochronology of a Late Quaternary lacustrine record from the Monticchiomaar (Vulture volcano southern Italy) Quat Sci Rev 15 155165
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
800 S M Davies and others
Newton A J amp Dugmore A J 1993 Tephrochronology of Core C from Lago Grande di Mon-ticchio In Paleolimnology of European Maar Lakes (ed J F W Negendank amp B Zolitschka)Lecture Notes in Earth Science vol 49 333348 Springer
Oldmacreld F Appleby P G amp Thompson R 1980 Palaeoecological studies of lakes in theHighlands of Papua New Guinea J Ecol 68 457477
Orsi G Drsquo Antonio M de Vita S amp Gallo G 1992 The Neapolitan Yellow Tureg a large mag-nitude trachytic phreatoplinian eruption eruptive dynamics magma withdrawal and calderacollapse J Volcanol Geotherm Res 53 275287
Paterne M Guichard F Labeyrie J Gillot P Y amp Duplessy J C 1986 Tyrrhenian Seatephrochronology of the oxygen isotope record for the past 60 000 years Mar Geol 72259285
Paterne M Guichard F amp Labeyrie J 1988 Explosive activity of the south Italian volca-noes during the past 80 000 years as determined by marine tephrochronology J VolcanolGeotherm Res 34 153172
Paterne M Labeyrie J Guichard F Mazaud A amp Maitre F 1990 Fluctuations of the Cam-panian explosive volcanic activity (south Italy) during the past 190 000 years as determinedby marine tephrochronology Earth Planet Sci Lett 98 166174
Pawse A Beske-Diehl S amp Marshall S A 1998 Use of magnetic hysteresis properties andelectron spin resonance spectroscopy for the identimacrcation of volcanic ash a preliminary studyGeophys J Int 132 712720
Pearce N J G Westgate J A amp Perkins W T 1996 Developments in the analysis of singleglass shards in volcanic deposits by laser ablation ICP-MS quantitative and single internalstandard multi-element methods Quat Int 3436 213227
Pearce N J G Westgate J A Perkins W T Eastwood W J amp Shane P 1999 Theapplication of laser ablation ICP-MS to the analysis of volcanic glass shards from tephradeposits bulk glass and single shard analysis Global Planet Change 21 151171
Pilcher J R amp Hall V A 1992 Towards a tephrochronology for the Holocene of the north ofIreland Holocene 2 255259
Ponel P amp Lowe J J 1992 Coleopteran pollen and radiocarbon evidence from the Prato Spillarsquo Drsquo succession N Italy C R Acad Sci Paris Sparaer II 315 14251431
Rose N L Golding P N E amp Battarbee R W 1996 Selective concentration and enumerationof tephra shards from lake sediment cores Holocene 6 243246
Ruddiman W F amp Glover L K 1972 Vertical mixing of ice rafted volcanic ash in NorthAtlantic sediments Geol Soc Am Bull 83 28172836
Ruddiman W amp McIntyre A 1981 The North Atlantic Ocean during the last deglaciationPalaeogeogr Palaeoclimatol Palaeoecol 35 145214
Santacroce R 1987 Somma Vesuvius Quad Ric Sci 114 252
Sarna-Wojcicki A 2000 Tephrochronology In Quaternary geochronology methods and applica-tions (ed J S Noller J M Sowers amp W R Lettis) AGU Reference shelf vol 4 pp 357377Washington DC American Geophysical Union
Sejrup H P Sjiquest holm J Furnes H Beyer I Eide L Jansen E amp Mangerud J 1989Quaternary tephrochronology on the Iceland Plateau north of Iceland J Quat Sci 4 109114
Sikes E L Samson C R Guilderson T P amp Howard W R 2000 Old radiocarbon agesin the southwest Pacimacrc Ocean during the last glacial period and deglaciation Nature 405555558
Stein R Nam S-I Grobe H amp Hubbersten H 1996 Late Quaternary glacial history andshort term ice rafted debris deg uctuations along the East Greenland continental marine In LateQuaternary palaeoceanography of the North Atlantic margins (ed J T Andrews W E NAustin H Bergsten amp A E Jennings) pp 135151 Geological Society London SpecialPublication
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 801
Stuiver M amp Grootes P M 2000 GISP2 oxygen isotope ratios Quat Res 53 277284
Stuiver M Reimer P J Bard E Beck J W Burr G S Hughen K A Kromer BMcCormac G Van der Plicht J amp Spurk M 1998 INTCAL 98 radiocarbon age calibration24 0000 cal BP Radiocarbon 40 10411083
Sweatman T R amp Long J V P 1969 Quantitative electron microprobe analysis of rock formingminerals J Petrol 7 332379
Turney C S M 1998 Extraction of rhyolitic ash from minerogenic lake sediments J Paleolim-nol 19 199206
Turney C S M amp Lowe J J 2001 Tephrochronology In Tracking environmental changes inlake sediments physical and chemical techniques (ed W M Last amp J P Smol) DordrechtKluwer Academic
Turney C S M Harkness D D amp Lowe J J 1997 The use of microtephra horizons tocorrelate Lateglacial lake sediments successions in Scotland J Quat Sci 12 525531
Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
van den Bogaard P amp Schmincke H 1985 A widespread isochronous Late Quaternary tephralayer in central and northern Europe Geol Soc Am Bull 96 15541571
van den Bogaard B Dordeg er W Sandgren P amp Schmincke H-U 1994 Correlating theHolocene records Icelandic tephra found in Schleswig-Holstein (northern Germany) Natur-wissenschaften 81 554556
Vernet G amp Raynal J-P 2001 Tephrostratigraphy of the Limagne revisited Implications forLateglacial and Holocene Prehistory In Tephras chronology archaeology (ed E Juvignparae ampJ-P Raynal) pp 111116 Dossiers de lrsquo ArchparaeoLogis no 1 France
Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
Vezzoli L 1991 Tephra layers in Bannock Basin (eastern Mediterranean) Mar Geol 1002134
von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
Walker M J C Bjorck S Lowe J J Cwynar L C Johnsen S Knudsen K-L WohlfarthB amp INTIMATE Group 1999 Isotopic events in the GRIP ice core a stratotype for the LatePleistocene Quat Sci Rev 18 11431150
Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
Phil Trans R Soc Lond A (2002)
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802 S M Davies and others
Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 771
Tab
le1
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5
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dro
nic
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6
Ju
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et
al
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7
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8
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rck
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9
Du
gm
ore
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n(1
998)
10
Bjo
rck
et
al
(1992)
11
Kva
mm
eet
al
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12
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ewel
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987)
14
Di
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oet
al
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15
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ibri
as
etal
(1979)
16
Ju
vig
nparae
etal
(1987)
17
Dav
ies
et
al
(2001)
18
van
den
Bogaard
ampS
chm
inck
e(1
985)
19
Fri
edri
chet
al
(1999)
20
Bra
uer
eta
l(1
999)
21
Etl
ich
eret
al
(1987)
22
Tu
rney
etal
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23
Pate
rne
et
al
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24
Kel
ler
(1980)
25
Eir
parasup3kss
on
etal
(2000)
26
Hadeg
idaso
net
al
(2000)
27
Ale
ssio
etal
(1976)
28
Vez
zoli
(1991)
29
San
tacr
oce
(1987)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
772 S M Davies and others
Tab
le1
(Con
t)
(Th
eva
rve
age
for
the
Laach
erS
ee(E
)rsquoro
wis
12
880
yea
rs)
GR
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rce
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IT
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470
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7152
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364
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928
104
6
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977
736
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DS
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(04
2)
27
604
801
8210
019
200
200
614
174
272
1
100
ED
S(0
55)
(00
7)
(01
7)
(02
3)
(00
5)
(00
9)
(02
7)
(06
4)
(04
7)
30
598
604
3201
823
300
102
018
071
578
0
100
ED
S
(07
7)
(02
3)
(04
6)
(03
3)
(00
4)
(02
5)
(06
1)
(08
)(0
46)
un
kn
own
12
820
sect60
(C
ap
eak)
(16684
m)
Ref
eren
ces
1
this
stu
dy
2
Pate
rne
etal
(1988)
3
Narc
isi
(1996)
4
All
enet
al
(1999)
5
An
dro
nic
oet
al
(1995)
6
Ju
vig
nparae
et
al
(1996)
7
Bir
ks
et
al
(1996)
8
Bjo
rck
ampW
ast
egordma
rd(1
999)
9
Du
gm
ore
ampN
ewto
n(1
998)
10
Bjo
rck
et
al
(1992)
11
Kva
mm
eet
al
(1989)
12
Zoli
tsch
ka
etal
(1995)
13
Ju
vig
nparae
ampG
ewel
t(1
987)
14
Di
Vit
oet
al
(1999)
15
Del
ibri
as
etal
(1979)
16
Ju
vig
nparae
etal
(1987)
17
Dav
ies
et
al
(2001)
18
van
den
Bogaard
ampS
chm
inck
e(1
985)
19
Fri
edri
chet
al
(1999)
20
Bra
uer
eta
l(1
999)
21
Etl
ich
eret
al
(1987)
22
Tu
rney
etal
(1997)
23
Pate
rne
et
al
(1986)
24
Kel
ler
(1980)
25
Eir
parasup3kss
on
etal
(2000)
26
Hadeg
idaso
net
al
(2000)
27
Ale
ssio
etal
(1976)
28
Vez
zoli
(1991)
29
San
tacr
oce
(1987)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 773
Tab
le1
(Con
t)
GR
IPage
tep
hra
age
(ss0
8c
volc
an
ich
ori
zon
(14C
yrs
)ti
me-
scale
)n
SiO
2T
iO2
Al 2
O3
FeO
Mn
OM
gO
CaO
Na
2O
K2O
P2O
5to
tal
EP
MA
sou
rce
ref
La
Nu
gmicroere
ca11
400
12
549
922
9160
470
002
324
454
744
538
972
4W
DS
La
Nu
gmicroere
6
21
(MC
)
Nea
poli
tan
ca12
000
17
588
104
2177
631
901
006
525
940
686
9
962
8W
DS
Cam
pi
1Y
ello
w(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(0
78)
Fle
gre
i
Tu
reg(I
T)
568
106
0194
448
7
17
451
938
75
5
100
ED
S
596
804
9192
940
3
06
435
034
588
9
100
ED
S2
14
619
403
1196
329
9
02
019
943
485
7
100
ED
S
Borr
ob
ol
ca12
300
18
733
601
1122
914
700
601
207
635
837
6
955
1W
DS
Hek
la22
(IC
)(0
35)
(00
2)
(01
8)
(00
9)
(00
2)
(00
2)
(00
3)
(01
4)
(00
9)
(0
47)
un
kn
ow
n14
650
sect200
(Ca
pea
k)
(17458
m)
un
kn
ow
n14
650
sect200
(C
ap
eak)
(17506
m)
E-2
P
oll
ara
ca13
000
766
302
7138
810
8
01
015
025
239
7
100
ED
SA
eoli
an
2
23
24
pu
mic
e(I
T)
Isla
nd
s
KO
L-G
S-2
13
400
18
490
910
6148
8100
702
184
9126
521
400
902
8989
6W
DS
25
(IC
)
GS
-2B
AS
-113
400
3497
417
0132
7124
402
266
6118
124
802
103
4988
7W
DS
26
(IC
)
Ref
eren
ces
1
this
stu
dy
2
Pate
rne
etal
(1988)
3
Narc
isi
(1996)
4
All
enet
al
(1999)
5
An
dro
nic
oet
al
(1995)
6
Ju
vig
nparae
et
al
(1996)
7
Bir
ks
et
al
(1996)
8
Bjo
rck
ampW
ast
egordma
rd(1
999)
9
Du
gm
ore
ampN
ewto
n(1
998)
10
Bjo
rck
et
al
(1992)
11
Kva
mm
eet
al
(1989)
12
Zoli
tsch
ka
etal
(1995)
13
Ju
vig
nparae
ampG
ewel
t(1
987)
14
Di
Vit
oet
al
(1999)
15
Del
ibri
as
etal
(1979)
16
Ju
vig
nparae
etal
(1987)
17
Dav
ies
et
al
(2001)
18
van
den
Bogaard
ampS
chm
inck
e(1
985)
19
Fri
edri
chet
al
(1999)
20
Bra
uer
eta
l(1
999)
21
Etl
ich
eret
al
(1987)
22
Tu
rney
etal
(1997)
23
Pate
rne
et
al
(1986)
24
Kel
ler
(1980)
25
Eir
parasup3kss
on
etal
(2000)
26
Hadeg
idaso
net
al
(2000)
27
Ale
ssio
etal
(1976)
28
Vez
zoli
(1991)
29
San
tacr
oce
(1987)
Phil Trans R Soc Lond A (2002)
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774 S M Davies and others
Tab
le1
(Con
t)
(Th
evarv
eage
for
the
Gre
enis
h(I
T)rsquo
row
is17
560
yea
rs)
GR
IPage
tep
hra
age
(ss0
8c
volc
an
ich
ori
zon
(14C
yrs
)ti
me-
scale
)n
SiO
2T
iO2
Al 2
O3
FeO
Mn
OM
gO
CaO
Na
2O
K2O
P2O
5to
tal
EP
MA
sou
rce
ref
GS
-2B
AS
-213
400
6497
933
2122
4147
902
445
389
829
905
205
4979
4W
DS
26
(IC
)
GS
-2B
AS
-313
400
2538
529
9125
7131
203
132
174
729
507
707
7980
1W
DS
26
(IC
)
GS
-2B
AS
-414
000
7503
617
4145
1113
202
155
3100
528
010
5
975
7W
DS
26
(IC
)
Un
ita
dei
ca14
000
5648
804
7184
625
901
602
217
432
679
302
8100
ED
SP
hle
gre
an
3
27
Tef
ra(0
53
)(0
13
)(0
25)
(07
4)
(01
4)
(01
6)
(01
6)
(03
4)
(06
6)
(01
6)
Fie
lds
Su
per
iori
(IT
)
Y-1
(IT
)ca
14
000
16
600
413
7169
555
502
218
242
262
229
306
8100
ED
SE
tna
28
Bla
ck17
000
sect300
Fea
ther
(17890
m)
Gre
enis
hca
15
000
9618
704
190
731
601
804
328
531
586
202
6100
ED
SV
esu
viu
s3
4
(IT
)(0
70
)(0
08
)(0
45)
(06
8)
(01
0)
(01
0)
(05
9)
(05
3)
(05
8)
(01
6)
29
L9
(IT
)ca
16
000
15
626
704
4188
630
401
103
329
429
683
402
7100
ED
SV
esu
viu
s3
15
17
000
(14
2)
(01
4)
(07
2)
(11
1)
(00
9)
(02
4)
(06
6)
(04
8)
(06
5)
(01
8)
St
2-1
85
18
500
7504
015
1145
5112
002
466
9114
525
206
6
992
2W
DS
26
(IC
)
Ref
eren
ces
1
this
stu
dy
2
Pate
rne
etal
(1988)
3
Narc
isi
(1996)
4
All
enet
al
(1999)
5
An
dro
nic
oet
al
(1995)
6
Ju
vig
nparae
et
al
(1996)
7
Bir
ks
et
al
(1996)
8
Bjo
rck
ampW
ast
egordma
rd(1
999)
9
Du
gm
ore
ampN
ewto
n(1
998)
10
Bjo
rck
et
al
(1992)
11
Kva
mm
eet
al
(1989)
12
Zoli
tsch
ka
etal
(1995)
13
Ju
vig
nparae
ampG
ewel
t(1
987)
14
Di
Vit
oet
al
(1999)
15
Del
ibri
as
etal
(1979)
16
Ju
vig
nparae
etal
(1987)
17
Dav
ies
et
al
(2001)
18
van
den
Bogaard
ampS
chm
inck
e(1
985)
19
Fri
edri
chet
al
(1999)
20
Bra
uer
eta
l(1
999)
21
Etl
ich
eret
al
(1987)
22
Tu
rney
etal
(1997)
23
Pate
rne
et
al
(1986)
24
Kel
ler
(1980)
25
Eir
parasup3kss
on
etal
(2000)
26
Hadeg
idaso
net
al
(2000)
27
Ale
ssio
etal
(1976)
28
Vez
zoli
(1991)
29
San
tacr
oce
(1987)
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 775
Altogether 34 tephra layers have been reported from sediment sequences in Europeand the NE Atlantic region which date to the period between 185 and 80 14C ka BP(table 1) Because tephra layers are deposited virtually instantaneously (in geologicalterms) they enotectively represent time-parallel marker horizons within stratigraphicalsequences (Westgate amp Gorton 1981 Sarna-Wojcicki 2000 Turney amp Lowe 2001) Intheory therefore all 34 tephras could prove valuable for correlation purposes eitherin a local context or in those cases where the ash deposits have been widely dispersedbetween regional sequences In practice however very little is known about the fullgeographical dispersal of the majority of the ash layers listed in table 1 Furthermorecorrelation by tephrostratigraphy will only work if the various ash layers have wellcharacterized geochemical signatures While some geochemical data are available forthe majority of the tephras listed in table 1 the collective data are far from robustand no geochemical data have yet been published for some
Nonetheless there is mounting evidence to show that some of the tephra depositslisted in table 1 are not only geochemically distinct but are also much more widelydispersed across Europe than was initially realized Stratigraphic records of thebetter-known tephras were initially limited to observations of visible tephra layersThe development of a technique that enables detection of tephra layers that are invis-ible to the naked eye (micro-tephra) in Late Glacial sequences has greatly extendedthe area over which some of the ashes can be traced (Lowe amp Turney 1997 Turneyet al 1997 Turney 1998 Wastegard et al 1998 2000a b) Most of this research sofar has focused on micro-tephra layers originating from Icelandic centres distributedthroughout northern Europe Here we report on further development of this line ofresearch with new evidence for the occurrence of micro-tephra layers in a site insouthern Europe The results suggest that there is great potential for tracing someash layers that originated from Italian volcanic complexes over much larger tracts ofsouthern and central Europe than records of visible tephra deposits allow This inturn greatly enhances the scope for making precise correlations not only betweenparts of southern Europe but also between continental and marine (MediterraneanSea) sequences
2 Micro-tephra extraction techniques
Micro-tephra horizons are composed of glass shards that are generally between 80and 24 m m (long axis) in size and that are present in such low concentration insedimentary sequences that they can only be detected by the use of a particle sep-aration technique Several factors inreguence the concentration of shards such as dis-tance from the volcanic source precipitation patterns during the eruption and sub-sequent tephra dispersal and sedimentary processes within the catchment In someterrestrial sequences micro-tephra horizons with a peak concentration (peak con-centration tends to coincide with the shy rst occurrence of glass shards in a sedimentsequence which is then taken to mark the time of maximum ash deposition) as lowas 10 shards cmiexcl3 has been conshy rmed whereas other sites have recorded as muchas 8000 shards cmiexcl3 (Turney et al 1997) In complete contrast tephra horizons inthe GRIP ice core have been identishy ed based on a single glass shard only (Gronvoldet al 1995)
Enotective separation techniques for the detection and isolation of tephra particlesfrom sedimentary sequences have been developed These include ashing of organic
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776 S M Davies and others
matter (Pilcher amp Hall 1992) digestion of biogenic and opaline silica (Rose et al 1996) the use of magnetic properties of ash layers (see for example Oldshy eld et al 1980 van den Bogaard et al 1994 Pawse et al 1998) X-ray analysis (Dugmore ampNewton 1992) and a density separation (regotation) technique (Turney 1998) Den-sity separation has proved exceedingly useful for the detection of small glass shardspresent in low concentrations in mineral-rich Late Glacial sediments This involvesthe separation and concentration of particles of predetermined specishy c gravity withthe use of a heavy liquid and subsequent identishy cation of glass shards with the useof a polarizing light microscope (for further details see Turney (1998)) This methodhas been particularly successful in the detection of tephras of rhyolitic compositionthat have a specishy c density of 2325 g cmiexcl3 (Lowe amp Turney 1997 Turney et al 1997 2001 Turney 1998 Wastegard et al 1998 2000a b) It is this technique thathas resulted in the wider recognition of micro-tephras in Europe as discussed below
3 Geochemical ` ngerprintingrsquo of tephra layers
The 34 tephras listed in table 1 have originated from four major volcanic complexesIceland the Massif Central in central France the Eifel district near Bonn and threevolcanic centres in Italy (the Campanian group Etna and the Aeolian Islands (seeshy gure 2)) An important matter to resolve is the extent to which the various magmasand ashes generated by these volcanic complexes can be geochemically shy ngerprintedThis is especially important in the case of tephras which have originated from thesame volcanic centre in which there may have been limited geochemical evolution ofmagmas over time In this section we summarize the approach generally adopted todetermine the geochemical character of visible and micro-tephras as background tothe geochemical data summarized in table 1 In the subsequent section of the paperwe review the present state of knowledge concerning all 34 tephras listed in table 1
Glass shards formed during the rapid cooling of magma are thought to have acomposition that is representative of the bulk geochemistry of the magma (Barker1983) hence widely dispersed glass particles are regarded as the most appropriateconstituents of pyroclastic material for geochemical analysis If a tephra deposit canbe shown to have a distinct geochemical signature then it can be used to correlatethe stratigraphic units in which it occurs (tephrostratigraphy) as well as to datethese units (tephrochronology) if the ages of the tephras are known (Westgate ampGorton 1981) A key element of building a tephrostratigraphical framework there-fore is to establish as rigorously as possible the geochemical composition of theindividual tephras used in its construction Robust and directly comparable geo-chemical datasets are dimacr cult to assemble for glass however because it is highlyunstable material particularly prone to sodium mobilization
The technique most widely employed to establish the geochemical signature of atephra is electron probe micro-analysis (EPMA) This enables grain-discrete determi-nations of the major elements within an individual glass shard which is of particularbeneshy t in the analysis of micro-tephra layers which generally contain glass particlesin low concentration The glass surface is bombarded with an electron beam and theX-ray energy produced is unique to each element while the intensity of the signalemitted is proportional to the amount of that element in the glass shard (Hunt amp Hill1993) Measurement can be by either energy dispersive spectrometry (EDS) or wave-length dispersive spectrometry (WDS) EDS has a lower precision mainly because
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European tephrochronological framework for Termination 1 777
N
0 500 km
Confirmed records of Vedde Ash (visible occurrences)
New records of Vedde Ash from flotation method
Extended area of Vedde Ash detection (micro-tephra)
Known area of Laacher See Tephra (visible occurrences)
Confirmed records of Neapolitan Yellow Tuff (visible occurrences)
New record of Neapolitan Yellow Tuff from flotation method
Known area of Neapolitan Yellow Tuff
Volcanic centres of particular relevance to this study
Other major volcanic centres in Europe
Figure 2 Location of the principal volcanic centres that were active during Termination 1 andthe Early Holocene The known distribution of the Vedde Ash (VA) Laacher See (LST) andNeapolitan Yellow Tureg (NYT) are shown
the behaviour of each element cannot be monitored independently during measure-ment and so this approach fails to detect for example any signishy cant mobilizationof sodium during the bombardment process (Hunt amp Hill 1993) Although WDSrequires a higher beam current and a longer counting time than EDS the formeronoters the distinct advantage of sequential acquisition of elemental data so that thedegree of sodium loss can be tracked The morphology of individual glass shards canalso distort EDS data a problem that is reduced when using WDS because for thisprocedure glass shards are mounted in an epoxy resin and polished to provide aregat surface for analysis Hence data should always be obtained using WDS whereverpossible
Even when WDS is used as a common tool for determining the geochemical spectraof samples aberrant results can arise that inreguence data comparisons For examplesome glass shards may contain tiny crystalline inclusions of feldspar and these shouldbe avoided when selecting surface points for analysis (Hunt amp Hill 2001) Hunt amp Hill
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778 S M Davies and others
6
4
2
40 50 60 70 80
K2O
(
)
SiO2 ()
Laacher See
Iceland
Veidivoumltn-Dyngjufjoumlll
Katla (basalt)
Grimsvoumltn-Kverkfjoumlll
Hekla
Katla (rhyolitic)
0
Icelandic volcanic centres8
10
Massif Central
Etna
Campanian
Figure 3 Bi-plot of SiO2 and K2 O concentrations in tephras derived from the main Europeanash provinces (modimacred after Mangerud et al 1984) The Campanian Massif Central and Etnaconcentrations are based on the data presented in table 1
(2001) have concluded that small variations in the laboratory procedures employedto determine glass chemistry can lead to misidentishy cation of sources for glass shardsand give an example of shards with a Jan Mayen provenance wrongly attributedto an Icelandic source Clearly there is a need for standardization of laboratoryprocedures and while a number of recommendations have recently been advocated(Froggatt 1992 Hunt amp Hill 1993 Hunt et al 1998) there is still some variation inlaboratory and operator practice (Hunt amp Hill 1996) Standardization is also requiredin the form in which results are presented to ensure comparability Normalizationof the data to 100 a practice employed by some researchers can obscure poorresults and hence lead to incorrect comparisons (Hunt amp Hill 1993) However othersargue that it may actually facilitate comparisons between samples by removing thedistorting enotects of the water component contained in glass shards (see for exampleFroggatt 1992) The majority of the published Italian and some of the Eifel datahave been normalized while those from other parts of Europe have not and hencedata comparisons are not always straightforward
Table 1 provides mean values and standard deviations for major oxide concentra-tions obtained from those tephras for which data are presently available The tableincludes previously unpublished WDS results for the Neapolitan Yellow Tunot (NYTdiscussed in x 4 below) and for the Mercato Tephra While individual tephra layersmay be geochemically distinct the geochemical envelopes representing the collectivedata obtained from all of the tephras assigned to each major volcanic province showsignishy cant overlaps as is illustrated in the bi-plots and ternary plots (shy gures 3 and 4)of selected oxide concentration data It is clear therefore that measurement of majoroxide concentrations does not satisfactorily discriminate between some tephras orig-inating from dinoterent volcanic centres (as noted by van den Bogaard amp Schmincke(1985) and Frezzotti amp Narcisi (1996) with respect to Eifel and Italian tephras)nor of tephras of dinoterent age originating from the same volcanic centre (Bond et
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European tephrochronological framework for Termination 1 779
40 50 60 70 80
K2O
(
)
SiO2 ()
shyshyshyshy
shy
shyshy
shyshyshy
shy
shy
shy
shy
reg
reg regreg
regregregregreg regregregregreg
FF
F
ll
l
l
4 8 12 16
reg
regreg
regreg
regregreg
regreg
regregreg
shy
F
l shyshyshyshyshy shyshyshyshyshyshy
F
F
l
ll
FeO ()
TiO
2 (
)
reg
l
Iceland
Eifel
F
shy ItalyMassif Central
100
80
60
40
20
100
80
60
40
20
100 80 60 40 20
CaO
FeO
K2O
regregreg
reg
reg
reg
reg
reg
reg
regregreg
shyF
F
F
regreg
l
lllshy
shyshyshy
shyshyshy
l
0
2
4
6
8
10
0
1
2
3
4
5
regreg
regreg
regreg
regreg
regreg
reg
reg
regreg
l
l
ll
shy
shyshy
shyshy
shy
shyshy
FF
F
100
80
60
40
20
100
80
60
40
20
100 80 60 40 20
K2ONa2O
CaO
(c) (d)
(a)
(b)
Figure 4 Plots of selected geochemical data obtained from tephras of Termination 1 age (seetable 1) (a) Bi-plot of mean SiO2 and K2 O values (b) Bi-plot of mean FeO and TiO2 values(c) Ternary plot indicating variations in the proportions of FeO CaO and K2 O (d) Ternaryplot indicating variations in the proportion of CaO Na2 O and K2 O
al 2001) Individual tephra layers are presently assigned to a particular volcanicevent on the basis of a combination of criteria usually including examination of thephysical properties (eg refractive index and surface detail of the glass shards) thestratigraphic position of the layer and independent assessment of the age of the layeras well as any geochemical data that may be available The construction of a tephro-stratigraphical scheme would clearly beneshy t from the application of a more diagnostic
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780 S M Davies and others
geochemical tool One approach that has promise is the analysis of trace and rareearth elements using an ultraviolet laser ablation inductively coupled plasma massspectrometer (UV-LA-ICP-MS) (Pearce et al 1996 1999 Eastwood et al 1999)This approach has been applied successfully to analysis of tephras of Mid-Holoceneage but not yet to tephras that fall within the period of interest here
4 Tephra layers in Europe and the North Atlantic regiondated to between 185 and 80 14C ka
(a) Icelandic province
The Icelandic volcanic systems are divided into three main groups based on theirgeochemical characteristics tholeiitic basalts transitional alkali basalts and alkaliolivine basalts (Jakobsson 1979) Collectively magmas from the Icelandic provincespan a wide geochemical spectrum although individual volcanic centres have tightgeochemical distributions (shy gure 3) for four of the main centres Grimsvotn-Kverfjolland Veidvotn-Dyngjufoll which form part of the northern (tholeiitic) volcanic zoneand Hekla and Katla which fall within the eastern (alkali olivine basalt and transi-tional alkali basalt) volcanic zone (Haregidason et al 2000) These appear to be thekey centres for the tephras listed in table 1 that have been assigned an Icelandicorigin
One of the best-known and most widely dispersed tephra horizons in northernEurope that has an Icelandic origin is the Vedde Ash (VA) which was depositedca 103 14C ka BP (Birks et al 1996 Wastegard et al 1998) within the GS-1Younger Dryas chronozone This ash is believed to originate from the Katla complexwithin the transitional alkali basalt province (Mangerud et al 1984 Lacasse et al 1995) in the south of the island The ash has a bimodal geochemical composition (rhy-olitic and basaltic) which is thought to reregect derivation from two separate magmachambers Studies of recent volcanic events in Iceland have shown that the mostexplosive eruptions generating the largest amounts of tephra occur in this tran-sitional alkali basalt province (Haregidason et al 2000) It is also believed that thewidespread distribution of this ash was caused by the development of co-ignimbriteash plumes during an ignimbrite-forming eruption (Lacasse et al 1995)
Layers of VA that are visible to the naked eye have been found in lake sediments inwestern Norway (Mangerud et al 1984) and the Inner Hebrides Scotland (Davies etal 2001) and in marine cores throughout the NE Atlantic (see for example Kvammeet al 1989 Lacasse et al 1995) in the northern North Sea (Long amp Morton 1987)on the Iceland plateau (Ruddiman amp McIntyre 1981 Sejrup et al 1989) and on theeast Greenland continental margin (Stein et al 1996) The distribution of the VAin North Atlantic marine sequences is characterized by an arcuate lobe extendingsouthwest from the Denmark Strait and curving eastwards to mid-latitudes in theNorth Atlantic (Lacasse et al 1995) This strongly suggests deposition from raftedice which was displaced to the southwest and south in a circulating counterclockwisegyre (Ruddiman amp Glover 1972) This may well reregect Katlarsquos close proximity tothe southern coast of Iceland with the Vedde tephra being deposited on ice thatcalved directly into the North Atlantic (Haregidason et al 2000) However depositionvia the atmosphere almost certainly took place as well as is indicated by the recentdiscoveries of rhyolitic VA in micro-tephra form in several sites in Scotland (Turneyet al 1997) southern Sweden (Wastegard et al 1998 2000a) and western Russia
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(Wastegard et al 2000b) A more recent discovery of a relatively high concentrationof rhyolitic VA glass shards in the northern Netherlands indicates that the ash maywell have been dispersed much further south than previously thought (S M Davies2002 unpublished work) Finally glass shards assigned to the VA have also beendiscovered in the GRIP ice core and dated to 11 980 sect 80 GRIP yr BP (Gronvold etal 1995) This discovery is extremely important for it indicates that the VA maywell provide a reliable time-parallel marker horizon between ice-core marine andterrestrial records
Two other important Icelandic ash layers the Borrobol and Saksunarvatn Tephraswere deposited near the beginning and end of the Last TerminationEarly Holoceneinterval respectively The Borrobol Tephra was discovered for the shy rst time in lakesediments in several sites in Scotland and as yet is known only in micro-tephra formIt has been dated in Scottish sites to ca 123 14C ka BP (Turney et al 1997) Whatis thought to be a contemporaneous tephra has been detected in marine sedimentson the North Icelandic shelf (Eirplusmn ksson et al 2000) This certainly has a very similargeochemical composition to those reported from Scotland but the horizon in whichit was discovered on the North Iceland plateau has been dated to 134 14C ka Theage discrepancy between the Scottish and Icelandic Borrobol Tephra layers may wellreregect the inreguence of a marine reservoir error although the possibility that severaltephras with similar geochemical composition were erupted over a period exceeding1000 yr cannot be ruled out (Larsen 2000)
The Saksunarvatn Ash appears to have been one of the largest Holocene eruptionsin Iceland It has a tholeiitic basaltic composition which is considered to indicate anorigin in the Grimsvotn or Kverfjoll complex (shy gure 3) (Mangerud et al 1986) Layersof this ash have been identishy ed in sites on the Faroe Islands (Mangerud et al 1986Dugmore amp Newton 1998 Wastegard et al 2001) the Shetland Isles (Bennet et al 1992) northern Germany (Merkt et al 1993) western Norway (micro-tephra) (Birkset al 1996) and in the GRIP (Gronvold et al 1995) and NordGRIP ice cores (S MDavies 2002 unpublished work) It has been dated to between 9060 and 8930 14C kaBP (Birks et al 1996) in Norway and to ca 10 240 sect 30 GRIP yr BP in the GRIPice core (Gronvold et al 1995) The Saksunarvatn Ash may thus provide a secondimportant widespread time-parallel marker between ice-core marine and terrestrialrecords
Other Icelandic tephras of rhyolitic amacr nity are less well known in terms of theirdistribution and geochemical variation The Hogstorpsmossen Tephra reported fromSweden (Bjorck amp Wastegard 1999) and the L3754 tephra discovered in the FaroeIslands (Dugmore amp Newton 1998) are known from single sites only and so theirpotential for tephrostratigraphy is uncertain at present Furthermore the geochem-ical spectrum of the Hogstorpsmossen Tephra is based on a small dataset with lowanalytical totals
A number of tephras of basaltic composition have originated from Iceland buttheir distributions are largely conshy ned to Iceland or to marine cores collected fromclose to the Iceland coast or in the North Atlantic These include the tephras listedas 1-THOL-1 1-THOL-2 KOL-GS-2 GS-2BAS-1 GS-2BAS-2 GS-2BAS-3 andGS-2BAS-4 in table 1 (Kvamme et al 1989 Bjorck et al 1992 Eirplusmn ksson et al 2000 Haregidason et al 2000) The shy rst two in this list are tholeiitic basaltic tephrasassociated with the VA in a complex series of tephras collectively termed NorthAtlantic Ash Zone 1 (NAAZ1) which has been detected in numerous marine cores
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782 S M Davies and others
from the North Atlantic Initially thought to represent a single eruption analysisof high-resolution sediment sequences from Lake Torfadalsvatn in northern Iceland(Bjorck et al 1992) the Hebridean Shelf near NW Scotland (Austin amp Kroon 1996)the St Kilda Basin (Hunt et al 1995) and the open North Atlantic (Bond et al 2001)has demonstrated that NAAZ1 comprises a series of distinct ashes that probablyreregect separate eruption events 1-THOL-1 is thought to originate from Veidivotn(shy gure 3) while Grimsvotn may have been the source of 1-THOL-2 (Kvamme et al 1989)
KOL-GS-2 is also of tholeiitic basaltic composition but is thought to originatefrom the Kolbeinsey Ridge system (Eirplusmn ksson et al 2000) To date this tephra hasbeen detected in one marine core only within the same record on the North Ice-landic shelf as that from which the correlative of the Borrobol Tephra was alsoreported (Eirplusmn ksson et al 2000) GS-2BAS-1 to GS-2BAS-4 are of uncertain ori-gin but are thought to have been deposited at roughly the same time as KOL-GS-2(ca 134 14C ka BP (Haregidason et al 2000))
The limited distribution of these basaltic tephras a feature that is not unique toIcelandic basaltic material may reregect two factors the relative magnitude of the vol-canic eruptions from which they were derived and the limited aerial transportationof basaltic glass which is denser than rhyolitic material However a rather surpris-ing recent discovery is that of visible basaltic VA in a site on the Isle of Skye inthe Inner Hebrides Scotland (shy gure 5) (Davies et al 2001) All other occurrencesof VA in Scotland are exclusively of rhyolitic material and in micro-tephra formonly (Turney et al 1997 Turney 1998) Clearly basaltic tephra must have beentransported subaerially as far south as Skye and the reason why it has not beendetected at other sites in Scotland is puzzling We suspect that this partly reregectsthe laboratory methods employed to separate glass shards present in low concentra-tion within a micro-tephra layer from the host sediment The technique used is adensity-separation (regotation) procedure (Turney 1998) and as basaltic shards havea specishy c density similar to quartz one of the most abundant minerals in lake sedi-ments of Late Glacial age basaltic material is dimacr cult to detect using this methodThis hypothesis is currently under investigation and alternative detection methodsare being explored including magnetic separation (Mackie et al 2002)
Several other events listed in table 1 that are of probable Icelandic origin includetephras recorded in the GRIP ice core including visible (eg the `Black Featherrsquo)tephras as well as uncertain tephras inferred from distinct Ca peaks (S Johnsen2001 personal communication) No glass shards have yet been detected in the latterbut a volcanic origin is assumed because high Ca peaks are associated with knowntephras in other Greenland ice cores (S Johnsen 2001 personal communication)These are referred to as `unknownrsquo in table 1 No geochemical analyses are availablefrom these horizons so their origin must remain speculative but a possible source isIceland in view of its proximity to the Greenland ice sheet and assumed atmosphericcirculation patterns
(b) Eifel province
There are two prominent tephra events dated to the Termination 1Early Holocenetime-span that originated from the Eifel province the Laacher See Tephra (LST)and the Ulmener Maar Tephra (UMT) Visible occurrences of the LST indicate that
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European tephrochronological framework for Termination 1 783
Vedde Ash
615 625 635 645 655depth (cm)
organic lake mudsHolocene
silty clayGS-1Younger Dryas
organic lake mudsGI-1Alleroslashd
100 microm
(a)
(b)
Figure 5 (a) Photograph of the visible VA layer discovered at Loch Ashik Isle of Skye InnerHebrides Scotland (b) Light microscope photograph showing the rich content of basaltic shards(examples are indicated by the arrows) within this layer (8024 m m size fraction)
this ash was dispersed over much of central Europe (van den Bogaard amp Schmincke1985 Friedrich et al 1999 Litt amp Stebich 1999) The LST is dated by radiocarbonto ca 110 14C ka BP (van den Bogaard amp Schmincke 1985) and to 11 063sect12 14C BP(Friedrich et al 1999) by varve chronology to 1288 varve ka BP (Brauer et al 1999Litt et al 2001) and by ArAr dating to 129 ka cal BP (van den Bogaard 1995) Ithas a phonolitic composition and is thought to have originated from a plinian andphreatomagmatic eruption with the distal ash being carried in three distinct plumesone to the northeast towards Poland one to the west and the third to the southcovering the Jura Mountains and north Italy (van den Bogaard amp Schmincke 1985Juvigne et al 1995 Bossuet et al 1997) This pattern is thought to reregect altitu-dinal variations in the predominant wind direction Sedimentary sequences near thevolcanic source indicate that the LST consists of three main layers which represent
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784 S M Davies and others
dinoterent eruption phases These are grouped together as the Laacher See TephraFormation but the three individual units can be traced within and between a seriesof depositional fans The geochemical data obtained from these three LST layersshow signishy cant variations as reregected in the ternary plots (shy gure 4)
The Early Holocene Ulmener Maar Tephra (UMT) is of rhyolitic composition andappears to be restricted to sites in Germany though this conclusion is also based onrecords of visible tephras only It is dated to ca 956 14C ka BP and to 110 varve ka(Zolitschka et al 1995 Litt et al 2001)
(c) Massif Central province
The Massif Central tephras are mainly of basaltic trachyandesitic compositionwhich is distinct from the other ash provinces (shy gures 3 and 4) and their known dis-tributions are mostly conshy ned to the Massif Central region The ages of the MassifCentral tephras are based on radiocarbon dates obtained from mire and lake sedi-ments which `bracketrsquo the tephras The La Nugsup3ere Tephra with an age of 114 14C kaBP is the oldest Massif Central tephra identishy ed so far within the time-span of inter-est (Etlicher et al 1987 Juvigne et al 1996) The two Godivelle Tephras (5 and 4)are close in age but extensive radiocarbon dating suggests distinct ages of 107and 103 14C ka BP respectively (Juvigne et al 1996) The age of the Puy de DomeTephra is less certain as the estimate is based on only one radiocarbon date froma site in the southern Chaplusmn ne des Puys (table 1) This tephra is thought to havea trachyte composition (Juvigne 1993) although no major element concentrationshave yet been published
The ChopineKilianVasset tephras are thought to be derived from three separateEarly Holocene eruptions although the stratigraphic succession is not known atpresent These trachytic tephras have been radiocarbon dated to ca 854sect150 14C kaBP but are thought to have erupted separately within ca 260 yr (Juvigne et al 1996) This series of tephras is considerably more widespread than the others fromthe region having been identishy ed as far east as the Jura Mountains (Martini amp Duret1965 Martini 1970) Some other ash falls that originated from the Chaplusmn ne des Puysappear to be of local importance only (Vernet et al 1998 Vernet amp Raynal 2001)Geochemical data are currently available for only three of the Massif Central tephrasand so far as is known no attempt has yet been made to identify these tephras inmicro-tephra form
(d ) Italian provinces
The Italian tephras from this period can be assigned to three main volcanic com-plexes the Campanian volcanic shy elds around Naples Etna on Sicily and the AeolianIslands The Campanian complex which includes the Phlegrean Fields Vesuviusand Ischia is mainly trachytic in composition with a geochemical spectrum that isquite distinct from those of the Etna complex and of the Aeolian Islands (shy gure 3)Tephras originating from one or more of these three complexes have been detectedin marine cores from the Tyrrhenian and Adriatic seas as well as other parts of theMediterranean Sea (Keller et al 1978 Paterne et al 1986 1988 1990 Langone etal 1996) and in lake sequences in southern Italy such as Lago Grande di Monticchio(Newton amp Dugmore 1993 Narcisi 1996 Allen et al 1999) and central Italy such asLago Albano near Rome (Calanchi et al 1996) Some work has also been conducted
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European tephrochronological framework for Termination 1 785
in or close to the volcanic source areas in an attempt to establish the full sequenceof volcanic eruptions during the Late Quaternary (see for example Di Vito et al 1999) There are nine Italian tephras reported from marine and lake sequences thatdate from the period between 185 and 80 14C ka BP In all instances the recordsare of visible layers of tephra The ages of some of these are poorly established atpresent with conregicting data obtained from dinoterent sites The ages suggested intable 1 are those favoured in the most recent publications but these may requirere-assessment in the light of future research
The two oldest known tephras in the time-period of interest are the L9 and Green-ish Tephras both recorded as separate features within the annually laminated Lagodi Monticchio maar sequence The lowest of the two L9 is considered to be the cor-relative of the `basalrsquo plinian eruption of Vesuvius (Narcisi 1996) Age estimates ofa palaeosol that underlies the Vesuvius tephra sequence are ca 1617 14C ka BP forthis event (Delibrias et al 1979) L9 has a trachytic composition very similar to theGreenish Tephra (table 1) However L9 which is also a product of Vesuvius is foundstratigraphically below the Greenish Tephra in the Lago di Monticchio core TheGreenish Tephra is dated in the Monticchio sequence to 17 560 varve yr BP (Allenet al 1999) and has a calibrated radiocarbon age estimate of 17 830 sect 300 cal BP(Andronico et al 1995) Both tephras have a dominantly eastwards dispersal basedon the occurrences of visible layers (Santacroce 1987 Narcisi 1996) Both tephrasalso have a trachytic composition and as can be seen from table 1 the reportedgeochemical spectra are very close indeed with the standard deviations overlappingfor almost every major element This could present problems for tephrostratigra-phy where only one of the tephras is evident in a sediment sequence in particularbecause they are so close in age This is a good example of where an analysis oftrace and rare earth elements might be required to make a clear distinction betweentephras with very similar major oxide concentrations
The Y-1 Tephra also termed the Biancavilla Montalto Ignimbrite (Vezzoli 1991)is a product of Etna and has been identishy ed as a visible benmoritic tephra horizonthroughout the central Mediterranean (Paterne et al 1988) including central Italyand the Adriatic Sea (Vezzoli 1991 Narcisi 1993 Calanchi et al 1996) It has anestimated age of ca 140 14C ka BP The Unita dei Tefra Superiori tephra which hasbeen detected as far east as Lago di Monticchio in south-central Italy (Narcisi 1996)is also dated to ca 140 14C ka BP (Alessio et al 1976) but it is thought that thesource of this tephra lies in the Phlegrean Fields No geochemical data are availablefrom the presumed source region|the data reported in table 1 were obtained fromthe Lago di Monticchio record (Narcisi 1996)
The NYT which is equivalent to the C-2 tephra reported from various marinesequences has also been traced throughout central Italy and the Adriatic Sea (Pat-erne et al 1988 Calanchi et al 1996 Di Vito et al 1999) (shy gure 2) In the centralApennines region it formed the parent material for a soil that started to developat the beginning of the Holocene period (Frezzotti amp Narcisi 1996) Also originatingfrom the Campi Flegrei caldera it is dated to ca 120 14C ka BP (Di Vito et al 1999) Published geochemical data based on EDS indicate three dinoterent geochemicalpopulations varying from latite to phonotrachyte in composition (Orsi et al 1992Paterne et al 1988) (table 1) We report in x 4 of this paper on new data obtainedfrom the NYT by WDS and it is the mean of these new data that is included intable 1 Comparisons with the previously published EDS data are provided (table 1)
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786 S M Davies and others
The new data indicate clearly that the NYT originated from the Campanian volcaniccentre
In the interval between the dispersal of the NYT (ca 120 14C ka BP) and 95 14Cka BP there appear to have been as many as 34 eruptions in the Campi Flegrei caldera(Di Vito et al 1999) Of these only one appears to have been detected widely in theregion the Pomici Principali (also termed the Agnano Formation or C-1 tephra inmarine records (Paterne et al 1988) This was the product of the highest magnitudeeruption from this epoch and is dated to between 976 sect 300 and 1032 sect 50 14C kaBP (Delibrias et al 1979 Di Vito et al 1999) or to 122 varve ka BP based on theMonticchio varve chronology (Allen et al 1999) It is trachytic in composition andappears to have had a mainly eastwards dispersal
The Mercato Tephra dated to ca 80 14C ka BP and originally analysed usingEDS has a phonolitic composition and is believed to have been generated by Vesu-vius (Paterne et al 1988) New WDS data obtained from reference samples col-lected from an exposure to the west of Naples support these conclusions (table 1 andAppendix A) The silica content of the WDS analyses are ca 3 lower than thoseobtained using EDS (table 1) which may reregect the fact that the EDS data werenormalized
The only tephra listed in table 1 that is thought to have originated from the AeolianIslands is the Pollara pumice also referred to as the E2 tephra in marine sequences(Paterne et al 1986 1988) The limited geochemical data available so far suggest itto be the only Italian tephra listed in table 1 that is rhyolitic in composition Littlemore is known about this ash which has not been recorded extensively except thatits age is estimated to be ca 130 14C ka BP (Keller 1980)
5 Extending the known distributions of European tephras
Figure 2 summarizes schematically the known distributions of three of the tephrasreferred to in the preceding section the VA the LST and the NYT Following theintroduction of a laboratory method that enables the detection of micro-tephra parti-cles in mineral-rich sediment the VA has been traced to sites that are located muchfarther south (into The Netherlands) and east (as far as St Petersburg) than thedistribution limits based on occurrences of visible layers of the ash As a result con-tinental sequences over a much larger area in northern Europe can now be correlateddirectly with marine and ice-core records using the VA as a time-parallel marker
This suggests therefore that other prominent ash layers such as the LST andNYT should also be detectable over larger tracts of Europe than is presently thecase if suitable sites are examined for the presence of micro-tephra horizons To testthis assertion we examined lake sediment deposits of Last Termination age froma site in the northern Apennines in order to establish whether the NYT could bedetected in micro-tephra form The site selected Prato Spilla `Crsquo lies well to thenorth of the localities in central and southern Italy and in the Adriatic Sea fromwhich visible records of the NYT have been reported Prato Spilla `Crsquo lies at an alti-tude of ca 1350 m in the Appennino Parmense ca 60 km south of Parma and 15 kmeast of Pontremoli The site contains a continuous sediment sequence spanning theLast Termination and most of the Holocene Detailed pollen and coleopteran strati-graphical records which have been radiocarbon dated have been published for thissite (Lowe 1992 Ponel amp Lowe 1992 Lowe amp Watson 1993)
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Figure 6 Light microscope photograph of an NYT glass shard from Prato Spilla Crsquosequence assigned on geochemical grounds to the NYT
The methods adopted for sub-sampling of the Prato Spilla `Crsquo sequence for thequantishy cation of glass shard concentrations and for subsequent electron microprobeanalysis of selected glass shards followed those described elsewhere (Turney 1998)In summary contiguous samples of 1 cm stratigraphic interval were extracted fromthe sequence to establish presenceabsence of glass shards Each of the 1 cm3 blocksin which tephra particles was detected was then examined with more care andshard concentrations were quantishy ed for each sub-sample Micro-tephra particleswere detected in shy ve samples (shy gure 6) but were predominantly clustered around500 cm in the part of the sequence assigned on pollen-stratigraphic grounds to theLate Glacial Interstadial or the `Allerfrac12drsquo|indeed the part of the succession in whichthe NYT would be expected to occur Peak concentrations of micro-tephra particlesreach 225 shards cmiexcl3 and are conshy ned to a single 1 cm thick sample in the sequencewhich probably represents the time of maximum deposition of the ash
Electron microprobe measurements based on WDS were obtained from the surfacesof 21 separate glass shards extracted from the sample with peak shard concentrations(Appendix A) Since only EDS measurements were available for the NYT prior to thepresent study we also obtained WDS measurements from 17 shards extracted fromthe visible layer of NYT that is exposed on Procida Island which lies in the type-locality for the NYT close to the city of Naples (Appendix A) The results providenot only a more comprehensive geochemical dataset for the NYT than was previ-ously available but also a consistent basis for comparison with the Prato Spilla `Crsquodataset All of the WDS data reported here (Appendix A) were measured at the samelaboratory (Tephrochronology Analytical Unit University of Edinburgh) using thesame sample pretreatment and preparation protocol The WDS results for the NYTdinoter to a minor degree from the EDS results (table 1 and Appendix A) especiallywith respect to the amounts of silica aluminium and calcium measured The EDS
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788 S M Davies and others
4 8FeO ()
TiO
2 (
) Neapolitan Yellow Tuff(Procida)Neapolitan Yellow Tuff(Prato Spilla lsquoCrsquo)
0
1
2
3
40 50 60 70
MgO
(
)
SiO2 ()
K2O
(
)
40 50 60 70
0
04
08
4
8
12
SiO2 ()
(a)(b)
(c)
Figure 7 Bi-plots of SiO2 K2 O SiO2 MgO and FeOTiO2 for the WDS analyses obtainedfrom glass shards of the NYT from Procida (Naples) and Prato Spilla Crsquo Means and standarddeviations are shown
results show a higher degree of statistical scatter than the WDS measurements whichmay reregect the fact that the data were normalized combined with the inreguence ofvariation in water content between shards
There is a very close correspondence between the WDS data for the Prato Spilla `Crsquomicro-tephra shards and those obtained from the type-material near Naples (shy g-ure 7) The geochemical data strongly suggest therefore that the NYT is representedat the Prato Spilla `Crsquo site by a discrete layer of micro-tephra particles This conclu-sion is compatible with the pollen-stratigraphic data from the site and accords withage estimates for the NYT (ca 120 14C ka BP) obtained from other sites (Paterneet al 1990)
These results encourage us to believe that many if not all of the tephras listedin table 1 will be detectable over much larger tracts of Europe than is presently thecase if appropriate research is undertaken to detect layers of micro-tephra particlesin selected sites The authors are presently engaged in a major continent-wide pro-gramme of research in collaboration with a number of European research groupsdesigned to test this hypothesis The focus in this research is on those parts of Europewhere we expect to shy nd overlapping `apronsrsquo of tephra deposition originating fromthe Italian Eifel Massif Central and Icelandic provinces For example a number ofsites in parts of southern France northern Italy and perhaps western Switzerlandmay have received inreguxes of micro-tephra originating from the Italian and Eifelprovinces and perhaps also from the Massif Central Sites in parts of Germany Den-mark and southern Sweden for example may in turn have received tephra depositsfrom both of the Icelandic and Eifel provinces If this proves to be the case then thestage will be set for the construction of a tephrostratigraphical framework for Europewhich will enable Last Termination sequences to be correlated on a continent-widebasis using micro- and visible tephra layers as time-parallel stratigraphic markersFurthermore there is also the possibility that other tephras remain to be discovered
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European tephrochronological framework for Termination 1 789
those which either because of the magnitude or nature of some volcanic eruptionswere distributed over parts of Europe in micro-tephra form only
6 European tephrostratigraphy and the chronology of eventsduring the Last Termination and Early Holocene
One of the crucial issues in Late Quaternary palaeoenvironmental research thatremains to be resolved is the degree to which climatic events inferred from oceanicterrestrial and ice-core records were synchronous during the Last Termination andEarly Holocene If the ice-core records provide realistic estimates of the rates anddurations of climatic events during this period then comparisons between individ-ual records have to be enotected with at least a decadal precision The problem thispresents and the role that tephrostratigraphy can play in resolving some of thedimacr culties involved are put into perspective in shy gure 8
Figure 8 shows some of the data used to calibrate radiocarbon dates (the LakeSuigetsu and Cariaco Basin datasets) plotted against the GRIP ss08c ice-core recordof macr 18O variations The latter has been selected by the INTIMATE group as an arbi-trary and temporary standard for this period and used to deshy ne an event stratig-raphy scheme (shy gure 1) for the Last Termination (see Bjorck et al 1998 Walker etal 2001) As has been alluded to in earlier sections of this paper the uncertaintiesassociated with all of the dating methods currently employed preclude precise com-parisons of ice-core marine and terrestrial records Oceanic and terrestrial recordsmostly rely upon radiocarbon dating locally supplemented in a few cases by varvechronology Imprecisions in radiocarbon dates can arise through site-specishy c fac-tors (eg hard-water or mineral carbon errors in freshwater sequences and reservoirerrors in marine sequences) sample selection laboratory measurements of 14C activ-ity and other factors (Lowe amp Walker 2000) Further imprecision may be introducedby the calibration of radiocarbon dates since the uncertainties in the dataset usedto calibrate pre-Holocene radiocarbon dates INTCAL98 are far higher than forthe Holocene which is based on dendro-calibration (Stuiver et al 1998) There arealso uncertainties anotecting varve chronologies while the ss08c ice-core chronologyfor the Last Termination dinoters signishy cantly from the GISP2 record and indeedfrom other models of the GRIP record (Lowe et al 2001) Published comparisonsbetween ice-core marine and terrestrial records for the Last Termination seldom takeinto account the true magnitude of the dating uncertainties involved and frequentlyemploy circular reasoning
Figure 8 shows the positions on the radiocarbon time-scale of 20 of the tephrasdiscussed earlier in this paper these being the ones for which reasonably conshy dentradiocarbon age estimates can be made (though these will be subject to revised esti-mates in the future) A high number of these occur in the period 14080 14C kaBP but we conshy dently anticipate the discovery in the future of additional tephras(perhaps in micro-tephra form only) which will date to the period 185140 14C kaBP Tephras detected in the GRIP ice core over the same time-interval are plottedon the calendar time-scale in shy gure 8 By providing key `time-linesrsquo between recordstephrostratigraphy can help to resolve some of the dating uncertainties referredto earlier by for example enabling direct comparisons of discrepant age estimatesobtained using dinoterent methods (cf Litt et al 2001) It can also provide estimatesof the magnitudes of the reservoir errors that anotected various marine sectors at dif-
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790 S M Davies and others
-44
-40
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-32
cale
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rs B
P
8000
9000
10 0
00
11 0
00
12 0
00
13 0
00
14 0
00
15 0
00
16 0
00
17 0
00
18 0
00
14C age (BP)
VA
SA
Un
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Hol
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cher
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God
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-TH
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ocircme
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lmen
er M
aar
amp L
3574
radiocarbon dated European tephra horizons
Cho
pine
Kili
an V
asse
tM
erca
to
God
ivel
le 4
Pom
ici P
rinc
ipal
i amp V
edde
Polla
ra p
umic
eK
OL
-GS-
2 amp
GS
-2B
AS-
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GS
-2B
AS-
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nita
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Tef
raSu
peri
ori amp
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-1
Gre
enis
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L9
20 0
0018
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16 0
0014
000
12 0
0010
000
-44
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800
600
400
200 0
GISP2 volcanicsulphate conc (ppb)
1000
Nea
polit
an Y
ello
w T
uff
GISP2 18O (permil) dGRIP 18O (permil) d
Figure 8 For description see opposite
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 791
ferent times through a comparison of radiocarbon dates obtained from marine andterrestrial horizons in which the same tephra has been detected (see for exampleAustin et al 1995 Bondevik et al 2001 Haregidason et al 2000) Tephrostratigraphymay provide an independent test of suggestions that some of the climatic changesduring the Last Termination were time-transgressive as illustrated for some appar-ently contrasting climatic trends in Iceland Britain and NW Russia (Lowe 2001) Ofparticular importance as far as establishing `leadsrsquo and `lagsrsquo in climatic changes isconcerned are the tephra records from the Greenland ice cores The discovery of theVedde and Saksunarvatn ashes in the GRIP record (Gronvold et al 1995) alreadyprovides a basis for making direct comparisons between marine terrestrial and ice-core records It is a matter of some urgency that the incidence of tephra depositsin the Greenland ice cores be more fully explored in the hope that this will lead tothe recognition of additional time-parallel links between the ice-core records on theone hand and oceanic and terrestrial records on the other An investigation of thenew NordGRIP record for this purpose is currently in progress (S M Davies 2002unpublished data)
Finally a fuller and more reshy ned tephrostratigraphical scheme for Europe will alsohave other applications It will provide an important database for those investigatingthe timing and frequency of volcanic eruptions in Europe during the past 20 000 yror so as well as of the geochemical evolution of the dinoterent volcanic centres overthat period A fuller record of the distribution of micro-tephras may also provideinformation on atmospheric circulation patterns during the dispersal and depositionperiods as well as on the nature and altitude of the eruption columns which mayin turn provide inferences about magma viscosity
This paper is a contribution to the INTIMATE project of the INQUA Palaeoclimate Com-mission and the work is supported by a Leverhulme Trust Research project (grant allocationnumber F07537C) entitled Testing hypotheses of rapid climate change using tephrochronol-ogyrsquo SMDrsquo s contribution was completed during possession of a NERC PhD studentship(GT 0499ES162) We are extremely grateful to Dr Peter G Hill for his assistance withthe EPMA analyses at the Tephrochronology Analytical Unit University of Edinburgh We alsothank Dr G Mastrolorenzo (Vesuvius Observatory) and Miss G Swindle for assistance duringthe macreld investigations in Naples Thanks are also expressed to two anonymous reviewers forcomments on an earlier draft
Appendix A
Table 2 shows the major oxide concentrations of NYT glass shards from Procidaand Prato Spilla `Crsquo and of the Mercato Tephra from the Naples area (see x 4 forsite context) All oxides are shown as weight and total iron is expressed as FeO
Figure 8 Radiocarbon calibration curve for Termination 1 and the Early Holocene compared with theGRIP macr 18 O event stratigraphy the GRIP ss08c and GISP2 macr 18 O records (wwwngdcnoaagov) andknown tephra horizons from this period The shaded areas represent the cooler climatic episodes andare labelled with the Greenland stratotype terminology (Bjorck et al 1998) Where radiocarbon agesare reported in table 1 as a range the mean is given here Abbreviations for GRIP horizons are asfollows Un unknown (approximate positions are given (S Johnsen 2001 personal communication))SA Saksunarvatn Ash VA Vedde Ash BF Black Feather Sulphate concentrations from the GISP2record are also shown (Zielinski et al 1996) Open circles denote radiocarbon calibration data fromLake Suigetsu (Kitagawa amp van der Plicht 2000) Filled circles denote radiocarbon calibration data fromCariaco Basin assuming a marine reservoir age of 420 14 C yr (Hughen et al 1998)
Phil Trans R Soc Lond A (2002)
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792 S M Davies and others
Tab
le2
Majo
roxi
de
con
cen
trati
on
sof
NY
Tgl
ass
shard
sfr
om
Pro
cida
an
dP
rato
Spil
laC
rsquoan
dof
the
Mer
cato
Tep
hra
from
the
Naple
sare
a(s
eex4
for
site
con
text
)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
roci
da)
1584
204
0177
634
201
106
828
635
197
5969
1W
DS
2598
603
9178
027
101
204
924
244
583
4965
8W
DS
3586
604
5173
631
100
805
924
342
183
0951
9W
DS
4583
903
9177
933
000
906
924
540
486
9958
3W
DS
5605
106
8179
126
901
204
923
243
086
1976
4W
DS
6591
704
5177
332
801
006
425
740
887
8968
0W
DS
7581
804
1178
031
501
107
125
640
086
9956
1W
DS
8589
504
2179
533
701
506
926
740
987
5970
4W
DS
9592
003
9178
135
101
007
026
443
585
7972
7W
DS
10
591
404
2174
631
601
105
723
442
482
6957
0W
DS
11
593
403
6177
131
301
506
726
439
188
5967
6W
DS
12
588
103
8176
128
100
505
525
141
583
4952
1W
DS
13
577
003
8176
533
500
807
228
140
384
8952
0W
DS
14
586
004
7179
735
300
706
827
842
984
6968
5W
DS
15
588
104
2180
629
400
505
924
937
993
0964
5W
DS
16
579
603
9178
536
501
308
228
836
087
1959
9W
DS
17
580
103
9177
631
500
907
327
039
488
9956
6W
DS
mea
n588
104
2177
631
901
006
525
940
686
9962
8
sd
(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(07
8)
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 793
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
rato
Spil
laC
rsquo)
1552
105
4177
247
401
914
38
735
578
9951
1W
DS
2557
305
7179
845
701
512
640
136
581
5960
6W
DS
3595
004
4173
724
302
003
117
652
877
8950
7W
DS
4575
704
2179
433
001
406
627
043
083
6953
7W
DS
5599
904
0178
826
401
304
421
841
688
4966
5W
DS
6591
103
8177
826
601
105
022
443
888
8960
2W
DS
7565
304
5180
939
501
410
532
535
791
8962
1W
DS
8597
606
9180
826
501
604
821
546
684
6970
7W
DS
9571
805
6179
939
801
109
932
240
883
6964
7W
DS
10
588
603
7176
527
601
104
721
042
487
7953
3W
DS
11
559
404
9180
544
501
812
339
435
878
6957
2W
DS
12
594
704
0181
328
301
705
522
144
785
6967
9W
DS
13
611
103
7187
016
900
802
419
938
195
9975
8W
DS
14
599
204
4181
128
601
404
620
844
986
6971
6W
DS
15
601
204
4177
328
302
004
722
446
385
5972
1W
DS
16
595
104
5176
428
801
504
722
744
884
3962
8W
DS
17
603
704
1177
825
101
503
520
348
181
2965
3W
DS
18
558
704
5179
647
401
813
139
836
879
0960
7W
DS
19
589
602
8178
830
901
606
622
436
091
8960
5W
DS
20
553
606
3178
647
401
913
840
136
978
0956
6W
DS
21
579
004
0175
739
000
708
328
338
286
7959
9W
DS
mea
n582
804
6179
033
401
507
427
341
484
8962
1
sd
(1
87)
(01
0)
(02
7)
(09
2)
(00
4)
(03
9)
(08
0)
(04
9)
(05
0)
(07
0)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
794 S M Davies and others
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)
1575
202
7194
219
701
101
016
374
766
9951
8W
DS
2575
802
9194
523
902
201
520
273
564
5959
0W
DS
3574
301
4205
219
101
100
416
481
266
1965
2W
DS
4575
500
7206
018
002
000
415
181
669
3968
6W
DS
5580
000
9208
018
601
300
515
883
367
1975
5W
DS
6571
001
0206
016
101
600
515
078
967
1957
2W
DS
7577
501
1201
117
101
500
620
675
655
4950
5W
DS
8573
700
9212
717
101
900
815
187
564
2973
9W
DS
9580
301
3208
715
801
400
824
81
754
1968
1W
DS
10
574
400
6211
18
402
00
516
480
567
8971
6W
DS
11
577
200
7214
212
501
200
829
879
247
962
6W
DS
12
572
200
9211
217
301
501
15
980
465
9966
3W
DS
13
571
800
7210
417
402
201
16
184
467
2971
2W
DS
14
567
300
9208
916
901
400
917
383
262
5959
3W
DS
15
568
600
8205
918
202
101
414
682
666
6960
8W
DS
16
572
501
1211
318
202
01
215
884
364
5970
9W
DS
17
572
901
2212
916
502
101
215
883
667
2973
4W
DS
18
573
01
4211
716
301
801
416
83
365
5970
4W
DS
19
569
201
1207
418
602
101
414
982
964
961
6W
DS
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
3)
(04
2)
(01
3)
(00
1)
(00
2)
(01
)(0
39)
(01
1)
(02
5)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
References
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Hoek W Z amp Bohncke S J P 2001 Oxygen isotope wiggle matching as a tool for synchronisingice-core and terrestrial records over Termination 1 Quat Sci Rev 20 12511264
Hughen K A Overpeck J T Peterson L C amp Trumbore S 1996 Rapid climate changes inthe tropical Atlantic region during the last deglaciation Nature 380 5153
Hughen K A Overpeck J T amp Lehman J 1998 A new 14 C calibration data set for the LastDeglaciation Radiocarbon 39 483494
Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
Hunt J B amp Hill P G 1996 An inter-laboratory comparison of the electron probe microanalysisof glass geochemistry Quat Int 3436 229241
Hunt J B amp Hill P G 2001 Tephrological implications of beam sizesample size ereg ects inelectron microprobe analysis of glass shards J Quat Sci 16 105117
Hunt J B Fannin N G T Hill P G amp Peacock J D 1995 The tephrochronology andradiocarbon dating of North Atlantic Late Quaternary sediments an example from the StKilda Basin In The tectonics sedimentation and palaeoceanography of the North Atlanticregion (ed R A Scrutton M S Stoker G B Shimmield amp A W Tudhope) vol 90pp 227248 Geological Society of London Special Publication
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Juvignparae E amp Gewelt M 1987 La Narse drsquo Ampoix comme tparaephrostratotype dans la Chasup3 ne desPuys mparaeridionale (France) Bull Ass Fr Etud Quat 29 3749
Juvignparae E Kozarski S amp Nowaczyk B 1995 The occurrence of Laacher See Tephra in Pomera-nia NW Poland Boreas 24 225231
Juvignparae E Bastin B Delibrias G Evin J Gewelt M Gilot E amp Streel M 1996 Acomprehensive pollen and tephra based chronostratigraphic model for the Lateglacial andHolocene period in the French Massif Central Quat Int 3436 113120
Keller J 1980 The island of Vulcano Rend Soc It Mineral Petrolog 36 369414
Keller J Ryan W B F Ninkovich D amp Altherr R 1978 Explosive volcanic activity in theMediterranean over the past 200 000 years as recorded in deep sea sediments Geol Soc AmBull 89 591604
Kitagawa H amp van der Plicht J 2000 Atmospheric radiocarbon calibration beyond 11 900 calBP from Lake Suigetsu laminated sediments Radiocarbon 42 369380
Kvamme T Mangerud J Furnes H amp Ruddiman W F 1989 Geochemistry of Pleistoceneash zones in cores from the North Atlantic Norsk Geol Tids 69 251272
Lacasse C Sigurdsson H Johannesson H Paterne M amp Carey S 1995 Source of Ash zone 1in the North Atlantic Bull Volcanol 57 1832
Langone L Asioli A Corregiari A amp Trincardi F 1996 Age depth modelling through theLate-Quaternary deposits of the central Adriatic Basin In Palaeoenvironmental analysis ofItalian crater lake and Adriatic sediments (ed F Oldmacreld amp P Guilizzoni) vol 55 pp 177196 Memorie dellrsquo Instituto Italiano di Idrobiologia
Larsen G 2000 Holocene volcanism in Iceland and tephrochronology as a tool in volcanologyIn Iceland 2000 modern processes and past environments Keele University UK
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 799
Litt T amp Stebich M 1999 Bio- and chronostratigraphy of the Lateglacial in the Eifel regionGermany Quat Int 61 516
Litt T Brauer A Goslar T Merkt J Balaga K Muller H Ralska-Jasiewiczowa MStebich M amp Negendank J F W 2001 Correlation and synchronisation of Lateglacialcontinental sequences in northern Central Europe based on annually laminated lacustrinesediments Quat Sci Rev 20 12331249
Long D amp Morton A C 1987 An ash fall within the Loch Lomond stadial J Quat Sci 297101
Lotter A F Eicher U Siegenthaler U amp Birks H J B 1992 Lateglacial climatic oscillationsas recorded in Swiss lake sediments J Quat Sci 7 187204
Lowe J J 1992 Lateglacial and Early Holocene lake sediments from the Northern ApenninesItaly|pollen stratigraphy and radiocarbon dating Boreas 21 193208
Lowe J J 2001 Abrupt climatic changes in Europe during the last glacialinterglacial tran-sition the potential for testing hypotheses on the synchroneity of climatic events usingtephrochronology Global Planet Change 603 7384
Lowe J J amp Turney C S M 1997 Vedde Ash layer discovered in a small lake basin on theScottish mainland J Geol Soc Lond 154 605612
Lowe J J amp Walker M J C 2000 Radiocarbon dating the last glacialinterglacial transition(ca 14914 C ka BP) in terrestrial and marine records the need for new quality assuranceprotocols Radiocarbon 42 5368
Lowe J J amp Watson C 1993 Lateglacial and Early Holocene pollen stratigraphy of the northernApennines Italy Quat Sci Rev 12 727738
Lowe J J Birks H H Brooks S J Coope G R Harkness D D Mayle F E SheldrickC Turney C S M amp Walker M J C 1999 The chronology of palaeoenvironmental changesduring the Last GlacialHolocene transition towards an event stratigraphy for the BritishIsles J Geol Soc Lond 156 397410
Lowe J J Hoek W Z amp INTIMATE group 2001 Inter-regional correlation of palaeoclimaticrecords for the Last GlacialInterglacial transition a protocol for improved precision recom-mended by the INTIMATE project group Quat Sci Rev 20 11751187
Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
Mangerud J Lie S E Furnes H Kristiansen I L amp Liquest mo L 1984 A Younger Dryas ashbed in western Norway and its possible correlation with tephra beds from the Norwegian Seaand North Atlantic Quat Res 21 85104
Mangerud J Furnes H amp Jparaohansen J 1986 A 9000 year-old ash bed on the Faroe IslandsQuat Res 26 262265
Martini J 1970 Recherche de retombparaees volcaniques dans le sud-est de la France et la Suisseoccidentale Arch Sci 23 641674
Martini J amp Duret J J 1965 Note preliminaire sur la presence drsquo un niveau de cendres vol-caniques dans des sparaediments post-glaciaires des environs de Genmicroeve Arch Sci 18 587588
Mayewski P A Meeker L D Twickler M S Whitlow S Yang Q Lyons W B amp Pren-tice M 1997 Major features and forcing of high latitudes Northern Hemisphere atmosphericcirculation using a 110 000 year long glaciochemical series J Geophys Res 102 345365
Merkt J Muller H Knabe W Muller P amp Weiser T 1993 The Early Holocene Saksunarvatntephra found in lake sediments in NW Germany Boreas 22 93100
Narcisi B 1993 Segnalazione di un livello piroclastico di provenienza etnea nellrsquo area del Fucino(Italia Centrale) Quaternario 6 8792
Narcisi B 1996 Tephrochronology of a Late Quaternary lacustrine record from the Monticchiomaar (Vulture volcano southern Italy) Quat Sci Rev 15 155165
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
800 S M Davies and others
Newton A J amp Dugmore A J 1993 Tephrochronology of Core C from Lago Grande di Mon-ticchio In Paleolimnology of European Maar Lakes (ed J F W Negendank amp B Zolitschka)Lecture Notes in Earth Science vol 49 333348 Springer
Oldmacreld F Appleby P G amp Thompson R 1980 Palaeoecological studies of lakes in theHighlands of Papua New Guinea J Ecol 68 457477
Orsi G Drsquo Antonio M de Vita S amp Gallo G 1992 The Neapolitan Yellow Tureg a large mag-nitude trachytic phreatoplinian eruption eruptive dynamics magma withdrawal and calderacollapse J Volcanol Geotherm Res 53 275287
Paterne M Guichard F Labeyrie J Gillot P Y amp Duplessy J C 1986 Tyrrhenian Seatephrochronology of the oxygen isotope record for the past 60 000 years Mar Geol 72259285
Paterne M Guichard F amp Labeyrie J 1988 Explosive activity of the south Italian volca-noes during the past 80 000 years as determined by marine tephrochronology J VolcanolGeotherm Res 34 153172
Paterne M Labeyrie J Guichard F Mazaud A amp Maitre F 1990 Fluctuations of the Cam-panian explosive volcanic activity (south Italy) during the past 190 000 years as determinedby marine tephrochronology Earth Planet Sci Lett 98 166174
Pawse A Beske-Diehl S amp Marshall S A 1998 Use of magnetic hysteresis properties andelectron spin resonance spectroscopy for the identimacrcation of volcanic ash a preliminary studyGeophys J Int 132 712720
Pearce N J G Westgate J A amp Perkins W T 1996 Developments in the analysis of singleglass shards in volcanic deposits by laser ablation ICP-MS quantitative and single internalstandard multi-element methods Quat Int 3436 213227
Pearce N J G Westgate J A Perkins W T Eastwood W J amp Shane P 1999 Theapplication of laser ablation ICP-MS to the analysis of volcanic glass shards from tephradeposits bulk glass and single shard analysis Global Planet Change 21 151171
Pilcher J R amp Hall V A 1992 Towards a tephrochronology for the Holocene of the north ofIreland Holocene 2 255259
Ponel P amp Lowe J J 1992 Coleopteran pollen and radiocarbon evidence from the Prato Spillarsquo Drsquo succession N Italy C R Acad Sci Paris Sparaer II 315 14251431
Rose N L Golding P N E amp Battarbee R W 1996 Selective concentration and enumerationof tephra shards from lake sediment cores Holocene 6 243246
Ruddiman W F amp Glover L K 1972 Vertical mixing of ice rafted volcanic ash in NorthAtlantic sediments Geol Soc Am Bull 83 28172836
Ruddiman W amp McIntyre A 1981 The North Atlantic Ocean during the last deglaciationPalaeogeogr Palaeoclimatol Palaeoecol 35 145214
Santacroce R 1987 Somma Vesuvius Quad Ric Sci 114 252
Sarna-Wojcicki A 2000 Tephrochronology In Quaternary geochronology methods and applica-tions (ed J S Noller J M Sowers amp W R Lettis) AGU Reference shelf vol 4 pp 357377Washington DC American Geophysical Union
Sejrup H P Sjiquest holm J Furnes H Beyer I Eide L Jansen E amp Mangerud J 1989Quaternary tephrochronology on the Iceland Plateau north of Iceland J Quat Sci 4 109114
Sikes E L Samson C R Guilderson T P amp Howard W R 2000 Old radiocarbon agesin the southwest Pacimacrc Ocean during the last glacial period and deglaciation Nature 405555558
Stein R Nam S-I Grobe H amp Hubbersten H 1996 Late Quaternary glacial history andshort term ice rafted debris deg uctuations along the East Greenland continental marine In LateQuaternary palaeoceanography of the North Atlantic margins (ed J T Andrews W E NAustin H Bergsten amp A E Jennings) pp 135151 Geological Society London SpecialPublication
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 801
Stuiver M amp Grootes P M 2000 GISP2 oxygen isotope ratios Quat Res 53 277284
Stuiver M Reimer P J Bard E Beck J W Burr G S Hughen K A Kromer BMcCormac G Van der Plicht J amp Spurk M 1998 INTCAL 98 radiocarbon age calibration24 0000 cal BP Radiocarbon 40 10411083
Sweatman T R amp Long J V P 1969 Quantitative electron microprobe analysis of rock formingminerals J Petrol 7 332379
Turney C S M 1998 Extraction of rhyolitic ash from minerogenic lake sediments J Paleolim-nol 19 199206
Turney C S M amp Lowe J J 2001 Tephrochronology In Tracking environmental changes inlake sediments physical and chemical techniques (ed W M Last amp J P Smol) DordrechtKluwer Academic
Turney C S M Harkness D D amp Lowe J J 1997 The use of microtephra horizons tocorrelate Lateglacial lake sediments successions in Scotland J Quat Sci 12 525531
Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
van den Bogaard P amp Schmincke H 1985 A widespread isochronous Late Quaternary tephralayer in central and northern Europe Geol Soc Am Bull 96 15541571
van den Bogaard B Dordeg er W Sandgren P amp Schmincke H-U 1994 Correlating theHolocene records Icelandic tephra found in Schleswig-Holstein (northern Germany) Natur-wissenschaften 81 554556
Vernet G amp Raynal J-P 2001 Tephrostratigraphy of the Limagne revisited Implications forLateglacial and Holocene Prehistory In Tephras chronology archaeology (ed E Juvignparae ampJ-P Raynal) pp 111116 Dossiers de lrsquo ArchparaeoLogis no 1 France
Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
Vezzoli L 1991 Tephra layers in Bannock Basin (eastern Mediterranean) Mar Geol 1002134
von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
Walker M J C Bjorck S Lowe J J Cwynar L C Johnsen S Knudsen K-L WohlfarthB amp INTIMATE Group 1999 Isotopic events in the GRIP ice core a stratotype for the LatePleistocene Quat Sci Rev 18 11431150
Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
802 S M Davies and others
Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
772 S M Davies and others
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le1
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t)
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rve
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200
700
210
485
969
9
100
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300
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0
100
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(02
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(04
6)
(03
3)
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4)
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5)
(06
1)
(08
)(0
46)
un
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own
12
820
sect60
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(16684
m)
Ref
eren
ces
1
this
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dy
2
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rne
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3
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isi
(1996)
4
All
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al
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5
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dro
nic
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al
(1995)
6
Ju
vig
nparae
et
al
(1996)
7
Bir
ks
et
al
(1996)
8
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rck
ampW
ast
egordma
rd(1
999)
9
Du
gm
ore
ampN
ewto
n(1
998)
10
Bjo
rck
et
al
(1992)
11
Kva
mm
eet
al
(1989)
12
Zoli
tsch
ka
etal
(1995)
13
Ju
vig
nparae
ampG
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t(1
987)
14
Di
Vit
oet
al
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15
Del
ibri
as
etal
(1979)
16
Ju
vig
nparae
etal
(1987)
17
Dav
ies
et
al
(2001)
18
van
den
Bogaard
ampS
chm
inck
e(1
985)
19
Fri
edri
chet
al
(1999)
20
Bra
uer
eta
l(1
999)
21
Etl
ich
eret
al
(1987)
22
Tu
rney
etal
(1997)
23
Pate
rne
et
al
(1986)
24
Kel
ler
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25
Eir
parasup3kss
on
etal
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26
Hadeg
idaso
net
al
(2000)
27
Ale
ssio
etal
(1976)
28
Vez
zoli
(1991)
29
San
tacr
oce
(1987)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 773
Tab
le1
(Con
t)
GR
IPage
tep
hra
age
(ss0
8c
volc
an
ich
ori
zon
(14C
yrs
)ti
me-
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)n
SiO
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tal
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MA
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rce
ref
La
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ca11
400
12
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922
9160
470
002
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744
538
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La
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6
21
(MC
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Nea
poli
tan
ca12
000
17
588
104
2177
631
901
006
525
940
686
9
962
8W
DS
Cam
pi
1Y
ello
w(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(0
78)
Fle
gre
i
Tu
reg(I
T)
568
106
0194
448
7
17
451
938
75
5
100
ED
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596
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9192
940
3
06
435
034
588
9
100
ED
S2
14
619
403
1196
329
9
02
019
943
485
7
100
ED
S
Borr
ob
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ca12
300
18
733
601
1122
914
700
601
207
635
837
6
955
1W
DS
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la22
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(00
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(01
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(00
9)
(00
2)
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2)
(00
3)
(01
4)
(00
9)
(0
47)
un
kn
ow
n14
650
sect200
(Ca
pea
k)
(17458
m)
un
kn
ow
n14
650
sect200
(C
ap
eak)
(17506
m)
E-2
P
oll
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ca13
000
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302
7138
810
8
01
015
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7
100
ED
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eren
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nic
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6
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vig
nparae
et
al
(1996)
7
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et
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8
Bjo
rck
ampW
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n(1
998)
10
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rck
et
al
(1992)
11
Kva
mm
eet
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12
Zoli
tsch
ka
etal
(1995)
13
Ju
vig
nparae
ampG
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t(1
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14
Di
Vit
oet
al
(1999)
15
Del
ibri
as
etal
(1979)
16
Ju
vig
nparae
etal
(1987)
17
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et
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(2001)
18
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den
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ampS
chm
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19
Fri
edri
chet
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(1999)
20
Bra
uer
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l(1
999)
21
Etl
ich
eret
al
(1987)
22
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rney
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(1997)
23
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rne
et
al
(1986)
24
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ler
(1980)
25
Eir
parasup3kss
on
etal
(2000)
26
Hadeg
idaso
net
al
(2000)
27
Ale
ssio
etal
(1976)
28
Vez
zoli
(1991)
29
San
tacr
oce
(1987)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
774 S M Davies and others
Tab
le1
(Con
t)
(Th
evarv
eage
for
the
Gre
enis
h(I
T)rsquo
row
is17
560
yea
rs)
GR
IPage
tep
hra
age
(ss0
8c
volc
an
ich
ori
zon
(14C
yrs
)ti
me-
scale
)n
SiO
2T
iO2
Al 2
O3
FeO
Mn
OM
gO
CaO
Na
2O
K2O
P2O
5to
tal
EP
MA
sou
rce
ref
GS
-2B
AS
-213
400
6497
933
2122
4147
902
445
389
829
905
205
4979
4W
DS
26
(IC
)
GS
-2B
AS
-313
400
2538
529
9125
7131
203
132
174
729
507
707
7980
1W
DS
26
(IC
)
GS
-2B
AS
-414
000
7503
617
4145
1113
202
155
3100
528
010
5
975
7W
DS
26
(IC
)
Un
ita
dei
ca14
000
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804
7184
625
901
602
217
432
679
302
8100
ED
SP
hle
gre
an
3
27
Tef
ra(0
53
)(0
13
)(0
25)
(07
4)
(01
4)
(01
6)
(01
6)
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4)
(06
6)
(01
6)
Fie
lds
Su
per
iori
(IT
)
Y-1
(IT
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14
000
16
600
413
7169
555
502
218
242
262
229
306
8100
ED
SE
tna
28
Bla
ck17
000
sect300
Fea
ther
(17890
m)
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enis
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15
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(IC
)
Ref
eren
ces
1
this
stu
dy
2
Pate
rne
etal
(1988)
3
Narc
isi
(1996)
4
All
enet
al
(1999)
5
An
dro
nic
oet
al
(1995)
6
Ju
vig
nparae
et
al
(1996)
7
Bir
ks
et
al
(1996)
8
Bjo
rck
ampW
ast
egordma
rd(1
999)
9
Du
gm
ore
ampN
ewto
n(1
998)
10
Bjo
rck
et
al
(1992)
11
Kva
mm
eet
al
(1989)
12
Zoli
tsch
ka
etal
(1995)
13
Ju
vig
nparae
ampG
ewel
t(1
987)
14
Di
Vit
oet
al
(1999)
15
Del
ibri
as
etal
(1979)
16
Ju
vig
nparae
etal
(1987)
17
Dav
ies
et
al
(2001)
18
van
den
Bogaard
ampS
chm
inck
e(1
985)
19
Fri
edri
chet
al
(1999)
20
Bra
uer
eta
l(1
999)
21
Etl
ich
eret
al
(1987)
22
Tu
rney
etal
(1997)
23
Pate
rne
et
al
(1986)
24
Kel
ler
(1980)
25
Eir
parasup3kss
on
etal
(2000)
26
Hadeg
idaso
net
al
(2000)
27
Ale
ssio
etal
(1976)
28
Vez
zoli
(1991)
29
San
tacr
oce
(1987)
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European tephrochronological framework for Termination 1 775
Altogether 34 tephra layers have been reported from sediment sequences in Europeand the NE Atlantic region which date to the period between 185 and 80 14C ka BP(table 1) Because tephra layers are deposited virtually instantaneously (in geologicalterms) they enotectively represent time-parallel marker horizons within stratigraphicalsequences (Westgate amp Gorton 1981 Sarna-Wojcicki 2000 Turney amp Lowe 2001) Intheory therefore all 34 tephras could prove valuable for correlation purposes eitherin a local context or in those cases where the ash deposits have been widely dispersedbetween regional sequences In practice however very little is known about the fullgeographical dispersal of the majority of the ash layers listed in table 1 Furthermorecorrelation by tephrostratigraphy will only work if the various ash layers have wellcharacterized geochemical signatures While some geochemical data are available forthe majority of the tephras listed in table 1 the collective data are far from robustand no geochemical data have yet been published for some
Nonetheless there is mounting evidence to show that some of the tephra depositslisted in table 1 are not only geochemically distinct but are also much more widelydispersed across Europe than was initially realized Stratigraphic records of thebetter-known tephras were initially limited to observations of visible tephra layersThe development of a technique that enables detection of tephra layers that are invis-ible to the naked eye (micro-tephra) in Late Glacial sequences has greatly extendedthe area over which some of the ashes can be traced (Lowe amp Turney 1997 Turneyet al 1997 Turney 1998 Wastegard et al 1998 2000a b) Most of this research sofar has focused on micro-tephra layers originating from Icelandic centres distributedthroughout northern Europe Here we report on further development of this line ofresearch with new evidence for the occurrence of micro-tephra layers in a site insouthern Europe The results suggest that there is great potential for tracing someash layers that originated from Italian volcanic complexes over much larger tracts ofsouthern and central Europe than records of visible tephra deposits allow This inturn greatly enhances the scope for making precise correlations not only betweenparts of southern Europe but also between continental and marine (MediterraneanSea) sequences
2 Micro-tephra extraction techniques
Micro-tephra horizons are composed of glass shards that are generally between 80and 24 m m (long axis) in size and that are present in such low concentration insedimentary sequences that they can only be detected by the use of a particle sep-aration technique Several factors inreguence the concentration of shards such as dis-tance from the volcanic source precipitation patterns during the eruption and sub-sequent tephra dispersal and sedimentary processes within the catchment In someterrestrial sequences micro-tephra horizons with a peak concentration (peak con-centration tends to coincide with the shy rst occurrence of glass shards in a sedimentsequence which is then taken to mark the time of maximum ash deposition) as lowas 10 shards cmiexcl3 has been conshy rmed whereas other sites have recorded as muchas 8000 shards cmiexcl3 (Turney et al 1997) In complete contrast tephra horizons inthe GRIP ice core have been identishy ed based on a single glass shard only (Gronvoldet al 1995)
Enotective separation techniques for the detection and isolation of tephra particlesfrom sedimentary sequences have been developed These include ashing of organic
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matter (Pilcher amp Hall 1992) digestion of biogenic and opaline silica (Rose et al 1996) the use of magnetic properties of ash layers (see for example Oldshy eld et al 1980 van den Bogaard et al 1994 Pawse et al 1998) X-ray analysis (Dugmore ampNewton 1992) and a density separation (regotation) technique (Turney 1998) Den-sity separation has proved exceedingly useful for the detection of small glass shardspresent in low concentrations in mineral-rich Late Glacial sediments This involvesthe separation and concentration of particles of predetermined specishy c gravity withthe use of a heavy liquid and subsequent identishy cation of glass shards with the useof a polarizing light microscope (for further details see Turney (1998)) This methodhas been particularly successful in the detection of tephras of rhyolitic compositionthat have a specishy c density of 2325 g cmiexcl3 (Lowe amp Turney 1997 Turney et al 1997 2001 Turney 1998 Wastegard et al 1998 2000a b) It is this technique thathas resulted in the wider recognition of micro-tephras in Europe as discussed below
3 Geochemical ` ngerprintingrsquo of tephra layers
The 34 tephras listed in table 1 have originated from four major volcanic complexesIceland the Massif Central in central France the Eifel district near Bonn and threevolcanic centres in Italy (the Campanian group Etna and the Aeolian Islands (seeshy gure 2)) An important matter to resolve is the extent to which the various magmasand ashes generated by these volcanic complexes can be geochemically shy ngerprintedThis is especially important in the case of tephras which have originated from thesame volcanic centre in which there may have been limited geochemical evolution ofmagmas over time In this section we summarize the approach generally adopted todetermine the geochemical character of visible and micro-tephras as background tothe geochemical data summarized in table 1 In the subsequent section of the paperwe review the present state of knowledge concerning all 34 tephras listed in table 1
Glass shards formed during the rapid cooling of magma are thought to have acomposition that is representative of the bulk geochemistry of the magma (Barker1983) hence widely dispersed glass particles are regarded as the most appropriateconstituents of pyroclastic material for geochemical analysis If a tephra deposit canbe shown to have a distinct geochemical signature then it can be used to correlatethe stratigraphic units in which it occurs (tephrostratigraphy) as well as to datethese units (tephrochronology) if the ages of the tephras are known (Westgate ampGorton 1981) A key element of building a tephrostratigraphical framework there-fore is to establish as rigorously as possible the geochemical composition of theindividual tephras used in its construction Robust and directly comparable geo-chemical datasets are dimacr cult to assemble for glass however because it is highlyunstable material particularly prone to sodium mobilization
The technique most widely employed to establish the geochemical signature of atephra is electron probe micro-analysis (EPMA) This enables grain-discrete determi-nations of the major elements within an individual glass shard which is of particularbeneshy t in the analysis of micro-tephra layers which generally contain glass particlesin low concentration The glass surface is bombarded with an electron beam and theX-ray energy produced is unique to each element while the intensity of the signalemitted is proportional to the amount of that element in the glass shard (Hunt amp Hill1993) Measurement can be by either energy dispersive spectrometry (EDS) or wave-length dispersive spectrometry (WDS) EDS has a lower precision mainly because
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European tephrochronological framework for Termination 1 777
N
0 500 km
Confirmed records of Vedde Ash (visible occurrences)
New records of Vedde Ash from flotation method
Extended area of Vedde Ash detection (micro-tephra)
Known area of Laacher See Tephra (visible occurrences)
Confirmed records of Neapolitan Yellow Tuff (visible occurrences)
New record of Neapolitan Yellow Tuff from flotation method
Known area of Neapolitan Yellow Tuff
Volcanic centres of particular relevance to this study
Other major volcanic centres in Europe
Figure 2 Location of the principal volcanic centres that were active during Termination 1 andthe Early Holocene The known distribution of the Vedde Ash (VA) Laacher See (LST) andNeapolitan Yellow Tureg (NYT) are shown
the behaviour of each element cannot be monitored independently during measure-ment and so this approach fails to detect for example any signishy cant mobilizationof sodium during the bombardment process (Hunt amp Hill 1993) Although WDSrequires a higher beam current and a longer counting time than EDS the formeronoters the distinct advantage of sequential acquisition of elemental data so that thedegree of sodium loss can be tracked The morphology of individual glass shards canalso distort EDS data a problem that is reduced when using WDS because for thisprocedure glass shards are mounted in an epoxy resin and polished to provide aregat surface for analysis Hence data should always be obtained using WDS whereverpossible
Even when WDS is used as a common tool for determining the geochemical spectraof samples aberrant results can arise that inreguence data comparisons For examplesome glass shards may contain tiny crystalline inclusions of feldspar and these shouldbe avoided when selecting surface points for analysis (Hunt amp Hill 2001) Hunt amp Hill
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6
4
2
40 50 60 70 80
K2O
(
)
SiO2 ()
Laacher See
Iceland
Veidivoumltn-Dyngjufjoumlll
Katla (basalt)
Grimsvoumltn-Kverkfjoumlll
Hekla
Katla (rhyolitic)
0
Icelandic volcanic centres8
10
Massif Central
Etna
Campanian
Figure 3 Bi-plot of SiO2 and K2 O concentrations in tephras derived from the main Europeanash provinces (modimacred after Mangerud et al 1984) The Campanian Massif Central and Etnaconcentrations are based on the data presented in table 1
(2001) have concluded that small variations in the laboratory procedures employedto determine glass chemistry can lead to misidentishy cation of sources for glass shardsand give an example of shards with a Jan Mayen provenance wrongly attributedto an Icelandic source Clearly there is a need for standardization of laboratoryprocedures and while a number of recommendations have recently been advocated(Froggatt 1992 Hunt amp Hill 1993 Hunt et al 1998) there is still some variation inlaboratory and operator practice (Hunt amp Hill 1996) Standardization is also requiredin the form in which results are presented to ensure comparability Normalizationof the data to 100 a practice employed by some researchers can obscure poorresults and hence lead to incorrect comparisons (Hunt amp Hill 1993) However othersargue that it may actually facilitate comparisons between samples by removing thedistorting enotects of the water component contained in glass shards (see for exampleFroggatt 1992) The majority of the published Italian and some of the Eifel datahave been normalized while those from other parts of Europe have not and hencedata comparisons are not always straightforward
Table 1 provides mean values and standard deviations for major oxide concentra-tions obtained from those tephras for which data are presently available The tableincludes previously unpublished WDS results for the Neapolitan Yellow Tunot (NYTdiscussed in x 4 below) and for the Mercato Tephra While individual tephra layersmay be geochemically distinct the geochemical envelopes representing the collectivedata obtained from all of the tephras assigned to each major volcanic province showsignishy cant overlaps as is illustrated in the bi-plots and ternary plots (shy gures 3 and 4)of selected oxide concentration data It is clear therefore that measurement of majoroxide concentrations does not satisfactorily discriminate between some tephras orig-inating from dinoterent volcanic centres (as noted by van den Bogaard amp Schmincke(1985) and Frezzotti amp Narcisi (1996) with respect to Eifel and Italian tephras)nor of tephras of dinoterent age originating from the same volcanic centre (Bond et
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European tephrochronological framework for Termination 1 779
40 50 60 70 80
K2O
(
)
SiO2 ()
shyshyshyshy
shy
shyshy
shyshyshy
shy
shy
shy
shy
reg
reg regreg
regregregregreg regregregregreg
FF
F
ll
l
l
4 8 12 16
reg
regreg
regreg
regregreg
regreg
regregreg
shy
F
l shyshyshyshyshy shyshyshyshyshyshy
F
F
l
ll
FeO ()
TiO
2 (
)
reg
l
Iceland
Eifel
F
shy ItalyMassif Central
100
80
60
40
20
100
80
60
40
20
100 80 60 40 20
CaO
FeO
K2O
regregreg
reg
reg
reg
reg
reg
reg
regregreg
shyF
F
F
regreg
l
lllshy
shyshyshy
shyshyshy
l
0
2
4
6
8
10
0
1
2
3
4
5
regreg
regreg
regreg
regreg
regreg
reg
reg
regreg
l
l
ll
shy
shyshy
shyshy
shy
shyshy
FF
F
100
80
60
40
20
100
80
60
40
20
100 80 60 40 20
K2ONa2O
CaO
(c) (d)
(a)
(b)
Figure 4 Plots of selected geochemical data obtained from tephras of Termination 1 age (seetable 1) (a) Bi-plot of mean SiO2 and K2 O values (b) Bi-plot of mean FeO and TiO2 values(c) Ternary plot indicating variations in the proportions of FeO CaO and K2 O (d) Ternaryplot indicating variations in the proportion of CaO Na2 O and K2 O
al 2001) Individual tephra layers are presently assigned to a particular volcanicevent on the basis of a combination of criteria usually including examination of thephysical properties (eg refractive index and surface detail of the glass shards) thestratigraphic position of the layer and independent assessment of the age of the layeras well as any geochemical data that may be available The construction of a tephro-stratigraphical scheme would clearly beneshy t from the application of a more diagnostic
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geochemical tool One approach that has promise is the analysis of trace and rareearth elements using an ultraviolet laser ablation inductively coupled plasma massspectrometer (UV-LA-ICP-MS) (Pearce et al 1996 1999 Eastwood et al 1999)This approach has been applied successfully to analysis of tephras of Mid-Holoceneage but not yet to tephras that fall within the period of interest here
4 Tephra layers in Europe and the North Atlantic regiondated to between 185 and 80 14C ka
(a) Icelandic province
The Icelandic volcanic systems are divided into three main groups based on theirgeochemical characteristics tholeiitic basalts transitional alkali basalts and alkaliolivine basalts (Jakobsson 1979) Collectively magmas from the Icelandic provincespan a wide geochemical spectrum although individual volcanic centres have tightgeochemical distributions (shy gure 3) for four of the main centres Grimsvotn-Kverfjolland Veidvotn-Dyngjufoll which form part of the northern (tholeiitic) volcanic zoneand Hekla and Katla which fall within the eastern (alkali olivine basalt and transi-tional alkali basalt) volcanic zone (Haregidason et al 2000) These appear to be thekey centres for the tephras listed in table 1 that have been assigned an Icelandicorigin
One of the best-known and most widely dispersed tephra horizons in northernEurope that has an Icelandic origin is the Vedde Ash (VA) which was depositedca 103 14C ka BP (Birks et al 1996 Wastegard et al 1998) within the GS-1Younger Dryas chronozone This ash is believed to originate from the Katla complexwithin the transitional alkali basalt province (Mangerud et al 1984 Lacasse et al 1995) in the south of the island The ash has a bimodal geochemical composition (rhy-olitic and basaltic) which is thought to reregect derivation from two separate magmachambers Studies of recent volcanic events in Iceland have shown that the mostexplosive eruptions generating the largest amounts of tephra occur in this tran-sitional alkali basalt province (Haregidason et al 2000) It is also believed that thewidespread distribution of this ash was caused by the development of co-ignimbriteash plumes during an ignimbrite-forming eruption (Lacasse et al 1995)
Layers of VA that are visible to the naked eye have been found in lake sediments inwestern Norway (Mangerud et al 1984) and the Inner Hebrides Scotland (Davies etal 2001) and in marine cores throughout the NE Atlantic (see for example Kvammeet al 1989 Lacasse et al 1995) in the northern North Sea (Long amp Morton 1987)on the Iceland plateau (Ruddiman amp McIntyre 1981 Sejrup et al 1989) and on theeast Greenland continental margin (Stein et al 1996) The distribution of the VAin North Atlantic marine sequences is characterized by an arcuate lobe extendingsouthwest from the Denmark Strait and curving eastwards to mid-latitudes in theNorth Atlantic (Lacasse et al 1995) This strongly suggests deposition from raftedice which was displaced to the southwest and south in a circulating counterclockwisegyre (Ruddiman amp Glover 1972) This may well reregect Katlarsquos close proximity tothe southern coast of Iceland with the Vedde tephra being deposited on ice thatcalved directly into the North Atlantic (Haregidason et al 2000) However depositionvia the atmosphere almost certainly took place as well as is indicated by the recentdiscoveries of rhyolitic VA in micro-tephra form in several sites in Scotland (Turneyet al 1997) southern Sweden (Wastegard et al 1998 2000a) and western Russia
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(Wastegard et al 2000b) A more recent discovery of a relatively high concentrationof rhyolitic VA glass shards in the northern Netherlands indicates that the ash maywell have been dispersed much further south than previously thought (S M Davies2002 unpublished work) Finally glass shards assigned to the VA have also beendiscovered in the GRIP ice core and dated to 11 980 sect 80 GRIP yr BP (Gronvold etal 1995) This discovery is extremely important for it indicates that the VA maywell provide a reliable time-parallel marker horizon between ice-core marine andterrestrial records
Two other important Icelandic ash layers the Borrobol and Saksunarvatn Tephraswere deposited near the beginning and end of the Last TerminationEarly Holoceneinterval respectively The Borrobol Tephra was discovered for the shy rst time in lakesediments in several sites in Scotland and as yet is known only in micro-tephra formIt has been dated in Scottish sites to ca 123 14C ka BP (Turney et al 1997) Whatis thought to be a contemporaneous tephra has been detected in marine sedimentson the North Icelandic shelf (Eirplusmn ksson et al 2000) This certainly has a very similargeochemical composition to those reported from Scotland but the horizon in whichit was discovered on the North Iceland plateau has been dated to 134 14C ka Theage discrepancy between the Scottish and Icelandic Borrobol Tephra layers may wellreregect the inreguence of a marine reservoir error although the possibility that severaltephras with similar geochemical composition were erupted over a period exceeding1000 yr cannot be ruled out (Larsen 2000)
The Saksunarvatn Ash appears to have been one of the largest Holocene eruptionsin Iceland It has a tholeiitic basaltic composition which is considered to indicate anorigin in the Grimsvotn or Kverfjoll complex (shy gure 3) (Mangerud et al 1986) Layersof this ash have been identishy ed in sites on the Faroe Islands (Mangerud et al 1986Dugmore amp Newton 1998 Wastegard et al 2001) the Shetland Isles (Bennet et al 1992) northern Germany (Merkt et al 1993) western Norway (micro-tephra) (Birkset al 1996) and in the GRIP (Gronvold et al 1995) and NordGRIP ice cores (S MDavies 2002 unpublished work) It has been dated to between 9060 and 8930 14C kaBP (Birks et al 1996) in Norway and to ca 10 240 sect 30 GRIP yr BP in the GRIPice core (Gronvold et al 1995) The Saksunarvatn Ash may thus provide a secondimportant widespread time-parallel marker between ice-core marine and terrestrialrecords
Other Icelandic tephras of rhyolitic amacr nity are less well known in terms of theirdistribution and geochemical variation The Hogstorpsmossen Tephra reported fromSweden (Bjorck amp Wastegard 1999) and the L3754 tephra discovered in the FaroeIslands (Dugmore amp Newton 1998) are known from single sites only and so theirpotential for tephrostratigraphy is uncertain at present Furthermore the geochem-ical spectrum of the Hogstorpsmossen Tephra is based on a small dataset with lowanalytical totals
A number of tephras of basaltic composition have originated from Iceland buttheir distributions are largely conshy ned to Iceland or to marine cores collected fromclose to the Iceland coast or in the North Atlantic These include the tephras listedas 1-THOL-1 1-THOL-2 KOL-GS-2 GS-2BAS-1 GS-2BAS-2 GS-2BAS-3 andGS-2BAS-4 in table 1 (Kvamme et al 1989 Bjorck et al 1992 Eirplusmn ksson et al 2000 Haregidason et al 2000) The shy rst two in this list are tholeiitic basaltic tephrasassociated with the VA in a complex series of tephras collectively termed NorthAtlantic Ash Zone 1 (NAAZ1) which has been detected in numerous marine cores
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from the North Atlantic Initially thought to represent a single eruption analysisof high-resolution sediment sequences from Lake Torfadalsvatn in northern Iceland(Bjorck et al 1992) the Hebridean Shelf near NW Scotland (Austin amp Kroon 1996)the St Kilda Basin (Hunt et al 1995) and the open North Atlantic (Bond et al 2001)has demonstrated that NAAZ1 comprises a series of distinct ashes that probablyreregect separate eruption events 1-THOL-1 is thought to originate from Veidivotn(shy gure 3) while Grimsvotn may have been the source of 1-THOL-2 (Kvamme et al 1989)
KOL-GS-2 is also of tholeiitic basaltic composition but is thought to originatefrom the Kolbeinsey Ridge system (Eirplusmn ksson et al 2000) To date this tephra hasbeen detected in one marine core only within the same record on the North Ice-landic shelf as that from which the correlative of the Borrobol Tephra was alsoreported (Eirplusmn ksson et al 2000) GS-2BAS-1 to GS-2BAS-4 are of uncertain ori-gin but are thought to have been deposited at roughly the same time as KOL-GS-2(ca 134 14C ka BP (Haregidason et al 2000))
The limited distribution of these basaltic tephras a feature that is not unique toIcelandic basaltic material may reregect two factors the relative magnitude of the vol-canic eruptions from which they were derived and the limited aerial transportationof basaltic glass which is denser than rhyolitic material However a rather surpris-ing recent discovery is that of visible basaltic VA in a site on the Isle of Skye inthe Inner Hebrides Scotland (shy gure 5) (Davies et al 2001) All other occurrencesof VA in Scotland are exclusively of rhyolitic material and in micro-tephra formonly (Turney et al 1997 Turney 1998) Clearly basaltic tephra must have beentransported subaerially as far south as Skye and the reason why it has not beendetected at other sites in Scotland is puzzling We suspect that this partly reregectsthe laboratory methods employed to separate glass shards present in low concentra-tion within a micro-tephra layer from the host sediment The technique used is adensity-separation (regotation) procedure (Turney 1998) and as basaltic shards havea specishy c density similar to quartz one of the most abundant minerals in lake sedi-ments of Late Glacial age basaltic material is dimacr cult to detect using this methodThis hypothesis is currently under investigation and alternative detection methodsare being explored including magnetic separation (Mackie et al 2002)
Several other events listed in table 1 that are of probable Icelandic origin includetephras recorded in the GRIP ice core including visible (eg the `Black Featherrsquo)tephras as well as uncertain tephras inferred from distinct Ca peaks (S Johnsen2001 personal communication) No glass shards have yet been detected in the latterbut a volcanic origin is assumed because high Ca peaks are associated with knowntephras in other Greenland ice cores (S Johnsen 2001 personal communication)These are referred to as `unknownrsquo in table 1 No geochemical analyses are availablefrom these horizons so their origin must remain speculative but a possible source isIceland in view of its proximity to the Greenland ice sheet and assumed atmosphericcirculation patterns
(b) Eifel province
There are two prominent tephra events dated to the Termination 1Early Holocenetime-span that originated from the Eifel province the Laacher See Tephra (LST)and the Ulmener Maar Tephra (UMT) Visible occurrences of the LST indicate that
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Vedde Ash
615 625 635 645 655depth (cm)
organic lake mudsHolocene
silty clayGS-1Younger Dryas
organic lake mudsGI-1Alleroslashd
100 microm
(a)
(b)
Figure 5 (a) Photograph of the visible VA layer discovered at Loch Ashik Isle of Skye InnerHebrides Scotland (b) Light microscope photograph showing the rich content of basaltic shards(examples are indicated by the arrows) within this layer (8024 m m size fraction)
this ash was dispersed over much of central Europe (van den Bogaard amp Schmincke1985 Friedrich et al 1999 Litt amp Stebich 1999) The LST is dated by radiocarbonto ca 110 14C ka BP (van den Bogaard amp Schmincke 1985) and to 11 063sect12 14C BP(Friedrich et al 1999) by varve chronology to 1288 varve ka BP (Brauer et al 1999Litt et al 2001) and by ArAr dating to 129 ka cal BP (van den Bogaard 1995) Ithas a phonolitic composition and is thought to have originated from a plinian andphreatomagmatic eruption with the distal ash being carried in three distinct plumesone to the northeast towards Poland one to the west and the third to the southcovering the Jura Mountains and north Italy (van den Bogaard amp Schmincke 1985Juvigne et al 1995 Bossuet et al 1997) This pattern is thought to reregect altitu-dinal variations in the predominant wind direction Sedimentary sequences near thevolcanic source indicate that the LST consists of three main layers which represent
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dinoterent eruption phases These are grouped together as the Laacher See TephraFormation but the three individual units can be traced within and between a seriesof depositional fans The geochemical data obtained from these three LST layersshow signishy cant variations as reregected in the ternary plots (shy gure 4)
The Early Holocene Ulmener Maar Tephra (UMT) is of rhyolitic composition andappears to be restricted to sites in Germany though this conclusion is also based onrecords of visible tephras only It is dated to ca 956 14C ka BP and to 110 varve ka(Zolitschka et al 1995 Litt et al 2001)
(c) Massif Central province
The Massif Central tephras are mainly of basaltic trachyandesitic compositionwhich is distinct from the other ash provinces (shy gures 3 and 4) and their known dis-tributions are mostly conshy ned to the Massif Central region The ages of the MassifCentral tephras are based on radiocarbon dates obtained from mire and lake sedi-ments which `bracketrsquo the tephras The La Nugsup3ere Tephra with an age of 114 14C kaBP is the oldest Massif Central tephra identishy ed so far within the time-span of inter-est (Etlicher et al 1987 Juvigne et al 1996) The two Godivelle Tephras (5 and 4)are close in age but extensive radiocarbon dating suggests distinct ages of 107and 103 14C ka BP respectively (Juvigne et al 1996) The age of the Puy de DomeTephra is less certain as the estimate is based on only one radiocarbon date froma site in the southern Chaplusmn ne des Puys (table 1) This tephra is thought to havea trachyte composition (Juvigne 1993) although no major element concentrationshave yet been published
The ChopineKilianVasset tephras are thought to be derived from three separateEarly Holocene eruptions although the stratigraphic succession is not known atpresent These trachytic tephras have been radiocarbon dated to ca 854sect150 14C kaBP but are thought to have erupted separately within ca 260 yr (Juvigne et al 1996) This series of tephras is considerably more widespread than the others fromthe region having been identishy ed as far east as the Jura Mountains (Martini amp Duret1965 Martini 1970) Some other ash falls that originated from the Chaplusmn ne des Puysappear to be of local importance only (Vernet et al 1998 Vernet amp Raynal 2001)Geochemical data are currently available for only three of the Massif Central tephrasand so far as is known no attempt has yet been made to identify these tephras inmicro-tephra form
(d ) Italian provinces
The Italian tephras from this period can be assigned to three main volcanic com-plexes the Campanian volcanic shy elds around Naples Etna on Sicily and the AeolianIslands The Campanian complex which includes the Phlegrean Fields Vesuviusand Ischia is mainly trachytic in composition with a geochemical spectrum that isquite distinct from those of the Etna complex and of the Aeolian Islands (shy gure 3)Tephras originating from one or more of these three complexes have been detectedin marine cores from the Tyrrhenian and Adriatic seas as well as other parts of theMediterranean Sea (Keller et al 1978 Paterne et al 1986 1988 1990 Langone etal 1996) and in lake sequences in southern Italy such as Lago Grande di Monticchio(Newton amp Dugmore 1993 Narcisi 1996 Allen et al 1999) and central Italy such asLago Albano near Rome (Calanchi et al 1996) Some work has also been conducted
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European tephrochronological framework for Termination 1 785
in or close to the volcanic source areas in an attempt to establish the full sequenceof volcanic eruptions during the Late Quaternary (see for example Di Vito et al 1999) There are nine Italian tephras reported from marine and lake sequences thatdate from the period between 185 and 80 14C ka BP In all instances the recordsare of visible layers of tephra The ages of some of these are poorly established atpresent with conregicting data obtained from dinoterent sites The ages suggested intable 1 are those favoured in the most recent publications but these may requirere-assessment in the light of future research
The two oldest known tephras in the time-period of interest are the L9 and Green-ish Tephras both recorded as separate features within the annually laminated Lagodi Monticchio maar sequence The lowest of the two L9 is considered to be the cor-relative of the `basalrsquo plinian eruption of Vesuvius (Narcisi 1996) Age estimates ofa palaeosol that underlies the Vesuvius tephra sequence are ca 1617 14C ka BP forthis event (Delibrias et al 1979) L9 has a trachytic composition very similar to theGreenish Tephra (table 1) However L9 which is also a product of Vesuvius is foundstratigraphically below the Greenish Tephra in the Lago di Monticchio core TheGreenish Tephra is dated in the Monticchio sequence to 17 560 varve yr BP (Allenet al 1999) and has a calibrated radiocarbon age estimate of 17 830 sect 300 cal BP(Andronico et al 1995) Both tephras have a dominantly eastwards dispersal basedon the occurrences of visible layers (Santacroce 1987 Narcisi 1996) Both tephrasalso have a trachytic composition and as can be seen from table 1 the reportedgeochemical spectra are very close indeed with the standard deviations overlappingfor almost every major element This could present problems for tephrostratigra-phy where only one of the tephras is evident in a sediment sequence in particularbecause they are so close in age This is a good example of where an analysis oftrace and rare earth elements might be required to make a clear distinction betweentephras with very similar major oxide concentrations
The Y-1 Tephra also termed the Biancavilla Montalto Ignimbrite (Vezzoli 1991)is a product of Etna and has been identishy ed as a visible benmoritic tephra horizonthroughout the central Mediterranean (Paterne et al 1988) including central Italyand the Adriatic Sea (Vezzoli 1991 Narcisi 1993 Calanchi et al 1996) It has anestimated age of ca 140 14C ka BP The Unita dei Tefra Superiori tephra which hasbeen detected as far east as Lago di Monticchio in south-central Italy (Narcisi 1996)is also dated to ca 140 14C ka BP (Alessio et al 1976) but it is thought that thesource of this tephra lies in the Phlegrean Fields No geochemical data are availablefrom the presumed source region|the data reported in table 1 were obtained fromthe Lago di Monticchio record (Narcisi 1996)
The NYT which is equivalent to the C-2 tephra reported from various marinesequences has also been traced throughout central Italy and the Adriatic Sea (Pat-erne et al 1988 Calanchi et al 1996 Di Vito et al 1999) (shy gure 2) In the centralApennines region it formed the parent material for a soil that started to developat the beginning of the Holocene period (Frezzotti amp Narcisi 1996) Also originatingfrom the Campi Flegrei caldera it is dated to ca 120 14C ka BP (Di Vito et al 1999) Published geochemical data based on EDS indicate three dinoterent geochemicalpopulations varying from latite to phonotrachyte in composition (Orsi et al 1992Paterne et al 1988) (table 1) We report in x 4 of this paper on new data obtainedfrom the NYT by WDS and it is the mean of these new data that is included intable 1 Comparisons with the previously published EDS data are provided (table 1)
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786 S M Davies and others
The new data indicate clearly that the NYT originated from the Campanian volcaniccentre
In the interval between the dispersal of the NYT (ca 120 14C ka BP) and 95 14Cka BP there appear to have been as many as 34 eruptions in the Campi Flegrei caldera(Di Vito et al 1999) Of these only one appears to have been detected widely in theregion the Pomici Principali (also termed the Agnano Formation or C-1 tephra inmarine records (Paterne et al 1988) This was the product of the highest magnitudeeruption from this epoch and is dated to between 976 sect 300 and 1032 sect 50 14C kaBP (Delibrias et al 1979 Di Vito et al 1999) or to 122 varve ka BP based on theMonticchio varve chronology (Allen et al 1999) It is trachytic in composition andappears to have had a mainly eastwards dispersal
The Mercato Tephra dated to ca 80 14C ka BP and originally analysed usingEDS has a phonolitic composition and is believed to have been generated by Vesu-vius (Paterne et al 1988) New WDS data obtained from reference samples col-lected from an exposure to the west of Naples support these conclusions (table 1 andAppendix A) The silica content of the WDS analyses are ca 3 lower than thoseobtained using EDS (table 1) which may reregect the fact that the EDS data werenormalized
The only tephra listed in table 1 that is thought to have originated from the AeolianIslands is the Pollara pumice also referred to as the E2 tephra in marine sequences(Paterne et al 1986 1988) The limited geochemical data available so far suggest itto be the only Italian tephra listed in table 1 that is rhyolitic in composition Littlemore is known about this ash which has not been recorded extensively except thatits age is estimated to be ca 130 14C ka BP (Keller 1980)
5 Extending the known distributions of European tephras
Figure 2 summarizes schematically the known distributions of three of the tephrasreferred to in the preceding section the VA the LST and the NYT Following theintroduction of a laboratory method that enables the detection of micro-tephra parti-cles in mineral-rich sediment the VA has been traced to sites that are located muchfarther south (into The Netherlands) and east (as far as St Petersburg) than thedistribution limits based on occurrences of visible layers of the ash As a result con-tinental sequences over a much larger area in northern Europe can now be correlateddirectly with marine and ice-core records using the VA as a time-parallel marker
This suggests therefore that other prominent ash layers such as the LST andNYT should also be detectable over larger tracts of Europe than is presently thecase if suitable sites are examined for the presence of micro-tephra horizons To testthis assertion we examined lake sediment deposits of Last Termination age froma site in the northern Apennines in order to establish whether the NYT could bedetected in micro-tephra form The site selected Prato Spilla `Crsquo lies well to thenorth of the localities in central and southern Italy and in the Adriatic Sea fromwhich visible records of the NYT have been reported Prato Spilla `Crsquo lies at an alti-tude of ca 1350 m in the Appennino Parmense ca 60 km south of Parma and 15 kmeast of Pontremoli The site contains a continuous sediment sequence spanning theLast Termination and most of the Holocene Detailed pollen and coleopteran strati-graphical records which have been radiocarbon dated have been published for thissite (Lowe 1992 Ponel amp Lowe 1992 Lowe amp Watson 1993)
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European tephrochronological framework for Termination 1 787
Figure 6 Light microscope photograph of an NYT glass shard from Prato Spilla Crsquosequence assigned on geochemical grounds to the NYT
The methods adopted for sub-sampling of the Prato Spilla `Crsquo sequence for thequantishy cation of glass shard concentrations and for subsequent electron microprobeanalysis of selected glass shards followed those described elsewhere (Turney 1998)In summary contiguous samples of 1 cm stratigraphic interval were extracted fromthe sequence to establish presenceabsence of glass shards Each of the 1 cm3 blocksin which tephra particles was detected was then examined with more care andshard concentrations were quantishy ed for each sub-sample Micro-tephra particleswere detected in shy ve samples (shy gure 6) but were predominantly clustered around500 cm in the part of the sequence assigned on pollen-stratigraphic grounds to theLate Glacial Interstadial or the `Allerfrac12drsquo|indeed the part of the succession in whichthe NYT would be expected to occur Peak concentrations of micro-tephra particlesreach 225 shards cmiexcl3 and are conshy ned to a single 1 cm thick sample in the sequencewhich probably represents the time of maximum deposition of the ash
Electron microprobe measurements based on WDS were obtained from the surfacesof 21 separate glass shards extracted from the sample with peak shard concentrations(Appendix A) Since only EDS measurements were available for the NYT prior to thepresent study we also obtained WDS measurements from 17 shards extracted fromthe visible layer of NYT that is exposed on Procida Island which lies in the type-locality for the NYT close to the city of Naples (Appendix A) The results providenot only a more comprehensive geochemical dataset for the NYT than was previ-ously available but also a consistent basis for comparison with the Prato Spilla `Crsquodataset All of the WDS data reported here (Appendix A) were measured at the samelaboratory (Tephrochronology Analytical Unit University of Edinburgh) using thesame sample pretreatment and preparation protocol The WDS results for the NYTdinoter to a minor degree from the EDS results (table 1 and Appendix A) especiallywith respect to the amounts of silica aluminium and calcium measured The EDS
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788 S M Davies and others
4 8FeO ()
TiO
2 (
) Neapolitan Yellow Tuff(Procida)Neapolitan Yellow Tuff(Prato Spilla lsquoCrsquo)
0
1
2
3
40 50 60 70
MgO
(
)
SiO2 ()
K2O
(
)
40 50 60 70
0
04
08
4
8
12
SiO2 ()
(a)(b)
(c)
Figure 7 Bi-plots of SiO2 K2 O SiO2 MgO and FeOTiO2 for the WDS analyses obtainedfrom glass shards of the NYT from Procida (Naples) and Prato Spilla Crsquo Means and standarddeviations are shown
results show a higher degree of statistical scatter than the WDS measurements whichmay reregect the fact that the data were normalized combined with the inreguence ofvariation in water content between shards
There is a very close correspondence between the WDS data for the Prato Spilla `Crsquomicro-tephra shards and those obtained from the type-material near Naples (shy g-ure 7) The geochemical data strongly suggest therefore that the NYT is representedat the Prato Spilla `Crsquo site by a discrete layer of micro-tephra particles This conclu-sion is compatible with the pollen-stratigraphic data from the site and accords withage estimates for the NYT (ca 120 14C ka BP) obtained from other sites (Paterneet al 1990)
These results encourage us to believe that many if not all of the tephras listedin table 1 will be detectable over much larger tracts of Europe than is presently thecase if appropriate research is undertaken to detect layers of micro-tephra particlesin selected sites The authors are presently engaged in a major continent-wide pro-gramme of research in collaboration with a number of European research groupsdesigned to test this hypothesis The focus in this research is on those parts of Europewhere we expect to shy nd overlapping `apronsrsquo of tephra deposition originating fromthe Italian Eifel Massif Central and Icelandic provinces For example a number ofsites in parts of southern France northern Italy and perhaps western Switzerlandmay have received inreguxes of micro-tephra originating from the Italian and Eifelprovinces and perhaps also from the Massif Central Sites in parts of Germany Den-mark and southern Sweden for example may in turn have received tephra depositsfrom both of the Icelandic and Eifel provinces If this proves to be the case then thestage will be set for the construction of a tephrostratigraphical framework for Europewhich will enable Last Termination sequences to be correlated on a continent-widebasis using micro- and visible tephra layers as time-parallel stratigraphic markersFurthermore there is also the possibility that other tephras remain to be discovered
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European tephrochronological framework for Termination 1 789
those which either because of the magnitude or nature of some volcanic eruptionswere distributed over parts of Europe in micro-tephra form only
6 European tephrostratigraphy and the chronology of eventsduring the Last Termination and Early Holocene
One of the crucial issues in Late Quaternary palaeoenvironmental research thatremains to be resolved is the degree to which climatic events inferred from oceanicterrestrial and ice-core records were synchronous during the Last Termination andEarly Holocene If the ice-core records provide realistic estimates of the rates anddurations of climatic events during this period then comparisons between individ-ual records have to be enotected with at least a decadal precision The problem thispresents and the role that tephrostratigraphy can play in resolving some of thedimacr culties involved are put into perspective in shy gure 8
Figure 8 shows some of the data used to calibrate radiocarbon dates (the LakeSuigetsu and Cariaco Basin datasets) plotted against the GRIP ss08c ice-core recordof macr 18O variations The latter has been selected by the INTIMATE group as an arbi-trary and temporary standard for this period and used to deshy ne an event stratig-raphy scheme (shy gure 1) for the Last Termination (see Bjorck et al 1998 Walker etal 2001) As has been alluded to in earlier sections of this paper the uncertaintiesassociated with all of the dating methods currently employed preclude precise com-parisons of ice-core marine and terrestrial records Oceanic and terrestrial recordsmostly rely upon radiocarbon dating locally supplemented in a few cases by varvechronology Imprecisions in radiocarbon dates can arise through site-specishy c fac-tors (eg hard-water or mineral carbon errors in freshwater sequences and reservoirerrors in marine sequences) sample selection laboratory measurements of 14C activ-ity and other factors (Lowe amp Walker 2000) Further imprecision may be introducedby the calibration of radiocarbon dates since the uncertainties in the dataset usedto calibrate pre-Holocene radiocarbon dates INTCAL98 are far higher than forthe Holocene which is based on dendro-calibration (Stuiver et al 1998) There arealso uncertainties anotecting varve chronologies while the ss08c ice-core chronologyfor the Last Termination dinoters signishy cantly from the GISP2 record and indeedfrom other models of the GRIP record (Lowe et al 2001) Published comparisonsbetween ice-core marine and terrestrial records for the Last Termination seldom takeinto account the true magnitude of the dating uncertainties involved and frequentlyemploy circular reasoning
Figure 8 shows the positions on the radiocarbon time-scale of 20 of the tephrasdiscussed earlier in this paper these being the ones for which reasonably conshy dentradiocarbon age estimates can be made (though these will be subject to revised esti-mates in the future) A high number of these occur in the period 14080 14C kaBP but we conshy dently anticipate the discovery in the future of additional tephras(perhaps in micro-tephra form only) which will date to the period 185140 14C kaBP Tephras detected in the GRIP ice core over the same time-interval are plottedon the calendar time-scale in shy gure 8 By providing key `time-linesrsquo between recordstephrostratigraphy can help to resolve some of the dating uncertainties referredto earlier by for example enabling direct comparisons of discrepant age estimatesobtained using dinoterent methods (cf Litt et al 2001) It can also provide estimatesof the magnitudes of the reservoir errors that anotected various marine sectors at dif-
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790 S M Davies and others
-44
-40
-36
-32
cale
ndar
yea
rs B
P
8000
9000
10 0
00
11 0
00
12 0
00
13 0
00
14 0
00
15 0
00
16 0
00
17 0
00
18 0
00
14C age (BP)
VA
SA
Un
Un
Un
Un
Un
BF
Hol
ocen
eG
S-1
GI-
1aG
I-1b
GI-
1cG
I-1d
GI-
1eG
S-2
aG
S-2
bG
S-
2c
Bor
robo
l
La
Nug
egravere
Laa
cher
See
God
ivel
le 5
amp I
-TH
OL
-2
Puy
de D
ocircme
I-T
HO
L-1
Saks
unar
vatn
Houmlg
stor
psm
osse
nU
lmen
er M
aar
amp L
3574
radiocarbon dated European tephra horizons
Cho
pine
Kili
an V
asse
tM
erca
to
God
ivel
le 4
Pom
ici P
rinc
ipal
i amp V
edde
Polla
ra p
umic
eK
OL
-GS-
2 amp
GS
-2B
AS-
12
3
GS
-2B
AS-
4 U
nita
dei
Tef
raSu
peri
ori amp
laye
r Y
-1
Gre
enis
h
L9
20 0
0018
000
16 0
0014
000
12 0
0010
000
-44
-40
-36
-32
800
600
400
200 0
GISP2 volcanicsulphate conc (ppb)
1000
Nea
polit
an Y
ello
w T
uff
GISP2 18O (permil) dGRIP 18O (permil) d
Figure 8 For description see opposite
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European tephrochronological framework for Termination 1 791
ferent times through a comparison of radiocarbon dates obtained from marine andterrestrial horizons in which the same tephra has been detected (see for exampleAustin et al 1995 Bondevik et al 2001 Haregidason et al 2000) Tephrostratigraphymay provide an independent test of suggestions that some of the climatic changesduring the Last Termination were time-transgressive as illustrated for some appar-ently contrasting climatic trends in Iceland Britain and NW Russia (Lowe 2001) Ofparticular importance as far as establishing `leadsrsquo and `lagsrsquo in climatic changes isconcerned are the tephra records from the Greenland ice cores The discovery of theVedde and Saksunarvatn ashes in the GRIP record (Gronvold et al 1995) alreadyprovides a basis for making direct comparisons between marine terrestrial and ice-core records It is a matter of some urgency that the incidence of tephra depositsin the Greenland ice cores be more fully explored in the hope that this will lead tothe recognition of additional time-parallel links between the ice-core records on theone hand and oceanic and terrestrial records on the other An investigation of thenew NordGRIP record for this purpose is currently in progress (S M Davies 2002unpublished data)
Finally a fuller and more reshy ned tephrostratigraphical scheme for Europe will alsohave other applications It will provide an important database for those investigatingthe timing and frequency of volcanic eruptions in Europe during the past 20 000 yror so as well as of the geochemical evolution of the dinoterent volcanic centres overthat period A fuller record of the distribution of micro-tephras may also provideinformation on atmospheric circulation patterns during the dispersal and depositionperiods as well as on the nature and altitude of the eruption columns which mayin turn provide inferences about magma viscosity
This paper is a contribution to the INTIMATE project of the INQUA Palaeoclimate Com-mission and the work is supported by a Leverhulme Trust Research project (grant allocationnumber F07537C) entitled Testing hypotheses of rapid climate change using tephrochronol-ogyrsquo SMDrsquo s contribution was completed during possession of a NERC PhD studentship(GT 0499ES162) We are extremely grateful to Dr Peter G Hill for his assistance withthe EPMA analyses at the Tephrochronology Analytical Unit University of Edinburgh We alsothank Dr G Mastrolorenzo (Vesuvius Observatory) and Miss G Swindle for assistance duringthe macreld investigations in Naples Thanks are also expressed to two anonymous reviewers forcomments on an earlier draft
Appendix A
Table 2 shows the major oxide concentrations of NYT glass shards from Procidaand Prato Spilla `Crsquo and of the Mercato Tephra from the Naples area (see x 4 forsite context) All oxides are shown as weight and total iron is expressed as FeO
Figure 8 Radiocarbon calibration curve for Termination 1 and the Early Holocene compared with theGRIP macr 18 O event stratigraphy the GRIP ss08c and GISP2 macr 18 O records (wwwngdcnoaagov) andknown tephra horizons from this period The shaded areas represent the cooler climatic episodes andare labelled with the Greenland stratotype terminology (Bjorck et al 1998) Where radiocarbon agesare reported in table 1 as a range the mean is given here Abbreviations for GRIP horizons are asfollows Un unknown (approximate positions are given (S Johnsen 2001 personal communication))SA Saksunarvatn Ash VA Vedde Ash BF Black Feather Sulphate concentrations from the GISP2record are also shown (Zielinski et al 1996) Open circles denote radiocarbon calibration data fromLake Suigetsu (Kitagawa amp van der Plicht 2000) Filled circles denote radiocarbon calibration data fromCariaco Basin assuming a marine reservoir age of 420 14 C yr (Hughen et al 1998)
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792 S M Davies and others
Tab
le2
Majo
roxi
de
con
cen
trati
on
sof
NY
Tgl
ass
shard
sfr
om
Pro
cida
an
dP
rato
Spil
laC
rsquoan
dof
the
Mer
cato
Tep
hra
from
the
Naple
sare
a(s
eex4
for
site
con
text
)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
roci
da)
1584
204
0177
634
201
106
828
635
197
5969
1W
DS
2598
603
9178
027
101
204
924
244
583
4965
8W
DS
3586
604
5173
631
100
805
924
342
183
0951
9W
DS
4583
903
9177
933
000
906
924
540
486
9958
3W
DS
5605
106
8179
126
901
204
923
243
086
1976
4W
DS
6591
704
5177
332
801
006
425
740
887
8968
0W
DS
7581
804
1178
031
501
107
125
640
086
9956
1W
DS
8589
504
2179
533
701
506
926
740
987
5970
4W
DS
9592
003
9178
135
101
007
026
443
585
7972
7W
DS
10
591
404
2174
631
601
105
723
442
482
6957
0W
DS
11
593
403
6177
131
301
506
726
439
188
5967
6W
DS
12
588
103
8176
128
100
505
525
141
583
4952
1W
DS
13
577
003
8176
533
500
807
228
140
384
8952
0W
DS
14
586
004
7179
735
300
706
827
842
984
6968
5W
DS
15
588
104
2180
629
400
505
924
937
993
0964
5W
DS
16
579
603
9178
536
501
308
228
836
087
1959
9W
DS
17
580
103
9177
631
500
907
327
039
488
9956
6W
DS
mea
n588
104
2177
631
901
006
525
940
686
9962
8
sd
(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(07
8)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 793
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
rato
Spil
laC
rsquo)
1552
105
4177
247
401
914
38
735
578
9951
1W
DS
2557
305
7179
845
701
512
640
136
581
5960
6W
DS
3595
004
4173
724
302
003
117
652
877
8950
7W
DS
4575
704
2179
433
001
406
627
043
083
6953
7W
DS
5599
904
0178
826
401
304
421
841
688
4966
5W
DS
6591
103
8177
826
601
105
022
443
888
8960
2W
DS
7565
304
5180
939
501
410
532
535
791
8962
1W
DS
8597
606
9180
826
501
604
821
546
684
6970
7W
DS
9571
805
6179
939
801
109
932
240
883
6964
7W
DS
10
588
603
7176
527
601
104
721
042
487
7953
3W
DS
11
559
404
9180
544
501
812
339
435
878
6957
2W
DS
12
594
704
0181
328
301
705
522
144
785
6967
9W
DS
13
611
103
7187
016
900
802
419
938
195
9975
8W
DS
14
599
204
4181
128
601
404
620
844
986
6971
6W
DS
15
601
204
4177
328
302
004
722
446
385
5972
1W
DS
16
595
104
5176
428
801
504
722
744
884
3962
8W
DS
17
603
704
1177
825
101
503
520
348
181
2965
3W
DS
18
558
704
5179
647
401
813
139
836
879
0960
7W
DS
19
589
602
8178
830
901
606
622
436
091
8960
5W
DS
20
553
606
3178
647
401
913
840
136
978
0956
6W
DS
21
579
004
0175
739
000
708
328
338
286
7959
9W
DS
mea
n582
804
6179
033
401
507
427
341
484
8962
1
sd
(1
87)
(01
0)
(02
7)
(09
2)
(00
4)
(03
9)
(08
0)
(04
9)
(05
0)
(07
0)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
794 S M Davies and others
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)
1575
202
7194
219
701
101
016
374
766
9951
8W
DS
2575
802
9194
523
902
201
520
273
564
5959
0W
DS
3574
301
4205
219
101
100
416
481
266
1965
2W
DS
4575
500
7206
018
002
000
415
181
669
3968
6W
DS
5580
000
9208
018
601
300
515
883
367
1975
5W
DS
6571
001
0206
016
101
600
515
078
967
1957
2W
DS
7577
501
1201
117
101
500
620
675
655
4950
5W
DS
8573
700
9212
717
101
900
815
187
564
2973
9W
DS
9580
301
3208
715
801
400
824
81
754
1968
1W
DS
10
574
400
6211
18
402
00
516
480
567
8971
6W
DS
11
577
200
7214
212
501
200
829
879
247
962
6W
DS
12
572
200
9211
217
301
501
15
980
465
9966
3W
DS
13
571
800
7210
417
402
201
16
184
467
2971
2W
DS
14
567
300
9208
916
901
400
917
383
262
5959
3W
DS
15
568
600
8205
918
202
101
414
682
666
6960
8W
DS
16
572
501
1211
318
202
01
215
884
364
5970
9W
DS
17
572
901
2212
916
502
101
215
883
667
2973
4W
DS
18
573
01
4211
716
301
801
416
83
365
5970
4W
DS
19
569
201
1207
418
602
101
414
982
964
961
6W
DS
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
3)
(04
2)
(01
3)
(00
1)
(00
2)
(01
)(0
39)
(01
1)
(02
5)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
References
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Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
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European tephrochronological framework for Termination 1 799
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Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
Walker M J C Bjorck S Lowe J J Cwynar L C Johnsen S Knudsen K-L WohlfarthB amp INTIMATE Group 1999 Isotopic events in the GRIP ice core a stratotype for the LatePleistocene Quat Sci Rev 18 11431150
Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
Phil Trans R Soc Lond A (2002)
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802 S M Davies and others
Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
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European tephrochronological framework for Termination 1 773
Tab
le1
(Con
t)
GR
IPage
tep
hra
age
(ss0
8c
volc
an
ich
ori
zon
(14C
yrs
)ti
me-
scale
)n
SiO
2T
iO2
Al 2
O3
FeO
Mn
OM
gO
CaO
Na
2O
K2O
P2O
5to
tal
EP
MA
sou
rce
ref
La
Nu
gmicroere
ca11
400
12
549
922
9160
470
002
324
454
744
538
972
4W
DS
La
Nu
gmicroere
6
21
(MC
)
Nea
poli
tan
ca12
000
17
588
104
2177
631
901
006
525
940
686
9
962
8W
DS
Cam
pi
1Y
ello
w(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(0
78)
Fle
gre
i
Tu
reg(I
T)
568
106
0194
448
7
17
451
938
75
5
100
ED
S
596
804
9192
940
3
06
435
034
588
9
100
ED
S2
14
619
403
1196
329
9
02
019
943
485
7
100
ED
S
Borr
ob
ol
ca12
300
18
733
601
1122
914
700
601
207
635
837
6
955
1W
DS
Hek
la22
(IC
)(0
35)
(00
2)
(01
8)
(00
9)
(00
2)
(00
2)
(00
3)
(01
4)
(00
9)
(0
47)
un
kn
ow
n14
650
sect200
(Ca
pea
k)
(17458
m)
un
kn
ow
n14
650
sect200
(C
ap
eak)
(17506
m)
E-2
P
oll
ara
ca13
000
766
302
7138
810
8
01
015
025
239
7
100
ED
SA
eoli
an
2
23
24
pu
mic
e(I
T)
Isla
nd
s
KO
L-G
S-2
13
400
18
490
910
6148
8100
702
184
9126
521
400
902
8989
6W
DS
25
(IC
)
GS
-2B
AS
-113
400
3497
417
0132
7124
402
266
6118
124
802
103
4988
7W
DS
26
(IC
)
Ref
eren
ces
1
this
stu
dy
2
Pate
rne
etal
(1988)
3
Narc
isi
(1996)
4
All
enet
al
(1999)
5
An
dro
nic
oet
al
(1995)
6
Ju
vig
nparae
et
al
(1996)
7
Bir
ks
et
al
(1996)
8
Bjo
rck
ampW
ast
egordma
rd(1
999)
9
Du
gm
ore
ampN
ewto
n(1
998)
10
Bjo
rck
et
al
(1992)
11
Kva
mm
eet
al
(1989)
12
Zoli
tsch
ka
etal
(1995)
13
Ju
vig
nparae
ampG
ewel
t(1
987)
14
Di
Vit
oet
al
(1999)
15
Del
ibri
as
etal
(1979)
16
Ju
vig
nparae
etal
(1987)
17
Dav
ies
et
al
(2001)
18
van
den
Bogaard
ampS
chm
inck
e(1
985)
19
Fri
edri
chet
al
(1999)
20
Bra
uer
eta
l(1
999)
21
Etl
ich
eret
al
(1987)
22
Tu
rney
etal
(1997)
23
Pate
rne
et
al
(1986)
24
Kel
ler
(1980)
25
Eir
parasup3kss
on
etal
(2000)
26
Hadeg
idaso
net
al
(2000)
27
Ale
ssio
etal
(1976)
28
Vez
zoli
(1991)
29
San
tacr
oce
(1987)
Phil Trans R Soc Lond A (2002)
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774 S M Davies and others
Tab
le1
(Con
t)
(Th
evarv
eage
for
the
Gre
enis
h(I
T)rsquo
row
is17
560
yea
rs)
GR
IPage
tep
hra
age
(ss0
8c
volc
an
ich
ori
zon
(14C
yrs
)ti
me-
scale
)n
SiO
2T
iO2
Al 2
O3
FeO
Mn
OM
gO
CaO
Na
2O
K2O
P2O
5to
tal
EP
MA
sou
rce
ref
GS
-2B
AS
-213
400
6497
933
2122
4147
902
445
389
829
905
205
4979
4W
DS
26
(IC
)
GS
-2B
AS
-313
400
2538
529
9125
7131
203
132
174
729
507
707
7980
1W
DS
26
(IC
)
GS
-2B
AS
-414
000
7503
617
4145
1113
202
155
3100
528
010
5
975
7W
DS
26
(IC
)
Un
ita
dei
ca14
000
5648
804
7184
625
901
602
217
432
679
302
8100
ED
SP
hle
gre
an
3
27
Tef
ra(0
53
)(0
13
)(0
25)
(07
4)
(01
4)
(01
6)
(01
6)
(03
4)
(06
6)
(01
6)
Fie
lds
Su
per
iori
(IT
)
Y-1
(IT
)ca
14
000
16
600
413
7169
555
502
218
242
262
229
306
8100
ED
SE
tna
28
Bla
ck17
000
sect300
Fea
ther
(17890
m)
Gre
enis
hca
15
000
9618
704
190
731
601
804
328
531
586
202
6100
ED
SV
esu
viu
s3
4
(IT
)(0
70
)(0
08
)(0
45)
(06
8)
(01
0)
(01
0)
(05
9)
(05
3)
(05
8)
(01
6)
29
L9
(IT
)ca
16
000
15
626
704
4188
630
401
103
329
429
683
402
7100
ED
SV
esu
viu
s3
15
17
000
(14
2)
(01
4)
(07
2)
(11
1)
(00
9)
(02
4)
(06
6)
(04
8)
(06
5)
(01
8)
St
2-1
85
18
500
7504
015
1145
5112
002
466
9114
525
206
6
992
2W
DS
26
(IC
)
Ref
eren
ces
1
this
stu
dy
2
Pate
rne
etal
(1988)
3
Narc
isi
(1996)
4
All
enet
al
(1999)
5
An
dro
nic
oet
al
(1995)
6
Ju
vig
nparae
et
al
(1996)
7
Bir
ks
et
al
(1996)
8
Bjo
rck
ampW
ast
egordma
rd(1
999)
9
Du
gm
ore
ampN
ewto
n(1
998)
10
Bjo
rck
et
al
(1992)
11
Kva
mm
eet
al
(1989)
12
Zoli
tsch
ka
etal
(1995)
13
Ju
vig
nparae
ampG
ewel
t(1
987)
14
Di
Vit
oet
al
(1999)
15
Del
ibri
as
etal
(1979)
16
Ju
vig
nparae
etal
(1987)
17
Dav
ies
et
al
(2001)
18
van
den
Bogaard
ampS
chm
inck
e(1
985)
19
Fri
edri
chet
al
(1999)
20
Bra
uer
eta
l(1
999)
21
Etl
ich
eret
al
(1987)
22
Tu
rney
etal
(1997)
23
Pate
rne
et
al
(1986)
24
Kel
ler
(1980)
25
Eir
parasup3kss
on
etal
(2000)
26
Hadeg
idaso
net
al
(2000)
27
Ale
ssio
etal
(1976)
28
Vez
zoli
(1991)
29
San
tacr
oce
(1987)
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 775
Altogether 34 tephra layers have been reported from sediment sequences in Europeand the NE Atlantic region which date to the period between 185 and 80 14C ka BP(table 1) Because tephra layers are deposited virtually instantaneously (in geologicalterms) they enotectively represent time-parallel marker horizons within stratigraphicalsequences (Westgate amp Gorton 1981 Sarna-Wojcicki 2000 Turney amp Lowe 2001) Intheory therefore all 34 tephras could prove valuable for correlation purposes eitherin a local context or in those cases where the ash deposits have been widely dispersedbetween regional sequences In practice however very little is known about the fullgeographical dispersal of the majority of the ash layers listed in table 1 Furthermorecorrelation by tephrostratigraphy will only work if the various ash layers have wellcharacterized geochemical signatures While some geochemical data are available forthe majority of the tephras listed in table 1 the collective data are far from robustand no geochemical data have yet been published for some
Nonetheless there is mounting evidence to show that some of the tephra depositslisted in table 1 are not only geochemically distinct but are also much more widelydispersed across Europe than was initially realized Stratigraphic records of thebetter-known tephras were initially limited to observations of visible tephra layersThe development of a technique that enables detection of tephra layers that are invis-ible to the naked eye (micro-tephra) in Late Glacial sequences has greatly extendedthe area over which some of the ashes can be traced (Lowe amp Turney 1997 Turneyet al 1997 Turney 1998 Wastegard et al 1998 2000a b) Most of this research sofar has focused on micro-tephra layers originating from Icelandic centres distributedthroughout northern Europe Here we report on further development of this line ofresearch with new evidence for the occurrence of micro-tephra layers in a site insouthern Europe The results suggest that there is great potential for tracing someash layers that originated from Italian volcanic complexes over much larger tracts ofsouthern and central Europe than records of visible tephra deposits allow This inturn greatly enhances the scope for making precise correlations not only betweenparts of southern Europe but also between continental and marine (MediterraneanSea) sequences
2 Micro-tephra extraction techniques
Micro-tephra horizons are composed of glass shards that are generally between 80and 24 m m (long axis) in size and that are present in such low concentration insedimentary sequences that they can only be detected by the use of a particle sep-aration technique Several factors inreguence the concentration of shards such as dis-tance from the volcanic source precipitation patterns during the eruption and sub-sequent tephra dispersal and sedimentary processes within the catchment In someterrestrial sequences micro-tephra horizons with a peak concentration (peak con-centration tends to coincide with the shy rst occurrence of glass shards in a sedimentsequence which is then taken to mark the time of maximum ash deposition) as lowas 10 shards cmiexcl3 has been conshy rmed whereas other sites have recorded as muchas 8000 shards cmiexcl3 (Turney et al 1997) In complete contrast tephra horizons inthe GRIP ice core have been identishy ed based on a single glass shard only (Gronvoldet al 1995)
Enotective separation techniques for the detection and isolation of tephra particlesfrom sedimentary sequences have been developed These include ashing of organic
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776 S M Davies and others
matter (Pilcher amp Hall 1992) digestion of biogenic and opaline silica (Rose et al 1996) the use of magnetic properties of ash layers (see for example Oldshy eld et al 1980 van den Bogaard et al 1994 Pawse et al 1998) X-ray analysis (Dugmore ampNewton 1992) and a density separation (regotation) technique (Turney 1998) Den-sity separation has proved exceedingly useful for the detection of small glass shardspresent in low concentrations in mineral-rich Late Glacial sediments This involvesthe separation and concentration of particles of predetermined specishy c gravity withthe use of a heavy liquid and subsequent identishy cation of glass shards with the useof a polarizing light microscope (for further details see Turney (1998)) This methodhas been particularly successful in the detection of tephras of rhyolitic compositionthat have a specishy c density of 2325 g cmiexcl3 (Lowe amp Turney 1997 Turney et al 1997 2001 Turney 1998 Wastegard et al 1998 2000a b) It is this technique thathas resulted in the wider recognition of micro-tephras in Europe as discussed below
3 Geochemical ` ngerprintingrsquo of tephra layers
The 34 tephras listed in table 1 have originated from four major volcanic complexesIceland the Massif Central in central France the Eifel district near Bonn and threevolcanic centres in Italy (the Campanian group Etna and the Aeolian Islands (seeshy gure 2)) An important matter to resolve is the extent to which the various magmasand ashes generated by these volcanic complexes can be geochemically shy ngerprintedThis is especially important in the case of tephras which have originated from thesame volcanic centre in which there may have been limited geochemical evolution ofmagmas over time In this section we summarize the approach generally adopted todetermine the geochemical character of visible and micro-tephras as background tothe geochemical data summarized in table 1 In the subsequent section of the paperwe review the present state of knowledge concerning all 34 tephras listed in table 1
Glass shards formed during the rapid cooling of magma are thought to have acomposition that is representative of the bulk geochemistry of the magma (Barker1983) hence widely dispersed glass particles are regarded as the most appropriateconstituents of pyroclastic material for geochemical analysis If a tephra deposit canbe shown to have a distinct geochemical signature then it can be used to correlatethe stratigraphic units in which it occurs (tephrostratigraphy) as well as to datethese units (tephrochronology) if the ages of the tephras are known (Westgate ampGorton 1981) A key element of building a tephrostratigraphical framework there-fore is to establish as rigorously as possible the geochemical composition of theindividual tephras used in its construction Robust and directly comparable geo-chemical datasets are dimacr cult to assemble for glass however because it is highlyunstable material particularly prone to sodium mobilization
The technique most widely employed to establish the geochemical signature of atephra is electron probe micro-analysis (EPMA) This enables grain-discrete determi-nations of the major elements within an individual glass shard which is of particularbeneshy t in the analysis of micro-tephra layers which generally contain glass particlesin low concentration The glass surface is bombarded with an electron beam and theX-ray energy produced is unique to each element while the intensity of the signalemitted is proportional to the amount of that element in the glass shard (Hunt amp Hill1993) Measurement can be by either energy dispersive spectrometry (EDS) or wave-length dispersive spectrometry (WDS) EDS has a lower precision mainly because
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European tephrochronological framework for Termination 1 777
N
0 500 km
Confirmed records of Vedde Ash (visible occurrences)
New records of Vedde Ash from flotation method
Extended area of Vedde Ash detection (micro-tephra)
Known area of Laacher See Tephra (visible occurrences)
Confirmed records of Neapolitan Yellow Tuff (visible occurrences)
New record of Neapolitan Yellow Tuff from flotation method
Known area of Neapolitan Yellow Tuff
Volcanic centres of particular relevance to this study
Other major volcanic centres in Europe
Figure 2 Location of the principal volcanic centres that were active during Termination 1 andthe Early Holocene The known distribution of the Vedde Ash (VA) Laacher See (LST) andNeapolitan Yellow Tureg (NYT) are shown
the behaviour of each element cannot be monitored independently during measure-ment and so this approach fails to detect for example any signishy cant mobilizationof sodium during the bombardment process (Hunt amp Hill 1993) Although WDSrequires a higher beam current and a longer counting time than EDS the formeronoters the distinct advantage of sequential acquisition of elemental data so that thedegree of sodium loss can be tracked The morphology of individual glass shards canalso distort EDS data a problem that is reduced when using WDS because for thisprocedure glass shards are mounted in an epoxy resin and polished to provide aregat surface for analysis Hence data should always be obtained using WDS whereverpossible
Even when WDS is used as a common tool for determining the geochemical spectraof samples aberrant results can arise that inreguence data comparisons For examplesome glass shards may contain tiny crystalline inclusions of feldspar and these shouldbe avoided when selecting surface points for analysis (Hunt amp Hill 2001) Hunt amp Hill
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778 S M Davies and others
6
4
2
40 50 60 70 80
K2O
(
)
SiO2 ()
Laacher See
Iceland
Veidivoumltn-Dyngjufjoumlll
Katla (basalt)
Grimsvoumltn-Kverkfjoumlll
Hekla
Katla (rhyolitic)
0
Icelandic volcanic centres8
10
Massif Central
Etna
Campanian
Figure 3 Bi-plot of SiO2 and K2 O concentrations in tephras derived from the main Europeanash provinces (modimacred after Mangerud et al 1984) The Campanian Massif Central and Etnaconcentrations are based on the data presented in table 1
(2001) have concluded that small variations in the laboratory procedures employedto determine glass chemistry can lead to misidentishy cation of sources for glass shardsand give an example of shards with a Jan Mayen provenance wrongly attributedto an Icelandic source Clearly there is a need for standardization of laboratoryprocedures and while a number of recommendations have recently been advocated(Froggatt 1992 Hunt amp Hill 1993 Hunt et al 1998) there is still some variation inlaboratory and operator practice (Hunt amp Hill 1996) Standardization is also requiredin the form in which results are presented to ensure comparability Normalizationof the data to 100 a practice employed by some researchers can obscure poorresults and hence lead to incorrect comparisons (Hunt amp Hill 1993) However othersargue that it may actually facilitate comparisons between samples by removing thedistorting enotects of the water component contained in glass shards (see for exampleFroggatt 1992) The majority of the published Italian and some of the Eifel datahave been normalized while those from other parts of Europe have not and hencedata comparisons are not always straightforward
Table 1 provides mean values and standard deviations for major oxide concentra-tions obtained from those tephras for which data are presently available The tableincludes previously unpublished WDS results for the Neapolitan Yellow Tunot (NYTdiscussed in x 4 below) and for the Mercato Tephra While individual tephra layersmay be geochemically distinct the geochemical envelopes representing the collectivedata obtained from all of the tephras assigned to each major volcanic province showsignishy cant overlaps as is illustrated in the bi-plots and ternary plots (shy gures 3 and 4)of selected oxide concentration data It is clear therefore that measurement of majoroxide concentrations does not satisfactorily discriminate between some tephras orig-inating from dinoterent volcanic centres (as noted by van den Bogaard amp Schmincke(1985) and Frezzotti amp Narcisi (1996) with respect to Eifel and Italian tephras)nor of tephras of dinoterent age originating from the same volcanic centre (Bond et
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European tephrochronological framework for Termination 1 779
40 50 60 70 80
K2O
(
)
SiO2 ()
shyshyshyshy
shy
shyshy
shyshyshy
shy
shy
shy
shy
reg
reg regreg
regregregregreg regregregregreg
FF
F
ll
l
l
4 8 12 16
reg
regreg
regreg
regregreg
regreg
regregreg
shy
F
l shyshyshyshyshy shyshyshyshyshyshy
F
F
l
ll
FeO ()
TiO
2 (
)
reg
l
Iceland
Eifel
F
shy ItalyMassif Central
100
80
60
40
20
100
80
60
40
20
100 80 60 40 20
CaO
FeO
K2O
regregreg
reg
reg
reg
reg
reg
reg
regregreg
shyF
F
F
regreg
l
lllshy
shyshyshy
shyshyshy
l
0
2
4
6
8
10
0
1
2
3
4
5
regreg
regreg
regreg
regreg
regreg
reg
reg
regreg
l
l
ll
shy
shyshy
shyshy
shy
shyshy
FF
F
100
80
60
40
20
100
80
60
40
20
100 80 60 40 20
K2ONa2O
CaO
(c) (d)
(a)
(b)
Figure 4 Plots of selected geochemical data obtained from tephras of Termination 1 age (seetable 1) (a) Bi-plot of mean SiO2 and K2 O values (b) Bi-plot of mean FeO and TiO2 values(c) Ternary plot indicating variations in the proportions of FeO CaO and K2 O (d) Ternaryplot indicating variations in the proportion of CaO Na2 O and K2 O
al 2001) Individual tephra layers are presently assigned to a particular volcanicevent on the basis of a combination of criteria usually including examination of thephysical properties (eg refractive index and surface detail of the glass shards) thestratigraphic position of the layer and independent assessment of the age of the layeras well as any geochemical data that may be available The construction of a tephro-stratigraphical scheme would clearly beneshy t from the application of a more diagnostic
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780 S M Davies and others
geochemical tool One approach that has promise is the analysis of trace and rareearth elements using an ultraviolet laser ablation inductively coupled plasma massspectrometer (UV-LA-ICP-MS) (Pearce et al 1996 1999 Eastwood et al 1999)This approach has been applied successfully to analysis of tephras of Mid-Holoceneage but not yet to tephras that fall within the period of interest here
4 Tephra layers in Europe and the North Atlantic regiondated to between 185 and 80 14C ka
(a) Icelandic province
The Icelandic volcanic systems are divided into three main groups based on theirgeochemical characteristics tholeiitic basalts transitional alkali basalts and alkaliolivine basalts (Jakobsson 1979) Collectively magmas from the Icelandic provincespan a wide geochemical spectrum although individual volcanic centres have tightgeochemical distributions (shy gure 3) for four of the main centres Grimsvotn-Kverfjolland Veidvotn-Dyngjufoll which form part of the northern (tholeiitic) volcanic zoneand Hekla and Katla which fall within the eastern (alkali olivine basalt and transi-tional alkali basalt) volcanic zone (Haregidason et al 2000) These appear to be thekey centres for the tephras listed in table 1 that have been assigned an Icelandicorigin
One of the best-known and most widely dispersed tephra horizons in northernEurope that has an Icelandic origin is the Vedde Ash (VA) which was depositedca 103 14C ka BP (Birks et al 1996 Wastegard et al 1998) within the GS-1Younger Dryas chronozone This ash is believed to originate from the Katla complexwithin the transitional alkali basalt province (Mangerud et al 1984 Lacasse et al 1995) in the south of the island The ash has a bimodal geochemical composition (rhy-olitic and basaltic) which is thought to reregect derivation from two separate magmachambers Studies of recent volcanic events in Iceland have shown that the mostexplosive eruptions generating the largest amounts of tephra occur in this tran-sitional alkali basalt province (Haregidason et al 2000) It is also believed that thewidespread distribution of this ash was caused by the development of co-ignimbriteash plumes during an ignimbrite-forming eruption (Lacasse et al 1995)
Layers of VA that are visible to the naked eye have been found in lake sediments inwestern Norway (Mangerud et al 1984) and the Inner Hebrides Scotland (Davies etal 2001) and in marine cores throughout the NE Atlantic (see for example Kvammeet al 1989 Lacasse et al 1995) in the northern North Sea (Long amp Morton 1987)on the Iceland plateau (Ruddiman amp McIntyre 1981 Sejrup et al 1989) and on theeast Greenland continental margin (Stein et al 1996) The distribution of the VAin North Atlantic marine sequences is characterized by an arcuate lobe extendingsouthwest from the Denmark Strait and curving eastwards to mid-latitudes in theNorth Atlantic (Lacasse et al 1995) This strongly suggests deposition from raftedice which was displaced to the southwest and south in a circulating counterclockwisegyre (Ruddiman amp Glover 1972) This may well reregect Katlarsquos close proximity tothe southern coast of Iceland with the Vedde tephra being deposited on ice thatcalved directly into the North Atlantic (Haregidason et al 2000) However depositionvia the atmosphere almost certainly took place as well as is indicated by the recentdiscoveries of rhyolitic VA in micro-tephra form in several sites in Scotland (Turneyet al 1997) southern Sweden (Wastegard et al 1998 2000a) and western Russia
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(Wastegard et al 2000b) A more recent discovery of a relatively high concentrationof rhyolitic VA glass shards in the northern Netherlands indicates that the ash maywell have been dispersed much further south than previously thought (S M Davies2002 unpublished work) Finally glass shards assigned to the VA have also beendiscovered in the GRIP ice core and dated to 11 980 sect 80 GRIP yr BP (Gronvold etal 1995) This discovery is extremely important for it indicates that the VA maywell provide a reliable time-parallel marker horizon between ice-core marine andterrestrial records
Two other important Icelandic ash layers the Borrobol and Saksunarvatn Tephraswere deposited near the beginning and end of the Last TerminationEarly Holoceneinterval respectively The Borrobol Tephra was discovered for the shy rst time in lakesediments in several sites in Scotland and as yet is known only in micro-tephra formIt has been dated in Scottish sites to ca 123 14C ka BP (Turney et al 1997) Whatis thought to be a contemporaneous tephra has been detected in marine sedimentson the North Icelandic shelf (Eirplusmn ksson et al 2000) This certainly has a very similargeochemical composition to those reported from Scotland but the horizon in whichit was discovered on the North Iceland plateau has been dated to 134 14C ka Theage discrepancy between the Scottish and Icelandic Borrobol Tephra layers may wellreregect the inreguence of a marine reservoir error although the possibility that severaltephras with similar geochemical composition were erupted over a period exceeding1000 yr cannot be ruled out (Larsen 2000)
The Saksunarvatn Ash appears to have been one of the largest Holocene eruptionsin Iceland It has a tholeiitic basaltic composition which is considered to indicate anorigin in the Grimsvotn or Kverfjoll complex (shy gure 3) (Mangerud et al 1986) Layersof this ash have been identishy ed in sites on the Faroe Islands (Mangerud et al 1986Dugmore amp Newton 1998 Wastegard et al 2001) the Shetland Isles (Bennet et al 1992) northern Germany (Merkt et al 1993) western Norway (micro-tephra) (Birkset al 1996) and in the GRIP (Gronvold et al 1995) and NordGRIP ice cores (S MDavies 2002 unpublished work) It has been dated to between 9060 and 8930 14C kaBP (Birks et al 1996) in Norway and to ca 10 240 sect 30 GRIP yr BP in the GRIPice core (Gronvold et al 1995) The Saksunarvatn Ash may thus provide a secondimportant widespread time-parallel marker between ice-core marine and terrestrialrecords
Other Icelandic tephras of rhyolitic amacr nity are less well known in terms of theirdistribution and geochemical variation The Hogstorpsmossen Tephra reported fromSweden (Bjorck amp Wastegard 1999) and the L3754 tephra discovered in the FaroeIslands (Dugmore amp Newton 1998) are known from single sites only and so theirpotential for tephrostratigraphy is uncertain at present Furthermore the geochem-ical spectrum of the Hogstorpsmossen Tephra is based on a small dataset with lowanalytical totals
A number of tephras of basaltic composition have originated from Iceland buttheir distributions are largely conshy ned to Iceland or to marine cores collected fromclose to the Iceland coast or in the North Atlantic These include the tephras listedas 1-THOL-1 1-THOL-2 KOL-GS-2 GS-2BAS-1 GS-2BAS-2 GS-2BAS-3 andGS-2BAS-4 in table 1 (Kvamme et al 1989 Bjorck et al 1992 Eirplusmn ksson et al 2000 Haregidason et al 2000) The shy rst two in this list are tholeiitic basaltic tephrasassociated with the VA in a complex series of tephras collectively termed NorthAtlantic Ash Zone 1 (NAAZ1) which has been detected in numerous marine cores
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782 S M Davies and others
from the North Atlantic Initially thought to represent a single eruption analysisof high-resolution sediment sequences from Lake Torfadalsvatn in northern Iceland(Bjorck et al 1992) the Hebridean Shelf near NW Scotland (Austin amp Kroon 1996)the St Kilda Basin (Hunt et al 1995) and the open North Atlantic (Bond et al 2001)has demonstrated that NAAZ1 comprises a series of distinct ashes that probablyreregect separate eruption events 1-THOL-1 is thought to originate from Veidivotn(shy gure 3) while Grimsvotn may have been the source of 1-THOL-2 (Kvamme et al 1989)
KOL-GS-2 is also of tholeiitic basaltic composition but is thought to originatefrom the Kolbeinsey Ridge system (Eirplusmn ksson et al 2000) To date this tephra hasbeen detected in one marine core only within the same record on the North Ice-landic shelf as that from which the correlative of the Borrobol Tephra was alsoreported (Eirplusmn ksson et al 2000) GS-2BAS-1 to GS-2BAS-4 are of uncertain ori-gin but are thought to have been deposited at roughly the same time as KOL-GS-2(ca 134 14C ka BP (Haregidason et al 2000))
The limited distribution of these basaltic tephras a feature that is not unique toIcelandic basaltic material may reregect two factors the relative magnitude of the vol-canic eruptions from which they were derived and the limited aerial transportationof basaltic glass which is denser than rhyolitic material However a rather surpris-ing recent discovery is that of visible basaltic VA in a site on the Isle of Skye inthe Inner Hebrides Scotland (shy gure 5) (Davies et al 2001) All other occurrencesof VA in Scotland are exclusively of rhyolitic material and in micro-tephra formonly (Turney et al 1997 Turney 1998) Clearly basaltic tephra must have beentransported subaerially as far south as Skye and the reason why it has not beendetected at other sites in Scotland is puzzling We suspect that this partly reregectsthe laboratory methods employed to separate glass shards present in low concentra-tion within a micro-tephra layer from the host sediment The technique used is adensity-separation (regotation) procedure (Turney 1998) and as basaltic shards havea specishy c density similar to quartz one of the most abundant minerals in lake sedi-ments of Late Glacial age basaltic material is dimacr cult to detect using this methodThis hypothesis is currently under investigation and alternative detection methodsare being explored including magnetic separation (Mackie et al 2002)
Several other events listed in table 1 that are of probable Icelandic origin includetephras recorded in the GRIP ice core including visible (eg the `Black Featherrsquo)tephras as well as uncertain tephras inferred from distinct Ca peaks (S Johnsen2001 personal communication) No glass shards have yet been detected in the latterbut a volcanic origin is assumed because high Ca peaks are associated with knowntephras in other Greenland ice cores (S Johnsen 2001 personal communication)These are referred to as `unknownrsquo in table 1 No geochemical analyses are availablefrom these horizons so their origin must remain speculative but a possible source isIceland in view of its proximity to the Greenland ice sheet and assumed atmosphericcirculation patterns
(b) Eifel province
There are two prominent tephra events dated to the Termination 1Early Holocenetime-span that originated from the Eifel province the Laacher See Tephra (LST)and the Ulmener Maar Tephra (UMT) Visible occurrences of the LST indicate that
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European tephrochronological framework for Termination 1 783
Vedde Ash
615 625 635 645 655depth (cm)
organic lake mudsHolocene
silty clayGS-1Younger Dryas
organic lake mudsGI-1Alleroslashd
100 microm
(a)
(b)
Figure 5 (a) Photograph of the visible VA layer discovered at Loch Ashik Isle of Skye InnerHebrides Scotland (b) Light microscope photograph showing the rich content of basaltic shards(examples are indicated by the arrows) within this layer (8024 m m size fraction)
this ash was dispersed over much of central Europe (van den Bogaard amp Schmincke1985 Friedrich et al 1999 Litt amp Stebich 1999) The LST is dated by radiocarbonto ca 110 14C ka BP (van den Bogaard amp Schmincke 1985) and to 11 063sect12 14C BP(Friedrich et al 1999) by varve chronology to 1288 varve ka BP (Brauer et al 1999Litt et al 2001) and by ArAr dating to 129 ka cal BP (van den Bogaard 1995) Ithas a phonolitic composition and is thought to have originated from a plinian andphreatomagmatic eruption with the distal ash being carried in three distinct plumesone to the northeast towards Poland one to the west and the third to the southcovering the Jura Mountains and north Italy (van den Bogaard amp Schmincke 1985Juvigne et al 1995 Bossuet et al 1997) This pattern is thought to reregect altitu-dinal variations in the predominant wind direction Sedimentary sequences near thevolcanic source indicate that the LST consists of three main layers which represent
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784 S M Davies and others
dinoterent eruption phases These are grouped together as the Laacher See TephraFormation but the three individual units can be traced within and between a seriesof depositional fans The geochemical data obtained from these three LST layersshow signishy cant variations as reregected in the ternary plots (shy gure 4)
The Early Holocene Ulmener Maar Tephra (UMT) is of rhyolitic composition andappears to be restricted to sites in Germany though this conclusion is also based onrecords of visible tephras only It is dated to ca 956 14C ka BP and to 110 varve ka(Zolitschka et al 1995 Litt et al 2001)
(c) Massif Central province
The Massif Central tephras are mainly of basaltic trachyandesitic compositionwhich is distinct from the other ash provinces (shy gures 3 and 4) and their known dis-tributions are mostly conshy ned to the Massif Central region The ages of the MassifCentral tephras are based on radiocarbon dates obtained from mire and lake sedi-ments which `bracketrsquo the tephras The La Nugsup3ere Tephra with an age of 114 14C kaBP is the oldest Massif Central tephra identishy ed so far within the time-span of inter-est (Etlicher et al 1987 Juvigne et al 1996) The two Godivelle Tephras (5 and 4)are close in age but extensive radiocarbon dating suggests distinct ages of 107and 103 14C ka BP respectively (Juvigne et al 1996) The age of the Puy de DomeTephra is less certain as the estimate is based on only one radiocarbon date froma site in the southern Chaplusmn ne des Puys (table 1) This tephra is thought to havea trachyte composition (Juvigne 1993) although no major element concentrationshave yet been published
The ChopineKilianVasset tephras are thought to be derived from three separateEarly Holocene eruptions although the stratigraphic succession is not known atpresent These trachytic tephras have been radiocarbon dated to ca 854sect150 14C kaBP but are thought to have erupted separately within ca 260 yr (Juvigne et al 1996) This series of tephras is considerably more widespread than the others fromthe region having been identishy ed as far east as the Jura Mountains (Martini amp Duret1965 Martini 1970) Some other ash falls that originated from the Chaplusmn ne des Puysappear to be of local importance only (Vernet et al 1998 Vernet amp Raynal 2001)Geochemical data are currently available for only three of the Massif Central tephrasand so far as is known no attempt has yet been made to identify these tephras inmicro-tephra form
(d ) Italian provinces
The Italian tephras from this period can be assigned to three main volcanic com-plexes the Campanian volcanic shy elds around Naples Etna on Sicily and the AeolianIslands The Campanian complex which includes the Phlegrean Fields Vesuviusand Ischia is mainly trachytic in composition with a geochemical spectrum that isquite distinct from those of the Etna complex and of the Aeolian Islands (shy gure 3)Tephras originating from one or more of these three complexes have been detectedin marine cores from the Tyrrhenian and Adriatic seas as well as other parts of theMediterranean Sea (Keller et al 1978 Paterne et al 1986 1988 1990 Langone etal 1996) and in lake sequences in southern Italy such as Lago Grande di Monticchio(Newton amp Dugmore 1993 Narcisi 1996 Allen et al 1999) and central Italy such asLago Albano near Rome (Calanchi et al 1996) Some work has also been conducted
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European tephrochronological framework for Termination 1 785
in or close to the volcanic source areas in an attempt to establish the full sequenceof volcanic eruptions during the Late Quaternary (see for example Di Vito et al 1999) There are nine Italian tephras reported from marine and lake sequences thatdate from the period between 185 and 80 14C ka BP In all instances the recordsare of visible layers of tephra The ages of some of these are poorly established atpresent with conregicting data obtained from dinoterent sites The ages suggested intable 1 are those favoured in the most recent publications but these may requirere-assessment in the light of future research
The two oldest known tephras in the time-period of interest are the L9 and Green-ish Tephras both recorded as separate features within the annually laminated Lagodi Monticchio maar sequence The lowest of the two L9 is considered to be the cor-relative of the `basalrsquo plinian eruption of Vesuvius (Narcisi 1996) Age estimates ofa palaeosol that underlies the Vesuvius tephra sequence are ca 1617 14C ka BP forthis event (Delibrias et al 1979) L9 has a trachytic composition very similar to theGreenish Tephra (table 1) However L9 which is also a product of Vesuvius is foundstratigraphically below the Greenish Tephra in the Lago di Monticchio core TheGreenish Tephra is dated in the Monticchio sequence to 17 560 varve yr BP (Allenet al 1999) and has a calibrated radiocarbon age estimate of 17 830 sect 300 cal BP(Andronico et al 1995) Both tephras have a dominantly eastwards dispersal basedon the occurrences of visible layers (Santacroce 1987 Narcisi 1996) Both tephrasalso have a trachytic composition and as can be seen from table 1 the reportedgeochemical spectra are very close indeed with the standard deviations overlappingfor almost every major element This could present problems for tephrostratigra-phy where only one of the tephras is evident in a sediment sequence in particularbecause they are so close in age This is a good example of where an analysis oftrace and rare earth elements might be required to make a clear distinction betweentephras with very similar major oxide concentrations
The Y-1 Tephra also termed the Biancavilla Montalto Ignimbrite (Vezzoli 1991)is a product of Etna and has been identishy ed as a visible benmoritic tephra horizonthroughout the central Mediterranean (Paterne et al 1988) including central Italyand the Adriatic Sea (Vezzoli 1991 Narcisi 1993 Calanchi et al 1996) It has anestimated age of ca 140 14C ka BP The Unita dei Tefra Superiori tephra which hasbeen detected as far east as Lago di Monticchio in south-central Italy (Narcisi 1996)is also dated to ca 140 14C ka BP (Alessio et al 1976) but it is thought that thesource of this tephra lies in the Phlegrean Fields No geochemical data are availablefrom the presumed source region|the data reported in table 1 were obtained fromthe Lago di Monticchio record (Narcisi 1996)
The NYT which is equivalent to the C-2 tephra reported from various marinesequences has also been traced throughout central Italy and the Adriatic Sea (Pat-erne et al 1988 Calanchi et al 1996 Di Vito et al 1999) (shy gure 2) In the centralApennines region it formed the parent material for a soil that started to developat the beginning of the Holocene period (Frezzotti amp Narcisi 1996) Also originatingfrom the Campi Flegrei caldera it is dated to ca 120 14C ka BP (Di Vito et al 1999) Published geochemical data based on EDS indicate three dinoterent geochemicalpopulations varying from latite to phonotrachyte in composition (Orsi et al 1992Paterne et al 1988) (table 1) We report in x 4 of this paper on new data obtainedfrom the NYT by WDS and it is the mean of these new data that is included intable 1 Comparisons with the previously published EDS data are provided (table 1)
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786 S M Davies and others
The new data indicate clearly that the NYT originated from the Campanian volcaniccentre
In the interval between the dispersal of the NYT (ca 120 14C ka BP) and 95 14Cka BP there appear to have been as many as 34 eruptions in the Campi Flegrei caldera(Di Vito et al 1999) Of these only one appears to have been detected widely in theregion the Pomici Principali (also termed the Agnano Formation or C-1 tephra inmarine records (Paterne et al 1988) This was the product of the highest magnitudeeruption from this epoch and is dated to between 976 sect 300 and 1032 sect 50 14C kaBP (Delibrias et al 1979 Di Vito et al 1999) or to 122 varve ka BP based on theMonticchio varve chronology (Allen et al 1999) It is trachytic in composition andappears to have had a mainly eastwards dispersal
The Mercato Tephra dated to ca 80 14C ka BP and originally analysed usingEDS has a phonolitic composition and is believed to have been generated by Vesu-vius (Paterne et al 1988) New WDS data obtained from reference samples col-lected from an exposure to the west of Naples support these conclusions (table 1 andAppendix A) The silica content of the WDS analyses are ca 3 lower than thoseobtained using EDS (table 1) which may reregect the fact that the EDS data werenormalized
The only tephra listed in table 1 that is thought to have originated from the AeolianIslands is the Pollara pumice also referred to as the E2 tephra in marine sequences(Paterne et al 1986 1988) The limited geochemical data available so far suggest itto be the only Italian tephra listed in table 1 that is rhyolitic in composition Littlemore is known about this ash which has not been recorded extensively except thatits age is estimated to be ca 130 14C ka BP (Keller 1980)
5 Extending the known distributions of European tephras
Figure 2 summarizes schematically the known distributions of three of the tephrasreferred to in the preceding section the VA the LST and the NYT Following theintroduction of a laboratory method that enables the detection of micro-tephra parti-cles in mineral-rich sediment the VA has been traced to sites that are located muchfarther south (into The Netherlands) and east (as far as St Petersburg) than thedistribution limits based on occurrences of visible layers of the ash As a result con-tinental sequences over a much larger area in northern Europe can now be correlateddirectly with marine and ice-core records using the VA as a time-parallel marker
This suggests therefore that other prominent ash layers such as the LST andNYT should also be detectable over larger tracts of Europe than is presently thecase if suitable sites are examined for the presence of micro-tephra horizons To testthis assertion we examined lake sediment deposits of Last Termination age froma site in the northern Apennines in order to establish whether the NYT could bedetected in micro-tephra form The site selected Prato Spilla `Crsquo lies well to thenorth of the localities in central and southern Italy and in the Adriatic Sea fromwhich visible records of the NYT have been reported Prato Spilla `Crsquo lies at an alti-tude of ca 1350 m in the Appennino Parmense ca 60 km south of Parma and 15 kmeast of Pontremoli The site contains a continuous sediment sequence spanning theLast Termination and most of the Holocene Detailed pollen and coleopteran strati-graphical records which have been radiocarbon dated have been published for thissite (Lowe 1992 Ponel amp Lowe 1992 Lowe amp Watson 1993)
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Figure 6 Light microscope photograph of an NYT glass shard from Prato Spilla Crsquosequence assigned on geochemical grounds to the NYT
The methods adopted for sub-sampling of the Prato Spilla `Crsquo sequence for thequantishy cation of glass shard concentrations and for subsequent electron microprobeanalysis of selected glass shards followed those described elsewhere (Turney 1998)In summary contiguous samples of 1 cm stratigraphic interval were extracted fromthe sequence to establish presenceabsence of glass shards Each of the 1 cm3 blocksin which tephra particles was detected was then examined with more care andshard concentrations were quantishy ed for each sub-sample Micro-tephra particleswere detected in shy ve samples (shy gure 6) but were predominantly clustered around500 cm in the part of the sequence assigned on pollen-stratigraphic grounds to theLate Glacial Interstadial or the `Allerfrac12drsquo|indeed the part of the succession in whichthe NYT would be expected to occur Peak concentrations of micro-tephra particlesreach 225 shards cmiexcl3 and are conshy ned to a single 1 cm thick sample in the sequencewhich probably represents the time of maximum deposition of the ash
Electron microprobe measurements based on WDS were obtained from the surfacesof 21 separate glass shards extracted from the sample with peak shard concentrations(Appendix A) Since only EDS measurements were available for the NYT prior to thepresent study we also obtained WDS measurements from 17 shards extracted fromthe visible layer of NYT that is exposed on Procida Island which lies in the type-locality for the NYT close to the city of Naples (Appendix A) The results providenot only a more comprehensive geochemical dataset for the NYT than was previ-ously available but also a consistent basis for comparison with the Prato Spilla `Crsquodataset All of the WDS data reported here (Appendix A) were measured at the samelaboratory (Tephrochronology Analytical Unit University of Edinburgh) using thesame sample pretreatment and preparation protocol The WDS results for the NYTdinoter to a minor degree from the EDS results (table 1 and Appendix A) especiallywith respect to the amounts of silica aluminium and calcium measured The EDS
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788 S M Davies and others
4 8FeO ()
TiO
2 (
) Neapolitan Yellow Tuff(Procida)Neapolitan Yellow Tuff(Prato Spilla lsquoCrsquo)
0
1
2
3
40 50 60 70
MgO
(
)
SiO2 ()
K2O
(
)
40 50 60 70
0
04
08
4
8
12
SiO2 ()
(a)(b)
(c)
Figure 7 Bi-plots of SiO2 K2 O SiO2 MgO and FeOTiO2 for the WDS analyses obtainedfrom glass shards of the NYT from Procida (Naples) and Prato Spilla Crsquo Means and standarddeviations are shown
results show a higher degree of statistical scatter than the WDS measurements whichmay reregect the fact that the data were normalized combined with the inreguence ofvariation in water content between shards
There is a very close correspondence between the WDS data for the Prato Spilla `Crsquomicro-tephra shards and those obtained from the type-material near Naples (shy g-ure 7) The geochemical data strongly suggest therefore that the NYT is representedat the Prato Spilla `Crsquo site by a discrete layer of micro-tephra particles This conclu-sion is compatible with the pollen-stratigraphic data from the site and accords withage estimates for the NYT (ca 120 14C ka BP) obtained from other sites (Paterneet al 1990)
These results encourage us to believe that many if not all of the tephras listedin table 1 will be detectable over much larger tracts of Europe than is presently thecase if appropriate research is undertaken to detect layers of micro-tephra particlesin selected sites The authors are presently engaged in a major continent-wide pro-gramme of research in collaboration with a number of European research groupsdesigned to test this hypothesis The focus in this research is on those parts of Europewhere we expect to shy nd overlapping `apronsrsquo of tephra deposition originating fromthe Italian Eifel Massif Central and Icelandic provinces For example a number ofsites in parts of southern France northern Italy and perhaps western Switzerlandmay have received inreguxes of micro-tephra originating from the Italian and Eifelprovinces and perhaps also from the Massif Central Sites in parts of Germany Den-mark and southern Sweden for example may in turn have received tephra depositsfrom both of the Icelandic and Eifel provinces If this proves to be the case then thestage will be set for the construction of a tephrostratigraphical framework for Europewhich will enable Last Termination sequences to be correlated on a continent-widebasis using micro- and visible tephra layers as time-parallel stratigraphic markersFurthermore there is also the possibility that other tephras remain to be discovered
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European tephrochronological framework for Termination 1 789
those which either because of the magnitude or nature of some volcanic eruptionswere distributed over parts of Europe in micro-tephra form only
6 European tephrostratigraphy and the chronology of eventsduring the Last Termination and Early Holocene
One of the crucial issues in Late Quaternary palaeoenvironmental research thatremains to be resolved is the degree to which climatic events inferred from oceanicterrestrial and ice-core records were synchronous during the Last Termination andEarly Holocene If the ice-core records provide realistic estimates of the rates anddurations of climatic events during this period then comparisons between individ-ual records have to be enotected with at least a decadal precision The problem thispresents and the role that tephrostratigraphy can play in resolving some of thedimacr culties involved are put into perspective in shy gure 8
Figure 8 shows some of the data used to calibrate radiocarbon dates (the LakeSuigetsu and Cariaco Basin datasets) plotted against the GRIP ss08c ice-core recordof macr 18O variations The latter has been selected by the INTIMATE group as an arbi-trary and temporary standard for this period and used to deshy ne an event stratig-raphy scheme (shy gure 1) for the Last Termination (see Bjorck et al 1998 Walker etal 2001) As has been alluded to in earlier sections of this paper the uncertaintiesassociated with all of the dating methods currently employed preclude precise com-parisons of ice-core marine and terrestrial records Oceanic and terrestrial recordsmostly rely upon radiocarbon dating locally supplemented in a few cases by varvechronology Imprecisions in radiocarbon dates can arise through site-specishy c fac-tors (eg hard-water or mineral carbon errors in freshwater sequences and reservoirerrors in marine sequences) sample selection laboratory measurements of 14C activ-ity and other factors (Lowe amp Walker 2000) Further imprecision may be introducedby the calibration of radiocarbon dates since the uncertainties in the dataset usedto calibrate pre-Holocene radiocarbon dates INTCAL98 are far higher than forthe Holocene which is based on dendro-calibration (Stuiver et al 1998) There arealso uncertainties anotecting varve chronologies while the ss08c ice-core chronologyfor the Last Termination dinoters signishy cantly from the GISP2 record and indeedfrom other models of the GRIP record (Lowe et al 2001) Published comparisonsbetween ice-core marine and terrestrial records for the Last Termination seldom takeinto account the true magnitude of the dating uncertainties involved and frequentlyemploy circular reasoning
Figure 8 shows the positions on the radiocarbon time-scale of 20 of the tephrasdiscussed earlier in this paper these being the ones for which reasonably conshy dentradiocarbon age estimates can be made (though these will be subject to revised esti-mates in the future) A high number of these occur in the period 14080 14C kaBP but we conshy dently anticipate the discovery in the future of additional tephras(perhaps in micro-tephra form only) which will date to the period 185140 14C kaBP Tephras detected in the GRIP ice core over the same time-interval are plottedon the calendar time-scale in shy gure 8 By providing key `time-linesrsquo between recordstephrostratigraphy can help to resolve some of the dating uncertainties referredto earlier by for example enabling direct comparisons of discrepant age estimatesobtained using dinoterent methods (cf Litt et al 2001) It can also provide estimatesof the magnitudes of the reservoir errors that anotected various marine sectors at dif-
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790 S M Davies and others
-44
-40
-36
-32
cale
ndar
yea
rs B
P
8000
9000
10 0
00
11 0
00
12 0
00
13 0
00
14 0
00
15 0
00
16 0
00
17 0
00
18 0
00
14C age (BP)
VA
SA
Un
Un
Un
Un
Un
BF
Hol
ocen
eG
S-1
GI-
1aG
I-1b
GI-
1cG
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GI-
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S-2
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S-2
bG
S-
2c
Bor
robo
l
La
Nug
egravere
Laa
cher
See
God
ivel
le 5
amp I
-TH
OL
-2
Puy
de D
ocircme
I-T
HO
L-1
Saks
unar
vatn
Houmlg
stor
psm
osse
nU
lmen
er M
aar
amp L
3574
radiocarbon dated European tephra horizons
Cho
pine
Kili
an V
asse
tM
erca
to
God
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le 4
Pom
ici P
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ipal
i amp V
edde
Polla
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-GS-
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GS
-2B
AS-
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AS-
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Gre
enis
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20 0
0018
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12 0
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800
600
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GISP2 volcanicsulphate conc (ppb)
1000
Nea
polit
an Y
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uff
GISP2 18O (permil) dGRIP 18O (permil) d
Figure 8 For description see opposite
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 791
ferent times through a comparison of radiocarbon dates obtained from marine andterrestrial horizons in which the same tephra has been detected (see for exampleAustin et al 1995 Bondevik et al 2001 Haregidason et al 2000) Tephrostratigraphymay provide an independent test of suggestions that some of the climatic changesduring the Last Termination were time-transgressive as illustrated for some appar-ently contrasting climatic trends in Iceland Britain and NW Russia (Lowe 2001) Ofparticular importance as far as establishing `leadsrsquo and `lagsrsquo in climatic changes isconcerned are the tephra records from the Greenland ice cores The discovery of theVedde and Saksunarvatn ashes in the GRIP record (Gronvold et al 1995) alreadyprovides a basis for making direct comparisons between marine terrestrial and ice-core records It is a matter of some urgency that the incidence of tephra depositsin the Greenland ice cores be more fully explored in the hope that this will lead tothe recognition of additional time-parallel links between the ice-core records on theone hand and oceanic and terrestrial records on the other An investigation of thenew NordGRIP record for this purpose is currently in progress (S M Davies 2002unpublished data)
Finally a fuller and more reshy ned tephrostratigraphical scheme for Europe will alsohave other applications It will provide an important database for those investigatingthe timing and frequency of volcanic eruptions in Europe during the past 20 000 yror so as well as of the geochemical evolution of the dinoterent volcanic centres overthat period A fuller record of the distribution of micro-tephras may also provideinformation on atmospheric circulation patterns during the dispersal and depositionperiods as well as on the nature and altitude of the eruption columns which mayin turn provide inferences about magma viscosity
This paper is a contribution to the INTIMATE project of the INQUA Palaeoclimate Com-mission and the work is supported by a Leverhulme Trust Research project (grant allocationnumber F07537C) entitled Testing hypotheses of rapid climate change using tephrochronol-ogyrsquo SMDrsquo s contribution was completed during possession of a NERC PhD studentship(GT 0499ES162) We are extremely grateful to Dr Peter G Hill for his assistance withthe EPMA analyses at the Tephrochronology Analytical Unit University of Edinburgh We alsothank Dr G Mastrolorenzo (Vesuvius Observatory) and Miss G Swindle for assistance duringthe macreld investigations in Naples Thanks are also expressed to two anonymous reviewers forcomments on an earlier draft
Appendix A
Table 2 shows the major oxide concentrations of NYT glass shards from Procidaand Prato Spilla `Crsquo and of the Mercato Tephra from the Naples area (see x 4 forsite context) All oxides are shown as weight and total iron is expressed as FeO
Figure 8 Radiocarbon calibration curve for Termination 1 and the Early Holocene compared with theGRIP macr 18 O event stratigraphy the GRIP ss08c and GISP2 macr 18 O records (wwwngdcnoaagov) andknown tephra horizons from this period The shaded areas represent the cooler climatic episodes andare labelled with the Greenland stratotype terminology (Bjorck et al 1998) Where radiocarbon agesare reported in table 1 as a range the mean is given here Abbreviations for GRIP horizons are asfollows Un unknown (approximate positions are given (S Johnsen 2001 personal communication))SA Saksunarvatn Ash VA Vedde Ash BF Black Feather Sulphate concentrations from the GISP2record are also shown (Zielinski et al 1996) Open circles denote radiocarbon calibration data fromLake Suigetsu (Kitagawa amp van der Plicht 2000) Filled circles denote radiocarbon calibration data fromCariaco Basin assuming a marine reservoir age of 420 14 C yr (Hughen et al 1998)
Phil Trans R Soc Lond A (2002)
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792 S M Davies and others
Tab
le2
Majo
roxi
de
con
cen
trati
on
sof
NY
Tgl
ass
shard
sfr
om
Pro
cida
an
dP
rato
Spil
laC
rsquoan
dof
the
Mer
cato
Tep
hra
from
the
Naple
sare
a(s
eex4
for
site
con
text
)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
roci
da)
1584
204
0177
634
201
106
828
635
197
5969
1W
DS
2598
603
9178
027
101
204
924
244
583
4965
8W
DS
3586
604
5173
631
100
805
924
342
183
0951
9W
DS
4583
903
9177
933
000
906
924
540
486
9958
3W
DS
5605
106
8179
126
901
204
923
243
086
1976
4W
DS
6591
704
5177
332
801
006
425
740
887
8968
0W
DS
7581
804
1178
031
501
107
125
640
086
9956
1W
DS
8589
504
2179
533
701
506
926
740
987
5970
4W
DS
9592
003
9178
135
101
007
026
443
585
7972
7W
DS
10
591
404
2174
631
601
105
723
442
482
6957
0W
DS
11
593
403
6177
131
301
506
726
439
188
5967
6W
DS
12
588
103
8176
128
100
505
525
141
583
4952
1W
DS
13
577
003
8176
533
500
807
228
140
384
8952
0W
DS
14
586
004
7179
735
300
706
827
842
984
6968
5W
DS
15
588
104
2180
629
400
505
924
937
993
0964
5W
DS
16
579
603
9178
536
501
308
228
836
087
1959
9W
DS
17
580
103
9177
631
500
907
327
039
488
9956
6W
DS
mea
n588
104
2177
631
901
006
525
940
686
9962
8
sd
(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(07
8)
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 793
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
rato
Spil
laC
rsquo)
1552
105
4177
247
401
914
38
735
578
9951
1W
DS
2557
305
7179
845
701
512
640
136
581
5960
6W
DS
3595
004
4173
724
302
003
117
652
877
8950
7W
DS
4575
704
2179
433
001
406
627
043
083
6953
7W
DS
5599
904
0178
826
401
304
421
841
688
4966
5W
DS
6591
103
8177
826
601
105
022
443
888
8960
2W
DS
7565
304
5180
939
501
410
532
535
791
8962
1W
DS
8597
606
9180
826
501
604
821
546
684
6970
7W
DS
9571
805
6179
939
801
109
932
240
883
6964
7W
DS
10
588
603
7176
527
601
104
721
042
487
7953
3W
DS
11
559
404
9180
544
501
812
339
435
878
6957
2W
DS
12
594
704
0181
328
301
705
522
144
785
6967
9W
DS
13
611
103
7187
016
900
802
419
938
195
9975
8W
DS
14
599
204
4181
128
601
404
620
844
986
6971
6W
DS
15
601
204
4177
328
302
004
722
446
385
5972
1W
DS
16
595
104
5176
428
801
504
722
744
884
3962
8W
DS
17
603
704
1177
825
101
503
520
348
181
2965
3W
DS
18
558
704
5179
647
401
813
139
836
879
0960
7W
DS
19
589
602
8178
830
901
606
622
436
091
8960
5W
DS
20
553
606
3178
647
401
913
840
136
978
0956
6W
DS
21
579
004
0175
739
000
708
328
338
286
7959
9W
DS
mea
n582
804
6179
033
401
507
427
341
484
8962
1
sd
(1
87)
(01
0)
(02
7)
(09
2)
(00
4)
(03
9)
(08
0)
(04
9)
(05
0)
(07
0)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
794 S M Davies and others
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)
1575
202
7194
219
701
101
016
374
766
9951
8W
DS
2575
802
9194
523
902
201
520
273
564
5959
0W
DS
3574
301
4205
219
101
100
416
481
266
1965
2W
DS
4575
500
7206
018
002
000
415
181
669
3968
6W
DS
5580
000
9208
018
601
300
515
883
367
1975
5W
DS
6571
001
0206
016
101
600
515
078
967
1957
2W
DS
7577
501
1201
117
101
500
620
675
655
4950
5W
DS
8573
700
9212
717
101
900
815
187
564
2973
9W
DS
9580
301
3208
715
801
400
824
81
754
1968
1W
DS
10
574
400
6211
18
402
00
516
480
567
8971
6W
DS
11
577
200
7214
212
501
200
829
879
247
962
6W
DS
12
572
200
9211
217
301
501
15
980
465
9966
3W
DS
13
571
800
7210
417
402
201
16
184
467
2971
2W
DS
14
567
300
9208
916
901
400
917
383
262
5959
3W
DS
15
568
600
8205
918
202
101
414
682
666
6960
8W
DS
16
572
501
1211
318
202
01
215
884
364
5970
9W
DS
17
572
901
2212
916
502
101
215
883
667
2973
4W
DS
18
573
01
4211
716
301
801
416
83
365
5970
4W
DS
19
569
201
1207
418
602
101
414
982
964
961
6W
DS
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
3)
(04
2)
(01
3)
(00
1)
(00
2)
(01
)(0
39)
(01
1)
(02
5)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
References
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Hughen K A Overpeck J T amp Lehman J 1998 A new 14 C calibration data set for the LastDeglaciation Radiocarbon 39 483494
Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
Hunt J B amp Hill P G 1996 An inter-laboratory comparison of the electron probe microanalysisof glass geochemistry Quat Int 3436 229241
Hunt J B amp Hill P G 2001 Tephrological implications of beam sizesample size ereg ects inelectron microprobe analysis of glass shards J Quat Sci 16 105117
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Juvignparae E amp Gewelt M 1987 La Narse drsquo Ampoix comme tparaephrostratotype dans la Chasup3 ne desPuys mparaeridionale (France) Bull Ass Fr Etud Quat 29 3749
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Juvignparae E Bastin B Delibrias G Evin J Gewelt M Gilot E amp Streel M 1996 Acomprehensive pollen and tephra based chronostratigraphic model for the Lateglacial andHolocene period in the French Massif Central Quat Int 3436 113120
Keller J 1980 The island of Vulcano Rend Soc It Mineral Petrolog 36 369414
Keller J Ryan W B F Ninkovich D amp Altherr R 1978 Explosive volcanic activity in theMediterranean over the past 200 000 years as recorded in deep sea sediments Geol Soc AmBull 89 591604
Kitagawa H amp van der Plicht J 2000 Atmospheric radiocarbon calibration beyond 11 900 calBP from Lake Suigetsu laminated sediments Radiocarbon 42 369380
Kvamme T Mangerud J Furnes H amp Ruddiman W F 1989 Geochemistry of Pleistoceneash zones in cores from the North Atlantic Norsk Geol Tids 69 251272
Lacasse C Sigurdsson H Johannesson H Paterne M amp Carey S 1995 Source of Ash zone 1in the North Atlantic Bull Volcanol 57 1832
Langone L Asioli A Corregiari A amp Trincardi F 1996 Age depth modelling through theLate-Quaternary deposits of the central Adriatic Basin In Palaeoenvironmental analysis ofItalian crater lake and Adriatic sediments (ed F Oldmacreld amp P Guilizzoni) vol 55 pp 177196 Memorie dellrsquo Instituto Italiano di Idrobiologia
Larsen G 2000 Holocene volcanism in Iceland and tephrochronology as a tool in volcanologyIn Iceland 2000 modern processes and past environments Keele University UK
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 799
Litt T amp Stebich M 1999 Bio- and chronostratigraphy of the Lateglacial in the Eifel regionGermany Quat Int 61 516
Litt T Brauer A Goslar T Merkt J Balaga K Muller H Ralska-Jasiewiczowa MStebich M amp Negendank J F W 2001 Correlation and synchronisation of Lateglacialcontinental sequences in northern Central Europe based on annually laminated lacustrinesediments Quat Sci Rev 20 12331249
Long D amp Morton A C 1987 An ash fall within the Loch Lomond stadial J Quat Sci 297101
Lotter A F Eicher U Siegenthaler U amp Birks H J B 1992 Lateglacial climatic oscillationsas recorded in Swiss lake sediments J Quat Sci 7 187204
Lowe J J 1992 Lateglacial and Early Holocene lake sediments from the Northern ApenninesItaly|pollen stratigraphy and radiocarbon dating Boreas 21 193208
Lowe J J 2001 Abrupt climatic changes in Europe during the last glacialinterglacial tran-sition the potential for testing hypotheses on the synchroneity of climatic events usingtephrochronology Global Planet Change 603 7384
Lowe J J amp Turney C S M 1997 Vedde Ash layer discovered in a small lake basin on theScottish mainland J Geol Soc Lond 154 605612
Lowe J J amp Walker M J C 2000 Radiocarbon dating the last glacialinterglacial transition(ca 14914 C ka BP) in terrestrial and marine records the need for new quality assuranceprotocols Radiocarbon 42 5368
Lowe J J amp Watson C 1993 Lateglacial and Early Holocene pollen stratigraphy of the northernApennines Italy Quat Sci Rev 12 727738
Lowe J J Birks H H Brooks S J Coope G R Harkness D D Mayle F E SheldrickC Turney C S M amp Walker M J C 1999 The chronology of palaeoenvironmental changesduring the Last GlacialHolocene transition towards an event stratigraphy for the BritishIsles J Geol Soc Lond 156 397410
Lowe J J Hoek W Z amp INTIMATE group 2001 Inter-regional correlation of palaeoclimaticrecords for the Last GlacialInterglacial transition a protocol for improved precision recom-mended by the INTIMATE project group Quat Sci Rev 20 11751187
Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
Mangerud J Lie S E Furnes H Kristiansen I L amp Liquest mo L 1984 A Younger Dryas ashbed in western Norway and its possible correlation with tephra beds from the Norwegian Seaand North Atlantic Quat Res 21 85104
Mangerud J Furnes H amp Jparaohansen J 1986 A 9000 year-old ash bed on the Faroe IslandsQuat Res 26 262265
Martini J 1970 Recherche de retombparaees volcaniques dans le sud-est de la France et la Suisseoccidentale Arch Sci 23 641674
Martini J amp Duret J J 1965 Note preliminaire sur la presence drsquo un niveau de cendres vol-caniques dans des sparaediments post-glaciaires des environs de Genmicroeve Arch Sci 18 587588
Mayewski P A Meeker L D Twickler M S Whitlow S Yang Q Lyons W B amp Pren-tice M 1997 Major features and forcing of high latitudes Northern Hemisphere atmosphericcirculation using a 110 000 year long glaciochemical series J Geophys Res 102 345365
Merkt J Muller H Knabe W Muller P amp Weiser T 1993 The Early Holocene Saksunarvatntephra found in lake sediments in NW Germany Boreas 22 93100
Narcisi B 1993 Segnalazione di un livello piroclastico di provenienza etnea nellrsquo area del Fucino(Italia Centrale) Quaternario 6 8792
Narcisi B 1996 Tephrochronology of a Late Quaternary lacustrine record from the Monticchiomaar (Vulture volcano southern Italy) Quat Sci Rev 15 155165
Phil Trans R Soc Lond A (2002)
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Newton A J amp Dugmore A J 1993 Tephrochronology of Core C from Lago Grande di Mon-ticchio In Paleolimnology of European Maar Lakes (ed J F W Negendank amp B Zolitschka)Lecture Notes in Earth Science vol 49 333348 Springer
Oldmacreld F Appleby P G amp Thompson R 1980 Palaeoecological studies of lakes in theHighlands of Papua New Guinea J Ecol 68 457477
Orsi G Drsquo Antonio M de Vita S amp Gallo G 1992 The Neapolitan Yellow Tureg a large mag-nitude trachytic phreatoplinian eruption eruptive dynamics magma withdrawal and calderacollapse J Volcanol Geotherm Res 53 275287
Paterne M Guichard F Labeyrie J Gillot P Y amp Duplessy J C 1986 Tyrrhenian Seatephrochronology of the oxygen isotope record for the past 60 000 years Mar Geol 72259285
Paterne M Guichard F amp Labeyrie J 1988 Explosive activity of the south Italian volca-noes during the past 80 000 years as determined by marine tephrochronology J VolcanolGeotherm Res 34 153172
Paterne M Labeyrie J Guichard F Mazaud A amp Maitre F 1990 Fluctuations of the Cam-panian explosive volcanic activity (south Italy) during the past 190 000 years as determinedby marine tephrochronology Earth Planet Sci Lett 98 166174
Pawse A Beske-Diehl S amp Marshall S A 1998 Use of magnetic hysteresis properties andelectron spin resonance spectroscopy for the identimacrcation of volcanic ash a preliminary studyGeophys J Int 132 712720
Pearce N J G Westgate J A amp Perkins W T 1996 Developments in the analysis of singleglass shards in volcanic deposits by laser ablation ICP-MS quantitative and single internalstandard multi-element methods Quat Int 3436 213227
Pearce N J G Westgate J A Perkins W T Eastwood W J amp Shane P 1999 Theapplication of laser ablation ICP-MS to the analysis of volcanic glass shards from tephradeposits bulk glass and single shard analysis Global Planet Change 21 151171
Pilcher J R amp Hall V A 1992 Towards a tephrochronology for the Holocene of the north ofIreland Holocene 2 255259
Ponel P amp Lowe J J 1992 Coleopteran pollen and radiocarbon evidence from the Prato Spillarsquo Drsquo succession N Italy C R Acad Sci Paris Sparaer II 315 14251431
Rose N L Golding P N E amp Battarbee R W 1996 Selective concentration and enumerationof tephra shards from lake sediment cores Holocene 6 243246
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Ruddiman W amp McIntyre A 1981 The North Atlantic Ocean during the last deglaciationPalaeogeogr Palaeoclimatol Palaeoecol 35 145214
Santacroce R 1987 Somma Vesuvius Quad Ric Sci 114 252
Sarna-Wojcicki A 2000 Tephrochronology In Quaternary geochronology methods and applica-tions (ed J S Noller J M Sowers amp W R Lettis) AGU Reference shelf vol 4 pp 357377Washington DC American Geophysical Union
Sejrup H P Sjiquest holm J Furnes H Beyer I Eide L Jansen E amp Mangerud J 1989Quaternary tephrochronology on the Iceland Plateau north of Iceland J Quat Sci 4 109114
Sikes E L Samson C R Guilderson T P amp Howard W R 2000 Old radiocarbon agesin the southwest Pacimacrc Ocean during the last glacial period and deglaciation Nature 405555558
Stein R Nam S-I Grobe H amp Hubbersten H 1996 Late Quaternary glacial history andshort term ice rafted debris deg uctuations along the East Greenland continental marine In LateQuaternary palaeoceanography of the North Atlantic margins (ed J T Andrews W E NAustin H Bergsten amp A E Jennings) pp 135151 Geological Society London SpecialPublication
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 801
Stuiver M amp Grootes P M 2000 GISP2 oxygen isotope ratios Quat Res 53 277284
Stuiver M Reimer P J Bard E Beck J W Burr G S Hughen K A Kromer BMcCormac G Van der Plicht J amp Spurk M 1998 INTCAL 98 radiocarbon age calibration24 0000 cal BP Radiocarbon 40 10411083
Sweatman T R amp Long J V P 1969 Quantitative electron microprobe analysis of rock formingminerals J Petrol 7 332379
Turney C S M 1998 Extraction of rhyolitic ash from minerogenic lake sediments J Paleolim-nol 19 199206
Turney C S M amp Lowe J J 2001 Tephrochronology In Tracking environmental changes inlake sediments physical and chemical techniques (ed W M Last amp J P Smol) DordrechtKluwer Academic
Turney C S M Harkness D D amp Lowe J J 1997 The use of microtephra horizons tocorrelate Lateglacial lake sediments successions in Scotland J Quat Sci 12 525531
Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
van den Bogaard P amp Schmincke H 1985 A widespread isochronous Late Quaternary tephralayer in central and northern Europe Geol Soc Am Bull 96 15541571
van den Bogaard B Dordeg er W Sandgren P amp Schmincke H-U 1994 Correlating theHolocene records Icelandic tephra found in Schleswig-Holstein (northern Germany) Natur-wissenschaften 81 554556
Vernet G amp Raynal J-P 2001 Tephrostratigraphy of the Limagne revisited Implications forLateglacial and Holocene Prehistory In Tephras chronology archaeology (ed E Juvignparae ampJ-P Raynal) pp 111116 Dossiers de lrsquo ArchparaeoLogis no 1 France
Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
Vezzoli L 1991 Tephra layers in Bannock Basin (eastern Mediterranean) Mar Geol 1002134
von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
Walker M J C Bjorck S Lowe J J Cwynar L C Johnsen S Knudsen K-L WohlfarthB amp INTIMATE Group 1999 Isotopic events in the GRIP ice core a stratotype for the LatePleistocene Quat Sci Rev 18 11431150
Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
802 S M Davies and others
Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
774 S M Davies and others
Tab
le1
(Con
t)
(Th
evarv
eage
for
the
Gre
enis
h(I
T)rsquo
row
is17
560
yea
rs)
GR
IPage
tep
hra
age
(ss0
8c
volc
an
ich
ori
zon
(14C
yrs
)ti
me-
scale
)n
SiO
2T
iO2
Al 2
O3
FeO
Mn
OM
gO
CaO
Na
2O
K2O
P2O
5to
tal
EP
MA
sou
rce
ref
GS
-2B
AS
-213
400
6497
933
2122
4147
902
445
389
829
905
205
4979
4W
DS
26
(IC
)
GS
-2B
AS
-313
400
2538
529
9125
7131
203
132
174
729
507
707
7980
1W
DS
26
(IC
)
GS
-2B
AS
-414
000
7503
617
4145
1113
202
155
3100
528
010
5
975
7W
DS
26
(IC
)
Un
ita
dei
ca14
000
5648
804
7184
625
901
602
217
432
679
302
8100
ED
SP
hle
gre
an
3
27
Tef
ra(0
53
)(0
13
)(0
25)
(07
4)
(01
4)
(01
6)
(01
6)
(03
4)
(06
6)
(01
6)
Fie
lds
Su
per
iori
(IT
)
Y-1
(IT
)ca
14
000
16
600
413
7169
555
502
218
242
262
229
306
8100
ED
SE
tna
28
Bla
ck17
000
sect300
Fea
ther
(17890
m)
Gre
enis
hca
15
000
9618
704
190
731
601
804
328
531
586
202
6100
ED
SV
esu
viu
s3
4
(IT
)(0
70
)(0
08
)(0
45)
(06
8)
(01
0)
(01
0)
(05
9)
(05
3)
(05
8)
(01
6)
29
L9
(IT
)ca
16
000
15
626
704
4188
630
401
103
329
429
683
402
7100
ED
SV
esu
viu
s3
15
17
000
(14
2)
(01
4)
(07
2)
(11
1)
(00
9)
(02
4)
(06
6)
(04
8)
(06
5)
(01
8)
St
2-1
85
18
500
7504
015
1145
5112
002
466
9114
525
206
6
992
2W
DS
26
(IC
)
Ref
eren
ces
1
this
stu
dy
2
Pate
rne
etal
(1988)
3
Narc
isi
(1996)
4
All
enet
al
(1999)
5
An
dro
nic
oet
al
(1995)
6
Ju
vig
nparae
et
al
(1996)
7
Bir
ks
et
al
(1996)
8
Bjo
rck
ampW
ast
egordma
rd(1
999)
9
Du
gm
ore
ampN
ewto
n(1
998)
10
Bjo
rck
et
al
(1992)
11
Kva
mm
eet
al
(1989)
12
Zoli
tsch
ka
etal
(1995)
13
Ju
vig
nparae
ampG
ewel
t(1
987)
14
Di
Vit
oet
al
(1999)
15
Del
ibri
as
etal
(1979)
16
Ju
vig
nparae
etal
(1987)
17
Dav
ies
et
al
(2001)
18
van
den
Bogaard
ampS
chm
inck
e(1
985)
19
Fri
edri
chet
al
(1999)
20
Bra
uer
eta
l(1
999)
21
Etl
ich
eret
al
(1987)
22
Tu
rney
etal
(1997)
23
Pate
rne
et
al
(1986)
24
Kel
ler
(1980)
25
Eir
parasup3kss
on
etal
(2000)
26
Hadeg
idaso
net
al
(2000)
27
Ale
ssio
etal
(1976)
28
Vez
zoli
(1991)
29
San
tacr
oce
(1987)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 775
Altogether 34 tephra layers have been reported from sediment sequences in Europeand the NE Atlantic region which date to the period between 185 and 80 14C ka BP(table 1) Because tephra layers are deposited virtually instantaneously (in geologicalterms) they enotectively represent time-parallel marker horizons within stratigraphicalsequences (Westgate amp Gorton 1981 Sarna-Wojcicki 2000 Turney amp Lowe 2001) Intheory therefore all 34 tephras could prove valuable for correlation purposes eitherin a local context or in those cases where the ash deposits have been widely dispersedbetween regional sequences In practice however very little is known about the fullgeographical dispersal of the majority of the ash layers listed in table 1 Furthermorecorrelation by tephrostratigraphy will only work if the various ash layers have wellcharacterized geochemical signatures While some geochemical data are available forthe majority of the tephras listed in table 1 the collective data are far from robustand no geochemical data have yet been published for some
Nonetheless there is mounting evidence to show that some of the tephra depositslisted in table 1 are not only geochemically distinct but are also much more widelydispersed across Europe than was initially realized Stratigraphic records of thebetter-known tephras were initially limited to observations of visible tephra layersThe development of a technique that enables detection of tephra layers that are invis-ible to the naked eye (micro-tephra) in Late Glacial sequences has greatly extendedthe area over which some of the ashes can be traced (Lowe amp Turney 1997 Turneyet al 1997 Turney 1998 Wastegard et al 1998 2000a b) Most of this research sofar has focused on micro-tephra layers originating from Icelandic centres distributedthroughout northern Europe Here we report on further development of this line ofresearch with new evidence for the occurrence of micro-tephra layers in a site insouthern Europe The results suggest that there is great potential for tracing someash layers that originated from Italian volcanic complexes over much larger tracts ofsouthern and central Europe than records of visible tephra deposits allow This inturn greatly enhances the scope for making precise correlations not only betweenparts of southern Europe but also between continental and marine (MediterraneanSea) sequences
2 Micro-tephra extraction techniques
Micro-tephra horizons are composed of glass shards that are generally between 80and 24 m m (long axis) in size and that are present in such low concentration insedimentary sequences that they can only be detected by the use of a particle sep-aration technique Several factors inreguence the concentration of shards such as dis-tance from the volcanic source precipitation patterns during the eruption and sub-sequent tephra dispersal and sedimentary processes within the catchment In someterrestrial sequences micro-tephra horizons with a peak concentration (peak con-centration tends to coincide with the shy rst occurrence of glass shards in a sedimentsequence which is then taken to mark the time of maximum ash deposition) as lowas 10 shards cmiexcl3 has been conshy rmed whereas other sites have recorded as muchas 8000 shards cmiexcl3 (Turney et al 1997) In complete contrast tephra horizons inthe GRIP ice core have been identishy ed based on a single glass shard only (Gronvoldet al 1995)
Enotective separation techniques for the detection and isolation of tephra particlesfrom sedimentary sequences have been developed These include ashing of organic
Phil Trans R Soc Lond A (2002)
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776 S M Davies and others
matter (Pilcher amp Hall 1992) digestion of biogenic and opaline silica (Rose et al 1996) the use of magnetic properties of ash layers (see for example Oldshy eld et al 1980 van den Bogaard et al 1994 Pawse et al 1998) X-ray analysis (Dugmore ampNewton 1992) and a density separation (regotation) technique (Turney 1998) Den-sity separation has proved exceedingly useful for the detection of small glass shardspresent in low concentrations in mineral-rich Late Glacial sediments This involvesthe separation and concentration of particles of predetermined specishy c gravity withthe use of a heavy liquid and subsequent identishy cation of glass shards with the useof a polarizing light microscope (for further details see Turney (1998)) This methodhas been particularly successful in the detection of tephras of rhyolitic compositionthat have a specishy c density of 2325 g cmiexcl3 (Lowe amp Turney 1997 Turney et al 1997 2001 Turney 1998 Wastegard et al 1998 2000a b) It is this technique thathas resulted in the wider recognition of micro-tephras in Europe as discussed below
3 Geochemical ` ngerprintingrsquo of tephra layers
The 34 tephras listed in table 1 have originated from four major volcanic complexesIceland the Massif Central in central France the Eifel district near Bonn and threevolcanic centres in Italy (the Campanian group Etna and the Aeolian Islands (seeshy gure 2)) An important matter to resolve is the extent to which the various magmasand ashes generated by these volcanic complexes can be geochemically shy ngerprintedThis is especially important in the case of tephras which have originated from thesame volcanic centre in which there may have been limited geochemical evolution ofmagmas over time In this section we summarize the approach generally adopted todetermine the geochemical character of visible and micro-tephras as background tothe geochemical data summarized in table 1 In the subsequent section of the paperwe review the present state of knowledge concerning all 34 tephras listed in table 1
Glass shards formed during the rapid cooling of magma are thought to have acomposition that is representative of the bulk geochemistry of the magma (Barker1983) hence widely dispersed glass particles are regarded as the most appropriateconstituents of pyroclastic material for geochemical analysis If a tephra deposit canbe shown to have a distinct geochemical signature then it can be used to correlatethe stratigraphic units in which it occurs (tephrostratigraphy) as well as to datethese units (tephrochronology) if the ages of the tephras are known (Westgate ampGorton 1981) A key element of building a tephrostratigraphical framework there-fore is to establish as rigorously as possible the geochemical composition of theindividual tephras used in its construction Robust and directly comparable geo-chemical datasets are dimacr cult to assemble for glass however because it is highlyunstable material particularly prone to sodium mobilization
The technique most widely employed to establish the geochemical signature of atephra is electron probe micro-analysis (EPMA) This enables grain-discrete determi-nations of the major elements within an individual glass shard which is of particularbeneshy t in the analysis of micro-tephra layers which generally contain glass particlesin low concentration The glass surface is bombarded with an electron beam and theX-ray energy produced is unique to each element while the intensity of the signalemitted is proportional to the amount of that element in the glass shard (Hunt amp Hill1993) Measurement can be by either energy dispersive spectrometry (EDS) or wave-length dispersive spectrometry (WDS) EDS has a lower precision mainly because
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 777
N
0 500 km
Confirmed records of Vedde Ash (visible occurrences)
New records of Vedde Ash from flotation method
Extended area of Vedde Ash detection (micro-tephra)
Known area of Laacher See Tephra (visible occurrences)
Confirmed records of Neapolitan Yellow Tuff (visible occurrences)
New record of Neapolitan Yellow Tuff from flotation method
Known area of Neapolitan Yellow Tuff
Volcanic centres of particular relevance to this study
Other major volcanic centres in Europe
Figure 2 Location of the principal volcanic centres that were active during Termination 1 andthe Early Holocene The known distribution of the Vedde Ash (VA) Laacher See (LST) andNeapolitan Yellow Tureg (NYT) are shown
the behaviour of each element cannot be monitored independently during measure-ment and so this approach fails to detect for example any signishy cant mobilizationof sodium during the bombardment process (Hunt amp Hill 1993) Although WDSrequires a higher beam current and a longer counting time than EDS the formeronoters the distinct advantage of sequential acquisition of elemental data so that thedegree of sodium loss can be tracked The morphology of individual glass shards canalso distort EDS data a problem that is reduced when using WDS because for thisprocedure glass shards are mounted in an epoxy resin and polished to provide aregat surface for analysis Hence data should always be obtained using WDS whereverpossible
Even when WDS is used as a common tool for determining the geochemical spectraof samples aberrant results can arise that inreguence data comparisons For examplesome glass shards may contain tiny crystalline inclusions of feldspar and these shouldbe avoided when selecting surface points for analysis (Hunt amp Hill 2001) Hunt amp Hill
Phil Trans R Soc Lond A (2002)
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778 S M Davies and others
6
4
2
40 50 60 70 80
K2O
(
)
SiO2 ()
Laacher See
Iceland
Veidivoumltn-Dyngjufjoumlll
Katla (basalt)
Grimsvoumltn-Kverkfjoumlll
Hekla
Katla (rhyolitic)
0
Icelandic volcanic centres8
10
Massif Central
Etna
Campanian
Figure 3 Bi-plot of SiO2 and K2 O concentrations in tephras derived from the main Europeanash provinces (modimacred after Mangerud et al 1984) The Campanian Massif Central and Etnaconcentrations are based on the data presented in table 1
(2001) have concluded that small variations in the laboratory procedures employedto determine glass chemistry can lead to misidentishy cation of sources for glass shardsand give an example of shards with a Jan Mayen provenance wrongly attributedto an Icelandic source Clearly there is a need for standardization of laboratoryprocedures and while a number of recommendations have recently been advocated(Froggatt 1992 Hunt amp Hill 1993 Hunt et al 1998) there is still some variation inlaboratory and operator practice (Hunt amp Hill 1996) Standardization is also requiredin the form in which results are presented to ensure comparability Normalizationof the data to 100 a practice employed by some researchers can obscure poorresults and hence lead to incorrect comparisons (Hunt amp Hill 1993) However othersargue that it may actually facilitate comparisons between samples by removing thedistorting enotects of the water component contained in glass shards (see for exampleFroggatt 1992) The majority of the published Italian and some of the Eifel datahave been normalized while those from other parts of Europe have not and hencedata comparisons are not always straightforward
Table 1 provides mean values and standard deviations for major oxide concentra-tions obtained from those tephras for which data are presently available The tableincludes previously unpublished WDS results for the Neapolitan Yellow Tunot (NYTdiscussed in x 4 below) and for the Mercato Tephra While individual tephra layersmay be geochemically distinct the geochemical envelopes representing the collectivedata obtained from all of the tephras assigned to each major volcanic province showsignishy cant overlaps as is illustrated in the bi-plots and ternary plots (shy gures 3 and 4)of selected oxide concentration data It is clear therefore that measurement of majoroxide concentrations does not satisfactorily discriminate between some tephras orig-inating from dinoterent volcanic centres (as noted by van den Bogaard amp Schmincke(1985) and Frezzotti amp Narcisi (1996) with respect to Eifel and Italian tephras)nor of tephras of dinoterent age originating from the same volcanic centre (Bond et
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European tephrochronological framework for Termination 1 779
40 50 60 70 80
K2O
(
)
SiO2 ()
shyshyshyshy
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shyshy
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shy
shy
shy
shy
reg
reg regreg
regregregregreg regregregregreg
FF
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4 8 12 16
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l shyshyshyshyshy shyshyshyshyshyshy
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F
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ll
FeO ()
TiO
2 (
)
reg
l
Iceland
Eifel
F
shy ItalyMassif Central
100
80
60
40
20
100
80
60
40
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100 80 60 40 20
CaO
FeO
K2O
regregreg
reg
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lllshy
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0
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regreg
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FF
F
100
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60
40
20
100
80
60
40
20
100 80 60 40 20
K2ONa2O
CaO
(c) (d)
(a)
(b)
Figure 4 Plots of selected geochemical data obtained from tephras of Termination 1 age (seetable 1) (a) Bi-plot of mean SiO2 and K2 O values (b) Bi-plot of mean FeO and TiO2 values(c) Ternary plot indicating variations in the proportions of FeO CaO and K2 O (d) Ternaryplot indicating variations in the proportion of CaO Na2 O and K2 O
al 2001) Individual tephra layers are presently assigned to a particular volcanicevent on the basis of a combination of criteria usually including examination of thephysical properties (eg refractive index and surface detail of the glass shards) thestratigraphic position of the layer and independent assessment of the age of the layeras well as any geochemical data that may be available The construction of a tephro-stratigraphical scheme would clearly beneshy t from the application of a more diagnostic
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780 S M Davies and others
geochemical tool One approach that has promise is the analysis of trace and rareearth elements using an ultraviolet laser ablation inductively coupled plasma massspectrometer (UV-LA-ICP-MS) (Pearce et al 1996 1999 Eastwood et al 1999)This approach has been applied successfully to analysis of tephras of Mid-Holoceneage but not yet to tephras that fall within the period of interest here
4 Tephra layers in Europe and the North Atlantic regiondated to between 185 and 80 14C ka
(a) Icelandic province
The Icelandic volcanic systems are divided into three main groups based on theirgeochemical characteristics tholeiitic basalts transitional alkali basalts and alkaliolivine basalts (Jakobsson 1979) Collectively magmas from the Icelandic provincespan a wide geochemical spectrum although individual volcanic centres have tightgeochemical distributions (shy gure 3) for four of the main centres Grimsvotn-Kverfjolland Veidvotn-Dyngjufoll which form part of the northern (tholeiitic) volcanic zoneand Hekla and Katla which fall within the eastern (alkali olivine basalt and transi-tional alkali basalt) volcanic zone (Haregidason et al 2000) These appear to be thekey centres for the tephras listed in table 1 that have been assigned an Icelandicorigin
One of the best-known and most widely dispersed tephra horizons in northernEurope that has an Icelandic origin is the Vedde Ash (VA) which was depositedca 103 14C ka BP (Birks et al 1996 Wastegard et al 1998) within the GS-1Younger Dryas chronozone This ash is believed to originate from the Katla complexwithin the transitional alkali basalt province (Mangerud et al 1984 Lacasse et al 1995) in the south of the island The ash has a bimodal geochemical composition (rhy-olitic and basaltic) which is thought to reregect derivation from two separate magmachambers Studies of recent volcanic events in Iceland have shown that the mostexplosive eruptions generating the largest amounts of tephra occur in this tran-sitional alkali basalt province (Haregidason et al 2000) It is also believed that thewidespread distribution of this ash was caused by the development of co-ignimbriteash plumes during an ignimbrite-forming eruption (Lacasse et al 1995)
Layers of VA that are visible to the naked eye have been found in lake sediments inwestern Norway (Mangerud et al 1984) and the Inner Hebrides Scotland (Davies etal 2001) and in marine cores throughout the NE Atlantic (see for example Kvammeet al 1989 Lacasse et al 1995) in the northern North Sea (Long amp Morton 1987)on the Iceland plateau (Ruddiman amp McIntyre 1981 Sejrup et al 1989) and on theeast Greenland continental margin (Stein et al 1996) The distribution of the VAin North Atlantic marine sequences is characterized by an arcuate lobe extendingsouthwest from the Denmark Strait and curving eastwards to mid-latitudes in theNorth Atlantic (Lacasse et al 1995) This strongly suggests deposition from raftedice which was displaced to the southwest and south in a circulating counterclockwisegyre (Ruddiman amp Glover 1972) This may well reregect Katlarsquos close proximity tothe southern coast of Iceland with the Vedde tephra being deposited on ice thatcalved directly into the North Atlantic (Haregidason et al 2000) However depositionvia the atmosphere almost certainly took place as well as is indicated by the recentdiscoveries of rhyolitic VA in micro-tephra form in several sites in Scotland (Turneyet al 1997) southern Sweden (Wastegard et al 1998 2000a) and western Russia
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European tephrochronological framework for Termination 1 781
(Wastegard et al 2000b) A more recent discovery of a relatively high concentrationof rhyolitic VA glass shards in the northern Netherlands indicates that the ash maywell have been dispersed much further south than previously thought (S M Davies2002 unpublished work) Finally glass shards assigned to the VA have also beendiscovered in the GRIP ice core and dated to 11 980 sect 80 GRIP yr BP (Gronvold etal 1995) This discovery is extremely important for it indicates that the VA maywell provide a reliable time-parallel marker horizon between ice-core marine andterrestrial records
Two other important Icelandic ash layers the Borrobol and Saksunarvatn Tephraswere deposited near the beginning and end of the Last TerminationEarly Holoceneinterval respectively The Borrobol Tephra was discovered for the shy rst time in lakesediments in several sites in Scotland and as yet is known only in micro-tephra formIt has been dated in Scottish sites to ca 123 14C ka BP (Turney et al 1997) Whatis thought to be a contemporaneous tephra has been detected in marine sedimentson the North Icelandic shelf (Eirplusmn ksson et al 2000) This certainly has a very similargeochemical composition to those reported from Scotland but the horizon in whichit was discovered on the North Iceland plateau has been dated to 134 14C ka Theage discrepancy between the Scottish and Icelandic Borrobol Tephra layers may wellreregect the inreguence of a marine reservoir error although the possibility that severaltephras with similar geochemical composition were erupted over a period exceeding1000 yr cannot be ruled out (Larsen 2000)
The Saksunarvatn Ash appears to have been one of the largest Holocene eruptionsin Iceland It has a tholeiitic basaltic composition which is considered to indicate anorigin in the Grimsvotn or Kverfjoll complex (shy gure 3) (Mangerud et al 1986) Layersof this ash have been identishy ed in sites on the Faroe Islands (Mangerud et al 1986Dugmore amp Newton 1998 Wastegard et al 2001) the Shetland Isles (Bennet et al 1992) northern Germany (Merkt et al 1993) western Norway (micro-tephra) (Birkset al 1996) and in the GRIP (Gronvold et al 1995) and NordGRIP ice cores (S MDavies 2002 unpublished work) It has been dated to between 9060 and 8930 14C kaBP (Birks et al 1996) in Norway and to ca 10 240 sect 30 GRIP yr BP in the GRIPice core (Gronvold et al 1995) The Saksunarvatn Ash may thus provide a secondimportant widespread time-parallel marker between ice-core marine and terrestrialrecords
Other Icelandic tephras of rhyolitic amacr nity are less well known in terms of theirdistribution and geochemical variation The Hogstorpsmossen Tephra reported fromSweden (Bjorck amp Wastegard 1999) and the L3754 tephra discovered in the FaroeIslands (Dugmore amp Newton 1998) are known from single sites only and so theirpotential for tephrostratigraphy is uncertain at present Furthermore the geochem-ical spectrum of the Hogstorpsmossen Tephra is based on a small dataset with lowanalytical totals
A number of tephras of basaltic composition have originated from Iceland buttheir distributions are largely conshy ned to Iceland or to marine cores collected fromclose to the Iceland coast or in the North Atlantic These include the tephras listedas 1-THOL-1 1-THOL-2 KOL-GS-2 GS-2BAS-1 GS-2BAS-2 GS-2BAS-3 andGS-2BAS-4 in table 1 (Kvamme et al 1989 Bjorck et al 1992 Eirplusmn ksson et al 2000 Haregidason et al 2000) The shy rst two in this list are tholeiitic basaltic tephrasassociated with the VA in a complex series of tephras collectively termed NorthAtlantic Ash Zone 1 (NAAZ1) which has been detected in numerous marine cores
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782 S M Davies and others
from the North Atlantic Initially thought to represent a single eruption analysisof high-resolution sediment sequences from Lake Torfadalsvatn in northern Iceland(Bjorck et al 1992) the Hebridean Shelf near NW Scotland (Austin amp Kroon 1996)the St Kilda Basin (Hunt et al 1995) and the open North Atlantic (Bond et al 2001)has demonstrated that NAAZ1 comprises a series of distinct ashes that probablyreregect separate eruption events 1-THOL-1 is thought to originate from Veidivotn(shy gure 3) while Grimsvotn may have been the source of 1-THOL-2 (Kvamme et al 1989)
KOL-GS-2 is also of tholeiitic basaltic composition but is thought to originatefrom the Kolbeinsey Ridge system (Eirplusmn ksson et al 2000) To date this tephra hasbeen detected in one marine core only within the same record on the North Ice-landic shelf as that from which the correlative of the Borrobol Tephra was alsoreported (Eirplusmn ksson et al 2000) GS-2BAS-1 to GS-2BAS-4 are of uncertain ori-gin but are thought to have been deposited at roughly the same time as KOL-GS-2(ca 134 14C ka BP (Haregidason et al 2000))
The limited distribution of these basaltic tephras a feature that is not unique toIcelandic basaltic material may reregect two factors the relative magnitude of the vol-canic eruptions from which they were derived and the limited aerial transportationof basaltic glass which is denser than rhyolitic material However a rather surpris-ing recent discovery is that of visible basaltic VA in a site on the Isle of Skye inthe Inner Hebrides Scotland (shy gure 5) (Davies et al 2001) All other occurrencesof VA in Scotland are exclusively of rhyolitic material and in micro-tephra formonly (Turney et al 1997 Turney 1998) Clearly basaltic tephra must have beentransported subaerially as far south as Skye and the reason why it has not beendetected at other sites in Scotland is puzzling We suspect that this partly reregectsthe laboratory methods employed to separate glass shards present in low concentra-tion within a micro-tephra layer from the host sediment The technique used is adensity-separation (regotation) procedure (Turney 1998) and as basaltic shards havea specishy c density similar to quartz one of the most abundant minerals in lake sedi-ments of Late Glacial age basaltic material is dimacr cult to detect using this methodThis hypothesis is currently under investigation and alternative detection methodsare being explored including magnetic separation (Mackie et al 2002)
Several other events listed in table 1 that are of probable Icelandic origin includetephras recorded in the GRIP ice core including visible (eg the `Black Featherrsquo)tephras as well as uncertain tephras inferred from distinct Ca peaks (S Johnsen2001 personal communication) No glass shards have yet been detected in the latterbut a volcanic origin is assumed because high Ca peaks are associated with knowntephras in other Greenland ice cores (S Johnsen 2001 personal communication)These are referred to as `unknownrsquo in table 1 No geochemical analyses are availablefrom these horizons so their origin must remain speculative but a possible source isIceland in view of its proximity to the Greenland ice sheet and assumed atmosphericcirculation patterns
(b) Eifel province
There are two prominent tephra events dated to the Termination 1Early Holocenetime-span that originated from the Eifel province the Laacher See Tephra (LST)and the Ulmener Maar Tephra (UMT) Visible occurrences of the LST indicate that
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European tephrochronological framework for Termination 1 783
Vedde Ash
615 625 635 645 655depth (cm)
organic lake mudsHolocene
silty clayGS-1Younger Dryas
organic lake mudsGI-1Alleroslashd
100 microm
(a)
(b)
Figure 5 (a) Photograph of the visible VA layer discovered at Loch Ashik Isle of Skye InnerHebrides Scotland (b) Light microscope photograph showing the rich content of basaltic shards(examples are indicated by the arrows) within this layer (8024 m m size fraction)
this ash was dispersed over much of central Europe (van den Bogaard amp Schmincke1985 Friedrich et al 1999 Litt amp Stebich 1999) The LST is dated by radiocarbonto ca 110 14C ka BP (van den Bogaard amp Schmincke 1985) and to 11 063sect12 14C BP(Friedrich et al 1999) by varve chronology to 1288 varve ka BP (Brauer et al 1999Litt et al 2001) and by ArAr dating to 129 ka cal BP (van den Bogaard 1995) Ithas a phonolitic composition and is thought to have originated from a plinian andphreatomagmatic eruption with the distal ash being carried in three distinct plumesone to the northeast towards Poland one to the west and the third to the southcovering the Jura Mountains and north Italy (van den Bogaard amp Schmincke 1985Juvigne et al 1995 Bossuet et al 1997) This pattern is thought to reregect altitu-dinal variations in the predominant wind direction Sedimentary sequences near thevolcanic source indicate that the LST consists of three main layers which represent
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784 S M Davies and others
dinoterent eruption phases These are grouped together as the Laacher See TephraFormation but the three individual units can be traced within and between a seriesof depositional fans The geochemical data obtained from these three LST layersshow signishy cant variations as reregected in the ternary plots (shy gure 4)
The Early Holocene Ulmener Maar Tephra (UMT) is of rhyolitic composition andappears to be restricted to sites in Germany though this conclusion is also based onrecords of visible tephras only It is dated to ca 956 14C ka BP and to 110 varve ka(Zolitschka et al 1995 Litt et al 2001)
(c) Massif Central province
The Massif Central tephras are mainly of basaltic trachyandesitic compositionwhich is distinct from the other ash provinces (shy gures 3 and 4) and their known dis-tributions are mostly conshy ned to the Massif Central region The ages of the MassifCentral tephras are based on radiocarbon dates obtained from mire and lake sedi-ments which `bracketrsquo the tephras The La Nugsup3ere Tephra with an age of 114 14C kaBP is the oldest Massif Central tephra identishy ed so far within the time-span of inter-est (Etlicher et al 1987 Juvigne et al 1996) The two Godivelle Tephras (5 and 4)are close in age but extensive radiocarbon dating suggests distinct ages of 107and 103 14C ka BP respectively (Juvigne et al 1996) The age of the Puy de DomeTephra is less certain as the estimate is based on only one radiocarbon date froma site in the southern Chaplusmn ne des Puys (table 1) This tephra is thought to havea trachyte composition (Juvigne 1993) although no major element concentrationshave yet been published
The ChopineKilianVasset tephras are thought to be derived from three separateEarly Holocene eruptions although the stratigraphic succession is not known atpresent These trachytic tephras have been radiocarbon dated to ca 854sect150 14C kaBP but are thought to have erupted separately within ca 260 yr (Juvigne et al 1996) This series of tephras is considerably more widespread than the others fromthe region having been identishy ed as far east as the Jura Mountains (Martini amp Duret1965 Martini 1970) Some other ash falls that originated from the Chaplusmn ne des Puysappear to be of local importance only (Vernet et al 1998 Vernet amp Raynal 2001)Geochemical data are currently available for only three of the Massif Central tephrasand so far as is known no attempt has yet been made to identify these tephras inmicro-tephra form
(d ) Italian provinces
The Italian tephras from this period can be assigned to three main volcanic com-plexes the Campanian volcanic shy elds around Naples Etna on Sicily and the AeolianIslands The Campanian complex which includes the Phlegrean Fields Vesuviusand Ischia is mainly trachytic in composition with a geochemical spectrum that isquite distinct from those of the Etna complex and of the Aeolian Islands (shy gure 3)Tephras originating from one or more of these three complexes have been detectedin marine cores from the Tyrrhenian and Adriatic seas as well as other parts of theMediterranean Sea (Keller et al 1978 Paterne et al 1986 1988 1990 Langone etal 1996) and in lake sequences in southern Italy such as Lago Grande di Monticchio(Newton amp Dugmore 1993 Narcisi 1996 Allen et al 1999) and central Italy such asLago Albano near Rome (Calanchi et al 1996) Some work has also been conducted
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European tephrochronological framework for Termination 1 785
in or close to the volcanic source areas in an attempt to establish the full sequenceof volcanic eruptions during the Late Quaternary (see for example Di Vito et al 1999) There are nine Italian tephras reported from marine and lake sequences thatdate from the period between 185 and 80 14C ka BP In all instances the recordsare of visible layers of tephra The ages of some of these are poorly established atpresent with conregicting data obtained from dinoterent sites The ages suggested intable 1 are those favoured in the most recent publications but these may requirere-assessment in the light of future research
The two oldest known tephras in the time-period of interest are the L9 and Green-ish Tephras both recorded as separate features within the annually laminated Lagodi Monticchio maar sequence The lowest of the two L9 is considered to be the cor-relative of the `basalrsquo plinian eruption of Vesuvius (Narcisi 1996) Age estimates ofa palaeosol that underlies the Vesuvius tephra sequence are ca 1617 14C ka BP forthis event (Delibrias et al 1979) L9 has a trachytic composition very similar to theGreenish Tephra (table 1) However L9 which is also a product of Vesuvius is foundstratigraphically below the Greenish Tephra in the Lago di Monticchio core TheGreenish Tephra is dated in the Monticchio sequence to 17 560 varve yr BP (Allenet al 1999) and has a calibrated radiocarbon age estimate of 17 830 sect 300 cal BP(Andronico et al 1995) Both tephras have a dominantly eastwards dispersal basedon the occurrences of visible layers (Santacroce 1987 Narcisi 1996) Both tephrasalso have a trachytic composition and as can be seen from table 1 the reportedgeochemical spectra are very close indeed with the standard deviations overlappingfor almost every major element This could present problems for tephrostratigra-phy where only one of the tephras is evident in a sediment sequence in particularbecause they are so close in age This is a good example of where an analysis oftrace and rare earth elements might be required to make a clear distinction betweentephras with very similar major oxide concentrations
The Y-1 Tephra also termed the Biancavilla Montalto Ignimbrite (Vezzoli 1991)is a product of Etna and has been identishy ed as a visible benmoritic tephra horizonthroughout the central Mediterranean (Paterne et al 1988) including central Italyand the Adriatic Sea (Vezzoli 1991 Narcisi 1993 Calanchi et al 1996) It has anestimated age of ca 140 14C ka BP The Unita dei Tefra Superiori tephra which hasbeen detected as far east as Lago di Monticchio in south-central Italy (Narcisi 1996)is also dated to ca 140 14C ka BP (Alessio et al 1976) but it is thought that thesource of this tephra lies in the Phlegrean Fields No geochemical data are availablefrom the presumed source region|the data reported in table 1 were obtained fromthe Lago di Monticchio record (Narcisi 1996)
The NYT which is equivalent to the C-2 tephra reported from various marinesequences has also been traced throughout central Italy and the Adriatic Sea (Pat-erne et al 1988 Calanchi et al 1996 Di Vito et al 1999) (shy gure 2) In the centralApennines region it formed the parent material for a soil that started to developat the beginning of the Holocene period (Frezzotti amp Narcisi 1996) Also originatingfrom the Campi Flegrei caldera it is dated to ca 120 14C ka BP (Di Vito et al 1999) Published geochemical data based on EDS indicate three dinoterent geochemicalpopulations varying from latite to phonotrachyte in composition (Orsi et al 1992Paterne et al 1988) (table 1) We report in x 4 of this paper on new data obtainedfrom the NYT by WDS and it is the mean of these new data that is included intable 1 Comparisons with the previously published EDS data are provided (table 1)
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786 S M Davies and others
The new data indicate clearly that the NYT originated from the Campanian volcaniccentre
In the interval between the dispersal of the NYT (ca 120 14C ka BP) and 95 14Cka BP there appear to have been as many as 34 eruptions in the Campi Flegrei caldera(Di Vito et al 1999) Of these only one appears to have been detected widely in theregion the Pomici Principali (also termed the Agnano Formation or C-1 tephra inmarine records (Paterne et al 1988) This was the product of the highest magnitudeeruption from this epoch and is dated to between 976 sect 300 and 1032 sect 50 14C kaBP (Delibrias et al 1979 Di Vito et al 1999) or to 122 varve ka BP based on theMonticchio varve chronology (Allen et al 1999) It is trachytic in composition andappears to have had a mainly eastwards dispersal
The Mercato Tephra dated to ca 80 14C ka BP and originally analysed usingEDS has a phonolitic composition and is believed to have been generated by Vesu-vius (Paterne et al 1988) New WDS data obtained from reference samples col-lected from an exposure to the west of Naples support these conclusions (table 1 andAppendix A) The silica content of the WDS analyses are ca 3 lower than thoseobtained using EDS (table 1) which may reregect the fact that the EDS data werenormalized
The only tephra listed in table 1 that is thought to have originated from the AeolianIslands is the Pollara pumice also referred to as the E2 tephra in marine sequences(Paterne et al 1986 1988) The limited geochemical data available so far suggest itto be the only Italian tephra listed in table 1 that is rhyolitic in composition Littlemore is known about this ash which has not been recorded extensively except thatits age is estimated to be ca 130 14C ka BP (Keller 1980)
5 Extending the known distributions of European tephras
Figure 2 summarizes schematically the known distributions of three of the tephrasreferred to in the preceding section the VA the LST and the NYT Following theintroduction of a laboratory method that enables the detection of micro-tephra parti-cles in mineral-rich sediment the VA has been traced to sites that are located muchfarther south (into The Netherlands) and east (as far as St Petersburg) than thedistribution limits based on occurrences of visible layers of the ash As a result con-tinental sequences over a much larger area in northern Europe can now be correlateddirectly with marine and ice-core records using the VA as a time-parallel marker
This suggests therefore that other prominent ash layers such as the LST andNYT should also be detectable over larger tracts of Europe than is presently thecase if suitable sites are examined for the presence of micro-tephra horizons To testthis assertion we examined lake sediment deposits of Last Termination age froma site in the northern Apennines in order to establish whether the NYT could bedetected in micro-tephra form The site selected Prato Spilla `Crsquo lies well to thenorth of the localities in central and southern Italy and in the Adriatic Sea fromwhich visible records of the NYT have been reported Prato Spilla `Crsquo lies at an alti-tude of ca 1350 m in the Appennino Parmense ca 60 km south of Parma and 15 kmeast of Pontremoli The site contains a continuous sediment sequence spanning theLast Termination and most of the Holocene Detailed pollen and coleopteran strati-graphical records which have been radiocarbon dated have been published for thissite (Lowe 1992 Ponel amp Lowe 1992 Lowe amp Watson 1993)
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European tephrochronological framework for Termination 1 787
Figure 6 Light microscope photograph of an NYT glass shard from Prato Spilla Crsquosequence assigned on geochemical grounds to the NYT
The methods adopted for sub-sampling of the Prato Spilla `Crsquo sequence for thequantishy cation of glass shard concentrations and for subsequent electron microprobeanalysis of selected glass shards followed those described elsewhere (Turney 1998)In summary contiguous samples of 1 cm stratigraphic interval were extracted fromthe sequence to establish presenceabsence of glass shards Each of the 1 cm3 blocksin which tephra particles was detected was then examined with more care andshard concentrations were quantishy ed for each sub-sample Micro-tephra particleswere detected in shy ve samples (shy gure 6) but were predominantly clustered around500 cm in the part of the sequence assigned on pollen-stratigraphic grounds to theLate Glacial Interstadial or the `Allerfrac12drsquo|indeed the part of the succession in whichthe NYT would be expected to occur Peak concentrations of micro-tephra particlesreach 225 shards cmiexcl3 and are conshy ned to a single 1 cm thick sample in the sequencewhich probably represents the time of maximum deposition of the ash
Electron microprobe measurements based on WDS were obtained from the surfacesof 21 separate glass shards extracted from the sample with peak shard concentrations(Appendix A) Since only EDS measurements were available for the NYT prior to thepresent study we also obtained WDS measurements from 17 shards extracted fromthe visible layer of NYT that is exposed on Procida Island which lies in the type-locality for the NYT close to the city of Naples (Appendix A) The results providenot only a more comprehensive geochemical dataset for the NYT than was previ-ously available but also a consistent basis for comparison with the Prato Spilla `Crsquodataset All of the WDS data reported here (Appendix A) were measured at the samelaboratory (Tephrochronology Analytical Unit University of Edinburgh) using thesame sample pretreatment and preparation protocol The WDS results for the NYTdinoter to a minor degree from the EDS results (table 1 and Appendix A) especiallywith respect to the amounts of silica aluminium and calcium measured The EDS
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788 S M Davies and others
4 8FeO ()
TiO
2 (
) Neapolitan Yellow Tuff(Procida)Neapolitan Yellow Tuff(Prato Spilla lsquoCrsquo)
0
1
2
3
40 50 60 70
MgO
(
)
SiO2 ()
K2O
(
)
40 50 60 70
0
04
08
4
8
12
SiO2 ()
(a)(b)
(c)
Figure 7 Bi-plots of SiO2 K2 O SiO2 MgO and FeOTiO2 for the WDS analyses obtainedfrom glass shards of the NYT from Procida (Naples) and Prato Spilla Crsquo Means and standarddeviations are shown
results show a higher degree of statistical scatter than the WDS measurements whichmay reregect the fact that the data were normalized combined with the inreguence ofvariation in water content between shards
There is a very close correspondence between the WDS data for the Prato Spilla `Crsquomicro-tephra shards and those obtained from the type-material near Naples (shy g-ure 7) The geochemical data strongly suggest therefore that the NYT is representedat the Prato Spilla `Crsquo site by a discrete layer of micro-tephra particles This conclu-sion is compatible with the pollen-stratigraphic data from the site and accords withage estimates for the NYT (ca 120 14C ka BP) obtained from other sites (Paterneet al 1990)
These results encourage us to believe that many if not all of the tephras listedin table 1 will be detectable over much larger tracts of Europe than is presently thecase if appropriate research is undertaken to detect layers of micro-tephra particlesin selected sites The authors are presently engaged in a major continent-wide pro-gramme of research in collaboration with a number of European research groupsdesigned to test this hypothesis The focus in this research is on those parts of Europewhere we expect to shy nd overlapping `apronsrsquo of tephra deposition originating fromthe Italian Eifel Massif Central and Icelandic provinces For example a number ofsites in parts of southern France northern Italy and perhaps western Switzerlandmay have received inreguxes of micro-tephra originating from the Italian and Eifelprovinces and perhaps also from the Massif Central Sites in parts of Germany Den-mark and southern Sweden for example may in turn have received tephra depositsfrom both of the Icelandic and Eifel provinces If this proves to be the case then thestage will be set for the construction of a tephrostratigraphical framework for Europewhich will enable Last Termination sequences to be correlated on a continent-widebasis using micro- and visible tephra layers as time-parallel stratigraphic markersFurthermore there is also the possibility that other tephras remain to be discovered
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 789
those which either because of the magnitude or nature of some volcanic eruptionswere distributed over parts of Europe in micro-tephra form only
6 European tephrostratigraphy and the chronology of eventsduring the Last Termination and Early Holocene
One of the crucial issues in Late Quaternary palaeoenvironmental research thatremains to be resolved is the degree to which climatic events inferred from oceanicterrestrial and ice-core records were synchronous during the Last Termination andEarly Holocene If the ice-core records provide realistic estimates of the rates anddurations of climatic events during this period then comparisons between individ-ual records have to be enotected with at least a decadal precision The problem thispresents and the role that tephrostratigraphy can play in resolving some of thedimacr culties involved are put into perspective in shy gure 8
Figure 8 shows some of the data used to calibrate radiocarbon dates (the LakeSuigetsu and Cariaco Basin datasets) plotted against the GRIP ss08c ice-core recordof macr 18O variations The latter has been selected by the INTIMATE group as an arbi-trary and temporary standard for this period and used to deshy ne an event stratig-raphy scheme (shy gure 1) for the Last Termination (see Bjorck et al 1998 Walker etal 2001) As has been alluded to in earlier sections of this paper the uncertaintiesassociated with all of the dating methods currently employed preclude precise com-parisons of ice-core marine and terrestrial records Oceanic and terrestrial recordsmostly rely upon radiocarbon dating locally supplemented in a few cases by varvechronology Imprecisions in radiocarbon dates can arise through site-specishy c fac-tors (eg hard-water or mineral carbon errors in freshwater sequences and reservoirerrors in marine sequences) sample selection laboratory measurements of 14C activ-ity and other factors (Lowe amp Walker 2000) Further imprecision may be introducedby the calibration of radiocarbon dates since the uncertainties in the dataset usedto calibrate pre-Holocene radiocarbon dates INTCAL98 are far higher than forthe Holocene which is based on dendro-calibration (Stuiver et al 1998) There arealso uncertainties anotecting varve chronologies while the ss08c ice-core chronologyfor the Last Termination dinoters signishy cantly from the GISP2 record and indeedfrom other models of the GRIP record (Lowe et al 2001) Published comparisonsbetween ice-core marine and terrestrial records for the Last Termination seldom takeinto account the true magnitude of the dating uncertainties involved and frequentlyemploy circular reasoning
Figure 8 shows the positions on the radiocarbon time-scale of 20 of the tephrasdiscussed earlier in this paper these being the ones for which reasonably conshy dentradiocarbon age estimates can be made (though these will be subject to revised esti-mates in the future) A high number of these occur in the period 14080 14C kaBP but we conshy dently anticipate the discovery in the future of additional tephras(perhaps in micro-tephra form only) which will date to the period 185140 14C kaBP Tephras detected in the GRIP ice core over the same time-interval are plottedon the calendar time-scale in shy gure 8 By providing key `time-linesrsquo between recordstephrostratigraphy can help to resolve some of the dating uncertainties referredto earlier by for example enabling direct comparisons of discrepant age estimatesobtained using dinoterent methods (cf Litt et al 2001) It can also provide estimatesof the magnitudes of the reservoir errors that anotected various marine sectors at dif-
Phil Trans R Soc Lond A (2002)
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790 S M Davies and others
-44
-40
-36
-32
cale
ndar
yea
rs B
P
8000
9000
10 0
00
11 0
00
12 0
00
13 0
00
14 0
00
15 0
00
16 0
00
17 0
00
18 0
00
14C age (BP)
VA
SA
Un
Un
Un
Un
Un
BF
Hol
ocen
eG
S-1
GI-
1aG
I-1b
GI-
1cG
I-1d
GI-
1eG
S-2
aG
S-2
bG
S-
2c
Bor
robo
l
La
Nug
egravere
Laa
cher
See
God
ivel
le 5
amp I
-TH
OL
-2
Puy
de D
ocircme
I-T
HO
L-1
Saks
unar
vatn
Houmlg
stor
psm
osse
nU
lmen
er M
aar
amp L
3574
radiocarbon dated European tephra horizons
Cho
pine
Kili
an V
asse
tM
erca
to
God
ivel
le 4
Pom
ici P
rinc
ipal
i amp V
edde
Polla
ra p
umic
eK
OL
-GS-
2 amp
GS
-2B
AS-
12
3
GS
-2B
AS-
4 U
nita
dei
Tef
raSu
peri
ori amp
laye
r Y
-1
Gre
enis
h
L9
20 0
0018
000
16 0
0014
000
12 0
0010
000
-44
-40
-36
-32
800
600
400
200 0
GISP2 volcanicsulphate conc (ppb)
1000
Nea
polit
an Y
ello
w T
uff
GISP2 18O (permil) dGRIP 18O (permil) d
Figure 8 For description see opposite
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 791
ferent times through a comparison of radiocarbon dates obtained from marine andterrestrial horizons in which the same tephra has been detected (see for exampleAustin et al 1995 Bondevik et al 2001 Haregidason et al 2000) Tephrostratigraphymay provide an independent test of suggestions that some of the climatic changesduring the Last Termination were time-transgressive as illustrated for some appar-ently contrasting climatic trends in Iceland Britain and NW Russia (Lowe 2001) Ofparticular importance as far as establishing `leadsrsquo and `lagsrsquo in climatic changes isconcerned are the tephra records from the Greenland ice cores The discovery of theVedde and Saksunarvatn ashes in the GRIP record (Gronvold et al 1995) alreadyprovides a basis for making direct comparisons between marine terrestrial and ice-core records It is a matter of some urgency that the incidence of tephra depositsin the Greenland ice cores be more fully explored in the hope that this will lead tothe recognition of additional time-parallel links between the ice-core records on theone hand and oceanic and terrestrial records on the other An investigation of thenew NordGRIP record for this purpose is currently in progress (S M Davies 2002unpublished data)
Finally a fuller and more reshy ned tephrostratigraphical scheme for Europe will alsohave other applications It will provide an important database for those investigatingthe timing and frequency of volcanic eruptions in Europe during the past 20 000 yror so as well as of the geochemical evolution of the dinoterent volcanic centres overthat period A fuller record of the distribution of micro-tephras may also provideinformation on atmospheric circulation patterns during the dispersal and depositionperiods as well as on the nature and altitude of the eruption columns which mayin turn provide inferences about magma viscosity
This paper is a contribution to the INTIMATE project of the INQUA Palaeoclimate Com-mission and the work is supported by a Leverhulme Trust Research project (grant allocationnumber F07537C) entitled Testing hypotheses of rapid climate change using tephrochronol-ogyrsquo SMDrsquo s contribution was completed during possession of a NERC PhD studentship(GT 0499ES162) We are extremely grateful to Dr Peter G Hill for his assistance withthe EPMA analyses at the Tephrochronology Analytical Unit University of Edinburgh We alsothank Dr G Mastrolorenzo (Vesuvius Observatory) and Miss G Swindle for assistance duringthe macreld investigations in Naples Thanks are also expressed to two anonymous reviewers forcomments on an earlier draft
Appendix A
Table 2 shows the major oxide concentrations of NYT glass shards from Procidaand Prato Spilla `Crsquo and of the Mercato Tephra from the Naples area (see x 4 forsite context) All oxides are shown as weight and total iron is expressed as FeO
Figure 8 Radiocarbon calibration curve for Termination 1 and the Early Holocene compared with theGRIP macr 18 O event stratigraphy the GRIP ss08c and GISP2 macr 18 O records (wwwngdcnoaagov) andknown tephra horizons from this period The shaded areas represent the cooler climatic episodes andare labelled with the Greenland stratotype terminology (Bjorck et al 1998) Where radiocarbon agesare reported in table 1 as a range the mean is given here Abbreviations for GRIP horizons are asfollows Un unknown (approximate positions are given (S Johnsen 2001 personal communication))SA Saksunarvatn Ash VA Vedde Ash BF Black Feather Sulphate concentrations from the GISP2record are also shown (Zielinski et al 1996) Open circles denote radiocarbon calibration data fromLake Suigetsu (Kitagawa amp van der Plicht 2000) Filled circles denote radiocarbon calibration data fromCariaco Basin assuming a marine reservoir age of 420 14 C yr (Hughen et al 1998)
Phil Trans R Soc Lond A (2002)
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792 S M Davies and others
Tab
le2
Majo
roxi
de
con
cen
trati
on
sof
NY
Tgl
ass
shard
sfr
om
Pro
cida
an
dP
rato
Spil
laC
rsquoan
dof
the
Mer
cato
Tep
hra
from
the
Naple
sare
a(s
eex4
for
site
con
text
)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
roci
da)
1584
204
0177
634
201
106
828
635
197
5969
1W
DS
2598
603
9178
027
101
204
924
244
583
4965
8W
DS
3586
604
5173
631
100
805
924
342
183
0951
9W
DS
4583
903
9177
933
000
906
924
540
486
9958
3W
DS
5605
106
8179
126
901
204
923
243
086
1976
4W
DS
6591
704
5177
332
801
006
425
740
887
8968
0W
DS
7581
804
1178
031
501
107
125
640
086
9956
1W
DS
8589
504
2179
533
701
506
926
740
987
5970
4W
DS
9592
003
9178
135
101
007
026
443
585
7972
7W
DS
10
591
404
2174
631
601
105
723
442
482
6957
0W
DS
11
593
403
6177
131
301
506
726
439
188
5967
6W
DS
12
588
103
8176
128
100
505
525
141
583
4952
1W
DS
13
577
003
8176
533
500
807
228
140
384
8952
0W
DS
14
586
004
7179
735
300
706
827
842
984
6968
5W
DS
15
588
104
2180
629
400
505
924
937
993
0964
5W
DS
16
579
603
9178
536
501
308
228
836
087
1959
9W
DS
17
580
103
9177
631
500
907
327
039
488
9956
6W
DS
mea
n588
104
2177
631
901
006
525
940
686
9962
8
sd
(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(07
8)
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 793
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
rato
Spil
laC
rsquo)
1552
105
4177
247
401
914
38
735
578
9951
1W
DS
2557
305
7179
845
701
512
640
136
581
5960
6W
DS
3595
004
4173
724
302
003
117
652
877
8950
7W
DS
4575
704
2179
433
001
406
627
043
083
6953
7W
DS
5599
904
0178
826
401
304
421
841
688
4966
5W
DS
6591
103
8177
826
601
105
022
443
888
8960
2W
DS
7565
304
5180
939
501
410
532
535
791
8962
1W
DS
8597
606
9180
826
501
604
821
546
684
6970
7W
DS
9571
805
6179
939
801
109
932
240
883
6964
7W
DS
10
588
603
7176
527
601
104
721
042
487
7953
3W
DS
11
559
404
9180
544
501
812
339
435
878
6957
2W
DS
12
594
704
0181
328
301
705
522
144
785
6967
9W
DS
13
611
103
7187
016
900
802
419
938
195
9975
8W
DS
14
599
204
4181
128
601
404
620
844
986
6971
6W
DS
15
601
204
4177
328
302
004
722
446
385
5972
1W
DS
16
595
104
5176
428
801
504
722
744
884
3962
8W
DS
17
603
704
1177
825
101
503
520
348
181
2965
3W
DS
18
558
704
5179
647
401
813
139
836
879
0960
7W
DS
19
589
602
8178
830
901
606
622
436
091
8960
5W
DS
20
553
606
3178
647
401
913
840
136
978
0956
6W
DS
21
579
004
0175
739
000
708
328
338
286
7959
9W
DS
mea
n582
804
6179
033
401
507
427
341
484
8962
1
sd
(1
87)
(01
0)
(02
7)
(09
2)
(00
4)
(03
9)
(08
0)
(04
9)
(05
0)
(07
0)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
794 S M Davies and others
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)
1575
202
7194
219
701
101
016
374
766
9951
8W
DS
2575
802
9194
523
902
201
520
273
564
5959
0W
DS
3574
301
4205
219
101
100
416
481
266
1965
2W
DS
4575
500
7206
018
002
000
415
181
669
3968
6W
DS
5580
000
9208
018
601
300
515
883
367
1975
5W
DS
6571
001
0206
016
101
600
515
078
967
1957
2W
DS
7577
501
1201
117
101
500
620
675
655
4950
5W
DS
8573
700
9212
717
101
900
815
187
564
2973
9W
DS
9580
301
3208
715
801
400
824
81
754
1968
1W
DS
10
574
400
6211
18
402
00
516
480
567
8971
6W
DS
11
577
200
7214
212
501
200
829
879
247
962
6W
DS
12
572
200
9211
217
301
501
15
980
465
9966
3W
DS
13
571
800
7210
417
402
201
16
184
467
2971
2W
DS
14
567
300
9208
916
901
400
917
383
262
5959
3W
DS
15
568
600
8205
918
202
101
414
682
666
6960
8W
DS
16
572
501
1211
318
202
01
215
884
364
5970
9W
DS
17
572
901
2212
916
502
101
215
883
667
2973
4W
DS
18
573
01
4211
716
301
801
416
83
365
5970
4W
DS
19
569
201
1207
418
602
101
414
982
964
961
6W
DS
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
3)
(04
2)
(01
3)
(00
1)
(00
2)
(01
)(0
39)
(01
1)
(02
5)
Phil Trans R Soc Lond A (2002)
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796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
References
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European tephrochronological framework for Termination 1 797
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Brauer A Endres C Gunter C Litt T Stebich M amp Negendank J F W 1999 Highresolution sediment and vegetation responses to Younger Dryas climate change in varved lakesediments from Meerfelder Maar Germany Quat Sci Rev 18 321329
Brooks S J Mayle F E amp Lowe J J 1997 Chironomid based Lateglacial climatic recon-struction for southeast Scotland J Quat Sci 12 161167
Calanchi N Dinelli E Gasparatto G amp Lucchini F 1996 Etnean tephra layer in Albanolake and Adriatic Sea cores new macrndings of Y-1 layer in the central Mediterranean area ActaVulcan 8 713
Coope G R Lemdahl G Lowe J J amp Walkling A 1998 Temperature gradients in northernEurope during the last glacialHolocene transition (149 ka BP) interpreted from coleopternassemblages J Quat Sci 13 419433
Dansgaard W (and 10 others) 1993 Evidence for general instability of past climate from a250 kyr ice-core record Nature 363 218220
Davies S M Turney C S M amp Lowe J J 2001 Identimacrcation and signimacrcance of a visiblebasalt-rich Vedde Ash layer in a Late-glacial sequence on the Isle of Skye Inner HebridesScotland J Quat Sci 16 99104
Delibrias G Di Paola G M Rosi M amp Santacroce R 1979 La storia eruttiva del complessovulcanico Somma Vesuvio ricostruita dalle successini piroclastiche del Monte Somma RendSoc It Mineral Petrolog 35 411438
Di Vito M A Isaia R Orsi G Southon J de Vita S Drsquo Antonio M Pappalardo L ampPiochi M 1999 Volcanism and deformation since 12 000 years at the Campi Flegrei caldera(Italy) J Volcanol Geophys Res 91 221246
Dugmore A J amp Newton A J 1992 Thin tephra layers in peat revealed by X-radiography JArchaeol Sci 19 163170
Dugmore A J amp Newton A J 1998 Holocene tephra layers in the Faroe Islands Frodskaparrit46 191204
Eastwood A J Pearce N J G Westgate J A Perkins W T Lamb H F amp RobertsN 1999 Geochemistry of Santorini tephra in lake sediments from southwest Turkey GlobalPlanet Change 21 1729
Eirpara sup3 ksson J Knudsen K L Hadeg idason H amp Henriksen P 2000 Lateglacial and Holocenepalaeoceanography of the North Icelandic shelf J Quat Sci 15 2342
Etlicher B Janssen C R Juvignparae E amp Van Leeuwen J F N 1987 Le Haut Forez (MassifCentral France) aprmicroes le Plparaeniglaciaire Wurmien environnement et tparaephra du volcan de LaNugmicroere Bull Ass Fr Etud Quat 4 229239
Frezzotti M amp Narcisi B 1996 Late Quaternary Tephra derived paleosols in central Italyrsquo scarbonate Apennine range stratigraphical and paleoclimatological implications Quat Int3436 147153
Friedrich M Kromer B Spurk M Hofmann J amp Kaiser K F 1999 Paleoenvironment andradiocarbon calibration as derived from LateglacialEarly Holocene tree-ring chronologiesQuat Int 61 2739
Froggatt P C 1992 Standardisation of the chemical analysis of tephra deposits Report of theICCT working group Quat Int 1314 9396
Gronvold K Oskarsson N Johnsen S J Clausen H B Hammer C U Bond G amp Bard E1995 Ash layers from Iceland in the GRIP ice core correlated with oceanic and land sedimentsEarth Planet Sci Lett 135 149155
Phil Trans R Soc Lond A (2002)
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Hadeg idason H Eirpara sup3 ksson J amp van Kreveld S 2000 The tephrochronology of Iceland and theNorth Atlantic region during the Middle and Late Quaternary a review J Quat Sci 15322
Hoek W Z amp Bohncke S J P 2001 Oxygen isotope wiggle matching as a tool for synchronisingice-core and terrestrial records over Termination 1 Quat Sci Rev 20 12511264
Hughen K A Overpeck J T Peterson L C amp Trumbore S 1996 Rapid climate changes inthe tropical Atlantic region during the last deglaciation Nature 380 5153
Hughen K A Overpeck J T amp Lehman J 1998 A new 14 C calibration data set for the LastDeglaciation Radiocarbon 39 483494
Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
Hunt J B amp Hill P G 1996 An inter-laboratory comparison of the electron probe microanalysisof glass geochemistry Quat Int 3436 229241
Hunt J B amp Hill P G 2001 Tephrological implications of beam sizesample size ereg ects inelectron microprobe analysis of glass shards J Quat Sci 16 105117
Hunt J B Fannin N G T Hill P G amp Peacock J D 1995 The tephrochronology andradiocarbon dating of North Atlantic Late Quaternary sediments an example from the StKilda Basin In The tectonics sedimentation and palaeoceanography of the North Atlanticregion (ed R A Scrutton M S Stoker G B Shimmield amp A W Tudhope) vol 90pp 227248 Geological Society of London Special Publication
Hunt J B Clift P D Lacasse C Vallier T L amp Werner R 1998 Standardisation ofelectron probe microanalysis of glass geochemistry In Proc ODP Scientimacrc Results vol 152pp 8591 College Station TX Ocean Drilling Program
Jakobsson S P 1979 Outline of the petrology of Iceland Jokull 29 5773
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Juvignparae E 1993 Contribution microa la tparaephrostratigraphie du Quaternaire et son application microa lagparaeomorphologie Mparaem Serv Explicat Cartes Gparaeol Min Belg 36 166
Juvignparae E amp Gewelt M 1987 La Narse drsquo Ampoix comme tparaephrostratotype dans la Chasup3 ne desPuys mparaeridionale (France) Bull Ass Fr Etud Quat 29 3749
Juvignparae E Kozarski S amp Nowaczyk B 1995 The occurrence of Laacher See Tephra in Pomera-nia NW Poland Boreas 24 225231
Juvignparae E Bastin B Delibrias G Evin J Gewelt M Gilot E amp Streel M 1996 Acomprehensive pollen and tephra based chronostratigraphic model for the Lateglacial andHolocene period in the French Massif Central Quat Int 3436 113120
Keller J 1980 The island of Vulcano Rend Soc It Mineral Petrolog 36 369414
Keller J Ryan W B F Ninkovich D amp Altherr R 1978 Explosive volcanic activity in theMediterranean over the past 200 000 years as recorded in deep sea sediments Geol Soc AmBull 89 591604
Kitagawa H amp van der Plicht J 2000 Atmospheric radiocarbon calibration beyond 11 900 calBP from Lake Suigetsu laminated sediments Radiocarbon 42 369380
Kvamme T Mangerud J Furnes H amp Ruddiman W F 1989 Geochemistry of Pleistoceneash zones in cores from the North Atlantic Norsk Geol Tids 69 251272
Lacasse C Sigurdsson H Johannesson H Paterne M amp Carey S 1995 Source of Ash zone 1in the North Atlantic Bull Volcanol 57 1832
Langone L Asioli A Corregiari A amp Trincardi F 1996 Age depth modelling through theLate-Quaternary deposits of the central Adriatic Basin In Palaeoenvironmental analysis ofItalian crater lake and Adriatic sediments (ed F Oldmacreld amp P Guilizzoni) vol 55 pp 177196 Memorie dellrsquo Instituto Italiano di Idrobiologia
Larsen G 2000 Holocene volcanism in Iceland and tephrochronology as a tool in volcanologyIn Iceland 2000 modern processes and past environments Keele University UK
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on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 799
Litt T amp Stebich M 1999 Bio- and chronostratigraphy of the Lateglacial in the Eifel regionGermany Quat Int 61 516
Litt T Brauer A Goslar T Merkt J Balaga K Muller H Ralska-Jasiewiczowa MStebich M amp Negendank J F W 2001 Correlation and synchronisation of Lateglacialcontinental sequences in northern Central Europe based on annually laminated lacustrinesediments Quat Sci Rev 20 12331249
Long D amp Morton A C 1987 An ash fall within the Loch Lomond stadial J Quat Sci 297101
Lotter A F Eicher U Siegenthaler U amp Birks H J B 1992 Lateglacial climatic oscillationsas recorded in Swiss lake sediments J Quat Sci 7 187204
Lowe J J 1992 Lateglacial and Early Holocene lake sediments from the Northern ApenninesItaly|pollen stratigraphy and radiocarbon dating Boreas 21 193208
Lowe J J 2001 Abrupt climatic changes in Europe during the last glacialinterglacial tran-sition the potential for testing hypotheses on the synchroneity of climatic events usingtephrochronology Global Planet Change 603 7384
Lowe J J amp Turney C S M 1997 Vedde Ash layer discovered in a small lake basin on theScottish mainland J Geol Soc Lond 154 605612
Lowe J J amp Walker M J C 2000 Radiocarbon dating the last glacialinterglacial transition(ca 14914 C ka BP) in terrestrial and marine records the need for new quality assuranceprotocols Radiocarbon 42 5368
Lowe J J amp Watson C 1993 Lateglacial and Early Holocene pollen stratigraphy of the northernApennines Italy Quat Sci Rev 12 727738
Lowe J J Birks H H Brooks S J Coope G R Harkness D D Mayle F E SheldrickC Turney C S M amp Walker M J C 1999 The chronology of palaeoenvironmental changesduring the Last GlacialHolocene transition towards an event stratigraphy for the BritishIsles J Geol Soc Lond 156 397410
Lowe J J Hoek W Z amp INTIMATE group 2001 Inter-regional correlation of palaeoclimaticrecords for the Last GlacialInterglacial transition a protocol for improved precision recom-mended by the INTIMATE project group Quat Sci Rev 20 11751187
Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
Mangerud J Lie S E Furnes H Kristiansen I L amp Liquest mo L 1984 A Younger Dryas ashbed in western Norway and its possible correlation with tephra beds from the Norwegian Seaand North Atlantic Quat Res 21 85104
Mangerud J Furnes H amp Jparaohansen J 1986 A 9000 year-old ash bed on the Faroe IslandsQuat Res 26 262265
Martini J 1970 Recherche de retombparaees volcaniques dans le sud-est de la France et la Suisseoccidentale Arch Sci 23 641674
Martini J amp Duret J J 1965 Note preliminaire sur la presence drsquo un niveau de cendres vol-caniques dans des sparaediments post-glaciaires des environs de Genmicroeve Arch Sci 18 587588
Mayewski P A Meeker L D Twickler M S Whitlow S Yang Q Lyons W B amp Pren-tice M 1997 Major features and forcing of high latitudes Northern Hemisphere atmosphericcirculation using a 110 000 year long glaciochemical series J Geophys Res 102 345365
Merkt J Muller H Knabe W Muller P amp Weiser T 1993 The Early Holocene Saksunarvatntephra found in lake sediments in NW Germany Boreas 22 93100
Narcisi B 1993 Segnalazione di un livello piroclastico di provenienza etnea nellrsquo area del Fucino(Italia Centrale) Quaternario 6 8792
Narcisi B 1996 Tephrochronology of a Late Quaternary lacustrine record from the Monticchiomaar (Vulture volcano southern Italy) Quat Sci Rev 15 155165
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
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Newton A J amp Dugmore A J 1993 Tephrochronology of Core C from Lago Grande di Mon-ticchio In Paleolimnology of European Maar Lakes (ed J F W Negendank amp B Zolitschka)Lecture Notes in Earth Science vol 49 333348 Springer
Oldmacreld F Appleby P G amp Thompson R 1980 Palaeoecological studies of lakes in theHighlands of Papua New Guinea J Ecol 68 457477
Orsi G Drsquo Antonio M de Vita S amp Gallo G 1992 The Neapolitan Yellow Tureg a large mag-nitude trachytic phreatoplinian eruption eruptive dynamics magma withdrawal and calderacollapse J Volcanol Geotherm Res 53 275287
Paterne M Guichard F Labeyrie J Gillot P Y amp Duplessy J C 1986 Tyrrhenian Seatephrochronology of the oxygen isotope record for the past 60 000 years Mar Geol 72259285
Paterne M Guichard F amp Labeyrie J 1988 Explosive activity of the south Italian volca-noes during the past 80 000 years as determined by marine tephrochronology J VolcanolGeotherm Res 34 153172
Paterne M Labeyrie J Guichard F Mazaud A amp Maitre F 1990 Fluctuations of the Cam-panian explosive volcanic activity (south Italy) during the past 190 000 years as determinedby marine tephrochronology Earth Planet Sci Lett 98 166174
Pawse A Beske-Diehl S amp Marshall S A 1998 Use of magnetic hysteresis properties andelectron spin resonance spectroscopy for the identimacrcation of volcanic ash a preliminary studyGeophys J Int 132 712720
Pearce N J G Westgate J A amp Perkins W T 1996 Developments in the analysis of singleglass shards in volcanic deposits by laser ablation ICP-MS quantitative and single internalstandard multi-element methods Quat Int 3436 213227
Pearce N J G Westgate J A Perkins W T Eastwood W J amp Shane P 1999 Theapplication of laser ablation ICP-MS to the analysis of volcanic glass shards from tephradeposits bulk glass and single shard analysis Global Planet Change 21 151171
Pilcher J R amp Hall V A 1992 Towards a tephrochronology for the Holocene of the north ofIreland Holocene 2 255259
Ponel P amp Lowe J J 1992 Coleopteran pollen and radiocarbon evidence from the Prato Spillarsquo Drsquo succession N Italy C R Acad Sci Paris Sparaer II 315 14251431
Rose N L Golding P N E amp Battarbee R W 1996 Selective concentration and enumerationof tephra shards from lake sediment cores Holocene 6 243246
Ruddiman W F amp Glover L K 1972 Vertical mixing of ice rafted volcanic ash in NorthAtlantic sediments Geol Soc Am Bull 83 28172836
Ruddiman W amp McIntyre A 1981 The North Atlantic Ocean during the last deglaciationPalaeogeogr Palaeoclimatol Palaeoecol 35 145214
Santacroce R 1987 Somma Vesuvius Quad Ric Sci 114 252
Sarna-Wojcicki A 2000 Tephrochronology In Quaternary geochronology methods and applica-tions (ed J S Noller J M Sowers amp W R Lettis) AGU Reference shelf vol 4 pp 357377Washington DC American Geophysical Union
Sejrup H P Sjiquest holm J Furnes H Beyer I Eide L Jansen E amp Mangerud J 1989Quaternary tephrochronology on the Iceland Plateau north of Iceland J Quat Sci 4 109114
Sikes E L Samson C R Guilderson T P amp Howard W R 2000 Old radiocarbon agesin the southwest Pacimacrc Ocean during the last glacial period and deglaciation Nature 405555558
Stein R Nam S-I Grobe H amp Hubbersten H 1996 Late Quaternary glacial history andshort term ice rafted debris deg uctuations along the East Greenland continental marine In LateQuaternary palaeoceanography of the North Atlantic margins (ed J T Andrews W E NAustin H Bergsten amp A E Jennings) pp 135151 Geological Society London SpecialPublication
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 801
Stuiver M amp Grootes P M 2000 GISP2 oxygen isotope ratios Quat Res 53 277284
Stuiver M Reimer P J Bard E Beck J W Burr G S Hughen K A Kromer BMcCormac G Van der Plicht J amp Spurk M 1998 INTCAL 98 radiocarbon age calibration24 0000 cal BP Radiocarbon 40 10411083
Sweatman T R amp Long J V P 1969 Quantitative electron microprobe analysis of rock formingminerals J Petrol 7 332379
Turney C S M 1998 Extraction of rhyolitic ash from minerogenic lake sediments J Paleolim-nol 19 199206
Turney C S M amp Lowe J J 2001 Tephrochronology In Tracking environmental changes inlake sediments physical and chemical techniques (ed W M Last amp J P Smol) DordrechtKluwer Academic
Turney C S M Harkness D D amp Lowe J J 1997 The use of microtephra horizons tocorrelate Lateglacial lake sediments successions in Scotland J Quat Sci 12 525531
Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
van den Bogaard P amp Schmincke H 1985 A widespread isochronous Late Quaternary tephralayer in central and northern Europe Geol Soc Am Bull 96 15541571
van den Bogaard B Dordeg er W Sandgren P amp Schmincke H-U 1994 Correlating theHolocene records Icelandic tephra found in Schleswig-Holstein (northern Germany) Natur-wissenschaften 81 554556
Vernet G amp Raynal J-P 2001 Tephrostratigraphy of the Limagne revisited Implications forLateglacial and Holocene Prehistory In Tephras chronology archaeology (ed E Juvignparae ampJ-P Raynal) pp 111116 Dossiers de lrsquo ArchparaeoLogis no 1 France
Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
Vezzoli L 1991 Tephra layers in Bannock Basin (eastern Mediterranean) Mar Geol 1002134
von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
Walker M J C Bjorck S Lowe J J Cwynar L C Johnsen S Knudsen K-L WohlfarthB amp INTIMATE Group 1999 Isotopic events in the GRIP ice core a stratotype for the LatePleistocene Quat Sci Rev 18 11431150
Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
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Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
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European tephrochronological framework for Termination 1 775
Altogether 34 tephra layers have been reported from sediment sequences in Europeand the NE Atlantic region which date to the period between 185 and 80 14C ka BP(table 1) Because tephra layers are deposited virtually instantaneously (in geologicalterms) they enotectively represent time-parallel marker horizons within stratigraphicalsequences (Westgate amp Gorton 1981 Sarna-Wojcicki 2000 Turney amp Lowe 2001) Intheory therefore all 34 tephras could prove valuable for correlation purposes eitherin a local context or in those cases where the ash deposits have been widely dispersedbetween regional sequences In practice however very little is known about the fullgeographical dispersal of the majority of the ash layers listed in table 1 Furthermorecorrelation by tephrostratigraphy will only work if the various ash layers have wellcharacterized geochemical signatures While some geochemical data are available forthe majority of the tephras listed in table 1 the collective data are far from robustand no geochemical data have yet been published for some
Nonetheless there is mounting evidence to show that some of the tephra depositslisted in table 1 are not only geochemically distinct but are also much more widelydispersed across Europe than was initially realized Stratigraphic records of thebetter-known tephras were initially limited to observations of visible tephra layersThe development of a technique that enables detection of tephra layers that are invis-ible to the naked eye (micro-tephra) in Late Glacial sequences has greatly extendedthe area over which some of the ashes can be traced (Lowe amp Turney 1997 Turneyet al 1997 Turney 1998 Wastegard et al 1998 2000a b) Most of this research sofar has focused on micro-tephra layers originating from Icelandic centres distributedthroughout northern Europe Here we report on further development of this line ofresearch with new evidence for the occurrence of micro-tephra layers in a site insouthern Europe The results suggest that there is great potential for tracing someash layers that originated from Italian volcanic complexes over much larger tracts ofsouthern and central Europe than records of visible tephra deposits allow This inturn greatly enhances the scope for making precise correlations not only betweenparts of southern Europe but also between continental and marine (MediterraneanSea) sequences
2 Micro-tephra extraction techniques
Micro-tephra horizons are composed of glass shards that are generally between 80and 24 m m (long axis) in size and that are present in such low concentration insedimentary sequences that they can only be detected by the use of a particle sep-aration technique Several factors inreguence the concentration of shards such as dis-tance from the volcanic source precipitation patterns during the eruption and sub-sequent tephra dispersal and sedimentary processes within the catchment In someterrestrial sequences micro-tephra horizons with a peak concentration (peak con-centration tends to coincide with the shy rst occurrence of glass shards in a sedimentsequence which is then taken to mark the time of maximum ash deposition) as lowas 10 shards cmiexcl3 has been conshy rmed whereas other sites have recorded as muchas 8000 shards cmiexcl3 (Turney et al 1997) In complete contrast tephra horizons inthe GRIP ice core have been identishy ed based on a single glass shard only (Gronvoldet al 1995)
Enotective separation techniques for the detection and isolation of tephra particlesfrom sedimentary sequences have been developed These include ashing of organic
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776 S M Davies and others
matter (Pilcher amp Hall 1992) digestion of biogenic and opaline silica (Rose et al 1996) the use of magnetic properties of ash layers (see for example Oldshy eld et al 1980 van den Bogaard et al 1994 Pawse et al 1998) X-ray analysis (Dugmore ampNewton 1992) and a density separation (regotation) technique (Turney 1998) Den-sity separation has proved exceedingly useful for the detection of small glass shardspresent in low concentrations in mineral-rich Late Glacial sediments This involvesthe separation and concentration of particles of predetermined specishy c gravity withthe use of a heavy liquid and subsequent identishy cation of glass shards with the useof a polarizing light microscope (for further details see Turney (1998)) This methodhas been particularly successful in the detection of tephras of rhyolitic compositionthat have a specishy c density of 2325 g cmiexcl3 (Lowe amp Turney 1997 Turney et al 1997 2001 Turney 1998 Wastegard et al 1998 2000a b) It is this technique thathas resulted in the wider recognition of micro-tephras in Europe as discussed below
3 Geochemical ` ngerprintingrsquo of tephra layers
The 34 tephras listed in table 1 have originated from four major volcanic complexesIceland the Massif Central in central France the Eifel district near Bonn and threevolcanic centres in Italy (the Campanian group Etna and the Aeolian Islands (seeshy gure 2)) An important matter to resolve is the extent to which the various magmasand ashes generated by these volcanic complexes can be geochemically shy ngerprintedThis is especially important in the case of tephras which have originated from thesame volcanic centre in which there may have been limited geochemical evolution ofmagmas over time In this section we summarize the approach generally adopted todetermine the geochemical character of visible and micro-tephras as background tothe geochemical data summarized in table 1 In the subsequent section of the paperwe review the present state of knowledge concerning all 34 tephras listed in table 1
Glass shards formed during the rapid cooling of magma are thought to have acomposition that is representative of the bulk geochemistry of the magma (Barker1983) hence widely dispersed glass particles are regarded as the most appropriateconstituents of pyroclastic material for geochemical analysis If a tephra deposit canbe shown to have a distinct geochemical signature then it can be used to correlatethe stratigraphic units in which it occurs (tephrostratigraphy) as well as to datethese units (tephrochronology) if the ages of the tephras are known (Westgate ampGorton 1981) A key element of building a tephrostratigraphical framework there-fore is to establish as rigorously as possible the geochemical composition of theindividual tephras used in its construction Robust and directly comparable geo-chemical datasets are dimacr cult to assemble for glass however because it is highlyunstable material particularly prone to sodium mobilization
The technique most widely employed to establish the geochemical signature of atephra is electron probe micro-analysis (EPMA) This enables grain-discrete determi-nations of the major elements within an individual glass shard which is of particularbeneshy t in the analysis of micro-tephra layers which generally contain glass particlesin low concentration The glass surface is bombarded with an electron beam and theX-ray energy produced is unique to each element while the intensity of the signalemitted is proportional to the amount of that element in the glass shard (Hunt amp Hill1993) Measurement can be by either energy dispersive spectrometry (EDS) or wave-length dispersive spectrometry (WDS) EDS has a lower precision mainly because
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 777
N
0 500 km
Confirmed records of Vedde Ash (visible occurrences)
New records of Vedde Ash from flotation method
Extended area of Vedde Ash detection (micro-tephra)
Known area of Laacher See Tephra (visible occurrences)
Confirmed records of Neapolitan Yellow Tuff (visible occurrences)
New record of Neapolitan Yellow Tuff from flotation method
Known area of Neapolitan Yellow Tuff
Volcanic centres of particular relevance to this study
Other major volcanic centres in Europe
Figure 2 Location of the principal volcanic centres that were active during Termination 1 andthe Early Holocene The known distribution of the Vedde Ash (VA) Laacher See (LST) andNeapolitan Yellow Tureg (NYT) are shown
the behaviour of each element cannot be monitored independently during measure-ment and so this approach fails to detect for example any signishy cant mobilizationof sodium during the bombardment process (Hunt amp Hill 1993) Although WDSrequires a higher beam current and a longer counting time than EDS the formeronoters the distinct advantage of sequential acquisition of elemental data so that thedegree of sodium loss can be tracked The morphology of individual glass shards canalso distort EDS data a problem that is reduced when using WDS because for thisprocedure glass shards are mounted in an epoxy resin and polished to provide aregat surface for analysis Hence data should always be obtained using WDS whereverpossible
Even when WDS is used as a common tool for determining the geochemical spectraof samples aberrant results can arise that inreguence data comparisons For examplesome glass shards may contain tiny crystalline inclusions of feldspar and these shouldbe avoided when selecting surface points for analysis (Hunt amp Hill 2001) Hunt amp Hill
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778 S M Davies and others
6
4
2
40 50 60 70 80
K2O
(
)
SiO2 ()
Laacher See
Iceland
Veidivoumltn-Dyngjufjoumlll
Katla (basalt)
Grimsvoumltn-Kverkfjoumlll
Hekla
Katla (rhyolitic)
0
Icelandic volcanic centres8
10
Massif Central
Etna
Campanian
Figure 3 Bi-plot of SiO2 and K2 O concentrations in tephras derived from the main Europeanash provinces (modimacred after Mangerud et al 1984) The Campanian Massif Central and Etnaconcentrations are based on the data presented in table 1
(2001) have concluded that small variations in the laboratory procedures employedto determine glass chemistry can lead to misidentishy cation of sources for glass shardsand give an example of shards with a Jan Mayen provenance wrongly attributedto an Icelandic source Clearly there is a need for standardization of laboratoryprocedures and while a number of recommendations have recently been advocated(Froggatt 1992 Hunt amp Hill 1993 Hunt et al 1998) there is still some variation inlaboratory and operator practice (Hunt amp Hill 1996) Standardization is also requiredin the form in which results are presented to ensure comparability Normalizationof the data to 100 a practice employed by some researchers can obscure poorresults and hence lead to incorrect comparisons (Hunt amp Hill 1993) However othersargue that it may actually facilitate comparisons between samples by removing thedistorting enotects of the water component contained in glass shards (see for exampleFroggatt 1992) The majority of the published Italian and some of the Eifel datahave been normalized while those from other parts of Europe have not and hencedata comparisons are not always straightforward
Table 1 provides mean values and standard deviations for major oxide concentra-tions obtained from those tephras for which data are presently available The tableincludes previously unpublished WDS results for the Neapolitan Yellow Tunot (NYTdiscussed in x 4 below) and for the Mercato Tephra While individual tephra layersmay be geochemically distinct the geochemical envelopes representing the collectivedata obtained from all of the tephras assigned to each major volcanic province showsignishy cant overlaps as is illustrated in the bi-plots and ternary plots (shy gures 3 and 4)of selected oxide concentration data It is clear therefore that measurement of majoroxide concentrations does not satisfactorily discriminate between some tephras orig-inating from dinoterent volcanic centres (as noted by van den Bogaard amp Schmincke(1985) and Frezzotti amp Narcisi (1996) with respect to Eifel and Italian tephras)nor of tephras of dinoterent age originating from the same volcanic centre (Bond et
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European tephrochronological framework for Termination 1 779
40 50 60 70 80
K2O
(
)
SiO2 ()
shyshyshyshy
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shyshy
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shy
shy
reg
reg regreg
regregregregreg regregregregreg
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4 8 12 16
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l shyshyshyshyshy shyshyshyshyshyshy
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F
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ll
FeO ()
TiO
2 (
)
reg
l
Iceland
Eifel
F
shy ItalyMassif Central
100
80
60
40
20
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80
60
40
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100 80 60 40 20
CaO
FeO
K2O
regregreg
reg
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lllshy
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0
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regreg
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FF
F
100
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60
40
20
100
80
60
40
20
100 80 60 40 20
K2ONa2O
CaO
(c) (d)
(a)
(b)
Figure 4 Plots of selected geochemical data obtained from tephras of Termination 1 age (seetable 1) (a) Bi-plot of mean SiO2 and K2 O values (b) Bi-plot of mean FeO and TiO2 values(c) Ternary plot indicating variations in the proportions of FeO CaO and K2 O (d) Ternaryplot indicating variations in the proportion of CaO Na2 O and K2 O
al 2001) Individual tephra layers are presently assigned to a particular volcanicevent on the basis of a combination of criteria usually including examination of thephysical properties (eg refractive index and surface detail of the glass shards) thestratigraphic position of the layer and independent assessment of the age of the layeras well as any geochemical data that may be available The construction of a tephro-stratigraphical scheme would clearly beneshy t from the application of a more diagnostic
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780 S M Davies and others
geochemical tool One approach that has promise is the analysis of trace and rareearth elements using an ultraviolet laser ablation inductively coupled plasma massspectrometer (UV-LA-ICP-MS) (Pearce et al 1996 1999 Eastwood et al 1999)This approach has been applied successfully to analysis of tephras of Mid-Holoceneage but not yet to tephras that fall within the period of interest here
4 Tephra layers in Europe and the North Atlantic regiondated to between 185 and 80 14C ka
(a) Icelandic province
The Icelandic volcanic systems are divided into three main groups based on theirgeochemical characteristics tholeiitic basalts transitional alkali basalts and alkaliolivine basalts (Jakobsson 1979) Collectively magmas from the Icelandic provincespan a wide geochemical spectrum although individual volcanic centres have tightgeochemical distributions (shy gure 3) for four of the main centres Grimsvotn-Kverfjolland Veidvotn-Dyngjufoll which form part of the northern (tholeiitic) volcanic zoneand Hekla and Katla which fall within the eastern (alkali olivine basalt and transi-tional alkali basalt) volcanic zone (Haregidason et al 2000) These appear to be thekey centres for the tephras listed in table 1 that have been assigned an Icelandicorigin
One of the best-known and most widely dispersed tephra horizons in northernEurope that has an Icelandic origin is the Vedde Ash (VA) which was depositedca 103 14C ka BP (Birks et al 1996 Wastegard et al 1998) within the GS-1Younger Dryas chronozone This ash is believed to originate from the Katla complexwithin the transitional alkali basalt province (Mangerud et al 1984 Lacasse et al 1995) in the south of the island The ash has a bimodal geochemical composition (rhy-olitic and basaltic) which is thought to reregect derivation from two separate magmachambers Studies of recent volcanic events in Iceland have shown that the mostexplosive eruptions generating the largest amounts of tephra occur in this tran-sitional alkali basalt province (Haregidason et al 2000) It is also believed that thewidespread distribution of this ash was caused by the development of co-ignimbriteash plumes during an ignimbrite-forming eruption (Lacasse et al 1995)
Layers of VA that are visible to the naked eye have been found in lake sediments inwestern Norway (Mangerud et al 1984) and the Inner Hebrides Scotland (Davies etal 2001) and in marine cores throughout the NE Atlantic (see for example Kvammeet al 1989 Lacasse et al 1995) in the northern North Sea (Long amp Morton 1987)on the Iceland plateau (Ruddiman amp McIntyre 1981 Sejrup et al 1989) and on theeast Greenland continental margin (Stein et al 1996) The distribution of the VAin North Atlantic marine sequences is characterized by an arcuate lobe extendingsouthwest from the Denmark Strait and curving eastwards to mid-latitudes in theNorth Atlantic (Lacasse et al 1995) This strongly suggests deposition from raftedice which was displaced to the southwest and south in a circulating counterclockwisegyre (Ruddiman amp Glover 1972) This may well reregect Katlarsquos close proximity tothe southern coast of Iceland with the Vedde tephra being deposited on ice thatcalved directly into the North Atlantic (Haregidason et al 2000) However depositionvia the atmosphere almost certainly took place as well as is indicated by the recentdiscoveries of rhyolitic VA in micro-tephra form in several sites in Scotland (Turneyet al 1997) southern Sweden (Wastegard et al 1998 2000a) and western Russia
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European tephrochronological framework for Termination 1 781
(Wastegard et al 2000b) A more recent discovery of a relatively high concentrationof rhyolitic VA glass shards in the northern Netherlands indicates that the ash maywell have been dispersed much further south than previously thought (S M Davies2002 unpublished work) Finally glass shards assigned to the VA have also beendiscovered in the GRIP ice core and dated to 11 980 sect 80 GRIP yr BP (Gronvold etal 1995) This discovery is extremely important for it indicates that the VA maywell provide a reliable time-parallel marker horizon between ice-core marine andterrestrial records
Two other important Icelandic ash layers the Borrobol and Saksunarvatn Tephraswere deposited near the beginning and end of the Last TerminationEarly Holoceneinterval respectively The Borrobol Tephra was discovered for the shy rst time in lakesediments in several sites in Scotland and as yet is known only in micro-tephra formIt has been dated in Scottish sites to ca 123 14C ka BP (Turney et al 1997) Whatis thought to be a contemporaneous tephra has been detected in marine sedimentson the North Icelandic shelf (Eirplusmn ksson et al 2000) This certainly has a very similargeochemical composition to those reported from Scotland but the horizon in whichit was discovered on the North Iceland plateau has been dated to 134 14C ka Theage discrepancy between the Scottish and Icelandic Borrobol Tephra layers may wellreregect the inreguence of a marine reservoir error although the possibility that severaltephras with similar geochemical composition were erupted over a period exceeding1000 yr cannot be ruled out (Larsen 2000)
The Saksunarvatn Ash appears to have been one of the largest Holocene eruptionsin Iceland It has a tholeiitic basaltic composition which is considered to indicate anorigin in the Grimsvotn or Kverfjoll complex (shy gure 3) (Mangerud et al 1986) Layersof this ash have been identishy ed in sites on the Faroe Islands (Mangerud et al 1986Dugmore amp Newton 1998 Wastegard et al 2001) the Shetland Isles (Bennet et al 1992) northern Germany (Merkt et al 1993) western Norway (micro-tephra) (Birkset al 1996) and in the GRIP (Gronvold et al 1995) and NordGRIP ice cores (S MDavies 2002 unpublished work) It has been dated to between 9060 and 8930 14C kaBP (Birks et al 1996) in Norway and to ca 10 240 sect 30 GRIP yr BP in the GRIPice core (Gronvold et al 1995) The Saksunarvatn Ash may thus provide a secondimportant widespread time-parallel marker between ice-core marine and terrestrialrecords
Other Icelandic tephras of rhyolitic amacr nity are less well known in terms of theirdistribution and geochemical variation The Hogstorpsmossen Tephra reported fromSweden (Bjorck amp Wastegard 1999) and the L3754 tephra discovered in the FaroeIslands (Dugmore amp Newton 1998) are known from single sites only and so theirpotential for tephrostratigraphy is uncertain at present Furthermore the geochem-ical spectrum of the Hogstorpsmossen Tephra is based on a small dataset with lowanalytical totals
A number of tephras of basaltic composition have originated from Iceland buttheir distributions are largely conshy ned to Iceland or to marine cores collected fromclose to the Iceland coast or in the North Atlantic These include the tephras listedas 1-THOL-1 1-THOL-2 KOL-GS-2 GS-2BAS-1 GS-2BAS-2 GS-2BAS-3 andGS-2BAS-4 in table 1 (Kvamme et al 1989 Bjorck et al 1992 Eirplusmn ksson et al 2000 Haregidason et al 2000) The shy rst two in this list are tholeiitic basaltic tephrasassociated with the VA in a complex series of tephras collectively termed NorthAtlantic Ash Zone 1 (NAAZ1) which has been detected in numerous marine cores
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782 S M Davies and others
from the North Atlantic Initially thought to represent a single eruption analysisof high-resolution sediment sequences from Lake Torfadalsvatn in northern Iceland(Bjorck et al 1992) the Hebridean Shelf near NW Scotland (Austin amp Kroon 1996)the St Kilda Basin (Hunt et al 1995) and the open North Atlantic (Bond et al 2001)has demonstrated that NAAZ1 comprises a series of distinct ashes that probablyreregect separate eruption events 1-THOL-1 is thought to originate from Veidivotn(shy gure 3) while Grimsvotn may have been the source of 1-THOL-2 (Kvamme et al 1989)
KOL-GS-2 is also of tholeiitic basaltic composition but is thought to originatefrom the Kolbeinsey Ridge system (Eirplusmn ksson et al 2000) To date this tephra hasbeen detected in one marine core only within the same record on the North Ice-landic shelf as that from which the correlative of the Borrobol Tephra was alsoreported (Eirplusmn ksson et al 2000) GS-2BAS-1 to GS-2BAS-4 are of uncertain ori-gin but are thought to have been deposited at roughly the same time as KOL-GS-2(ca 134 14C ka BP (Haregidason et al 2000))
The limited distribution of these basaltic tephras a feature that is not unique toIcelandic basaltic material may reregect two factors the relative magnitude of the vol-canic eruptions from which they were derived and the limited aerial transportationof basaltic glass which is denser than rhyolitic material However a rather surpris-ing recent discovery is that of visible basaltic VA in a site on the Isle of Skye inthe Inner Hebrides Scotland (shy gure 5) (Davies et al 2001) All other occurrencesof VA in Scotland are exclusively of rhyolitic material and in micro-tephra formonly (Turney et al 1997 Turney 1998) Clearly basaltic tephra must have beentransported subaerially as far south as Skye and the reason why it has not beendetected at other sites in Scotland is puzzling We suspect that this partly reregectsthe laboratory methods employed to separate glass shards present in low concentra-tion within a micro-tephra layer from the host sediment The technique used is adensity-separation (regotation) procedure (Turney 1998) and as basaltic shards havea specishy c density similar to quartz one of the most abundant minerals in lake sedi-ments of Late Glacial age basaltic material is dimacr cult to detect using this methodThis hypothesis is currently under investigation and alternative detection methodsare being explored including magnetic separation (Mackie et al 2002)
Several other events listed in table 1 that are of probable Icelandic origin includetephras recorded in the GRIP ice core including visible (eg the `Black Featherrsquo)tephras as well as uncertain tephras inferred from distinct Ca peaks (S Johnsen2001 personal communication) No glass shards have yet been detected in the latterbut a volcanic origin is assumed because high Ca peaks are associated with knowntephras in other Greenland ice cores (S Johnsen 2001 personal communication)These are referred to as `unknownrsquo in table 1 No geochemical analyses are availablefrom these horizons so their origin must remain speculative but a possible source isIceland in view of its proximity to the Greenland ice sheet and assumed atmosphericcirculation patterns
(b) Eifel province
There are two prominent tephra events dated to the Termination 1Early Holocenetime-span that originated from the Eifel province the Laacher See Tephra (LST)and the Ulmener Maar Tephra (UMT) Visible occurrences of the LST indicate that
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European tephrochronological framework for Termination 1 783
Vedde Ash
615 625 635 645 655depth (cm)
organic lake mudsHolocene
silty clayGS-1Younger Dryas
organic lake mudsGI-1Alleroslashd
100 microm
(a)
(b)
Figure 5 (a) Photograph of the visible VA layer discovered at Loch Ashik Isle of Skye InnerHebrides Scotland (b) Light microscope photograph showing the rich content of basaltic shards(examples are indicated by the arrows) within this layer (8024 m m size fraction)
this ash was dispersed over much of central Europe (van den Bogaard amp Schmincke1985 Friedrich et al 1999 Litt amp Stebich 1999) The LST is dated by radiocarbonto ca 110 14C ka BP (van den Bogaard amp Schmincke 1985) and to 11 063sect12 14C BP(Friedrich et al 1999) by varve chronology to 1288 varve ka BP (Brauer et al 1999Litt et al 2001) and by ArAr dating to 129 ka cal BP (van den Bogaard 1995) Ithas a phonolitic composition and is thought to have originated from a plinian andphreatomagmatic eruption with the distal ash being carried in three distinct plumesone to the northeast towards Poland one to the west and the third to the southcovering the Jura Mountains and north Italy (van den Bogaard amp Schmincke 1985Juvigne et al 1995 Bossuet et al 1997) This pattern is thought to reregect altitu-dinal variations in the predominant wind direction Sedimentary sequences near thevolcanic source indicate that the LST consists of three main layers which represent
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784 S M Davies and others
dinoterent eruption phases These are grouped together as the Laacher See TephraFormation but the three individual units can be traced within and between a seriesof depositional fans The geochemical data obtained from these three LST layersshow signishy cant variations as reregected in the ternary plots (shy gure 4)
The Early Holocene Ulmener Maar Tephra (UMT) is of rhyolitic composition andappears to be restricted to sites in Germany though this conclusion is also based onrecords of visible tephras only It is dated to ca 956 14C ka BP and to 110 varve ka(Zolitschka et al 1995 Litt et al 2001)
(c) Massif Central province
The Massif Central tephras are mainly of basaltic trachyandesitic compositionwhich is distinct from the other ash provinces (shy gures 3 and 4) and their known dis-tributions are mostly conshy ned to the Massif Central region The ages of the MassifCentral tephras are based on radiocarbon dates obtained from mire and lake sedi-ments which `bracketrsquo the tephras The La Nugsup3ere Tephra with an age of 114 14C kaBP is the oldest Massif Central tephra identishy ed so far within the time-span of inter-est (Etlicher et al 1987 Juvigne et al 1996) The two Godivelle Tephras (5 and 4)are close in age but extensive radiocarbon dating suggests distinct ages of 107and 103 14C ka BP respectively (Juvigne et al 1996) The age of the Puy de DomeTephra is less certain as the estimate is based on only one radiocarbon date froma site in the southern Chaplusmn ne des Puys (table 1) This tephra is thought to havea trachyte composition (Juvigne 1993) although no major element concentrationshave yet been published
The ChopineKilianVasset tephras are thought to be derived from three separateEarly Holocene eruptions although the stratigraphic succession is not known atpresent These trachytic tephras have been radiocarbon dated to ca 854sect150 14C kaBP but are thought to have erupted separately within ca 260 yr (Juvigne et al 1996) This series of tephras is considerably more widespread than the others fromthe region having been identishy ed as far east as the Jura Mountains (Martini amp Duret1965 Martini 1970) Some other ash falls that originated from the Chaplusmn ne des Puysappear to be of local importance only (Vernet et al 1998 Vernet amp Raynal 2001)Geochemical data are currently available for only three of the Massif Central tephrasand so far as is known no attempt has yet been made to identify these tephras inmicro-tephra form
(d ) Italian provinces
The Italian tephras from this period can be assigned to three main volcanic com-plexes the Campanian volcanic shy elds around Naples Etna on Sicily and the AeolianIslands The Campanian complex which includes the Phlegrean Fields Vesuviusand Ischia is mainly trachytic in composition with a geochemical spectrum that isquite distinct from those of the Etna complex and of the Aeolian Islands (shy gure 3)Tephras originating from one or more of these three complexes have been detectedin marine cores from the Tyrrhenian and Adriatic seas as well as other parts of theMediterranean Sea (Keller et al 1978 Paterne et al 1986 1988 1990 Langone etal 1996) and in lake sequences in southern Italy such as Lago Grande di Monticchio(Newton amp Dugmore 1993 Narcisi 1996 Allen et al 1999) and central Italy such asLago Albano near Rome (Calanchi et al 1996) Some work has also been conducted
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European tephrochronological framework for Termination 1 785
in or close to the volcanic source areas in an attempt to establish the full sequenceof volcanic eruptions during the Late Quaternary (see for example Di Vito et al 1999) There are nine Italian tephras reported from marine and lake sequences thatdate from the period between 185 and 80 14C ka BP In all instances the recordsare of visible layers of tephra The ages of some of these are poorly established atpresent with conregicting data obtained from dinoterent sites The ages suggested intable 1 are those favoured in the most recent publications but these may requirere-assessment in the light of future research
The two oldest known tephras in the time-period of interest are the L9 and Green-ish Tephras both recorded as separate features within the annually laminated Lagodi Monticchio maar sequence The lowest of the two L9 is considered to be the cor-relative of the `basalrsquo plinian eruption of Vesuvius (Narcisi 1996) Age estimates ofa palaeosol that underlies the Vesuvius tephra sequence are ca 1617 14C ka BP forthis event (Delibrias et al 1979) L9 has a trachytic composition very similar to theGreenish Tephra (table 1) However L9 which is also a product of Vesuvius is foundstratigraphically below the Greenish Tephra in the Lago di Monticchio core TheGreenish Tephra is dated in the Monticchio sequence to 17 560 varve yr BP (Allenet al 1999) and has a calibrated radiocarbon age estimate of 17 830 sect 300 cal BP(Andronico et al 1995) Both tephras have a dominantly eastwards dispersal basedon the occurrences of visible layers (Santacroce 1987 Narcisi 1996) Both tephrasalso have a trachytic composition and as can be seen from table 1 the reportedgeochemical spectra are very close indeed with the standard deviations overlappingfor almost every major element This could present problems for tephrostratigra-phy where only one of the tephras is evident in a sediment sequence in particularbecause they are so close in age This is a good example of where an analysis oftrace and rare earth elements might be required to make a clear distinction betweentephras with very similar major oxide concentrations
The Y-1 Tephra also termed the Biancavilla Montalto Ignimbrite (Vezzoli 1991)is a product of Etna and has been identishy ed as a visible benmoritic tephra horizonthroughout the central Mediterranean (Paterne et al 1988) including central Italyand the Adriatic Sea (Vezzoli 1991 Narcisi 1993 Calanchi et al 1996) It has anestimated age of ca 140 14C ka BP The Unita dei Tefra Superiori tephra which hasbeen detected as far east as Lago di Monticchio in south-central Italy (Narcisi 1996)is also dated to ca 140 14C ka BP (Alessio et al 1976) but it is thought that thesource of this tephra lies in the Phlegrean Fields No geochemical data are availablefrom the presumed source region|the data reported in table 1 were obtained fromthe Lago di Monticchio record (Narcisi 1996)
The NYT which is equivalent to the C-2 tephra reported from various marinesequences has also been traced throughout central Italy and the Adriatic Sea (Pat-erne et al 1988 Calanchi et al 1996 Di Vito et al 1999) (shy gure 2) In the centralApennines region it formed the parent material for a soil that started to developat the beginning of the Holocene period (Frezzotti amp Narcisi 1996) Also originatingfrom the Campi Flegrei caldera it is dated to ca 120 14C ka BP (Di Vito et al 1999) Published geochemical data based on EDS indicate three dinoterent geochemicalpopulations varying from latite to phonotrachyte in composition (Orsi et al 1992Paterne et al 1988) (table 1) We report in x 4 of this paper on new data obtainedfrom the NYT by WDS and it is the mean of these new data that is included intable 1 Comparisons with the previously published EDS data are provided (table 1)
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786 S M Davies and others
The new data indicate clearly that the NYT originated from the Campanian volcaniccentre
In the interval between the dispersal of the NYT (ca 120 14C ka BP) and 95 14Cka BP there appear to have been as many as 34 eruptions in the Campi Flegrei caldera(Di Vito et al 1999) Of these only one appears to have been detected widely in theregion the Pomici Principali (also termed the Agnano Formation or C-1 tephra inmarine records (Paterne et al 1988) This was the product of the highest magnitudeeruption from this epoch and is dated to between 976 sect 300 and 1032 sect 50 14C kaBP (Delibrias et al 1979 Di Vito et al 1999) or to 122 varve ka BP based on theMonticchio varve chronology (Allen et al 1999) It is trachytic in composition andappears to have had a mainly eastwards dispersal
The Mercato Tephra dated to ca 80 14C ka BP and originally analysed usingEDS has a phonolitic composition and is believed to have been generated by Vesu-vius (Paterne et al 1988) New WDS data obtained from reference samples col-lected from an exposure to the west of Naples support these conclusions (table 1 andAppendix A) The silica content of the WDS analyses are ca 3 lower than thoseobtained using EDS (table 1) which may reregect the fact that the EDS data werenormalized
The only tephra listed in table 1 that is thought to have originated from the AeolianIslands is the Pollara pumice also referred to as the E2 tephra in marine sequences(Paterne et al 1986 1988) The limited geochemical data available so far suggest itto be the only Italian tephra listed in table 1 that is rhyolitic in composition Littlemore is known about this ash which has not been recorded extensively except thatits age is estimated to be ca 130 14C ka BP (Keller 1980)
5 Extending the known distributions of European tephras
Figure 2 summarizes schematically the known distributions of three of the tephrasreferred to in the preceding section the VA the LST and the NYT Following theintroduction of a laboratory method that enables the detection of micro-tephra parti-cles in mineral-rich sediment the VA has been traced to sites that are located muchfarther south (into The Netherlands) and east (as far as St Petersburg) than thedistribution limits based on occurrences of visible layers of the ash As a result con-tinental sequences over a much larger area in northern Europe can now be correlateddirectly with marine and ice-core records using the VA as a time-parallel marker
This suggests therefore that other prominent ash layers such as the LST andNYT should also be detectable over larger tracts of Europe than is presently thecase if suitable sites are examined for the presence of micro-tephra horizons To testthis assertion we examined lake sediment deposits of Last Termination age froma site in the northern Apennines in order to establish whether the NYT could bedetected in micro-tephra form The site selected Prato Spilla `Crsquo lies well to thenorth of the localities in central and southern Italy and in the Adriatic Sea fromwhich visible records of the NYT have been reported Prato Spilla `Crsquo lies at an alti-tude of ca 1350 m in the Appennino Parmense ca 60 km south of Parma and 15 kmeast of Pontremoli The site contains a continuous sediment sequence spanning theLast Termination and most of the Holocene Detailed pollen and coleopteran strati-graphical records which have been radiocarbon dated have been published for thissite (Lowe 1992 Ponel amp Lowe 1992 Lowe amp Watson 1993)
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European tephrochronological framework for Termination 1 787
Figure 6 Light microscope photograph of an NYT glass shard from Prato Spilla Crsquosequence assigned on geochemical grounds to the NYT
The methods adopted for sub-sampling of the Prato Spilla `Crsquo sequence for thequantishy cation of glass shard concentrations and for subsequent electron microprobeanalysis of selected glass shards followed those described elsewhere (Turney 1998)In summary contiguous samples of 1 cm stratigraphic interval were extracted fromthe sequence to establish presenceabsence of glass shards Each of the 1 cm3 blocksin which tephra particles was detected was then examined with more care andshard concentrations were quantishy ed for each sub-sample Micro-tephra particleswere detected in shy ve samples (shy gure 6) but were predominantly clustered around500 cm in the part of the sequence assigned on pollen-stratigraphic grounds to theLate Glacial Interstadial or the `Allerfrac12drsquo|indeed the part of the succession in whichthe NYT would be expected to occur Peak concentrations of micro-tephra particlesreach 225 shards cmiexcl3 and are conshy ned to a single 1 cm thick sample in the sequencewhich probably represents the time of maximum deposition of the ash
Electron microprobe measurements based on WDS were obtained from the surfacesof 21 separate glass shards extracted from the sample with peak shard concentrations(Appendix A) Since only EDS measurements were available for the NYT prior to thepresent study we also obtained WDS measurements from 17 shards extracted fromthe visible layer of NYT that is exposed on Procida Island which lies in the type-locality for the NYT close to the city of Naples (Appendix A) The results providenot only a more comprehensive geochemical dataset for the NYT than was previ-ously available but also a consistent basis for comparison with the Prato Spilla `Crsquodataset All of the WDS data reported here (Appendix A) were measured at the samelaboratory (Tephrochronology Analytical Unit University of Edinburgh) using thesame sample pretreatment and preparation protocol The WDS results for the NYTdinoter to a minor degree from the EDS results (table 1 and Appendix A) especiallywith respect to the amounts of silica aluminium and calcium measured The EDS
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788 S M Davies and others
4 8FeO ()
TiO
2 (
) Neapolitan Yellow Tuff(Procida)Neapolitan Yellow Tuff(Prato Spilla lsquoCrsquo)
0
1
2
3
40 50 60 70
MgO
(
)
SiO2 ()
K2O
(
)
40 50 60 70
0
04
08
4
8
12
SiO2 ()
(a)(b)
(c)
Figure 7 Bi-plots of SiO2 K2 O SiO2 MgO and FeOTiO2 for the WDS analyses obtainedfrom glass shards of the NYT from Procida (Naples) and Prato Spilla Crsquo Means and standarddeviations are shown
results show a higher degree of statistical scatter than the WDS measurements whichmay reregect the fact that the data were normalized combined with the inreguence ofvariation in water content between shards
There is a very close correspondence between the WDS data for the Prato Spilla `Crsquomicro-tephra shards and those obtained from the type-material near Naples (shy g-ure 7) The geochemical data strongly suggest therefore that the NYT is representedat the Prato Spilla `Crsquo site by a discrete layer of micro-tephra particles This conclu-sion is compatible with the pollen-stratigraphic data from the site and accords withage estimates for the NYT (ca 120 14C ka BP) obtained from other sites (Paterneet al 1990)
These results encourage us to believe that many if not all of the tephras listedin table 1 will be detectable over much larger tracts of Europe than is presently thecase if appropriate research is undertaken to detect layers of micro-tephra particlesin selected sites The authors are presently engaged in a major continent-wide pro-gramme of research in collaboration with a number of European research groupsdesigned to test this hypothesis The focus in this research is on those parts of Europewhere we expect to shy nd overlapping `apronsrsquo of tephra deposition originating fromthe Italian Eifel Massif Central and Icelandic provinces For example a number ofsites in parts of southern France northern Italy and perhaps western Switzerlandmay have received inreguxes of micro-tephra originating from the Italian and Eifelprovinces and perhaps also from the Massif Central Sites in parts of Germany Den-mark and southern Sweden for example may in turn have received tephra depositsfrom both of the Icelandic and Eifel provinces If this proves to be the case then thestage will be set for the construction of a tephrostratigraphical framework for Europewhich will enable Last Termination sequences to be correlated on a continent-widebasis using micro- and visible tephra layers as time-parallel stratigraphic markersFurthermore there is also the possibility that other tephras remain to be discovered
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 789
those which either because of the magnitude or nature of some volcanic eruptionswere distributed over parts of Europe in micro-tephra form only
6 European tephrostratigraphy and the chronology of eventsduring the Last Termination and Early Holocene
One of the crucial issues in Late Quaternary palaeoenvironmental research thatremains to be resolved is the degree to which climatic events inferred from oceanicterrestrial and ice-core records were synchronous during the Last Termination andEarly Holocene If the ice-core records provide realistic estimates of the rates anddurations of climatic events during this period then comparisons between individ-ual records have to be enotected with at least a decadal precision The problem thispresents and the role that tephrostratigraphy can play in resolving some of thedimacr culties involved are put into perspective in shy gure 8
Figure 8 shows some of the data used to calibrate radiocarbon dates (the LakeSuigetsu and Cariaco Basin datasets) plotted against the GRIP ss08c ice-core recordof macr 18O variations The latter has been selected by the INTIMATE group as an arbi-trary and temporary standard for this period and used to deshy ne an event stratig-raphy scheme (shy gure 1) for the Last Termination (see Bjorck et al 1998 Walker etal 2001) As has been alluded to in earlier sections of this paper the uncertaintiesassociated with all of the dating methods currently employed preclude precise com-parisons of ice-core marine and terrestrial records Oceanic and terrestrial recordsmostly rely upon radiocarbon dating locally supplemented in a few cases by varvechronology Imprecisions in radiocarbon dates can arise through site-specishy c fac-tors (eg hard-water or mineral carbon errors in freshwater sequences and reservoirerrors in marine sequences) sample selection laboratory measurements of 14C activ-ity and other factors (Lowe amp Walker 2000) Further imprecision may be introducedby the calibration of radiocarbon dates since the uncertainties in the dataset usedto calibrate pre-Holocene radiocarbon dates INTCAL98 are far higher than forthe Holocene which is based on dendro-calibration (Stuiver et al 1998) There arealso uncertainties anotecting varve chronologies while the ss08c ice-core chronologyfor the Last Termination dinoters signishy cantly from the GISP2 record and indeedfrom other models of the GRIP record (Lowe et al 2001) Published comparisonsbetween ice-core marine and terrestrial records for the Last Termination seldom takeinto account the true magnitude of the dating uncertainties involved and frequentlyemploy circular reasoning
Figure 8 shows the positions on the radiocarbon time-scale of 20 of the tephrasdiscussed earlier in this paper these being the ones for which reasonably conshy dentradiocarbon age estimates can be made (though these will be subject to revised esti-mates in the future) A high number of these occur in the period 14080 14C kaBP but we conshy dently anticipate the discovery in the future of additional tephras(perhaps in micro-tephra form only) which will date to the period 185140 14C kaBP Tephras detected in the GRIP ice core over the same time-interval are plottedon the calendar time-scale in shy gure 8 By providing key `time-linesrsquo between recordstephrostratigraphy can help to resolve some of the dating uncertainties referredto earlier by for example enabling direct comparisons of discrepant age estimatesobtained using dinoterent methods (cf Litt et al 2001) It can also provide estimatesof the magnitudes of the reservoir errors that anotected various marine sectors at dif-
Phil Trans R Soc Lond A (2002)
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790 S M Davies and others
-44
-40
-36
-32
cale
ndar
yea
rs B
P
8000
9000
10 0
00
11 0
00
12 0
00
13 0
00
14 0
00
15 0
00
16 0
00
17 0
00
18 0
00
14C age (BP)
VA
SA
Un
Un
Un
Un
Un
BF
Hol
ocen
eG
S-1
GI-
1aG
I-1b
GI-
1cG
I-1d
GI-
1eG
S-2
aG
S-2
bG
S-
2c
Bor
robo
l
La
Nug
egravere
Laa
cher
See
God
ivel
le 5
amp I
-TH
OL
-2
Puy
de D
ocircme
I-T
HO
L-1
Saks
unar
vatn
Houmlg
stor
psm
osse
nU
lmen
er M
aar
amp L
3574
radiocarbon dated European tephra horizons
Cho
pine
Kili
an V
asse
tM
erca
to
God
ivel
le 4
Pom
ici P
rinc
ipal
i amp V
edde
Polla
ra p
umic
eK
OL
-GS-
2 amp
GS
-2B
AS-
12
3
GS
-2B
AS-
4 U
nita
dei
Tef
raSu
peri
ori amp
laye
r Y
-1
Gre
enis
h
L9
20 0
0018
000
16 0
0014
000
12 0
0010
000
-44
-40
-36
-32
800
600
400
200 0
GISP2 volcanicsulphate conc (ppb)
1000
Nea
polit
an Y
ello
w T
uff
GISP2 18O (permil) dGRIP 18O (permil) d
Figure 8 For description see opposite
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 791
ferent times through a comparison of radiocarbon dates obtained from marine andterrestrial horizons in which the same tephra has been detected (see for exampleAustin et al 1995 Bondevik et al 2001 Haregidason et al 2000) Tephrostratigraphymay provide an independent test of suggestions that some of the climatic changesduring the Last Termination were time-transgressive as illustrated for some appar-ently contrasting climatic trends in Iceland Britain and NW Russia (Lowe 2001) Ofparticular importance as far as establishing `leadsrsquo and `lagsrsquo in climatic changes isconcerned are the tephra records from the Greenland ice cores The discovery of theVedde and Saksunarvatn ashes in the GRIP record (Gronvold et al 1995) alreadyprovides a basis for making direct comparisons between marine terrestrial and ice-core records It is a matter of some urgency that the incidence of tephra depositsin the Greenland ice cores be more fully explored in the hope that this will lead tothe recognition of additional time-parallel links between the ice-core records on theone hand and oceanic and terrestrial records on the other An investigation of thenew NordGRIP record for this purpose is currently in progress (S M Davies 2002unpublished data)
Finally a fuller and more reshy ned tephrostratigraphical scheme for Europe will alsohave other applications It will provide an important database for those investigatingthe timing and frequency of volcanic eruptions in Europe during the past 20 000 yror so as well as of the geochemical evolution of the dinoterent volcanic centres overthat period A fuller record of the distribution of micro-tephras may also provideinformation on atmospheric circulation patterns during the dispersal and depositionperiods as well as on the nature and altitude of the eruption columns which mayin turn provide inferences about magma viscosity
This paper is a contribution to the INTIMATE project of the INQUA Palaeoclimate Com-mission and the work is supported by a Leverhulme Trust Research project (grant allocationnumber F07537C) entitled Testing hypotheses of rapid climate change using tephrochronol-ogyrsquo SMDrsquo s contribution was completed during possession of a NERC PhD studentship(GT 0499ES162) We are extremely grateful to Dr Peter G Hill for his assistance withthe EPMA analyses at the Tephrochronology Analytical Unit University of Edinburgh We alsothank Dr G Mastrolorenzo (Vesuvius Observatory) and Miss G Swindle for assistance duringthe macreld investigations in Naples Thanks are also expressed to two anonymous reviewers forcomments on an earlier draft
Appendix A
Table 2 shows the major oxide concentrations of NYT glass shards from Procidaand Prato Spilla `Crsquo and of the Mercato Tephra from the Naples area (see x 4 forsite context) All oxides are shown as weight and total iron is expressed as FeO
Figure 8 Radiocarbon calibration curve for Termination 1 and the Early Holocene compared with theGRIP macr 18 O event stratigraphy the GRIP ss08c and GISP2 macr 18 O records (wwwngdcnoaagov) andknown tephra horizons from this period The shaded areas represent the cooler climatic episodes andare labelled with the Greenland stratotype terminology (Bjorck et al 1998) Where radiocarbon agesare reported in table 1 as a range the mean is given here Abbreviations for GRIP horizons are asfollows Un unknown (approximate positions are given (S Johnsen 2001 personal communication))SA Saksunarvatn Ash VA Vedde Ash BF Black Feather Sulphate concentrations from the GISP2record are also shown (Zielinski et al 1996) Open circles denote radiocarbon calibration data fromLake Suigetsu (Kitagawa amp van der Plicht 2000) Filled circles denote radiocarbon calibration data fromCariaco Basin assuming a marine reservoir age of 420 14 C yr (Hughen et al 1998)
Phil Trans R Soc Lond A (2002)
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792 S M Davies and others
Tab
le2
Majo
roxi
de
con
cen
trati
on
sof
NY
Tgl
ass
shard
sfr
om
Pro
cida
an
dP
rato
Spil
laC
rsquoan
dof
the
Mer
cato
Tep
hra
from
the
Naple
sare
a(s
eex4
for
site
con
text
)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
roci
da)
1584
204
0177
634
201
106
828
635
197
5969
1W
DS
2598
603
9178
027
101
204
924
244
583
4965
8W
DS
3586
604
5173
631
100
805
924
342
183
0951
9W
DS
4583
903
9177
933
000
906
924
540
486
9958
3W
DS
5605
106
8179
126
901
204
923
243
086
1976
4W
DS
6591
704
5177
332
801
006
425
740
887
8968
0W
DS
7581
804
1178
031
501
107
125
640
086
9956
1W
DS
8589
504
2179
533
701
506
926
740
987
5970
4W
DS
9592
003
9178
135
101
007
026
443
585
7972
7W
DS
10
591
404
2174
631
601
105
723
442
482
6957
0W
DS
11
593
403
6177
131
301
506
726
439
188
5967
6W
DS
12
588
103
8176
128
100
505
525
141
583
4952
1W
DS
13
577
003
8176
533
500
807
228
140
384
8952
0W
DS
14
586
004
7179
735
300
706
827
842
984
6968
5W
DS
15
588
104
2180
629
400
505
924
937
993
0964
5W
DS
16
579
603
9178
536
501
308
228
836
087
1959
9W
DS
17
580
103
9177
631
500
907
327
039
488
9956
6W
DS
mea
n588
104
2177
631
901
006
525
940
686
9962
8
sd
(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(07
8)
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 793
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
rato
Spil
laC
rsquo)
1552
105
4177
247
401
914
38
735
578
9951
1W
DS
2557
305
7179
845
701
512
640
136
581
5960
6W
DS
3595
004
4173
724
302
003
117
652
877
8950
7W
DS
4575
704
2179
433
001
406
627
043
083
6953
7W
DS
5599
904
0178
826
401
304
421
841
688
4966
5W
DS
6591
103
8177
826
601
105
022
443
888
8960
2W
DS
7565
304
5180
939
501
410
532
535
791
8962
1W
DS
8597
606
9180
826
501
604
821
546
684
6970
7W
DS
9571
805
6179
939
801
109
932
240
883
6964
7W
DS
10
588
603
7176
527
601
104
721
042
487
7953
3W
DS
11
559
404
9180
544
501
812
339
435
878
6957
2W
DS
12
594
704
0181
328
301
705
522
144
785
6967
9W
DS
13
611
103
7187
016
900
802
419
938
195
9975
8W
DS
14
599
204
4181
128
601
404
620
844
986
6971
6W
DS
15
601
204
4177
328
302
004
722
446
385
5972
1W
DS
16
595
104
5176
428
801
504
722
744
884
3962
8W
DS
17
603
704
1177
825
101
503
520
348
181
2965
3W
DS
18
558
704
5179
647
401
813
139
836
879
0960
7W
DS
19
589
602
8178
830
901
606
622
436
091
8960
5W
DS
20
553
606
3178
647
401
913
840
136
978
0956
6W
DS
21
579
004
0175
739
000
708
328
338
286
7959
9W
DS
mea
n582
804
6179
033
401
507
427
341
484
8962
1
sd
(1
87)
(01
0)
(02
7)
(09
2)
(00
4)
(03
9)
(08
0)
(04
9)
(05
0)
(07
0)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
794 S M Davies and others
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)
1575
202
7194
219
701
101
016
374
766
9951
8W
DS
2575
802
9194
523
902
201
520
273
564
5959
0W
DS
3574
301
4205
219
101
100
416
481
266
1965
2W
DS
4575
500
7206
018
002
000
415
181
669
3968
6W
DS
5580
000
9208
018
601
300
515
883
367
1975
5W
DS
6571
001
0206
016
101
600
515
078
967
1957
2W
DS
7577
501
1201
117
101
500
620
675
655
4950
5W
DS
8573
700
9212
717
101
900
815
187
564
2973
9W
DS
9580
301
3208
715
801
400
824
81
754
1968
1W
DS
10
574
400
6211
18
402
00
516
480
567
8971
6W
DS
11
577
200
7214
212
501
200
829
879
247
962
6W
DS
12
572
200
9211
217
301
501
15
980
465
9966
3W
DS
13
571
800
7210
417
402
201
16
184
467
2971
2W
DS
14
567
300
9208
916
901
400
917
383
262
5959
3W
DS
15
568
600
8205
918
202
101
414
682
666
6960
8W
DS
16
572
501
1211
318
202
01
215
884
364
5970
9W
DS
17
572
901
2212
916
502
101
215
883
667
2973
4W
DS
18
573
01
4211
716
301
801
416
83
365
5970
4W
DS
19
569
201
1207
418
602
101
414
982
964
961
6W
DS
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
3)
(04
2)
(01
3)
(00
1)
(00
2)
(01
)(0
39)
(01
1)
(02
5)
Phil Trans R Soc Lond A (2002)
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796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
References
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European tephrochronological framework for Termination 1 797
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Bossuet G Richard H Magny M amp Rossy M 1997 A new occurrence of Laacher See Tephrain the central Jura (France) The mire of Le Lautrey C R Acad Sci Paris Sparaer IIa 3254348
Brauer A Endres C Gunter C Litt T Stebich M amp Negendank J F W 1999 Highresolution sediment and vegetation responses to Younger Dryas climate change in varved lakesediments from Meerfelder Maar Germany Quat Sci Rev 18 321329
Brooks S J Mayle F E amp Lowe J J 1997 Chironomid based Lateglacial climatic recon-struction for southeast Scotland J Quat Sci 12 161167
Calanchi N Dinelli E Gasparatto G amp Lucchini F 1996 Etnean tephra layer in Albanolake and Adriatic Sea cores new macrndings of Y-1 layer in the central Mediterranean area ActaVulcan 8 713
Coope G R Lemdahl G Lowe J J amp Walkling A 1998 Temperature gradients in northernEurope during the last glacialHolocene transition (149 ka BP) interpreted from coleopternassemblages J Quat Sci 13 419433
Dansgaard W (and 10 others) 1993 Evidence for general instability of past climate from a250 kyr ice-core record Nature 363 218220
Davies S M Turney C S M amp Lowe J J 2001 Identimacrcation and signimacrcance of a visiblebasalt-rich Vedde Ash layer in a Late-glacial sequence on the Isle of Skye Inner HebridesScotland J Quat Sci 16 99104
Delibrias G Di Paola G M Rosi M amp Santacroce R 1979 La storia eruttiva del complessovulcanico Somma Vesuvio ricostruita dalle successini piroclastiche del Monte Somma RendSoc It Mineral Petrolog 35 411438
Di Vito M A Isaia R Orsi G Southon J de Vita S Drsquo Antonio M Pappalardo L ampPiochi M 1999 Volcanism and deformation since 12 000 years at the Campi Flegrei caldera(Italy) J Volcanol Geophys Res 91 221246
Dugmore A J amp Newton A J 1992 Thin tephra layers in peat revealed by X-radiography JArchaeol Sci 19 163170
Dugmore A J amp Newton A J 1998 Holocene tephra layers in the Faroe Islands Frodskaparrit46 191204
Eastwood A J Pearce N J G Westgate J A Perkins W T Lamb H F amp RobertsN 1999 Geochemistry of Santorini tephra in lake sediments from southwest Turkey GlobalPlanet Change 21 1729
Eirpara sup3 ksson J Knudsen K L Hadeg idason H amp Henriksen P 2000 Lateglacial and Holocenepalaeoceanography of the North Icelandic shelf J Quat Sci 15 2342
Etlicher B Janssen C R Juvignparae E amp Van Leeuwen J F N 1987 Le Haut Forez (MassifCentral France) aprmicroes le Plparaeniglaciaire Wurmien environnement et tparaephra du volcan de LaNugmicroere Bull Ass Fr Etud Quat 4 229239
Frezzotti M amp Narcisi B 1996 Late Quaternary Tephra derived paleosols in central Italyrsquo scarbonate Apennine range stratigraphical and paleoclimatological implications Quat Int3436 147153
Friedrich M Kromer B Spurk M Hofmann J amp Kaiser K F 1999 Paleoenvironment andradiocarbon calibration as derived from LateglacialEarly Holocene tree-ring chronologiesQuat Int 61 2739
Froggatt P C 1992 Standardisation of the chemical analysis of tephra deposits Report of theICCT working group Quat Int 1314 9396
Gronvold K Oskarsson N Johnsen S J Clausen H B Hammer C U Bond G amp Bard E1995 Ash layers from Iceland in the GRIP ice core correlated with oceanic and land sedimentsEarth Planet Sci Lett 135 149155
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
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Hadeg idason H Eirpara sup3 ksson J amp van Kreveld S 2000 The tephrochronology of Iceland and theNorth Atlantic region during the Middle and Late Quaternary a review J Quat Sci 15322
Hoek W Z amp Bohncke S J P 2001 Oxygen isotope wiggle matching as a tool for synchronisingice-core and terrestrial records over Termination 1 Quat Sci Rev 20 12511264
Hughen K A Overpeck J T Peterson L C amp Trumbore S 1996 Rapid climate changes inthe tropical Atlantic region during the last deglaciation Nature 380 5153
Hughen K A Overpeck J T amp Lehman J 1998 A new 14 C calibration data set for the LastDeglaciation Radiocarbon 39 483494
Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
Hunt J B amp Hill P G 1996 An inter-laboratory comparison of the electron probe microanalysisof glass geochemistry Quat Int 3436 229241
Hunt J B amp Hill P G 2001 Tephrological implications of beam sizesample size ereg ects inelectron microprobe analysis of glass shards J Quat Sci 16 105117
Hunt J B Fannin N G T Hill P G amp Peacock J D 1995 The tephrochronology andradiocarbon dating of North Atlantic Late Quaternary sediments an example from the StKilda Basin In The tectonics sedimentation and palaeoceanography of the North Atlanticregion (ed R A Scrutton M S Stoker G B Shimmield amp A W Tudhope) vol 90pp 227248 Geological Society of London Special Publication
Hunt J B Clift P D Lacasse C Vallier T L amp Werner R 1998 Standardisation ofelectron probe microanalysis of glass geochemistry In Proc ODP Scientimacrc Results vol 152pp 8591 College Station TX Ocean Drilling Program
Jakobsson S P 1979 Outline of the petrology of Iceland Jokull 29 5773
Juvignparae E 1987 Deux retombparaees volcaniques tardiglaciaires dans le Cparaezallier (Massif CentralFrance) Bull Ass Fr Etud Quat 13 37
Juvignparae E 1993 Contribution microa la tparaephrostratigraphie du Quaternaire et son application microa lagparaeomorphologie Mparaem Serv Explicat Cartes Gparaeol Min Belg 36 166
Juvignparae E amp Gewelt M 1987 La Narse drsquo Ampoix comme tparaephrostratotype dans la Chasup3 ne desPuys mparaeridionale (France) Bull Ass Fr Etud Quat 29 3749
Juvignparae E Kozarski S amp Nowaczyk B 1995 The occurrence of Laacher See Tephra in Pomera-nia NW Poland Boreas 24 225231
Juvignparae E Bastin B Delibrias G Evin J Gewelt M Gilot E amp Streel M 1996 Acomprehensive pollen and tephra based chronostratigraphic model for the Lateglacial andHolocene period in the French Massif Central Quat Int 3436 113120
Keller J 1980 The island of Vulcano Rend Soc It Mineral Petrolog 36 369414
Keller J Ryan W B F Ninkovich D amp Altherr R 1978 Explosive volcanic activity in theMediterranean over the past 200 000 years as recorded in deep sea sediments Geol Soc AmBull 89 591604
Kitagawa H amp van der Plicht J 2000 Atmospheric radiocarbon calibration beyond 11 900 calBP from Lake Suigetsu laminated sediments Radiocarbon 42 369380
Kvamme T Mangerud J Furnes H amp Ruddiman W F 1989 Geochemistry of Pleistoceneash zones in cores from the North Atlantic Norsk Geol Tids 69 251272
Lacasse C Sigurdsson H Johannesson H Paterne M amp Carey S 1995 Source of Ash zone 1in the North Atlantic Bull Volcanol 57 1832
Langone L Asioli A Corregiari A amp Trincardi F 1996 Age depth modelling through theLate-Quaternary deposits of the central Adriatic Basin In Palaeoenvironmental analysis ofItalian crater lake and Adriatic sediments (ed F Oldmacreld amp P Guilizzoni) vol 55 pp 177196 Memorie dellrsquo Instituto Italiano di Idrobiologia
Larsen G 2000 Holocene volcanism in Iceland and tephrochronology as a tool in volcanologyIn Iceland 2000 modern processes and past environments Keele University UK
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 799
Litt T amp Stebich M 1999 Bio- and chronostratigraphy of the Lateglacial in the Eifel regionGermany Quat Int 61 516
Litt T Brauer A Goslar T Merkt J Balaga K Muller H Ralska-Jasiewiczowa MStebich M amp Negendank J F W 2001 Correlation and synchronisation of Lateglacialcontinental sequences in northern Central Europe based on annually laminated lacustrinesediments Quat Sci Rev 20 12331249
Long D amp Morton A C 1987 An ash fall within the Loch Lomond stadial J Quat Sci 297101
Lotter A F Eicher U Siegenthaler U amp Birks H J B 1992 Lateglacial climatic oscillationsas recorded in Swiss lake sediments J Quat Sci 7 187204
Lowe J J 1992 Lateglacial and Early Holocene lake sediments from the Northern ApenninesItaly|pollen stratigraphy and radiocarbon dating Boreas 21 193208
Lowe J J 2001 Abrupt climatic changes in Europe during the last glacialinterglacial tran-sition the potential for testing hypotheses on the synchroneity of climatic events usingtephrochronology Global Planet Change 603 7384
Lowe J J amp Turney C S M 1997 Vedde Ash layer discovered in a small lake basin on theScottish mainland J Geol Soc Lond 154 605612
Lowe J J amp Walker M J C 2000 Radiocarbon dating the last glacialinterglacial transition(ca 14914 C ka BP) in terrestrial and marine records the need for new quality assuranceprotocols Radiocarbon 42 5368
Lowe J J amp Watson C 1993 Lateglacial and Early Holocene pollen stratigraphy of the northernApennines Italy Quat Sci Rev 12 727738
Lowe J J Birks H H Brooks S J Coope G R Harkness D D Mayle F E SheldrickC Turney C S M amp Walker M J C 1999 The chronology of palaeoenvironmental changesduring the Last GlacialHolocene transition towards an event stratigraphy for the BritishIsles J Geol Soc Lond 156 397410
Lowe J J Hoek W Z amp INTIMATE group 2001 Inter-regional correlation of palaeoclimaticrecords for the Last GlacialInterglacial transition a protocol for improved precision recom-mended by the INTIMATE project group Quat Sci Rev 20 11751187
Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
Mangerud J Lie S E Furnes H Kristiansen I L amp Liquest mo L 1984 A Younger Dryas ashbed in western Norway and its possible correlation with tephra beds from the Norwegian Seaand North Atlantic Quat Res 21 85104
Mangerud J Furnes H amp Jparaohansen J 1986 A 9000 year-old ash bed on the Faroe IslandsQuat Res 26 262265
Martini J 1970 Recherche de retombparaees volcaniques dans le sud-est de la France et la Suisseoccidentale Arch Sci 23 641674
Martini J amp Duret J J 1965 Note preliminaire sur la presence drsquo un niveau de cendres vol-caniques dans des sparaediments post-glaciaires des environs de Genmicroeve Arch Sci 18 587588
Mayewski P A Meeker L D Twickler M S Whitlow S Yang Q Lyons W B amp Pren-tice M 1997 Major features and forcing of high latitudes Northern Hemisphere atmosphericcirculation using a 110 000 year long glaciochemical series J Geophys Res 102 345365
Merkt J Muller H Knabe W Muller P amp Weiser T 1993 The Early Holocene Saksunarvatntephra found in lake sediments in NW Germany Boreas 22 93100
Narcisi B 1993 Segnalazione di un livello piroclastico di provenienza etnea nellrsquo area del Fucino(Italia Centrale) Quaternario 6 8792
Narcisi B 1996 Tephrochronology of a Late Quaternary lacustrine record from the Monticchiomaar (Vulture volcano southern Italy) Quat Sci Rev 15 155165
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
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Newton A J amp Dugmore A J 1993 Tephrochronology of Core C from Lago Grande di Mon-ticchio In Paleolimnology of European Maar Lakes (ed J F W Negendank amp B Zolitschka)Lecture Notes in Earth Science vol 49 333348 Springer
Oldmacreld F Appleby P G amp Thompson R 1980 Palaeoecological studies of lakes in theHighlands of Papua New Guinea J Ecol 68 457477
Orsi G Drsquo Antonio M de Vita S amp Gallo G 1992 The Neapolitan Yellow Tureg a large mag-nitude trachytic phreatoplinian eruption eruptive dynamics magma withdrawal and calderacollapse J Volcanol Geotherm Res 53 275287
Paterne M Guichard F Labeyrie J Gillot P Y amp Duplessy J C 1986 Tyrrhenian Seatephrochronology of the oxygen isotope record for the past 60 000 years Mar Geol 72259285
Paterne M Guichard F amp Labeyrie J 1988 Explosive activity of the south Italian volca-noes during the past 80 000 years as determined by marine tephrochronology J VolcanolGeotherm Res 34 153172
Paterne M Labeyrie J Guichard F Mazaud A amp Maitre F 1990 Fluctuations of the Cam-panian explosive volcanic activity (south Italy) during the past 190 000 years as determinedby marine tephrochronology Earth Planet Sci Lett 98 166174
Pawse A Beske-Diehl S amp Marshall S A 1998 Use of magnetic hysteresis properties andelectron spin resonance spectroscopy for the identimacrcation of volcanic ash a preliminary studyGeophys J Int 132 712720
Pearce N J G Westgate J A amp Perkins W T 1996 Developments in the analysis of singleglass shards in volcanic deposits by laser ablation ICP-MS quantitative and single internalstandard multi-element methods Quat Int 3436 213227
Pearce N J G Westgate J A Perkins W T Eastwood W J amp Shane P 1999 Theapplication of laser ablation ICP-MS to the analysis of volcanic glass shards from tephradeposits bulk glass and single shard analysis Global Planet Change 21 151171
Pilcher J R amp Hall V A 1992 Towards a tephrochronology for the Holocene of the north ofIreland Holocene 2 255259
Ponel P amp Lowe J J 1992 Coleopteran pollen and radiocarbon evidence from the Prato Spillarsquo Drsquo succession N Italy C R Acad Sci Paris Sparaer II 315 14251431
Rose N L Golding P N E amp Battarbee R W 1996 Selective concentration and enumerationof tephra shards from lake sediment cores Holocene 6 243246
Ruddiman W F amp Glover L K 1972 Vertical mixing of ice rafted volcanic ash in NorthAtlantic sediments Geol Soc Am Bull 83 28172836
Ruddiman W amp McIntyre A 1981 The North Atlantic Ocean during the last deglaciationPalaeogeogr Palaeoclimatol Palaeoecol 35 145214
Santacroce R 1987 Somma Vesuvius Quad Ric Sci 114 252
Sarna-Wojcicki A 2000 Tephrochronology In Quaternary geochronology methods and applica-tions (ed J S Noller J M Sowers amp W R Lettis) AGU Reference shelf vol 4 pp 357377Washington DC American Geophysical Union
Sejrup H P Sjiquest holm J Furnes H Beyer I Eide L Jansen E amp Mangerud J 1989Quaternary tephrochronology on the Iceland Plateau north of Iceland J Quat Sci 4 109114
Sikes E L Samson C R Guilderson T P amp Howard W R 2000 Old radiocarbon agesin the southwest Pacimacrc Ocean during the last glacial period and deglaciation Nature 405555558
Stein R Nam S-I Grobe H amp Hubbersten H 1996 Late Quaternary glacial history andshort term ice rafted debris deg uctuations along the East Greenland continental marine In LateQuaternary palaeoceanography of the North Atlantic margins (ed J T Andrews W E NAustin H Bergsten amp A E Jennings) pp 135151 Geological Society London SpecialPublication
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 801
Stuiver M amp Grootes P M 2000 GISP2 oxygen isotope ratios Quat Res 53 277284
Stuiver M Reimer P J Bard E Beck J W Burr G S Hughen K A Kromer BMcCormac G Van der Plicht J amp Spurk M 1998 INTCAL 98 radiocarbon age calibration24 0000 cal BP Radiocarbon 40 10411083
Sweatman T R amp Long J V P 1969 Quantitative electron microprobe analysis of rock formingminerals J Petrol 7 332379
Turney C S M 1998 Extraction of rhyolitic ash from minerogenic lake sediments J Paleolim-nol 19 199206
Turney C S M amp Lowe J J 2001 Tephrochronology In Tracking environmental changes inlake sediments physical and chemical techniques (ed W M Last amp J P Smol) DordrechtKluwer Academic
Turney C S M Harkness D D amp Lowe J J 1997 The use of microtephra horizons tocorrelate Lateglacial lake sediments successions in Scotland J Quat Sci 12 525531
Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
van den Bogaard P amp Schmincke H 1985 A widespread isochronous Late Quaternary tephralayer in central and northern Europe Geol Soc Am Bull 96 15541571
van den Bogaard B Dordeg er W Sandgren P amp Schmincke H-U 1994 Correlating theHolocene records Icelandic tephra found in Schleswig-Holstein (northern Germany) Natur-wissenschaften 81 554556
Vernet G amp Raynal J-P 2001 Tephrostratigraphy of the Limagne revisited Implications forLateglacial and Holocene Prehistory In Tephras chronology archaeology (ed E Juvignparae ampJ-P Raynal) pp 111116 Dossiers de lrsquo ArchparaeoLogis no 1 France
Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
Vezzoli L 1991 Tephra layers in Bannock Basin (eastern Mediterranean) Mar Geol 1002134
von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
Walker M J C Bjorck S Lowe J J Cwynar L C Johnsen S Knudsen K-L WohlfarthB amp INTIMATE Group 1999 Isotopic events in the GRIP ice core a stratotype for the LatePleistocene Quat Sci Rev 18 11431150
Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
Phil Trans R Soc Lond A (2002)
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802 S M Davies and others
Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
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776 S M Davies and others
matter (Pilcher amp Hall 1992) digestion of biogenic and opaline silica (Rose et al 1996) the use of magnetic properties of ash layers (see for example Oldshy eld et al 1980 van den Bogaard et al 1994 Pawse et al 1998) X-ray analysis (Dugmore ampNewton 1992) and a density separation (regotation) technique (Turney 1998) Den-sity separation has proved exceedingly useful for the detection of small glass shardspresent in low concentrations in mineral-rich Late Glacial sediments This involvesthe separation and concentration of particles of predetermined specishy c gravity withthe use of a heavy liquid and subsequent identishy cation of glass shards with the useof a polarizing light microscope (for further details see Turney (1998)) This methodhas been particularly successful in the detection of tephras of rhyolitic compositionthat have a specishy c density of 2325 g cmiexcl3 (Lowe amp Turney 1997 Turney et al 1997 2001 Turney 1998 Wastegard et al 1998 2000a b) It is this technique thathas resulted in the wider recognition of micro-tephras in Europe as discussed below
3 Geochemical ` ngerprintingrsquo of tephra layers
The 34 tephras listed in table 1 have originated from four major volcanic complexesIceland the Massif Central in central France the Eifel district near Bonn and threevolcanic centres in Italy (the Campanian group Etna and the Aeolian Islands (seeshy gure 2)) An important matter to resolve is the extent to which the various magmasand ashes generated by these volcanic complexes can be geochemically shy ngerprintedThis is especially important in the case of tephras which have originated from thesame volcanic centre in which there may have been limited geochemical evolution ofmagmas over time In this section we summarize the approach generally adopted todetermine the geochemical character of visible and micro-tephras as background tothe geochemical data summarized in table 1 In the subsequent section of the paperwe review the present state of knowledge concerning all 34 tephras listed in table 1
Glass shards formed during the rapid cooling of magma are thought to have acomposition that is representative of the bulk geochemistry of the magma (Barker1983) hence widely dispersed glass particles are regarded as the most appropriateconstituents of pyroclastic material for geochemical analysis If a tephra deposit canbe shown to have a distinct geochemical signature then it can be used to correlatethe stratigraphic units in which it occurs (tephrostratigraphy) as well as to datethese units (tephrochronology) if the ages of the tephras are known (Westgate ampGorton 1981) A key element of building a tephrostratigraphical framework there-fore is to establish as rigorously as possible the geochemical composition of theindividual tephras used in its construction Robust and directly comparable geo-chemical datasets are dimacr cult to assemble for glass however because it is highlyunstable material particularly prone to sodium mobilization
The technique most widely employed to establish the geochemical signature of atephra is electron probe micro-analysis (EPMA) This enables grain-discrete determi-nations of the major elements within an individual glass shard which is of particularbeneshy t in the analysis of micro-tephra layers which generally contain glass particlesin low concentration The glass surface is bombarded with an electron beam and theX-ray energy produced is unique to each element while the intensity of the signalemitted is proportional to the amount of that element in the glass shard (Hunt amp Hill1993) Measurement can be by either energy dispersive spectrometry (EDS) or wave-length dispersive spectrometry (WDS) EDS has a lower precision mainly because
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 777
N
0 500 km
Confirmed records of Vedde Ash (visible occurrences)
New records of Vedde Ash from flotation method
Extended area of Vedde Ash detection (micro-tephra)
Known area of Laacher See Tephra (visible occurrences)
Confirmed records of Neapolitan Yellow Tuff (visible occurrences)
New record of Neapolitan Yellow Tuff from flotation method
Known area of Neapolitan Yellow Tuff
Volcanic centres of particular relevance to this study
Other major volcanic centres in Europe
Figure 2 Location of the principal volcanic centres that were active during Termination 1 andthe Early Holocene The known distribution of the Vedde Ash (VA) Laacher See (LST) andNeapolitan Yellow Tureg (NYT) are shown
the behaviour of each element cannot be monitored independently during measure-ment and so this approach fails to detect for example any signishy cant mobilizationof sodium during the bombardment process (Hunt amp Hill 1993) Although WDSrequires a higher beam current and a longer counting time than EDS the formeronoters the distinct advantage of sequential acquisition of elemental data so that thedegree of sodium loss can be tracked The morphology of individual glass shards canalso distort EDS data a problem that is reduced when using WDS because for thisprocedure glass shards are mounted in an epoxy resin and polished to provide aregat surface for analysis Hence data should always be obtained using WDS whereverpossible
Even when WDS is used as a common tool for determining the geochemical spectraof samples aberrant results can arise that inreguence data comparisons For examplesome glass shards may contain tiny crystalline inclusions of feldspar and these shouldbe avoided when selecting surface points for analysis (Hunt amp Hill 2001) Hunt amp Hill
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778 S M Davies and others
6
4
2
40 50 60 70 80
K2O
(
)
SiO2 ()
Laacher See
Iceland
Veidivoumltn-Dyngjufjoumlll
Katla (basalt)
Grimsvoumltn-Kverkfjoumlll
Hekla
Katla (rhyolitic)
0
Icelandic volcanic centres8
10
Massif Central
Etna
Campanian
Figure 3 Bi-plot of SiO2 and K2 O concentrations in tephras derived from the main Europeanash provinces (modimacred after Mangerud et al 1984) The Campanian Massif Central and Etnaconcentrations are based on the data presented in table 1
(2001) have concluded that small variations in the laboratory procedures employedto determine glass chemistry can lead to misidentishy cation of sources for glass shardsand give an example of shards with a Jan Mayen provenance wrongly attributedto an Icelandic source Clearly there is a need for standardization of laboratoryprocedures and while a number of recommendations have recently been advocated(Froggatt 1992 Hunt amp Hill 1993 Hunt et al 1998) there is still some variation inlaboratory and operator practice (Hunt amp Hill 1996) Standardization is also requiredin the form in which results are presented to ensure comparability Normalizationof the data to 100 a practice employed by some researchers can obscure poorresults and hence lead to incorrect comparisons (Hunt amp Hill 1993) However othersargue that it may actually facilitate comparisons between samples by removing thedistorting enotects of the water component contained in glass shards (see for exampleFroggatt 1992) The majority of the published Italian and some of the Eifel datahave been normalized while those from other parts of Europe have not and hencedata comparisons are not always straightforward
Table 1 provides mean values and standard deviations for major oxide concentra-tions obtained from those tephras for which data are presently available The tableincludes previously unpublished WDS results for the Neapolitan Yellow Tunot (NYTdiscussed in x 4 below) and for the Mercato Tephra While individual tephra layersmay be geochemically distinct the geochemical envelopes representing the collectivedata obtained from all of the tephras assigned to each major volcanic province showsignishy cant overlaps as is illustrated in the bi-plots and ternary plots (shy gures 3 and 4)of selected oxide concentration data It is clear therefore that measurement of majoroxide concentrations does not satisfactorily discriminate between some tephras orig-inating from dinoterent volcanic centres (as noted by van den Bogaard amp Schmincke(1985) and Frezzotti amp Narcisi (1996) with respect to Eifel and Italian tephras)nor of tephras of dinoterent age originating from the same volcanic centre (Bond et
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 779
40 50 60 70 80
K2O
(
)
SiO2 ()
shyshyshyshy
shy
shyshy
shyshyshy
shy
shy
shy
shy
reg
reg regreg
regregregregreg regregregregreg
FF
F
ll
l
l
4 8 12 16
reg
regreg
regreg
regregreg
regreg
regregreg
shy
F
l shyshyshyshyshy shyshyshyshyshyshy
F
F
l
ll
FeO ()
TiO
2 (
)
reg
l
Iceland
Eifel
F
shy ItalyMassif Central
100
80
60
40
20
100
80
60
40
20
100 80 60 40 20
CaO
FeO
K2O
regregreg
reg
reg
reg
reg
reg
reg
regregreg
shyF
F
F
regreg
l
lllshy
shyshyshy
shyshyshy
l
0
2
4
6
8
10
0
1
2
3
4
5
regreg
regreg
regreg
regreg
regreg
reg
reg
regreg
l
l
ll
shy
shyshy
shyshy
shy
shyshy
FF
F
100
80
60
40
20
100
80
60
40
20
100 80 60 40 20
K2ONa2O
CaO
(c) (d)
(a)
(b)
Figure 4 Plots of selected geochemical data obtained from tephras of Termination 1 age (seetable 1) (a) Bi-plot of mean SiO2 and K2 O values (b) Bi-plot of mean FeO and TiO2 values(c) Ternary plot indicating variations in the proportions of FeO CaO and K2 O (d) Ternaryplot indicating variations in the proportion of CaO Na2 O and K2 O
al 2001) Individual tephra layers are presently assigned to a particular volcanicevent on the basis of a combination of criteria usually including examination of thephysical properties (eg refractive index and surface detail of the glass shards) thestratigraphic position of the layer and independent assessment of the age of the layeras well as any geochemical data that may be available The construction of a tephro-stratigraphical scheme would clearly beneshy t from the application of a more diagnostic
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780 S M Davies and others
geochemical tool One approach that has promise is the analysis of trace and rareearth elements using an ultraviolet laser ablation inductively coupled plasma massspectrometer (UV-LA-ICP-MS) (Pearce et al 1996 1999 Eastwood et al 1999)This approach has been applied successfully to analysis of tephras of Mid-Holoceneage but not yet to tephras that fall within the period of interest here
4 Tephra layers in Europe and the North Atlantic regiondated to between 185 and 80 14C ka
(a) Icelandic province
The Icelandic volcanic systems are divided into three main groups based on theirgeochemical characteristics tholeiitic basalts transitional alkali basalts and alkaliolivine basalts (Jakobsson 1979) Collectively magmas from the Icelandic provincespan a wide geochemical spectrum although individual volcanic centres have tightgeochemical distributions (shy gure 3) for four of the main centres Grimsvotn-Kverfjolland Veidvotn-Dyngjufoll which form part of the northern (tholeiitic) volcanic zoneand Hekla and Katla which fall within the eastern (alkali olivine basalt and transi-tional alkali basalt) volcanic zone (Haregidason et al 2000) These appear to be thekey centres for the tephras listed in table 1 that have been assigned an Icelandicorigin
One of the best-known and most widely dispersed tephra horizons in northernEurope that has an Icelandic origin is the Vedde Ash (VA) which was depositedca 103 14C ka BP (Birks et al 1996 Wastegard et al 1998) within the GS-1Younger Dryas chronozone This ash is believed to originate from the Katla complexwithin the transitional alkali basalt province (Mangerud et al 1984 Lacasse et al 1995) in the south of the island The ash has a bimodal geochemical composition (rhy-olitic and basaltic) which is thought to reregect derivation from two separate magmachambers Studies of recent volcanic events in Iceland have shown that the mostexplosive eruptions generating the largest amounts of tephra occur in this tran-sitional alkali basalt province (Haregidason et al 2000) It is also believed that thewidespread distribution of this ash was caused by the development of co-ignimbriteash plumes during an ignimbrite-forming eruption (Lacasse et al 1995)
Layers of VA that are visible to the naked eye have been found in lake sediments inwestern Norway (Mangerud et al 1984) and the Inner Hebrides Scotland (Davies etal 2001) and in marine cores throughout the NE Atlantic (see for example Kvammeet al 1989 Lacasse et al 1995) in the northern North Sea (Long amp Morton 1987)on the Iceland plateau (Ruddiman amp McIntyre 1981 Sejrup et al 1989) and on theeast Greenland continental margin (Stein et al 1996) The distribution of the VAin North Atlantic marine sequences is characterized by an arcuate lobe extendingsouthwest from the Denmark Strait and curving eastwards to mid-latitudes in theNorth Atlantic (Lacasse et al 1995) This strongly suggests deposition from raftedice which was displaced to the southwest and south in a circulating counterclockwisegyre (Ruddiman amp Glover 1972) This may well reregect Katlarsquos close proximity tothe southern coast of Iceland with the Vedde tephra being deposited on ice thatcalved directly into the North Atlantic (Haregidason et al 2000) However depositionvia the atmosphere almost certainly took place as well as is indicated by the recentdiscoveries of rhyolitic VA in micro-tephra form in several sites in Scotland (Turneyet al 1997) southern Sweden (Wastegard et al 1998 2000a) and western Russia
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(Wastegard et al 2000b) A more recent discovery of a relatively high concentrationof rhyolitic VA glass shards in the northern Netherlands indicates that the ash maywell have been dispersed much further south than previously thought (S M Davies2002 unpublished work) Finally glass shards assigned to the VA have also beendiscovered in the GRIP ice core and dated to 11 980 sect 80 GRIP yr BP (Gronvold etal 1995) This discovery is extremely important for it indicates that the VA maywell provide a reliable time-parallel marker horizon between ice-core marine andterrestrial records
Two other important Icelandic ash layers the Borrobol and Saksunarvatn Tephraswere deposited near the beginning and end of the Last TerminationEarly Holoceneinterval respectively The Borrobol Tephra was discovered for the shy rst time in lakesediments in several sites in Scotland and as yet is known only in micro-tephra formIt has been dated in Scottish sites to ca 123 14C ka BP (Turney et al 1997) Whatis thought to be a contemporaneous tephra has been detected in marine sedimentson the North Icelandic shelf (Eirplusmn ksson et al 2000) This certainly has a very similargeochemical composition to those reported from Scotland but the horizon in whichit was discovered on the North Iceland plateau has been dated to 134 14C ka Theage discrepancy between the Scottish and Icelandic Borrobol Tephra layers may wellreregect the inreguence of a marine reservoir error although the possibility that severaltephras with similar geochemical composition were erupted over a period exceeding1000 yr cannot be ruled out (Larsen 2000)
The Saksunarvatn Ash appears to have been one of the largest Holocene eruptionsin Iceland It has a tholeiitic basaltic composition which is considered to indicate anorigin in the Grimsvotn or Kverfjoll complex (shy gure 3) (Mangerud et al 1986) Layersof this ash have been identishy ed in sites on the Faroe Islands (Mangerud et al 1986Dugmore amp Newton 1998 Wastegard et al 2001) the Shetland Isles (Bennet et al 1992) northern Germany (Merkt et al 1993) western Norway (micro-tephra) (Birkset al 1996) and in the GRIP (Gronvold et al 1995) and NordGRIP ice cores (S MDavies 2002 unpublished work) It has been dated to between 9060 and 8930 14C kaBP (Birks et al 1996) in Norway and to ca 10 240 sect 30 GRIP yr BP in the GRIPice core (Gronvold et al 1995) The Saksunarvatn Ash may thus provide a secondimportant widespread time-parallel marker between ice-core marine and terrestrialrecords
Other Icelandic tephras of rhyolitic amacr nity are less well known in terms of theirdistribution and geochemical variation The Hogstorpsmossen Tephra reported fromSweden (Bjorck amp Wastegard 1999) and the L3754 tephra discovered in the FaroeIslands (Dugmore amp Newton 1998) are known from single sites only and so theirpotential for tephrostratigraphy is uncertain at present Furthermore the geochem-ical spectrum of the Hogstorpsmossen Tephra is based on a small dataset with lowanalytical totals
A number of tephras of basaltic composition have originated from Iceland buttheir distributions are largely conshy ned to Iceland or to marine cores collected fromclose to the Iceland coast or in the North Atlantic These include the tephras listedas 1-THOL-1 1-THOL-2 KOL-GS-2 GS-2BAS-1 GS-2BAS-2 GS-2BAS-3 andGS-2BAS-4 in table 1 (Kvamme et al 1989 Bjorck et al 1992 Eirplusmn ksson et al 2000 Haregidason et al 2000) The shy rst two in this list are tholeiitic basaltic tephrasassociated with the VA in a complex series of tephras collectively termed NorthAtlantic Ash Zone 1 (NAAZ1) which has been detected in numerous marine cores
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782 S M Davies and others
from the North Atlantic Initially thought to represent a single eruption analysisof high-resolution sediment sequences from Lake Torfadalsvatn in northern Iceland(Bjorck et al 1992) the Hebridean Shelf near NW Scotland (Austin amp Kroon 1996)the St Kilda Basin (Hunt et al 1995) and the open North Atlantic (Bond et al 2001)has demonstrated that NAAZ1 comprises a series of distinct ashes that probablyreregect separate eruption events 1-THOL-1 is thought to originate from Veidivotn(shy gure 3) while Grimsvotn may have been the source of 1-THOL-2 (Kvamme et al 1989)
KOL-GS-2 is also of tholeiitic basaltic composition but is thought to originatefrom the Kolbeinsey Ridge system (Eirplusmn ksson et al 2000) To date this tephra hasbeen detected in one marine core only within the same record on the North Ice-landic shelf as that from which the correlative of the Borrobol Tephra was alsoreported (Eirplusmn ksson et al 2000) GS-2BAS-1 to GS-2BAS-4 are of uncertain ori-gin but are thought to have been deposited at roughly the same time as KOL-GS-2(ca 134 14C ka BP (Haregidason et al 2000))
The limited distribution of these basaltic tephras a feature that is not unique toIcelandic basaltic material may reregect two factors the relative magnitude of the vol-canic eruptions from which they were derived and the limited aerial transportationof basaltic glass which is denser than rhyolitic material However a rather surpris-ing recent discovery is that of visible basaltic VA in a site on the Isle of Skye inthe Inner Hebrides Scotland (shy gure 5) (Davies et al 2001) All other occurrencesof VA in Scotland are exclusively of rhyolitic material and in micro-tephra formonly (Turney et al 1997 Turney 1998) Clearly basaltic tephra must have beentransported subaerially as far south as Skye and the reason why it has not beendetected at other sites in Scotland is puzzling We suspect that this partly reregectsthe laboratory methods employed to separate glass shards present in low concentra-tion within a micro-tephra layer from the host sediment The technique used is adensity-separation (regotation) procedure (Turney 1998) and as basaltic shards havea specishy c density similar to quartz one of the most abundant minerals in lake sedi-ments of Late Glacial age basaltic material is dimacr cult to detect using this methodThis hypothesis is currently under investigation and alternative detection methodsare being explored including magnetic separation (Mackie et al 2002)
Several other events listed in table 1 that are of probable Icelandic origin includetephras recorded in the GRIP ice core including visible (eg the `Black Featherrsquo)tephras as well as uncertain tephras inferred from distinct Ca peaks (S Johnsen2001 personal communication) No glass shards have yet been detected in the latterbut a volcanic origin is assumed because high Ca peaks are associated with knowntephras in other Greenland ice cores (S Johnsen 2001 personal communication)These are referred to as `unknownrsquo in table 1 No geochemical analyses are availablefrom these horizons so their origin must remain speculative but a possible source isIceland in view of its proximity to the Greenland ice sheet and assumed atmosphericcirculation patterns
(b) Eifel province
There are two prominent tephra events dated to the Termination 1Early Holocenetime-span that originated from the Eifel province the Laacher See Tephra (LST)and the Ulmener Maar Tephra (UMT) Visible occurrences of the LST indicate that
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European tephrochronological framework for Termination 1 783
Vedde Ash
615 625 635 645 655depth (cm)
organic lake mudsHolocene
silty clayGS-1Younger Dryas
organic lake mudsGI-1Alleroslashd
100 microm
(a)
(b)
Figure 5 (a) Photograph of the visible VA layer discovered at Loch Ashik Isle of Skye InnerHebrides Scotland (b) Light microscope photograph showing the rich content of basaltic shards(examples are indicated by the arrows) within this layer (8024 m m size fraction)
this ash was dispersed over much of central Europe (van den Bogaard amp Schmincke1985 Friedrich et al 1999 Litt amp Stebich 1999) The LST is dated by radiocarbonto ca 110 14C ka BP (van den Bogaard amp Schmincke 1985) and to 11 063sect12 14C BP(Friedrich et al 1999) by varve chronology to 1288 varve ka BP (Brauer et al 1999Litt et al 2001) and by ArAr dating to 129 ka cal BP (van den Bogaard 1995) Ithas a phonolitic composition and is thought to have originated from a plinian andphreatomagmatic eruption with the distal ash being carried in three distinct plumesone to the northeast towards Poland one to the west and the third to the southcovering the Jura Mountains and north Italy (van den Bogaard amp Schmincke 1985Juvigne et al 1995 Bossuet et al 1997) This pattern is thought to reregect altitu-dinal variations in the predominant wind direction Sedimentary sequences near thevolcanic source indicate that the LST consists of three main layers which represent
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784 S M Davies and others
dinoterent eruption phases These are grouped together as the Laacher See TephraFormation but the three individual units can be traced within and between a seriesof depositional fans The geochemical data obtained from these three LST layersshow signishy cant variations as reregected in the ternary plots (shy gure 4)
The Early Holocene Ulmener Maar Tephra (UMT) is of rhyolitic composition andappears to be restricted to sites in Germany though this conclusion is also based onrecords of visible tephras only It is dated to ca 956 14C ka BP and to 110 varve ka(Zolitschka et al 1995 Litt et al 2001)
(c) Massif Central province
The Massif Central tephras are mainly of basaltic trachyandesitic compositionwhich is distinct from the other ash provinces (shy gures 3 and 4) and their known dis-tributions are mostly conshy ned to the Massif Central region The ages of the MassifCentral tephras are based on radiocarbon dates obtained from mire and lake sedi-ments which `bracketrsquo the tephras The La Nugsup3ere Tephra with an age of 114 14C kaBP is the oldest Massif Central tephra identishy ed so far within the time-span of inter-est (Etlicher et al 1987 Juvigne et al 1996) The two Godivelle Tephras (5 and 4)are close in age but extensive radiocarbon dating suggests distinct ages of 107and 103 14C ka BP respectively (Juvigne et al 1996) The age of the Puy de DomeTephra is less certain as the estimate is based on only one radiocarbon date froma site in the southern Chaplusmn ne des Puys (table 1) This tephra is thought to havea trachyte composition (Juvigne 1993) although no major element concentrationshave yet been published
The ChopineKilianVasset tephras are thought to be derived from three separateEarly Holocene eruptions although the stratigraphic succession is not known atpresent These trachytic tephras have been radiocarbon dated to ca 854sect150 14C kaBP but are thought to have erupted separately within ca 260 yr (Juvigne et al 1996) This series of tephras is considerably more widespread than the others fromthe region having been identishy ed as far east as the Jura Mountains (Martini amp Duret1965 Martini 1970) Some other ash falls that originated from the Chaplusmn ne des Puysappear to be of local importance only (Vernet et al 1998 Vernet amp Raynal 2001)Geochemical data are currently available for only three of the Massif Central tephrasand so far as is known no attempt has yet been made to identify these tephras inmicro-tephra form
(d ) Italian provinces
The Italian tephras from this period can be assigned to three main volcanic com-plexes the Campanian volcanic shy elds around Naples Etna on Sicily and the AeolianIslands The Campanian complex which includes the Phlegrean Fields Vesuviusand Ischia is mainly trachytic in composition with a geochemical spectrum that isquite distinct from those of the Etna complex and of the Aeolian Islands (shy gure 3)Tephras originating from one or more of these three complexes have been detectedin marine cores from the Tyrrhenian and Adriatic seas as well as other parts of theMediterranean Sea (Keller et al 1978 Paterne et al 1986 1988 1990 Langone etal 1996) and in lake sequences in southern Italy such as Lago Grande di Monticchio(Newton amp Dugmore 1993 Narcisi 1996 Allen et al 1999) and central Italy such asLago Albano near Rome (Calanchi et al 1996) Some work has also been conducted
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European tephrochronological framework for Termination 1 785
in or close to the volcanic source areas in an attempt to establish the full sequenceof volcanic eruptions during the Late Quaternary (see for example Di Vito et al 1999) There are nine Italian tephras reported from marine and lake sequences thatdate from the period between 185 and 80 14C ka BP In all instances the recordsare of visible layers of tephra The ages of some of these are poorly established atpresent with conregicting data obtained from dinoterent sites The ages suggested intable 1 are those favoured in the most recent publications but these may requirere-assessment in the light of future research
The two oldest known tephras in the time-period of interest are the L9 and Green-ish Tephras both recorded as separate features within the annually laminated Lagodi Monticchio maar sequence The lowest of the two L9 is considered to be the cor-relative of the `basalrsquo plinian eruption of Vesuvius (Narcisi 1996) Age estimates ofa palaeosol that underlies the Vesuvius tephra sequence are ca 1617 14C ka BP forthis event (Delibrias et al 1979) L9 has a trachytic composition very similar to theGreenish Tephra (table 1) However L9 which is also a product of Vesuvius is foundstratigraphically below the Greenish Tephra in the Lago di Monticchio core TheGreenish Tephra is dated in the Monticchio sequence to 17 560 varve yr BP (Allenet al 1999) and has a calibrated radiocarbon age estimate of 17 830 sect 300 cal BP(Andronico et al 1995) Both tephras have a dominantly eastwards dispersal basedon the occurrences of visible layers (Santacroce 1987 Narcisi 1996) Both tephrasalso have a trachytic composition and as can be seen from table 1 the reportedgeochemical spectra are very close indeed with the standard deviations overlappingfor almost every major element This could present problems for tephrostratigra-phy where only one of the tephras is evident in a sediment sequence in particularbecause they are so close in age This is a good example of where an analysis oftrace and rare earth elements might be required to make a clear distinction betweentephras with very similar major oxide concentrations
The Y-1 Tephra also termed the Biancavilla Montalto Ignimbrite (Vezzoli 1991)is a product of Etna and has been identishy ed as a visible benmoritic tephra horizonthroughout the central Mediterranean (Paterne et al 1988) including central Italyand the Adriatic Sea (Vezzoli 1991 Narcisi 1993 Calanchi et al 1996) It has anestimated age of ca 140 14C ka BP The Unita dei Tefra Superiori tephra which hasbeen detected as far east as Lago di Monticchio in south-central Italy (Narcisi 1996)is also dated to ca 140 14C ka BP (Alessio et al 1976) but it is thought that thesource of this tephra lies in the Phlegrean Fields No geochemical data are availablefrom the presumed source region|the data reported in table 1 were obtained fromthe Lago di Monticchio record (Narcisi 1996)
The NYT which is equivalent to the C-2 tephra reported from various marinesequences has also been traced throughout central Italy and the Adriatic Sea (Pat-erne et al 1988 Calanchi et al 1996 Di Vito et al 1999) (shy gure 2) In the centralApennines region it formed the parent material for a soil that started to developat the beginning of the Holocene period (Frezzotti amp Narcisi 1996) Also originatingfrom the Campi Flegrei caldera it is dated to ca 120 14C ka BP (Di Vito et al 1999) Published geochemical data based on EDS indicate three dinoterent geochemicalpopulations varying from latite to phonotrachyte in composition (Orsi et al 1992Paterne et al 1988) (table 1) We report in x 4 of this paper on new data obtainedfrom the NYT by WDS and it is the mean of these new data that is included intable 1 Comparisons with the previously published EDS data are provided (table 1)
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786 S M Davies and others
The new data indicate clearly that the NYT originated from the Campanian volcaniccentre
In the interval between the dispersal of the NYT (ca 120 14C ka BP) and 95 14Cka BP there appear to have been as many as 34 eruptions in the Campi Flegrei caldera(Di Vito et al 1999) Of these only one appears to have been detected widely in theregion the Pomici Principali (also termed the Agnano Formation or C-1 tephra inmarine records (Paterne et al 1988) This was the product of the highest magnitudeeruption from this epoch and is dated to between 976 sect 300 and 1032 sect 50 14C kaBP (Delibrias et al 1979 Di Vito et al 1999) or to 122 varve ka BP based on theMonticchio varve chronology (Allen et al 1999) It is trachytic in composition andappears to have had a mainly eastwards dispersal
The Mercato Tephra dated to ca 80 14C ka BP and originally analysed usingEDS has a phonolitic composition and is believed to have been generated by Vesu-vius (Paterne et al 1988) New WDS data obtained from reference samples col-lected from an exposure to the west of Naples support these conclusions (table 1 andAppendix A) The silica content of the WDS analyses are ca 3 lower than thoseobtained using EDS (table 1) which may reregect the fact that the EDS data werenormalized
The only tephra listed in table 1 that is thought to have originated from the AeolianIslands is the Pollara pumice also referred to as the E2 tephra in marine sequences(Paterne et al 1986 1988) The limited geochemical data available so far suggest itto be the only Italian tephra listed in table 1 that is rhyolitic in composition Littlemore is known about this ash which has not been recorded extensively except thatits age is estimated to be ca 130 14C ka BP (Keller 1980)
5 Extending the known distributions of European tephras
Figure 2 summarizes schematically the known distributions of three of the tephrasreferred to in the preceding section the VA the LST and the NYT Following theintroduction of a laboratory method that enables the detection of micro-tephra parti-cles in mineral-rich sediment the VA has been traced to sites that are located muchfarther south (into The Netherlands) and east (as far as St Petersburg) than thedistribution limits based on occurrences of visible layers of the ash As a result con-tinental sequences over a much larger area in northern Europe can now be correlateddirectly with marine and ice-core records using the VA as a time-parallel marker
This suggests therefore that other prominent ash layers such as the LST andNYT should also be detectable over larger tracts of Europe than is presently thecase if suitable sites are examined for the presence of micro-tephra horizons To testthis assertion we examined lake sediment deposits of Last Termination age froma site in the northern Apennines in order to establish whether the NYT could bedetected in micro-tephra form The site selected Prato Spilla `Crsquo lies well to thenorth of the localities in central and southern Italy and in the Adriatic Sea fromwhich visible records of the NYT have been reported Prato Spilla `Crsquo lies at an alti-tude of ca 1350 m in the Appennino Parmense ca 60 km south of Parma and 15 kmeast of Pontremoli The site contains a continuous sediment sequence spanning theLast Termination and most of the Holocene Detailed pollen and coleopteran strati-graphical records which have been radiocarbon dated have been published for thissite (Lowe 1992 Ponel amp Lowe 1992 Lowe amp Watson 1993)
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Figure 6 Light microscope photograph of an NYT glass shard from Prato Spilla Crsquosequence assigned on geochemical grounds to the NYT
The methods adopted for sub-sampling of the Prato Spilla `Crsquo sequence for thequantishy cation of glass shard concentrations and for subsequent electron microprobeanalysis of selected glass shards followed those described elsewhere (Turney 1998)In summary contiguous samples of 1 cm stratigraphic interval were extracted fromthe sequence to establish presenceabsence of glass shards Each of the 1 cm3 blocksin which tephra particles was detected was then examined with more care andshard concentrations were quantishy ed for each sub-sample Micro-tephra particleswere detected in shy ve samples (shy gure 6) but were predominantly clustered around500 cm in the part of the sequence assigned on pollen-stratigraphic grounds to theLate Glacial Interstadial or the `Allerfrac12drsquo|indeed the part of the succession in whichthe NYT would be expected to occur Peak concentrations of micro-tephra particlesreach 225 shards cmiexcl3 and are conshy ned to a single 1 cm thick sample in the sequencewhich probably represents the time of maximum deposition of the ash
Electron microprobe measurements based on WDS were obtained from the surfacesof 21 separate glass shards extracted from the sample with peak shard concentrations(Appendix A) Since only EDS measurements were available for the NYT prior to thepresent study we also obtained WDS measurements from 17 shards extracted fromthe visible layer of NYT that is exposed on Procida Island which lies in the type-locality for the NYT close to the city of Naples (Appendix A) The results providenot only a more comprehensive geochemical dataset for the NYT than was previ-ously available but also a consistent basis for comparison with the Prato Spilla `Crsquodataset All of the WDS data reported here (Appendix A) were measured at the samelaboratory (Tephrochronology Analytical Unit University of Edinburgh) using thesame sample pretreatment and preparation protocol The WDS results for the NYTdinoter to a minor degree from the EDS results (table 1 and Appendix A) especiallywith respect to the amounts of silica aluminium and calcium measured The EDS
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788 S M Davies and others
4 8FeO ()
TiO
2 (
) Neapolitan Yellow Tuff(Procida)Neapolitan Yellow Tuff(Prato Spilla lsquoCrsquo)
0
1
2
3
40 50 60 70
MgO
(
)
SiO2 ()
K2O
(
)
40 50 60 70
0
04
08
4
8
12
SiO2 ()
(a)(b)
(c)
Figure 7 Bi-plots of SiO2 K2 O SiO2 MgO and FeOTiO2 for the WDS analyses obtainedfrom glass shards of the NYT from Procida (Naples) and Prato Spilla Crsquo Means and standarddeviations are shown
results show a higher degree of statistical scatter than the WDS measurements whichmay reregect the fact that the data were normalized combined with the inreguence ofvariation in water content between shards
There is a very close correspondence between the WDS data for the Prato Spilla `Crsquomicro-tephra shards and those obtained from the type-material near Naples (shy g-ure 7) The geochemical data strongly suggest therefore that the NYT is representedat the Prato Spilla `Crsquo site by a discrete layer of micro-tephra particles This conclu-sion is compatible with the pollen-stratigraphic data from the site and accords withage estimates for the NYT (ca 120 14C ka BP) obtained from other sites (Paterneet al 1990)
These results encourage us to believe that many if not all of the tephras listedin table 1 will be detectable over much larger tracts of Europe than is presently thecase if appropriate research is undertaken to detect layers of micro-tephra particlesin selected sites The authors are presently engaged in a major continent-wide pro-gramme of research in collaboration with a number of European research groupsdesigned to test this hypothesis The focus in this research is on those parts of Europewhere we expect to shy nd overlapping `apronsrsquo of tephra deposition originating fromthe Italian Eifel Massif Central and Icelandic provinces For example a number ofsites in parts of southern France northern Italy and perhaps western Switzerlandmay have received inreguxes of micro-tephra originating from the Italian and Eifelprovinces and perhaps also from the Massif Central Sites in parts of Germany Den-mark and southern Sweden for example may in turn have received tephra depositsfrom both of the Icelandic and Eifel provinces If this proves to be the case then thestage will be set for the construction of a tephrostratigraphical framework for Europewhich will enable Last Termination sequences to be correlated on a continent-widebasis using micro- and visible tephra layers as time-parallel stratigraphic markersFurthermore there is also the possibility that other tephras remain to be discovered
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European tephrochronological framework for Termination 1 789
those which either because of the magnitude or nature of some volcanic eruptionswere distributed over parts of Europe in micro-tephra form only
6 European tephrostratigraphy and the chronology of eventsduring the Last Termination and Early Holocene
One of the crucial issues in Late Quaternary palaeoenvironmental research thatremains to be resolved is the degree to which climatic events inferred from oceanicterrestrial and ice-core records were synchronous during the Last Termination andEarly Holocene If the ice-core records provide realistic estimates of the rates anddurations of climatic events during this period then comparisons between individ-ual records have to be enotected with at least a decadal precision The problem thispresents and the role that tephrostratigraphy can play in resolving some of thedimacr culties involved are put into perspective in shy gure 8
Figure 8 shows some of the data used to calibrate radiocarbon dates (the LakeSuigetsu and Cariaco Basin datasets) plotted against the GRIP ss08c ice-core recordof macr 18O variations The latter has been selected by the INTIMATE group as an arbi-trary and temporary standard for this period and used to deshy ne an event stratig-raphy scheme (shy gure 1) for the Last Termination (see Bjorck et al 1998 Walker etal 2001) As has been alluded to in earlier sections of this paper the uncertaintiesassociated with all of the dating methods currently employed preclude precise com-parisons of ice-core marine and terrestrial records Oceanic and terrestrial recordsmostly rely upon radiocarbon dating locally supplemented in a few cases by varvechronology Imprecisions in radiocarbon dates can arise through site-specishy c fac-tors (eg hard-water or mineral carbon errors in freshwater sequences and reservoirerrors in marine sequences) sample selection laboratory measurements of 14C activ-ity and other factors (Lowe amp Walker 2000) Further imprecision may be introducedby the calibration of radiocarbon dates since the uncertainties in the dataset usedto calibrate pre-Holocene radiocarbon dates INTCAL98 are far higher than forthe Holocene which is based on dendro-calibration (Stuiver et al 1998) There arealso uncertainties anotecting varve chronologies while the ss08c ice-core chronologyfor the Last Termination dinoters signishy cantly from the GISP2 record and indeedfrom other models of the GRIP record (Lowe et al 2001) Published comparisonsbetween ice-core marine and terrestrial records for the Last Termination seldom takeinto account the true magnitude of the dating uncertainties involved and frequentlyemploy circular reasoning
Figure 8 shows the positions on the radiocarbon time-scale of 20 of the tephrasdiscussed earlier in this paper these being the ones for which reasonably conshy dentradiocarbon age estimates can be made (though these will be subject to revised esti-mates in the future) A high number of these occur in the period 14080 14C kaBP but we conshy dently anticipate the discovery in the future of additional tephras(perhaps in micro-tephra form only) which will date to the period 185140 14C kaBP Tephras detected in the GRIP ice core over the same time-interval are plottedon the calendar time-scale in shy gure 8 By providing key `time-linesrsquo between recordstephrostratigraphy can help to resolve some of the dating uncertainties referredto earlier by for example enabling direct comparisons of discrepant age estimatesobtained using dinoterent methods (cf Litt et al 2001) It can also provide estimatesof the magnitudes of the reservoir errors that anotected various marine sectors at dif-
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790 S M Davies and others
-44
-40
-36
-32
cale
ndar
yea
rs B
P
8000
9000
10 0
00
11 0
00
12 0
00
13 0
00
14 0
00
15 0
00
16 0
00
17 0
00
18 0
00
14C age (BP)
VA
SA
Un
Un
Un
Un
Un
BF
Hol
ocen
eG
S-1
GI-
1aG
I-1b
GI-
1cG
I-1d
GI-
1eG
S-2
aG
S-2
bG
S-
2c
Bor
robo
l
La
Nug
egravere
Laa
cher
See
God
ivel
le 5
amp I
-TH
OL
-2
Puy
de D
ocircme
I-T
HO
L-1
Saks
unar
vatn
Houmlg
stor
psm
osse
nU
lmen
er M
aar
amp L
3574
radiocarbon dated European tephra horizons
Cho
pine
Kili
an V
asse
tM
erca
to
God
ivel
le 4
Pom
ici P
rinc
ipal
i amp V
edde
Polla
ra p
umic
eK
OL
-GS-
2 amp
GS
-2B
AS-
12
3
GS
-2B
AS-
4 U
nita
dei
Tef
raSu
peri
ori amp
laye
r Y
-1
Gre
enis
h
L9
20 0
0018
000
16 0
0014
000
12 0
0010
000
-44
-40
-36
-32
800
600
400
200 0
GISP2 volcanicsulphate conc (ppb)
1000
Nea
polit
an Y
ello
w T
uff
GISP2 18O (permil) dGRIP 18O (permil) d
Figure 8 For description see opposite
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 791
ferent times through a comparison of radiocarbon dates obtained from marine andterrestrial horizons in which the same tephra has been detected (see for exampleAustin et al 1995 Bondevik et al 2001 Haregidason et al 2000) Tephrostratigraphymay provide an independent test of suggestions that some of the climatic changesduring the Last Termination were time-transgressive as illustrated for some appar-ently contrasting climatic trends in Iceland Britain and NW Russia (Lowe 2001) Ofparticular importance as far as establishing `leadsrsquo and `lagsrsquo in climatic changes isconcerned are the tephra records from the Greenland ice cores The discovery of theVedde and Saksunarvatn ashes in the GRIP record (Gronvold et al 1995) alreadyprovides a basis for making direct comparisons between marine terrestrial and ice-core records It is a matter of some urgency that the incidence of tephra depositsin the Greenland ice cores be more fully explored in the hope that this will lead tothe recognition of additional time-parallel links between the ice-core records on theone hand and oceanic and terrestrial records on the other An investigation of thenew NordGRIP record for this purpose is currently in progress (S M Davies 2002unpublished data)
Finally a fuller and more reshy ned tephrostratigraphical scheme for Europe will alsohave other applications It will provide an important database for those investigatingthe timing and frequency of volcanic eruptions in Europe during the past 20 000 yror so as well as of the geochemical evolution of the dinoterent volcanic centres overthat period A fuller record of the distribution of micro-tephras may also provideinformation on atmospheric circulation patterns during the dispersal and depositionperiods as well as on the nature and altitude of the eruption columns which mayin turn provide inferences about magma viscosity
This paper is a contribution to the INTIMATE project of the INQUA Palaeoclimate Com-mission and the work is supported by a Leverhulme Trust Research project (grant allocationnumber F07537C) entitled Testing hypotheses of rapid climate change using tephrochronol-ogyrsquo SMDrsquo s contribution was completed during possession of a NERC PhD studentship(GT 0499ES162) We are extremely grateful to Dr Peter G Hill for his assistance withthe EPMA analyses at the Tephrochronology Analytical Unit University of Edinburgh We alsothank Dr G Mastrolorenzo (Vesuvius Observatory) and Miss G Swindle for assistance duringthe macreld investigations in Naples Thanks are also expressed to two anonymous reviewers forcomments on an earlier draft
Appendix A
Table 2 shows the major oxide concentrations of NYT glass shards from Procidaand Prato Spilla `Crsquo and of the Mercato Tephra from the Naples area (see x 4 forsite context) All oxides are shown as weight and total iron is expressed as FeO
Figure 8 Radiocarbon calibration curve for Termination 1 and the Early Holocene compared with theGRIP macr 18 O event stratigraphy the GRIP ss08c and GISP2 macr 18 O records (wwwngdcnoaagov) andknown tephra horizons from this period The shaded areas represent the cooler climatic episodes andare labelled with the Greenland stratotype terminology (Bjorck et al 1998) Where radiocarbon agesare reported in table 1 as a range the mean is given here Abbreviations for GRIP horizons are asfollows Un unknown (approximate positions are given (S Johnsen 2001 personal communication))SA Saksunarvatn Ash VA Vedde Ash BF Black Feather Sulphate concentrations from the GISP2record are also shown (Zielinski et al 1996) Open circles denote radiocarbon calibration data fromLake Suigetsu (Kitagawa amp van der Plicht 2000) Filled circles denote radiocarbon calibration data fromCariaco Basin assuming a marine reservoir age of 420 14 C yr (Hughen et al 1998)
Phil Trans R Soc Lond A (2002)
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792 S M Davies and others
Tab
le2
Majo
roxi
de
con
cen
trati
on
sof
NY
Tgl
ass
shard
sfr
om
Pro
cida
an
dP
rato
Spil
laC
rsquoan
dof
the
Mer
cato
Tep
hra
from
the
Naple
sare
a(s
eex4
for
site
con
text
)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
roci
da)
1584
204
0177
634
201
106
828
635
197
5969
1W
DS
2598
603
9178
027
101
204
924
244
583
4965
8W
DS
3586
604
5173
631
100
805
924
342
183
0951
9W
DS
4583
903
9177
933
000
906
924
540
486
9958
3W
DS
5605
106
8179
126
901
204
923
243
086
1976
4W
DS
6591
704
5177
332
801
006
425
740
887
8968
0W
DS
7581
804
1178
031
501
107
125
640
086
9956
1W
DS
8589
504
2179
533
701
506
926
740
987
5970
4W
DS
9592
003
9178
135
101
007
026
443
585
7972
7W
DS
10
591
404
2174
631
601
105
723
442
482
6957
0W
DS
11
593
403
6177
131
301
506
726
439
188
5967
6W
DS
12
588
103
8176
128
100
505
525
141
583
4952
1W
DS
13
577
003
8176
533
500
807
228
140
384
8952
0W
DS
14
586
004
7179
735
300
706
827
842
984
6968
5W
DS
15
588
104
2180
629
400
505
924
937
993
0964
5W
DS
16
579
603
9178
536
501
308
228
836
087
1959
9W
DS
17
580
103
9177
631
500
907
327
039
488
9956
6W
DS
mea
n588
104
2177
631
901
006
525
940
686
9962
8
sd
(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(07
8)
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 793
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
rato
Spil
laC
rsquo)
1552
105
4177
247
401
914
38
735
578
9951
1W
DS
2557
305
7179
845
701
512
640
136
581
5960
6W
DS
3595
004
4173
724
302
003
117
652
877
8950
7W
DS
4575
704
2179
433
001
406
627
043
083
6953
7W
DS
5599
904
0178
826
401
304
421
841
688
4966
5W
DS
6591
103
8177
826
601
105
022
443
888
8960
2W
DS
7565
304
5180
939
501
410
532
535
791
8962
1W
DS
8597
606
9180
826
501
604
821
546
684
6970
7W
DS
9571
805
6179
939
801
109
932
240
883
6964
7W
DS
10
588
603
7176
527
601
104
721
042
487
7953
3W
DS
11
559
404
9180
544
501
812
339
435
878
6957
2W
DS
12
594
704
0181
328
301
705
522
144
785
6967
9W
DS
13
611
103
7187
016
900
802
419
938
195
9975
8W
DS
14
599
204
4181
128
601
404
620
844
986
6971
6W
DS
15
601
204
4177
328
302
004
722
446
385
5972
1W
DS
16
595
104
5176
428
801
504
722
744
884
3962
8W
DS
17
603
704
1177
825
101
503
520
348
181
2965
3W
DS
18
558
704
5179
647
401
813
139
836
879
0960
7W
DS
19
589
602
8178
830
901
606
622
436
091
8960
5W
DS
20
553
606
3178
647
401
913
840
136
978
0956
6W
DS
21
579
004
0175
739
000
708
328
338
286
7959
9W
DS
mea
n582
804
6179
033
401
507
427
341
484
8962
1
sd
(1
87)
(01
0)
(02
7)
(09
2)
(00
4)
(03
9)
(08
0)
(04
9)
(05
0)
(07
0)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
794 S M Davies and others
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)
1575
202
7194
219
701
101
016
374
766
9951
8W
DS
2575
802
9194
523
902
201
520
273
564
5959
0W
DS
3574
301
4205
219
101
100
416
481
266
1965
2W
DS
4575
500
7206
018
002
000
415
181
669
3968
6W
DS
5580
000
9208
018
601
300
515
883
367
1975
5W
DS
6571
001
0206
016
101
600
515
078
967
1957
2W
DS
7577
501
1201
117
101
500
620
675
655
4950
5W
DS
8573
700
9212
717
101
900
815
187
564
2973
9W
DS
9580
301
3208
715
801
400
824
81
754
1968
1W
DS
10
574
400
6211
18
402
00
516
480
567
8971
6W
DS
11
577
200
7214
212
501
200
829
879
247
962
6W
DS
12
572
200
9211
217
301
501
15
980
465
9966
3W
DS
13
571
800
7210
417
402
201
16
184
467
2971
2W
DS
14
567
300
9208
916
901
400
917
383
262
5959
3W
DS
15
568
600
8205
918
202
101
414
682
666
6960
8W
DS
16
572
501
1211
318
202
01
215
884
364
5970
9W
DS
17
572
901
2212
916
502
101
215
883
667
2973
4W
DS
18
573
01
4211
716
301
801
416
83
365
5970
4W
DS
19
569
201
1207
418
602
101
414
982
964
961
6W
DS
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
3)
(04
2)
(01
3)
(00
1)
(00
2)
(01
)(0
39)
(01
1)
(02
5)
Phil Trans R Soc Lond A (2002)
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796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
References
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Hoek W Z amp Bohncke S J P 2001 Oxygen isotope wiggle matching as a tool for synchronisingice-core and terrestrial records over Termination 1 Quat Sci Rev 20 12511264
Hughen K A Overpeck J T Peterson L C amp Trumbore S 1996 Rapid climate changes inthe tropical Atlantic region during the last deglaciation Nature 380 5153
Hughen K A Overpeck J T amp Lehman J 1998 A new 14 C calibration data set for the LastDeglaciation Radiocarbon 39 483494
Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
Hunt J B amp Hill P G 1996 An inter-laboratory comparison of the electron probe microanalysisof glass geochemistry Quat Int 3436 229241
Hunt J B amp Hill P G 2001 Tephrological implications of beam sizesample size ereg ects inelectron microprobe analysis of glass shards J Quat Sci 16 105117
Hunt J B Fannin N G T Hill P G amp Peacock J D 1995 The tephrochronology andradiocarbon dating of North Atlantic Late Quaternary sediments an example from the StKilda Basin In The tectonics sedimentation and palaeoceanography of the North Atlanticregion (ed R A Scrutton M S Stoker G B Shimmield amp A W Tudhope) vol 90pp 227248 Geological Society of London Special Publication
Hunt J B Clift P D Lacasse C Vallier T L amp Werner R 1998 Standardisation ofelectron probe microanalysis of glass geochemistry In Proc ODP Scientimacrc Results vol 152pp 8591 College Station TX Ocean Drilling Program
Jakobsson S P 1979 Outline of the petrology of Iceland Jokull 29 5773
Juvignparae E 1987 Deux retombparaees volcaniques tardiglaciaires dans le Cparaezallier (Massif CentralFrance) Bull Ass Fr Etud Quat 13 37
Juvignparae E 1993 Contribution microa la tparaephrostratigraphie du Quaternaire et son application microa lagparaeomorphologie Mparaem Serv Explicat Cartes Gparaeol Min Belg 36 166
Juvignparae E amp Gewelt M 1987 La Narse drsquo Ampoix comme tparaephrostratotype dans la Chasup3 ne desPuys mparaeridionale (France) Bull Ass Fr Etud Quat 29 3749
Juvignparae E Kozarski S amp Nowaczyk B 1995 The occurrence of Laacher See Tephra in Pomera-nia NW Poland Boreas 24 225231
Juvignparae E Bastin B Delibrias G Evin J Gewelt M Gilot E amp Streel M 1996 Acomprehensive pollen and tephra based chronostratigraphic model for the Lateglacial andHolocene period in the French Massif Central Quat Int 3436 113120
Keller J 1980 The island of Vulcano Rend Soc It Mineral Petrolog 36 369414
Keller J Ryan W B F Ninkovich D amp Altherr R 1978 Explosive volcanic activity in theMediterranean over the past 200 000 years as recorded in deep sea sediments Geol Soc AmBull 89 591604
Kitagawa H amp van der Plicht J 2000 Atmospheric radiocarbon calibration beyond 11 900 calBP from Lake Suigetsu laminated sediments Radiocarbon 42 369380
Kvamme T Mangerud J Furnes H amp Ruddiman W F 1989 Geochemistry of Pleistoceneash zones in cores from the North Atlantic Norsk Geol Tids 69 251272
Lacasse C Sigurdsson H Johannesson H Paterne M amp Carey S 1995 Source of Ash zone 1in the North Atlantic Bull Volcanol 57 1832
Langone L Asioli A Corregiari A amp Trincardi F 1996 Age depth modelling through theLate-Quaternary deposits of the central Adriatic Basin In Palaeoenvironmental analysis ofItalian crater lake and Adriatic sediments (ed F Oldmacreld amp P Guilizzoni) vol 55 pp 177196 Memorie dellrsquo Instituto Italiano di Idrobiologia
Larsen G 2000 Holocene volcanism in Iceland and tephrochronology as a tool in volcanologyIn Iceland 2000 modern processes and past environments Keele University UK
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 799
Litt T amp Stebich M 1999 Bio- and chronostratigraphy of the Lateglacial in the Eifel regionGermany Quat Int 61 516
Litt T Brauer A Goslar T Merkt J Balaga K Muller H Ralska-Jasiewiczowa MStebich M amp Negendank J F W 2001 Correlation and synchronisation of Lateglacialcontinental sequences in northern Central Europe based on annually laminated lacustrinesediments Quat Sci Rev 20 12331249
Long D amp Morton A C 1987 An ash fall within the Loch Lomond stadial J Quat Sci 297101
Lotter A F Eicher U Siegenthaler U amp Birks H J B 1992 Lateglacial climatic oscillationsas recorded in Swiss lake sediments J Quat Sci 7 187204
Lowe J J 1992 Lateglacial and Early Holocene lake sediments from the Northern ApenninesItaly|pollen stratigraphy and radiocarbon dating Boreas 21 193208
Lowe J J 2001 Abrupt climatic changes in Europe during the last glacialinterglacial tran-sition the potential for testing hypotheses on the synchroneity of climatic events usingtephrochronology Global Planet Change 603 7384
Lowe J J amp Turney C S M 1997 Vedde Ash layer discovered in a small lake basin on theScottish mainland J Geol Soc Lond 154 605612
Lowe J J amp Walker M J C 2000 Radiocarbon dating the last glacialinterglacial transition(ca 14914 C ka BP) in terrestrial and marine records the need for new quality assuranceprotocols Radiocarbon 42 5368
Lowe J J amp Watson C 1993 Lateglacial and Early Holocene pollen stratigraphy of the northernApennines Italy Quat Sci Rev 12 727738
Lowe J J Birks H H Brooks S J Coope G R Harkness D D Mayle F E SheldrickC Turney C S M amp Walker M J C 1999 The chronology of palaeoenvironmental changesduring the Last GlacialHolocene transition towards an event stratigraphy for the BritishIsles J Geol Soc Lond 156 397410
Lowe J J Hoek W Z amp INTIMATE group 2001 Inter-regional correlation of palaeoclimaticrecords for the Last GlacialInterglacial transition a protocol for improved precision recom-mended by the INTIMATE project group Quat Sci Rev 20 11751187
Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
Mangerud J Lie S E Furnes H Kristiansen I L amp Liquest mo L 1984 A Younger Dryas ashbed in western Norway and its possible correlation with tephra beds from the Norwegian Seaand North Atlantic Quat Res 21 85104
Mangerud J Furnes H amp Jparaohansen J 1986 A 9000 year-old ash bed on the Faroe IslandsQuat Res 26 262265
Martini J 1970 Recherche de retombparaees volcaniques dans le sud-est de la France et la Suisseoccidentale Arch Sci 23 641674
Martini J amp Duret J J 1965 Note preliminaire sur la presence drsquo un niveau de cendres vol-caniques dans des sparaediments post-glaciaires des environs de Genmicroeve Arch Sci 18 587588
Mayewski P A Meeker L D Twickler M S Whitlow S Yang Q Lyons W B amp Pren-tice M 1997 Major features and forcing of high latitudes Northern Hemisphere atmosphericcirculation using a 110 000 year long glaciochemical series J Geophys Res 102 345365
Merkt J Muller H Knabe W Muller P amp Weiser T 1993 The Early Holocene Saksunarvatntephra found in lake sediments in NW Germany Boreas 22 93100
Narcisi B 1993 Segnalazione di un livello piroclastico di provenienza etnea nellrsquo area del Fucino(Italia Centrale) Quaternario 6 8792
Narcisi B 1996 Tephrochronology of a Late Quaternary lacustrine record from the Monticchiomaar (Vulture volcano southern Italy) Quat Sci Rev 15 155165
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
800 S M Davies and others
Newton A J amp Dugmore A J 1993 Tephrochronology of Core C from Lago Grande di Mon-ticchio In Paleolimnology of European Maar Lakes (ed J F W Negendank amp B Zolitschka)Lecture Notes in Earth Science vol 49 333348 Springer
Oldmacreld F Appleby P G amp Thompson R 1980 Palaeoecological studies of lakes in theHighlands of Papua New Guinea J Ecol 68 457477
Orsi G Drsquo Antonio M de Vita S amp Gallo G 1992 The Neapolitan Yellow Tureg a large mag-nitude trachytic phreatoplinian eruption eruptive dynamics magma withdrawal and calderacollapse J Volcanol Geotherm Res 53 275287
Paterne M Guichard F Labeyrie J Gillot P Y amp Duplessy J C 1986 Tyrrhenian Seatephrochronology of the oxygen isotope record for the past 60 000 years Mar Geol 72259285
Paterne M Guichard F amp Labeyrie J 1988 Explosive activity of the south Italian volca-noes during the past 80 000 years as determined by marine tephrochronology J VolcanolGeotherm Res 34 153172
Paterne M Labeyrie J Guichard F Mazaud A amp Maitre F 1990 Fluctuations of the Cam-panian explosive volcanic activity (south Italy) during the past 190 000 years as determinedby marine tephrochronology Earth Planet Sci Lett 98 166174
Pawse A Beske-Diehl S amp Marshall S A 1998 Use of magnetic hysteresis properties andelectron spin resonance spectroscopy for the identimacrcation of volcanic ash a preliminary studyGeophys J Int 132 712720
Pearce N J G Westgate J A amp Perkins W T 1996 Developments in the analysis of singleglass shards in volcanic deposits by laser ablation ICP-MS quantitative and single internalstandard multi-element methods Quat Int 3436 213227
Pearce N J G Westgate J A Perkins W T Eastwood W J amp Shane P 1999 Theapplication of laser ablation ICP-MS to the analysis of volcanic glass shards from tephradeposits bulk glass and single shard analysis Global Planet Change 21 151171
Pilcher J R amp Hall V A 1992 Towards a tephrochronology for the Holocene of the north ofIreland Holocene 2 255259
Ponel P amp Lowe J J 1992 Coleopteran pollen and radiocarbon evidence from the Prato Spillarsquo Drsquo succession N Italy C R Acad Sci Paris Sparaer II 315 14251431
Rose N L Golding P N E amp Battarbee R W 1996 Selective concentration and enumerationof tephra shards from lake sediment cores Holocene 6 243246
Ruddiman W F amp Glover L K 1972 Vertical mixing of ice rafted volcanic ash in NorthAtlantic sediments Geol Soc Am Bull 83 28172836
Ruddiman W amp McIntyre A 1981 The North Atlantic Ocean during the last deglaciationPalaeogeogr Palaeoclimatol Palaeoecol 35 145214
Santacroce R 1987 Somma Vesuvius Quad Ric Sci 114 252
Sarna-Wojcicki A 2000 Tephrochronology In Quaternary geochronology methods and applica-tions (ed J S Noller J M Sowers amp W R Lettis) AGU Reference shelf vol 4 pp 357377Washington DC American Geophysical Union
Sejrup H P Sjiquest holm J Furnes H Beyer I Eide L Jansen E amp Mangerud J 1989Quaternary tephrochronology on the Iceland Plateau north of Iceland J Quat Sci 4 109114
Sikes E L Samson C R Guilderson T P amp Howard W R 2000 Old radiocarbon agesin the southwest Pacimacrc Ocean during the last glacial period and deglaciation Nature 405555558
Stein R Nam S-I Grobe H amp Hubbersten H 1996 Late Quaternary glacial history andshort term ice rafted debris deg uctuations along the East Greenland continental marine In LateQuaternary palaeoceanography of the North Atlantic margins (ed J T Andrews W E NAustin H Bergsten amp A E Jennings) pp 135151 Geological Society London SpecialPublication
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 801
Stuiver M amp Grootes P M 2000 GISP2 oxygen isotope ratios Quat Res 53 277284
Stuiver M Reimer P J Bard E Beck J W Burr G S Hughen K A Kromer BMcCormac G Van der Plicht J amp Spurk M 1998 INTCAL 98 radiocarbon age calibration24 0000 cal BP Radiocarbon 40 10411083
Sweatman T R amp Long J V P 1969 Quantitative electron microprobe analysis of rock formingminerals J Petrol 7 332379
Turney C S M 1998 Extraction of rhyolitic ash from minerogenic lake sediments J Paleolim-nol 19 199206
Turney C S M amp Lowe J J 2001 Tephrochronology In Tracking environmental changes inlake sediments physical and chemical techniques (ed W M Last amp J P Smol) DordrechtKluwer Academic
Turney C S M Harkness D D amp Lowe J J 1997 The use of microtephra horizons tocorrelate Lateglacial lake sediments successions in Scotland J Quat Sci 12 525531
Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
van den Bogaard P amp Schmincke H 1985 A widespread isochronous Late Quaternary tephralayer in central and northern Europe Geol Soc Am Bull 96 15541571
van den Bogaard B Dordeg er W Sandgren P amp Schmincke H-U 1994 Correlating theHolocene records Icelandic tephra found in Schleswig-Holstein (northern Germany) Natur-wissenschaften 81 554556
Vernet G amp Raynal J-P 2001 Tephrostratigraphy of the Limagne revisited Implications forLateglacial and Holocene Prehistory In Tephras chronology archaeology (ed E Juvignparae ampJ-P Raynal) pp 111116 Dossiers de lrsquo ArchparaeoLogis no 1 France
Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
Vezzoli L 1991 Tephra layers in Bannock Basin (eastern Mediterranean) Mar Geol 1002134
von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
Walker M J C Bjorck S Lowe J J Cwynar L C Johnsen S Knudsen K-L WohlfarthB amp INTIMATE Group 1999 Isotopic events in the GRIP ice core a stratotype for the LatePleistocene Quat Sci Rev 18 11431150
Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
Phil Trans R Soc Lond A (2002)
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802 S M Davies and others
Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
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European tephrochronological framework for Termination 1 777
N
0 500 km
Confirmed records of Vedde Ash (visible occurrences)
New records of Vedde Ash from flotation method
Extended area of Vedde Ash detection (micro-tephra)
Known area of Laacher See Tephra (visible occurrences)
Confirmed records of Neapolitan Yellow Tuff (visible occurrences)
New record of Neapolitan Yellow Tuff from flotation method
Known area of Neapolitan Yellow Tuff
Volcanic centres of particular relevance to this study
Other major volcanic centres in Europe
Figure 2 Location of the principal volcanic centres that were active during Termination 1 andthe Early Holocene The known distribution of the Vedde Ash (VA) Laacher See (LST) andNeapolitan Yellow Tureg (NYT) are shown
the behaviour of each element cannot be monitored independently during measure-ment and so this approach fails to detect for example any signishy cant mobilizationof sodium during the bombardment process (Hunt amp Hill 1993) Although WDSrequires a higher beam current and a longer counting time than EDS the formeronoters the distinct advantage of sequential acquisition of elemental data so that thedegree of sodium loss can be tracked The morphology of individual glass shards canalso distort EDS data a problem that is reduced when using WDS because for thisprocedure glass shards are mounted in an epoxy resin and polished to provide aregat surface for analysis Hence data should always be obtained using WDS whereverpossible
Even when WDS is used as a common tool for determining the geochemical spectraof samples aberrant results can arise that inreguence data comparisons For examplesome glass shards may contain tiny crystalline inclusions of feldspar and these shouldbe avoided when selecting surface points for analysis (Hunt amp Hill 2001) Hunt amp Hill
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778 S M Davies and others
6
4
2
40 50 60 70 80
K2O
(
)
SiO2 ()
Laacher See
Iceland
Veidivoumltn-Dyngjufjoumlll
Katla (basalt)
Grimsvoumltn-Kverkfjoumlll
Hekla
Katla (rhyolitic)
0
Icelandic volcanic centres8
10
Massif Central
Etna
Campanian
Figure 3 Bi-plot of SiO2 and K2 O concentrations in tephras derived from the main Europeanash provinces (modimacred after Mangerud et al 1984) The Campanian Massif Central and Etnaconcentrations are based on the data presented in table 1
(2001) have concluded that small variations in the laboratory procedures employedto determine glass chemistry can lead to misidentishy cation of sources for glass shardsand give an example of shards with a Jan Mayen provenance wrongly attributedto an Icelandic source Clearly there is a need for standardization of laboratoryprocedures and while a number of recommendations have recently been advocated(Froggatt 1992 Hunt amp Hill 1993 Hunt et al 1998) there is still some variation inlaboratory and operator practice (Hunt amp Hill 1996) Standardization is also requiredin the form in which results are presented to ensure comparability Normalizationof the data to 100 a practice employed by some researchers can obscure poorresults and hence lead to incorrect comparisons (Hunt amp Hill 1993) However othersargue that it may actually facilitate comparisons between samples by removing thedistorting enotects of the water component contained in glass shards (see for exampleFroggatt 1992) The majority of the published Italian and some of the Eifel datahave been normalized while those from other parts of Europe have not and hencedata comparisons are not always straightforward
Table 1 provides mean values and standard deviations for major oxide concentra-tions obtained from those tephras for which data are presently available The tableincludes previously unpublished WDS results for the Neapolitan Yellow Tunot (NYTdiscussed in x 4 below) and for the Mercato Tephra While individual tephra layersmay be geochemically distinct the geochemical envelopes representing the collectivedata obtained from all of the tephras assigned to each major volcanic province showsignishy cant overlaps as is illustrated in the bi-plots and ternary plots (shy gures 3 and 4)of selected oxide concentration data It is clear therefore that measurement of majoroxide concentrations does not satisfactorily discriminate between some tephras orig-inating from dinoterent volcanic centres (as noted by van den Bogaard amp Schmincke(1985) and Frezzotti amp Narcisi (1996) with respect to Eifel and Italian tephras)nor of tephras of dinoterent age originating from the same volcanic centre (Bond et
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 779
40 50 60 70 80
K2O
(
)
SiO2 ()
shyshyshyshy
shy
shyshy
shyshyshy
shy
shy
shy
shy
reg
reg regreg
regregregregreg regregregregreg
FF
F
ll
l
l
4 8 12 16
reg
regreg
regreg
regregreg
regreg
regregreg
shy
F
l shyshyshyshyshy shyshyshyshyshyshy
F
F
l
ll
FeO ()
TiO
2 (
)
reg
l
Iceland
Eifel
F
shy ItalyMassif Central
100
80
60
40
20
100
80
60
40
20
100 80 60 40 20
CaO
FeO
K2O
regregreg
reg
reg
reg
reg
reg
reg
regregreg
shyF
F
F
regreg
l
lllshy
shyshyshy
shyshyshy
l
0
2
4
6
8
10
0
1
2
3
4
5
regreg
regreg
regreg
regreg
regreg
reg
reg
regreg
l
l
ll
shy
shyshy
shyshy
shy
shyshy
FF
F
100
80
60
40
20
100
80
60
40
20
100 80 60 40 20
K2ONa2O
CaO
(c) (d)
(a)
(b)
Figure 4 Plots of selected geochemical data obtained from tephras of Termination 1 age (seetable 1) (a) Bi-plot of mean SiO2 and K2 O values (b) Bi-plot of mean FeO and TiO2 values(c) Ternary plot indicating variations in the proportions of FeO CaO and K2 O (d) Ternaryplot indicating variations in the proportion of CaO Na2 O and K2 O
al 2001) Individual tephra layers are presently assigned to a particular volcanicevent on the basis of a combination of criteria usually including examination of thephysical properties (eg refractive index and surface detail of the glass shards) thestratigraphic position of the layer and independent assessment of the age of the layeras well as any geochemical data that may be available The construction of a tephro-stratigraphical scheme would clearly beneshy t from the application of a more diagnostic
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780 S M Davies and others
geochemical tool One approach that has promise is the analysis of trace and rareearth elements using an ultraviolet laser ablation inductively coupled plasma massspectrometer (UV-LA-ICP-MS) (Pearce et al 1996 1999 Eastwood et al 1999)This approach has been applied successfully to analysis of tephras of Mid-Holoceneage but not yet to tephras that fall within the period of interest here
4 Tephra layers in Europe and the North Atlantic regiondated to between 185 and 80 14C ka
(a) Icelandic province
The Icelandic volcanic systems are divided into three main groups based on theirgeochemical characteristics tholeiitic basalts transitional alkali basalts and alkaliolivine basalts (Jakobsson 1979) Collectively magmas from the Icelandic provincespan a wide geochemical spectrum although individual volcanic centres have tightgeochemical distributions (shy gure 3) for four of the main centres Grimsvotn-Kverfjolland Veidvotn-Dyngjufoll which form part of the northern (tholeiitic) volcanic zoneand Hekla and Katla which fall within the eastern (alkali olivine basalt and transi-tional alkali basalt) volcanic zone (Haregidason et al 2000) These appear to be thekey centres for the tephras listed in table 1 that have been assigned an Icelandicorigin
One of the best-known and most widely dispersed tephra horizons in northernEurope that has an Icelandic origin is the Vedde Ash (VA) which was depositedca 103 14C ka BP (Birks et al 1996 Wastegard et al 1998) within the GS-1Younger Dryas chronozone This ash is believed to originate from the Katla complexwithin the transitional alkali basalt province (Mangerud et al 1984 Lacasse et al 1995) in the south of the island The ash has a bimodal geochemical composition (rhy-olitic and basaltic) which is thought to reregect derivation from two separate magmachambers Studies of recent volcanic events in Iceland have shown that the mostexplosive eruptions generating the largest amounts of tephra occur in this tran-sitional alkali basalt province (Haregidason et al 2000) It is also believed that thewidespread distribution of this ash was caused by the development of co-ignimbriteash plumes during an ignimbrite-forming eruption (Lacasse et al 1995)
Layers of VA that are visible to the naked eye have been found in lake sediments inwestern Norway (Mangerud et al 1984) and the Inner Hebrides Scotland (Davies etal 2001) and in marine cores throughout the NE Atlantic (see for example Kvammeet al 1989 Lacasse et al 1995) in the northern North Sea (Long amp Morton 1987)on the Iceland plateau (Ruddiman amp McIntyre 1981 Sejrup et al 1989) and on theeast Greenland continental margin (Stein et al 1996) The distribution of the VAin North Atlantic marine sequences is characterized by an arcuate lobe extendingsouthwest from the Denmark Strait and curving eastwards to mid-latitudes in theNorth Atlantic (Lacasse et al 1995) This strongly suggests deposition from raftedice which was displaced to the southwest and south in a circulating counterclockwisegyre (Ruddiman amp Glover 1972) This may well reregect Katlarsquos close proximity tothe southern coast of Iceland with the Vedde tephra being deposited on ice thatcalved directly into the North Atlantic (Haregidason et al 2000) However depositionvia the atmosphere almost certainly took place as well as is indicated by the recentdiscoveries of rhyolitic VA in micro-tephra form in several sites in Scotland (Turneyet al 1997) southern Sweden (Wastegard et al 1998 2000a) and western Russia
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European tephrochronological framework for Termination 1 781
(Wastegard et al 2000b) A more recent discovery of a relatively high concentrationof rhyolitic VA glass shards in the northern Netherlands indicates that the ash maywell have been dispersed much further south than previously thought (S M Davies2002 unpublished work) Finally glass shards assigned to the VA have also beendiscovered in the GRIP ice core and dated to 11 980 sect 80 GRIP yr BP (Gronvold etal 1995) This discovery is extremely important for it indicates that the VA maywell provide a reliable time-parallel marker horizon between ice-core marine andterrestrial records
Two other important Icelandic ash layers the Borrobol and Saksunarvatn Tephraswere deposited near the beginning and end of the Last TerminationEarly Holoceneinterval respectively The Borrobol Tephra was discovered for the shy rst time in lakesediments in several sites in Scotland and as yet is known only in micro-tephra formIt has been dated in Scottish sites to ca 123 14C ka BP (Turney et al 1997) Whatis thought to be a contemporaneous tephra has been detected in marine sedimentson the North Icelandic shelf (Eirplusmn ksson et al 2000) This certainly has a very similargeochemical composition to those reported from Scotland but the horizon in whichit was discovered on the North Iceland plateau has been dated to 134 14C ka Theage discrepancy between the Scottish and Icelandic Borrobol Tephra layers may wellreregect the inreguence of a marine reservoir error although the possibility that severaltephras with similar geochemical composition were erupted over a period exceeding1000 yr cannot be ruled out (Larsen 2000)
The Saksunarvatn Ash appears to have been one of the largest Holocene eruptionsin Iceland It has a tholeiitic basaltic composition which is considered to indicate anorigin in the Grimsvotn or Kverfjoll complex (shy gure 3) (Mangerud et al 1986) Layersof this ash have been identishy ed in sites on the Faroe Islands (Mangerud et al 1986Dugmore amp Newton 1998 Wastegard et al 2001) the Shetland Isles (Bennet et al 1992) northern Germany (Merkt et al 1993) western Norway (micro-tephra) (Birkset al 1996) and in the GRIP (Gronvold et al 1995) and NordGRIP ice cores (S MDavies 2002 unpublished work) It has been dated to between 9060 and 8930 14C kaBP (Birks et al 1996) in Norway and to ca 10 240 sect 30 GRIP yr BP in the GRIPice core (Gronvold et al 1995) The Saksunarvatn Ash may thus provide a secondimportant widespread time-parallel marker between ice-core marine and terrestrialrecords
Other Icelandic tephras of rhyolitic amacr nity are less well known in terms of theirdistribution and geochemical variation The Hogstorpsmossen Tephra reported fromSweden (Bjorck amp Wastegard 1999) and the L3754 tephra discovered in the FaroeIslands (Dugmore amp Newton 1998) are known from single sites only and so theirpotential for tephrostratigraphy is uncertain at present Furthermore the geochem-ical spectrum of the Hogstorpsmossen Tephra is based on a small dataset with lowanalytical totals
A number of tephras of basaltic composition have originated from Iceland buttheir distributions are largely conshy ned to Iceland or to marine cores collected fromclose to the Iceland coast or in the North Atlantic These include the tephras listedas 1-THOL-1 1-THOL-2 KOL-GS-2 GS-2BAS-1 GS-2BAS-2 GS-2BAS-3 andGS-2BAS-4 in table 1 (Kvamme et al 1989 Bjorck et al 1992 Eirplusmn ksson et al 2000 Haregidason et al 2000) The shy rst two in this list are tholeiitic basaltic tephrasassociated with the VA in a complex series of tephras collectively termed NorthAtlantic Ash Zone 1 (NAAZ1) which has been detected in numerous marine cores
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782 S M Davies and others
from the North Atlantic Initially thought to represent a single eruption analysisof high-resolution sediment sequences from Lake Torfadalsvatn in northern Iceland(Bjorck et al 1992) the Hebridean Shelf near NW Scotland (Austin amp Kroon 1996)the St Kilda Basin (Hunt et al 1995) and the open North Atlantic (Bond et al 2001)has demonstrated that NAAZ1 comprises a series of distinct ashes that probablyreregect separate eruption events 1-THOL-1 is thought to originate from Veidivotn(shy gure 3) while Grimsvotn may have been the source of 1-THOL-2 (Kvamme et al 1989)
KOL-GS-2 is also of tholeiitic basaltic composition but is thought to originatefrom the Kolbeinsey Ridge system (Eirplusmn ksson et al 2000) To date this tephra hasbeen detected in one marine core only within the same record on the North Ice-landic shelf as that from which the correlative of the Borrobol Tephra was alsoreported (Eirplusmn ksson et al 2000) GS-2BAS-1 to GS-2BAS-4 are of uncertain ori-gin but are thought to have been deposited at roughly the same time as KOL-GS-2(ca 134 14C ka BP (Haregidason et al 2000))
The limited distribution of these basaltic tephras a feature that is not unique toIcelandic basaltic material may reregect two factors the relative magnitude of the vol-canic eruptions from which they were derived and the limited aerial transportationof basaltic glass which is denser than rhyolitic material However a rather surpris-ing recent discovery is that of visible basaltic VA in a site on the Isle of Skye inthe Inner Hebrides Scotland (shy gure 5) (Davies et al 2001) All other occurrencesof VA in Scotland are exclusively of rhyolitic material and in micro-tephra formonly (Turney et al 1997 Turney 1998) Clearly basaltic tephra must have beentransported subaerially as far south as Skye and the reason why it has not beendetected at other sites in Scotland is puzzling We suspect that this partly reregectsthe laboratory methods employed to separate glass shards present in low concentra-tion within a micro-tephra layer from the host sediment The technique used is adensity-separation (regotation) procedure (Turney 1998) and as basaltic shards havea specishy c density similar to quartz one of the most abundant minerals in lake sedi-ments of Late Glacial age basaltic material is dimacr cult to detect using this methodThis hypothesis is currently under investigation and alternative detection methodsare being explored including magnetic separation (Mackie et al 2002)
Several other events listed in table 1 that are of probable Icelandic origin includetephras recorded in the GRIP ice core including visible (eg the `Black Featherrsquo)tephras as well as uncertain tephras inferred from distinct Ca peaks (S Johnsen2001 personal communication) No glass shards have yet been detected in the latterbut a volcanic origin is assumed because high Ca peaks are associated with knowntephras in other Greenland ice cores (S Johnsen 2001 personal communication)These are referred to as `unknownrsquo in table 1 No geochemical analyses are availablefrom these horizons so their origin must remain speculative but a possible source isIceland in view of its proximity to the Greenland ice sheet and assumed atmosphericcirculation patterns
(b) Eifel province
There are two prominent tephra events dated to the Termination 1Early Holocenetime-span that originated from the Eifel province the Laacher See Tephra (LST)and the Ulmener Maar Tephra (UMT) Visible occurrences of the LST indicate that
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European tephrochronological framework for Termination 1 783
Vedde Ash
615 625 635 645 655depth (cm)
organic lake mudsHolocene
silty clayGS-1Younger Dryas
organic lake mudsGI-1Alleroslashd
100 microm
(a)
(b)
Figure 5 (a) Photograph of the visible VA layer discovered at Loch Ashik Isle of Skye InnerHebrides Scotland (b) Light microscope photograph showing the rich content of basaltic shards(examples are indicated by the arrows) within this layer (8024 m m size fraction)
this ash was dispersed over much of central Europe (van den Bogaard amp Schmincke1985 Friedrich et al 1999 Litt amp Stebich 1999) The LST is dated by radiocarbonto ca 110 14C ka BP (van den Bogaard amp Schmincke 1985) and to 11 063sect12 14C BP(Friedrich et al 1999) by varve chronology to 1288 varve ka BP (Brauer et al 1999Litt et al 2001) and by ArAr dating to 129 ka cal BP (van den Bogaard 1995) Ithas a phonolitic composition and is thought to have originated from a plinian andphreatomagmatic eruption with the distal ash being carried in three distinct plumesone to the northeast towards Poland one to the west and the third to the southcovering the Jura Mountains and north Italy (van den Bogaard amp Schmincke 1985Juvigne et al 1995 Bossuet et al 1997) This pattern is thought to reregect altitu-dinal variations in the predominant wind direction Sedimentary sequences near thevolcanic source indicate that the LST consists of three main layers which represent
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784 S M Davies and others
dinoterent eruption phases These are grouped together as the Laacher See TephraFormation but the three individual units can be traced within and between a seriesof depositional fans The geochemical data obtained from these three LST layersshow signishy cant variations as reregected in the ternary plots (shy gure 4)
The Early Holocene Ulmener Maar Tephra (UMT) is of rhyolitic composition andappears to be restricted to sites in Germany though this conclusion is also based onrecords of visible tephras only It is dated to ca 956 14C ka BP and to 110 varve ka(Zolitschka et al 1995 Litt et al 2001)
(c) Massif Central province
The Massif Central tephras are mainly of basaltic trachyandesitic compositionwhich is distinct from the other ash provinces (shy gures 3 and 4) and their known dis-tributions are mostly conshy ned to the Massif Central region The ages of the MassifCentral tephras are based on radiocarbon dates obtained from mire and lake sedi-ments which `bracketrsquo the tephras The La Nugsup3ere Tephra with an age of 114 14C kaBP is the oldest Massif Central tephra identishy ed so far within the time-span of inter-est (Etlicher et al 1987 Juvigne et al 1996) The two Godivelle Tephras (5 and 4)are close in age but extensive radiocarbon dating suggests distinct ages of 107and 103 14C ka BP respectively (Juvigne et al 1996) The age of the Puy de DomeTephra is less certain as the estimate is based on only one radiocarbon date froma site in the southern Chaplusmn ne des Puys (table 1) This tephra is thought to havea trachyte composition (Juvigne 1993) although no major element concentrationshave yet been published
The ChopineKilianVasset tephras are thought to be derived from three separateEarly Holocene eruptions although the stratigraphic succession is not known atpresent These trachytic tephras have been radiocarbon dated to ca 854sect150 14C kaBP but are thought to have erupted separately within ca 260 yr (Juvigne et al 1996) This series of tephras is considerably more widespread than the others fromthe region having been identishy ed as far east as the Jura Mountains (Martini amp Duret1965 Martini 1970) Some other ash falls that originated from the Chaplusmn ne des Puysappear to be of local importance only (Vernet et al 1998 Vernet amp Raynal 2001)Geochemical data are currently available for only three of the Massif Central tephrasand so far as is known no attempt has yet been made to identify these tephras inmicro-tephra form
(d ) Italian provinces
The Italian tephras from this period can be assigned to three main volcanic com-plexes the Campanian volcanic shy elds around Naples Etna on Sicily and the AeolianIslands The Campanian complex which includes the Phlegrean Fields Vesuviusand Ischia is mainly trachytic in composition with a geochemical spectrum that isquite distinct from those of the Etna complex and of the Aeolian Islands (shy gure 3)Tephras originating from one or more of these three complexes have been detectedin marine cores from the Tyrrhenian and Adriatic seas as well as other parts of theMediterranean Sea (Keller et al 1978 Paterne et al 1986 1988 1990 Langone etal 1996) and in lake sequences in southern Italy such as Lago Grande di Monticchio(Newton amp Dugmore 1993 Narcisi 1996 Allen et al 1999) and central Italy such asLago Albano near Rome (Calanchi et al 1996) Some work has also been conducted
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European tephrochronological framework for Termination 1 785
in or close to the volcanic source areas in an attempt to establish the full sequenceof volcanic eruptions during the Late Quaternary (see for example Di Vito et al 1999) There are nine Italian tephras reported from marine and lake sequences thatdate from the period between 185 and 80 14C ka BP In all instances the recordsare of visible layers of tephra The ages of some of these are poorly established atpresent with conregicting data obtained from dinoterent sites The ages suggested intable 1 are those favoured in the most recent publications but these may requirere-assessment in the light of future research
The two oldest known tephras in the time-period of interest are the L9 and Green-ish Tephras both recorded as separate features within the annually laminated Lagodi Monticchio maar sequence The lowest of the two L9 is considered to be the cor-relative of the `basalrsquo plinian eruption of Vesuvius (Narcisi 1996) Age estimates ofa palaeosol that underlies the Vesuvius tephra sequence are ca 1617 14C ka BP forthis event (Delibrias et al 1979) L9 has a trachytic composition very similar to theGreenish Tephra (table 1) However L9 which is also a product of Vesuvius is foundstratigraphically below the Greenish Tephra in the Lago di Monticchio core TheGreenish Tephra is dated in the Monticchio sequence to 17 560 varve yr BP (Allenet al 1999) and has a calibrated radiocarbon age estimate of 17 830 sect 300 cal BP(Andronico et al 1995) Both tephras have a dominantly eastwards dispersal basedon the occurrences of visible layers (Santacroce 1987 Narcisi 1996) Both tephrasalso have a trachytic composition and as can be seen from table 1 the reportedgeochemical spectra are very close indeed with the standard deviations overlappingfor almost every major element This could present problems for tephrostratigra-phy where only one of the tephras is evident in a sediment sequence in particularbecause they are so close in age This is a good example of where an analysis oftrace and rare earth elements might be required to make a clear distinction betweentephras with very similar major oxide concentrations
The Y-1 Tephra also termed the Biancavilla Montalto Ignimbrite (Vezzoli 1991)is a product of Etna and has been identishy ed as a visible benmoritic tephra horizonthroughout the central Mediterranean (Paterne et al 1988) including central Italyand the Adriatic Sea (Vezzoli 1991 Narcisi 1993 Calanchi et al 1996) It has anestimated age of ca 140 14C ka BP The Unita dei Tefra Superiori tephra which hasbeen detected as far east as Lago di Monticchio in south-central Italy (Narcisi 1996)is also dated to ca 140 14C ka BP (Alessio et al 1976) but it is thought that thesource of this tephra lies in the Phlegrean Fields No geochemical data are availablefrom the presumed source region|the data reported in table 1 were obtained fromthe Lago di Monticchio record (Narcisi 1996)
The NYT which is equivalent to the C-2 tephra reported from various marinesequences has also been traced throughout central Italy and the Adriatic Sea (Pat-erne et al 1988 Calanchi et al 1996 Di Vito et al 1999) (shy gure 2) In the centralApennines region it formed the parent material for a soil that started to developat the beginning of the Holocene period (Frezzotti amp Narcisi 1996) Also originatingfrom the Campi Flegrei caldera it is dated to ca 120 14C ka BP (Di Vito et al 1999) Published geochemical data based on EDS indicate three dinoterent geochemicalpopulations varying from latite to phonotrachyte in composition (Orsi et al 1992Paterne et al 1988) (table 1) We report in x 4 of this paper on new data obtainedfrom the NYT by WDS and it is the mean of these new data that is included intable 1 Comparisons with the previously published EDS data are provided (table 1)
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786 S M Davies and others
The new data indicate clearly that the NYT originated from the Campanian volcaniccentre
In the interval between the dispersal of the NYT (ca 120 14C ka BP) and 95 14Cka BP there appear to have been as many as 34 eruptions in the Campi Flegrei caldera(Di Vito et al 1999) Of these only one appears to have been detected widely in theregion the Pomici Principali (also termed the Agnano Formation or C-1 tephra inmarine records (Paterne et al 1988) This was the product of the highest magnitudeeruption from this epoch and is dated to between 976 sect 300 and 1032 sect 50 14C kaBP (Delibrias et al 1979 Di Vito et al 1999) or to 122 varve ka BP based on theMonticchio varve chronology (Allen et al 1999) It is trachytic in composition andappears to have had a mainly eastwards dispersal
The Mercato Tephra dated to ca 80 14C ka BP and originally analysed usingEDS has a phonolitic composition and is believed to have been generated by Vesu-vius (Paterne et al 1988) New WDS data obtained from reference samples col-lected from an exposure to the west of Naples support these conclusions (table 1 andAppendix A) The silica content of the WDS analyses are ca 3 lower than thoseobtained using EDS (table 1) which may reregect the fact that the EDS data werenormalized
The only tephra listed in table 1 that is thought to have originated from the AeolianIslands is the Pollara pumice also referred to as the E2 tephra in marine sequences(Paterne et al 1986 1988) The limited geochemical data available so far suggest itto be the only Italian tephra listed in table 1 that is rhyolitic in composition Littlemore is known about this ash which has not been recorded extensively except thatits age is estimated to be ca 130 14C ka BP (Keller 1980)
5 Extending the known distributions of European tephras
Figure 2 summarizes schematically the known distributions of three of the tephrasreferred to in the preceding section the VA the LST and the NYT Following theintroduction of a laboratory method that enables the detection of micro-tephra parti-cles in mineral-rich sediment the VA has been traced to sites that are located muchfarther south (into The Netherlands) and east (as far as St Petersburg) than thedistribution limits based on occurrences of visible layers of the ash As a result con-tinental sequences over a much larger area in northern Europe can now be correlateddirectly with marine and ice-core records using the VA as a time-parallel marker
This suggests therefore that other prominent ash layers such as the LST andNYT should also be detectable over larger tracts of Europe than is presently thecase if suitable sites are examined for the presence of micro-tephra horizons To testthis assertion we examined lake sediment deposits of Last Termination age froma site in the northern Apennines in order to establish whether the NYT could bedetected in micro-tephra form The site selected Prato Spilla `Crsquo lies well to thenorth of the localities in central and southern Italy and in the Adriatic Sea fromwhich visible records of the NYT have been reported Prato Spilla `Crsquo lies at an alti-tude of ca 1350 m in the Appennino Parmense ca 60 km south of Parma and 15 kmeast of Pontremoli The site contains a continuous sediment sequence spanning theLast Termination and most of the Holocene Detailed pollen and coleopteran strati-graphical records which have been radiocarbon dated have been published for thissite (Lowe 1992 Ponel amp Lowe 1992 Lowe amp Watson 1993)
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European tephrochronological framework for Termination 1 787
Figure 6 Light microscope photograph of an NYT glass shard from Prato Spilla Crsquosequence assigned on geochemical grounds to the NYT
The methods adopted for sub-sampling of the Prato Spilla `Crsquo sequence for thequantishy cation of glass shard concentrations and for subsequent electron microprobeanalysis of selected glass shards followed those described elsewhere (Turney 1998)In summary contiguous samples of 1 cm stratigraphic interval were extracted fromthe sequence to establish presenceabsence of glass shards Each of the 1 cm3 blocksin which tephra particles was detected was then examined with more care andshard concentrations were quantishy ed for each sub-sample Micro-tephra particleswere detected in shy ve samples (shy gure 6) but were predominantly clustered around500 cm in the part of the sequence assigned on pollen-stratigraphic grounds to theLate Glacial Interstadial or the `Allerfrac12drsquo|indeed the part of the succession in whichthe NYT would be expected to occur Peak concentrations of micro-tephra particlesreach 225 shards cmiexcl3 and are conshy ned to a single 1 cm thick sample in the sequencewhich probably represents the time of maximum deposition of the ash
Electron microprobe measurements based on WDS were obtained from the surfacesof 21 separate glass shards extracted from the sample with peak shard concentrations(Appendix A) Since only EDS measurements were available for the NYT prior to thepresent study we also obtained WDS measurements from 17 shards extracted fromthe visible layer of NYT that is exposed on Procida Island which lies in the type-locality for the NYT close to the city of Naples (Appendix A) The results providenot only a more comprehensive geochemical dataset for the NYT than was previ-ously available but also a consistent basis for comparison with the Prato Spilla `Crsquodataset All of the WDS data reported here (Appendix A) were measured at the samelaboratory (Tephrochronology Analytical Unit University of Edinburgh) using thesame sample pretreatment and preparation protocol The WDS results for the NYTdinoter to a minor degree from the EDS results (table 1 and Appendix A) especiallywith respect to the amounts of silica aluminium and calcium measured The EDS
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788 S M Davies and others
4 8FeO ()
TiO
2 (
) Neapolitan Yellow Tuff(Procida)Neapolitan Yellow Tuff(Prato Spilla lsquoCrsquo)
0
1
2
3
40 50 60 70
MgO
(
)
SiO2 ()
K2O
(
)
40 50 60 70
0
04
08
4
8
12
SiO2 ()
(a)(b)
(c)
Figure 7 Bi-plots of SiO2 K2 O SiO2 MgO and FeOTiO2 for the WDS analyses obtainedfrom glass shards of the NYT from Procida (Naples) and Prato Spilla Crsquo Means and standarddeviations are shown
results show a higher degree of statistical scatter than the WDS measurements whichmay reregect the fact that the data were normalized combined with the inreguence ofvariation in water content between shards
There is a very close correspondence between the WDS data for the Prato Spilla `Crsquomicro-tephra shards and those obtained from the type-material near Naples (shy g-ure 7) The geochemical data strongly suggest therefore that the NYT is representedat the Prato Spilla `Crsquo site by a discrete layer of micro-tephra particles This conclu-sion is compatible with the pollen-stratigraphic data from the site and accords withage estimates for the NYT (ca 120 14C ka BP) obtained from other sites (Paterneet al 1990)
These results encourage us to believe that many if not all of the tephras listedin table 1 will be detectable over much larger tracts of Europe than is presently thecase if appropriate research is undertaken to detect layers of micro-tephra particlesin selected sites The authors are presently engaged in a major continent-wide pro-gramme of research in collaboration with a number of European research groupsdesigned to test this hypothesis The focus in this research is on those parts of Europewhere we expect to shy nd overlapping `apronsrsquo of tephra deposition originating fromthe Italian Eifel Massif Central and Icelandic provinces For example a number ofsites in parts of southern France northern Italy and perhaps western Switzerlandmay have received inreguxes of micro-tephra originating from the Italian and Eifelprovinces and perhaps also from the Massif Central Sites in parts of Germany Den-mark and southern Sweden for example may in turn have received tephra depositsfrom both of the Icelandic and Eifel provinces If this proves to be the case then thestage will be set for the construction of a tephrostratigraphical framework for Europewhich will enable Last Termination sequences to be correlated on a continent-widebasis using micro- and visible tephra layers as time-parallel stratigraphic markersFurthermore there is also the possibility that other tephras remain to be discovered
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European tephrochronological framework for Termination 1 789
those which either because of the magnitude or nature of some volcanic eruptionswere distributed over parts of Europe in micro-tephra form only
6 European tephrostratigraphy and the chronology of eventsduring the Last Termination and Early Holocene
One of the crucial issues in Late Quaternary palaeoenvironmental research thatremains to be resolved is the degree to which climatic events inferred from oceanicterrestrial and ice-core records were synchronous during the Last Termination andEarly Holocene If the ice-core records provide realistic estimates of the rates anddurations of climatic events during this period then comparisons between individ-ual records have to be enotected with at least a decadal precision The problem thispresents and the role that tephrostratigraphy can play in resolving some of thedimacr culties involved are put into perspective in shy gure 8
Figure 8 shows some of the data used to calibrate radiocarbon dates (the LakeSuigetsu and Cariaco Basin datasets) plotted against the GRIP ss08c ice-core recordof macr 18O variations The latter has been selected by the INTIMATE group as an arbi-trary and temporary standard for this period and used to deshy ne an event stratig-raphy scheme (shy gure 1) for the Last Termination (see Bjorck et al 1998 Walker etal 2001) As has been alluded to in earlier sections of this paper the uncertaintiesassociated with all of the dating methods currently employed preclude precise com-parisons of ice-core marine and terrestrial records Oceanic and terrestrial recordsmostly rely upon radiocarbon dating locally supplemented in a few cases by varvechronology Imprecisions in radiocarbon dates can arise through site-specishy c fac-tors (eg hard-water or mineral carbon errors in freshwater sequences and reservoirerrors in marine sequences) sample selection laboratory measurements of 14C activ-ity and other factors (Lowe amp Walker 2000) Further imprecision may be introducedby the calibration of radiocarbon dates since the uncertainties in the dataset usedto calibrate pre-Holocene radiocarbon dates INTCAL98 are far higher than forthe Holocene which is based on dendro-calibration (Stuiver et al 1998) There arealso uncertainties anotecting varve chronologies while the ss08c ice-core chronologyfor the Last Termination dinoters signishy cantly from the GISP2 record and indeedfrom other models of the GRIP record (Lowe et al 2001) Published comparisonsbetween ice-core marine and terrestrial records for the Last Termination seldom takeinto account the true magnitude of the dating uncertainties involved and frequentlyemploy circular reasoning
Figure 8 shows the positions on the radiocarbon time-scale of 20 of the tephrasdiscussed earlier in this paper these being the ones for which reasonably conshy dentradiocarbon age estimates can be made (though these will be subject to revised esti-mates in the future) A high number of these occur in the period 14080 14C kaBP but we conshy dently anticipate the discovery in the future of additional tephras(perhaps in micro-tephra form only) which will date to the period 185140 14C kaBP Tephras detected in the GRIP ice core over the same time-interval are plottedon the calendar time-scale in shy gure 8 By providing key `time-linesrsquo between recordstephrostratigraphy can help to resolve some of the dating uncertainties referredto earlier by for example enabling direct comparisons of discrepant age estimatesobtained using dinoterent methods (cf Litt et al 2001) It can also provide estimatesof the magnitudes of the reservoir errors that anotected various marine sectors at dif-
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790 S M Davies and others
-44
-40
-36
-32
cale
ndar
yea
rs B
P
8000
9000
10 0
00
11 0
00
12 0
00
13 0
00
14 0
00
15 0
00
16 0
00
17 0
00
18 0
00
14C age (BP)
VA
SA
Un
Un
Un
Un
Un
BF
Hol
ocen
eG
S-1
GI-
1aG
I-1b
GI-
1cG
I-1d
GI-
1eG
S-2
aG
S-2
bG
S-
2c
Bor
robo
l
La
Nug
egravere
Laa
cher
See
God
ivel
le 5
amp I
-TH
OL
-2
Puy
de D
ocircme
I-T
HO
L-1
Saks
unar
vatn
Houmlg
stor
psm
osse
nU
lmen
er M
aar
amp L
3574
radiocarbon dated European tephra horizons
Cho
pine
Kili
an V
asse
tM
erca
to
God
ivel
le 4
Pom
ici P
rinc
ipal
i amp V
edde
Polla
ra p
umic
eK
OL
-GS-
2 amp
GS
-2B
AS-
12
3
GS
-2B
AS-
4 U
nita
dei
Tef
raSu
peri
ori amp
laye
r Y
-1
Gre
enis
h
L9
20 0
0018
000
16 0
0014
000
12 0
0010
000
-44
-40
-36
-32
800
600
400
200 0
GISP2 volcanicsulphate conc (ppb)
1000
Nea
polit
an Y
ello
w T
uff
GISP2 18O (permil) dGRIP 18O (permil) d
Figure 8 For description see opposite
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European tephrochronological framework for Termination 1 791
ferent times through a comparison of radiocarbon dates obtained from marine andterrestrial horizons in which the same tephra has been detected (see for exampleAustin et al 1995 Bondevik et al 2001 Haregidason et al 2000) Tephrostratigraphymay provide an independent test of suggestions that some of the climatic changesduring the Last Termination were time-transgressive as illustrated for some appar-ently contrasting climatic trends in Iceland Britain and NW Russia (Lowe 2001) Ofparticular importance as far as establishing `leadsrsquo and `lagsrsquo in climatic changes isconcerned are the tephra records from the Greenland ice cores The discovery of theVedde and Saksunarvatn ashes in the GRIP record (Gronvold et al 1995) alreadyprovides a basis for making direct comparisons between marine terrestrial and ice-core records It is a matter of some urgency that the incidence of tephra depositsin the Greenland ice cores be more fully explored in the hope that this will lead tothe recognition of additional time-parallel links between the ice-core records on theone hand and oceanic and terrestrial records on the other An investigation of thenew NordGRIP record for this purpose is currently in progress (S M Davies 2002unpublished data)
Finally a fuller and more reshy ned tephrostratigraphical scheme for Europe will alsohave other applications It will provide an important database for those investigatingthe timing and frequency of volcanic eruptions in Europe during the past 20 000 yror so as well as of the geochemical evolution of the dinoterent volcanic centres overthat period A fuller record of the distribution of micro-tephras may also provideinformation on atmospheric circulation patterns during the dispersal and depositionperiods as well as on the nature and altitude of the eruption columns which mayin turn provide inferences about magma viscosity
This paper is a contribution to the INTIMATE project of the INQUA Palaeoclimate Com-mission and the work is supported by a Leverhulme Trust Research project (grant allocationnumber F07537C) entitled Testing hypotheses of rapid climate change using tephrochronol-ogyrsquo SMDrsquo s contribution was completed during possession of a NERC PhD studentship(GT 0499ES162) We are extremely grateful to Dr Peter G Hill for his assistance withthe EPMA analyses at the Tephrochronology Analytical Unit University of Edinburgh We alsothank Dr G Mastrolorenzo (Vesuvius Observatory) and Miss G Swindle for assistance duringthe macreld investigations in Naples Thanks are also expressed to two anonymous reviewers forcomments on an earlier draft
Appendix A
Table 2 shows the major oxide concentrations of NYT glass shards from Procidaand Prato Spilla `Crsquo and of the Mercato Tephra from the Naples area (see x 4 forsite context) All oxides are shown as weight and total iron is expressed as FeO
Figure 8 Radiocarbon calibration curve for Termination 1 and the Early Holocene compared with theGRIP macr 18 O event stratigraphy the GRIP ss08c and GISP2 macr 18 O records (wwwngdcnoaagov) andknown tephra horizons from this period The shaded areas represent the cooler climatic episodes andare labelled with the Greenland stratotype terminology (Bjorck et al 1998) Where radiocarbon agesare reported in table 1 as a range the mean is given here Abbreviations for GRIP horizons are asfollows Un unknown (approximate positions are given (S Johnsen 2001 personal communication))SA Saksunarvatn Ash VA Vedde Ash BF Black Feather Sulphate concentrations from the GISP2record are also shown (Zielinski et al 1996) Open circles denote radiocarbon calibration data fromLake Suigetsu (Kitagawa amp van der Plicht 2000) Filled circles denote radiocarbon calibration data fromCariaco Basin assuming a marine reservoir age of 420 14 C yr (Hughen et al 1998)
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792 S M Davies and others
Tab
le2
Majo
roxi
de
con
cen
trati
on
sof
NY
Tgl
ass
shard
sfr
om
Pro
cida
an
dP
rato
Spil
laC
rsquoan
dof
the
Mer
cato
Tep
hra
from
the
Naple
sare
a(s
eex4
for
site
con
text
)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
roci
da)
1584
204
0177
634
201
106
828
635
197
5969
1W
DS
2598
603
9178
027
101
204
924
244
583
4965
8W
DS
3586
604
5173
631
100
805
924
342
183
0951
9W
DS
4583
903
9177
933
000
906
924
540
486
9958
3W
DS
5605
106
8179
126
901
204
923
243
086
1976
4W
DS
6591
704
5177
332
801
006
425
740
887
8968
0W
DS
7581
804
1178
031
501
107
125
640
086
9956
1W
DS
8589
504
2179
533
701
506
926
740
987
5970
4W
DS
9592
003
9178
135
101
007
026
443
585
7972
7W
DS
10
591
404
2174
631
601
105
723
442
482
6957
0W
DS
11
593
403
6177
131
301
506
726
439
188
5967
6W
DS
12
588
103
8176
128
100
505
525
141
583
4952
1W
DS
13
577
003
8176
533
500
807
228
140
384
8952
0W
DS
14
586
004
7179
735
300
706
827
842
984
6968
5W
DS
15
588
104
2180
629
400
505
924
937
993
0964
5W
DS
16
579
603
9178
536
501
308
228
836
087
1959
9W
DS
17
580
103
9177
631
500
907
327
039
488
9956
6W
DS
mea
n588
104
2177
631
901
006
525
940
686
9962
8
sd
(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(07
8)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 793
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
rato
Spil
laC
rsquo)
1552
105
4177
247
401
914
38
735
578
9951
1W
DS
2557
305
7179
845
701
512
640
136
581
5960
6W
DS
3595
004
4173
724
302
003
117
652
877
8950
7W
DS
4575
704
2179
433
001
406
627
043
083
6953
7W
DS
5599
904
0178
826
401
304
421
841
688
4966
5W
DS
6591
103
8177
826
601
105
022
443
888
8960
2W
DS
7565
304
5180
939
501
410
532
535
791
8962
1W
DS
8597
606
9180
826
501
604
821
546
684
6970
7W
DS
9571
805
6179
939
801
109
932
240
883
6964
7W
DS
10
588
603
7176
527
601
104
721
042
487
7953
3W
DS
11
559
404
9180
544
501
812
339
435
878
6957
2W
DS
12
594
704
0181
328
301
705
522
144
785
6967
9W
DS
13
611
103
7187
016
900
802
419
938
195
9975
8W
DS
14
599
204
4181
128
601
404
620
844
986
6971
6W
DS
15
601
204
4177
328
302
004
722
446
385
5972
1W
DS
16
595
104
5176
428
801
504
722
744
884
3962
8W
DS
17
603
704
1177
825
101
503
520
348
181
2965
3W
DS
18
558
704
5179
647
401
813
139
836
879
0960
7W
DS
19
589
602
8178
830
901
606
622
436
091
8960
5W
DS
20
553
606
3178
647
401
913
840
136
978
0956
6W
DS
21
579
004
0175
739
000
708
328
338
286
7959
9W
DS
mea
n582
804
6179
033
401
507
427
341
484
8962
1
sd
(1
87)
(01
0)
(02
7)
(09
2)
(00
4)
(03
9)
(08
0)
(04
9)
(05
0)
(07
0)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
794 S M Davies and others
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)
1575
202
7194
219
701
101
016
374
766
9951
8W
DS
2575
802
9194
523
902
201
520
273
564
5959
0W
DS
3574
301
4205
219
101
100
416
481
266
1965
2W
DS
4575
500
7206
018
002
000
415
181
669
3968
6W
DS
5580
000
9208
018
601
300
515
883
367
1975
5W
DS
6571
001
0206
016
101
600
515
078
967
1957
2W
DS
7577
501
1201
117
101
500
620
675
655
4950
5W
DS
8573
700
9212
717
101
900
815
187
564
2973
9W
DS
9580
301
3208
715
801
400
824
81
754
1968
1W
DS
10
574
400
6211
18
402
00
516
480
567
8971
6W
DS
11
577
200
7214
212
501
200
829
879
247
962
6W
DS
12
572
200
9211
217
301
501
15
980
465
9966
3W
DS
13
571
800
7210
417
402
201
16
184
467
2971
2W
DS
14
567
300
9208
916
901
400
917
383
262
5959
3W
DS
15
568
600
8205
918
202
101
414
682
666
6960
8W
DS
16
572
501
1211
318
202
01
215
884
364
5970
9W
DS
17
572
901
2212
916
502
101
215
883
667
2973
4W
DS
18
573
01
4211
716
301
801
416
83
365
5970
4W
DS
19
569
201
1207
418
602
101
414
982
964
961
6W
DS
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
3)
(04
2)
(01
3)
(00
1)
(00
2)
(01
)(0
39)
(01
1)
(02
5)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
References
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Di Vito M A Isaia R Orsi G Southon J de Vita S Drsquo Antonio M Pappalardo L ampPiochi M 1999 Volcanism and deformation since 12 000 years at the Campi Flegrei caldera(Italy) J Volcanol Geophys Res 91 221246
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Dugmore A J amp Newton A J 1998 Holocene tephra layers in the Faroe Islands Frodskaparrit46 191204
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Frezzotti M amp Narcisi B 1996 Late Quaternary Tephra derived paleosols in central Italyrsquo scarbonate Apennine range stratigraphical and paleoclimatological implications Quat Int3436 147153
Friedrich M Kromer B Spurk M Hofmann J amp Kaiser K F 1999 Paleoenvironment andradiocarbon calibration as derived from LateglacialEarly Holocene tree-ring chronologiesQuat Int 61 2739
Froggatt P C 1992 Standardisation of the chemical analysis of tephra deposits Report of theICCT working group Quat Int 1314 9396
Gronvold K Oskarsson N Johnsen S J Clausen H B Hammer C U Bond G amp Bard E1995 Ash layers from Iceland in the GRIP ice core correlated with oceanic and land sedimentsEarth Planet Sci Lett 135 149155
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Hadeg idason H Eirpara sup3 ksson J amp van Kreveld S 2000 The tephrochronology of Iceland and theNorth Atlantic region during the Middle and Late Quaternary a review J Quat Sci 15322
Hoek W Z amp Bohncke S J P 2001 Oxygen isotope wiggle matching as a tool for synchronisingice-core and terrestrial records over Termination 1 Quat Sci Rev 20 12511264
Hughen K A Overpeck J T Peterson L C amp Trumbore S 1996 Rapid climate changes inthe tropical Atlantic region during the last deglaciation Nature 380 5153
Hughen K A Overpeck J T amp Lehman J 1998 A new 14 C calibration data set for the LastDeglaciation Radiocarbon 39 483494
Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
Hunt J B amp Hill P G 1996 An inter-laboratory comparison of the electron probe microanalysisof glass geochemistry Quat Int 3436 229241
Hunt J B amp Hill P G 2001 Tephrological implications of beam sizesample size ereg ects inelectron microprobe analysis of glass shards J Quat Sci 16 105117
Hunt J B Fannin N G T Hill P G amp Peacock J D 1995 The tephrochronology andradiocarbon dating of North Atlantic Late Quaternary sediments an example from the StKilda Basin In The tectonics sedimentation and palaeoceanography of the North Atlanticregion (ed R A Scrutton M S Stoker G B Shimmield amp A W Tudhope) vol 90pp 227248 Geological Society of London Special Publication
Hunt J B Clift P D Lacasse C Vallier T L amp Werner R 1998 Standardisation ofelectron probe microanalysis of glass geochemistry In Proc ODP Scientimacrc Results vol 152pp 8591 College Station TX Ocean Drilling Program
Jakobsson S P 1979 Outline of the petrology of Iceland Jokull 29 5773
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Juvignparae E 1993 Contribution microa la tparaephrostratigraphie du Quaternaire et son application microa lagparaeomorphologie Mparaem Serv Explicat Cartes Gparaeol Min Belg 36 166
Juvignparae E amp Gewelt M 1987 La Narse drsquo Ampoix comme tparaephrostratotype dans la Chasup3 ne desPuys mparaeridionale (France) Bull Ass Fr Etud Quat 29 3749
Juvignparae E Kozarski S amp Nowaczyk B 1995 The occurrence of Laacher See Tephra in Pomera-nia NW Poland Boreas 24 225231
Juvignparae E Bastin B Delibrias G Evin J Gewelt M Gilot E amp Streel M 1996 Acomprehensive pollen and tephra based chronostratigraphic model for the Lateglacial andHolocene period in the French Massif Central Quat Int 3436 113120
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Keller J Ryan W B F Ninkovich D amp Altherr R 1978 Explosive volcanic activity in theMediterranean over the past 200 000 years as recorded in deep sea sediments Geol Soc AmBull 89 591604
Kitagawa H amp van der Plicht J 2000 Atmospheric radiocarbon calibration beyond 11 900 calBP from Lake Suigetsu laminated sediments Radiocarbon 42 369380
Kvamme T Mangerud J Furnes H amp Ruddiman W F 1989 Geochemistry of Pleistoceneash zones in cores from the North Atlantic Norsk Geol Tids 69 251272
Lacasse C Sigurdsson H Johannesson H Paterne M amp Carey S 1995 Source of Ash zone 1in the North Atlantic Bull Volcanol 57 1832
Langone L Asioli A Corregiari A amp Trincardi F 1996 Age depth modelling through theLate-Quaternary deposits of the central Adriatic Basin In Palaeoenvironmental analysis ofItalian crater lake and Adriatic sediments (ed F Oldmacreld amp P Guilizzoni) vol 55 pp 177196 Memorie dellrsquo Instituto Italiano di Idrobiologia
Larsen G 2000 Holocene volcanism in Iceland and tephrochronology as a tool in volcanologyIn Iceland 2000 modern processes and past environments Keele University UK
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European tephrochronological framework for Termination 1 799
Litt T amp Stebich M 1999 Bio- and chronostratigraphy of the Lateglacial in the Eifel regionGermany Quat Int 61 516
Litt T Brauer A Goslar T Merkt J Balaga K Muller H Ralska-Jasiewiczowa MStebich M amp Negendank J F W 2001 Correlation and synchronisation of Lateglacialcontinental sequences in northern Central Europe based on annually laminated lacustrinesediments Quat Sci Rev 20 12331249
Long D amp Morton A C 1987 An ash fall within the Loch Lomond stadial J Quat Sci 297101
Lotter A F Eicher U Siegenthaler U amp Birks H J B 1992 Lateglacial climatic oscillationsas recorded in Swiss lake sediments J Quat Sci 7 187204
Lowe J J 1992 Lateglacial and Early Holocene lake sediments from the Northern ApenninesItaly|pollen stratigraphy and radiocarbon dating Boreas 21 193208
Lowe J J 2001 Abrupt climatic changes in Europe during the last glacialinterglacial tran-sition the potential for testing hypotheses on the synchroneity of climatic events usingtephrochronology Global Planet Change 603 7384
Lowe J J amp Turney C S M 1997 Vedde Ash layer discovered in a small lake basin on theScottish mainland J Geol Soc Lond 154 605612
Lowe J J amp Walker M J C 2000 Radiocarbon dating the last glacialinterglacial transition(ca 14914 C ka BP) in terrestrial and marine records the need for new quality assuranceprotocols Radiocarbon 42 5368
Lowe J J amp Watson C 1993 Lateglacial and Early Holocene pollen stratigraphy of the northernApennines Italy Quat Sci Rev 12 727738
Lowe J J Birks H H Brooks S J Coope G R Harkness D D Mayle F E SheldrickC Turney C S M amp Walker M J C 1999 The chronology of palaeoenvironmental changesduring the Last GlacialHolocene transition towards an event stratigraphy for the BritishIsles J Geol Soc Lond 156 397410
Lowe J J Hoek W Z amp INTIMATE group 2001 Inter-regional correlation of palaeoclimaticrecords for the Last GlacialInterglacial transition a protocol for improved precision recom-mended by the INTIMATE project group Quat Sci Rev 20 11751187
Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
Mangerud J Lie S E Furnes H Kristiansen I L amp Liquest mo L 1984 A Younger Dryas ashbed in western Norway and its possible correlation with tephra beds from the Norwegian Seaand North Atlantic Quat Res 21 85104
Mangerud J Furnes H amp Jparaohansen J 1986 A 9000 year-old ash bed on the Faroe IslandsQuat Res 26 262265
Martini J 1970 Recherche de retombparaees volcaniques dans le sud-est de la France et la Suisseoccidentale Arch Sci 23 641674
Martini J amp Duret J J 1965 Note preliminaire sur la presence drsquo un niveau de cendres vol-caniques dans des sparaediments post-glaciaires des environs de Genmicroeve Arch Sci 18 587588
Mayewski P A Meeker L D Twickler M S Whitlow S Yang Q Lyons W B amp Pren-tice M 1997 Major features and forcing of high latitudes Northern Hemisphere atmosphericcirculation using a 110 000 year long glaciochemical series J Geophys Res 102 345365
Merkt J Muller H Knabe W Muller P amp Weiser T 1993 The Early Holocene Saksunarvatntephra found in lake sediments in NW Germany Boreas 22 93100
Narcisi B 1993 Segnalazione di un livello piroclastico di provenienza etnea nellrsquo area del Fucino(Italia Centrale) Quaternario 6 8792
Narcisi B 1996 Tephrochronology of a Late Quaternary lacustrine record from the Monticchiomaar (Vulture volcano southern Italy) Quat Sci Rev 15 155165
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800 S M Davies and others
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Oldmacreld F Appleby P G amp Thompson R 1980 Palaeoecological studies of lakes in theHighlands of Papua New Guinea J Ecol 68 457477
Orsi G Drsquo Antonio M de Vita S amp Gallo G 1992 The Neapolitan Yellow Tureg a large mag-nitude trachytic phreatoplinian eruption eruptive dynamics magma withdrawal and calderacollapse J Volcanol Geotherm Res 53 275287
Paterne M Guichard F Labeyrie J Gillot P Y amp Duplessy J C 1986 Tyrrhenian Seatephrochronology of the oxygen isotope record for the past 60 000 years Mar Geol 72259285
Paterne M Guichard F amp Labeyrie J 1988 Explosive activity of the south Italian volca-noes during the past 80 000 years as determined by marine tephrochronology J VolcanolGeotherm Res 34 153172
Paterne M Labeyrie J Guichard F Mazaud A amp Maitre F 1990 Fluctuations of the Cam-panian explosive volcanic activity (south Italy) during the past 190 000 years as determinedby marine tephrochronology Earth Planet Sci Lett 98 166174
Pawse A Beske-Diehl S amp Marshall S A 1998 Use of magnetic hysteresis properties andelectron spin resonance spectroscopy for the identimacrcation of volcanic ash a preliminary studyGeophys J Int 132 712720
Pearce N J G Westgate J A amp Perkins W T 1996 Developments in the analysis of singleglass shards in volcanic deposits by laser ablation ICP-MS quantitative and single internalstandard multi-element methods Quat Int 3436 213227
Pearce N J G Westgate J A Perkins W T Eastwood W J amp Shane P 1999 Theapplication of laser ablation ICP-MS to the analysis of volcanic glass shards from tephradeposits bulk glass and single shard analysis Global Planet Change 21 151171
Pilcher J R amp Hall V A 1992 Towards a tephrochronology for the Holocene of the north ofIreland Holocene 2 255259
Ponel P amp Lowe J J 1992 Coleopteran pollen and radiocarbon evidence from the Prato Spillarsquo Drsquo succession N Italy C R Acad Sci Paris Sparaer II 315 14251431
Rose N L Golding P N E amp Battarbee R W 1996 Selective concentration and enumerationof tephra shards from lake sediment cores Holocene 6 243246
Ruddiman W F amp Glover L K 1972 Vertical mixing of ice rafted volcanic ash in NorthAtlantic sediments Geol Soc Am Bull 83 28172836
Ruddiman W amp McIntyre A 1981 The North Atlantic Ocean during the last deglaciationPalaeogeogr Palaeoclimatol Palaeoecol 35 145214
Santacroce R 1987 Somma Vesuvius Quad Ric Sci 114 252
Sarna-Wojcicki A 2000 Tephrochronology In Quaternary geochronology methods and applica-tions (ed J S Noller J M Sowers amp W R Lettis) AGU Reference shelf vol 4 pp 357377Washington DC American Geophysical Union
Sejrup H P Sjiquest holm J Furnes H Beyer I Eide L Jansen E amp Mangerud J 1989Quaternary tephrochronology on the Iceland Plateau north of Iceland J Quat Sci 4 109114
Sikes E L Samson C R Guilderson T P amp Howard W R 2000 Old radiocarbon agesin the southwest Pacimacrc Ocean during the last glacial period and deglaciation Nature 405555558
Stein R Nam S-I Grobe H amp Hubbersten H 1996 Late Quaternary glacial history andshort term ice rafted debris deg uctuations along the East Greenland continental marine In LateQuaternary palaeoceanography of the North Atlantic margins (ed J T Andrews W E NAustin H Bergsten amp A E Jennings) pp 135151 Geological Society London SpecialPublication
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Stuiver M amp Grootes P M 2000 GISP2 oxygen isotope ratios Quat Res 53 277284
Stuiver M Reimer P J Bard E Beck J W Burr G S Hughen K A Kromer BMcCormac G Van der Plicht J amp Spurk M 1998 INTCAL 98 radiocarbon age calibration24 0000 cal BP Radiocarbon 40 10411083
Sweatman T R amp Long J V P 1969 Quantitative electron microprobe analysis of rock formingminerals J Petrol 7 332379
Turney C S M 1998 Extraction of rhyolitic ash from minerogenic lake sediments J Paleolim-nol 19 199206
Turney C S M amp Lowe J J 2001 Tephrochronology In Tracking environmental changes inlake sediments physical and chemical techniques (ed W M Last amp J P Smol) DordrechtKluwer Academic
Turney C S M Harkness D D amp Lowe J J 1997 The use of microtephra horizons tocorrelate Lateglacial lake sediments successions in Scotland J Quat Sci 12 525531
Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
van den Bogaard P amp Schmincke H 1985 A widespread isochronous Late Quaternary tephralayer in central and northern Europe Geol Soc Am Bull 96 15541571
van den Bogaard B Dordeg er W Sandgren P amp Schmincke H-U 1994 Correlating theHolocene records Icelandic tephra found in Schleswig-Holstein (northern Germany) Natur-wissenschaften 81 554556
Vernet G amp Raynal J-P 2001 Tephrostratigraphy of the Limagne revisited Implications forLateglacial and Holocene Prehistory In Tephras chronology archaeology (ed E Juvignparae ampJ-P Raynal) pp 111116 Dossiers de lrsquo ArchparaeoLogis no 1 France
Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
Vezzoli L 1991 Tephra layers in Bannock Basin (eastern Mediterranean) Mar Geol 1002134
von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
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Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
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802 S M Davies and others
Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
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778 S M Davies and others
6
4
2
40 50 60 70 80
K2O
(
)
SiO2 ()
Laacher See
Iceland
Veidivoumltn-Dyngjufjoumlll
Katla (basalt)
Grimsvoumltn-Kverkfjoumlll
Hekla
Katla (rhyolitic)
0
Icelandic volcanic centres8
10
Massif Central
Etna
Campanian
Figure 3 Bi-plot of SiO2 and K2 O concentrations in tephras derived from the main Europeanash provinces (modimacred after Mangerud et al 1984) The Campanian Massif Central and Etnaconcentrations are based on the data presented in table 1
(2001) have concluded that small variations in the laboratory procedures employedto determine glass chemistry can lead to misidentishy cation of sources for glass shardsand give an example of shards with a Jan Mayen provenance wrongly attributedto an Icelandic source Clearly there is a need for standardization of laboratoryprocedures and while a number of recommendations have recently been advocated(Froggatt 1992 Hunt amp Hill 1993 Hunt et al 1998) there is still some variation inlaboratory and operator practice (Hunt amp Hill 1996) Standardization is also requiredin the form in which results are presented to ensure comparability Normalizationof the data to 100 a practice employed by some researchers can obscure poorresults and hence lead to incorrect comparisons (Hunt amp Hill 1993) However othersargue that it may actually facilitate comparisons between samples by removing thedistorting enotects of the water component contained in glass shards (see for exampleFroggatt 1992) The majority of the published Italian and some of the Eifel datahave been normalized while those from other parts of Europe have not and hencedata comparisons are not always straightforward
Table 1 provides mean values and standard deviations for major oxide concentra-tions obtained from those tephras for which data are presently available The tableincludes previously unpublished WDS results for the Neapolitan Yellow Tunot (NYTdiscussed in x 4 below) and for the Mercato Tephra While individual tephra layersmay be geochemically distinct the geochemical envelopes representing the collectivedata obtained from all of the tephras assigned to each major volcanic province showsignishy cant overlaps as is illustrated in the bi-plots and ternary plots (shy gures 3 and 4)of selected oxide concentration data It is clear therefore that measurement of majoroxide concentrations does not satisfactorily discriminate between some tephras orig-inating from dinoterent volcanic centres (as noted by van den Bogaard amp Schmincke(1985) and Frezzotti amp Narcisi (1996) with respect to Eifel and Italian tephras)nor of tephras of dinoterent age originating from the same volcanic centre (Bond et
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European tephrochronological framework for Termination 1 779
40 50 60 70 80
K2O
(
)
SiO2 ()
shyshyshyshy
shy
shyshy
shyshyshy
shy
shy
shy
shy
reg
reg regreg
regregregregreg regregregregreg
FF
F
ll
l
l
4 8 12 16
reg
regreg
regreg
regregreg
regreg
regregreg
shy
F
l shyshyshyshyshy shyshyshyshyshyshy
F
F
l
ll
FeO ()
TiO
2 (
)
reg
l
Iceland
Eifel
F
shy ItalyMassif Central
100
80
60
40
20
100
80
60
40
20
100 80 60 40 20
CaO
FeO
K2O
regregreg
reg
reg
reg
reg
reg
reg
regregreg
shyF
F
F
regreg
l
lllshy
shyshyshy
shyshyshy
l
0
2
4
6
8
10
0
1
2
3
4
5
regreg
regreg
regreg
regreg
regreg
reg
reg
regreg
l
l
ll
shy
shyshy
shyshy
shy
shyshy
FF
F
100
80
60
40
20
100
80
60
40
20
100 80 60 40 20
K2ONa2O
CaO
(c) (d)
(a)
(b)
Figure 4 Plots of selected geochemical data obtained from tephras of Termination 1 age (seetable 1) (a) Bi-plot of mean SiO2 and K2 O values (b) Bi-plot of mean FeO and TiO2 values(c) Ternary plot indicating variations in the proportions of FeO CaO and K2 O (d) Ternaryplot indicating variations in the proportion of CaO Na2 O and K2 O
al 2001) Individual tephra layers are presently assigned to a particular volcanicevent on the basis of a combination of criteria usually including examination of thephysical properties (eg refractive index and surface detail of the glass shards) thestratigraphic position of the layer and independent assessment of the age of the layeras well as any geochemical data that may be available The construction of a tephro-stratigraphical scheme would clearly beneshy t from the application of a more diagnostic
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780 S M Davies and others
geochemical tool One approach that has promise is the analysis of trace and rareearth elements using an ultraviolet laser ablation inductively coupled plasma massspectrometer (UV-LA-ICP-MS) (Pearce et al 1996 1999 Eastwood et al 1999)This approach has been applied successfully to analysis of tephras of Mid-Holoceneage but not yet to tephras that fall within the period of interest here
4 Tephra layers in Europe and the North Atlantic regiondated to between 185 and 80 14C ka
(a) Icelandic province
The Icelandic volcanic systems are divided into three main groups based on theirgeochemical characteristics tholeiitic basalts transitional alkali basalts and alkaliolivine basalts (Jakobsson 1979) Collectively magmas from the Icelandic provincespan a wide geochemical spectrum although individual volcanic centres have tightgeochemical distributions (shy gure 3) for four of the main centres Grimsvotn-Kverfjolland Veidvotn-Dyngjufoll which form part of the northern (tholeiitic) volcanic zoneand Hekla and Katla which fall within the eastern (alkali olivine basalt and transi-tional alkali basalt) volcanic zone (Haregidason et al 2000) These appear to be thekey centres for the tephras listed in table 1 that have been assigned an Icelandicorigin
One of the best-known and most widely dispersed tephra horizons in northernEurope that has an Icelandic origin is the Vedde Ash (VA) which was depositedca 103 14C ka BP (Birks et al 1996 Wastegard et al 1998) within the GS-1Younger Dryas chronozone This ash is believed to originate from the Katla complexwithin the transitional alkali basalt province (Mangerud et al 1984 Lacasse et al 1995) in the south of the island The ash has a bimodal geochemical composition (rhy-olitic and basaltic) which is thought to reregect derivation from two separate magmachambers Studies of recent volcanic events in Iceland have shown that the mostexplosive eruptions generating the largest amounts of tephra occur in this tran-sitional alkali basalt province (Haregidason et al 2000) It is also believed that thewidespread distribution of this ash was caused by the development of co-ignimbriteash plumes during an ignimbrite-forming eruption (Lacasse et al 1995)
Layers of VA that are visible to the naked eye have been found in lake sediments inwestern Norway (Mangerud et al 1984) and the Inner Hebrides Scotland (Davies etal 2001) and in marine cores throughout the NE Atlantic (see for example Kvammeet al 1989 Lacasse et al 1995) in the northern North Sea (Long amp Morton 1987)on the Iceland plateau (Ruddiman amp McIntyre 1981 Sejrup et al 1989) and on theeast Greenland continental margin (Stein et al 1996) The distribution of the VAin North Atlantic marine sequences is characterized by an arcuate lobe extendingsouthwest from the Denmark Strait and curving eastwards to mid-latitudes in theNorth Atlantic (Lacasse et al 1995) This strongly suggests deposition from raftedice which was displaced to the southwest and south in a circulating counterclockwisegyre (Ruddiman amp Glover 1972) This may well reregect Katlarsquos close proximity tothe southern coast of Iceland with the Vedde tephra being deposited on ice thatcalved directly into the North Atlantic (Haregidason et al 2000) However depositionvia the atmosphere almost certainly took place as well as is indicated by the recentdiscoveries of rhyolitic VA in micro-tephra form in several sites in Scotland (Turneyet al 1997) southern Sweden (Wastegard et al 1998 2000a) and western Russia
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European tephrochronological framework for Termination 1 781
(Wastegard et al 2000b) A more recent discovery of a relatively high concentrationof rhyolitic VA glass shards in the northern Netherlands indicates that the ash maywell have been dispersed much further south than previously thought (S M Davies2002 unpublished work) Finally glass shards assigned to the VA have also beendiscovered in the GRIP ice core and dated to 11 980 sect 80 GRIP yr BP (Gronvold etal 1995) This discovery is extremely important for it indicates that the VA maywell provide a reliable time-parallel marker horizon between ice-core marine andterrestrial records
Two other important Icelandic ash layers the Borrobol and Saksunarvatn Tephraswere deposited near the beginning and end of the Last TerminationEarly Holoceneinterval respectively The Borrobol Tephra was discovered for the shy rst time in lakesediments in several sites in Scotland and as yet is known only in micro-tephra formIt has been dated in Scottish sites to ca 123 14C ka BP (Turney et al 1997) Whatis thought to be a contemporaneous tephra has been detected in marine sedimentson the North Icelandic shelf (Eirplusmn ksson et al 2000) This certainly has a very similargeochemical composition to those reported from Scotland but the horizon in whichit was discovered on the North Iceland plateau has been dated to 134 14C ka Theage discrepancy between the Scottish and Icelandic Borrobol Tephra layers may wellreregect the inreguence of a marine reservoir error although the possibility that severaltephras with similar geochemical composition were erupted over a period exceeding1000 yr cannot be ruled out (Larsen 2000)
The Saksunarvatn Ash appears to have been one of the largest Holocene eruptionsin Iceland It has a tholeiitic basaltic composition which is considered to indicate anorigin in the Grimsvotn or Kverfjoll complex (shy gure 3) (Mangerud et al 1986) Layersof this ash have been identishy ed in sites on the Faroe Islands (Mangerud et al 1986Dugmore amp Newton 1998 Wastegard et al 2001) the Shetland Isles (Bennet et al 1992) northern Germany (Merkt et al 1993) western Norway (micro-tephra) (Birkset al 1996) and in the GRIP (Gronvold et al 1995) and NordGRIP ice cores (S MDavies 2002 unpublished work) It has been dated to between 9060 and 8930 14C kaBP (Birks et al 1996) in Norway and to ca 10 240 sect 30 GRIP yr BP in the GRIPice core (Gronvold et al 1995) The Saksunarvatn Ash may thus provide a secondimportant widespread time-parallel marker between ice-core marine and terrestrialrecords
Other Icelandic tephras of rhyolitic amacr nity are less well known in terms of theirdistribution and geochemical variation The Hogstorpsmossen Tephra reported fromSweden (Bjorck amp Wastegard 1999) and the L3754 tephra discovered in the FaroeIslands (Dugmore amp Newton 1998) are known from single sites only and so theirpotential for tephrostratigraphy is uncertain at present Furthermore the geochem-ical spectrum of the Hogstorpsmossen Tephra is based on a small dataset with lowanalytical totals
A number of tephras of basaltic composition have originated from Iceland buttheir distributions are largely conshy ned to Iceland or to marine cores collected fromclose to the Iceland coast or in the North Atlantic These include the tephras listedas 1-THOL-1 1-THOL-2 KOL-GS-2 GS-2BAS-1 GS-2BAS-2 GS-2BAS-3 andGS-2BAS-4 in table 1 (Kvamme et al 1989 Bjorck et al 1992 Eirplusmn ksson et al 2000 Haregidason et al 2000) The shy rst two in this list are tholeiitic basaltic tephrasassociated with the VA in a complex series of tephras collectively termed NorthAtlantic Ash Zone 1 (NAAZ1) which has been detected in numerous marine cores
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782 S M Davies and others
from the North Atlantic Initially thought to represent a single eruption analysisof high-resolution sediment sequences from Lake Torfadalsvatn in northern Iceland(Bjorck et al 1992) the Hebridean Shelf near NW Scotland (Austin amp Kroon 1996)the St Kilda Basin (Hunt et al 1995) and the open North Atlantic (Bond et al 2001)has demonstrated that NAAZ1 comprises a series of distinct ashes that probablyreregect separate eruption events 1-THOL-1 is thought to originate from Veidivotn(shy gure 3) while Grimsvotn may have been the source of 1-THOL-2 (Kvamme et al 1989)
KOL-GS-2 is also of tholeiitic basaltic composition but is thought to originatefrom the Kolbeinsey Ridge system (Eirplusmn ksson et al 2000) To date this tephra hasbeen detected in one marine core only within the same record on the North Ice-landic shelf as that from which the correlative of the Borrobol Tephra was alsoreported (Eirplusmn ksson et al 2000) GS-2BAS-1 to GS-2BAS-4 are of uncertain ori-gin but are thought to have been deposited at roughly the same time as KOL-GS-2(ca 134 14C ka BP (Haregidason et al 2000))
The limited distribution of these basaltic tephras a feature that is not unique toIcelandic basaltic material may reregect two factors the relative magnitude of the vol-canic eruptions from which they were derived and the limited aerial transportationof basaltic glass which is denser than rhyolitic material However a rather surpris-ing recent discovery is that of visible basaltic VA in a site on the Isle of Skye inthe Inner Hebrides Scotland (shy gure 5) (Davies et al 2001) All other occurrencesof VA in Scotland are exclusively of rhyolitic material and in micro-tephra formonly (Turney et al 1997 Turney 1998) Clearly basaltic tephra must have beentransported subaerially as far south as Skye and the reason why it has not beendetected at other sites in Scotland is puzzling We suspect that this partly reregectsthe laboratory methods employed to separate glass shards present in low concentra-tion within a micro-tephra layer from the host sediment The technique used is adensity-separation (regotation) procedure (Turney 1998) and as basaltic shards havea specishy c density similar to quartz one of the most abundant minerals in lake sedi-ments of Late Glacial age basaltic material is dimacr cult to detect using this methodThis hypothesis is currently under investigation and alternative detection methodsare being explored including magnetic separation (Mackie et al 2002)
Several other events listed in table 1 that are of probable Icelandic origin includetephras recorded in the GRIP ice core including visible (eg the `Black Featherrsquo)tephras as well as uncertain tephras inferred from distinct Ca peaks (S Johnsen2001 personal communication) No glass shards have yet been detected in the latterbut a volcanic origin is assumed because high Ca peaks are associated with knowntephras in other Greenland ice cores (S Johnsen 2001 personal communication)These are referred to as `unknownrsquo in table 1 No geochemical analyses are availablefrom these horizons so their origin must remain speculative but a possible source isIceland in view of its proximity to the Greenland ice sheet and assumed atmosphericcirculation patterns
(b) Eifel province
There are two prominent tephra events dated to the Termination 1Early Holocenetime-span that originated from the Eifel province the Laacher See Tephra (LST)and the Ulmener Maar Tephra (UMT) Visible occurrences of the LST indicate that
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European tephrochronological framework for Termination 1 783
Vedde Ash
615 625 635 645 655depth (cm)
organic lake mudsHolocene
silty clayGS-1Younger Dryas
organic lake mudsGI-1Alleroslashd
100 microm
(a)
(b)
Figure 5 (a) Photograph of the visible VA layer discovered at Loch Ashik Isle of Skye InnerHebrides Scotland (b) Light microscope photograph showing the rich content of basaltic shards(examples are indicated by the arrows) within this layer (8024 m m size fraction)
this ash was dispersed over much of central Europe (van den Bogaard amp Schmincke1985 Friedrich et al 1999 Litt amp Stebich 1999) The LST is dated by radiocarbonto ca 110 14C ka BP (van den Bogaard amp Schmincke 1985) and to 11 063sect12 14C BP(Friedrich et al 1999) by varve chronology to 1288 varve ka BP (Brauer et al 1999Litt et al 2001) and by ArAr dating to 129 ka cal BP (van den Bogaard 1995) Ithas a phonolitic composition and is thought to have originated from a plinian andphreatomagmatic eruption with the distal ash being carried in three distinct plumesone to the northeast towards Poland one to the west and the third to the southcovering the Jura Mountains and north Italy (van den Bogaard amp Schmincke 1985Juvigne et al 1995 Bossuet et al 1997) This pattern is thought to reregect altitu-dinal variations in the predominant wind direction Sedimentary sequences near thevolcanic source indicate that the LST consists of three main layers which represent
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784 S M Davies and others
dinoterent eruption phases These are grouped together as the Laacher See TephraFormation but the three individual units can be traced within and between a seriesof depositional fans The geochemical data obtained from these three LST layersshow signishy cant variations as reregected in the ternary plots (shy gure 4)
The Early Holocene Ulmener Maar Tephra (UMT) is of rhyolitic composition andappears to be restricted to sites in Germany though this conclusion is also based onrecords of visible tephras only It is dated to ca 956 14C ka BP and to 110 varve ka(Zolitschka et al 1995 Litt et al 2001)
(c) Massif Central province
The Massif Central tephras are mainly of basaltic trachyandesitic compositionwhich is distinct from the other ash provinces (shy gures 3 and 4) and their known dis-tributions are mostly conshy ned to the Massif Central region The ages of the MassifCentral tephras are based on radiocarbon dates obtained from mire and lake sedi-ments which `bracketrsquo the tephras The La Nugsup3ere Tephra with an age of 114 14C kaBP is the oldest Massif Central tephra identishy ed so far within the time-span of inter-est (Etlicher et al 1987 Juvigne et al 1996) The two Godivelle Tephras (5 and 4)are close in age but extensive radiocarbon dating suggests distinct ages of 107and 103 14C ka BP respectively (Juvigne et al 1996) The age of the Puy de DomeTephra is less certain as the estimate is based on only one radiocarbon date froma site in the southern Chaplusmn ne des Puys (table 1) This tephra is thought to havea trachyte composition (Juvigne 1993) although no major element concentrationshave yet been published
The ChopineKilianVasset tephras are thought to be derived from three separateEarly Holocene eruptions although the stratigraphic succession is not known atpresent These trachytic tephras have been radiocarbon dated to ca 854sect150 14C kaBP but are thought to have erupted separately within ca 260 yr (Juvigne et al 1996) This series of tephras is considerably more widespread than the others fromthe region having been identishy ed as far east as the Jura Mountains (Martini amp Duret1965 Martini 1970) Some other ash falls that originated from the Chaplusmn ne des Puysappear to be of local importance only (Vernet et al 1998 Vernet amp Raynal 2001)Geochemical data are currently available for only three of the Massif Central tephrasand so far as is known no attempt has yet been made to identify these tephras inmicro-tephra form
(d ) Italian provinces
The Italian tephras from this period can be assigned to three main volcanic com-plexes the Campanian volcanic shy elds around Naples Etna on Sicily and the AeolianIslands The Campanian complex which includes the Phlegrean Fields Vesuviusand Ischia is mainly trachytic in composition with a geochemical spectrum that isquite distinct from those of the Etna complex and of the Aeolian Islands (shy gure 3)Tephras originating from one or more of these three complexes have been detectedin marine cores from the Tyrrhenian and Adriatic seas as well as other parts of theMediterranean Sea (Keller et al 1978 Paterne et al 1986 1988 1990 Langone etal 1996) and in lake sequences in southern Italy such as Lago Grande di Monticchio(Newton amp Dugmore 1993 Narcisi 1996 Allen et al 1999) and central Italy such asLago Albano near Rome (Calanchi et al 1996) Some work has also been conducted
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European tephrochronological framework for Termination 1 785
in or close to the volcanic source areas in an attempt to establish the full sequenceof volcanic eruptions during the Late Quaternary (see for example Di Vito et al 1999) There are nine Italian tephras reported from marine and lake sequences thatdate from the period between 185 and 80 14C ka BP In all instances the recordsare of visible layers of tephra The ages of some of these are poorly established atpresent with conregicting data obtained from dinoterent sites The ages suggested intable 1 are those favoured in the most recent publications but these may requirere-assessment in the light of future research
The two oldest known tephras in the time-period of interest are the L9 and Green-ish Tephras both recorded as separate features within the annually laminated Lagodi Monticchio maar sequence The lowest of the two L9 is considered to be the cor-relative of the `basalrsquo plinian eruption of Vesuvius (Narcisi 1996) Age estimates ofa palaeosol that underlies the Vesuvius tephra sequence are ca 1617 14C ka BP forthis event (Delibrias et al 1979) L9 has a trachytic composition very similar to theGreenish Tephra (table 1) However L9 which is also a product of Vesuvius is foundstratigraphically below the Greenish Tephra in the Lago di Monticchio core TheGreenish Tephra is dated in the Monticchio sequence to 17 560 varve yr BP (Allenet al 1999) and has a calibrated radiocarbon age estimate of 17 830 sect 300 cal BP(Andronico et al 1995) Both tephras have a dominantly eastwards dispersal basedon the occurrences of visible layers (Santacroce 1987 Narcisi 1996) Both tephrasalso have a trachytic composition and as can be seen from table 1 the reportedgeochemical spectra are very close indeed with the standard deviations overlappingfor almost every major element This could present problems for tephrostratigra-phy where only one of the tephras is evident in a sediment sequence in particularbecause they are so close in age This is a good example of where an analysis oftrace and rare earth elements might be required to make a clear distinction betweentephras with very similar major oxide concentrations
The Y-1 Tephra also termed the Biancavilla Montalto Ignimbrite (Vezzoli 1991)is a product of Etna and has been identishy ed as a visible benmoritic tephra horizonthroughout the central Mediterranean (Paterne et al 1988) including central Italyand the Adriatic Sea (Vezzoli 1991 Narcisi 1993 Calanchi et al 1996) It has anestimated age of ca 140 14C ka BP The Unita dei Tefra Superiori tephra which hasbeen detected as far east as Lago di Monticchio in south-central Italy (Narcisi 1996)is also dated to ca 140 14C ka BP (Alessio et al 1976) but it is thought that thesource of this tephra lies in the Phlegrean Fields No geochemical data are availablefrom the presumed source region|the data reported in table 1 were obtained fromthe Lago di Monticchio record (Narcisi 1996)
The NYT which is equivalent to the C-2 tephra reported from various marinesequences has also been traced throughout central Italy and the Adriatic Sea (Pat-erne et al 1988 Calanchi et al 1996 Di Vito et al 1999) (shy gure 2) In the centralApennines region it formed the parent material for a soil that started to developat the beginning of the Holocene period (Frezzotti amp Narcisi 1996) Also originatingfrom the Campi Flegrei caldera it is dated to ca 120 14C ka BP (Di Vito et al 1999) Published geochemical data based on EDS indicate three dinoterent geochemicalpopulations varying from latite to phonotrachyte in composition (Orsi et al 1992Paterne et al 1988) (table 1) We report in x 4 of this paper on new data obtainedfrom the NYT by WDS and it is the mean of these new data that is included intable 1 Comparisons with the previously published EDS data are provided (table 1)
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786 S M Davies and others
The new data indicate clearly that the NYT originated from the Campanian volcaniccentre
In the interval between the dispersal of the NYT (ca 120 14C ka BP) and 95 14Cka BP there appear to have been as many as 34 eruptions in the Campi Flegrei caldera(Di Vito et al 1999) Of these only one appears to have been detected widely in theregion the Pomici Principali (also termed the Agnano Formation or C-1 tephra inmarine records (Paterne et al 1988) This was the product of the highest magnitudeeruption from this epoch and is dated to between 976 sect 300 and 1032 sect 50 14C kaBP (Delibrias et al 1979 Di Vito et al 1999) or to 122 varve ka BP based on theMonticchio varve chronology (Allen et al 1999) It is trachytic in composition andappears to have had a mainly eastwards dispersal
The Mercato Tephra dated to ca 80 14C ka BP and originally analysed usingEDS has a phonolitic composition and is believed to have been generated by Vesu-vius (Paterne et al 1988) New WDS data obtained from reference samples col-lected from an exposure to the west of Naples support these conclusions (table 1 andAppendix A) The silica content of the WDS analyses are ca 3 lower than thoseobtained using EDS (table 1) which may reregect the fact that the EDS data werenormalized
The only tephra listed in table 1 that is thought to have originated from the AeolianIslands is the Pollara pumice also referred to as the E2 tephra in marine sequences(Paterne et al 1986 1988) The limited geochemical data available so far suggest itto be the only Italian tephra listed in table 1 that is rhyolitic in composition Littlemore is known about this ash which has not been recorded extensively except thatits age is estimated to be ca 130 14C ka BP (Keller 1980)
5 Extending the known distributions of European tephras
Figure 2 summarizes schematically the known distributions of three of the tephrasreferred to in the preceding section the VA the LST and the NYT Following theintroduction of a laboratory method that enables the detection of micro-tephra parti-cles in mineral-rich sediment the VA has been traced to sites that are located muchfarther south (into The Netherlands) and east (as far as St Petersburg) than thedistribution limits based on occurrences of visible layers of the ash As a result con-tinental sequences over a much larger area in northern Europe can now be correlateddirectly with marine and ice-core records using the VA as a time-parallel marker
This suggests therefore that other prominent ash layers such as the LST andNYT should also be detectable over larger tracts of Europe than is presently thecase if suitable sites are examined for the presence of micro-tephra horizons To testthis assertion we examined lake sediment deposits of Last Termination age froma site in the northern Apennines in order to establish whether the NYT could bedetected in micro-tephra form The site selected Prato Spilla `Crsquo lies well to thenorth of the localities in central and southern Italy and in the Adriatic Sea fromwhich visible records of the NYT have been reported Prato Spilla `Crsquo lies at an alti-tude of ca 1350 m in the Appennino Parmense ca 60 km south of Parma and 15 kmeast of Pontremoli The site contains a continuous sediment sequence spanning theLast Termination and most of the Holocene Detailed pollen and coleopteran strati-graphical records which have been radiocarbon dated have been published for thissite (Lowe 1992 Ponel amp Lowe 1992 Lowe amp Watson 1993)
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European tephrochronological framework for Termination 1 787
Figure 6 Light microscope photograph of an NYT glass shard from Prato Spilla Crsquosequence assigned on geochemical grounds to the NYT
The methods adopted for sub-sampling of the Prato Spilla `Crsquo sequence for thequantishy cation of glass shard concentrations and for subsequent electron microprobeanalysis of selected glass shards followed those described elsewhere (Turney 1998)In summary contiguous samples of 1 cm stratigraphic interval were extracted fromthe sequence to establish presenceabsence of glass shards Each of the 1 cm3 blocksin which tephra particles was detected was then examined with more care andshard concentrations were quantishy ed for each sub-sample Micro-tephra particleswere detected in shy ve samples (shy gure 6) but were predominantly clustered around500 cm in the part of the sequence assigned on pollen-stratigraphic grounds to theLate Glacial Interstadial or the `Allerfrac12drsquo|indeed the part of the succession in whichthe NYT would be expected to occur Peak concentrations of micro-tephra particlesreach 225 shards cmiexcl3 and are conshy ned to a single 1 cm thick sample in the sequencewhich probably represents the time of maximum deposition of the ash
Electron microprobe measurements based on WDS were obtained from the surfacesof 21 separate glass shards extracted from the sample with peak shard concentrations(Appendix A) Since only EDS measurements were available for the NYT prior to thepresent study we also obtained WDS measurements from 17 shards extracted fromthe visible layer of NYT that is exposed on Procida Island which lies in the type-locality for the NYT close to the city of Naples (Appendix A) The results providenot only a more comprehensive geochemical dataset for the NYT than was previ-ously available but also a consistent basis for comparison with the Prato Spilla `Crsquodataset All of the WDS data reported here (Appendix A) were measured at the samelaboratory (Tephrochronology Analytical Unit University of Edinburgh) using thesame sample pretreatment and preparation protocol The WDS results for the NYTdinoter to a minor degree from the EDS results (table 1 and Appendix A) especiallywith respect to the amounts of silica aluminium and calcium measured The EDS
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788 S M Davies and others
4 8FeO ()
TiO
2 (
) Neapolitan Yellow Tuff(Procida)Neapolitan Yellow Tuff(Prato Spilla lsquoCrsquo)
0
1
2
3
40 50 60 70
MgO
(
)
SiO2 ()
K2O
(
)
40 50 60 70
0
04
08
4
8
12
SiO2 ()
(a)(b)
(c)
Figure 7 Bi-plots of SiO2 K2 O SiO2 MgO and FeOTiO2 for the WDS analyses obtainedfrom glass shards of the NYT from Procida (Naples) and Prato Spilla Crsquo Means and standarddeviations are shown
results show a higher degree of statistical scatter than the WDS measurements whichmay reregect the fact that the data were normalized combined with the inreguence ofvariation in water content between shards
There is a very close correspondence between the WDS data for the Prato Spilla `Crsquomicro-tephra shards and those obtained from the type-material near Naples (shy g-ure 7) The geochemical data strongly suggest therefore that the NYT is representedat the Prato Spilla `Crsquo site by a discrete layer of micro-tephra particles This conclu-sion is compatible with the pollen-stratigraphic data from the site and accords withage estimates for the NYT (ca 120 14C ka BP) obtained from other sites (Paterneet al 1990)
These results encourage us to believe that many if not all of the tephras listedin table 1 will be detectable over much larger tracts of Europe than is presently thecase if appropriate research is undertaken to detect layers of micro-tephra particlesin selected sites The authors are presently engaged in a major continent-wide pro-gramme of research in collaboration with a number of European research groupsdesigned to test this hypothesis The focus in this research is on those parts of Europewhere we expect to shy nd overlapping `apronsrsquo of tephra deposition originating fromthe Italian Eifel Massif Central and Icelandic provinces For example a number ofsites in parts of southern France northern Italy and perhaps western Switzerlandmay have received inreguxes of micro-tephra originating from the Italian and Eifelprovinces and perhaps also from the Massif Central Sites in parts of Germany Den-mark and southern Sweden for example may in turn have received tephra depositsfrom both of the Icelandic and Eifel provinces If this proves to be the case then thestage will be set for the construction of a tephrostratigraphical framework for Europewhich will enable Last Termination sequences to be correlated on a continent-widebasis using micro- and visible tephra layers as time-parallel stratigraphic markersFurthermore there is also the possibility that other tephras remain to be discovered
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European tephrochronological framework for Termination 1 789
those which either because of the magnitude or nature of some volcanic eruptionswere distributed over parts of Europe in micro-tephra form only
6 European tephrostratigraphy and the chronology of eventsduring the Last Termination and Early Holocene
One of the crucial issues in Late Quaternary palaeoenvironmental research thatremains to be resolved is the degree to which climatic events inferred from oceanicterrestrial and ice-core records were synchronous during the Last Termination andEarly Holocene If the ice-core records provide realistic estimates of the rates anddurations of climatic events during this period then comparisons between individ-ual records have to be enotected with at least a decadal precision The problem thispresents and the role that tephrostratigraphy can play in resolving some of thedimacr culties involved are put into perspective in shy gure 8
Figure 8 shows some of the data used to calibrate radiocarbon dates (the LakeSuigetsu and Cariaco Basin datasets) plotted against the GRIP ss08c ice-core recordof macr 18O variations The latter has been selected by the INTIMATE group as an arbi-trary and temporary standard for this period and used to deshy ne an event stratig-raphy scheme (shy gure 1) for the Last Termination (see Bjorck et al 1998 Walker etal 2001) As has been alluded to in earlier sections of this paper the uncertaintiesassociated with all of the dating methods currently employed preclude precise com-parisons of ice-core marine and terrestrial records Oceanic and terrestrial recordsmostly rely upon radiocarbon dating locally supplemented in a few cases by varvechronology Imprecisions in radiocarbon dates can arise through site-specishy c fac-tors (eg hard-water or mineral carbon errors in freshwater sequences and reservoirerrors in marine sequences) sample selection laboratory measurements of 14C activ-ity and other factors (Lowe amp Walker 2000) Further imprecision may be introducedby the calibration of radiocarbon dates since the uncertainties in the dataset usedto calibrate pre-Holocene radiocarbon dates INTCAL98 are far higher than forthe Holocene which is based on dendro-calibration (Stuiver et al 1998) There arealso uncertainties anotecting varve chronologies while the ss08c ice-core chronologyfor the Last Termination dinoters signishy cantly from the GISP2 record and indeedfrom other models of the GRIP record (Lowe et al 2001) Published comparisonsbetween ice-core marine and terrestrial records for the Last Termination seldom takeinto account the true magnitude of the dating uncertainties involved and frequentlyemploy circular reasoning
Figure 8 shows the positions on the radiocarbon time-scale of 20 of the tephrasdiscussed earlier in this paper these being the ones for which reasonably conshy dentradiocarbon age estimates can be made (though these will be subject to revised esti-mates in the future) A high number of these occur in the period 14080 14C kaBP but we conshy dently anticipate the discovery in the future of additional tephras(perhaps in micro-tephra form only) which will date to the period 185140 14C kaBP Tephras detected in the GRIP ice core over the same time-interval are plottedon the calendar time-scale in shy gure 8 By providing key `time-linesrsquo between recordstephrostratigraphy can help to resolve some of the dating uncertainties referredto earlier by for example enabling direct comparisons of discrepant age estimatesobtained using dinoterent methods (cf Litt et al 2001) It can also provide estimatesof the magnitudes of the reservoir errors that anotected various marine sectors at dif-
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790 S M Davies and others
-44
-40
-36
-32
cale
ndar
yea
rs B
P
8000
9000
10 0
00
11 0
00
12 0
00
13 0
00
14 0
00
15 0
00
16 0
00
17 0
00
18 0
00
14C age (BP)
VA
SA
Un
Un
Un
Un
Un
BF
Hol
ocen
eG
S-1
GI-
1aG
I-1b
GI-
1cG
I-1d
GI-
1eG
S-2
aG
S-2
bG
S-
2c
Bor
robo
l
La
Nug
egravere
Laa
cher
See
God
ivel
le 5
amp I
-TH
OL
-2
Puy
de D
ocircme
I-T
HO
L-1
Saks
unar
vatn
Houmlg
stor
psm
osse
nU
lmen
er M
aar
amp L
3574
radiocarbon dated European tephra horizons
Cho
pine
Kili
an V
asse
tM
erca
to
God
ivel
le 4
Pom
ici P
rinc
ipal
i amp V
edde
Polla
ra p
umic
eK
OL
-GS-
2 amp
GS
-2B
AS-
12
3
GS
-2B
AS-
4 U
nita
dei
Tef
raSu
peri
ori amp
laye
r Y
-1
Gre
enis
h
L9
20 0
0018
000
16 0
0014
000
12 0
0010
000
-44
-40
-36
-32
800
600
400
200 0
GISP2 volcanicsulphate conc (ppb)
1000
Nea
polit
an Y
ello
w T
uff
GISP2 18O (permil) dGRIP 18O (permil) d
Figure 8 For description see opposite
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European tephrochronological framework for Termination 1 791
ferent times through a comparison of radiocarbon dates obtained from marine andterrestrial horizons in which the same tephra has been detected (see for exampleAustin et al 1995 Bondevik et al 2001 Haregidason et al 2000) Tephrostratigraphymay provide an independent test of suggestions that some of the climatic changesduring the Last Termination were time-transgressive as illustrated for some appar-ently contrasting climatic trends in Iceland Britain and NW Russia (Lowe 2001) Ofparticular importance as far as establishing `leadsrsquo and `lagsrsquo in climatic changes isconcerned are the tephra records from the Greenland ice cores The discovery of theVedde and Saksunarvatn ashes in the GRIP record (Gronvold et al 1995) alreadyprovides a basis for making direct comparisons between marine terrestrial and ice-core records It is a matter of some urgency that the incidence of tephra depositsin the Greenland ice cores be more fully explored in the hope that this will lead tothe recognition of additional time-parallel links between the ice-core records on theone hand and oceanic and terrestrial records on the other An investigation of thenew NordGRIP record for this purpose is currently in progress (S M Davies 2002unpublished data)
Finally a fuller and more reshy ned tephrostratigraphical scheme for Europe will alsohave other applications It will provide an important database for those investigatingthe timing and frequency of volcanic eruptions in Europe during the past 20 000 yror so as well as of the geochemical evolution of the dinoterent volcanic centres overthat period A fuller record of the distribution of micro-tephras may also provideinformation on atmospheric circulation patterns during the dispersal and depositionperiods as well as on the nature and altitude of the eruption columns which mayin turn provide inferences about magma viscosity
This paper is a contribution to the INTIMATE project of the INQUA Palaeoclimate Com-mission and the work is supported by a Leverhulme Trust Research project (grant allocationnumber F07537C) entitled Testing hypotheses of rapid climate change using tephrochronol-ogyrsquo SMDrsquo s contribution was completed during possession of a NERC PhD studentship(GT 0499ES162) We are extremely grateful to Dr Peter G Hill for his assistance withthe EPMA analyses at the Tephrochronology Analytical Unit University of Edinburgh We alsothank Dr G Mastrolorenzo (Vesuvius Observatory) and Miss G Swindle for assistance duringthe macreld investigations in Naples Thanks are also expressed to two anonymous reviewers forcomments on an earlier draft
Appendix A
Table 2 shows the major oxide concentrations of NYT glass shards from Procidaand Prato Spilla `Crsquo and of the Mercato Tephra from the Naples area (see x 4 forsite context) All oxides are shown as weight and total iron is expressed as FeO
Figure 8 Radiocarbon calibration curve for Termination 1 and the Early Holocene compared with theGRIP macr 18 O event stratigraphy the GRIP ss08c and GISP2 macr 18 O records (wwwngdcnoaagov) andknown tephra horizons from this period The shaded areas represent the cooler climatic episodes andare labelled with the Greenland stratotype terminology (Bjorck et al 1998) Where radiocarbon agesare reported in table 1 as a range the mean is given here Abbreviations for GRIP horizons are asfollows Un unknown (approximate positions are given (S Johnsen 2001 personal communication))SA Saksunarvatn Ash VA Vedde Ash BF Black Feather Sulphate concentrations from the GISP2record are also shown (Zielinski et al 1996) Open circles denote radiocarbon calibration data fromLake Suigetsu (Kitagawa amp van der Plicht 2000) Filled circles denote radiocarbon calibration data fromCariaco Basin assuming a marine reservoir age of 420 14 C yr (Hughen et al 1998)
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792 S M Davies and others
Tab
le2
Majo
roxi
de
con
cen
trati
on
sof
NY
Tgl
ass
shard
sfr
om
Pro
cida
an
dP
rato
Spil
laC
rsquoan
dof
the
Mer
cato
Tep
hra
from
the
Naple
sare
a(s
eex4
for
site
con
text
)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
roci
da)
1584
204
0177
634
201
106
828
635
197
5969
1W
DS
2598
603
9178
027
101
204
924
244
583
4965
8W
DS
3586
604
5173
631
100
805
924
342
183
0951
9W
DS
4583
903
9177
933
000
906
924
540
486
9958
3W
DS
5605
106
8179
126
901
204
923
243
086
1976
4W
DS
6591
704
5177
332
801
006
425
740
887
8968
0W
DS
7581
804
1178
031
501
107
125
640
086
9956
1W
DS
8589
504
2179
533
701
506
926
740
987
5970
4W
DS
9592
003
9178
135
101
007
026
443
585
7972
7W
DS
10
591
404
2174
631
601
105
723
442
482
6957
0W
DS
11
593
403
6177
131
301
506
726
439
188
5967
6W
DS
12
588
103
8176
128
100
505
525
141
583
4952
1W
DS
13
577
003
8176
533
500
807
228
140
384
8952
0W
DS
14
586
004
7179
735
300
706
827
842
984
6968
5W
DS
15
588
104
2180
629
400
505
924
937
993
0964
5W
DS
16
579
603
9178
536
501
308
228
836
087
1959
9W
DS
17
580
103
9177
631
500
907
327
039
488
9956
6W
DS
mea
n588
104
2177
631
901
006
525
940
686
9962
8
sd
(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(07
8)
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 793
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
rato
Spil
laC
rsquo)
1552
105
4177
247
401
914
38
735
578
9951
1W
DS
2557
305
7179
845
701
512
640
136
581
5960
6W
DS
3595
004
4173
724
302
003
117
652
877
8950
7W
DS
4575
704
2179
433
001
406
627
043
083
6953
7W
DS
5599
904
0178
826
401
304
421
841
688
4966
5W
DS
6591
103
8177
826
601
105
022
443
888
8960
2W
DS
7565
304
5180
939
501
410
532
535
791
8962
1W
DS
8597
606
9180
826
501
604
821
546
684
6970
7W
DS
9571
805
6179
939
801
109
932
240
883
6964
7W
DS
10
588
603
7176
527
601
104
721
042
487
7953
3W
DS
11
559
404
9180
544
501
812
339
435
878
6957
2W
DS
12
594
704
0181
328
301
705
522
144
785
6967
9W
DS
13
611
103
7187
016
900
802
419
938
195
9975
8W
DS
14
599
204
4181
128
601
404
620
844
986
6971
6W
DS
15
601
204
4177
328
302
004
722
446
385
5972
1W
DS
16
595
104
5176
428
801
504
722
744
884
3962
8W
DS
17
603
704
1177
825
101
503
520
348
181
2965
3W
DS
18
558
704
5179
647
401
813
139
836
879
0960
7W
DS
19
589
602
8178
830
901
606
622
436
091
8960
5W
DS
20
553
606
3178
647
401
913
840
136
978
0956
6W
DS
21
579
004
0175
739
000
708
328
338
286
7959
9W
DS
mea
n582
804
6179
033
401
507
427
341
484
8962
1
sd
(1
87)
(01
0)
(02
7)
(09
2)
(00
4)
(03
9)
(08
0)
(04
9)
(05
0)
(07
0)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
794 S M Davies and others
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)
1575
202
7194
219
701
101
016
374
766
9951
8W
DS
2575
802
9194
523
902
201
520
273
564
5959
0W
DS
3574
301
4205
219
101
100
416
481
266
1965
2W
DS
4575
500
7206
018
002
000
415
181
669
3968
6W
DS
5580
000
9208
018
601
300
515
883
367
1975
5W
DS
6571
001
0206
016
101
600
515
078
967
1957
2W
DS
7577
501
1201
117
101
500
620
675
655
4950
5W
DS
8573
700
9212
717
101
900
815
187
564
2973
9W
DS
9580
301
3208
715
801
400
824
81
754
1968
1W
DS
10
574
400
6211
18
402
00
516
480
567
8971
6W
DS
11
577
200
7214
212
501
200
829
879
247
962
6W
DS
12
572
200
9211
217
301
501
15
980
465
9966
3W
DS
13
571
800
7210
417
402
201
16
184
467
2971
2W
DS
14
567
300
9208
916
901
400
917
383
262
5959
3W
DS
15
568
600
8205
918
202
101
414
682
666
6960
8W
DS
16
572
501
1211
318
202
01
215
884
364
5970
9W
DS
17
572
901
2212
916
502
101
215
883
667
2973
4W
DS
18
573
01
4211
716
301
801
416
83
365
5970
4W
DS
19
569
201
1207
418
602
101
414
982
964
961
6W
DS
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
3)
(04
2)
(01
3)
(00
1)
(00
2)
(01
)(0
39)
(01
1)
(02
5)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
References
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Hughen K A Overpeck J T Peterson L C amp Trumbore S 1996 Rapid climate changes inthe tropical Atlantic region during the last deglaciation Nature 380 5153
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Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
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Larsen G 2000 Holocene volcanism in Iceland and tephrochronology as a tool in volcanologyIn Iceland 2000 modern processes and past environments Keele University UK
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Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
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Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 779
40 50 60 70 80
K2O
(
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shyshyshyshy
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shyshyshy
shy
shy
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reg
reg regreg
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shy
F
l shyshyshyshyshy shyshyshyshyshyshy
F
F
l
ll
FeO ()
TiO
2 (
)
reg
l
Iceland
Eifel
F
shy ItalyMassif Central
100
80
60
40
20
100
80
60
40
20
100 80 60 40 20
CaO
FeO
K2O
regregreg
reg
reg
reg
reg
reg
reg
regregreg
shyF
F
F
regreg
l
lllshy
shyshyshy
shyshyshy
l
0
2
4
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0
1
2
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4
5
regreg
regreg
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regreg
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reg
reg
regreg
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shyshy
shyshy
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shyshy
FF
F
100
80
60
40
20
100
80
60
40
20
100 80 60 40 20
K2ONa2O
CaO
(c) (d)
(a)
(b)
Figure 4 Plots of selected geochemical data obtained from tephras of Termination 1 age (seetable 1) (a) Bi-plot of mean SiO2 and K2 O values (b) Bi-plot of mean FeO and TiO2 values(c) Ternary plot indicating variations in the proportions of FeO CaO and K2 O (d) Ternaryplot indicating variations in the proportion of CaO Na2 O and K2 O
al 2001) Individual tephra layers are presently assigned to a particular volcanicevent on the basis of a combination of criteria usually including examination of thephysical properties (eg refractive index and surface detail of the glass shards) thestratigraphic position of the layer and independent assessment of the age of the layeras well as any geochemical data that may be available The construction of a tephro-stratigraphical scheme would clearly beneshy t from the application of a more diagnostic
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780 S M Davies and others
geochemical tool One approach that has promise is the analysis of trace and rareearth elements using an ultraviolet laser ablation inductively coupled plasma massspectrometer (UV-LA-ICP-MS) (Pearce et al 1996 1999 Eastwood et al 1999)This approach has been applied successfully to analysis of tephras of Mid-Holoceneage but not yet to tephras that fall within the period of interest here
4 Tephra layers in Europe and the North Atlantic regiondated to between 185 and 80 14C ka
(a) Icelandic province
The Icelandic volcanic systems are divided into three main groups based on theirgeochemical characteristics tholeiitic basalts transitional alkali basalts and alkaliolivine basalts (Jakobsson 1979) Collectively magmas from the Icelandic provincespan a wide geochemical spectrum although individual volcanic centres have tightgeochemical distributions (shy gure 3) for four of the main centres Grimsvotn-Kverfjolland Veidvotn-Dyngjufoll which form part of the northern (tholeiitic) volcanic zoneand Hekla and Katla which fall within the eastern (alkali olivine basalt and transi-tional alkali basalt) volcanic zone (Haregidason et al 2000) These appear to be thekey centres for the tephras listed in table 1 that have been assigned an Icelandicorigin
One of the best-known and most widely dispersed tephra horizons in northernEurope that has an Icelandic origin is the Vedde Ash (VA) which was depositedca 103 14C ka BP (Birks et al 1996 Wastegard et al 1998) within the GS-1Younger Dryas chronozone This ash is believed to originate from the Katla complexwithin the transitional alkali basalt province (Mangerud et al 1984 Lacasse et al 1995) in the south of the island The ash has a bimodal geochemical composition (rhy-olitic and basaltic) which is thought to reregect derivation from two separate magmachambers Studies of recent volcanic events in Iceland have shown that the mostexplosive eruptions generating the largest amounts of tephra occur in this tran-sitional alkali basalt province (Haregidason et al 2000) It is also believed that thewidespread distribution of this ash was caused by the development of co-ignimbriteash plumes during an ignimbrite-forming eruption (Lacasse et al 1995)
Layers of VA that are visible to the naked eye have been found in lake sediments inwestern Norway (Mangerud et al 1984) and the Inner Hebrides Scotland (Davies etal 2001) and in marine cores throughout the NE Atlantic (see for example Kvammeet al 1989 Lacasse et al 1995) in the northern North Sea (Long amp Morton 1987)on the Iceland plateau (Ruddiman amp McIntyre 1981 Sejrup et al 1989) and on theeast Greenland continental margin (Stein et al 1996) The distribution of the VAin North Atlantic marine sequences is characterized by an arcuate lobe extendingsouthwest from the Denmark Strait and curving eastwards to mid-latitudes in theNorth Atlantic (Lacasse et al 1995) This strongly suggests deposition from raftedice which was displaced to the southwest and south in a circulating counterclockwisegyre (Ruddiman amp Glover 1972) This may well reregect Katlarsquos close proximity tothe southern coast of Iceland with the Vedde tephra being deposited on ice thatcalved directly into the North Atlantic (Haregidason et al 2000) However depositionvia the atmosphere almost certainly took place as well as is indicated by the recentdiscoveries of rhyolitic VA in micro-tephra form in several sites in Scotland (Turneyet al 1997) southern Sweden (Wastegard et al 1998 2000a) and western Russia
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European tephrochronological framework for Termination 1 781
(Wastegard et al 2000b) A more recent discovery of a relatively high concentrationof rhyolitic VA glass shards in the northern Netherlands indicates that the ash maywell have been dispersed much further south than previously thought (S M Davies2002 unpublished work) Finally glass shards assigned to the VA have also beendiscovered in the GRIP ice core and dated to 11 980 sect 80 GRIP yr BP (Gronvold etal 1995) This discovery is extremely important for it indicates that the VA maywell provide a reliable time-parallel marker horizon between ice-core marine andterrestrial records
Two other important Icelandic ash layers the Borrobol and Saksunarvatn Tephraswere deposited near the beginning and end of the Last TerminationEarly Holoceneinterval respectively The Borrobol Tephra was discovered for the shy rst time in lakesediments in several sites in Scotland and as yet is known only in micro-tephra formIt has been dated in Scottish sites to ca 123 14C ka BP (Turney et al 1997) Whatis thought to be a contemporaneous tephra has been detected in marine sedimentson the North Icelandic shelf (Eirplusmn ksson et al 2000) This certainly has a very similargeochemical composition to those reported from Scotland but the horizon in whichit was discovered on the North Iceland plateau has been dated to 134 14C ka Theage discrepancy between the Scottish and Icelandic Borrobol Tephra layers may wellreregect the inreguence of a marine reservoir error although the possibility that severaltephras with similar geochemical composition were erupted over a period exceeding1000 yr cannot be ruled out (Larsen 2000)
The Saksunarvatn Ash appears to have been one of the largest Holocene eruptionsin Iceland It has a tholeiitic basaltic composition which is considered to indicate anorigin in the Grimsvotn or Kverfjoll complex (shy gure 3) (Mangerud et al 1986) Layersof this ash have been identishy ed in sites on the Faroe Islands (Mangerud et al 1986Dugmore amp Newton 1998 Wastegard et al 2001) the Shetland Isles (Bennet et al 1992) northern Germany (Merkt et al 1993) western Norway (micro-tephra) (Birkset al 1996) and in the GRIP (Gronvold et al 1995) and NordGRIP ice cores (S MDavies 2002 unpublished work) It has been dated to between 9060 and 8930 14C kaBP (Birks et al 1996) in Norway and to ca 10 240 sect 30 GRIP yr BP in the GRIPice core (Gronvold et al 1995) The Saksunarvatn Ash may thus provide a secondimportant widespread time-parallel marker between ice-core marine and terrestrialrecords
Other Icelandic tephras of rhyolitic amacr nity are less well known in terms of theirdistribution and geochemical variation The Hogstorpsmossen Tephra reported fromSweden (Bjorck amp Wastegard 1999) and the L3754 tephra discovered in the FaroeIslands (Dugmore amp Newton 1998) are known from single sites only and so theirpotential for tephrostratigraphy is uncertain at present Furthermore the geochem-ical spectrum of the Hogstorpsmossen Tephra is based on a small dataset with lowanalytical totals
A number of tephras of basaltic composition have originated from Iceland buttheir distributions are largely conshy ned to Iceland or to marine cores collected fromclose to the Iceland coast or in the North Atlantic These include the tephras listedas 1-THOL-1 1-THOL-2 KOL-GS-2 GS-2BAS-1 GS-2BAS-2 GS-2BAS-3 andGS-2BAS-4 in table 1 (Kvamme et al 1989 Bjorck et al 1992 Eirplusmn ksson et al 2000 Haregidason et al 2000) The shy rst two in this list are tholeiitic basaltic tephrasassociated with the VA in a complex series of tephras collectively termed NorthAtlantic Ash Zone 1 (NAAZ1) which has been detected in numerous marine cores
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782 S M Davies and others
from the North Atlantic Initially thought to represent a single eruption analysisof high-resolution sediment sequences from Lake Torfadalsvatn in northern Iceland(Bjorck et al 1992) the Hebridean Shelf near NW Scotland (Austin amp Kroon 1996)the St Kilda Basin (Hunt et al 1995) and the open North Atlantic (Bond et al 2001)has demonstrated that NAAZ1 comprises a series of distinct ashes that probablyreregect separate eruption events 1-THOL-1 is thought to originate from Veidivotn(shy gure 3) while Grimsvotn may have been the source of 1-THOL-2 (Kvamme et al 1989)
KOL-GS-2 is also of tholeiitic basaltic composition but is thought to originatefrom the Kolbeinsey Ridge system (Eirplusmn ksson et al 2000) To date this tephra hasbeen detected in one marine core only within the same record on the North Ice-landic shelf as that from which the correlative of the Borrobol Tephra was alsoreported (Eirplusmn ksson et al 2000) GS-2BAS-1 to GS-2BAS-4 are of uncertain ori-gin but are thought to have been deposited at roughly the same time as KOL-GS-2(ca 134 14C ka BP (Haregidason et al 2000))
The limited distribution of these basaltic tephras a feature that is not unique toIcelandic basaltic material may reregect two factors the relative magnitude of the vol-canic eruptions from which they were derived and the limited aerial transportationof basaltic glass which is denser than rhyolitic material However a rather surpris-ing recent discovery is that of visible basaltic VA in a site on the Isle of Skye inthe Inner Hebrides Scotland (shy gure 5) (Davies et al 2001) All other occurrencesof VA in Scotland are exclusively of rhyolitic material and in micro-tephra formonly (Turney et al 1997 Turney 1998) Clearly basaltic tephra must have beentransported subaerially as far south as Skye and the reason why it has not beendetected at other sites in Scotland is puzzling We suspect that this partly reregectsthe laboratory methods employed to separate glass shards present in low concentra-tion within a micro-tephra layer from the host sediment The technique used is adensity-separation (regotation) procedure (Turney 1998) and as basaltic shards havea specishy c density similar to quartz one of the most abundant minerals in lake sedi-ments of Late Glacial age basaltic material is dimacr cult to detect using this methodThis hypothesis is currently under investigation and alternative detection methodsare being explored including magnetic separation (Mackie et al 2002)
Several other events listed in table 1 that are of probable Icelandic origin includetephras recorded in the GRIP ice core including visible (eg the `Black Featherrsquo)tephras as well as uncertain tephras inferred from distinct Ca peaks (S Johnsen2001 personal communication) No glass shards have yet been detected in the latterbut a volcanic origin is assumed because high Ca peaks are associated with knowntephras in other Greenland ice cores (S Johnsen 2001 personal communication)These are referred to as `unknownrsquo in table 1 No geochemical analyses are availablefrom these horizons so their origin must remain speculative but a possible source isIceland in view of its proximity to the Greenland ice sheet and assumed atmosphericcirculation patterns
(b) Eifel province
There are two prominent tephra events dated to the Termination 1Early Holocenetime-span that originated from the Eifel province the Laacher See Tephra (LST)and the Ulmener Maar Tephra (UMT) Visible occurrences of the LST indicate that
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European tephrochronological framework for Termination 1 783
Vedde Ash
615 625 635 645 655depth (cm)
organic lake mudsHolocene
silty clayGS-1Younger Dryas
organic lake mudsGI-1Alleroslashd
100 microm
(a)
(b)
Figure 5 (a) Photograph of the visible VA layer discovered at Loch Ashik Isle of Skye InnerHebrides Scotland (b) Light microscope photograph showing the rich content of basaltic shards(examples are indicated by the arrows) within this layer (8024 m m size fraction)
this ash was dispersed over much of central Europe (van den Bogaard amp Schmincke1985 Friedrich et al 1999 Litt amp Stebich 1999) The LST is dated by radiocarbonto ca 110 14C ka BP (van den Bogaard amp Schmincke 1985) and to 11 063sect12 14C BP(Friedrich et al 1999) by varve chronology to 1288 varve ka BP (Brauer et al 1999Litt et al 2001) and by ArAr dating to 129 ka cal BP (van den Bogaard 1995) Ithas a phonolitic composition and is thought to have originated from a plinian andphreatomagmatic eruption with the distal ash being carried in three distinct plumesone to the northeast towards Poland one to the west and the third to the southcovering the Jura Mountains and north Italy (van den Bogaard amp Schmincke 1985Juvigne et al 1995 Bossuet et al 1997) This pattern is thought to reregect altitu-dinal variations in the predominant wind direction Sedimentary sequences near thevolcanic source indicate that the LST consists of three main layers which represent
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784 S M Davies and others
dinoterent eruption phases These are grouped together as the Laacher See TephraFormation but the three individual units can be traced within and between a seriesof depositional fans The geochemical data obtained from these three LST layersshow signishy cant variations as reregected in the ternary plots (shy gure 4)
The Early Holocene Ulmener Maar Tephra (UMT) is of rhyolitic composition andappears to be restricted to sites in Germany though this conclusion is also based onrecords of visible tephras only It is dated to ca 956 14C ka BP and to 110 varve ka(Zolitschka et al 1995 Litt et al 2001)
(c) Massif Central province
The Massif Central tephras are mainly of basaltic trachyandesitic compositionwhich is distinct from the other ash provinces (shy gures 3 and 4) and their known dis-tributions are mostly conshy ned to the Massif Central region The ages of the MassifCentral tephras are based on radiocarbon dates obtained from mire and lake sedi-ments which `bracketrsquo the tephras The La Nugsup3ere Tephra with an age of 114 14C kaBP is the oldest Massif Central tephra identishy ed so far within the time-span of inter-est (Etlicher et al 1987 Juvigne et al 1996) The two Godivelle Tephras (5 and 4)are close in age but extensive radiocarbon dating suggests distinct ages of 107and 103 14C ka BP respectively (Juvigne et al 1996) The age of the Puy de DomeTephra is less certain as the estimate is based on only one radiocarbon date froma site in the southern Chaplusmn ne des Puys (table 1) This tephra is thought to havea trachyte composition (Juvigne 1993) although no major element concentrationshave yet been published
The ChopineKilianVasset tephras are thought to be derived from three separateEarly Holocene eruptions although the stratigraphic succession is not known atpresent These trachytic tephras have been radiocarbon dated to ca 854sect150 14C kaBP but are thought to have erupted separately within ca 260 yr (Juvigne et al 1996) This series of tephras is considerably more widespread than the others fromthe region having been identishy ed as far east as the Jura Mountains (Martini amp Duret1965 Martini 1970) Some other ash falls that originated from the Chaplusmn ne des Puysappear to be of local importance only (Vernet et al 1998 Vernet amp Raynal 2001)Geochemical data are currently available for only three of the Massif Central tephrasand so far as is known no attempt has yet been made to identify these tephras inmicro-tephra form
(d ) Italian provinces
The Italian tephras from this period can be assigned to three main volcanic com-plexes the Campanian volcanic shy elds around Naples Etna on Sicily and the AeolianIslands The Campanian complex which includes the Phlegrean Fields Vesuviusand Ischia is mainly trachytic in composition with a geochemical spectrum that isquite distinct from those of the Etna complex and of the Aeolian Islands (shy gure 3)Tephras originating from one or more of these three complexes have been detectedin marine cores from the Tyrrhenian and Adriatic seas as well as other parts of theMediterranean Sea (Keller et al 1978 Paterne et al 1986 1988 1990 Langone etal 1996) and in lake sequences in southern Italy such as Lago Grande di Monticchio(Newton amp Dugmore 1993 Narcisi 1996 Allen et al 1999) and central Italy such asLago Albano near Rome (Calanchi et al 1996) Some work has also been conducted
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European tephrochronological framework for Termination 1 785
in or close to the volcanic source areas in an attempt to establish the full sequenceof volcanic eruptions during the Late Quaternary (see for example Di Vito et al 1999) There are nine Italian tephras reported from marine and lake sequences thatdate from the period between 185 and 80 14C ka BP In all instances the recordsare of visible layers of tephra The ages of some of these are poorly established atpresent with conregicting data obtained from dinoterent sites The ages suggested intable 1 are those favoured in the most recent publications but these may requirere-assessment in the light of future research
The two oldest known tephras in the time-period of interest are the L9 and Green-ish Tephras both recorded as separate features within the annually laminated Lagodi Monticchio maar sequence The lowest of the two L9 is considered to be the cor-relative of the `basalrsquo plinian eruption of Vesuvius (Narcisi 1996) Age estimates ofa palaeosol that underlies the Vesuvius tephra sequence are ca 1617 14C ka BP forthis event (Delibrias et al 1979) L9 has a trachytic composition very similar to theGreenish Tephra (table 1) However L9 which is also a product of Vesuvius is foundstratigraphically below the Greenish Tephra in the Lago di Monticchio core TheGreenish Tephra is dated in the Monticchio sequence to 17 560 varve yr BP (Allenet al 1999) and has a calibrated radiocarbon age estimate of 17 830 sect 300 cal BP(Andronico et al 1995) Both tephras have a dominantly eastwards dispersal basedon the occurrences of visible layers (Santacroce 1987 Narcisi 1996) Both tephrasalso have a trachytic composition and as can be seen from table 1 the reportedgeochemical spectra are very close indeed with the standard deviations overlappingfor almost every major element This could present problems for tephrostratigra-phy where only one of the tephras is evident in a sediment sequence in particularbecause they are so close in age This is a good example of where an analysis oftrace and rare earth elements might be required to make a clear distinction betweentephras with very similar major oxide concentrations
The Y-1 Tephra also termed the Biancavilla Montalto Ignimbrite (Vezzoli 1991)is a product of Etna and has been identishy ed as a visible benmoritic tephra horizonthroughout the central Mediterranean (Paterne et al 1988) including central Italyand the Adriatic Sea (Vezzoli 1991 Narcisi 1993 Calanchi et al 1996) It has anestimated age of ca 140 14C ka BP The Unita dei Tefra Superiori tephra which hasbeen detected as far east as Lago di Monticchio in south-central Italy (Narcisi 1996)is also dated to ca 140 14C ka BP (Alessio et al 1976) but it is thought that thesource of this tephra lies in the Phlegrean Fields No geochemical data are availablefrom the presumed source region|the data reported in table 1 were obtained fromthe Lago di Monticchio record (Narcisi 1996)
The NYT which is equivalent to the C-2 tephra reported from various marinesequences has also been traced throughout central Italy and the Adriatic Sea (Pat-erne et al 1988 Calanchi et al 1996 Di Vito et al 1999) (shy gure 2) In the centralApennines region it formed the parent material for a soil that started to developat the beginning of the Holocene period (Frezzotti amp Narcisi 1996) Also originatingfrom the Campi Flegrei caldera it is dated to ca 120 14C ka BP (Di Vito et al 1999) Published geochemical data based on EDS indicate three dinoterent geochemicalpopulations varying from latite to phonotrachyte in composition (Orsi et al 1992Paterne et al 1988) (table 1) We report in x 4 of this paper on new data obtainedfrom the NYT by WDS and it is the mean of these new data that is included intable 1 Comparisons with the previously published EDS data are provided (table 1)
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786 S M Davies and others
The new data indicate clearly that the NYT originated from the Campanian volcaniccentre
In the interval between the dispersal of the NYT (ca 120 14C ka BP) and 95 14Cka BP there appear to have been as many as 34 eruptions in the Campi Flegrei caldera(Di Vito et al 1999) Of these only one appears to have been detected widely in theregion the Pomici Principali (also termed the Agnano Formation or C-1 tephra inmarine records (Paterne et al 1988) This was the product of the highest magnitudeeruption from this epoch and is dated to between 976 sect 300 and 1032 sect 50 14C kaBP (Delibrias et al 1979 Di Vito et al 1999) or to 122 varve ka BP based on theMonticchio varve chronology (Allen et al 1999) It is trachytic in composition andappears to have had a mainly eastwards dispersal
The Mercato Tephra dated to ca 80 14C ka BP and originally analysed usingEDS has a phonolitic composition and is believed to have been generated by Vesu-vius (Paterne et al 1988) New WDS data obtained from reference samples col-lected from an exposure to the west of Naples support these conclusions (table 1 andAppendix A) The silica content of the WDS analyses are ca 3 lower than thoseobtained using EDS (table 1) which may reregect the fact that the EDS data werenormalized
The only tephra listed in table 1 that is thought to have originated from the AeolianIslands is the Pollara pumice also referred to as the E2 tephra in marine sequences(Paterne et al 1986 1988) The limited geochemical data available so far suggest itto be the only Italian tephra listed in table 1 that is rhyolitic in composition Littlemore is known about this ash which has not been recorded extensively except thatits age is estimated to be ca 130 14C ka BP (Keller 1980)
5 Extending the known distributions of European tephras
Figure 2 summarizes schematically the known distributions of three of the tephrasreferred to in the preceding section the VA the LST and the NYT Following theintroduction of a laboratory method that enables the detection of micro-tephra parti-cles in mineral-rich sediment the VA has been traced to sites that are located muchfarther south (into The Netherlands) and east (as far as St Petersburg) than thedistribution limits based on occurrences of visible layers of the ash As a result con-tinental sequences over a much larger area in northern Europe can now be correlateddirectly with marine and ice-core records using the VA as a time-parallel marker
This suggests therefore that other prominent ash layers such as the LST andNYT should also be detectable over larger tracts of Europe than is presently thecase if suitable sites are examined for the presence of micro-tephra horizons To testthis assertion we examined lake sediment deposits of Last Termination age froma site in the northern Apennines in order to establish whether the NYT could bedetected in micro-tephra form The site selected Prato Spilla `Crsquo lies well to thenorth of the localities in central and southern Italy and in the Adriatic Sea fromwhich visible records of the NYT have been reported Prato Spilla `Crsquo lies at an alti-tude of ca 1350 m in the Appennino Parmense ca 60 km south of Parma and 15 kmeast of Pontremoli The site contains a continuous sediment sequence spanning theLast Termination and most of the Holocene Detailed pollen and coleopteran strati-graphical records which have been radiocarbon dated have been published for thissite (Lowe 1992 Ponel amp Lowe 1992 Lowe amp Watson 1993)
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European tephrochronological framework for Termination 1 787
Figure 6 Light microscope photograph of an NYT glass shard from Prato Spilla Crsquosequence assigned on geochemical grounds to the NYT
The methods adopted for sub-sampling of the Prato Spilla `Crsquo sequence for thequantishy cation of glass shard concentrations and for subsequent electron microprobeanalysis of selected glass shards followed those described elsewhere (Turney 1998)In summary contiguous samples of 1 cm stratigraphic interval were extracted fromthe sequence to establish presenceabsence of glass shards Each of the 1 cm3 blocksin which tephra particles was detected was then examined with more care andshard concentrations were quantishy ed for each sub-sample Micro-tephra particleswere detected in shy ve samples (shy gure 6) but were predominantly clustered around500 cm in the part of the sequence assigned on pollen-stratigraphic grounds to theLate Glacial Interstadial or the `Allerfrac12drsquo|indeed the part of the succession in whichthe NYT would be expected to occur Peak concentrations of micro-tephra particlesreach 225 shards cmiexcl3 and are conshy ned to a single 1 cm thick sample in the sequencewhich probably represents the time of maximum deposition of the ash
Electron microprobe measurements based on WDS were obtained from the surfacesof 21 separate glass shards extracted from the sample with peak shard concentrations(Appendix A) Since only EDS measurements were available for the NYT prior to thepresent study we also obtained WDS measurements from 17 shards extracted fromthe visible layer of NYT that is exposed on Procida Island which lies in the type-locality for the NYT close to the city of Naples (Appendix A) The results providenot only a more comprehensive geochemical dataset for the NYT than was previ-ously available but also a consistent basis for comparison with the Prato Spilla `Crsquodataset All of the WDS data reported here (Appendix A) were measured at the samelaboratory (Tephrochronology Analytical Unit University of Edinburgh) using thesame sample pretreatment and preparation protocol The WDS results for the NYTdinoter to a minor degree from the EDS results (table 1 and Appendix A) especiallywith respect to the amounts of silica aluminium and calcium measured The EDS
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788 S M Davies and others
4 8FeO ()
TiO
2 (
) Neapolitan Yellow Tuff(Procida)Neapolitan Yellow Tuff(Prato Spilla lsquoCrsquo)
0
1
2
3
40 50 60 70
MgO
(
)
SiO2 ()
K2O
(
)
40 50 60 70
0
04
08
4
8
12
SiO2 ()
(a)(b)
(c)
Figure 7 Bi-plots of SiO2 K2 O SiO2 MgO and FeOTiO2 for the WDS analyses obtainedfrom glass shards of the NYT from Procida (Naples) and Prato Spilla Crsquo Means and standarddeviations are shown
results show a higher degree of statistical scatter than the WDS measurements whichmay reregect the fact that the data were normalized combined with the inreguence ofvariation in water content between shards
There is a very close correspondence between the WDS data for the Prato Spilla `Crsquomicro-tephra shards and those obtained from the type-material near Naples (shy g-ure 7) The geochemical data strongly suggest therefore that the NYT is representedat the Prato Spilla `Crsquo site by a discrete layer of micro-tephra particles This conclu-sion is compatible with the pollen-stratigraphic data from the site and accords withage estimates for the NYT (ca 120 14C ka BP) obtained from other sites (Paterneet al 1990)
These results encourage us to believe that many if not all of the tephras listedin table 1 will be detectable over much larger tracts of Europe than is presently thecase if appropriate research is undertaken to detect layers of micro-tephra particlesin selected sites The authors are presently engaged in a major continent-wide pro-gramme of research in collaboration with a number of European research groupsdesigned to test this hypothesis The focus in this research is on those parts of Europewhere we expect to shy nd overlapping `apronsrsquo of tephra deposition originating fromthe Italian Eifel Massif Central and Icelandic provinces For example a number ofsites in parts of southern France northern Italy and perhaps western Switzerlandmay have received inreguxes of micro-tephra originating from the Italian and Eifelprovinces and perhaps also from the Massif Central Sites in parts of Germany Den-mark and southern Sweden for example may in turn have received tephra depositsfrom both of the Icelandic and Eifel provinces If this proves to be the case then thestage will be set for the construction of a tephrostratigraphical framework for Europewhich will enable Last Termination sequences to be correlated on a continent-widebasis using micro- and visible tephra layers as time-parallel stratigraphic markersFurthermore there is also the possibility that other tephras remain to be discovered
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European tephrochronological framework for Termination 1 789
those which either because of the magnitude or nature of some volcanic eruptionswere distributed over parts of Europe in micro-tephra form only
6 European tephrostratigraphy and the chronology of eventsduring the Last Termination and Early Holocene
One of the crucial issues in Late Quaternary palaeoenvironmental research thatremains to be resolved is the degree to which climatic events inferred from oceanicterrestrial and ice-core records were synchronous during the Last Termination andEarly Holocene If the ice-core records provide realistic estimates of the rates anddurations of climatic events during this period then comparisons between individ-ual records have to be enotected with at least a decadal precision The problem thispresents and the role that tephrostratigraphy can play in resolving some of thedimacr culties involved are put into perspective in shy gure 8
Figure 8 shows some of the data used to calibrate radiocarbon dates (the LakeSuigetsu and Cariaco Basin datasets) plotted against the GRIP ss08c ice-core recordof macr 18O variations The latter has been selected by the INTIMATE group as an arbi-trary and temporary standard for this period and used to deshy ne an event stratig-raphy scheme (shy gure 1) for the Last Termination (see Bjorck et al 1998 Walker etal 2001) As has been alluded to in earlier sections of this paper the uncertaintiesassociated with all of the dating methods currently employed preclude precise com-parisons of ice-core marine and terrestrial records Oceanic and terrestrial recordsmostly rely upon radiocarbon dating locally supplemented in a few cases by varvechronology Imprecisions in radiocarbon dates can arise through site-specishy c fac-tors (eg hard-water or mineral carbon errors in freshwater sequences and reservoirerrors in marine sequences) sample selection laboratory measurements of 14C activ-ity and other factors (Lowe amp Walker 2000) Further imprecision may be introducedby the calibration of radiocarbon dates since the uncertainties in the dataset usedto calibrate pre-Holocene radiocarbon dates INTCAL98 are far higher than forthe Holocene which is based on dendro-calibration (Stuiver et al 1998) There arealso uncertainties anotecting varve chronologies while the ss08c ice-core chronologyfor the Last Termination dinoters signishy cantly from the GISP2 record and indeedfrom other models of the GRIP record (Lowe et al 2001) Published comparisonsbetween ice-core marine and terrestrial records for the Last Termination seldom takeinto account the true magnitude of the dating uncertainties involved and frequentlyemploy circular reasoning
Figure 8 shows the positions on the radiocarbon time-scale of 20 of the tephrasdiscussed earlier in this paper these being the ones for which reasonably conshy dentradiocarbon age estimates can be made (though these will be subject to revised esti-mates in the future) A high number of these occur in the period 14080 14C kaBP but we conshy dently anticipate the discovery in the future of additional tephras(perhaps in micro-tephra form only) which will date to the period 185140 14C kaBP Tephras detected in the GRIP ice core over the same time-interval are plottedon the calendar time-scale in shy gure 8 By providing key `time-linesrsquo between recordstephrostratigraphy can help to resolve some of the dating uncertainties referredto earlier by for example enabling direct comparisons of discrepant age estimatesobtained using dinoterent methods (cf Litt et al 2001) It can also provide estimatesof the magnitudes of the reservoir errors that anotected various marine sectors at dif-
Phil Trans R Soc Lond A (2002)
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790 S M Davies and others
-44
-40
-36
-32
cale
ndar
yea
rs B
P
8000
9000
10 0
00
11 0
00
12 0
00
13 0
00
14 0
00
15 0
00
16 0
00
17 0
00
18 0
00
14C age (BP)
VA
SA
Un
Un
Un
Un
Un
BF
Hol
ocen
eG
S-1
GI-
1aG
I-1b
GI-
1cG
I-1d
GI-
1eG
S-2
aG
S-2
bG
S-
2c
Bor
robo
l
La
Nug
egravere
Laa
cher
See
God
ivel
le 5
amp I
-TH
OL
-2
Puy
de D
ocircme
I-T
HO
L-1
Saks
unar
vatn
Houmlg
stor
psm
osse
nU
lmen
er M
aar
amp L
3574
radiocarbon dated European tephra horizons
Cho
pine
Kili
an V
asse
tM
erca
to
God
ivel
le 4
Pom
ici P
rinc
ipal
i amp V
edde
Polla
ra p
umic
eK
OL
-GS-
2 amp
GS
-2B
AS-
12
3
GS
-2B
AS-
4 U
nita
dei
Tef
raSu
peri
ori amp
laye
r Y
-1
Gre
enis
h
L9
20 0
0018
000
16 0
0014
000
12 0
0010
000
-44
-40
-36
-32
800
600
400
200 0
GISP2 volcanicsulphate conc (ppb)
1000
Nea
polit
an Y
ello
w T
uff
GISP2 18O (permil) dGRIP 18O (permil) d
Figure 8 For description see opposite
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 791
ferent times through a comparison of radiocarbon dates obtained from marine andterrestrial horizons in which the same tephra has been detected (see for exampleAustin et al 1995 Bondevik et al 2001 Haregidason et al 2000) Tephrostratigraphymay provide an independent test of suggestions that some of the climatic changesduring the Last Termination were time-transgressive as illustrated for some appar-ently contrasting climatic trends in Iceland Britain and NW Russia (Lowe 2001) Ofparticular importance as far as establishing `leadsrsquo and `lagsrsquo in climatic changes isconcerned are the tephra records from the Greenland ice cores The discovery of theVedde and Saksunarvatn ashes in the GRIP record (Gronvold et al 1995) alreadyprovides a basis for making direct comparisons between marine terrestrial and ice-core records It is a matter of some urgency that the incidence of tephra depositsin the Greenland ice cores be more fully explored in the hope that this will lead tothe recognition of additional time-parallel links between the ice-core records on theone hand and oceanic and terrestrial records on the other An investigation of thenew NordGRIP record for this purpose is currently in progress (S M Davies 2002unpublished data)
Finally a fuller and more reshy ned tephrostratigraphical scheme for Europe will alsohave other applications It will provide an important database for those investigatingthe timing and frequency of volcanic eruptions in Europe during the past 20 000 yror so as well as of the geochemical evolution of the dinoterent volcanic centres overthat period A fuller record of the distribution of micro-tephras may also provideinformation on atmospheric circulation patterns during the dispersal and depositionperiods as well as on the nature and altitude of the eruption columns which mayin turn provide inferences about magma viscosity
This paper is a contribution to the INTIMATE project of the INQUA Palaeoclimate Com-mission and the work is supported by a Leverhulme Trust Research project (grant allocationnumber F07537C) entitled Testing hypotheses of rapid climate change using tephrochronol-ogyrsquo SMDrsquo s contribution was completed during possession of a NERC PhD studentship(GT 0499ES162) We are extremely grateful to Dr Peter G Hill for his assistance withthe EPMA analyses at the Tephrochronology Analytical Unit University of Edinburgh We alsothank Dr G Mastrolorenzo (Vesuvius Observatory) and Miss G Swindle for assistance duringthe macreld investigations in Naples Thanks are also expressed to two anonymous reviewers forcomments on an earlier draft
Appendix A
Table 2 shows the major oxide concentrations of NYT glass shards from Procidaand Prato Spilla `Crsquo and of the Mercato Tephra from the Naples area (see x 4 forsite context) All oxides are shown as weight and total iron is expressed as FeO
Figure 8 Radiocarbon calibration curve for Termination 1 and the Early Holocene compared with theGRIP macr 18 O event stratigraphy the GRIP ss08c and GISP2 macr 18 O records (wwwngdcnoaagov) andknown tephra horizons from this period The shaded areas represent the cooler climatic episodes andare labelled with the Greenland stratotype terminology (Bjorck et al 1998) Where radiocarbon agesare reported in table 1 as a range the mean is given here Abbreviations for GRIP horizons are asfollows Un unknown (approximate positions are given (S Johnsen 2001 personal communication))SA Saksunarvatn Ash VA Vedde Ash BF Black Feather Sulphate concentrations from the GISP2record are also shown (Zielinski et al 1996) Open circles denote radiocarbon calibration data fromLake Suigetsu (Kitagawa amp van der Plicht 2000) Filled circles denote radiocarbon calibration data fromCariaco Basin assuming a marine reservoir age of 420 14 C yr (Hughen et al 1998)
Phil Trans R Soc Lond A (2002)
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792 S M Davies and others
Tab
le2
Majo
roxi
de
con
cen
trati
on
sof
NY
Tgl
ass
shard
sfr
om
Pro
cida
an
dP
rato
Spil
laC
rsquoan
dof
the
Mer
cato
Tep
hra
from
the
Naple
sare
a(s
eex4
for
site
con
text
)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
roci
da)
1584
204
0177
634
201
106
828
635
197
5969
1W
DS
2598
603
9178
027
101
204
924
244
583
4965
8W
DS
3586
604
5173
631
100
805
924
342
183
0951
9W
DS
4583
903
9177
933
000
906
924
540
486
9958
3W
DS
5605
106
8179
126
901
204
923
243
086
1976
4W
DS
6591
704
5177
332
801
006
425
740
887
8968
0W
DS
7581
804
1178
031
501
107
125
640
086
9956
1W
DS
8589
504
2179
533
701
506
926
740
987
5970
4W
DS
9592
003
9178
135
101
007
026
443
585
7972
7W
DS
10
591
404
2174
631
601
105
723
442
482
6957
0W
DS
11
593
403
6177
131
301
506
726
439
188
5967
6W
DS
12
588
103
8176
128
100
505
525
141
583
4952
1W
DS
13
577
003
8176
533
500
807
228
140
384
8952
0W
DS
14
586
004
7179
735
300
706
827
842
984
6968
5W
DS
15
588
104
2180
629
400
505
924
937
993
0964
5W
DS
16
579
603
9178
536
501
308
228
836
087
1959
9W
DS
17
580
103
9177
631
500
907
327
039
488
9956
6W
DS
mea
n588
104
2177
631
901
006
525
940
686
9962
8
sd
(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(07
8)
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 793
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
rato
Spil
laC
rsquo)
1552
105
4177
247
401
914
38
735
578
9951
1W
DS
2557
305
7179
845
701
512
640
136
581
5960
6W
DS
3595
004
4173
724
302
003
117
652
877
8950
7W
DS
4575
704
2179
433
001
406
627
043
083
6953
7W
DS
5599
904
0178
826
401
304
421
841
688
4966
5W
DS
6591
103
8177
826
601
105
022
443
888
8960
2W
DS
7565
304
5180
939
501
410
532
535
791
8962
1W
DS
8597
606
9180
826
501
604
821
546
684
6970
7W
DS
9571
805
6179
939
801
109
932
240
883
6964
7W
DS
10
588
603
7176
527
601
104
721
042
487
7953
3W
DS
11
559
404
9180
544
501
812
339
435
878
6957
2W
DS
12
594
704
0181
328
301
705
522
144
785
6967
9W
DS
13
611
103
7187
016
900
802
419
938
195
9975
8W
DS
14
599
204
4181
128
601
404
620
844
986
6971
6W
DS
15
601
204
4177
328
302
004
722
446
385
5972
1W
DS
16
595
104
5176
428
801
504
722
744
884
3962
8W
DS
17
603
704
1177
825
101
503
520
348
181
2965
3W
DS
18
558
704
5179
647
401
813
139
836
879
0960
7W
DS
19
589
602
8178
830
901
606
622
436
091
8960
5W
DS
20
553
606
3178
647
401
913
840
136
978
0956
6W
DS
21
579
004
0175
739
000
708
328
338
286
7959
9W
DS
mea
n582
804
6179
033
401
507
427
341
484
8962
1
sd
(1
87)
(01
0)
(02
7)
(09
2)
(00
4)
(03
9)
(08
0)
(04
9)
(05
0)
(07
0)
Phil Trans R Soc Lond A (2002)
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794 S M Davies and others
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)
1575
202
7194
219
701
101
016
374
766
9951
8W
DS
2575
802
9194
523
902
201
520
273
564
5959
0W
DS
3574
301
4205
219
101
100
416
481
266
1965
2W
DS
4575
500
7206
018
002
000
415
181
669
3968
6W
DS
5580
000
9208
018
601
300
515
883
367
1975
5W
DS
6571
001
0206
016
101
600
515
078
967
1957
2W
DS
7577
501
1201
117
101
500
620
675
655
4950
5W
DS
8573
700
9212
717
101
900
815
187
564
2973
9W
DS
9580
301
3208
715
801
400
824
81
754
1968
1W
DS
10
574
400
6211
18
402
00
516
480
567
8971
6W
DS
11
577
200
7214
212
501
200
829
879
247
962
6W
DS
12
572
200
9211
217
301
501
15
980
465
9966
3W
DS
13
571
800
7210
417
402
201
16
184
467
2971
2W
DS
14
567
300
9208
916
901
400
917
383
262
5959
3W
DS
15
568
600
8205
918
202
101
414
682
666
6960
8W
DS
16
572
501
1211
318
202
01
215
884
364
5970
9W
DS
17
572
901
2212
916
502
101
215
883
667
2973
4W
DS
18
573
01
4211
716
301
801
416
83
365
5970
4W
DS
19
569
201
1207
418
602
101
414
982
964
961
6W
DS
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
3)
(04
2)
(01
3)
(00
1)
(00
2)
(01
)(0
39)
(01
1)
(02
5)
Phil Trans R Soc Lond A (2002)
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796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
References
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Dugmore A J amp Newton A J 1992 Thin tephra layers in peat revealed by X-radiography JArchaeol Sci 19 163170
Dugmore A J amp Newton A J 1998 Holocene tephra layers in the Faroe Islands Frodskaparrit46 191204
Eastwood A J Pearce N J G Westgate J A Perkins W T Lamb H F amp RobertsN 1999 Geochemistry of Santorini tephra in lake sediments from southwest Turkey GlobalPlanet Change 21 1729
Eirpara sup3 ksson J Knudsen K L Hadeg idason H amp Henriksen P 2000 Lateglacial and Holocenepalaeoceanography of the North Icelandic shelf J Quat Sci 15 2342
Etlicher B Janssen C R Juvignparae E amp Van Leeuwen J F N 1987 Le Haut Forez (MassifCentral France) aprmicroes le Plparaeniglaciaire Wurmien environnement et tparaephra du volcan de LaNugmicroere Bull Ass Fr Etud Quat 4 229239
Frezzotti M amp Narcisi B 1996 Late Quaternary Tephra derived paleosols in central Italyrsquo scarbonate Apennine range stratigraphical and paleoclimatological implications Quat Int3436 147153
Friedrich M Kromer B Spurk M Hofmann J amp Kaiser K F 1999 Paleoenvironment andradiocarbon calibration as derived from LateglacialEarly Holocene tree-ring chronologiesQuat Int 61 2739
Froggatt P C 1992 Standardisation of the chemical analysis of tephra deposits Report of theICCT working group Quat Int 1314 9396
Gronvold K Oskarsson N Johnsen S J Clausen H B Hammer C U Bond G amp Bard E1995 Ash layers from Iceland in the GRIP ice core correlated with oceanic and land sedimentsEarth Planet Sci Lett 135 149155
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
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Hadeg idason H Eirpara sup3 ksson J amp van Kreveld S 2000 The tephrochronology of Iceland and theNorth Atlantic region during the Middle and Late Quaternary a review J Quat Sci 15322
Hoek W Z amp Bohncke S J P 2001 Oxygen isotope wiggle matching as a tool for synchronisingice-core and terrestrial records over Termination 1 Quat Sci Rev 20 12511264
Hughen K A Overpeck J T Peterson L C amp Trumbore S 1996 Rapid climate changes inthe tropical Atlantic region during the last deglaciation Nature 380 5153
Hughen K A Overpeck J T amp Lehman J 1998 A new 14 C calibration data set for the LastDeglaciation Radiocarbon 39 483494
Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
Hunt J B amp Hill P G 1996 An inter-laboratory comparison of the electron probe microanalysisof glass geochemistry Quat Int 3436 229241
Hunt J B amp Hill P G 2001 Tephrological implications of beam sizesample size ereg ects inelectron microprobe analysis of glass shards J Quat Sci 16 105117
Hunt J B Fannin N G T Hill P G amp Peacock J D 1995 The tephrochronology andradiocarbon dating of North Atlantic Late Quaternary sediments an example from the StKilda Basin In The tectonics sedimentation and palaeoceanography of the North Atlanticregion (ed R A Scrutton M S Stoker G B Shimmield amp A W Tudhope) vol 90pp 227248 Geological Society of London Special Publication
Hunt J B Clift P D Lacasse C Vallier T L amp Werner R 1998 Standardisation ofelectron probe microanalysis of glass geochemistry In Proc ODP Scientimacrc Results vol 152pp 8591 College Station TX Ocean Drilling Program
Jakobsson S P 1979 Outline of the petrology of Iceland Jokull 29 5773
Juvignparae E 1987 Deux retombparaees volcaniques tardiglaciaires dans le Cparaezallier (Massif CentralFrance) Bull Ass Fr Etud Quat 13 37
Juvignparae E 1993 Contribution microa la tparaephrostratigraphie du Quaternaire et son application microa lagparaeomorphologie Mparaem Serv Explicat Cartes Gparaeol Min Belg 36 166
Juvignparae E amp Gewelt M 1987 La Narse drsquo Ampoix comme tparaephrostratotype dans la Chasup3 ne desPuys mparaeridionale (France) Bull Ass Fr Etud Quat 29 3749
Juvignparae E Kozarski S amp Nowaczyk B 1995 The occurrence of Laacher See Tephra in Pomera-nia NW Poland Boreas 24 225231
Juvignparae E Bastin B Delibrias G Evin J Gewelt M Gilot E amp Streel M 1996 Acomprehensive pollen and tephra based chronostratigraphic model for the Lateglacial andHolocene period in the French Massif Central Quat Int 3436 113120
Keller J 1980 The island of Vulcano Rend Soc It Mineral Petrolog 36 369414
Keller J Ryan W B F Ninkovich D amp Altherr R 1978 Explosive volcanic activity in theMediterranean over the past 200 000 years as recorded in deep sea sediments Geol Soc AmBull 89 591604
Kitagawa H amp van der Plicht J 2000 Atmospheric radiocarbon calibration beyond 11 900 calBP from Lake Suigetsu laminated sediments Radiocarbon 42 369380
Kvamme T Mangerud J Furnes H amp Ruddiman W F 1989 Geochemistry of Pleistoceneash zones in cores from the North Atlantic Norsk Geol Tids 69 251272
Lacasse C Sigurdsson H Johannesson H Paterne M amp Carey S 1995 Source of Ash zone 1in the North Atlantic Bull Volcanol 57 1832
Langone L Asioli A Corregiari A amp Trincardi F 1996 Age depth modelling through theLate-Quaternary deposits of the central Adriatic Basin In Palaeoenvironmental analysis ofItalian crater lake and Adriatic sediments (ed F Oldmacreld amp P Guilizzoni) vol 55 pp 177196 Memorie dellrsquo Instituto Italiano di Idrobiologia
Larsen G 2000 Holocene volcanism in Iceland and tephrochronology as a tool in volcanologyIn Iceland 2000 modern processes and past environments Keele University UK
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 799
Litt T amp Stebich M 1999 Bio- and chronostratigraphy of the Lateglacial in the Eifel regionGermany Quat Int 61 516
Litt T Brauer A Goslar T Merkt J Balaga K Muller H Ralska-Jasiewiczowa MStebich M amp Negendank J F W 2001 Correlation and synchronisation of Lateglacialcontinental sequences in northern Central Europe based on annually laminated lacustrinesediments Quat Sci Rev 20 12331249
Long D amp Morton A C 1987 An ash fall within the Loch Lomond stadial J Quat Sci 297101
Lotter A F Eicher U Siegenthaler U amp Birks H J B 1992 Lateglacial climatic oscillationsas recorded in Swiss lake sediments J Quat Sci 7 187204
Lowe J J 1992 Lateglacial and Early Holocene lake sediments from the Northern ApenninesItaly|pollen stratigraphy and radiocarbon dating Boreas 21 193208
Lowe J J 2001 Abrupt climatic changes in Europe during the last glacialinterglacial tran-sition the potential for testing hypotheses on the synchroneity of climatic events usingtephrochronology Global Planet Change 603 7384
Lowe J J amp Turney C S M 1997 Vedde Ash layer discovered in a small lake basin on theScottish mainland J Geol Soc Lond 154 605612
Lowe J J amp Walker M J C 2000 Radiocarbon dating the last glacialinterglacial transition(ca 14914 C ka BP) in terrestrial and marine records the need for new quality assuranceprotocols Radiocarbon 42 5368
Lowe J J amp Watson C 1993 Lateglacial and Early Holocene pollen stratigraphy of the northernApennines Italy Quat Sci Rev 12 727738
Lowe J J Birks H H Brooks S J Coope G R Harkness D D Mayle F E SheldrickC Turney C S M amp Walker M J C 1999 The chronology of palaeoenvironmental changesduring the Last GlacialHolocene transition towards an event stratigraphy for the BritishIsles J Geol Soc Lond 156 397410
Lowe J J Hoek W Z amp INTIMATE group 2001 Inter-regional correlation of palaeoclimaticrecords for the Last GlacialInterglacial transition a protocol for improved precision recom-mended by the INTIMATE project group Quat Sci Rev 20 11751187
Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
Mangerud J Lie S E Furnes H Kristiansen I L amp Liquest mo L 1984 A Younger Dryas ashbed in western Norway and its possible correlation with tephra beds from the Norwegian Seaand North Atlantic Quat Res 21 85104
Mangerud J Furnes H amp Jparaohansen J 1986 A 9000 year-old ash bed on the Faroe IslandsQuat Res 26 262265
Martini J 1970 Recherche de retombparaees volcaniques dans le sud-est de la France et la Suisseoccidentale Arch Sci 23 641674
Martini J amp Duret J J 1965 Note preliminaire sur la presence drsquo un niveau de cendres vol-caniques dans des sparaediments post-glaciaires des environs de Genmicroeve Arch Sci 18 587588
Mayewski P A Meeker L D Twickler M S Whitlow S Yang Q Lyons W B amp Pren-tice M 1997 Major features and forcing of high latitudes Northern Hemisphere atmosphericcirculation using a 110 000 year long glaciochemical series J Geophys Res 102 345365
Merkt J Muller H Knabe W Muller P amp Weiser T 1993 The Early Holocene Saksunarvatntephra found in lake sediments in NW Germany Boreas 22 93100
Narcisi B 1993 Segnalazione di un livello piroclastico di provenienza etnea nellrsquo area del Fucino(Italia Centrale) Quaternario 6 8792
Narcisi B 1996 Tephrochronology of a Late Quaternary lacustrine record from the Monticchiomaar (Vulture volcano southern Italy) Quat Sci Rev 15 155165
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on September 20 2011rstaroyalsocietypublishingorgDownloaded from
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Newton A J amp Dugmore A J 1993 Tephrochronology of Core C from Lago Grande di Mon-ticchio In Paleolimnology of European Maar Lakes (ed J F W Negendank amp B Zolitschka)Lecture Notes in Earth Science vol 49 333348 Springer
Oldmacreld F Appleby P G amp Thompson R 1980 Palaeoecological studies of lakes in theHighlands of Papua New Guinea J Ecol 68 457477
Orsi G Drsquo Antonio M de Vita S amp Gallo G 1992 The Neapolitan Yellow Tureg a large mag-nitude trachytic phreatoplinian eruption eruptive dynamics magma withdrawal and calderacollapse J Volcanol Geotherm Res 53 275287
Paterne M Guichard F Labeyrie J Gillot P Y amp Duplessy J C 1986 Tyrrhenian Seatephrochronology of the oxygen isotope record for the past 60 000 years Mar Geol 72259285
Paterne M Guichard F amp Labeyrie J 1988 Explosive activity of the south Italian volca-noes during the past 80 000 years as determined by marine tephrochronology J VolcanolGeotherm Res 34 153172
Paterne M Labeyrie J Guichard F Mazaud A amp Maitre F 1990 Fluctuations of the Cam-panian explosive volcanic activity (south Italy) during the past 190 000 years as determinedby marine tephrochronology Earth Planet Sci Lett 98 166174
Pawse A Beske-Diehl S amp Marshall S A 1998 Use of magnetic hysteresis properties andelectron spin resonance spectroscopy for the identimacrcation of volcanic ash a preliminary studyGeophys J Int 132 712720
Pearce N J G Westgate J A amp Perkins W T 1996 Developments in the analysis of singleglass shards in volcanic deposits by laser ablation ICP-MS quantitative and single internalstandard multi-element methods Quat Int 3436 213227
Pearce N J G Westgate J A Perkins W T Eastwood W J amp Shane P 1999 Theapplication of laser ablation ICP-MS to the analysis of volcanic glass shards from tephradeposits bulk glass and single shard analysis Global Planet Change 21 151171
Pilcher J R amp Hall V A 1992 Towards a tephrochronology for the Holocene of the north ofIreland Holocene 2 255259
Ponel P amp Lowe J J 1992 Coleopteran pollen and radiocarbon evidence from the Prato Spillarsquo Drsquo succession N Italy C R Acad Sci Paris Sparaer II 315 14251431
Rose N L Golding P N E amp Battarbee R W 1996 Selective concentration and enumerationof tephra shards from lake sediment cores Holocene 6 243246
Ruddiman W F amp Glover L K 1972 Vertical mixing of ice rafted volcanic ash in NorthAtlantic sediments Geol Soc Am Bull 83 28172836
Ruddiman W amp McIntyre A 1981 The North Atlantic Ocean during the last deglaciationPalaeogeogr Palaeoclimatol Palaeoecol 35 145214
Santacroce R 1987 Somma Vesuvius Quad Ric Sci 114 252
Sarna-Wojcicki A 2000 Tephrochronology In Quaternary geochronology methods and applica-tions (ed J S Noller J M Sowers amp W R Lettis) AGU Reference shelf vol 4 pp 357377Washington DC American Geophysical Union
Sejrup H P Sjiquest holm J Furnes H Beyer I Eide L Jansen E amp Mangerud J 1989Quaternary tephrochronology on the Iceland Plateau north of Iceland J Quat Sci 4 109114
Sikes E L Samson C R Guilderson T P amp Howard W R 2000 Old radiocarbon agesin the southwest Pacimacrc Ocean during the last glacial period and deglaciation Nature 405555558
Stein R Nam S-I Grobe H amp Hubbersten H 1996 Late Quaternary glacial history andshort term ice rafted debris deg uctuations along the East Greenland continental marine In LateQuaternary palaeoceanography of the North Atlantic margins (ed J T Andrews W E NAustin H Bergsten amp A E Jennings) pp 135151 Geological Society London SpecialPublication
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 801
Stuiver M amp Grootes P M 2000 GISP2 oxygen isotope ratios Quat Res 53 277284
Stuiver M Reimer P J Bard E Beck J W Burr G S Hughen K A Kromer BMcCormac G Van der Plicht J amp Spurk M 1998 INTCAL 98 radiocarbon age calibration24 0000 cal BP Radiocarbon 40 10411083
Sweatman T R amp Long J V P 1969 Quantitative electron microprobe analysis of rock formingminerals J Petrol 7 332379
Turney C S M 1998 Extraction of rhyolitic ash from minerogenic lake sediments J Paleolim-nol 19 199206
Turney C S M amp Lowe J J 2001 Tephrochronology In Tracking environmental changes inlake sediments physical and chemical techniques (ed W M Last amp J P Smol) DordrechtKluwer Academic
Turney C S M Harkness D D amp Lowe J J 1997 The use of microtephra horizons tocorrelate Lateglacial lake sediments successions in Scotland J Quat Sci 12 525531
Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
van den Bogaard P amp Schmincke H 1985 A widespread isochronous Late Quaternary tephralayer in central and northern Europe Geol Soc Am Bull 96 15541571
van den Bogaard B Dordeg er W Sandgren P amp Schmincke H-U 1994 Correlating theHolocene records Icelandic tephra found in Schleswig-Holstein (northern Germany) Natur-wissenschaften 81 554556
Vernet G amp Raynal J-P 2001 Tephrostratigraphy of the Limagne revisited Implications forLateglacial and Holocene Prehistory In Tephras chronology archaeology (ed E Juvignparae ampJ-P Raynal) pp 111116 Dossiers de lrsquo ArchparaeoLogis no 1 France
Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
Vezzoli L 1991 Tephra layers in Bannock Basin (eastern Mediterranean) Mar Geol 1002134
von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
Walker M J C Bjorck S Lowe J J Cwynar L C Johnsen S Knudsen K-L WohlfarthB amp INTIMATE Group 1999 Isotopic events in the GRIP ice core a stratotype for the LatePleistocene Quat Sci Rev 18 11431150
Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
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Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
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780 S M Davies and others
geochemical tool One approach that has promise is the analysis of trace and rareearth elements using an ultraviolet laser ablation inductively coupled plasma massspectrometer (UV-LA-ICP-MS) (Pearce et al 1996 1999 Eastwood et al 1999)This approach has been applied successfully to analysis of tephras of Mid-Holoceneage but not yet to tephras that fall within the period of interest here
4 Tephra layers in Europe and the North Atlantic regiondated to between 185 and 80 14C ka
(a) Icelandic province
The Icelandic volcanic systems are divided into three main groups based on theirgeochemical characteristics tholeiitic basalts transitional alkali basalts and alkaliolivine basalts (Jakobsson 1979) Collectively magmas from the Icelandic provincespan a wide geochemical spectrum although individual volcanic centres have tightgeochemical distributions (shy gure 3) for four of the main centres Grimsvotn-Kverfjolland Veidvotn-Dyngjufoll which form part of the northern (tholeiitic) volcanic zoneand Hekla and Katla which fall within the eastern (alkali olivine basalt and transi-tional alkali basalt) volcanic zone (Haregidason et al 2000) These appear to be thekey centres for the tephras listed in table 1 that have been assigned an Icelandicorigin
One of the best-known and most widely dispersed tephra horizons in northernEurope that has an Icelandic origin is the Vedde Ash (VA) which was depositedca 103 14C ka BP (Birks et al 1996 Wastegard et al 1998) within the GS-1Younger Dryas chronozone This ash is believed to originate from the Katla complexwithin the transitional alkali basalt province (Mangerud et al 1984 Lacasse et al 1995) in the south of the island The ash has a bimodal geochemical composition (rhy-olitic and basaltic) which is thought to reregect derivation from two separate magmachambers Studies of recent volcanic events in Iceland have shown that the mostexplosive eruptions generating the largest amounts of tephra occur in this tran-sitional alkali basalt province (Haregidason et al 2000) It is also believed that thewidespread distribution of this ash was caused by the development of co-ignimbriteash plumes during an ignimbrite-forming eruption (Lacasse et al 1995)
Layers of VA that are visible to the naked eye have been found in lake sediments inwestern Norway (Mangerud et al 1984) and the Inner Hebrides Scotland (Davies etal 2001) and in marine cores throughout the NE Atlantic (see for example Kvammeet al 1989 Lacasse et al 1995) in the northern North Sea (Long amp Morton 1987)on the Iceland plateau (Ruddiman amp McIntyre 1981 Sejrup et al 1989) and on theeast Greenland continental margin (Stein et al 1996) The distribution of the VAin North Atlantic marine sequences is characterized by an arcuate lobe extendingsouthwest from the Denmark Strait and curving eastwards to mid-latitudes in theNorth Atlantic (Lacasse et al 1995) This strongly suggests deposition from raftedice which was displaced to the southwest and south in a circulating counterclockwisegyre (Ruddiman amp Glover 1972) This may well reregect Katlarsquos close proximity tothe southern coast of Iceland with the Vedde tephra being deposited on ice thatcalved directly into the North Atlantic (Haregidason et al 2000) However depositionvia the atmosphere almost certainly took place as well as is indicated by the recentdiscoveries of rhyolitic VA in micro-tephra form in several sites in Scotland (Turneyet al 1997) southern Sweden (Wastegard et al 1998 2000a) and western Russia
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(Wastegard et al 2000b) A more recent discovery of a relatively high concentrationof rhyolitic VA glass shards in the northern Netherlands indicates that the ash maywell have been dispersed much further south than previously thought (S M Davies2002 unpublished work) Finally glass shards assigned to the VA have also beendiscovered in the GRIP ice core and dated to 11 980 sect 80 GRIP yr BP (Gronvold etal 1995) This discovery is extremely important for it indicates that the VA maywell provide a reliable time-parallel marker horizon between ice-core marine andterrestrial records
Two other important Icelandic ash layers the Borrobol and Saksunarvatn Tephraswere deposited near the beginning and end of the Last TerminationEarly Holoceneinterval respectively The Borrobol Tephra was discovered for the shy rst time in lakesediments in several sites in Scotland and as yet is known only in micro-tephra formIt has been dated in Scottish sites to ca 123 14C ka BP (Turney et al 1997) Whatis thought to be a contemporaneous tephra has been detected in marine sedimentson the North Icelandic shelf (Eirplusmn ksson et al 2000) This certainly has a very similargeochemical composition to those reported from Scotland but the horizon in whichit was discovered on the North Iceland plateau has been dated to 134 14C ka Theage discrepancy between the Scottish and Icelandic Borrobol Tephra layers may wellreregect the inreguence of a marine reservoir error although the possibility that severaltephras with similar geochemical composition were erupted over a period exceeding1000 yr cannot be ruled out (Larsen 2000)
The Saksunarvatn Ash appears to have been one of the largest Holocene eruptionsin Iceland It has a tholeiitic basaltic composition which is considered to indicate anorigin in the Grimsvotn or Kverfjoll complex (shy gure 3) (Mangerud et al 1986) Layersof this ash have been identishy ed in sites on the Faroe Islands (Mangerud et al 1986Dugmore amp Newton 1998 Wastegard et al 2001) the Shetland Isles (Bennet et al 1992) northern Germany (Merkt et al 1993) western Norway (micro-tephra) (Birkset al 1996) and in the GRIP (Gronvold et al 1995) and NordGRIP ice cores (S MDavies 2002 unpublished work) It has been dated to between 9060 and 8930 14C kaBP (Birks et al 1996) in Norway and to ca 10 240 sect 30 GRIP yr BP in the GRIPice core (Gronvold et al 1995) The Saksunarvatn Ash may thus provide a secondimportant widespread time-parallel marker between ice-core marine and terrestrialrecords
Other Icelandic tephras of rhyolitic amacr nity are less well known in terms of theirdistribution and geochemical variation The Hogstorpsmossen Tephra reported fromSweden (Bjorck amp Wastegard 1999) and the L3754 tephra discovered in the FaroeIslands (Dugmore amp Newton 1998) are known from single sites only and so theirpotential for tephrostratigraphy is uncertain at present Furthermore the geochem-ical spectrum of the Hogstorpsmossen Tephra is based on a small dataset with lowanalytical totals
A number of tephras of basaltic composition have originated from Iceland buttheir distributions are largely conshy ned to Iceland or to marine cores collected fromclose to the Iceland coast or in the North Atlantic These include the tephras listedas 1-THOL-1 1-THOL-2 KOL-GS-2 GS-2BAS-1 GS-2BAS-2 GS-2BAS-3 andGS-2BAS-4 in table 1 (Kvamme et al 1989 Bjorck et al 1992 Eirplusmn ksson et al 2000 Haregidason et al 2000) The shy rst two in this list are tholeiitic basaltic tephrasassociated with the VA in a complex series of tephras collectively termed NorthAtlantic Ash Zone 1 (NAAZ1) which has been detected in numerous marine cores
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782 S M Davies and others
from the North Atlantic Initially thought to represent a single eruption analysisof high-resolution sediment sequences from Lake Torfadalsvatn in northern Iceland(Bjorck et al 1992) the Hebridean Shelf near NW Scotland (Austin amp Kroon 1996)the St Kilda Basin (Hunt et al 1995) and the open North Atlantic (Bond et al 2001)has demonstrated that NAAZ1 comprises a series of distinct ashes that probablyreregect separate eruption events 1-THOL-1 is thought to originate from Veidivotn(shy gure 3) while Grimsvotn may have been the source of 1-THOL-2 (Kvamme et al 1989)
KOL-GS-2 is also of tholeiitic basaltic composition but is thought to originatefrom the Kolbeinsey Ridge system (Eirplusmn ksson et al 2000) To date this tephra hasbeen detected in one marine core only within the same record on the North Ice-landic shelf as that from which the correlative of the Borrobol Tephra was alsoreported (Eirplusmn ksson et al 2000) GS-2BAS-1 to GS-2BAS-4 are of uncertain ori-gin but are thought to have been deposited at roughly the same time as KOL-GS-2(ca 134 14C ka BP (Haregidason et al 2000))
The limited distribution of these basaltic tephras a feature that is not unique toIcelandic basaltic material may reregect two factors the relative magnitude of the vol-canic eruptions from which they were derived and the limited aerial transportationof basaltic glass which is denser than rhyolitic material However a rather surpris-ing recent discovery is that of visible basaltic VA in a site on the Isle of Skye inthe Inner Hebrides Scotland (shy gure 5) (Davies et al 2001) All other occurrencesof VA in Scotland are exclusively of rhyolitic material and in micro-tephra formonly (Turney et al 1997 Turney 1998) Clearly basaltic tephra must have beentransported subaerially as far south as Skye and the reason why it has not beendetected at other sites in Scotland is puzzling We suspect that this partly reregectsthe laboratory methods employed to separate glass shards present in low concentra-tion within a micro-tephra layer from the host sediment The technique used is adensity-separation (regotation) procedure (Turney 1998) and as basaltic shards havea specishy c density similar to quartz one of the most abundant minerals in lake sedi-ments of Late Glacial age basaltic material is dimacr cult to detect using this methodThis hypothesis is currently under investigation and alternative detection methodsare being explored including magnetic separation (Mackie et al 2002)
Several other events listed in table 1 that are of probable Icelandic origin includetephras recorded in the GRIP ice core including visible (eg the `Black Featherrsquo)tephras as well as uncertain tephras inferred from distinct Ca peaks (S Johnsen2001 personal communication) No glass shards have yet been detected in the latterbut a volcanic origin is assumed because high Ca peaks are associated with knowntephras in other Greenland ice cores (S Johnsen 2001 personal communication)These are referred to as `unknownrsquo in table 1 No geochemical analyses are availablefrom these horizons so their origin must remain speculative but a possible source isIceland in view of its proximity to the Greenland ice sheet and assumed atmosphericcirculation patterns
(b) Eifel province
There are two prominent tephra events dated to the Termination 1Early Holocenetime-span that originated from the Eifel province the Laacher See Tephra (LST)and the Ulmener Maar Tephra (UMT) Visible occurrences of the LST indicate that
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European tephrochronological framework for Termination 1 783
Vedde Ash
615 625 635 645 655depth (cm)
organic lake mudsHolocene
silty clayGS-1Younger Dryas
organic lake mudsGI-1Alleroslashd
100 microm
(a)
(b)
Figure 5 (a) Photograph of the visible VA layer discovered at Loch Ashik Isle of Skye InnerHebrides Scotland (b) Light microscope photograph showing the rich content of basaltic shards(examples are indicated by the arrows) within this layer (8024 m m size fraction)
this ash was dispersed over much of central Europe (van den Bogaard amp Schmincke1985 Friedrich et al 1999 Litt amp Stebich 1999) The LST is dated by radiocarbonto ca 110 14C ka BP (van den Bogaard amp Schmincke 1985) and to 11 063sect12 14C BP(Friedrich et al 1999) by varve chronology to 1288 varve ka BP (Brauer et al 1999Litt et al 2001) and by ArAr dating to 129 ka cal BP (van den Bogaard 1995) Ithas a phonolitic composition and is thought to have originated from a plinian andphreatomagmatic eruption with the distal ash being carried in three distinct plumesone to the northeast towards Poland one to the west and the third to the southcovering the Jura Mountains and north Italy (van den Bogaard amp Schmincke 1985Juvigne et al 1995 Bossuet et al 1997) This pattern is thought to reregect altitu-dinal variations in the predominant wind direction Sedimentary sequences near thevolcanic source indicate that the LST consists of three main layers which represent
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784 S M Davies and others
dinoterent eruption phases These are grouped together as the Laacher See TephraFormation but the three individual units can be traced within and between a seriesof depositional fans The geochemical data obtained from these three LST layersshow signishy cant variations as reregected in the ternary plots (shy gure 4)
The Early Holocene Ulmener Maar Tephra (UMT) is of rhyolitic composition andappears to be restricted to sites in Germany though this conclusion is also based onrecords of visible tephras only It is dated to ca 956 14C ka BP and to 110 varve ka(Zolitschka et al 1995 Litt et al 2001)
(c) Massif Central province
The Massif Central tephras are mainly of basaltic trachyandesitic compositionwhich is distinct from the other ash provinces (shy gures 3 and 4) and their known dis-tributions are mostly conshy ned to the Massif Central region The ages of the MassifCentral tephras are based on radiocarbon dates obtained from mire and lake sedi-ments which `bracketrsquo the tephras The La Nugsup3ere Tephra with an age of 114 14C kaBP is the oldest Massif Central tephra identishy ed so far within the time-span of inter-est (Etlicher et al 1987 Juvigne et al 1996) The two Godivelle Tephras (5 and 4)are close in age but extensive radiocarbon dating suggests distinct ages of 107and 103 14C ka BP respectively (Juvigne et al 1996) The age of the Puy de DomeTephra is less certain as the estimate is based on only one radiocarbon date froma site in the southern Chaplusmn ne des Puys (table 1) This tephra is thought to havea trachyte composition (Juvigne 1993) although no major element concentrationshave yet been published
The ChopineKilianVasset tephras are thought to be derived from three separateEarly Holocene eruptions although the stratigraphic succession is not known atpresent These trachytic tephras have been radiocarbon dated to ca 854sect150 14C kaBP but are thought to have erupted separately within ca 260 yr (Juvigne et al 1996) This series of tephras is considerably more widespread than the others fromthe region having been identishy ed as far east as the Jura Mountains (Martini amp Duret1965 Martini 1970) Some other ash falls that originated from the Chaplusmn ne des Puysappear to be of local importance only (Vernet et al 1998 Vernet amp Raynal 2001)Geochemical data are currently available for only three of the Massif Central tephrasand so far as is known no attempt has yet been made to identify these tephras inmicro-tephra form
(d ) Italian provinces
The Italian tephras from this period can be assigned to three main volcanic com-plexes the Campanian volcanic shy elds around Naples Etna on Sicily and the AeolianIslands The Campanian complex which includes the Phlegrean Fields Vesuviusand Ischia is mainly trachytic in composition with a geochemical spectrum that isquite distinct from those of the Etna complex and of the Aeolian Islands (shy gure 3)Tephras originating from one or more of these three complexes have been detectedin marine cores from the Tyrrhenian and Adriatic seas as well as other parts of theMediterranean Sea (Keller et al 1978 Paterne et al 1986 1988 1990 Langone etal 1996) and in lake sequences in southern Italy such as Lago Grande di Monticchio(Newton amp Dugmore 1993 Narcisi 1996 Allen et al 1999) and central Italy such asLago Albano near Rome (Calanchi et al 1996) Some work has also been conducted
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European tephrochronological framework for Termination 1 785
in or close to the volcanic source areas in an attempt to establish the full sequenceof volcanic eruptions during the Late Quaternary (see for example Di Vito et al 1999) There are nine Italian tephras reported from marine and lake sequences thatdate from the period between 185 and 80 14C ka BP In all instances the recordsare of visible layers of tephra The ages of some of these are poorly established atpresent with conregicting data obtained from dinoterent sites The ages suggested intable 1 are those favoured in the most recent publications but these may requirere-assessment in the light of future research
The two oldest known tephras in the time-period of interest are the L9 and Green-ish Tephras both recorded as separate features within the annually laminated Lagodi Monticchio maar sequence The lowest of the two L9 is considered to be the cor-relative of the `basalrsquo plinian eruption of Vesuvius (Narcisi 1996) Age estimates ofa palaeosol that underlies the Vesuvius tephra sequence are ca 1617 14C ka BP forthis event (Delibrias et al 1979) L9 has a trachytic composition very similar to theGreenish Tephra (table 1) However L9 which is also a product of Vesuvius is foundstratigraphically below the Greenish Tephra in the Lago di Monticchio core TheGreenish Tephra is dated in the Monticchio sequence to 17 560 varve yr BP (Allenet al 1999) and has a calibrated radiocarbon age estimate of 17 830 sect 300 cal BP(Andronico et al 1995) Both tephras have a dominantly eastwards dispersal basedon the occurrences of visible layers (Santacroce 1987 Narcisi 1996) Both tephrasalso have a trachytic composition and as can be seen from table 1 the reportedgeochemical spectra are very close indeed with the standard deviations overlappingfor almost every major element This could present problems for tephrostratigra-phy where only one of the tephras is evident in a sediment sequence in particularbecause they are so close in age This is a good example of where an analysis oftrace and rare earth elements might be required to make a clear distinction betweentephras with very similar major oxide concentrations
The Y-1 Tephra also termed the Biancavilla Montalto Ignimbrite (Vezzoli 1991)is a product of Etna and has been identishy ed as a visible benmoritic tephra horizonthroughout the central Mediterranean (Paterne et al 1988) including central Italyand the Adriatic Sea (Vezzoli 1991 Narcisi 1993 Calanchi et al 1996) It has anestimated age of ca 140 14C ka BP The Unita dei Tefra Superiori tephra which hasbeen detected as far east as Lago di Monticchio in south-central Italy (Narcisi 1996)is also dated to ca 140 14C ka BP (Alessio et al 1976) but it is thought that thesource of this tephra lies in the Phlegrean Fields No geochemical data are availablefrom the presumed source region|the data reported in table 1 were obtained fromthe Lago di Monticchio record (Narcisi 1996)
The NYT which is equivalent to the C-2 tephra reported from various marinesequences has also been traced throughout central Italy and the Adriatic Sea (Pat-erne et al 1988 Calanchi et al 1996 Di Vito et al 1999) (shy gure 2) In the centralApennines region it formed the parent material for a soil that started to developat the beginning of the Holocene period (Frezzotti amp Narcisi 1996) Also originatingfrom the Campi Flegrei caldera it is dated to ca 120 14C ka BP (Di Vito et al 1999) Published geochemical data based on EDS indicate three dinoterent geochemicalpopulations varying from latite to phonotrachyte in composition (Orsi et al 1992Paterne et al 1988) (table 1) We report in x 4 of this paper on new data obtainedfrom the NYT by WDS and it is the mean of these new data that is included intable 1 Comparisons with the previously published EDS data are provided (table 1)
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786 S M Davies and others
The new data indicate clearly that the NYT originated from the Campanian volcaniccentre
In the interval between the dispersal of the NYT (ca 120 14C ka BP) and 95 14Cka BP there appear to have been as many as 34 eruptions in the Campi Flegrei caldera(Di Vito et al 1999) Of these only one appears to have been detected widely in theregion the Pomici Principali (also termed the Agnano Formation or C-1 tephra inmarine records (Paterne et al 1988) This was the product of the highest magnitudeeruption from this epoch and is dated to between 976 sect 300 and 1032 sect 50 14C kaBP (Delibrias et al 1979 Di Vito et al 1999) or to 122 varve ka BP based on theMonticchio varve chronology (Allen et al 1999) It is trachytic in composition andappears to have had a mainly eastwards dispersal
The Mercato Tephra dated to ca 80 14C ka BP and originally analysed usingEDS has a phonolitic composition and is believed to have been generated by Vesu-vius (Paterne et al 1988) New WDS data obtained from reference samples col-lected from an exposure to the west of Naples support these conclusions (table 1 andAppendix A) The silica content of the WDS analyses are ca 3 lower than thoseobtained using EDS (table 1) which may reregect the fact that the EDS data werenormalized
The only tephra listed in table 1 that is thought to have originated from the AeolianIslands is the Pollara pumice also referred to as the E2 tephra in marine sequences(Paterne et al 1986 1988) The limited geochemical data available so far suggest itto be the only Italian tephra listed in table 1 that is rhyolitic in composition Littlemore is known about this ash which has not been recorded extensively except thatits age is estimated to be ca 130 14C ka BP (Keller 1980)
5 Extending the known distributions of European tephras
Figure 2 summarizes schematically the known distributions of three of the tephrasreferred to in the preceding section the VA the LST and the NYT Following theintroduction of a laboratory method that enables the detection of micro-tephra parti-cles in mineral-rich sediment the VA has been traced to sites that are located muchfarther south (into The Netherlands) and east (as far as St Petersburg) than thedistribution limits based on occurrences of visible layers of the ash As a result con-tinental sequences over a much larger area in northern Europe can now be correlateddirectly with marine and ice-core records using the VA as a time-parallel marker
This suggests therefore that other prominent ash layers such as the LST andNYT should also be detectable over larger tracts of Europe than is presently thecase if suitable sites are examined for the presence of micro-tephra horizons To testthis assertion we examined lake sediment deposits of Last Termination age froma site in the northern Apennines in order to establish whether the NYT could bedetected in micro-tephra form The site selected Prato Spilla `Crsquo lies well to thenorth of the localities in central and southern Italy and in the Adriatic Sea fromwhich visible records of the NYT have been reported Prato Spilla `Crsquo lies at an alti-tude of ca 1350 m in the Appennino Parmense ca 60 km south of Parma and 15 kmeast of Pontremoli The site contains a continuous sediment sequence spanning theLast Termination and most of the Holocene Detailed pollen and coleopteran strati-graphical records which have been radiocarbon dated have been published for thissite (Lowe 1992 Ponel amp Lowe 1992 Lowe amp Watson 1993)
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European tephrochronological framework for Termination 1 787
Figure 6 Light microscope photograph of an NYT glass shard from Prato Spilla Crsquosequence assigned on geochemical grounds to the NYT
The methods adopted for sub-sampling of the Prato Spilla `Crsquo sequence for thequantishy cation of glass shard concentrations and for subsequent electron microprobeanalysis of selected glass shards followed those described elsewhere (Turney 1998)In summary contiguous samples of 1 cm stratigraphic interval were extracted fromthe sequence to establish presenceabsence of glass shards Each of the 1 cm3 blocksin which tephra particles was detected was then examined with more care andshard concentrations were quantishy ed for each sub-sample Micro-tephra particleswere detected in shy ve samples (shy gure 6) but were predominantly clustered around500 cm in the part of the sequence assigned on pollen-stratigraphic grounds to theLate Glacial Interstadial or the `Allerfrac12drsquo|indeed the part of the succession in whichthe NYT would be expected to occur Peak concentrations of micro-tephra particlesreach 225 shards cmiexcl3 and are conshy ned to a single 1 cm thick sample in the sequencewhich probably represents the time of maximum deposition of the ash
Electron microprobe measurements based on WDS were obtained from the surfacesof 21 separate glass shards extracted from the sample with peak shard concentrations(Appendix A) Since only EDS measurements were available for the NYT prior to thepresent study we also obtained WDS measurements from 17 shards extracted fromthe visible layer of NYT that is exposed on Procida Island which lies in the type-locality for the NYT close to the city of Naples (Appendix A) The results providenot only a more comprehensive geochemical dataset for the NYT than was previ-ously available but also a consistent basis for comparison with the Prato Spilla `Crsquodataset All of the WDS data reported here (Appendix A) were measured at the samelaboratory (Tephrochronology Analytical Unit University of Edinburgh) using thesame sample pretreatment and preparation protocol The WDS results for the NYTdinoter to a minor degree from the EDS results (table 1 and Appendix A) especiallywith respect to the amounts of silica aluminium and calcium measured The EDS
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788 S M Davies and others
4 8FeO ()
TiO
2 (
) Neapolitan Yellow Tuff(Procida)Neapolitan Yellow Tuff(Prato Spilla lsquoCrsquo)
0
1
2
3
40 50 60 70
MgO
(
)
SiO2 ()
K2O
(
)
40 50 60 70
0
04
08
4
8
12
SiO2 ()
(a)(b)
(c)
Figure 7 Bi-plots of SiO2 K2 O SiO2 MgO and FeOTiO2 for the WDS analyses obtainedfrom glass shards of the NYT from Procida (Naples) and Prato Spilla Crsquo Means and standarddeviations are shown
results show a higher degree of statistical scatter than the WDS measurements whichmay reregect the fact that the data were normalized combined with the inreguence ofvariation in water content between shards
There is a very close correspondence between the WDS data for the Prato Spilla `Crsquomicro-tephra shards and those obtained from the type-material near Naples (shy g-ure 7) The geochemical data strongly suggest therefore that the NYT is representedat the Prato Spilla `Crsquo site by a discrete layer of micro-tephra particles This conclu-sion is compatible with the pollen-stratigraphic data from the site and accords withage estimates for the NYT (ca 120 14C ka BP) obtained from other sites (Paterneet al 1990)
These results encourage us to believe that many if not all of the tephras listedin table 1 will be detectable over much larger tracts of Europe than is presently thecase if appropriate research is undertaken to detect layers of micro-tephra particlesin selected sites The authors are presently engaged in a major continent-wide pro-gramme of research in collaboration with a number of European research groupsdesigned to test this hypothesis The focus in this research is on those parts of Europewhere we expect to shy nd overlapping `apronsrsquo of tephra deposition originating fromthe Italian Eifel Massif Central and Icelandic provinces For example a number ofsites in parts of southern France northern Italy and perhaps western Switzerlandmay have received inreguxes of micro-tephra originating from the Italian and Eifelprovinces and perhaps also from the Massif Central Sites in parts of Germany Den-mark and southern Sweden for example may in turn have received tephra depositsfrom both of the Icelandic and Eifel provinces If this proves to be the case then thestage will be set for the construction of a tephrostratigraphical framework for Europewhich will enable Last Termination sequences to be correlated on a continent-widebasis using micro- and visible tephra layers as time-parallel stratigraphic markersFurthermore there is also the possibility that other tephras remain to be discovered
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European tephrochronological framework for Termination 1 789
those which either because of the magnitude or nature of some volcanic eruptionswere distributed over parts of Europe in micro-tephra form only
6 European tephrostratigraphy and the chronology of eventsduring the Last Termination and Early Holocene
One of the crucial issues in Late Quaternary palaeoenvironmental research thatremains to be resolved is the degree to which climatic events inferred from oceanicterrestrial and ice-core records were synchronous during the Last Termination andEarly Holocene If the ice-core records provide realistic estimates of the rates anddurations of climatic events during this period then comparisons between individ-ual records have to be enotected with at least a decadal precision The problem thispresents and the role that tephrostratigraphy can play in resolving some of thedimacr culties involved are put into perspective in shy gure 8
Figure 8 shows some of the data used to calibrate radiocarbon dates (the LakeSuigetsu and Cariaco Basin datasets) plotted against the GRIP ss08c ice-core recordof macr 18O variations The latter has been selected by the INTIMATE group as an arbi-trary and temporary standard for this period and used to deshy ne an event stratig-raphy scheme (shy gure 1) for the Last Termination (see Bjorck et al 1998 Walker etal 2001) As has been alluded to in earlier sections of this paper the uncertaintiesassociated with all of the dating methods currently employed preclude precise com-parisons of ice-core marine and terrestrial records Oceanic and terrestrial recordsmostly rely upon radiocarbon dating locally supplemented in a few cases by varvechronology Imprecisions in radiocarbon dates can arise through site-specishy c fac-tors (eg hard-water or mineral carbon errors in freshwater sequences and reservoirerrors in marine sequences) sample selection laboratory measurements of 14C activ-ity and other factors (Lowe amp Walker 2000) Further imprecision may be introducedby the calibration of radiocarbon dates since the uncertainties in the dataset usedto calibrate pre-Holocene radiocarbon dates INTCAL98 are far higher than forthe Holocene which is based on dendro-calibration (Stuiver et al 1998) There arealso uncertainties anotecting varve chronologies while the ss08c ice-core chronologyfor the Last Termination dinoters signishy cantly from the GISP2 record and indeedfrom other models of the GRIP record (Lowe et al 2001) Published comparisonsbetween ice-core marine and terrestrial records for the Last Termination seldom takeinto account the true magnitude of the dating uncertainties involved and frequentlyemploy circular reasoning
Figure 8 shows the positions on the radiocarbon time-scale of 20 of the tephrasdiscussed earlier in this paper these being the ones for which reasonably conshy dentradiocarbon age estimates can be made (though these will be subject to revised esti-mates in the future) A high number of these occur in the period 14080 14C kaBP but we conshy dently anticipate the discovery in the future of additional tephras(perhaps in micro-tephra form only) which will date to the period 185140 14C kaBP Tephras detected in the GRIP ice core over the same time-interval are plottedon the calendar time-scale in shy gure 8 By providing key `time-linesrsquo between recordstephrostratigraphy can help to resolve some of the dating uncertainties referredto earlier by for example enabling direct comparisons of discrepant age estimatesobtained using dinoterent methods (cf Litt et al 2001) It can also provide estimatesof the magnitudes of the reservoir errors that anotected various marine sectors at dif-
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790 S M Davies and others
-44
-40
-36
-32
cale
ndar
yea
rs B
P
8000
9000
10 0
00
11 0
00
12 0
00
13 0
00
14 0
00
15 0
00
16 0
00
17 0
00
18 0
00
14C age (BP)
VA
SA
Un
Un
Un
Un
Un
BF
Hol
ocen
eG
S-1
GI-
1aG
I-1b
GI-
1cG
I-1d
GI-
1eG
S-2
aG
S-2
bG
S-
2c
Bor
robo
l
La
Nug
egravere
Laa
cher
See
God
ivel
le 5
amp I
-TH
OL
-2
Puy
de D
ocircme
I-T
HO
L-1
Saks
unar
vatn
Houmlg
stor
psm
osse
nU
lmen
er M
aar
amp L
3574
radiocarbon dated European tephra horizons
Cho
pine
Kili
an V
asse
tM
erca
to
God
ivel
le 4
Pom
ici P
rinc
ipal
i amp V
edde
Polla
ra p
umic
eK
OL
-GS-
2 amp
GS
-2B
AS-
12
3
GS
-2B
AS-
4 U
nita
dei
Tef
raSu
peri
ori amp
laye
r Y
-1
Gre
enis
h
L9
20 0
0018
000
16 0
0014
000
12 0
0010
000
-44
-40
-36
-32
800
600
400
200 0
GISP2 volcanicsulphate conc (ppb)
1000
Nea
polit
an Y
ello
w T
uff
GISP2 18O (permil) dGRIP 18O (permil) d
Figure 8 For description see opposite
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European tephrochronological framework for Termination 1 791
ferent times through a comparison of radiocarbon dates obtained from marine andterrestrial horizons in which the same tephra has been detected (see for exampleAustin et al 1995 Bondevik et al 2001 Haregidason et al 2000) Tephrostratigraphymay provide an independent test of suggestions that some of the climatic changesduring the Last Termination were time-transgressive as illustrated for some appar-ently contrasting climatic trends in Iceland Britain and NW Russia (Lowe 2001) Ofparticular importance as far as establishing `leadsrsquo and `lagsrsquo in climatic changes isconcerned are the tephra records from the Greenland ice cores The discovery of theVedde and Saksunarvatn ashes in the GRIP record (Gronvold et al 1995) alreadyprovides a basis for making direct comparisons between marine terrestrial and ice-core records It is a matter of some urgency that the incidence of tephra depositsin the Greenland ice cores be more fully explored in the hope that this will lead tothe recognition of additional time-parallel links between the ice-core records on theone hand and oceanic and terrestrial records on the other An investigation of thenew NordGRIP record for this purpose is currently in progress (S M Davies 2002unpublished data)
Finally a fuller and more reshy ned tephrostratigraphical scheme for Europe will alsohave other applications It will provide an important database for those investigatingthe timing and frequency of volcanic eruptions in Europe during the past 20 000 yror so as well as of the geochemical evolution of the dinoterent volcanic centres overthat period A fuller record of the distribution of micro-tephras may also provideinformation on atmospheric circulation patterns during the dispersal and depositionperiods as well as on the nature and altitude of the eruption columns which mayin turn provide inferences about magma viscosity
This paper is a contribution to the INTIMATE project of the INQUA Palaeoclimate Com-mission and the work is supported by a Leverhulme Trust Research project (grant allocationnumber F07537C) entitled Testing hypotheses of rapid climate change using tephrochronol-ogyrsquo SMDrsquo s contribution was completed during possession of a NERC PhD studentship(GT 0499ES162) We are extremely grateful to Dr Peter G Hill for his assistance withthe EPMA analyses at the Tephrochronology Analytical Unit University of Edinburgh We alsothank Dr G Mastrolorenzo (Vesuvius Observatory) and Miss G Swindle for assistance duringthe macreld investigations in Naples Thanks are also expressed to two anonymous reviewers forcomments on an earlier draft
Appendix A
Table 2 shows the major oxide concentrations of NYT glass shards from Procidaand Prato Spilla `Crsquo and of the Mercato Tephra from the Naples area (see x 4 forsite context) All oxides are shown as weight and total iron is expressed as FeO
Figure 8 Radiocarbon calibration curve for Termination 1 and the Early Holocene compared with theGRIP macr 18 O event stratigraphy the GRIP ss08c and GISP2 macr 18 O records (wwwngdcnoaagov) andknown tephra horizons from this period The shaded areas represent the cooler climatic episodes andare labelled with the Greenland stratotype terminology (Bjorck et al 1998) Where radiocarbon agesare reported in table 1 as a range the mean is given here Abbreviations for GRIP horizons are asfollows Un unknown (approximate positions are given (S Johnsen 2001 personal communication))SA Saksunarvatn Ash VA Vedde Ash BF Black Feather Sulphate concentrations from the GISP2record are also shown (Zielinski et al 1996) Open circles denote radiocarbon calibration data fromLake Suigetsu (Kitagawa amp van der Plicht 2000) Filled circles denote radiocarbon calibration data fromCariaco Basin assuming a marine reservoir age of 420 14 C yr (Hughen et al 1998)
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792 S M Davies and others
Tab
le2
Majo
roxi
de
con
cen
trati
on
sof
NY
Tgl
ass
shard
sfr
om
Pro
cida
an
dP
rato
Spil
laC
rsquoan
dof
the
Mer
cato
Tep
hra
from
the
Naple
sare
a(s
eex4
for
site
con
text
)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
roci
da)
1584
204
0177
634
201
106
828
635
197
5969
1W
DS
2598
603
9178
027
101
204
924
244
583
4965
8W
DS
3586
604
5173
631
100
805
924
342
183
0951
9W
DS
4583
903
9177
933
000
906
924
540
486
9958
3W
DS
5605
106
8179
126
901
204
923
243
086
1976
4W
DS
6591
704
5177
332
801
006
425
740
887
8968
0W
DS
7581
804
1178
031
501
107
125
640
086
9956
1W
DS
8589
504
2179
533
701
506
926
740
987
5970
4W
DS
9592
003
9178
135
101
007
026
443
585
7972
7W
DS
10
591
404
2174
631
601
105
723
442
482
6957
0W
DS
11
593
403
6177
131
301
506
726
439
188
5967
6W
DS
12
588
103
8176
128
100
505
525
141
583
4952
1W
DS
13
577
003
8176
533
500
807
228
140
384
8952
0W
DS
14
586
004
7179
735
300
706
827
842
984
6968
5W
DS
15
588
104
2180
629
400
505
924
937
993
0964
5W
DS
16
579
603
9178
536
501
308
228
836
087
1959
9W
DS
17
580
103
9177
631
500
907
327
039
488
9956
6W
DS
mea
n588
104
2177
631
901
006
525
940
686
9962
8
sd
(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(07
8)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 793
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
rato
Spil
laC
rsquo)
1552
105
4177
247
401
914
38
735
578
9951
1W
DS
2557
305
7179
845
701
512
640
136
581
5960
6W
DS
3595
004
4173
724
302
003
117
652
877
8950
7W
DS
4575
704
2179
433
001
406
627
043
083
6953
7W
DS
5599
904
0178
826
401
304
421
841
688
4966
5W
DS
6591
103
8177
826
601
105
022
443
888
8960
2W
DS
7565
304
5180
939
501
410
532
535
791
8962
1W
DS
8597
606
9180
826
501
604
821
546
684
6970
7W
DS
9571
805
6179
939
801
109
932
240
883
6964
7W
DS
10
588
603
7176
527
601
104
721
042
487
7953
3W
DS
11
559
404
9180
544
501
812
339
435
878
6957
2W
DS
12
594
704
0181
328
301
705
522
144
785
6967
9W
DS
13
611
103
7187
016
900
802
419
938
195
9975
8W
DS
14
599
204
4181
128
601
404
620
844
986
6971
6W
DS
15
601
204
4177
328
302
004
722
446
385
5972
1W
DS
16
595
104
5176
428
801
504
722
744
884
3962
8W
DS
17
603
704
1177
825
101
503
520
348
181
2965
3W
DS
18
558
704
5179
647
401
813
139
836
879
0960
7W
DS
19
589
602
8178
830
901
606
622
436
091
8960
5W
DS
20
553
606
3178
647
401
913
840
136
978
0956
6W
DS
21
579
004
0175
739
000
708
328
338
286
7959
9W
DS
mea
n582
804
6179
033
401
507
427
341
484
8962
1
sd
(1
87)
(01
0)
(02
7)
(09
2)
(00
4)
(03
9)
(08
0)
(04
9)
(05
0)
(07
0)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
794 S M Davies and others
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)
1575
202
7194
219
701
101
016
374
766
9951
8W
DS
2575
802
9194
523
902
201
520
273
564
5959
0W
DS
3574
301
4205
219
101
100
416
481
266
1965
2W
DS
4575
500
7206
018
002
000
415
181
669
3968
6W
DS
5580
000
9208
018
601
300
515
883
367
1975
5W
DS
6571
001
0206
016
101
600
515
078
967
1957
2W
DS
7577
501
1201
117
101
500
620
675
655
4950
5W
DS
8573
700
9212
717
101
900
815
187
564
2973
9W
DS
9580
301
3208
715
801
400
824
81
754
1968
1W
DS
10
574
400
6211
18
402
00
516
480
567
8971
6W
DS
11
577
200
7214
212
501
200
829
879
247
962
6W
DS
12
572
200
9211
217
301
501
15
980
465
9966
3W
DS
13
571
800
7210
417
402
201
16
184
467
2971
2W
DS
14
567
300
9208
916
901
400
917
383
262
5959
3W
DS
15
568
600
8205
918
202
101
414
682
666
6960
8W
DS
16
572
501
1211
318
202
01
215
884
364
5970
9W
DS
17
572
901
2212
916
502
101
215
883
667
2973
4W
DS
18
573
01
4211
716
301
801
416
83
365
5970
4W
DS
19
569
201
1207
418
602
101
414
982
964
961
6W
DS
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
3)
(04
2)
(01
3)
(00
1)
(00
2)
(01
)(0
39)
(01
1)
(02
5)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
References
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Hughen K A Overpeck J T Peterson L C amp Trumbore S 1996 Rapid climate changes inthe tropical Atlantic region during the last deglaciation Nature 380 5153
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Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
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Larsen G 2000 Holocene volcanism in Iceland and tephrochronology as a tool in volcanologyIn Iceland 2000 modern processes and past environments Keele University UK
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European tephrochronological framework for Termination 1 799
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Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
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Rose N L Golding P N E amp Battarbee R W 1996 Selective concentration and enumerationof tephra shards from lake sediment cores Holocene 6 243246
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Santacroce R 1987 Somma Vesuvius Quad Ric Sci 114 252
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Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 801
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Sweatman T R amp Long J V P 1969 Quantitative electron microprobe analysis of rock formingminerals J Petrol 7 332379
Turney C S M 1998 Extraction of rhyolitic ash from minerogenic lake sediments J Paleolim-nol 19 199206
Turney C S M amp Lowe J J 2001 Tephrochronology In Tracking environmental changes inlake sediments physical and chemical techniques (ed W M Last amp J P Smol) DordrechtKluwer Academic
Turney C S M Harkness D D amp Lowe J J 1997 The use of microtephra horizons tocorrelate Lateglacial lake sediments successions in Scotland J Quat Sci 12 525531
Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
van den Bogaard P amp Schmincke H 1985 A widespread isochronous Late Quaternary tephralayer in central and northern Europe Geol Soc Am Bull 96 15541571
van den Bogaard B Dordeg er W Sandgren P amp Schmincke H-U 1994 Correlating theHolocene records Icelandic tephra found in Schleswig-Holstein (northern Germany) Natur-wissenschaften 81 554556
Vernet G amp Raynal J-P 2001 Tephrostratigraphy of the Limagne revisited Implications forLateglacial and Holocene Prehistory In Tephras chronology archaeology (ed E Juvignparae ampJ-P Raynal) pp 111116 Dossiers de lrsquo ArchparaeoLogis no 1 France
Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
Vezzoli L 1991 Tephra layers in Bannock Basin (eastern Mediterranean) Mar Geol 1002134
von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
Walker M J C Bjorck S Lowe J J Cwynar L C Johnsen S Knudsen K-L WohlfarthB amp INTIMATE Group 1999 Isotopic events in the GRIP ice core a stratotype for the LatePleistocene Quat Sci Rev 18 11431150
Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
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Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
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European tephrochronological framework for Termination 1 781
(Wastegard et al 2000b) A more recent discovery of a relatively high concentrationof rhyolitic VA glass shards in the northern Netherlands indicates that the ash maywell have been dispersed much further south than previously thought (S M Davies2002 unpublished work) Finally glass shards assigned to the VA have also beendiscovered in the GRIP ice core and dated to 11 980 sect 80 GRIP yr BP (Gronvold etal 1995) This discovery is extremely important for it indicates that the VA maywell provide a reliable time-parallel marker horizon between ice-core marine andterrestrial records
Two other important Icelandic ash layers the Borrobol and Saksunarvatn Tephraswere deposited near the beginning and end of the Last TerminationEarly Holoceneinterval respectively The Borrobol Tephra was discovered for the shy rst time in lakesediments in several sites in Scotland and as yet is known only in micro-tephra formIt has been dated in Scottish sites to ca 123 14C ka BP (Turney et al 1997) Whatis thought to be a contemporaneous tephra has been detected in marine sedimentson the North Icelandic shelf (Eirplusmn ksson et al 2000) This certainly has a very similargeochemical composition to those reported from Scotland but the horizon in whichit was discovered on the North Iceland plateau has been dated to 134 14C ka Theage discrepancy between the Scottish and Icelandic Borrobol Tephra layers may wellreregect the inreguence of a marine reservoir error although the possibility that severaltephras with similar geochemical composition were erupted over a period exceeding1000 yr cannot be ruled out (Larsen 2000)
The Saksunarvatn Ash appears to have been one of the largest Holocene eruptionsin Iceland It has a tholeiitic basaltic composition which is considered to indicate anorigin in the Grimsvotn or Kverfjoll complex (shy gure 3) (Mangerud et al 1986) Layersof this ash have been identishy ed in sites on the Faroe Islands (Mangerud et al 1986Dugmore amp Newton 1998 Wastegard et al 2001) the Shetland Isles (Bennet et al 1992) northern Germany (Merkt et al 1993) western Norway (micro-tephra) (Birkset al 1996) and in the GRIP (Gronvold et al 1995) and NordGRIP ice cores (S MDavies 2002 unpublished work) It has been dated to between 9060 and 8930 14C kaBP (Birks et al 1996) in Norway and to ca 10 240 sect 30 GRIP yr BP in the GRIPice core (Gronvold et al 1995) The Saksunarvatn Ash may thus provide a secondimportant widespread time-parallel marker between ice-core marine and terrestrialrecords
Other Icelandic tephras of rhyolitic amacr nity are less well known in terms of theirdistribution and geochemical variation The Hogstorpsmossen Tephra reported fromSweden (Bjorck amp Wastegard 1999) and the L3754 tephra discovered in the FaroeIslands (Dugmore amp Newton 1998) are known from single sites only and so theirpotential for tephrostratigraphy is uncertain at present Furthermore the geochem-ical spectrum of the Hogstorpsmossen Tephra is based on a small dataset with lowanalytical totals
A number of tephras of basaltic composition have originated from Iceland buttheir distributions are largely conshy ned to Iceland or to marine cores collected fromclose to the Iceland coast or in the North Atlantic These include the tephras listedas 1-THOL-1 1-THOL-2 KOL-GS-2 GS-2BAS-1 GS-2BAS-2 GS-2BAS-3 andGS-2BAS-4 in table 1 (Kvamme et al 1989 Bjorck et al 1992 Eirplusmn ksson et al 2000 Haregidason et al 2000) The shy rst two in this list are tholeiitic basaltic tephrasassociated with the VA in a complex series of tephras collectively termed NorthAtlantic Ash Zone 1 (NAAZ1) which has been detected in numerous marine cores
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782 S M Davies and others
from the North Atlantic Initially thought to represent a single eruption analysisof high-resolution sediment sequences from Lake Torfadalsvatn in northern Iceland(Bjorck et al 1992) the Hebridean Shelf near NW Scotland (Austin amp Kroon 1996)the St Kilda Basin (Hunt et al 1995) and the open North Atlantic (Bond et al 2001)has demonstrated that NAAZ1 comprises a series of distinct ashes that probablyreregect separate eruption events 1-THOL-1 is thought to originate from Veidivotn(shy gure 3) while Grimsvotn may have been the source of 1-THOL-2 (Kvamme et al 1989)
KOL-GS-2 is also of tholeiitic basaltic composition but is thought to originatefrom the Kolbeinsey Ridge system (Eirplusmn ksson et al 2000) To date this tephra hasbeen detected in one marine core only within the same record on the North Ice-landic shelf as that from which the correlative of the Borrobol Tephra was alsoreported (Eirplusmn ksson et al 2000) GS-2BAS-1 to GS-2BAS-4 are of uncertain ori-gin but are thought to have been deposited at roughly the same time as KOL-GS-2(ca 134 14C ka BP (Haregidason et al 2000))
The limited distribution of these basaltic tephras a feature that is not unique toIcelandic basaltic material may reregect two factors the relative magnitude of the vol-canic eruptions from which they were derived and the limited aerial transportationof basaltic glass which is denser than rhyolitic material However a rather surpris-ing recent discovery is that of visible basaltic VA in a site on the Isle of Skye inthe Inner Hebrides Scotland (shy gure 5) (Davies et al 2001) All other occurrencesof VA in Scotland are exclusively of rhyolitic material and in micro-tephra formonly (Turney et al 1997 Turney 1998) Clearly basaltic tephra must have beentransported subaerially as far south as Skye and the reason why it has not beendetected at other sites in Scotland is puzzling We suspect that this partly reregectsthe laboratory methods employed to separate glass shards present in low concentra-tion within a micro-tephra layer from the host sediment The technique used is adensity-separation (regotation) procedure (Turney 1998) and as basaltic shards havea specishy c density similar to quartz one of the most abundant minerals in lake sedi-ments of Late Glacial age basaltic material is dimacr cult to detect using this methodThis hypothesis is currently under investigation and alternative detection methodsare being explored including magnetic separation (Mackie et al 2002)
Several other events listed in table 1 that are of probable Icelandic origin includetephras recorded in the GRIP ice core including visible (eg the `Black Featherrsquo)tephras as well as uncertain tephras inferred from distinct Ca peaks (S Johnsen2001 personal communication) No glass shards have yet been detected in the latterbut a volcanic origin is assumed because high Ca peaks are associated with knowntephras in other Greenland ice cores (S Johnsen 2001 personal communication)These are referred to as `unknownrsquo in table 1 No geochemical analyses are availablefrom these horizons so their origin must remain speculative but a possible source isIceland in view of its proximity to the Greenland ice sheet and assumed atmosphericcirculation patterns
(b) Eifel province
There are two prominent tephra events dated to the Termination 1Early Holocenetime-span that originated from the Eifel province the Laacher See Tephra (LST)and the Ulmener Maar Tephra (UMT) Visible occurrences of the LST indicate that
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European tephrochronological framework for Termination 1 783
Vedde Ash
615 625 635 645 655depth (cm)
organic lake mudsHolocene
silty clayGS-1Younger Dryas
organic lake mudsGI-1Alleroslashd
100 microm
(a)
(b)
Figure 5 (a) Photograph of the visible VA layer discovered at Loch Ashik Isle of Skye InnerHebrides Scotland (b) Light microscope photograph showing the rich content of basaltic shards(examples are indicated by the arrows) within this layer (8024 m m size fraction)
this ash was dispersed over much of central Europe (van den Bogaard amp Schmincke1985 Friedrich et al 1999 Litt amp Stebich 1999) The LST is dated by radiocarbonto ca 110 14C ka BP (van den Bogaard amp Schmincke 1985) and to 11 063sect12 14C BP(Friedrich et al 1999) by varve chronology to 1288 varve ka BP (Brauer et al 1999Litt et al 2001) and by ArAr dating to 129 ka cal BP (van den Bogaard 1995) Ithas a phonolitic composition and is thought to have originated from a plinian andphreatomagmatic eruption with the distal ash being carried in three distinct plumesone to the northeast towards Poland one to the west and the third to the southcovering the Jura Mountains and north Italy (van den Bogaard amp Schmincke 1985Juvigne et al 1995 Bossuet et al 1997) This pattern is thought to reregect altitu-dinal variations in the predominant wind direction Sedimentary sequences near thevolcanic source indicate that the LST consists of three main layers which represent
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784 S M Davies and others
dinoterent eruption phases These are grouped together as the Laacher See TephraFormation but the three individual units can be traced within and between a seriesof depositional fans The geochemical data obtained from these three LST layersshow signishy cant variations as reregected in the ternary plots (shy gure 4)
The Early Holocene Ulmener Maar Tephra (UMT) is of rhyolitic composition andappears to be restricted to sites in Germany though this conclusion is also based onrecords of visible tephras only It is dated to ca 956 14C ka BP and to 110 varve ka(Zolitschka et al 1995 Litt et al 2001)
(c) Massif Central province
The Massif Central tephras are mainly of basaltic trachyandesitic compositionwhich is distinct from the other ash provinces (shy gures 3 and 4) and their known dis-tributions are mostly conshy ned to the Massif Central region The ages of the MassifCentral tephras are based on radiocarbon dates obtained from mire and lake sedi-ments which `bracketrsquo the tephras The La Nugsup3ere Tephra with an age of 114 14C kaBP is the oldest Massif Central tephra identishy ed so far within the time-span of inter-est (Etlicher et al 1987 Juvigne et al 1996) The two Godivelle Tephras (5 and 4)are close in age but extensive radiocarbon dating suggests distinct ages of 107and 103 14C ka BP respectively (Juvigne et al 1996) The age of the Puy de DomeTephra is less certain as the estimate is based on only one radiocarbon date froma site in the southern Chaplusmn ne des Puys (table 1) This tephra is thought to havea trachyte composition (Juvigne 1993) although no major element concentrationshave yet been published
The ChopineKilianVasset tephras are thought to be derived from three separateEarly Holocene eruptions although the stratigraphic succession is not known atpresent These trachytic tephras have been radiocarbon dated to ca 854sect150 14C kaBP but are thought to have erupted separately within ca 260 yr (Juvigne et al 1996) This series of tephras is considerably more widespread than the others fromthe region having been identishy ed as far east as the Jura Mountains (Martini amp Duret1965 Martini 1970) Some other ash falls that originated from the Chaplusmn ne des Puysappear to be of local importance only (Vernet et al 1998 Vernet amp Raynal 2001)Geochemical data are currently available for only three of the Massif Central tephrasand so far as is known no attempt has yet been made to identify these tephras inmicro-tephra form
(d ) Italian provinces
The Italian tephras from this period can be assigned to three main volcanic com-plexes the Campanian volcanic shy elds around Naples Etna on Sicily and the AeolianIslands The Campanian complex which includes the Phlegrean Fields Vesuviusand Ischia is mainly trachytic in composition with a geochemical spectrum that isquite distinct from those of the Etna complex and of the Aeolian Islands (shy gure 3)Tephras originating from one or more of these three complexes have been detectedin marine cores from the Tyrrhenian and Adriatic seas as well as other parts of theMediterranean Sea (Keller et al 1978 Paterne et al 1986 1988 1990 Langone etal 1996) and in lake sequences in southern Italy such as Lago Grande di Monticchio(Newton amp Dugmore 1993 Narcisi 1996 Allen et al 1999) and central Italy such asLago Albano near Rome (Calanchi et al 1996) Some work has also been conducted
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European tephrochronological framework for Termination 1 785
in or close to the volcanic source areas in an attempt to establish the full sequenceof volcanic eruptions during the Late Quaternary (see for example Di Vito et al 1999) There are nine Italian tephras reported from marine and lake sequences thatdate from the period between 185 and 80 14C ka BP In all instances the recordsare of visible layers of tephra The ages of some of these are poorly established atpresent with conregicting data obtained from dinoterent sites The ages suggested intable 1 are those favoured in the most recent publications but these may requirere-assessment in the light of future research
The two oldest known tephras in the time-period of interest are the L9 and Green-ish Tephras both recorded as separate features within the annually laminated Lagodi Monticchio maar sequence The lowest of the two L9 is considered to be the cor-relative of the `basalrsquo plinian eruption of Vesuvius (Narcisi 1996) Age estimates ofa palaeosol that underlies the Vesuvius tephra sequence are ca 1617 14C ka BP forthis event (Delibrias et al 1979) L9 has a trachytic composition very similar to theGreenish Tephra (table 1) However L9 which is also a product of Vesuvius is foundstratigraphically below the Greenish Tephra in the Lago di Monticchio core TheGreenish Tephra is dated in the Monticchio sequence to 17 560 varve yr BP (Allenet al 1999) and has a calibrated radiocarbon age estimate of 17 830 sect 300 cal BP(Andronico et al 1995) Both tephras have a dominantly eastwards dispersal basedon the occurrences of visible layers (Santacroce 1987 Narcisi 1996) Both tephrasalso have a trachytic composition and as can be seen from table 1 the reportedgeochemical spectra are very close indeed with the standard deviations overlappingfor almost every major element This could present problems for tephrostratigra-phy where only one of the tephras is evident in a sediment sequence in particularbecause they are so close in age This is a good example of where an analysis oftrace and rare earth elements might be required to make a clear distinction betweentephras with very similar major oxide concentrations
The Y-1 Tephra also termed the Biancavilla Montalto Ignimbrite (Vezzoli 1991)is a product of Etna and has been identishy ed as a visible benmoritic tephra horizonthroughout the central Mediterranean (Paterne et al 1988) including central Italyand the Adriatic Sea (Vezzoli 1991 Narcisi 1993 Calanchi et al 1996) It has anestimated age of ca 140 14C ka BP The Unita dei Tefra Superiori tephra which hasbeen detected as far east as Lago di Monticchio in south-central Italy (Narcisi 1996)is also dated to ca 140 14C ka BP (Alessio et al 1976) but it is thought that thesource of this tephra lies in the Phlegrean Fields No geochemical data are availablefrom the presumed source region|the data reported in table 1 were obtained fromthe Lago di Monticchio record (Narcisi 1996)
The NYT which is equivalent to the C-2 tephra reported from various marinesequences has also been traced throughout central Italy and the Adriatic Sea (Pat-erne et al 1988 Calanchi et al 1996 Di Vito et al 1999) (shy gure 2) In the centralApennines region it formed the parent material for a soil that started to developat the beginning of the Holocene period (Frezzotti amp Narcisi 1996) Also originatingfrom the Campi Flegrei caldera it is dated to ca 120 14C ka BP (Di Vito et al 1999) Published geochemical data based on EDS indicate three dinoterent geochemicalpopulations varying from latite to phonotrachyte in composition (Orsi et al 1992Paterne et al 1988) (table 1) We report in x 4 of this paper on new data obtainedfrom the NYT by WDS and it is the mean of these new data that is included intable 1 Comparisons with the previously published EDS data are provided (table 1)
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786 S M Davies and others
The new data indicate clearly that the NYT originated from the Campanian volcaniccentre
In the interval between the dispersal of the NYT (ca 120 14C ka BP) and 95 14Cka BP there appear to have been as many as 34 eruptions in the Campi Flegrei caldera(Di Vito et al 1999) Of these only one appears to have been detected widely in theregion the Pomici Principali (also termed the Agnano Formation or C-1 tephra inmarine records (Paterne et al 1988) This was the product of the highest magnitudeeruption from this epoch and is dated to between 976 sect 300 and 1032 sect 50 14C kaBP (Delibrias et al 1979 Di Vito et al 1999) or to 122 varve ka BP based on theMonticchio varve chronology (Allen et al 1999) It is trachytic in composition andappears to have had a mainly eastwards dispersal
The Mercato Tephra dated to ca 80 14C ka BP and originally analysed usingEDS has a phonolitic composition and is believed to have been generated by Vesu-vius (Paterne et al 1988) New WDS data obtained from reference samples col-lected from an exposure to the west of Naples support these conclusions (table 1 andAppendix A) The silica content of the WDS analyses are ca 3 lower than thoseobtained using EDS (table 1) which may reregect the fact that the EDS data werenormalized
The only tephra listed in table 1 that is thought to have originated from the AeolianIslands is the Pollara pumice also referred to as the E2 tephra in marine sequences(Paterne et al 1986 1988) The limited geochemical data available so far suggest itto be the only Italian tephra listed in table 1 that is rhyolitic in composition Littlemore is known about this ash which has not been recorded extensively except thatits age is estimated to be ca 130 14C ka BP (Keller 1980)
5 Extending the known distributions of European tephras
Figure 2 summarizes schematically the known distributions of three of the tephrasreferred to in the preceding section the VA the LST and the NYT Following theintroduction of a laboratory method that enables the detection of micro-tephra parti-cles in mineral-rich sediment the VA has been traced to sites that are located muchfarther south (into The Netherlands) and east (as far as St Petersburg) than thedistribution limits based on occurrences of visible layers of the ash As a result con-tinental sequences over a much larger area in northern Europe can now be correlateddirectly with marine and ice-core records using the VA as a time-parallel marker
This suggests therefore that other prominent ash layers such as the LST andNYT should also be detectable over larger tracts of Europe than is presently thecase if suitable sites are examined for the presence of micro-tephra horizons To testthis assertion we examined lake sediment deposits of Last Termination age froma site in the northern Apennines in order to establish whether the NYT could bedetected in micro-tephra form The site selected Prato Spilla `Crsquo lies well to thenorth of the localities in central and southern Italy and in the Adriatic Sea fromwhich visible records of the NYT have been reported Prato Spilla `Crsquo lies at an alti-tude of ca 1350 m in the Appennino Parmense ca 60 km south of Parma and 15 kmeast of Pontremoli The site contains a continuous sediment sequence spanning theLast Termination and most of the Holocene Detailed pollen and coleopteran strati-graphical records which have been radiocarbon dated have been published for thissite (Lowe 1992 Ponel amp Lowe 1992 Lowe amp Watson 1993)
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European tephrochronological framework for Termination 1 787
Figure 6 Light microscope photograph of an NYT glass shard from Prato Spilla Crsquosequence assigned on geochemical grounds to the NYT
The methods adopted for sub-sampling of the Prato Spilla `Crsquo sequence for thequantishy cation of glass shard concentrations and for subsequent electron microprobeanalysis of selected glass shards followed those described elsewhere (Turney 1998)In summary contiguous samples of 1 cm stratigraphic interval were extracted fromthe sequence to establish presenceabsence of glass shards Each of the 1 cm3 blocksin which tephra particles was detected was then examined with more care andshard concentrations were quantishy ed for each sub-sample Micro-tephra particleswere detected in shy ve samples (shy gure 6) but were predominantly clustered around500 cm in the part of the sequence assigned on pollen-stratigraphic grounds to theLate Glacial Interstadial or the `Allerfrac12drsquo|indeed the part of the succession in whichthe NYT would be expected to occur Peak concentrations of micro-tephra particlesreach 225 shards cmiexcl3 and are conshy ned to a single 1 cm thick sample in the sequencewhich probably represents the time of maximum deposition of the ash
Electron microprobe measurements based on WDS were obtained from the surfacesof 21 separate glass shards extracted from the sample with peak shard concentrations(Appendix A) Since only EDS measurements were available for the NYT prior to thepresent study we also obtained WDS measurements from 17 shards extracted fromthe visible layer of NYT that is exposed on Procida Island which lies in the type-locality for the NYT close to the city of Naples (Appendix A) The results providenot only a more comprehensive geochemical dataset for the NYT than was previ-ously available but also a consistent basis for comparison with the Prato Spilla `Crsquodataset All of the WDS data reported here (Appendix A) were measured at the samelaboratory (Tephrochronology Analytical Unit University of Edinburgh) using thesame sample pretreatment and preparation protocol The WDS results for the NYTdinoter to a minor degree from the EDS results (table 1 and Appendix A) especiallywith respect to the amounts of silica aluminium and calcium measured The EDS
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788 S M Davies and others
4 8FeO ()
TiO
2 (
) Neapolitan Yellow Tuff(Procida)Neapolitan Yellow Tuff(Prato Spilla lsquoCrsquo)
0
1
2
3
40 50 60 70
MgO
(
)
SiO2 ()
K2O
(
)
40 50 60 70
0
04
08
4
8
12
SiO2 ()
(a)(b)
(c)
Figure 7 Bi-plots of SiO2 K2 O SiO2 MgO and FeOTiO2 for the WDS analyses obtainedfrom glass shards of the NYT from Procida (Naples) and Prato Spilla Crsquo Means and standarddeviations are shown
results show a higher degree of statistical scatter than the WDS measurements whichmay reregect the fact that the data were normalized combined with the inreguence ofvariation in water content between shards
There is a very close correspondence between the WDS data for the Prato Spilla `Crsquomicro-tephra shards and those obtained from the type-material near Naples (shy g-ure 7) The geochemical data strongly suggest therefore that the NYT is representedat the Prato Spilla `Crsquo site by a discrete layer of micro-tephra particles This conclu-sion is compatible with the pollen-stratigraphic data from the site and accords withage estimates for the NYT (ca 120 14C ka BP) obtained from other sites (Paterneet al 1990)
These results encourage us to believe that many if not all of the tephras listedin table 1 will be detectable over much larger tracts of Europe than is presently thecase if appropriate research is undertaken to detect layers of micro-tephra particlesin selected sites The authors are presently engaged in a major continent-wide pro-gramme of research in collaboration with a number of European research groupsdesigned to test this hypothesis The focus in this research is on those parts of Europewhere we expect to shy nd overlapping `apronsrsquo of tephra deposition originating fromthe Italian Eifel Massif Central and Icelandic provinces For example a number ofsites in parts of southern France northern Italy and perhaps western Switzerlandmay have received inreguxes of micro-tephra originating from the Italian and Eifelprovinces and perhaps also from the Massif Central Sites in parts of Germany Den-mark and southern Sweden for example may in turn have received tephra depositsfrom both of the Icelandic and Eifel provinces If this proves to be the case then thestage will be set for the construction of a tephrostratigraphical framework for Europewhich will enable Last Termination sequences to be correlated on a continent-widebasis using micro- and visible tephra layers as time-parallel stratigraphic markersFurthermore there is also the possibility that other tephras remain to be discovered
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European tephrochronological framework for Termination 1 789
those which either because of the magnitude or nature of some volcanic eruptionswere distributed over parts of Europe in micro-tephra form only
6 European tephrostratigraphy and the chronology of eventsduring the Last Termination and Early Holocene
One of the crucial issues in Late Quaternary palaeoenvironmental research thatremains to be resolved is the degree to which climatic events inferred from oceanicterrestrial and ice-core records were synchronous during the Last Termination andEarly Holocene If the ice-core records provide realistic estimates of the rates anddurations of climatic events during this period then comparisons between individ-ual records have to be enotected with at least a decadal precision The problem thispresents and the role that tephrostratigraphy can play in resolving some of thedimacr culties involved are put into perspective in shy gure 8
Figure 8 shows some of the data used to calibrate radiocarbon dates (the LakeSuigetsu and Cariaco Basin datasets) plotted against the GRIP ss08c ice-core recordof macr 18O variations The latter has been selected by the INTIMATE group as an arbi-trary and temporary standard for this period and used to deshy ne an event stratig-raphy scheme (shy gure 1) for the Last Termination (see Bjorck et al 1998 Walker etal 2001) As has been alluded to in earlier sections of this paper the uncertaintiesassociated with all of the dating methods currently employed preclude precise com-parisons of ice-core marine and terrestrial records Oceanic and terrestrial recordsmostly rely upon radiocarbon dating locally supplemented in a few cases by varvechronology Imprecisions in radiocarbon dates can arise through site-specishy c fac-tors (eg hard-water or mineral carbon errors in freshwater sequences and reservoirerrors in marine sequences) sample selection laboratory measurements of 14C activ-ity and other factors (Lowe amp Walker 2000) Further imprecision may be introducedby the calibration of radiocarbon dates since the uncertainties in the dataset usedto calibrate pre-Holocene radiocarbon dates INTCAL98 are far higher than forthe Holocene which is based on dendro-calibration (Stuiver et al 1998) There arealso uncertainties anotecting varve chronologies while the ss08c ice-core chronologyfor the Last Termination dinoters signishy cantly from the GISP2 record and indeedfrom other models of the GRIP record (Lowe et al 2001) Published comparisonsbetween ice-core marine and terrestrial records for the Last Termination seldom takeinto account the true magnitude of the dating uncertainties involved and frequentlyemploy circular reasoning
Figure 8 shows the positions on the radiocarbon time-scale of 20 of the tephrasdiscussed earlier in this paper these being the ones for which reasonably conshy dentradiocarbon age estimates can be made (though these will be subject to revised esti-mates in the future) A high number of these occur in the period 14080 14C kaBP but we conshy dently anticipate the discovery in the future of additional tephras(perhaps in micro-tephra form only) which will date to the period 185140 14C kaBP Tephras detected in the GRIP ice core over the same time-interval are plottedon the calendar time-scale in shy gure 8 By providing key `time-linesrsquo between recordstephrostratigraphy can help to resolve some of the dating uncertainties referredto earlier by for example enabling direct comparisons of discrepant age estimatesobtained using dinoterent methods (cf Litt et al 2001) It can also provide estimatesof the magnitudes of the reservoir errors that anotected various marine sectors at dif-
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790 S M Davies and others
-44
-40
-36
-32
cale
ndar
yea
rs B
P
8000
9000
10 0
00
11 0
00
12 0
00
13 0
00
14 0
00
15 0
00
16 0
00
17 0
00
18 0
00
14C age (BP)
VA
SA
Un
Un
Un
Un
Un
BF
Hol
ocen
eG
S-1
GI-
1aG
I-1b
GI-
1cG
I-1d
GI-
1eG
S-2
aG
S-2
bG
S-
2c
Bor
robo
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cher
See
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ivel
le 5
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de D
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L-1
Saks
unar
vatn
Houmlg
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psm
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nU
lmen
er M
aar
amp L
3574
radiocarbon dated European tephra horizons
Cho
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Kili
an V
asse
tM
erca
to
God
ivel
le 4
Pom
ici P
rinc
ipal
i amp V
edde
Polla
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-GS-
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GS
-2B
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-2B
AS-
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nita
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Tef
raSu
peri
ori amp
laye
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Gre
enis
h
L9
20 0
0018
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16 0
0014
000
12 0
0010
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800
600
400
200 0
GISP2 volcanicsulphate conc (ppb)
1000
Nea
polit
an Y
ello
w T
uff
GISP2 18O (permil) dGRIP 18O (permil) d
Figure 8 For description see opposite
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 791
ferent times through a comparison of radiocarbon dates obtained from marine andterrestrial horizons in which the same tephra has been detected (see for exampleAustin et al 1995 Bondevik et al 2001 Haregidason et al 2000) Tephrostratigraphymay provide an independent test of suggestions that some of the climatic changesduring the Last Termination were time-transgressive as illustrated for some appar-ently contrasting climatic trends in Iceland Britain and NW Russia (Lowe 2001) Ofparticular importance as far as establishing `leadsrsquo and `lagsrsquo in climatic changes isconcerned are the tephra records from the Greenland ice cores The discovery of theVedde and Saksunarvatn ashes in the GRIP record (Gronvold et al 1995) alreadyprovides a basis for making direct comparisons between marine terrestrial and ice-core records It is a matter of some urgency that the incidence of tephra depositsin the Greenland ice cores be more fully explored in the hope that this will lead tothe recognition of additional time-parallel links between the ice-core records on theone hand and oceanic and terrestrial records on the other An investigation of thenew NordGRIP record for this purpose is currently in progress (S M Davies 2002unpublished data)
Finally a fuller and more reshy ned tephrostratigraphical scheme for Europe will alsohave other applications It will provide an important database for those investigatingthe timing and frequency of volcanic eruptions in Europe during the past 20 000 yror so as well as of the geochemical evolution of the dinoterent volcanic centres overthat period A fuller record of the distribution of micro-tephras may also provideinformation on atmospheric circulation patterns during the dispersal and depositionperiods as well as on the nature and altitude of the eruption columns which mayin turn provide inferences about magma viscosity
This paper is a contribution to the INTIMATE project of the INQUA Palaeoclimate Com-mission and the work is supported by a Leverhulme Trust Research project (grant allocationnumber F07537C) entitled Testing hypotheses of rapid climate change using tephrochronol-ogyrsquo SMDrsquo s contribution was completed during possession of a NERC PhD studentship(GT 0499ES162) We are extremely grateful to Dr Peter G Hill for his assistance withthe EPMA analyses at the Tephrochronology Analytical Unit University of Edinburgh We alsothank Dr G Mastrolorenzo (Vesuvius Observatory) and Miss G Swindle for assistance duringthe macreld investigations in Naples Thanks are also expressed to two anonymous reviewers forcomments on an earlier draft
Appendix A
Table 2 shows the major oxide concentrations of NYT glass shards from Procidaand Prato Spilla `Crsquo and of the Mercato Tephra from the Naples area (see x 4 forsite context) All oxides are shown as weight and total iron is expressed as FeO
Figure 8 Radiocarbon calibration curve for Termination 1 and the Early Holocene compared with theGRIP macr 18 O event stratigraphy the GRIP ss08c and GISP2 macr 18 O records (wwwngdcnoaagov) andknown tephra horizons from this period The shaded areas represent the cooler climatic episodes andare labelled with the Greenland stratotype terminology (Bjorck et al 1998) Where radiocarbon agesare reported in table 1 as a range the mean is given here Abbreviations for GRIP horizons are asfollows Un unknown (approximate positions are given (S Johnsen 2001 personal communication))SA Saksunarvatn Ash VA Vedde Ash BF Black Feather Sulphate concentrations from the GISP2record are also shown (Zielinski et al 1996) Open circles denote radiocarbon calibration data fromLake Suigetsu (Kitagawa amp van der Plicht 2000) Filled circles denote radiocarbon calibration data fromCariaco Basin assuming a marine reservoir age of 420 14 C yr (Hughen et al 1998)
Phil Trans R Soc Lond A (2002)
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792 S M Davies and others
Tab
le2
Majo
roxi
de
con
cen
trati
on
sof
NY
Tgl
ass
shard
sfr
om
Pro
cida
an
dP
rato
Spil
laC
rsquoan
dof
the
Mer
cato
Tep
hra
from
the
Naple
sare
a(s
eex4
for
site
con
text
)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
roci
da)
1584
204
0177
634
201
106
828
635
197
5969
1W
DS
2598
603
9178
027
101
204
924
244
583
4965
8W
DS
3586
604
5173
631
100
805
924
342
183
0951
9W
DS
4583
903
9177
933
000
906
924
540
486
9958
3W
DS
5605
106
8179
126
901
204
923
243
086
1976
4W
DS
6591
704
5177
332
801
006
425
740
887
8968
0W
DS
7581
804
1178
031
501
107
125
640
086
9956
1W
DS
8589
504
2179
533
701
506
926
740
987
5970
4W
DS
9592
003
9178
135
101
007
026
443
585
7972
7W
DS
10
591
404
2174
631
601
105
723
442
482
6957
0W
DS
11
593
403
6177
131
301
506
726
439
188
5967
6W
DS
12
588
103
8176
128
100
505
525
141
583
4952
1W
DS
13
577
003
8176
533
500
807
228
140
384
8952
0W
DS
14
586
004
7179
735
300
706
827
842
984
6968
5W
DS
15
588
104
2180
629
400
505
924
937
993
0964
5W
DS
16
579
603
9178
536
501
308
228
836
087
1959
9W
DS
17
580
103
9177
631
500
907
327
039
488
9956
6W
DS
mea
n588
104
2177
631
901
006
525
940
686
9962
8
sd
(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(07
8)
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 793
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
rato
Spil
laC
rsquo)
1552
105
4177
247
401
914
38
735
578
9951
1W
DS
2557
305
7179
845
701
512
640
136
581
5960
6W
DS
3595
004
4173
724
302
003
117
652
877
8950
7W
DS
4575
704
2179
433
001
406
627
043
083
6953
7W
DS
5599
904
0178
826
401
304
421
841
688
4966
5W
DS
6591
103
8177
826
601
105
022
443
888
8960
2W
DS
7565
304
5180
939
501
410
532
535
791
8962
1W
DS
8597
606
9180
826
501
604
821
546
684
6970
7W
DS
9571
805
6179
939
801
109
932
240
883
6964
7W
DS
10
588
603
7176
527
601
104
721
042
487
7953
3W
DS
11
559
404
9180
544
501
812
339
435
878
6957
2W
DS
12
594
704
0181
328
301
705
522
144
785
6967
9W
DS
13
611
103
7187
016
900
802
419
938
195
9975
8W
DS
14
599
204
4181
128
601
404
620
844
986
6971
6W
DS
15
601
204
4177
328
302
004
722
446
385
5972
1W
DS
16
595
104
5176
428
801
504
722
744
884
3962
8W
DS
17
603
704
1177
825
101
503
520
348
181
2965
3W
DS
18
558
704
5179
647
401
813
139
836
879
0960
7W
DS
19
589
602
8178
830
901
606
622
436
091
8960
5W
DS
20
553
606
3178
647
401
913
840
136
978
0956
6W
DS
21
579
004
0175
739
000
708
328
338
286
7959
9W
DS
mea
n582
804
6179
033
401
507
427
341
484
8962
1
sd
(1
87)
(01
0)
(02
7)
(09
2)
(00
4)
(03
9)
(08
0)
(04
9)
(05
0)
(07
0)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
794 S M Davies and others
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)
1575
202
7194
219
701
101
016
374
766
9951
8W
DS
2575
802
9194
523
902
201
520
273
564
5959
0W
DS
3574
301
4205
219
101
100
416
481
266
1965
2W
DS
4575
500
7206
018
002
000
415
181
669
3968
6W
DS
5580
000
9208
018
601
300
515
883
367
1975
5W
DS
6571
001
0206
016
101
600
515
078
967
1957
2W
DS
7577
501
1201
117
101
500
620
675
655
4950
5W
DS
8573
700
9212
717
101
900
815
187
564
2973
9W
DS
9580
301
3208
715
801
400
824
81
754
1968
1W
DS
10
574
400
6211
18
402
00
516
480
567
8971
6W
DS
11
577
200
7214
212
501
200
829
879
247
962
6W
DS
12
572
200
9211
217
301
501
15
980
465
9966
3W
DS
13
571
800
7210
417
402
201
16
184
467
2971
2W
DS
14
567
300
9208
916
901
400
917
383
262
5959
3W
DS
15
568
600
8205
918
202
101
414
682
666
6960
8W
DS
16
572
501
1211
318
202
01
215
884
364
5970
9W
DS
17
572
901
2212
916
502
101
215
883
667
2973
4W
DS
18
573
01
4211
716
301
801
416
83
365
5970
4W
DS
19
569
201
1207
418
602
101
414
982
964
961
6W
DS
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
3)
(04
2)
(01
3)
(00
1)
(00
2)
(01
)(0
39)
(01
1)
(02
5)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
References
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Froggatt P C 1992 Standardisation of the chemical analysis of tephra deposits Report of theICCT working group Quat Int 1314 9396
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Hoek W Z amp Bohncke S J P 2001 Oxygen isotope wiggle matching as a tool for synchronisingice-core and terrestrial records over Termination 1 Quat Sci Rev 20 12511264
Hughen K A Overpeck J T Peterson L C amp Trumbore S 1996 Rapid climate changes inthe tropical Atlantic region during the last deglaciation Nature 380 5153
Hughen K A Overpeck J T amp Lehman J 1998 A new 14 C calibration data set for the LastDeglaciation Radiocarbon 39 483494
Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
Hunt J B amp Hill P G 1996 An inter-laboratory comparison of the electron probe microanalysisof glass geochemistry Quat Int 3436 229241
Hunt J B amp Hill P G 2001 Tephrological implications of beam sizesample size ereg ects inelectron microprobe analysis of glass shards J Quat Sci 16 105117
Hunt J B Fannin N G T Hill P G amp Peacock J D 1995 The tephrochronology andradiocarbon dating of North Atlantic Late Quaternary sediments an example from the StKilda Basin In The tectonics sedimentation and palaeoceanography of the North Atlanticregion (ed R A Scrutton M S Stoker G B Shimmield amp A W Tudhope) vol 90pp 227248 Geological Society of London Special Publication
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Jakobsson S P 1979 Outline of the petrology of Iceland Jokull 29 5773
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Juvignparae E 1993 Contribution microa la tparaephrostratigraphie du Quaternaire et son application microa lagparaeomorphologie Mparaem Serv Explicat Cartes Gparaeol Min Belg 36 166
Juvignparae E amp Gewelt M 1987 La Narse drsquo Ampoix comme tparaephrostratotype dans la Chasup3 ne desPuys mparaeridionale (France) Bull Ass Fr Etud Quat 29 3749
Juvignparae E Kozarski S amp Nowaczyk B 1995 The occurrence of Laacher See Tephra in Pomera-nia NW Poland Boreas 24 225231
Juvignparae E Bastin B Delibrias G Evin J Gewelt M Gilot E amp Streel M 1996 Acomprehensive pollen and tephra based chronostratigraphic model for the Lateglacial andHolocene period in the French Massif Central Quat Int 3436 113120
Keller J 1980 The island of Vulcano Rend Soc It Mineral Petrolog 36 369414
Keller J Ryan W B F Ninkovich D amp Altherr R 1978 Explosive volcanic activity in theMediterranean over the past 200 000 years as recorded in deep sea sediments Geol Soc AmBull 89 591604
Kitagawa H amp van der Plicht J 2000 Atmospheric radiocarbon calibration beyond 11 900 calBP from Lake Suigetsu laminated sediments Radiocarbon 42 369380
Kvamme T Mangerud J Furnes H amp Ruddiman W F 1989 Geochemistry of Pleistoceneash zones in cores from the North Atlantic Norsk Geol Tids 69 251272
Lacasse C Sigurdsson H Johannesson H Paterne M amp Carey S 1995 Source of Ash zone 1in the North Atlantic Bull Volcanol 57 1832
Langone L Asioli A Corregiari A amp Trincardi F 1996 Age depth modelling through theLate-Quaternary deposits of the central Adriatic Basin In Palaeoenvironmental analysis ofItalian crater lake and Adriatic sediments (ed F Oldmacreld amp P Guilizzoni) vol 55 pp 177196 Memorie dellrsquo Instituto Italiano di Idrobiologia
Larsen G 2000 Holocene volcanism in Iceland and tephrochronology as a tool in volcanologyIn Iceland 2000 modern processes and past environments Keele University UK
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 799
Litt T amp Stebich M 1999 Bio- and chronostratigraphy of the Lateglacial in the Eifel regionGermany Quat Int 61 516
Litt T Brauer A Goslar T Merkt J Balaga K Muller H Ralska-Jasiewiczowa MStebich M amp Negendank J F W 2001 Correlation and synchronisation of Lateglacialcontinental sequences in northern Central Europe based on annually laminated lacustrinesediments Quat Sci Rev 20 12331249
Long D amp Morton A C 1987 An ash fall within the Loch Lomond stadial J Quat Sci 297101
Lotter A F Eicher U Siegenthaler U amp Birks H J B 1992 Lateglacial climatic oscillationsas recorded in Swiss lake sediments J Quat Sci 7 187204
Lowe J J 1992 Lateglacial and Early Holocene lake sediments from the Northern ApenninesItaly|pollen stratigraphy and radiocarbon dating Boreas 21 193208
Lowe J J 2001 Abrupt climatic changes in Europe during the last glacialinterglacial tran-sition the potential for testing hypotheses on the synchroneity of climatic events usingtephrochronology Global Planet Change 603 7384
Lowe J J amp Turney C S M 1997 Vedde Ash layer discovered in a small lake basin on theScottish mainland J Geol Soc Lond 154 605612
Lowe J J amp Walker M J C 2000 Radiocarbon dating the last glacialinterglacial transition(ca 14914 C ka BP) in terrestrial and marine records the need for new quality assuranceprotocols Radiocarbon 42 5368
Lowe J J amp Watson C 1993 Lateglacial and Early Holocene pollen stratigraphy of the northernApennines Italy Quat Sci Rev 12 727738
Lowe J J Birks H H Brooks S J Coope G R Harkness D D Mayle F E SheldrickC Turney C S M amp Walker M J C 1999 The chronology of palaeoenvironmental changesduring the Last GlacialHolocene transition towards an event stratigraphy for the BritishIsles J Geol Soc Lond 156 397410
Lowe J J Hoek W Z amp INTIMATE group 2001 Inter-regional correlation of palaeoclimaticrecords for the Last GlacialInterglacial transition a protocol for improved precision recom-mended by the INTIMATE project group Quat Sci Rev 20 11751187
Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
Mangerud J Lie S E Furnes H Kristiansen I L amp Liquest mo L 1984 A Younger Dryas ashbed in western Norway and its possible correlation with tephra beds from the Norwegian Seaand North Atlantic Quat Res 21 85104
Mangerud J Furnes H amp Jparaohansen J 1986 A 9000 year-old ash bed on the Faroe IslandsQuat Res 26 262265
Martini J 1970 Recherche de retombparaees volcaniques dans le sud-est de la France et la Suisseoccidentale Arch Sci 23 641674
Martini J amp Duret J J 1965 Note preliminaire sur la presence drsquo un niveau de cendres vol-caniques dans des sparaediments post-glaciaires des environs de Genmicroeve Arch Sci 18 587588
Mayewski P A Meeker L D Twickler M S Whitlow S Yang Q Lyons W B amp Pren-tice M 1997 Major features and forcing of high latitudes Northern Hemisphere atmosphericcirculation using a 110 000 year long glaciochemical series J Geophys Res 102 345365
Merkt J Muller H Knabe W Muller P amp Weiser T 1993 The Early Holocene Saksunarvatntephra found in lake sediments in NW Germany Boreas 22 93100
Narcisi B 1993 Segnalazione di un livello piroclastico di provenienza etnea nellrsquo area del Fucino(Italia Centrale) Quaternario 6 8792
Narcisi B 1996 Tephrochronology of a Late Quaternary lacustrine record from the Monticchiomaar (Vulture volcano southern Italy) Quat Sci Rev 15 155165
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on September 20 2011rstaroyalsocietypublishingorgDownloaded from
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Newton A J amp Dugmore A J 1993 Tephrochronology of Core C from Lago Grande di Mon-ticchio In Paleolimnology of European Maar Lakes (ed J F W Negendank amp B Zolitschka)Lecture Notes in Earth Science vol 49 333348 Springer
Oldmacreld F Appleby P G amp Thompson R 1980 Palaeoecological studies of lakes in theHighlands of Papua New Guinea J Ecol 68 457477
Orsi G Drsquo Antonio M de Vita S amp Gallo G 1992 The Neapolitan Yellow Tureg a large mag-nitude trachytic phreatoplinian eruption eruptive dynamics magma withdrawal and calderacollapse J Volcanol Geotherm Res 53 275287
Paterne M Guichard F Labeyrie J Gillot P Y amp Duplessy J C 1986 Tyrrhenian Seatephrochronology of the oxygen isotope record for the past 60 000 years Mar Geol 72259285
Paterne M Guichard F amp Labeyrie J 1988 Explosive activity of the south Italian volca-noes during the past 80 000 years as determined by marine tephrochronology J VolcanolGeotherm Res 34 153172
Paterne M Labeyrie J Guichard F Mazaud A amp Maitre F 1990 Fluctuations of the Cam-panian explosive volcanic activity (south Italy) during the past 190 000 years as determinedby marine tephrochronology Earth Planet Sci Lett 98 166174
Pawse A Beske-Diehl S amp Marshall S A 1998 Use of magnetic hysteresis properties andelectron spin resonance spectroscopy for the identimacrcation of volcanic ash a preliminary studyGeophys J Int 132 712720
Pearce N J G Westgate J A amp Perkins W T 1996 Developments in the analysis of singleglass shards in volcanic deposits by laser ablation ICP-MS quantitative and single internalstandard multi-element methods Quat Int 3436 213227
Pearce N J G Westgate J A Perkins W T Eastwood W J amp Shane P 1999 Theapplication of laser ablation ICP-MS to the analysis of volcanic glass shards from tephradeposits bulk glass and single shard analysis Global Planet Change 21 151171
Pilcher J R amp Hall V A 1992 Towards a tephrochronology for the Holocene of the north ofIreland Holocene 2 255259
Ponel P amp Lowe J J 1992 Coleopteran pollen and radiocarbon evidence from the Prato Spillarsquo Drsquo succession N Italy C R Acad Sci Paris Sparaer II 315 14251431
Rose N L Golding P N E amp Battarbee R W 1996 Selective concentration and enumerationof tephra shards from lake sediment cores Holocene 6 243246
Ruddiman W F amp Glover L K 1972 Vertical mixing of ice rafted volcanic ash in NorthAtlantic sediments Geol Soc Am Bull 83 28172836
Ruddiman W amp McIntyre A 1981 The North Atlantic Ocean during the last deglaciationPalaeogeogr Palaeoclimatol Palaeoecol 35 145214
Santacroce R 1987 Somma Vesuvius Quad Ric Sci 114 252
Sarna-Wojcicki A 2000 Tephrochronology In Quaternary geochronology methods and applica-tions (ed J S Noller J M Sowers amp W R Lettis) AGU Reference shelf vol 4 pp 357377Washington DC American Geophysical Union
Sejrup H P Sjiquest holm J Furnes H Beyer I Eide L Jansen E amp Mangerud J 1989Quaternary tephrochronology on the Iceland Plateau north of Iceland J Quat Sci 4 109114
Sikes E L Samson C R Guilderson T P amp Howard W R 2000 Old radiocarbon agesin the southwest Pacimacrc Ocean during the last glacial period and deglaciation Nature 405555558
Stein R Nam S-I Grobe H amp Hubbersten H 1996 Late Quaternary glacial history andshort term ice rafted debris deg uctuations along the East Greenland continental marine In LateQuaternary palaeoceanography of the North Atlantic margins (ed J T Andrews W E NAustin H Bergsten amp A E Jennings) pp 135151 Geological Society London SpecialPublication
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European tephrochronological framework for Termination 1 801
Stuiver M amp Grootes P M 2000 GISP2 oxygen isotope ratios Quat Res 53 277284
Stuiver M Reimer P J Bard E Beck J W Burr G S Hughen K A Kromer BMcCormac G Van der Plicht J amp Spurk M 1998 INTCAL 98 radiocarbon age calibration24 0000 cal BP Radiocarbon 40 10411083
Sweatman T R amp Long J V P 1969 Quantitative electron microprobe analysis of rock formingminerals J Petrol 7 332379
Turney C S M 1998 Extraction of rhyolitic ash from minerogenic lake sediments J Paleolim-nol 19 199206
Turney C S M amp Lowe J J 2001 Tephrochronology In Tracking environmental changes inlake sediments physical and chemical techniques (ed W M Last amp J P Smol) DordrechtKluwer Academic
Turney C S M Harkness D D amp Lowe J J 1997 The use of microtephra horizons tocorrelate Lateglacial lake sediments successions in Scotland J Quat Sci 12 525531
Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
van den Bogaard P amp Schmincke H 1985 A widespread isochronous Late Quaternary tephralayer in central and northern Europe Geol Soc Am Bull 96 15541571
van den Bogaard B Dordeg er W Sandgren P amp Schmincke H-U 1994 Correlating theHolocene records Icelandic tephra found in Schleswig-Holstein (northern Germany) Natur-wissenschaften 81 554556
Vernet G amp Raynal J-P 2001 Tephrostratigraphy of the Limagne revisited Implications forLateglacial and Holocene Prehistory In Tephras chronology archaeology (ed E Juvignparae ampJ-P Raynal) pp 111116 Dossiers de lrsquo ArchparaeoLogis no 1 France
Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
Vezzoli L 1991 Tephra layers in Bannock Basin (eastern Mediterranean) Mar Geol 1002134
von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
Walker M J C Bjorck S Lowe J J Cwynar L C Johnsen S Knudsen K-L WohlfarthB amp INTIMATE Group 1999 Isotopic events in the GRIP ice core a stratotype for the LatePleistocene Quat Sci Rev 18 11431150
Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
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Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
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782 S M Davies and others
from the North Atlantic Initially thought to represent a single eruption analysisof high-resolution sediment sequences from Lake Torfadalsvatn in northern Iceland(Bjorck et al 1992) the Hebridean Shelf near NW Scotland (Austin amp Kroon 1996)the St Kilda Basin (Hunt et al 1995) and the open North Atlantic (Bond et al 2001)has demonstrated that NAAZ1 comprises a series of distinct ashes that probablyreregect separate eruption events 1-THOL-1 is thought to originate from Veidivotn(shy gure 3) while Grimsvotn may have been the source of 1-THOL-2 (Kvamme et al 1989)
KOL-GS-2 is also of tholeiitic basaltic composition but is thought to originatefrom the Kolbeinsey Ridge system (Eirplusmn ksson et al 2000) To date this tephra hasbeen detected in one marine core only within the same record on the North Ice-landic shelf as that from which the correlative of the Borrobol Tephra was alsoreported (Eirplusmn ksson et al 2000) GS-2BAS-1 to GS-2BAS-4 are of uncertain ori-gin but are thought to have been deposited at roughly the same time as KOL-GS-2(ca 134 14C ka BP (Haregidason et al 2000))
The limited distribution of these basaltic tephras a feature that is not unique toIcelandic basaltic material may reregect two factors the relative magnitude of the vol-canic eruptions from which they were derived and the limited aerial transportationof basaltic glass which is denser than rhyolitic material However a rather surpris-ing recent discovery is that of visible basaltic VA in a site on the Isle of Skye inthe Inner Hebrides Scotland (shy gure 5) (Davies et al 2001) All other occurrencesof VA in Scotland are exclusively of rhyolitic material and in micro-tephra formonly (Turney et al 1997 Turney 1998) Clearly basaltic tephra must have beentransported subaerially as far south as Skye and the reason why it has not beendetected at other sites in Scotland is puzzling We suspect that this partly reregectsthe laboratory methods employed to separate glass shards present in low concentra-tion within a micro-tephra layer from the host sediment The technique used is adensity-separation (regotation) procedure (Turney 1998) and as basaltic shards havea specishy c density similar to quartz one of the most abundant minerals in lake sedi-ments of Late Glacial age basaltic material is dimacr cult to detect using this methodThis hypothesis is currently under investigation and alternative detection methodsare being explored including magnetic separation (Mackie et al 2002)
Several other events listed in table 1 that are of probable Icelandic origin includetephras recorded in the GRIP ice core including visible (eg the `Black Featherrsquo)tephras as well as uncertain tephras inferred from distinct Ca peaks (S Johnsen2001 personal communication) No glass shards have yet been detected in the latterbut a volcanic origin is assumed because high Ca peaks are associated with knowntephras in other Greenland ice cores (S Johnsen 2001 personal communication)These are referred to as `unknownrsquo in table 1 No geochemical analyses are availablefrom these horizons so their origin must remain speculative but a possible source isIceland in view of its proximity to the Greenland ice sheet and assumed atmosphericcirculation patterns
(b) Eifel province
There are two prominent tephra events dated to the Termination 1Early Holocenetime-span that originated from the Eifel province the Laacher See Tephra (LST)and the Ulmener Maar Tephra (UMT) Visible occurrences of the LST indicate that
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European tephrochronological framework for Termination 1 783
Vedde Ash
615 625 635 645 655depth (cm)
organic lake mudsHolocene
silty clayGS-1Younger Dryas
organic lake mudsGI-1Alleroslashd
100 microm
(a)
(b)
Figure 5 (a) Photograph of the visible VA layer discovered at Loch Ashik Isle of Skye InnerHebrides Scotland (b) Light microscope photograph showing the rich content of basaltic shards(examples are indicated by the arrows) within this layer (8024 m m size fraction)
this ash was dispersed over much of central Europe (van den Bogaard amp Schmincke1985 Friedrich et al 1999 Litt amp Stebich 1999) The LST is dated by radiocarbonto ca 110 14C ka BP (van den Bogaard amp Schmincke 1985) and to 11 063sect12 14C BP(Friedrich et al 1999) by varve chronology to 1288 varve ka BP (Brauer et al 1999Litt et al 2001) and by ArAr dating to 129 ka cal BP (van den Bogaard 1995) Ithas a phonolitic composition and is thought to have originated from a plinian andphreatomagmatic eruption with the distal ash being carried in three distinct plumesone to the northeast towards Poland one to the west and the third to the southcovering the Jura Mountains and north Italy (van den Bogaard amp Schmincke 1985Juvigne et al 1995 Bossuet et al 1997) This pattern is thought to reregect altitu-dinal variations in the predominant wind direction Sedimentary sequences near thevolcanic source indicate that the LST consists of three main layers which represent
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784 S M Davies and others
dinoterent eruption phases These are grouped together as the Laacher See TephraFormation but the three individual units can be traced within and between a seriesof depositional fans The geochemical data obtained from these three LST layersshow signishy cant variations as reregected in the ternary plots (shy gure 4)
The Early Holocene Ulmener Maar Tephra (UMT) is of rhyolitic composition andappears to be restricted to sites in Germany though this conclusion is also based onrecords of visible tephras only It is dated to ca 956 14C ka BP and to 110 varve ka(Zolitschka et al 1995 Litt et al 2001)
(c) Massif Central province
The Massif Central tephras are mainly of basaltic trachyandesitic compositionwhich is distinct from the other ash provinces (shy gures 3 and 4) and their known dis-tributions are mostly conshy ned to the Massif Central region The ages of the MassifCentral tephras are based on radiocarbon dates obtained from mire and lake sedi-ments which `bracketrsquo the tephras The La Nugsup3ere Tephra with an age of 114 14C kaBP is the oldest Massif Central tephra identishy ed so far within the time-span of inter-est (Etlicher et al 1987 Juvigne et al 1996) The two Godivelle Tephras (5 and 4)are close in age but extensive radiocarbon dating suggests distinct ages of 107and 103 14C ka BP respectively (Juvigne et al 1996) The age of the Puy de DomeTephra is less certain as the estimate is based on only one radiocarbon date froma site in the southern Chaplusmn ne des Puys (table 1) This tephra is thought to havea trachyte composition (Juvigne 1993) although no major element concentrationshave yet been published
The ChopineKilianVasset tephras are thought to be derived from three separateEarly Holocene eruptions although the stratigraphic succession is not known atpresent These trachytic tephras have been radiocarbon dated to ca 854sect150 14C kaBP but are thought to have erupted separately within ca 260 yr (Juvigne et al 1996) This series of tephras is considerably more widespread than the others fromthe region having been identishy ed as far east as the Jura Mountains (Martini amp Duret1965 Martini 1970) Some other ash falls that originated from the Chaplusmn ne des Puysappear to be of local importance only (Vernet et al 1998 Vernet amp Raynal 2001)Geochemical data are currently available for only three of the Massif Central tephrasand so far as is known no attempt has yet been made to identify these tephras inmicro-tephra form
(d ) Italian provinces
The Italian tephras from this period can be assigned to three main volcanic com-plexes the Campanian volcanic shy elds around Naples Etna on Sicily and the AeolianIslands The Campanian complex which includes the Phlegrean Fields Vesuviusand Ischia is mainly trachytic in composition with a geochemical spectrum that isquite distinct from those of the Etna complex and of the Aeolian Islands (shy gure 3)Tephras originating from one or more of these three complexes have been detectedin marine cores from the Tyrrhenian and Adriatic seas as well as other parts of theMediterranean Sea (Keller et al 1978 Paterne et al 1986 1988 1990 Langone etal 1996) and in lake sequences in southern Italy such as Lago Grande di Monticchio(Newton amp Dugmore 1993 Narcisi 1996 Allen et al 1999) and central Italy such asLago Albano near Rome (Calanchi et al 1996) Some work has also been conducted
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European tephrochronological framework for Termination 1 785
in or close to the volcanic source areas in an attempt to establish the full sequenceof volcanic eruptions during the Late Quaternary (see for example Di Vito et al 1999) There are nine Italian tephras reported from marine and lake sequences thatdate from the period between 185 and 80 14C ka BP In all instances the recordsare of visible layers of tephra The ages of some of these are poorly established atpresent with conregicting data obtained from dinoterent sites The ages suggested intable 1 are those favoured in the most recent publications but these may requirere-assessment in the light of future research
The two oldest known tephras in the time-period of interest are the L9 and Green-ish Tephras both recorded as separate features within the annually laminated Lagodi Monticchio maar sequence The lowest of the two L9 is considered to be the cor-relative of the `basalrsquo plinian eruption of Vesuvius (Narcisi 1996) Age estimates ofa palaeosol that underlies the Vesuvius tephra sequence are ca 1617 14C ka BP forthis event (Delibrias et al 1979) L9 has a trachytic composition very similar to theGreenish Tephra (table 1) However L9 which is also a product of Vesuvius is foundstratigraphically below the Greenish Tephra in the Lago di Monticchio core TheGreenish Tephra is dated in the Monticchio sequence to 17 560 varve yr BP (Allenet al 1999) and has a calibrated radiocarbon age estimate of 17 830 sect 300 cal BP(Andronico et al 1995) Both tephras have a dominantly eastwards dispersal basedon the occurrences of visible layers (Santacroce 1987 Narcisi 1996) Both tephrasalso have a trachytic composition and as can be seen from table 1 the reportedgeochemical spectra are very close indeed with the standard deviations overlappingfor almost every major element This could present problems for tephrostratigra-phy where only one of the tephras is evident in a sediment sequence in particularbecause they are so close in age This is a good example of where an analysis oftrace and rare earth elements might be required to make a clear distinction betweentephras with very similar major oxide concentrations
The Y-1 Tephra also termed the Biancavilla Montalto Ignimbrite (Vezzoli 1991)is a product of Etna and has been identishy ed as a visible benmoritic tephra horizonthroughout the central Mediterranean (Paterne et al 1988) including central Italyand the Adriatic Sea (Vezzoli 1991 Narcisi 1993 Calanchi et al 1996) It has anestimated age of ca 140 14C ka BP The Unita dei Tefra Superiori tephra which hasbeen detected as far east as Lago di Monticchio in south-central Italy (Narcisi 1996)is also dated to ca 140 14C ka BP (Alessio et al 1976) but it is thought that thesource of this tephra lies in the Phlegrean Fields No geochemical data are availablefrom the presumed source region|the data reported in table 1 were obtained fromthe Lago di Monticchio record (Narcisi 1996)
The NYT which is equivalent to the C-2 tephra reported from various marinesequences has also been traced throughout central Italy and the Adriatic Sea (Pat-erne et al 1988 Calanchi et al 1996 Di Vito et al 1999) (shy gure 2) In the centralApennines region it formed the parent material for a soil that started to developat the beginning of the Holocene period (Frezzotti amp Narcisi 1996) Also originatingfrom the Campi Flegrei caldera it is dated to ca 120 14C ka BP (Di Vito et al 1999) Published geochemical data based on EDS indicate three dinoterent geochemicalpopulations varying from latite to phonotrachyte in composition (Orsi et al 1992Paterne et al 1988) (table 1) We report in x 4 of this paper on new data obtainedfrom the NYT by WDS and it is the mean of these new data that is included intable 1 Comparisons with the previously published EDS data are provided (table 1)
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786 S M Davies and others
The new data indicate clearly that the NYT originated from the Campanian volcaniccentre
In the interval between the dispersal of the NYT (ca 120 14C ka BP) and 95 14Cka BP there appear to have been as many as 34 eruptions in the Campi Flegrei caldera(Di Vito et al 1999) Of these only one appears to have been detected widely in theregion the Pomici Principali (also termed the Agnano Formation or C-1 tephra inmarine records (Paterne et al 1988) This was the product of the highest magnitudeeruption from this epoch and is dated to between 976 sect 300 and 1032 sect 50 14C kaBP (Delibrias et al 1979 Di Vito et al 1999) or to 122 varve ka BP based on theMonticchio varve chronology (Allen et al 1999) It is trachytic in composition andappears to have had a mainly eastwards dispersal
The Mercato Tephra dated to ca 80 14C ka BP and originally analysed usingEDS has a phonolitic composition and is believed to have been generated by Vesu-vius (Paterne et al 1988) New WDS data obtained from reference samples col-lected from an exposure to the west of Naples support these conclusions (table 1 andAppendix A) The silica content of the WDS analyses are ca 3 lower than thoseobtained using EDS (table 1) which may reregect the fact that the EDS data werenormalized
The only tephra listed in table 1 that is thought to have originated from the AeolianIslands is the Pollara pumice also referred to as the E2 tephra in marine sequences(Paterne et al 1986 1988) The limited geochemical data available so far suggest itto be the only Italian tephra listed in table 1 that is rhyolitic in composition Littlemore is known about this ash which has not been recorded extensively except thatits age is estimated to be ca 130 14C ka BP (Keller 1980)
5 Extending the known distributions of European tephras
Figure 2 summarizes schematically the known distributions of three of the tephrasreferred to in the preceding section the VA the LST and the NYT Following theintroduction of a laboratory method that enables the detection of micro-tephra parti-cles in mineral-rich sediment the VA has been traced to sites that are located muchfarther south (into The Netherlands) and east (as far as St Petersburg) than thedistribution limits based on occurrences of visible layers of the ash As a result con-tinental sequences over a much larger area in northern Europe can now be correlateddirectly with marine and ice-core records using the VA as a time-parallel marker
This suggests therefore that other prominent ash layers such as the LST andNYT should also be detectable over larger tracts of Europe than is presently thecase if suitable sites are examined for the presence of micro-tephra horizons To testthis assertion we examined lake sediment deposits of Last Termination age froma site in the northern Apennines in order to establish whether the NYT could bedetected in micro-tephra form The site selected Prato Spilla `Crsquo lies well to thenorth of the localities in central and southern Italy and in the Adriatic Sea fromwhich visible records of the NYT have been reported Prato Spilla `Crsquo lies at an alti-tude of ca 1350 m in the Appennino Parmense ca 60 km south of Parma and 15 kmeast of Pontremoli The site contains a continuous sediment sequence spanning theLast Termination and most of the Holocene Detailed pollen and coleopteran strati-graphical records which have been radiocarbon dated have been published for thissite (Lowe 1992 Ponel amp Lowe 1992 Lowe amp Watson 1993)
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European tephrochronological framework for Termination 1 787
Figure 6 Light microscope photograph of an NYT glass shard from Prato Spilla Crsquosequence assigned on geochemical grounds to the NYT
The methods adopted for sub-sampling of the Prato Spilla `Crsquo sequence for thequantishy cation of glass shard concentrations and for subsequent electron microprobeanalysis of selected glass shards followed those described elsewhere (Turney 1998)In summary contiguous samples of 1 cm stratigraphic interval were extracted fromthe sequence to establish presenceabsence of glass shards Each of the 1 cm3 blocksin which tephra particles was detected was then examined with more care andshard concentrations were quantishy ed for each sub-sample Micro-tephra particleswere detected in shy ve samples (shy gure 6) but were predominantly clustered around500 cm in the part of the sequence assigned on pollen-stratigraphic grounds to theLate Glacial Interstadial or the `Allerfrac12drsquo|indeed the part of the succession in whichthe NYT would be expected to occur Peak concentrations of micro-tephra particlesreach 225 shards cmiexcl3 and are conshy ned to a single 1 cm thick sample in the sequencewhich probably represents the time of maximum deposition of the ash
Electron microprobe measurements based on WDS were obtained from the surfacesof 21 separate glass shards extracted from the sample with peak shard concentrations(Appendix A) Since only EDS measurements were available for the NYT prior to thepresent study we also obtained WDS measurements from 17 shards extracted fromthe visible layer of NYT that is exposed on Procida Island which lies in the type-locality for the NYT close to the city of Naples (Appendix A) The results providenot only a more comprehensive geochemical dataset for the NYT than was previ-ously available but also a consistent basis for comparison with the Prato Spilla `Crsquodataset All of the WDS data reported here (Appendix A) were measured at the samelaboratory (Tephrochronology Analytical Unit University of Edinburgh) using thesame sample pretreatment and preparation protocol The WDS results for the NYTdinoter to a minor degree from the EDS results (table 1 and Appendix A) especiallywith respect to the amounts of silica aluminium and calcium measured The EDS
Phil Trans R Soc Lond A (2002)
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788 S M Davies and others
4 8FeO ()
TiO
2 (
) Neapolitan Yellow Tuff(Procida)Neapolitan Yellow Tuff(Prato Spilla lsquoCrsquo)
0
1
2
3
40 50 60 70
MgO
(
)
SiO2 ()
K2O
(
)
40 50 60 70
0
04
08
4
8
12
SiO2 ()
(a)(b)
(c)
Figure 7 Bi-plots of SiO2 K2 O SiO2 MgO and FeOTiO2 for the WDS analyses obtainedfrom glass shards of the NYT from Procida (Naples) and Prato Spilla Crsquo Means and standarddeviations are shown
results show a higher degree of statistical scatter than the WDS measurements whichmay reregect the fact that the data were normalized combined with the inreguence ofvariation in water content between shards
There is a very close correspondence between the WDS data for the Prato Spilla `Crsquomicro-tephra shards and those obtained from the type-material near Naples (shy g-ure 7) The geochemical data strongly suggest therefore that the NYT is representedat the Prato Spilla `Crsquo site by a discrete layer of micro-tephra particles This conclu-sion is compatible with the pollen-stratigraphic data from the site and accords withage estimates for the NYT (ca 120 14C ka BP) obtained from other sites (Paterneet al 1990)
These results encourage us to believe that many if not all of the tephras listedin table 1 will be detectable over much larger tracts of Europe than is presently thecase if appropriate research is undertaken to detect layers of micro-tephra particlesin selected sites The authors are presently engaged in a major continent-wide pro-gramme of research in collaboration with a number of European research groupsdesigned to test this hypothesis The focus in this research is on those parts of Europewhere we expect to shy nd overlapping `apronsrsquo of tephra deposition originating fromthe Italian Eifel Massif Central and Icelandic provinces For example a number ofsites in parts of southern France northern Italy and perhaps western Switzerlandmay have received inreguxes of micro-tephra originating from the Italian and Eifelprovinces and perhaps also from the Massif Central Sites in parts of Germany Den-mark and southern Sweden for example may in turn have received tephra depositsfrom both of the Icelandic and Eifel provinces If this proves to be the case then thestage will be set for the construction of a tephrostratigraphical framework for Europewhich will enable Last Termination sequences to be correlated on a continent-widebasis using micro- and visible tephra layers as time-parallel stratigraphic markersFurthermore there is also the possibility that other tephras remain to be discovered
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European tephrochronological framework for Termination 1 789
those which either because of the magnitude or nature of some volcanic eruptionswere distributed over parts of Europe in micro-tephra form only
6 European tephrostratigraphy and the chronology of eventsduring the Last Termination and Early Holocene
One of the crucial issues in Late Quaternary palaeoenvironmental research thatremains to be resolved is the degree to which climatic events inferred from oceanicterrestrial and ice-core records were synchronous during the Last Termination andEarly Holocene If the ice-core records provide realistic estimates of the rates anddurations of climatic events during this period then comparisons between individ-ual records have to be enotected with at least a decadal precision The problem thispresents and the role that tephrostratigraphy can play in resolving some of thedimacr culties involved are put into perspective in shy gure 8
Figure 8 shows some of the data used to calibrate radiocarbon dates (the LakeSuigetsu and Cariaco Basin datasets) plotted against the GRIP ss08c ice-core recordof macr 18O variations The latter has been selected by the INTIMATE group as an arbi-trary and temporary standard for this period and used to deshy ne an event stratig-raphy scheme (shy gure 1) for the Last Termination (see Bjorck et al 1998 Walker etal 2001) As has been alluded to in earlier sections of this paper the uncertaintiesassociated with all of the dating methods currently employed preclude precise com-parisons of ice-core marine and terrestrial records Oceanic and terrestrial recordsmostly rely upon radiocarbon dating locally supplemented in a few cases by varvechronology Imprecisions in radiocarbon dates can arise through site-specishy c fac-tors (eg hard-water or mineral carbon errors in freshwater sequences and reservoirerrors in marine sequences) sample selection laboratory measurements of 14C activ-ity and other factors (Lowe amp Walker 2000) Further imprecision may be introducedby the calibration of radiocarbon dates since the uncertainties in the dataset usedto calibrate pre-Holocene radiocarbon dates INTCAL98 are far higher than forthe Holocene which is based on dendro-calibration (Stuiver et al 1998) There arealso uncertainties anotecting varve chronologies while the ss08c ice-core chronologyfor the Last Termination dinoters signishy cantly from the GISP2 record and indeedfrom other models of the GRIP record (Lowe et al 2001) Published comparisonsbetween ice-core marine and terrestrial records for the Last Termination seldom takeinto account the true magnitude of the dating uncertainties involved and frequentlyemploy circular reasoning
Figure 8 shows the positions on the radiocarbon time-scale of 20 of the tephrasdiscussed earlier in this paper these being the ones for which reasonably conshy dentradiocarbon age estimates can be made (though these will be subject to revised esti-mates in the future) A high number of these occur in the period 14080 14C kaBP but we conshy dently anticipate the discovery in the future of additional tephras(perhaps in micro-tephra form only) which will date to the period 185140 14C kaBP Tephras detected in the GRIP ice core over the same time-interval are plottedon the calendar time-scale in shy gure 8 By providing key `time-linesrsquo between recordstephrostratigraphy can help to resolve some of the dating uncertainties referredto earlier by for example enabling direct comparisons of discrepant age estimatesobtained using dinoterent methods (cf Litt et al 2001) It can also provide estimatesof the magnitudes of the reservoir errors that anotected various marine sectors at dif-
Phil Trans R Soc Lond A (2002)
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790 S M Davies and others
-44
-40
-36
-32
cale
ndar
yea
rs B
P
8000
9000
10 0
00
11 0
00
12 0
00
13 0
00
14 0
00
15 0
00
16 0
00
17 0
00
18 0
00
14C age (BP)
VA
SA
Un
Un
Un
Un
Un
BF
Hol
ocen
eG
S-1
GI-
1aG
I-1b
GI-
1cG
I-1d
GI-
1eG
S-2
aG
S-2
bG
S-
2c
Bor
robo
l
La
Nug
egravere
Laa
cher
See
God
ivel
le 5
amp I
-TH
OL
-2
Puy
de D
ocircme
I-T
HO
L-1
Saks
unar
vatn
Houmlg
stor
psm
osse
nU
lmen
er M
aar
amp L
3574
radiocarbon dated European tephra horizons
Cho
pine
Kili
an V
asse
tM
erca
to
God
ivel
le 4
Pom
ici P
rinc
ipal
i amp V
edde
Polla
ra p
umic
eK
OL
-GS-
2 amp
GS
-2B
AS-
12
3
GS
-2B
AS-
4 U
nita
dei
Tef
raSu
peri
ori amp
laye
r Y
-1
Gre
enis
h
L9
20 0
0018
000
16 0
0014
000
12 0
0010
000
-44
-40
-36
-32
800
600
400
200 0
GISP2 volcanicsulphate conc (ppb)
1000
Nea
polit
an Y
ello
w T
uff
GISP2 18O (permil) dGRIP 18O (permil) d
Figure 8 For description see opposite
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 791
ferent times through a comparison of radiocarbon dates obtained from marine andterrestrial horizons in which the same tephra has been detected (see for exampleAustin et al 1995 Bondevik et al 2001 Haregidason et al 2000) Tephrostratigraphymay provide an independent test of suggestions that some of the climatic changesduring the Last Termination were time-transgressive as illustrated for some appar-ently contrasting climatic trends in Iceland Britain and NW Russia (Lowe 2001) Ofparticular importance as far as establishing `leadsrsquo and `lagsrsquo in climatic changes isconcerned are the tephra records from the Greenland ice cores The discovery of theVedde and Saksunarvatn ashes in the GRIP record (Gronvold et al 1995) alreadyprovides a basis for making direct comparisons between marine terrestrial and ice-core records It is a matter of some urgency that the incidence of tephra depositsin the Greenland ice cores be more fully explored in the hope that this will lead tothe recognition of additional time-parallel links between the ice-core records on theone hand and oceanic and terrestrial records on the other An investigation of thenew NordGRIP record for this purpose is currently in progress (S M Davies 2002unpublished data)
Finally a fuller and more reshy ned tephrostratigraphical scheme for Europe will alsohave other applications It will provide an important database for those investigatingthe timing and frequency of volcanic eruptions in Europe during the past 20 000 yror so as well as of the geochemical evolution of the dinoterent volcanic centres overthat period A fuller record of the distribution of micro-tephras may also provideinformation on atmospheric circulation patterns during the dispersal and depositionperiods as well as on the nature and altitude of the eruption columns which mayin turn provide inferences about magma viscosity
This paper is a contribution to the INTIMATE project of the INQUA Palaeoclimate Com-mission and the work is supported by a Leverhulme Trust Research project (grant allocationnumber F07537C) entitled Testing hypotheses of rapid climate change using tephrochronol-ogyrsquo SMDrsquo s contribution was completed during possession of a NERC PhD studentship(GT 0499ES162) We are extremely grateful to Dr Peter G Hill for his assistance withthe EPMA analyses at the Tephrochronology Analytical Unit University of Edinburgh We alsothank Dr G Mastrolorenzo (Vesuvius Observatory) and Miss G Swindle for assistance duringthe macreld investigations in Naples Thanks are also expressed to two anonymous reviewers forcomments on an earlier draft
Appendix A
Table 2 shows the major oxide concentrations of NYT glass shards from Procidaand Prato Spilla `Crsquo and of the Mercato Tephra from the Naples area (see x 4 forsite context) All oxides are shown as weight and total iron is expressed as FeO
Figure 8 Radiocarbon calibration curve for Termination 1 and the Early Holocene compared with theGRIP macr 18 O event stratigraphy the GRIP ss08c and GISP2 macr 18 O records (wwwngdcnoaagov) andknown tephra horizons from this period The shaded areas represent the cooler climatic episodes andare labelled with the Greenland stratotype terminology (Bjorck et al 1998) Where radiocarbon agesare reported in table 1 as a range the mean is given here Abbreviations for GRIP horizons are asfollows Un unknown (approximate positions are given (S Johnsen 2001 personal communication))SA Saksunarvatn Ash VA Vedde Ash BF Black Feather Sulphate concentrations from the GISP2record are also shown (Zielinski et al 1996) Open circles denote radiocarbon calibration data fromLake Suigetsu (Kitagawa amp van der Plicht 2000) Filled circles denote radiocarbon calibration data fromCariaco Basin assuming a marine reservoir age of 420 14 C yr (Hughen et al 1998)
Phil Trans R Soc Lond A (2002)
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792 S M Davies and others
Tab
le2
Majo
roxi
de
con
cen
trati
on
sof
NY
Tgl
ass
shard
sfr
om
Pro
cida
an
dP
rato
Spil
laC
rsquoan
dof
the
Mer
cato
Tep
hra
from
the
Naple
sare
a(s
eex4
for
site
con
text
)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
roci
da)
1584
204
0177
634
201
106
828
635
197
5969
1W
DS
2598
603
9178
027
101
204
924
244
583
4965
8W
DS
3586
604
5173
631
100
805
924
342
183
0951
9W
DS
4583
903
9177
933
000
906
924
540
486
9958
3W
DS
5605
106
8179
126
901
204
923
243
086
1976
4W
DS
6591
704
5177
332
801
006
425
740
887
8968
0W
DS
7581
804
1178
031
501
107
125
640
086
9956
1W
DS
8589
504
2179
533
701
506
926
740
987
5970
4W
DS
9592
003
9178
135
101
007
026
443
585
7972
7W
DS
10
591
404
2174
631
601
105
723
442
482
6957
0W
DS
11
593
403
6177
131
301
506
726
439
188
5967
6W
DS
12
588
103
8176
128
100
505
525
141
583
4952
1W
DS
13
577
003
8176
533
500
807
228
140
384
8952
0W
DS
14
586
004
7179
735
300
706
827
842
984
6968
5W
DS
15
588
104
2180
629
400
505
924
937
993
0964
5W
DS
16
579
603
9178
536
501
308
228
836
087
1959
9W
DS
17
580
103
9177
631
500
907
327
039
488
9956
6W
DS
mea
n588
104
2177
631
901
006
525
940
686
9962
8
sd
(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(07
8)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 793
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
rato
Spil
laC
rsquo)
1552
105
4177
247
401
914
38
735
578
9951
1W
DS
2557
305
7179
845
701
512
640
136
581
5960
6W
DS
3595
004
4173
724
302
003
117
652
877
8950
7W
DS
4575
704
2179
433
001
406
627
043
083
6953
7W
DS
5599
904
0178
826
401
304
421
841
688
4966
5W
DS
6591
103
8177
826
601
105
022
443
888
8960
2W
DS
7565
304
5180
939
501
410
532
535
791
8962
1W
DS
8597
606
9180
826
501
604
821
546
684
6970
7W
DS
9571
805
6179
939
801
109
932
240
883
6964
7W
DS
10
588
603
7176
527
601
104
721
042
487
7953
3W
DS
11
559
404
9180
544
501
812
339
435
878
6957
2W
DS
12
594
704
0181
328
301
705
522
144
785
6967
9W
DS
13
611
103
7187
016
900
802
419
938
195
9975
8W
DS
14
599
204
4181
128
601
404
620
844
986
6971
6W
DS
15
601
204
4177
328
302
004
722
446
385
5972
1W
DS
16
595
104
5176
428
801
504
722
744
884
3962
8W
DS
17
603
704
1177
825
101
503
520
348
181
2965
3W
DS
18
558
704
5179
647
401
813
139
836
879
0960
7W
DS
19
589
602
8178
830
901
606
622
436
091
8960
5W
DS
20
553
606
3178
647
401
913
840
136
978
0956
6W
DS
21
579
004
0175
739
000
708
328
338
286
7959
9W
DS
mea
n582
804
6179
033
401
507
427
341
484
8962
1
sd
(1
87)
(01
0)
(02
7)
(09
2)
(00
4)
(03
9)
(08
0)
(04
9)
(05
0)
(07
0)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
794 S M Davies and others
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)
1575
202
7194
219
701
101
016
374
766
9951
8W
DS
2575
802
9194
523
902
201
520
273
564
5959
0W
DS
3574
301
4205
219
101
100
416
481
266
1965
2W
DS
4575
500
7206
018
002
000
415
181
669
3968
6W
DS
5580
000
9208
018
601
300
515
883
367
1975
5W
DS
6571
001
0206
016
101
600
515
078
967
1957
2W
DS
7577
501
1201
117
101
500
620
675
655
4950
5W
DS
8573
700
9212
717
101
900
815
187
564
2973
9W
DS
9580
301
3208
715
801
400
824
81
754
1968
1W
DS
10
574
400
6211
18
402
00
516
480
567
8971
6W
DS
11
577
200
7214
212
501
200
829
879
247
962
6W
DS
12
572
200
9211
217
301
501
15
980
465
9966
3W
DS
13
571
800
7210
417
402
201
16
184
467
2971
2W
DS
14
567
300
9208
916
901
400
917
383
262
5959
3W
DS
15
568
600
8205
918
202
101
414
682
666
6960
8W
DS
16
572
501
1211
318
202
01
215
884
364
5970
9W
DS
17
572
901
2212
916
502
101
215
883
667
2973
4W
DS
18
573
01
4211
716
301
801
416
83
365
5970
4W
DS
19
569
201
1207
418
602
101
414
982
964
961
6W
DS
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
3)
(04
2)
(01
3)
(00
1)
(00
2)
(01
)(0
39)
(01
1)
(02
5)
Phil Trans R Soc Lond A (2002)
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796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
References
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Allen J R M (and 14 others) 1999 Rapid environmental changes in southern Europe duringthe last glacial period Nature 400 740743
Alley R B (and 10 others) 1993 Abrupt increase in Greenland snow accumulation at the endof the Younger Dryas Nature 362 527529
Andronico D Calderoni G Cioni R Sbrana A Sulpizio R amp Santacroce R 1995 Geo-logical map of Somma Vesuvius volcano Period Mineral 64 7788
Atkinson T C Brireg a K R amp Coope G R 1987 Seasonal temperature in Britain during thepast 22 000 years reconstructed using beetle remains Nature 325 587592
Austin W E N amp Kroon D 1996 Lateglacial sedimentology foraminifera and stable isotopestratigraphy of the Hebridean Continental Shelf northwest Scotland In Late Quaternarypalaeoceanography of the North Atlantic margins (ed J T Andrews W E N Austin HBergsten amp A E Jennings) vol 111 pp 187213 Geological Society of London SpecialPublication
Austin W E N Bard E Hunt J B Kroon D amp Peacock J D 1995 The 14 C age ofthe Vedde Ash implications for Younger Dryas marine reservoir corrections Radiocarbon 375362
Barker D S 1983 Igneous rocks Englewood Clireg s NJ Prentice-Hall
Bennet K D Boreham S amp Sharp M J 1992 Holocene history of environment vegetationand human settlement on Catta Ness Shetland J Ecol 80 241273
Birks H H Gulliksen S Hadeg idason H Mangerud J amp Possnert G 1996 New radiocarbondates for the Vedde Ash and the Saksunarvatn Ash from western Norway Quat Res 45119127
Bjorck J amp Wastegordm ard S 1999 Climate oscillations and tephrochronology in eastern middleSweden during the last glacialinterglacial transition J Quat Sci 14 399410
Bjorck S Ingparaolfsson O Hadeg idason H Hallsdparaottir M amp Anderson N J 1992 Lake Torfadals-vatn a high resolution record of the North Atlantic Ash zone I and the last glacialinterglacialenvironmental changes in Iceland Boreas 21 1522
Bjorck S Walker M J C Cwynar L Johnsen S Knudsen K Lowe J J Wohlfarth Bamp INTIMATE members 1998 An event stratigraphy for the Last Termination in the NorthAtlantic region based on the Greenland ice-core record a proposal by the INTIMATE groupJ Quat Sci 13 283292
Bjorck S Lowe J J amp Walker M J C 2001 Integration of ice core marine and terrestrialrecords of Termination 1 from the North Atlantic region Quat Sci Rev 20 11691274
Bond G C Mandeville C amp Horeg man S 2001 Were rhyolitic glasses in the Vedde Ash andin the North Atlanticrsquo s Ash zone 1 produced by the same volcanic eruption Quat Sci Rev20 11891199
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 797
Bondevik S Mangerud J amp Gulliksen S 2001 The marine 1 4 C age of the Vedde Ash Bedalong the west coast of Norway J Quat Sci 16 37
Bossuet G Richard H Magny M amp Rossy M 1997 A new occurrence of Laacher See Tephrain the central Jura (France) The mire of Le Lautrey C R Acad Sci Paris Sparaer IIa 3254348
Brauer A Endres C Gunter C Litt T Stebich M amp Negendank J F W 1999 Highresolution sediment and vegetation responses to Younger Dryas climate change in varved lakesediments from Meerfelder Maar Germany Quat Sci Rev 18 321329
Brooks S J Mayle F E amp Lowe J J 1997 Chironomid based Lateglacial climatic recon-struction for southeast Scotland J Quat Sci 12 161167
Calanchi N Dinelli E Gasparatto G amp Lucchini F 1996 Etnean tephra layer in Albanolake and Adriatic Sea cores new macrndings of Y-1 layer in the central Mediterranean area ActaVulcan 8 713
Coope G R Lemdahl G Lowe J J amp Walkling A 1998 Temperature gradients in northernEurope during the last glacialHolocene transition (149 ka BP) interpreted from coleopternassemblages J Quat Sci 13 419433
Dansgaard W (and 10 others) 1993 Evidence for general instability of past climate from a250 kyr ice-core record Nature 363 218220
Davies S M Turney C S M amp Lowe J J 2001 Identimacrcation and signimacrcance of a visiblebasalt-rich Vedde Ash layer in a Late-glacial sequence on the Isle of Skye Inner HebridesScotland J Quat Sci 16 99104
Delibrias G Di Paola G M Rosi M amp Santacroce R 1979 La storia eruttiva del complessovulcanico Somma Vesuvio ricostruita dalle successini piroclastiche del Monte Somma RendSoc It Mineral Petrolog 35 411438
Di Vito M A Isaia R Orsi G Southon J de Vita S Drsquo Antonio M Pappalardo L ampPiochi M 1999 Volcanism and deformation since 12 000 years at the Campi Flegrei caldera(Italy) J Volcanol Geophys Res 91 221246
Dugmore A J amp Newton A J 1992 Thin tephra layers in peat revealed by X-radiography JArchaeol Sci 19 163170
Dugmore A J amp Newton A J 1998 Holocene tephra layers in the Faroe Islands Frodskaparrit46 191204
Eastwood A J Pearce N J G Westgate J A Perkins W T Lamb H F amp RobertsN 1999 Geochemistry of Santorini tephra in lake sediments from southwest Turkey GlobalPlanet Change 21 1729
Eirpara sup3 ksson J Knudsen K L Hadeg idason H amp Henriksen P 2000 Lateglacial and Holocenepalaeoceanography of the North Icelandic shelf J Quat Sci 15 2342
Etlicher B Janssen C R Juvignparae E amp Van Leeuwen J F N 1987 Le Haut Forez (MassifCentral France) aprmicroes le Plparaeniglaciaire Wurmien environnement et tparaephra du volcan de LaNugmicroere Bull Ass Fr Etud Quat 4 229239
Frezzotti M amp Narcisi B 1996 Late Quaternary Tephra derived paleosols in central Italyrsquo scarbonate Apennine range stratigraphical and paleoclimatological implications Quat Int3436 147153
Friedrich M Kromer B Spurk M Hofmann J amp Kaiser K F 1999 Paleoenvironment andradiocarbon calibration as derived from LateglacialEarly Holocene tree-ring chronologiesQuat Int 61 2739
Froggatt P C 1992 Standardisation of the chemical analysis of tephra deposits Report of theICCT working group Quat Int 1314 9396
Gronvold K Oskarsson N Johnsen S J Clausen H B Hammer C U Bond G amp Bard E1995 Ash layers from Iceland in the GRIP ice core correlated with oceanic and land sedimentsEarth Planet Sci Lett 135 149155
Phil Trans R Soc Lond A (2002)
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798 S M Davies and others
Hadeg idason H Eirpara sup3 ksson J amp van Kreveld S 2000 The tephrochronology of Iceland and theNorth Atlantic region during the Middle and Late Quaternary a review J Quat Sci 15322
Hoek W Z amp Bohncke S J P 2001 Oxygen isotope wiggle matching as a tool for synchronisingice-core and terrestrial records over Termination 1 Quat Sci Rev 20 12511264
Hughen K A Overpeck J T Peterson L C amp Trumbore S 1996 Rapid climate changes inthe tropical Atlantic region during the last deglaciation Nature 380 5153
Hughen K A Overpeck J T amp Lehman J 1998 A new 14 C calibration data set for the LastDeglaciation Radiocarbon 39 483494
Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
Hunt J B amp Hill P G 1996 An inter-laboratory comparison of the electron probe microanalysisof glass geochemistry Quat Int 3436 229241
Hunt J B amp Hill P G 2001 Tephrological implications of beam sizesample size ereg ects inelectron microprobe analysis of glass shards J Quat Sci 16 105117
Hunt J B Fannin N G T Hill P G amp Peacock J D 1995 The tephrochronology andradiocarbon dating of North Atlantic Late Quaternary sediments an example from the StKilda Basin In The tectonics sedimentation and palaeoceanography of the North Atlanticregion (ed R A Scrutton M S Stoker G B Shimmield amp A W Tudhope) vol 90pp 227248 Geological Society of London Special Publication
Hunt J B Clift P D Lacasse C Vallier T L amp Werner R 1998 Standardisation ofelectron probe microanalysis of glass geochemistry In Proc ODP Scientimacrc Results vol 152pp 8591 College Station TX Ocean Drilling Program
Jakobsson S P 1979 Outline of the petrology of Iceland Jokull 29 5773
Juvignparae E 1987 Deux retombparaees volcaniques tardiglaciaires dans le Cparaezallier (Massif CentralFrance) Bull Ass Fr Etud Quat 13 37
Juvignparae E 1993 Contribution microa la tparaephrostratigraphie du Quaternaire et son application microa lagparaeomorphologie Mparaem Serv Explicat Cartes Gparaeol Min Belg 36 166
Juvignparae E amp Gewelt M 1987 La Narse drsquo Ampoix comme tparaephrostratotype dans la Chasup3 ne desPuys mparaeridionale (France) Bull Ass Fr Etud Quat 29 3749
Juvignparae E Kozarski S amp Nowaczyk B 1995 The occurrence of Laacher See Tephra in Pomera-nia NW Poland Boreas 24 225231
Juvignparae E Bastin B Delibrias G Evin J Gewelt M Gilot E amp Streel M 1996 Acomprehensive pollen and tephra based chronostratigraphic model for the Lateglacial andHolocene period in the French Massif Central Quat Int 3436 113120
Keller J 1980 The island of Vulcano Rend Soc It Mineral Petrolog 36 369414
Keller J Ryan W B F Ninkovich D amp Altherr R 1978 Explosive volcanic activity in theMediterranean over the past 200 000 years as recorded in deep sea sediments Geol Soc AmBull 89 591604
Kitagawa H amp van der Plicht J 2000 Atmospheric radiocarbon calibration beyond 11 900 calBP from Lake Suigetsu laminated sediments Radiocarbon 42 369380
Kvamme T Mangerud J Furnes H amp Ruddiman W F 1989 Geochemistry of Pleistoceneash zones in cores from the North Atlantic Norsk Geol Tids 69 251272
Lacasse C Sigurdsson H Johannesson H Paterne M amp Carey S 1995 Source of Ash zone 1in the North Atlantic Bull Volcanol 57 1832
Langone L Asioli A Corregiari A amp Trincardi F 1996 Age depth modelling through theLate-Quaternary deposits of the central Adriatic Basin In Palaeoenvironmental analysis ofItalian crater lake and Adriatic sediments (ed F Oldmacreld amp P Guilizzoni) vol 55 pp 177196 Memorie dellrsquo Instituto Italiano di Idrobiologia
Larsen G 2000 Holocene volcanism in Iceland and tephrochronology as a tool in volcanologyIn Iceland 2000 modern processes and past environments Keele University UK
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 799
Litt T amp Stebich M 1999 Bio- and chronostratigraphy of the Lateglacial in the Eifel regionGermany Quat Int 61 516
Litt T Brauer A Goslar T Merkt J Balaga K Muller H Ralska-Jasiewiczowa MStebich M amp Negendank J F W 2001 Correlation and synchronisation of Lateglacialcontinental sequences in northern Central Europe based on annually laminated lacustrinesediments Quat Sci Rev 20 12331249
Long D amp Morton A C 1987 An ash fall within the Loch Lomond stadial J Quat Sci 297101
Lotter A F Eicher U Siegenthaler U amp Birks H J B 1992 Lateglacial climatic oscillationsas recorded in Swiss lake sediments J Quat Sci 7 187204
Lowe J J 1992 Lateglacial and Early Holocene lake sediments from the Northern ApenninesItaly|pollen stratigraphy and radiocarbon dating Boreas 21 193208
Lowe J J 2001 Abrupt climatic changes in Europe during the last glacialinterglacial tran-sition the potential for testing hypotheses on the synchroneity of climatic events usingtephrochronology Global Planet Change 603 7384
Lowe J J amp Turney C S M 1997 Vedde Ash layer discovered in a small lake basin on theScottish mainland J Geol Soc Lond 154 605612
Lowe J J amp Walker M J C 2000 Radiocarbon dating the last glacialinterglacial transition(ca 14914 C ka BP) in terrestrial and marine records the need for new quality assuranceprotocols Radiocarbon 42 5368
Lowe J J amp Watson C 1993 Lateglacial and Early Holocene pollen stratigraphy of the northernApennines Italy Quat Sci Rev 12 727738
Lowe J J Birks H H Brooks S J Coope G R Harkness D D Mayle F E SheldrickC Turney C S M amp Walker M J C 1999 The chronology of palaeoenvironmental changesduring the Last GlacialHolocene transition towards an event stratigraphy for the BritishIsles J Geol Soc Lond 156 397410
Lowe J J Hoek W Z amp INTIMATE group 2001 Inter-regional correlation of palaeoclimaticrecords for the Last GlacialInterglacial transition a protocol for improved precision recom-mended by the INTIMATE project group Quat Sci Rev 20 11751187
Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
Mangerud J Lie S E Furnes H Kristiansen I L amp Liquest mo L 1984 A Younger Dryas ashbed in western Norway and its possible correlation with tephra beds from the Norwegian Seaand North Atlantic Quat Res 21 85104
Mangerud J Furnes H amp Jparaohansen J 1986 A 9000 year-old ash bed on the Faroe IslandsQuat Res 26 262265
Martini J 1970 Recherche de retombparaees volcaniques dans le sud-est de la France et la Suisseoccidentale Arch Sci 23 641674
Martini J amp Duret J J 1965 Note preliminaire sur la presence drsquo un niveau de cendres vol-caniques dans des sparaediments post-glaciaires des environs de Genmicroeve Arch Sci 18 587588
Mayewski P A Meeker L D Twickler M S Whitlow S Yang Q Lyons W B amp Pren-tice M 1997 Major features and forcing of high latitudes Northern Hemisphere atmosphericcirculation using a 110 000 year long glaciochemical series J Geophys Res 102 345365
Merkt J Muller H Knabe W Muller P amp Weiser T 1993 The Early Holocene Saksunarvatntephra found in lake sediments in NW Germany Boreas 22 93100
Narcisi B 1993 Segnalazione di un livello piroclastico di provenienza etnea nellrsquo area del Fucino(Italia Centrale) Quaternario 6 8792
Narcisi B 1996 Tephrochronology of a Late Quaternary lacustrine record from the Monticchiomaar (Vulture volcano southern Italy) Quat Sci Rev 15 155165
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
800 S M Davies and others
Newton A J amp Dugmore A J 1993 Tephrochronology of Core C from Lago Grande di Mon-ticchio In Paleolimnology of European Maar Lakes (ed J F W Negendank amp B Zolitschka)Lecture Notes in Earth Science vol 49 333348 Springer
Oldmacreld F Appleby P G amp Thompson R 1980 Palaeoecological studies of lakes in theHighlands of Papua New Guinea J Ecol 68 457477
Orsi G Drsquo Antonio M de Vita S amp Gallo G 1992 The Neapolitan Yellow Tureg a large mag-nitude trachytic phreatoplinian eruption eruptive dynamics magma withdrawal and calderacollapse J Volcanol Geotherm Res 53 275287
Paterne M Guichard F Labeyrie J Gillot P Y amp Duplessy J C 1986 Tyrrhenian Seatephrochronology of the oxygen isotope record for the past 60 000 years Mar Geol 72259285
Paterne M Guichard F amp Labeyrie J 1988 Explosive activity of the south Italian volca-noes during the past 80 000 years as determined by marine tephrochronology J VolcanolGeotherm Res 34 153172
Paterne M Labeyrie J Guichard F Mazaud A amp Maitre F 1990 Fluctuations of the Cam-panian explosive volcanic activity (south Italy) during the past 190 000 years as determinedby marine tephrochronology Earth Planet Sci Lett 98 166174
Pawse A Beske-Diehl S amp Marshall S A 1998 Use of magnetic hysteresis properties andelectron spin resonance spectroscopy for the identimacrcation of volcanic ash a preliminary studyGeophys J Int 132 712720
Pearce N J G Westgate J A amp Perkins W T 1996 Developments in the analysis of singleglass shards in volcanic deposits by laser ablation ICP-MS quantitative and single internalstandard multi-element methods Quat Int 3436 213227
Pearce N J G Westgate J A Perkins W T Eastwood W J amp Shane P 1999 Theapplication of laser ablation ICP-MS to the analysis of volcanic glass shards from tephradeposits bulk glass and single shard analysis Global Planet Change 21 151171
Pilcher J R amp Hall V A 1992 Towards a tephrochronology for the Holocene of the north ofIreland Holocene 2 255259
Ponel P amp Lowe J J 1992 Coleopteran pollen and radiocarbon evidence from the Prato Spillarsquo Drsquo succession N Italy C R Acad Sci Paris Sparaer II 315 14251431
Rose N L Golding P N E amp Battarbee R W 1996 Selective concentration and enumerationof tephra shards from lake sediment cores Holocene 6 243246
Ruddiman W F amp Glover L K 1972 Vertical mixing of ice rafted volcanic ash in NorthAtlantic sediments Geol Soc Am Bull 83 28172836
Ruddiman W amp McIntyre A 1981 The North Atlantic Ocean during the last deglaciationPalaeogeogr Palaeoclimatol Palaeoecol 35 145214
Santacroce R 1987 Somma Vesuvius Quad Ric Sci 114 252
Sarna-Wojcicki A 2000 Tephrochronology In Quaternary geochronology methods and applica-tions (ed J S Noller J M Sowers amp W R Lettis) AGU Reference shelf vol 4 pp 357377Washington DC American Geophysical Union
Sejrup H P Sjiquest holm J Furnes H Beyer I Eide L Jansen E amp Mangerud J 1989Quaternary tephrochronology on the Iceland Plateau north of Iceland J Quat Sci 4 109114
Sikes E L Samson C R Guilderson T P amp Howard W R 2000 Old radiocarbon agesin the southwest Pacimacrc Ocean during the last glacial period and deglaciation Nature 405555558
Stein R Nam S-I Grobe H amp Hubbersten H 1996 Late Quaternary glacial history andshort term ice rafted debris deg uctuations along the East Greenland continental marine In LateQuaternary palaeoceanography of the North Atlantic margins (ed J T Andrews W E NAustin H Bergsten amp A E Jennings) pp 135151 Geological Society London SpecialPublication
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 801
Stuiver M amp Grootes P M 2000 GISP2 oxygen isotope ratios Quat Res 53 277284
Stuiver M Reimer P J Bard E Beck J W Burr G S Hughen K A Kromer BMcCormac G Van der Plicht J amp Spurk M 1998 INTCAL 98 radiocarbon age calibration24 0000 cal BP Radiocarbon 40 10411083
Sweatman T R amp Long J V P 1969 Quantitative electron microprobe analysis of rock formingminerals J Petrol 7 332379
Turney C S M 1998 Extraction of rhyolitic ash from minerogenic lake sediments J Paleolim-nol 19 199206
Turney C S M amp Lowe J J 2001 Tephrochronology In Tracking environmental changes inlake sediments physical and chemical techniques (ed W M Last amp J P Smol) DordrechtKluwer Academic
Turney C S M Harkness D D amp Lowe J J 1997 The use of microtephra horizons tocorrelate Lateglacial lake sediments successions in Scotland J Quat Sci 12 525531
Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
van den Bogaard P amp Schmincke H 1985 A widespread isochronous Late Quaternary tephralayer in central and northern Europe Geol Soc Am Bull 96 15541571
van den Bogaard B Dordeg er W Sandgren P amp Schmincke H-U 1994 Correlating theHolocene records Icelandic tephra found in Schleswig-Holstein (northern Germany) Natur-wissenschaften 81 554556
Vernet G amp Raynal J-P 2001 Tephrostratigraphy of the Limagne revisited Implications forLateglacial and Holocene Prehistory In Tephras chronology archaeology (ed E Juvignparae ampJ-P Raynal) pp 111116 Dossiers de lrsquo ArchparaeoLogis no 1 France
Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
Vezzoli L 1991 Tephra layers in Bannock Basin (eastern Mediterranean) Mar Geol 1002134
von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
Walker M J C Bjorck S Lowe J J Cwynar L C Johnsen S Knudsen K-L WohlfarthB amp INTIMATE Group 1999 Isotopic events in the GRIP ice core a stratotype for the LatePleistocene Quat Sci Rev 18 11431150
Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
Phil Trans R Soc Lond A (2002)
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Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
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European tephrochronological framework for Termination 1 783
Vedde Ash
615 625 635 645 655depth (cm)
organic lake mudsHolocene
silty clayGS-1Younger Dryas
organic lake mudsGI-1Alleroslashd
100 microm
(a)
(b)
Figure 5 (a) Photograph of the visible VA layer discovered at Loch Ashik Isle of Skye InnerHebrides Scotland (b) Light microscope photograph showing the rich content of basaltic shards(examples are indicated by the arrows) within this layer (8024 m m size fraction)
this ash was dispersed over much of central Europe (van den Bogaard amp Schmincke1985 Friedrich et al 1999 Litt amp Stebich 1999) The LST is dated by radiocarbonto ca 110 14C ka BP (van den Bogaard amp Schmincke 1985) and to 11 063sect12 14C BP(Friedrich et al 1999) by varve chronology to 1288 varve ka BP (Brauer et al 1999Litt et al 2001) and by ArAr dating to 129 ka cal BP (van den Bogaard 1995) Ithas a phonolitic composition and is thought to have originated from a plinian andphreatomagmatic eruption with the distal ash being carried in three distinct plumesone to the northeast towards Poland one to the west and the third to the southcovering the Jura Mountains and north Italy (van den Bogaard amp Schmincke 1985Juvigne et al 1995 Bossuet et al 1997) This pattern is thought to reregect altitu-dinal variations in the predominant wind direction Sedimentary sequences near thevolcanic source indicate that the LST consists of three main layers which represent
Phil Trans R Soc Lond A (2002)
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784 S M Davies and others
dinoterent eruption phases These are grouped together as the Laacher See TephraFormation but the three individual units can be traced within and between a seriesof depositional fans The geochemical data obtained from these three LST layersshow signishy cant variations as reregected in the ternary plots (shy gure 4)
The Early Holocene Ulmener Maar Tephra (UMT) is of rhyolitic composition andappears to be restricted to sites in Germany though this conclusion is also based onrecords of visible tephras only It is dated to ca 956 14C ka BP and to 110 varve ka(Zolitschka et al 1995 Litt et al 2001)
(c) Massif Central province
The Massif Central tephras are mainly of basaltic trachyandesitic compositionwhich is distinct from the other ash provinces (shy gures 3 and 4) and their known dis-tributions are mostly conshy ned to the Massif Central region The ages of the MassifCentral tephras are based on radiocarbon dates obtained from mire and lake sedi-ments which `bracketrsquo the tephras The La Nugsup3ere Tephra with an age of 114 14C kaBP is the oldest Massif Central tephra identishy ed so far within the time-span of inter-est (Etlicher et al 1987 Juvigne et al 1996) The two Godivelle Tephras (5 and 4)are close in age but extensive radiocarbon dating suggests distinct ages of 107and 103 14C ka BP respectively (Juvigne et al 1996) The age of the Puy de DomeTephra is less certain as the estimate is based on only one radiocarbon date froma site in the southern Chaplusmn ne des Puys (table 1) This tephra is thought to havea trachyte composition (Juvigne 1993) although no major element concentrationshave yet been published
The ChopineKilianVasset tephras are thought to be derived from three separateEarly Holocene eruptions although the stratigraphic succession is not known atpresent These trachytic tephras have been radiocarbon dated to ca 854sect150 14C kaBP but are thought to have erupted separately within ca 260 yr (Juvigne et al 1996) This series of tephras is considerably more widespread than the others fromthe region having been identishy ed as far east as the Jura Mountains (Martini amp Duret1965 Martini 1970) Some other ash falls that originated from the Chaplusmn ne des Puysappear to be of local importance only (Vernet et al 1998 Vernet amp Raynal 2001)Geochemical data are currently available for only three of the Massif Central tephrasand so far as is known no attempt has yet been made to identify these tephras inmicro-tephra form
(d ) Italian provinces
The Italian tephras from this period can be assigned to three main volcanic com-plexes the Campanian volcanic shy elds around Naples Etna on Sicily and the AeolianIslands The Campanian complex which includes the Phlegrean Fields Vesuviusand Ischia is mainly trachytic in composition with a geochemical spectrum that isquite distinct from those of the Etna complex and of the Aeolian Islands (shy gure 3)Tephras originating from one or more of these three complexes have been detectedin marine cores from the Tyrrhenian and Adriatic seas as well as other parts of theMediterranean Sea (Keller et al 1978 Paterne et al 1986 1988 1990 Langone etal 1996) and in lake sequences in southern Italy such as Lago Grande di Monticchio(Newton amp Dugmore 1993 Narcisi 1996 Allen et al 1999) and central Italy such asLago Albano near Rome (Calanchi et al 1996) Some work has also been conducted
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European tephrochronological framework for Termination 1 785
in or close to the volcanic source areas in an attempt to establish the full sequenceof volcanic eruptions during the Late Quaternary (see for example Di Vito et al 1999) There are nine Italian tephras reported from marine and lake sequences thatdate from the period between 185 and 80 14C ka BP In all instances the recordsare of visible layers of tephra The ages of some of these are poorly established atpresent with conregicting data obtained from dinoterent sites The ages suggested intable 1 are those favoured in the most recent publications but these may requirere-assessment in the light of future research
The two oldest known tephras in the time-period of interest are the L9 and Green-ish Tephras both recorded as separate features within the annually laminated Lagodi Monticchio maar sequence The lowest of the two L9 is considered to be the cor-relative of the `basalrsquo plinian eruption of Vesuvius (Narcisi 1996) Age estimates ofa palaeosol that underlies the Vesuvius tephra sequence are ca 1617 14C ka BP forthis event (Delibrias et al 1979) L9 has a trachytic composition very similar to theGreenish Tephra (table 1) However L9 which is also a product of Vesuvius is foundstratigraphically below the Greenish Tephra in the Lago di Monticchio core TheGreenish Tephra is dated in the Monticchio sequence to 17 560 varve yr BP (Allenet al 1999) and has a calibrated radiocarbon age estimate of 17 830 sect 300 cal BP(Andronico et al 1995) Both tephras have a dominantly eastwards dispersal basedon the occurrences of visible layers (Santacroce 1987 Narcisi 1996) Both tephrasalso have a trachytic composition and as can be seen from table 1 the reportedgeochemical spectra are very close indeed with the standard deviations overlappingfor almost every major element This could present problems for tephrostratigra-phy where only one of the tephras is evident in a sediment sequence in particularbecause they are so close in age This is a good example of where an analysis oftrace and rare earth elements might be required to make a clear distinction betweentephras with very similar major oxide concentrations
The Y-1 Tephra also termed the Biancavilla Montalto Ignimbrite (Vezzoli 1991)is a product of Etna and has been identishy ed as a visible benmoritic tephra horizonthroughout the central Mediterranean (Paterne et al 1988) including central Italyand the Adriatic Sea (Vezzoli 1991 Narcisi 1993 Calanchi et al 1996) It has anestimated age of ca 140 14C ka BP The Unita dei Tefra Superiori tephra which hasbeen detected as far east as Lago di Monticchio in south-central Italy (Narcisi 1996)is also dated to ca 140 14C ka BP (Alessio et al 1976) but it is thought that thesource of this tephra lies in the Phlegrean Fields No geochemical data are availablefrom the presumed source region|the data reported in table 1 were obtained fromthe Lago di Monticchio record (Narcisi 1996)
The NYT which is equivalent to the C-2 tephra reported from various marinesequences has also been traced throughout central Italy and the Adriatic Sea (Pat-erne et al 1988 Calanchi et al 1996 Di Vito et al 1999) (shy gure 2) In the centralApennines region it formed the parent material for a soil that started to developat the beginning of the Holocene period (Frezzotti amp Narcisi 1996) Also originatingfrom the Campi Flegrei caldera it is dated to ca 120 14C ka BP (Di Vito et al 1999) Published geochemical data based on EDS indicate three dinoterent geochemicalpopulations varying from latite to phonotrachyte in composition (Orsi et al 1992Paterne et al 1988) (table 1) We report in x 4 of this paper on new data obtainedfrom the NYT by WDS and it is the mean of these new data that is included intable 1 Comparisons with the previously published EDS data are provided (table 1)
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786 S M Davies and others
The new data indicate clearly that the NYT originated from the Campanian volcaniccentre
In the interval between the dispersal of the NYT (ca 120 14C ka BP) and 95 14Cka BP there appear to have been as many as 34 eruptions in the Campi Flegrei caldera(Di Vito et al 1999) Of these only one appears to have been detected widely in theregion the Pomici Principali (also termed the Agnano Formation or C-1 tephra inmarine records (Paterne et al 1988) This was the product of the highest magnitudeeruption from this epoch and is dated to between 976 sect 300 and 1032 sect 50 14C kaBP (Delibrias et al 1979 Di Vito et al 1999) or to 122 varve ka BP based on theMonticchio varve chronology (Allen et al 1999) It is trachytic in composition andappears to have had a mainly eastwards dispersal
The Mercato Tephra dated to ca 80 14C ka BP and originally analysed usingEDS has a phonolitic composition and is believed to have been generated by Vesu-vius (Paterne et al 1988) New WDS data obtained from reference samples col-lected from an exposure to the west of Naples support these conclusions (table 1 andAppendix A) The silica content of the WDS analyses are ca 3 lower than thoseobtained using EDS (table 1) which may reregect the fact that the EDS data werenormalized
The only tephra listed in table 1 that is thought to have originated from the AeolianIslands is the Pollara pumice also referred to as the E2 tephra in marine sequences(Paterne et al 1986 1988) The limited geochemical data available so far suggest itto be the only Italian tephra listed in table 1 that is rhyolitic in composition Littlemore is known about this ash which has not been recorded extensively except thatits age is estimated to be ca 130 14C ka BP (Keller 1980)
5 Extending the known distributions of European tephras
Figure 2 summarizes schematically the known distributions of three of the tephrasreferred to in the preceding section the VA the LST and the NYT Following theintroduction of a laboratory method that enables the detection of micro-tephra parti-cles in mineral-rich sediment the VA has been traced to sites that are located muchfarther south (into The Netherlands) and east (as far as St Petersburg) than thedistribution limits based on occurrences of visible layers of the ash As a result con-tinental sequences over a much larger area in northern Europe can now be correlateddirectly with marine and ice-core records using the VA as a time-parallel marker
This suggests therefore that other prominent ash layers such as the LST andNYT should also be detectable over larger tracts of Europe than is presently thecase if suitable sites are examined for the presence of micro-tephra horizons To testthis assertion we examined lake sediment deposits of Last Termination age froma site in the northern Apennines in order to establish whether the NYT could bedetected in micro-tephra form The site selected Prato Spilla `Crsquo lies well to thenorth of the localities in central and southern Italy and in the Adriatic Sea fromwhich visible records of the NYT have been reported Prato Spilla `Crsquo lies at an alti-tude of ca 1350 m in the Appennino Parmense ca 60 km south of Parma and 15 kmeast of Pontremoli The site contains a continuous sediment sequence spanning theLast Termination and most of the Holocene Detailed pollen and coleopteran strati-graphical records which have been radiocarbon dated have been published for thissite (Lowe 1992 Ponel amp Lowe 1992 Lowe amp Watson 1993)
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European tephrochronological framework for Termination 1 787
Figure 6 Light microscope photograph of an NYT glass shard from Prato Spilla Crsquosequence assigned on geochemical grounds to the NYT
The methods adopted for sub-sampling of the Prato Spilla `Crsquo sequence for thequantishy cation of glass shard concentrations and for subsequent electron microprobeanalysis of selected glass shards followed those described elsewhere (Turney 1998)In summary contiguous samples of 1 cm stratigraphic interval were extracted fromthe sequence to establish presenceabsence of glass shards Each of the 1 cm3 blocksin which tephra particles was detected was then examined with more care andshard concentrations were quantishy ed for each sub-sample Micro-tephra particleswere detected in shy ve samples (shy gure 6) but were predominantly clustered around500 cm in the part of the sequence assigned on pollen-stratigraphic grounds to theLate Glacial Interstadial or the `Allerfrac12drsquo|indeed the part of the succession in whichthe NYT would be expected to occur Peak concentrations of micro-tephra particlesreach 225 shards cmiexcl3 and are conshy ned to a single 1 cm thick sample in the sequencewhich probably represents the time of maximum deposition of the ash
Electron microprobe measurements based on WDS were obtained from the surfacesof 21 separate glass shards extracted from the sample with peak shard concentrations(Appendix A) Since only EDS measurements were available for the NYT prior to thepresent study we also obtained WDS measurements from 17 shards extracted fromthe visible layer of NYT that is exposed on Procida Island which lies in the type-locality for the NYT close to the city of Naples (Appendix A) The results providenot only a more comprehensive geochemical dataset for the NYT than was previ-ously available but also a consistent basis for comparison with the Prato Spilla `Crsquodataset All of the WDS data reported here (Appendix A) were measured at the samelaboratory (Tephrochronology Analytical Unit University of Edinburgh) using thesame sample pretreatment and preparation protocol The WDS results for the NYTdinoter to a minor degree from the EDS results (table 1 and Appendix A) especiallywith respect to the amounts of silica aluminium and calcium measured The EDS
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788 S M Davies and others
4 8FeO ()
TiO
2 (
) Neapolitan Yellow Tuff(Procida)Neapolitan Yellow Tuff(Prato Spilla lsquoCrsquo)
0
1
2
3
40 50 60 70
MgO
(
)
SiO2 ()
K2O
(
)
40 50 60 70
0
04
08
4
8
12
SiO2 ()
(a)(b)
(c)
Figure 7 Bi-plots of SiO2 K2 O SiO2 MgO and FeOTiO2 for the WDS analyses obtainedfrom glass shards of the NYT from Procida (Naples) and Prato Spilla Crsquo Means and standarddeviations are shown
results show a higher degree of statistical scatter than the WDS measurements whichmay reregect the fact that the data were normalized combined with the inreguence ofvariation in water content between shards
There is a very close correspondence between the WDS data for the Prato Spilla `Crsquomicro-tephra shards and those obtained from the type-material near Naples (shy g-ure 7) The geochemical data strongly suggest therefore that the NYT is representedat the Prato Spilla `Crsquo site by a discrete layer of micro-tephra particles This conclu-sion is compatible with the pollen-stratigraphic data from the site and accords withage estimates for the NYT (ca 120 14C ka BP) obtained from other sites (Paterneet al 1990)
These results encourage us to believe that many if not all of the tephras listedin table 1 will be detectable over much larger tracts of Europe than is presently thecase if appropriate research is undertaken to detect layers of micro-tephra particlesin selected sites The authors are presently engaged in a major continent-wide pro-gramme of research in collaboration with a number of European research groupsdesigned to test this hypothesis The focus in this research is on those parts of Europewhere we expect to shy nd overlapping `apronsrsquo of tephra deposition originating fromthe Italian Eifel Massif Central and Icelandic provinces For example a number ofsites in parts of southern France northern Italy and perhaps western Switzerlandmay have received inreguxes of micro-tephra originating from the Italian and Eifelprovinces and perhaps also from the Massif Central Sites in parts of Germany Den-mark and southern Sweden for example may in turn have received tephra depositsfrom both of the Icelandic and Eifel provinces If this proves to be the case then thestage will be set for the construction of a tephrostratigraphical framework for Europewhich will enable Last Termination sequences to be correlated on a continent-widebasis using micro- and visible tephra layers as time-parallel stratigraphic markersFurthermore there is also the possibility that other tephras remain to be discovered
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European tephrochronological framework for Termination 1 789
those which either because of the magnitude or nature of some volcanic eruptionswere distributed over parts of Europe in micro-tephra form only
6 European tephrostratigraphy and the chronology of eventsduring the Last Termination and Early Holocene
One of the crucial issues in Late Quaternary palaeoenvironmental research thatremains to be resolved is the degree to which climatic events inferred from oceanicterrestrial and ice-core records were synchronous during the Last Termination andEarly Holocene If the ice-core records provide realistic estimates of the rates anddurations of climatic events during this period then comparisons between individ-ual records have to be enotected with at least a decadal precision The problem thispresents and the role that tephrostratigraphy can play in resolving some of thedimacr culties involved are put into perspective in shy gure 8
Figure 8 shows some of the data used to calibrate radiocarbon dates (the LakeSuigetsu and Cariaco Basin datasets) plotted against the GRIP ss08c ice-core recordof macr 18O variations The latter has been selected by the INTIMATE group as an arbi-trary and temporary standard for this period and used to deshy ne an event stratig-raphy scheme (shy gure 1) for the Last Termination (see Bjorck et al 1998 Walker etal 2001) As has been alluded to in earlier sections of this paper the uncertaintiesassociated with all of the dating methods currently employed preclude precise com-parisons of ice-core marine and terrestrial records Oceanic and terrestrial recordsmostly rely upon radiocarbon dating locally supplemented in a few cases by varvechronology Imprecisions in radiocarbon dates can arise through site-specishy c fac-tors (eg hard-water or mineral carbon errors in freshwater sequences and reservoirerrors in marine sequences) sample selection laboratory measurements of 14C activ-ity and other factors (Lowe amp Walker 2000) Further imprecision may be introducedby the calibration of radiocarbon dates since the uncertainties in the dataset usedto calibrate pre-Holocene radiocarbon dates INTCAL98 are far higher than forthe Holocene which is based on dendro-calibration (Stuiver et al 1998) There arealso uncertainties anotecting varve chronologies while the ss08c ice-core chronologyfor the Last Termination dinoters signishy cantly from the GISP2 record and indeedfrom other models of the GRIP record (Lowe et al 2001) Published comparisonsbetween ice-core marine and terrestrial records for the Last Termination seldom takeinto account the true magnitude of the dating uncertainties involved and frequentlyemploy circular reasoning
Figure 8 shows the positions on the radiocarbon time-scale of 20 of the tephrasdiscussed earlier in this paper these being the ones for which reasonably conshy dentradiocarbon age estimates can be made (though these will be subject to revised esti-mates in the future) A high number of these occur in the period 14080 14C kaBP but we conshy dently anticipate the discovery in the future of additional tephras(perhaps in micro-tephra form only) which will date to the period 185140 14C kaBP Tephras detected in the GRIP ice core over the same time-interval are plottedon the calendar time-scale in shy gure 8 By providing key `time-linesrsquo between recordstephrostratigraphy can help to resolve some of the dating uncertainties referredto earlier by for example enabling direct comparisons of discrepant age estimatesobtained using dinoterent methods (cf Litt et al 2001) It can also provide estimatesof the magnitudes of the reservoir errors that anotected various marine sectors at dif-
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790 S M Davies and others
-44
-40
-36
-32
cale
ndar
yea
rs B
P
8000
9000
10 0
00
11 0
00
12 0
00
13 0
00
14 0
00
15 0
00
16 0
00
17 0
00
18 0
00
14C age (BP)
VA
SA
Un
Un
Un
Un
Un
BF
Hol
ocen
eG
S-1
GI-
1aG
I-1b
GI-
1cG
I-1d
GI-
1eG
S-2
aG
S-2
bG
S-
2c
Bor
robo
l
La
Nug
egravere
Laa
cher
See
God
ivel
le 5
amp I
-TH
OL
-2
Puy
de D
ocircme
I-T
HO
L-1
Saks
unar
vatn
Houmlg
stor
psm
osse
nU
lmen
er M
aar
amp L
3574
radiocarbon dated European tephra horizons
Cho
pine
Kili
an V
asse
tM
erca
to
God
ivel
le 4
Pom
ici P
rinc
ipal
i amp V
edde
Polla
ra p
umic
eK
OL
-GS-
2 amp
GS
-2B
AS-
12
3
GS
-2B
AS-
4 U
nita
dei
Tef
raSu
peri
ori amp
laye
r Y
-1
Gre
enis
h
L9
20 0
0018
000
16 0
0014
000
12 0
0010
000
-44
-40
-36
-32
800
600
400
200 0
GISP2 volcanicsulphate conc (ppb)
1000
Nea
polit
an Y
ello
w T
uff
GISP2 18O (permil) dGRIP 18O (permil) d
Figure 8 For description see opposite
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European tephrochronological framework for Termination 1 791
ferent times through a comparison of radiocarbon dates obtained from marine andterrestrial horizons in which the same tephra has been detected (see for exampleAustin et al 1995 Bondevik et al 2001 Haregidason et al 2000) Tephrostratigraphymay provide an independent test of suggestions that some of the climatic changesduring the Last Termination were time-transgressive as illustrated for some appar-ently contrasting climatic trends in Iceland Britain and NW Russia (Lowe 2001) Ofparticular importance as far as establishing `leadsrsquo and `lagsrsquo in climatic changes isconcerned are the tephra records from the Greenland ice cores The discovery of theVedde and Saksunarvatn ashes in the GRIP record (Gronvold et al 1995) alreadyprovides a basis for making direct comparisons between marine terrestrial and ice-core records It is a matter of some urgency that the incidence of tephra depositsin the Greenland ice cores be more fully explored in the hope that this will lead tothe recognition of additional time-parallel links between the ice-core records on theone hand and oceanic and terrestrial records on the other An investigation of thenew NordGRIP record for this purpose is currently in progress (S M Davies 2002unpublished data)
Finally a fuller and more reshy ned tephrostratigraphical scheme for Europe will alsohave other applications It will provide an important database for those investigatingthe timing and frequency of volcanic eruptions in Europe during the past 20 000 yror so as well as of the geochemical evolution of the dinoterent volcanic centres overthat period A fuller record of the distribution of micro-tephras may also provideinformation on atmospheric circulation patterns during the dispersal and depositionperiods as well as on the nature and altitude of the eruption columns which mayin turn provide inferences about magma viscosity
This paper is a contribution to the INTIMATE project of the INQUA Palaeoclimate Com-mission and the work is supported by a Leverhulme Trust Research project (grant allocationnumber F07537C) entitled Testing hypotheses of rapid climate change using tephrochronol-ogyrsquo SMDrsquo s contribution was completed during possession of a NERC PhD studentship(GT 0499ES162) We are extremely grateful to Dr Peter G Hill for his assistance withthe EPMA analyses at the Tephrochronology Analytical Unit University of Edinburgh We alsothank Dr G Mastrolorenzo (Vesuvius Observatory) and Miss G Swindle for assistance duringthe macreld investigations in Naples Thanks are also expressed to two anonymous reviewers forcomments on an earlier draft
Appendix A
Table 2 shows the major oxide concentrations of NYT glass shards from Procidaand Prato Spilla `Crsquo and of the Mercato Tephra from the Naples area (see x 4 forsite context) All oxides are shown as weight and total iron is expressed as FeO
Figure 8 Radiocarbon calibration curve for Termination 1 and the Early Holocene compared with theGRIP macr 18 O event stratigraphy the GRIP ss08c and GISP2 macr 18 O records (wwwngdcnoaagov) andknown tephra horizons from this period The shaded areas represent the cooler climatic episodes andare labelled with the Greenland stratotype terminology (Bjorck et al 1998) Where radiocarbon agesare reported in table 1 as a range the mean is given here Abbreviations for GRIP horizons are asfollows Un unknown (approximate positions are given (S Johnsen 2001 personal communication))SA Saksunarvatn Ash VA Vedde Ash BF Black Feather Sulphate concentrations from the GISP2record are also shown (Zielinski et al 1996) Open circles denote radiocarbon calibration data fromLake Suigetsu (Kitagawa amp van der Plicht 2000) Filled circles denote radiocarbon calibration data fromCariaco Basin assuming a marine reservoir age of 420 14 C yr (Hughen et al 1998)
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792 S M Davies and others
Tab
le2
Majo
roxi
de
con
cen
trati
on
sof
NY
Tgl
ass
shard
sfr
om
Pro
cida
an
dP
rato
Spil
laC
rsquoan
dof
the
Mer
cato
Tep
hra
from
the
Naple
sare
a(s
eex4
for
site
con
text
)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
roci
da)
1584
204
0177
634
201
106
828
635
197
5969
1W
DS
2598
603
9178
027
101
204
924
244
583
4965
8W
DS
3586
604
5173
631
100
805
924
342
183
0951
9W
DS
4583
903
9177
933
000
906
924
540
486
9958
3W
DS
5605
106
8179
126
901
204
923
243
086
1976
4W
DS
6591
704
5177
332
801
006
425
740
887
8968
0W
DS
7581
804
1178
031
501
107
125
640
086
9956
1W
DS
8589
504
2179
533
701
506
926
740
987
5970
4W
DS
9592
003
9178
135
101
007
026
443
585
7972
7W
DS
10
591
404
2174
631
601
105
723
442
482
6957
0W
DS
11
593
403
6177
131
301
506
726
439
188
5967
6W
DS
12
588
103
8176
128
100
505
525
141
583
4952
1W
DS
13
577
003
8176
533
500
807
228
140
384
8952
0W
DS
14
586
004
7179
735
300
706
827
842
984
6968
5W
DS
15
588
104
2180
629
400
505
924
937
993
0964
5W
DS
16
579
603
9178
536
501
308
228
836
087
1959
9W
DS
17
580
103
9177
631
500
907
327
039
488
9956
6W
DS
mea
n588
104
2177
631
901
006
525
940
686
9962
8
sd
(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(07
8)
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 793
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
rato
Spil
laC
rsquo)
1552
105
4177
247
401
914
38
735
578
9951
1W
DS
2557
305
7179
845
701
512
640
136
581
5960
6W
DS
3595
004
4173
724
302
003
117
652
877
8950
7W
DS
4575
704
2179
433
001
406
627
043
083
6953
7W
DS
5599
904
0178
826
401
304
421
841
688
4966
5W
DS
6591
103
8177
826
601
105
022
443
888
8960
2W
DS
7565
304
5180
939
501
410
532
535
791
8962
1W
DS
8597
606
9180
826
501
604
821
546
684
6970
7W
DS
9571
805
6179
939
801
109
932
240
883
6964
7W
DS
10
588
603
7176
527
601
104
721
042
487
7953
3W
DS
11
559
404
9180
544
501
812
339
435
878
6957
2W
DS
12
594
704
0181
328
301
705
522
144
785
6967
9W
DS
13
611
103
7187
016
900
802
419
938
195
9975
8W
DS
14
599
204
4181
128
601
404
620
844
986
6971
6W
DS
15
601
204
4177
328
302
004
722
446
385
5972
1W
DS
16
595
104
5176
428
801
504
722
744
884
3962
8W
DS
17
603
704
1177
825
101
503
520
348
181
2965
3W
DS
18
558
704
5179
647
401
813
139
836
879
0960
7W
DS
19
589
602
8178
830
901
606
622
436
091
8960
5W
DS
20
553
606
3178
647
401
913
840
136
978
0956
6W
DS
21
579
004
0175
739
000
708
328
338
286
7959
9W
DS
mea
n582
804
6179
033
401
507
427
341
484
8962
1
sd
(1
87)
(01
0)
(02
7)
(09
2)
(00
4)
(03
9)
(08
0)
(04
9)
(05
0)
(07
0)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
794 S M Davies and others
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)
1575
202
7194
219
701
101
016
374
766
9951
8W
DS
2575
802
9194
523
902
201
520
273
564
5959
0W
DS
3574
301
4205
219
101
100
416
481
266
1965
2W
DS
4575
500
7206
018
002
000
415
181
669
3968
6W
DS
5580
000
9208
018
601
300
515
883
367
1975
5W
DS
6571
001
0206
016
101
600
515
078
967
1957
2W
DS
7577
501
1201
117
101
500
620
675
655
4950
5W
DS
8573
700
9212
717
101
900
815
187
564
2973
9W
DS
9580
301
3208
715
801
400
824
81
754
1968
1W
DS
10
574
400
6211
18
402
00
516
480
567
8971
6W
DS
11
577
200
7214
212
501
200
829
879
247
962
6W
DS
12
572
200
9211
217
301
501
15
980
465
9966
3W
DS
13
571
800
7210
417
402
201
16
184
467
2971
2W
DS
14
567
300
9208
916
901
400
917
383
262
5959
3W
DS
15
568
600
8205
918
202
101
414
682
666
6960
8W
DS
16
572
501
1211
318
202
01
215
884
364
5970
9W
DS
17
572
901
2212
916
502
101
215
883
667
2973
4W
DS
18
573
01
4211
716
301
801
416
83
365
5970
4W
DS
19
569
201
1207
418
602
101
414
982
964
961
6W
DS
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
3)
(04
2)
(01
3)
(00
1)
(00
2)
(01
)(0
39)
(01
1)
(02
5)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
References
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Phil Trans R Soc Lond A (2002)
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Gronvold K Oskarsson N Johnsen S J Clausen H B Hammer C U Bond G amp Bard E1995 Ash layers from Iceland in the GRIP ice core correlated with oceanic and land sedimentsEarth Planet Sci Lett 135 149155
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Hoek W Z amp Bohncke S J P 2001 Oxygen isotope wiggle matching as a tool for synchronisingice-core and terrestrial records over Termination 1 Quat Sci Rev 20 12511264
Hughen K A Overpeck J T Peterson L C amp Trumbore S 1996 Rapid climate changes inthe tropical Atlantic region during the last deglaciation Nature 380 5153
Hughen K A Overpeck J T amp Lehman J 1998 A new 14 C calibration data set for the LastDeglaciation Radiocarbon 39 483494
Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
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Hunt J B Clift P D Lacasse C Vallier T L amp Werner R 1998 Standardisation ofelectron probe microanalysis of glass geochemistry In Proc ODP Scientimacrc Results vol 152pp 8591 College Station TX Ocean Drilling Program
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Juvignparae E Kozarski S amp Nowaczyk B 1995 The occurrence of Laacher See Tephra in Pomera-nia NW Poland Boreas 24 225231
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Kitagawa H amp van der Plicht J 2000 Atmospheric radiocarbon calibration beyond 11 900 calBP from Lake Suigetsu laminated sediments Radiocarbon 42 369380
Kvamme T Mangerud J Furnes H amp Ruddiman W F 1989 Geochemistry of Pleistoceneash zones in cores from the North Atlantic Norsk Geol Tids 69 251272
Lacasse C Sigurdsson H Johannesson H Paterne M amp Carey S 1995 Source of Ash zone 1in the North Atlantic Bull Volcanol 57 1832
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Larsen G 2000 Holocene volcanism in Iceland and tephrochronology as a tool in volcanologyIn Iceland 2000 modern processes and past environments Keele University UK
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Litt T Brauer A Goslar T Merkt J Balaga K Muller H Ralska-Jasiewiczowa MStebich M amp Negendank J F W 2001 Correlation and synchronisation of Lateglacialcontinental sequences in northern Central Europe based on annually laminated lacustrinesediments Quat Sci Rev 20 12331249
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Lowe J J Hoek W Z amp INTIMATE group 2001 Inter-regional correlation of palaeoclimaticrecords for the Last GlacialInterglacial transition a protocol for improved precision recom-mended by the INTIMATE project group Quat Sci Rev 20 11751187
Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
Mangerud J Lie S E Furnes H Kristiansen I L amp Liquest mo L 1984 A Younger Dryas ashbed in western Norway and its possible correlation with tephra beds from the Norwegian Seaand North Atlantic Quat Res 21 85104
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Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
784 S M Davies and others
dinoterent eruption phases These are grouped together as the Laacher See TephraFormation but the three individual units can be traced within and between a seriesof depositional fans The geochemical data obtained from these three LST layersshow signishy cant variations as reregected in the ternary plots (shy gure 4)
The Early Holocene Ulmener Maar Tephra (UMT) is of rhyolitic composition andappears to be restricted to sites in Germany though this conclusion is also based onrecords of visible tephras only It is dated to ca 956 14C ka BP and to 110 varve ka(Zolitschka et al 1995 Litt et al 2001)
(c) Massif Central province
The Massif Central tephras are mainly of basaltic trachyandesitic compositionwhich is distinct from the other ash provinces (shy gures 3 and 4) and their known dis-tributions are mostly conshy ned to the Massif Central region The ages of the MassifCentral tephras are based on radiocarbon dates obtained from mire and lake sedi-ments which `bracketrsquo the tephras The La Nugsup3ere Tephra with an age of 114 14C kaBP is the oldest Massif Central tephra identishy ed so far within the time-span of inter-est (Etlicher et al 1987 Juvigne et al 1996) The two Godivelle Tephras (5 and 4)are close in age but extensive radiocarbon dating suggests distinct ages of 107and 103 14C ka BP respectively (Juvigne et al 1996) The age of the Puy de DomeTephra is less certain as the estimate is based on only one radiocarbon date froma site in the southern Chaplusmn ne des Puys (table 1) This tephra is thought to havea trachyte composition (Juvigne 1993) although no major element concentrationshave yet been published
The ChopineKilianVasset tephras are thought to be derived from three separateEarly Holocene eruptions although the stratigraphic succession is not known atpresent These trachytic tephras have been radiocarbon dated to ca 854sect150 14C kaBP but are thought to have erupted separately within ca 260 yr (Juvigne et al 1996) This series of tephras is considerably more widespread than the others fromthe region having been identishy ed as far east as the Jura Mountains (Martini amp Duret1965 Martini 1970) Some other ash falls that originated from the Chaplusmn ne des Puysappear to be of local importance only (Vernet et al 1998 Vernet amp Raynal 2001)Geochemical data are currently available for only three of the Massif Central tephrasand so far as is known no attempt has yet been made to identify these tephras inmicro-tephra form
(d ) Italian provinces
The Italian tephras from this period can be assigned to three main volcanic com-plexes the Campanian volcanic shy elds around Naples Etna on Sicily and the AeolianIslands The Campanian complex which includes the Phlegrean Fields Vesuviusand Ischia is mainly trachytic in composition with a geochemical spectrum that isquite distinct from those of the Etna complex and of the Aeolian Islands (shy gure 3)Tephras originating from one or more of these three complexes have been detectedin marine cores from the Tyrrhenian and Adriatic seas as well as other parts of theMediterranean Sea (Keller et al 1978 Paterne et al 1986 1988 1990 Langone etal 1996) and in lake sequences in southern Italy such as Lago Grande di Monticchio(Newton amp Dugmore 1993 Narcisi 1996 Allen et al 1999) and central Italy such asLago Albano near Rome (Calanchi et al 1996) Some work has also been conducted
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European tephrochronological framework for Termination 1 785
in or close to the volcanic source areas in an attempt to establish the full sequenceof volcanic eruptions during the Late Quaternary (see for example Di Vito et al 1999) There are nine Italian tephras reported from marine and lake sequences thatdate from the period between 185 and 80 14C ka BP In all instances the recordsare of visible layers of tephra The ages of some of these are poorly established atpresent with conregicting data obtained from dinoterent sites The ages suggested intable 1 are those favoured in the most recent publications but these may requirere-assessment in the light of future research
The two oldest known tephras in the time-period of interest are the L9 and Green-ish Tephras both recorded as separate features within the annually laminated Lagodi Monticchio maar sequence The lowest of the two L9 is considered to be the cor-relative of the `basalrsquo plinian eruption of Vesuvius (Narcisi 1996) Age estimates ofa palaeosol that underlies the Vesuvius tephra sequence are ca 1617 14C ka BP forthis event (Delibrias et al 1979) L9 has a trachytic composition very similar to theGreenish Tephra (table 1) However L9 which is also a product of Vesuvius is foundstratigraphically below the Greenish Tephra in the Lago di Monticchio core TheGreenish Tephra is dated in the Monticchio sequence to 17 560 varve yr BP (Allenet al 1999) and has a calibrated radiocarbon age estimate of 17 830 sect 300 cal BP(Andronico et al 1995) Both tephras have a dominantly eastwards dispersal basedon the occurrences of visible layers (Santacroce 1987 Narcisi 1996) Both tephrasalso have a trachytic composition and as can be seen from table 1 the reportedgeochemical spectra are very close indeed with the standard deviations overlappingfor almost every major element This could present problems for tephrostratigra-phy where only one of the tephras is evident in a sediment sequence in particularbecause they are so close in age This is a good example of where an analysis oftrace and rare earth elements might be required to make a clear distinction betweentephras with very similar major oxide concentrations
The Y-1 Tephra also termed the Biancavilla Montalto Ignimbrite (Vezzoli 1991)is a product of Etna and has been identishy ed as a visible benmoritic tephra horizonthroughout the central Mediterranean (Paterne et al 1988) including central Italyand the Adriatic Sea (Vezzoli 1991 Narcisi 1993 Calanchi et al 1996) It has anestimated age of ca 140 14C ka BP The Unita dei Tefra Superiori tephra which hasbeen detected as far east as Lago di Monticchio in south-central Italy (Narcisi 1996)is also dated to ca 140 14C ka BP (Alessio et al 1976) but it is thought that thesource of this tephra lies in the Phlegrean Fields No geochemical data are availablefrom the presumed source region|the data reported in table 1 were obtained fromthe Lago di Monticchio record (Narcisi 1996)
The NYT which is equivalent to the C-2 tephra reported from various marinesequences has also been traced throughout central Italy and the Adriatic Sea (Pat-erne et al 1988 Calanchi et al 1996 Di Vito et al 1999) (shy gure 2) In the centralApennines region it formed the parent material for a soil that started to developat the beginning of the Holocene period (Frezzotti amp Narcisi 1996) Also originatingfrom the Campi Flegrei caldera it is dated to ca 120 14C ka BP (Di Vito et al 1999) Published geochemical data based on EDS indicate three dinoterent geochemicalpopulations varying from latite to phonotrachyte in composition (Orsi et al 1992Paterne et al 1988) (table 1) We report in x 4 of this paper on new data obtainedfrom the NYT by WDS and it is the mean of these new data that is included intable 1 Comparisons with the previously published EDS data are provided (table 1)
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786 S M Davies and others
The new data indicate clearly that the NYT originated from the Campanian volcaniccentre
In the interval between the dispersal of the NYT (ca 120 14C ka BP) and 95 14Cka BP there appear to have been as many as 34 eruptions in the Campi Flegrei caldera(Di Vito et al 1999) Of these only one appears to have been detected widely in theregion the Pomici Principali (also termed the Agnano Formation or C-1 tephra inmarine records (Paterne et al 1988) This was the product of the highest magnitudeeruption from this epoch and is dated to between 976 sect 300 and 1032 sect 50 14C kaBP (Delibrias et al 1979 Di Vito et al 1999) or to 122 varve ka BP based on theMonticchio varve chronology (Allen et al 1999) It is trachytic in composition andappears to have had a mainly eastwards dispersal
The Mercato Tephra dated to ca 80 14C ka BP and originally analysed usingEDS has a phonolitic composition and is believed to have been generated by Vesu-vius (Paterne et al 1988) New WDS data obtained from reference samples col-lected from an exposure to the west of Naples support these conclusions (table 1 andAppendix A) The silica content of the WDS analyses are ca 3 lower than thoseobtained using EDS (table 1) which may reregect the fact that the EDS data werenormalized
The only tephra listed in table 1 that is thought to have originated from the AeolianIslands is the Pollara pumice also referred to as the E2 tephra in marine sequences(Paterne et al 1986 1988) The limited geochemical data available so far suggest itto be the only Italian tephra listed in table 1 that is rhyolitic in composition Littlemore is known about this ash which has not been recorded extensively except thatits age is estimated to be ca 130 14C ka BP (Keller 1980)
5 Extending the known distributions of European tephras
Figure 2 summarizes schematically the known distributions of three of the tephrasreferred to in the preceding section the VA the LST and the NYT Following theintroduction of a laboratory method that enables the detection of micro-tephra parti-cles in mineral-rich sediment the VA has been traced to sites that are located muchfarther south (into The Netherlands) and east (as far as St Petersburg) than thedistribution limits based on occurrences of visible layers of the ash As a result con-tinental sequences over a much larger area in northern Europe can now be correlateddirectly with marine and ice-core records using the VA as a time-parallel marker
This suggests therefore that other prominent ash layers such as the LST andNYT should also be detectable over larger tracts of Europe than is presently thecase if suitable sites are examined for the presence of micro-tephra horizons To testthis assertion we examined lake sediment deposits of Last Termination age froma site in the northern Apennines in order to establish whether the NYT could bedetected in micro-tephra form The site selected Prato Spilla `Crsquo lies well to thenorth of the localities in central and southern Italy and in the Adriatic Sea fromwhich visible records of the NYT have been reported Prato Spilla `Crsquo lies at an alti-tude of ca 1350 m in the Appennino Parmense ca 60 km south of Parma and 15 kmeast of Pontremoli The site contains a continuous sediment sequence spanning theLast Termination and most of the Holocene Detailed pollen and coleopteran strati-graphical records which have been radiocarbon dated have been published for thissite (Lowe 1992 Ponel amp Lowe 1992 Lowe amp Watson 1993)
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European tephrochronological framework for Termination 1 787
Figure 6 Light microscope photograph of an NYT glass shard from Prato Spilla Crsquosequence assigned on geochemical grounds to the NYT
The methods adopted for sub-sampling of the Prato Spilla `Crsquo sequence for thequantishy cation of glass shard concentrations and for subsequent electron microprobeanalysis of selected glass shards followed those described elsewhere (Turney 1998)In summary contiguous samples of 1 cm stratigraphic interval were extracted fromthe sequence to establish presenceabsence of glass shards Each of the 1 cm3 blocksin which tephra particles was detected was then examined with more care andshard concentrations were quantishy ed for each sub-sample Micro-tephra particleswere detected in shy ve samples (shy gure 6) but were predominantly clustered around500 cm in the part of the sequence assigned on pollen-stratigraphic grounds to theLate Glacial Interstadial or the `Allerfrac12drsquo|indeed the part of the succession in whichthe NYT would be expected to occur Peak concentrations of micro-tephra particlesreach 225 shards cmiexcl3 and are conshy ned to a single 1 cm thick sample in the sequencewhich probably represents the time of maximum deposition of the ash
Electron microprobe measurements based on WDS were obtained from the surfacesof 21 separate glass shards extracted from the sample with peak shard concentrations(Appendix A) Since only EDS measurements were available for the NYT prior to thepresent study we also obtained WDS measurements from 17 shards extracted fromthe visible layer of NYT that is exposed on Procida Island which lies in the type-locality for the NYT close to the city of Naples (Appendix A) The results providenot only a more comprehensive geochemical dataset for the NYT than was previ-ously available but also a consistent basis for comparison with the Prato Spilla `Crsquodataset All of the WDS data reported here (Appendix A) were measured at the samelaboratory (Tephrochronology Analytical Unit University of Edinburgh) using thesame sample pretreatment and preparation protocol The WDS results for the NYTdinoter to a minor degree from the EDS results (table 1 and Appendix A) especiallywith respect to the amounts of silica aluminium and calcium measured The EDS
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788 S M Davies and others
4 8FeO ()
TiO
2 (
) Neapolitan Yellow Tuff(Procida)Neapolitan Yellow Tuff(Prato Spilla lsquoCrsquo)
0
1
2
3
40 50 60 70
MgO
(
)
SiO2 ()
K2O
(
)
40 50 60 70
0
04
08
4
8
12
SiO2 ()
(a)(b)
(c)
Figure 7 Bi-plots of SiO2 K2 O SiO2 MgO and FeOTiO2 for the WDS analyses obtainedfrom glass shards of the NYT from Procida (Naples) and Prato Spilla Crsquo Means and standarddeviations are shown
results show a higher degree of statistical scatter than the WDS measurements whichmay reregect the fact that the data were normalized combined with the inreguence ofvariation in water content between shards
There is a very close correspondence between the WDS data for the Prato Spilla `Crsquomicro-tephra shards and those obtained from the type-material near Naples (shy g-ure 7) The geochemical data strongly suggest therefore that the NYT is representedat the Prato Spilla `Crsquo site by a discrete layer of micro-tephra particles This conclu-sion is compatible with the pollen-stratigraphic data from the site and accords withage estimates for the NYT (ca 120 14C ka BP) obtained from other sites (Paterneet al 1990)
These results encourage us to believe that many if not all of the tephras listedin table 1 will be detectable over much larger tracts of Europe than is presently thecase if appropriate research is undertaken to detect layers of micro-tephra particlesin selected sites The authors are presently engaged in a major continent-wide pro-gramme of research in collaboration with a number of European research groupsdesigned to test this hypothesis The focus in this research is on those parts of Europewhere we expect to shy nd overlapping `apronsrsquo of tephra deposition originating fromthe Italian Eifel Massif Central and Icelandic provinces For example a number ofsites in parts of southern France northern Italy and perhaps western Switzerlandmay have received inreguxes of micro-tephra originating from the Italian and Eifelprovinces and perhaps also from the Massif Central Sites in parts of Germany Den-mark and southern Sweden for example may in turn have received tephra depositsfrom both of the Icelandic and Eifel provinces If this proves to be the case then thestage will be set for the construction of a tephrostratigraphical framework for Europewhich will enable Last Termination sequences to be correlated on a continent-widebasis using micro- and visible tephra layers as time-parallel stratigraphic markersFurthermore there is also the possibility that other tephras remain to be discovered
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European tephrochronological framework for Termination 1 789
those which either because of the magnitude or nature of some volcanic eruptionswere distributed over parts of Europe in micro-tephra form only
6 European tephrostratigraphy and the chronology of eventsduring the Last Termination and Early Holocene
One of the crucial issues in Late Quaternary palaeoenvironmental research thatremains to be resolved is the degree to which climatic events inferred from oceanicterrestrial and ice-core records were synchronous during the Last Termination andEarly Holocene If the ice-core records provide realistic estimates of the rates anddurations of climatic events during this period then comparisons between individ-ual records have to be enotected with at least a decadal precision The problem thispresents and the role that tephrostratigraphy can play in resolving some of thedimacr culties involved are put into perspective in shy gure 8
Figure 8 shows some of the data used to calibrate radiocarbon dates (the LakeSuigetsu and Cariaco Basin datasets) plotted against the GRIP ss08c ice-core recordof macr 18O variations The latter has been selected by the INTIMATE group as an arbi-trary and temporary standard for this period and used to deshy ne an event stratig-raphy scheme (shy gure 1) for the Last Termination (see Bjorck et al 1998 Walker etal 2001) As has been alluded to in earlier sections of this paper the uncertaintiesassociated with all of the dating methods currently employed preclude precise com-parisons of ice-core marine and terrestrial records Oceanic and terrestrial recordsmostly rely upon radiocarbon dating locally supplemented in a few cases by varvechronology Imprecisions in radiocarbon dates can arise through site-specishy c fac-tors (eg hard-water or mineral carbon errors in freshwater sequences and reservoirerrors in marine sequences) sample selection laboratory measurements of 14C activ-ity and other factors (Lowe amp Walker 2000) Further imprecision may be introducedby the calibration of radiocarbon dates since the uncertainties in the dataset usedto calibrate pre-Holocene radiocarbon dates INTCAL98 are far higher than forthe Holocene which is based on dendro-calibration (Stuiver et al 1998) There arealso uncertainties anotecting varve chronologies while the ss08c ice-core chronologyfor the Last Termination dinoters signishy cantly from the GISP2 record and indeedfrom other models of the GRIP record (Lowe et al 2001) Published comparisonsbetween ice-core marine and terrestrial records for the Last Termination seldom takeinto account the true magnitude of the dating uncertainties involved and frequentlyemploy circular reasoning
Figure 8 shows the positions on the radiocarbon time-scale of 20 of the tephrasdiscussed earlier in this paper these being the ones for which reasonably conshy dentradiocarbon age estimates can be made (though these will be subject to revised esti-mates in the future) A high number of these occur in the period 14080 14C kaBP but we conshy dently anticipate the discovery in the future of additional tephras(perhaps in micro-tephra form only) which will date to the period 185140 14C kaBP Tephras detected in the GRIP ice core over the same time-interval are plottedon the calendar time-scale in shy gure 8 By providing key `time-linesrsquo between recordstephrostratigraphy can help to resolve some of the dating uncertainties referredto earlier by for example enabling direct comparisons of discrepant age estimatesobtained using dinoterent methods (cf Litt et al 2001) It can also provide estimatesof the magnitudes of the reservoir errors that anotected various marine sectors at dif-
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790 S M Davies and others
-44
-40
-36
-32
cale
ndar
yea
rs B
P
8000
9000
10 0
00
11 0
00
12 0
00
13 0
00
14 0
00
15 0
00
16 0
00
17 0
00
18 0
00
14C age (BP)
VA
SA
Un
Un
Un
Un
Un
BF
Hol
ocen
eG
S-1
GI-
1aG
I-1b
GI-
1cG
I-1d
GI-
1eG
S-2
aG
S-2
bG
S-
2c
Bor
robo
l
La
Nug
egravere
Laa
cher
See
God
ivel
le 5
amp I
-TH
OL
-2
Puy
de D
ocircme
I-T
HO
L-1
Saks
unar
vatn
Houmlg
stor
psm
osse
nU
lmen
er M
aar
amp L
3574
radiocarbon dated European tephra horizons
Cho
pine
Kili
an V
asse
tM
erca
to
God
ivel
le 4
Pom
ici P
rinc
ipal
i amp V
edde
Polla
ra p
umic
eK
OL
-GS-
2 amp
GS
-2B
AS-
12
3
GS
-2B
AS-
4 U
nita
dei
Tef
raSu
peri
ori amp
laye
r Y
-1
Gre
enis
h
L9
20 0
0018
000
16 0
0014
000
12 0
0010
000
-44
-40
-36
-32
800
600
400
200 0
GISP2 volcanicsulphate conc (ppb)
1000
Nea
polit
an Y
ello
w T
uff
GISP2 18O (permil) dGRIP 18O (permil) d
Figure 8 For description see opposite
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European tephrochronological framework for Termination 1 791
ferent times through a comparison of radiocarbon dates obtained from marine andterrestrial horizons in which the same tephra has been detected (see for exampleAustin et al 1995 Bondevik et al 2001 Haregidason et al 2000) Tephrostratigraphymay provide an independent test of suggestions that some of the climatic changesduring the Last Termination were time-transgressive as illustrated for some appar-ently contrasting climatic trends in Iceland Britain and NW Russia (Lowe 2001) Ofparticular importance as far as establishing `leadsrsquo and `lagsrsquo in climatic changes isconcerned are the tephra records from the Greenland ice cores The discovery of theVedde and Saksunarvatn ashes in the GRIP record (Gronvold et al 1995) alreadyprovides a basis for making direct comparisons between marine terrestrial and ice-core records It is a matter of some urgency that the incidence of tephra depositsin the Greenland ice cores be more fully explored in the hope that this will lead tothe recognition of additional time-parallel links between the ice-core records on theone hand and oceanic and terrestrial records on the other An investigation of thenew NordGRIP record for this purpose is currently in progress (S M Davies 2002unpublished data)
Finally a fuller and more reshy ned tephrostratigraphical scheme for Europe will alsohave other applications It will provide an important database for those investigatingthe timing and frequency of volcanic eruptions in Europe during the past 20 000 yror so as well as of the geochemical evolution of the dinoterent volcanic centres overthat period A fuller record of the distribution of micro-tephras may also provideinformation on atmospheric circulation patterns during the dispersal and depositionperiods as well as on the nature and altitude of the eruption columns which mayin turn provide inferences about magma viscosity
This paper is a contribution to the INTIMATE project of the INQUA Palaeoclimate Com-mission and the work is supported by a Leverhulme Trust Research project (grant allocationnumber F07537C) entitled Testing hypotheses of rapid climate change using tephrochronol-ogyrsquo SMDrsquo s contribution was completed during possession of a NERC PhD studentship(GT 0499ES162) We are extremely grateful to Dr Peter G Hill for his assistance withthe EPMA analyses at the Tephrochronology Analytical Unit University of Edinburgh We alsothank Dr G Mastrolorenzo (Vesuvius Observatory) and Miss G Swindle for assistance duringthe macreld investigations in Naples Thanks are also expressed to two anonymous reviewers forcomments on an earlier draft
Appendix A
Table 2 shows the major oxide concentrations of NYT glass shards from Procidaand Prato Spilla `Crsquo and of the Mercato Tephra from the Naples area (see x 4 forsite context) All oxides are shown as weight and total iron is expressed as FeO
Figure 8 Radiocarbon calibration curve for Termination 1 and the Early Holocene compared with theGRIP macr 18 O event stratigraphy the GRIP ss08c and GISP2 macr 18 O records (wwwngdcnoaagov) andknown tephra horizons from this period The shaded areas represent the cooler climatic episodes andare labelled with the Greenland stratotype terminology (Bjorck et al 1998) Where radiocarbon agesare reported in table 1 as a range the mean is given here Abbreviations for GRIP horizons are asfollows Un unknown (approximate positions are given (S Johnsen 2001 personal communication))SA Saksunarvatn Ash VA Vedde Ash BF Black Feather Sulphate concentrations from the GISP2record are also shown (Zielinski et al 1996) Open circles denote radiocarbon calibration data fromLake Suigetsu (Kitagawa amp van der Plicht 2000) Filled circles denote radiocarbon calibration data fromCariaco Basin assuming a marine reservoir age of 420 14 C yr (Hughen et al 1998)
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792 S M Davies and others
Tab
le2
Majo
roxi
de
con
cen
trati
on
sof
NY
Tgl
ass
shard
sfr
om
Pro
cida
an
dP
rato
Spil
laC
rsquoan
dof
the
Mer
cato
Tep
hra
from
the
Naple
sare
a(s
eex4
for
site
con
text
)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
roci
da)
1584
204
0177
634
201
106
828
635
197
5969
1W
DS
2598
603
9178
027
101
204
924
244
583
4965
8W
DS
3586
604
5173
631
100
805
924
342
183
0951
9W
DS
4583
903
9177
933
000
906
924
540
486
9958
3W
DS
5605
106
8179
126
901
204
923
243
086
1976
4W
DS
6591
704
5177
332
801
006
425
740
887
8968
0W
DS
7581
804
1178
031
501
107
125
640
086
9956
1W
DS
8589
504
2179
533
701
506
926
740
987
5970
4W
DS
9592
003
9178
135
101
007
026
443
585
7972
7W
DS
10
591
404
2174
631
601
105
723
442
482
6957
0W
DS
11
593
403
6177
131
301
506
726
439
188
5967
6W
DS
12
588
103
8176
128
100
505
525
141
583
4952
1W
DS
13
577
003
8176
533
500
807
228
140
384
8952
0W
DS
14
586
004
7179
735
300
706
827
842
984
6968
5W
DS
15
588
104
2180
629
400
505
924
937
993
0964
5W
DS
16
579
603
9178
536
501
308
228
836
087
1959
9W
DS
17
580
103
9177
631
500
907
327
039
488
9956
6W
DS
mea
n588
104
2177
631
901
006
525
940
686
9962
8
sd
(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(07
8)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 793
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
rato
Spil
laC
rsquo)
1552
105
4177
247
401
914
38
735
578
9951
1W
DS
2557
305
7179
845
701
512
640
136
581
5960
6W
DS
3595
004
4173
724
302
003
117
652
877
8950
7W
DS
4575
704
2179
433
001
406
627
043
083
6953
7W
DS
5599
904
0178
826
401
304
421
841
688
4966
5W
DS
6591
103
8177
826
601
105
022
443
888
8960
2W
DS
7565
304
5180
939
501
410
532
535
791
8962
1W
DS
8597
606
9180
826
501
604
821
546
684
6970
7W
DS
9571
805
6179
939
801
109
932
240
883
6964
7W
DS
10
588
603
7176
527
601
104
721
042
487
7953
3W
DS
11
559
404
9180
544
501
812
339
435
878
6957
2W
DS
12
594
704
0181
328
301
705
522
144
785
6967
9W
DS
13
611
103
7187
016
900
802
419
938
195
9975
8W
DS
14
599
204
4181
128
601
404
620
844
986
6971
6W
DS
15
601
204
4177
328
302
004
722
446
385
5972
1W
DS
16
595
104
5176
428
801
504
722
744
884
3962
8W
DS
17
603
704
1177
825
101
503
520
348
181
2965
3W
DS
18
558
704
5179
647
401
813
139
836
879
0960
7W
DS
19
589
602
8178
830
901
606
622
436
091
8960
5W
DS
20
553
606
3178
647
401
913
840
136
978
0956
6W
DS
21
579
004
0175
739
000
708
328
338
286
7959
9W
DS
mea
n582
804
6179
033
401
507
427
341
484
8962
1
sd
(1
87)
(01
0)
(02
7)
(09
2)
(00
4)
(03
9)
(08
0)
(04
9)
(05
0)
(07
0)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
794 S M Davies and others
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)
1575
202
7194
219
701
101
016
374
766
9951
8W
DS
2575
802
9194
523
902
201
520
273
564
5959
0W
DS
3574
301
4205
219
101
100
416
481
266
1965
2W
DS
4575
500
7206
018
002
000
415
181
669
3968
6W
DS
5580
000
9208
018
601
300
515
883
367
1975
5W
DS
6571
001
0206
016
101
600
515
078
967
1957
2W
DS
7577
501
1201
117
101
500
620
675
655
4950
5W
DS
8573
700
9212
717
101
900
815
187
564
2973
9W
DS
9580
301
3208
715
801
400
824
81
754
1968
1W
DS
10
574
400
6211
18
402
00
516
480
567
8971
6W
DS
11
577
200
7214
212
501
200
829
879
247
962
6W
DS
12
572
200
9211
217
301
501
15
980
465
9966
3W
DS
13
571
800
7210
417
402
201
16
184
467
2971
2W
DS
14
567
300
9208
916
901
400
917
383
262
5959
3W
DS
15
568
600
8205
918
202
101
414
682
666
6960
8W
DS
16
572
501
1211
318
202
01
215
884
364
5970
9W
DS
17
572
901
2212
916
502
101
215
883
667
2973
4W
DS
18
573
01
4211
716
301
801
416
83
365
5970
4W
DS
19
569
201
1207
418
602
101
414
982
964
961
6W
DS
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
3)
(04
2)
(01
3)
(00
1)
(00
2)
(01
)(0
39)
(01
1)
(02
5)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
References
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Hughen K A Overpeck J T Peterson L C amp Trumbore S 1996 Rapid climate changes inthe tropical Atlantic region during the last deglaciation Nature 380 5153
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Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
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European tephrochronological framework for Termination 1 799
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Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
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Rose N L Golding P N E amp Battarbee R W 1996 Selective concentration and enumerationof tephra shards from lake sediment cores Holocene 6 243246
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Santacroce R 1987 Somma Vesuvius Quad Ric Sci 114 252
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Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 801
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Sweatman T R amp Long J V P 1969 Quantitative electron microprobe analysis of rock formingminerals J Petrol 7 332379
Turney C S M 1998 Extraction of rhyolitic ash from minerogenic lake sediments J Paleolim-nol 19 199206
Turney C S M amp Lowe J J 2001 Tephrochronology In Tracking environmental changes inlake sediments physical and chemical techniques (ed W M Last amp J P Smol) DordrechtKluwer Academic
Turney C S M Harkness D D amp Lowe J J 1997 The use of microtephra horizons tocorrelate Lateglacial lake sediments successions in Scotland J Quat Sci 12 525531
Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
van den Bogaard P amp Schmincke H 1985 A widespread isochronous Late Quaternary tephralayer in central and northern Europe Geol Soc Am Bull 96 15541571
van den Bogaard B Dordeg er W Sandgren P amp Schmincke H-U 1994 Correlating theHolocene records Icelandic tephra found in Schleswig-Holstein (northern Germany) Natur-wissenschaften 81 554556
Vernet G amp Raynal J-P 2001 Tephrostratigraphy of the Limagne revisited Implications forLateglacial and Holocene Prehistory In Tephras chronology archaeology (ed E Juvignparae ampJ-P Raynal) pp 111116 Dossiers de lrsquo ArchparaeoLogis no 1 France
Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
Vezzoli L 1991 Tephra layers in Bannock Basin (eastern Mediterranean) Mar Geol 1002134
von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
Walker M J C Bjorck S Lowe J J Cwynar L C Johnsen S Knudsen K-L WohlfarthB amp INTIMATE Group 1999 Isotopic events in the GRIP ice core a stratotype for the LatePleistocene Quat Sci Rev 18 11431150
Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
802 S M Davies and others
Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 785
in or close to the volcanic source areas in an attempt to establish the full sequenceof volcanic eruptions during the Late Quaternary (see for example Di Vito et al 1999) There are nine Italian tephras reported from marine and lake sequences thatdate from the period between 185 and 80 14C ka BP In all instances the recordsare of visible layers of tephra The ages of some of these are poorly established atpresent with conregicting data obtained from dinoterent sites The ages suggested intable 1 are those favoured in the most recent publications but these may requirere-assessment in the light of future research
The two oldest known tephras in the time-period of interest are the L9 and Green-ish Tephras both recorded as separate features within the annually laminated Lagodi Monticchio maar sequence The lowest of the two L9 is considered to be the cor-relative of the `basalrsquo plinian eruption of Vesuvius (Narcisi 1996) Age estimates ofa palaeosol that underlies the Vesuvius tephra sequence are ca 1617 14C ka BP forthis event (Delibrias et al 1979) L9 has a trachytic composition very similar to theGreenish Tephra (table 1) However L9 which is also a product of Vesuvius is foundstratigraphically below the Greenish Tephra in the Lago di Monticchio core TheGreenish Tephra is dated in the Monticchio sequence to 17 560 varve yr BP (Allenet al 1999) and has a calibrated radiocarbon age estimate of 17 830 sect 300 cal BP(Andronico et al 1995) Both tephras have a dominantly eastwards dispersal basedon the occurrences of visible layers (Santacroce 1987 Narcisi 1996) Both tephrasalso have a trachytic composition and as can be seen from table 1 the reportedgeochemical spectra are very close indeed with the standard deviations overlappingfor almost every major element This could present problems for tephrostratigra-phy where only one of the tephras is evident in a sediment sequence in particularbecause they are so close in age This is a good example of where an analysis oftrace and rare earth elements might be required to make a clear distinction betweentephras with very similar major oxide concentrations
The Y-1 Tephra also termed the Biancavilla Montalto Ignimbrite (Vezzoli 1991)is a product of Etna and has been identishy ed as a visible benmoritic tephra horizonthroughout the central Mediterranean (Paterne et al 1988) including central Italyand the Adriatic Sea (Vezzoli 1991 Narcisi 1993 Calanchi et al 1996) It has anestimated age of ca 140 14C ka BP The Unita dei Tefra Superiori tephra which hasbeen detected as far east as Lago di Monticchio in south-central Italy (Narcisi 1996)is also dated to ca 140 14C ka BP (Alessio et al 1976) but it is thought that thesource of this tephra lies in the Phlegrean Fields No geochemical data are availablefrom the presumed source region|the data reported in table 1 were obtained fromthe Lago di Monticchio record (Narcisi 1996)
The NYT which is equivalent to the C-2 tephra reported from various marinesequences has also been traced throughout central Italy and the Adriatic Sea (Pat-erne et al 1988 Calanchi et al 1996 Di Vito et al 1999) (shy gure 2) In the centralApennines region it formed the parent material for a soil that started to developat the beginning of the Holocene period (Frezzotti amp Narcisi 1996) Also originatingfrom the Campi Flegrei caldera it is dated to ca 120 14C ka BP (Di Vito et al 1999) Published geochemical data based on EDS indicate three dinoterent geochemicalpopulations varying from latite to phonotrachyte in composition (Orsi et al 1992Paterne et al 1988) (table 1) We report in x 4 of this paper on new data obtainedfrom the NYT by WDS and it is the mean of these new data that is included intable 1 Comparisons with the previously published EDS data are provided (table 1)
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786 S M Davies and others
The new data indicate clearly that the NYT originated from the Campanian volcaniccentre
In the interval between the dispersal of the NYT (ca 120 14C ka BP) and 95 14Cka BP there appear to have been as many as 34 eruptions in the Campi Flegrei caldera(Di Vito et al 1999) Of these only one appears to have been detected widely in theregion the Pomici Principali (also termed the Agnano Formation or C-1 tephra inmarine records (Paterne et al 1988) This was the product of the highest magnitudeeruption from this epoch and is dated to between 976 sect 300 and 1032 sect 50 14C kaBP (Delibrias et al 1979 Di Vito et al 1999) or to 122 varve ka BP based on theMonticchio varve chronology (Allen et al 1999) It is trachytic in composition andappears to have had a mainly eastwards dispersal
The Mercato Tephra dated to ca 80 14C ka BP and originally analysed usingEDS has a phonolitic composition and is believed to have been generated by Vesu-vius (Paterne et al 1988) New WDS data obtained from reference samples col-lected from an exposure to the west of Naples support these conclusions (table 1 andAppendix A) The silica content of the WDS analyses are ca 3 lower than thoseobtained using EDS (table 1) which may reregect the fact that the EDS data werenormalized
The only tephra listed in table 1 that is thought to have originated from the AeolianIslands is the Pollara pumice also referred to as the E2 tephra in marine sequences(Paterne et al 1986 1988) The limited geochemical data available so far suggest itto be the only Italian tephra listed in table 1 that is rhyolitic in composition Littlemore is known about this ash which has not been recorded extensively except thatits age is estimated to be ca 130 14C ka BP (Keller 1980)
5 Extending the known distributions of European tephras
Figure 2 summarizes schematically the known distributions of three of the tephrasreferred to in the preceding section the VA the LST and the NYT Following theintroduction of a laboratory method that enables the detection of micro-tephra parti-cles in mineral-rich sediment the VA has been traced to sites that are located muchfarther south (into The Netherlands) and east (as far as St Petersburg) than thedistribution limits based on occurrences of visible layers of the ash As a result con-tinental sequences over a much larger area in northern Europe can now be correlateddirectly with marine and ice-core records using the VA as a time-parallel marker
This suggests therefore that other prominent ash layers such as the LST andNYT should also be detectable over larger tracts of Europe than is presently thecase if suitable sites are examined for the presence of micro-tephra horizons To testthis assertion we examined lake sediment deposits of Last Termination age froma site in the northern Apennines in order to establish whether the NYT could bedetected in micro-tephra form The site selected Prato Spilla `Crsquo lies well to thenorth of the localities in central and southern Italy and in the Adriatic Sea fromwhich visible records of the NYT have been reported Prato Spilla `Crsquo lies at an alti-tude of ca 1350 m in the Appennino Parmense ca 60 km south of Parma and 15 kmeast of Pontremoli The site contains a continuous sediment sequence spanning theLast Termination and most of the Holocene Detailed pollen and coleopteran strati-graphical records which have been radiocarbon dated have been published for thissite (Lowe 1992 Ponel amp Lowe 1992 Lowe amp Watson 1993)
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European tephrochronological framework for Termination 1 787
Figure 6 Light microscope photograph of an NYT glass shard from Prato Spilla Crsquosequence assigned on geochemical grounds to the NYT
The methods adopted for sub-sampling of the Prato Spilla `Crsquo sequence for thequantishy cation of glass shard concentrations and for subsequent electron microprobeanalysis of selected glass shards followed those described elsewhere (Turney 1998)In summary contiguous samples of 1 cm stratigraphic interval were extracted fromthe sequence to establish presenceabsence of glass shards Each of the 1 cm3 blocksin which tephra particles was detected was then examined with more care andshard concentrations were quantishy ed for each sub-sample Micro-tephra particleswere detected in shy ve samples (shy gure 6) but were predominantly clustered around500 cm in the part of the sequence assigned on pollen-stratigraphic grounds to theLate Glacial Interstadial or the `Allerfrac12drsquo|indeed the part of the succession in whichthe NYT would be expected to occur Peak concentrations of micro-tephra particlesreach 225 shards cmiexcl3 and are conshy ned to a single 1 cm thick sample in the sequencewhich probably represents the time of maximum deposition of the ash
Electron microprobe measurements based on WDS were obtained from the surfacesof 21 separate glass shards extracted from the sample with peak shard concentrations(Appendix A) Since only EDS measurements were available for the NYT prior to thepresent study we also obtained WDS measurements from 17 shards extracted fromthe visible layer of NYT that is exposed on Procida Island which lies in the type-locality for the NYT close to the city of Naples (Appendix A) The results providenot only a more comprehensive geochemical dataset for the NYT than was previ-ously available but also a consistent basis for comparison with the Prato Spilla `Crsquodataset All of the WDS data reported here (Appendix A) were measured at the samelaboratory (Tephrochronology Analytical Unit University of Edinburgh) using thesame sample pretreatment and preparation protocol The WDS results for the NYTdinoter to a minor degree from the EDS results (table 1 and Appendix A) especiallywith respect to the amounts of silica aluminium and calcium measured The EDS
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788 S M Davies and others
4 8FeO ()
TiO
2 (
) Neapolitan Yellow Tuff(Procida)Neapolitan Yellow Tuff(Prato Spilla lsquoCrsquo)
0
1
2
3
40 50 60 70
MgO
(
)
SiO2 ()
K2O
(
)
40 50 60 70
0
04
08
4
8
12
SiO2 ()
(a)(b)
(c)
Figure 7 Bi-plots of SiO2 K2 O SiO2 MgO and FeOTiO2 for the WDS analyses obtainedfrom glass shards of the NYT from Procida (Naples) and Prato Spilla Crsquo Means and standarddeviations are shown
results show a higher degree of statistical scatter than the WDS measurements whichmay reregect the fact that the data were normalized combined with the inreguence ofvariation in water content between shards
There is a very close correspondence between the WDS data for the Prato Spilla `Crsquomicro-tephra shards and those obtained from the type-material near Naples (shy g-ure 7) The geochemical data strongly suggest therefore that the NYT is representedat the Prato Spilla `Crsquo site by a discrete layer of micro-tephra particles This conclu-sion is compatible with the pollen-stratigraphic data from the site and accords withage estimates for the NYT (ca 120 14C ka BP) obtained from other sites (Paterneet al 1990)
These results encourage us to believe that many if not all of the tephras listedin table 1 will be detectable over much larger tracts of Europe than is presently thecase if appropriate research is undertaken to detect layers of micro-tephra particlesin selected sites The authors are presently engaged in a major continent-wide pro-gramme of research in collaboration with a number of European research groupsdesigned to test this hypothesis The focus in this research is on those parts of Europewhere we expect to shy nd overlapping `apronsrsquo of tephra deposition originating fromthe Italian Eifel Massif Central and Icelandic provinces For example a number ofsites in parts of southern France northern Italy and perhaps western Switzerlandmay have received inreguxes of micro-tephra originating from the Italian and Eifelprovinces and perhaps also from the Massif Central Sites in parts of Germany Den-mark and southern Sweden for example may in turn have received tephra depositsfrom both of the Icelandic and Eifel provinces If this proves to be the case then thestage will be set for the construction of a tephrostratigraphical framework for Europewhich will enable Last Termination sequences to be correlated on a continent-widebasis using micro- and visible tephra layers as time-parallel stratigraphic markersFurthermore there is also the possibility that other tephras remain to be discovered
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European tephrochronological framework for Termination 1 789
those which either because of the magnitude or nature of some volcanic eruptionswere distributed over parts of Europe in micro-tephra form only
6 European tephrostratigraphy and the chronology of eventsduring the Last Termination and Early Holocene
One of the crucial issues in Late Quaternary palaeoenvironmental research thatremains to be resolved is the degree to which climatic events inferred from oceanicterrestrial and ice-core records were synchronous during the Last Termination andEarly Holocene If the ice-core records provide realistic estimates of the rates anddurations of climatic events during this period then comparisons between individ-ual records have to be enotected with at least a decadal precision The problem thispresents and the role that tephrostratigraphy can play in resolving some of thedimacr culties involved are put into perspective in shy gure 8
Figure 8 shows some of the data used to calibrate radiocarbon dates (the LakeSuigetsu and Cariaco Basin datasets) plotted against the GRIP ss08c ice-core recordof macr 18O variations The latter has been selected by the INTIMATE group as an arbi-trary and temporary standard for this period and used to deshy ne an event stratig-raphy scheme (shy gure 1) for the Last Termination (see Bjorck et al 1998 Walker etal 2001) As has been alluded to in earlier sections of this paper the uncertaintiesassociated with all of the dating methods currently employed preclude precise com-parisons of ice-core marine and terrestrial records Oceanic and terrestrial recordsmostly rely upon radiocarbon dating locally supplemented in a few cases by varvechronology Imprecisions in radiocarbon dates can arise through site-specishy c fac-tors (eg hard-water or mineral carbon errors in freshwater sequences and reservoirerrors in marine sequences) sample selection laboratory measurements of 14C activ-ity and other factors (Lowe amp Walker 2000) Further imprecision may be introducedby the calibration of radiocarbon dates since the uncertainties in the dataset usedto calibrate pre-Holocene radiocarbon dates INTCAL98 are far higher than forthe Holocene which is based on dendro-calibration (Stuiver et al 1998) There arealso uncertainties anotecting varve chronologies while the ss08c ice-core chronologyfor the Last Termination dinoters signishy cantly from the GISP2 record and indeedfrom other models of the GRIP record (Lowe et al 2001) Published comparisonsbetween ice-core marine and terrestrial records for the Last Termination seldom takeinto account the true magnitude of the dating uncertainties involved and frequentlyemploy circular reasoning
Figure 8 shows the positions on the radiocarbon time-scale of 20 of the tephrasdiscussed earlier in this paper these being the ones for which reasonably conshy dentradiocarbon age estimates can be made (though these will be subject to revised esti-mates in the future) A high number of these occur in the period 14080 14C kaBP but we conshy dently anticipate the discovery in the future of additional tephras(perhaps in micro-tephra form only) which will date to the period 185140 14C kaBP Tephras detected in the GRIP ice core over the same time-interval are plottedon the calendar time-scale in shy gure 8 By providing key `time-linesrsquo between recordstephrostratigraphy can help to resolve some of the dating uncertainties referredto earlier by for example enabling direct comparisons of discrepant age estimatesobtained using dinoterent methods (cf Litt et al 2001) It can also provide estimatesof the magnitudes of the reservoir errors that anotected various marine sectors at dif-
Phil Trans R Soc Lond A (2002)
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790 S M Davies and others
-44
-40
-36
-32
cale
ndar
yea
rs B
P
8000
9000
10 0
00
11 0
00
12 0
00
13 0
00
14 0
00
15 0
00
16 0
00
17 0
00
18 0
00
14C age (BP)
VA
SA
Un
Un
Un
Un
Un
BF
Hol
ocen
eG
S-1
GI-
1aG
I-1b
GI-
1cG
I-1d
GI-
1eG
S-2
aG
S-2
bG
S-
2c
Bor
robo
l
La
Nug
egravere
Laa
cher
See
God
ivel
le 5
amp I
-TH
OL
-2
Puy
de D
ocircme
I-T
HO
L-1
Saks
unar
vatn
Houmlg
stor
psm
osse
nU
lmen
er M
aar
amp L
3574
radiocarbon dated European tephra horizons
Cho
pine
Kili
an V
asse
tM
erca
to
God
ivel
le 4
Pom
ici P
rinc
ipal
i amp V
edde
Polla
ra p
umic
eK
OL
-GS-
2 amp
GS
-2B
AS-
12
3
GS
-2B
AS-
4 U
nita
dei
Tef
raSu
peri
ori amp
laye
r Y
-1
Gre
enis
h
L9
20 0
0018
000
16 0
0014
000
12 0
0010
000
-44
-40
-36
-32
800
600
400
200 0
GISP2 volcanicsulphate conc (ppb)
1000
Nea
polit
an Y
ello
w T
uff
GISP2 18O (permil) dGRIP 18O (permil) d
Figure 8 For description see opposite
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European tephrochronological framework for Termination 1 791
ferent times through a comparison of radiocarbon dates obtained from marine andterrestrial horizons in which the same tephra has been detected (see for exampleAustin et al 1995 Bondevik et al 2001 Haregidason et al 2000) Tephrostratigraphymay provide an independent test of suggestions that some of the climatic changesduring the Last Termination were time-transgressive as illustrated for some appar-ently contrasting climatic trends in Iceland Britain and NW Russia (Lowe 2001) Ofparticular importance as far as establishing `leadsrsquo and `lagsrsquo in climatic changes isconcerned are the tephra records from the Greenland ice cores The discovery of theVedde and Saksunarvatn ashes in the GRIP record (Gronvold et al 1995) alreadyprovides a basis for making direct comparisons between marine terrestrial and ice-core records It is a matter of some urgency that the incidence of tephra depositsin the Greenland ice cores be more fully explored in the hope that this will lead tothe recognition of additional time-parallel links between the ice-core records on theone hand and oceanic and terrestrial records on the other An investigation of thenew NordGRIP record for this purpose is currently in progress (S M Davies 2002unpublished data)
Finally a fuller and more reshy ned tephrostratigraphical scheme for Europe will alsohave other applications It will provide an important database for those investigatingthe timing and frequency of volcanic eruptions in Europe during the past 20 000 yror so as well as of the geochemical evolution of the dinoterent volcanic centres overthat period A fuller record of the distribution of micro-tephras may also provideinformation on atmospheric circulation patterns during the dispersal and depositionperiods as well as on the nature and altitude of the eruption columns which mayin turn provide inferences about magma viscosity
This paper is a contribution to the INTIMATE project of the INQUA Palaeoclimate Com-mission and the work is supported by a Leverhulme Trust Research project (grant allocationnumber F07537C) entitled Testing hypotheses of rapid climate change using tephrochronol-ogyrsquo SMDrsquo s contribution was completed during possession of a NERC PhD studentship(GT 0499ES162) We are extremely grateful to Dr Peter G Hill for his assistance withthe EPMA analyses at the Tephrochronology Analytical Unit University of Edinburgh We alsothank Dr G Mastrolorenzo (Vesuvius Observatory) and Miss G Swindle for assistance duringthe macreld investigations in Naples Thanks are also expressed to two anonymous reviewers forcomments on an earlier draft
Appendix A
Table 2 shows the major oxide concentrations of NYT glass shards from Procidaand Prato Spilla `Crsquo and of the Mercato Tephra from the Naples area (see x 4 forsite context) All oxides are shown as weight and total iron is expressed as FeO
Figure 8 Radiocarbon calibration curve for Termination 1 and the Early Holocene compared with theGRIP macr 18 O event stratigraphy the GRIP ss08c and GISP2 macr 18 O records (wwwngdcnoaagov) andknown tephra horizons from this period The shaded areas represent the cooler climatic episodes andare labelled with the Greenland stratotype terminology (Bjorck et al 1998) Where radiocarbon agesare reported in table 1 as a range the mean is given here Abbreviations for GRIP horizons are asfollows Un unknown (approximate positions are given (S Johnsen 2001 personal communication))SA Saksunarvatn Ash VA Vedde Ash BF Black Feather Sulphate concentrations from the GISP2record are also shown (Zielinski et al 1996) Open circles denote radiocarbon calibration data fromLake Suigetsu (Kitagawa amp van der Plicht 2000) Filled circles denote radiocarbon calibration data fromCariaco Basin assuming a marine reservoir age of 420 14 C yr (Hughen et al 1998)
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792 S M Davies and others
Tab
le2
Majo
roxi
de
con
cen
trati
on
sof
NY
Tgl
ass
shard
sfr
om
Pro
cida
an
dP
rato
Spil
laC
rsquoan
dof
the
Mer
cato
Tep
hra
from
the
Naple
sare
a(s
eex4
for
site
con
text
)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
roci
da)
1584
204
0177
634
201
106
828
635
197
5969
1W
DS
2598
603
9178
027
101
204
924
244
583
4965
8W
DS
3586
604
5173
631
100
805
924
342
183
0951
9W
DS
4583
903
9177
933
000
906
924
540
486
9958
3W
DS
5605
106
8179
126
901
204
923
243
086
1976
4W
DS
6591
704
5177
332
801
006
425
740
887
8968
0W
DS
7581
804
1178
031
501
107
125
640
086
9956
1W
DS
8589
504
2179
533
701
506
926
740
987
5970
4W
DS
9592
003
9178
135
101
007
026
443
585
7972
7W
DS
10
591
404
2174
631
601
105
723
442
482
6957
0W
DS
11
593
403
6177
131
301
506
726
439
188
5967
6W
DS
12
588
103
8176
128
100
505
525
141
583
4952
1W
DS
13
577
003
8176
533
500
807
228
140
384
8952
0W
DS
14
586
004
7179
735
300
706
827
842
984
6968
5W
DS
15
588
104
2180
629
400
505
924
937
993
0964
5W
DS
16
579
603
9178
536
501
308
228
836
087
1959
9W
DS
17
580
103
9177
631
500
907
327
039
488
9956
6W
DS
mea
n588
104
2177
631
901
006
525
940
686
9962
8
sd
(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(07
8)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 793
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
rato
Spil
laC
rsquo)
1552
105
4177
247
401
914
38
735
578
9951
1W
DS
2557
305
7179
845
701
512
640
136
581
5960
6W
DS
3595
004
4173
724
302
003
117
652
877
8950
7W
DS
4575
704
2179
433
001
406
627
043
083
6953
7W
DS
5599
904
0178
826
401
304
421
841
688
4966
5W
DS
6591
103
8177
826
601
105
022
443
888
8960
2W
DS
7565
304
5180
939
501
410
532
535
791
8962
1W
DS
8597
606
9180
826
501
604
821
546
684
6970
7W
DS
9571
805
6179
939
801
109
932
240
883
6964
7W
DS
10
588
603
7176
527
601
104
721
042
487
7953
3W
DS
11
559
404
9180
544
501
812
339
435
878
6957
2W
DS
12
594
704
0181
328
301
705
522
144
785
6967
9W
DS
13
611
103
7187
016
900
802
419
938
195
9975
8W
DS
14
599
204
4181
128
601
404
620
844
986
6971
6W
DS
15
601
204
4177
328
302
004
722
446
385
5972
1W
DS
16
595
104
5176
428
801
504
722
744
884
3962
8W
DS
17
603
704
1177
825
101
503
520
348
181
2965
3W
DS
18
558
704
5179
647
401
813
139
836
879
0960
7W
DS
19
589
602
8178
830
901
606
622
436
091
8960
5W
DS
20
553
606
3178
647
401
913
840
136
978
0956
6W
DS
21
579
004
0175
739
000
708
328
338
286
7959
9W
DS
mea
n582
804
6179
033
401
507
427
341
484
8962
1
sd
(1
87)
(01
0)
(02
7)
(09
2)
(00
4)
(03
9)
(08
0)
(04
9)
(05
0)
(07
0)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
794 S M Davies and others
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)
1575
202
7194
219
701
101
016
374
766
9951
8W
DS
2575
802
9194
523
902
201
520
273
564
5959
0W
DS
3574
301
4205
219
101
100
416
481
266
1965
2W
DS
4575
500
7206
018
002
000
415
181
669
3968
6W
DS
5580
000
9208
018
601
300
515
883
367
1975
5W
DS
6571
001
0206
016
101
600
515
078
967
1957
2W
DS
7577
501
1201
117
101
500
620
675
655
4950
5W
DS
8573
700
9212
717
101
900
815
187
564
2973
9W
DS
9580
301
3208
715
801
400
824
81
754
1968
1W
DS
10
574
400
6211
18
402
00
516
480
567
8971
6W
DS
11
577
200
7214
212
501
200
829
879
247
962
6W
DS
12
572
200
9211
217
301
501
15
980
465
9966
3W
DS
13
571
800
7210
417
402
201
16
184
467
2971
2W
DS
14
567
300
9208
916
901
400
917
383
262
5959
3W
DS
15
568
600
8205
918
202
101
414
682
666
6960
8W
DS
16
572
501
1211
318
202
01
215
884
364
5970
9W
DS
17
572
901
2212
916
502
101
215
883
667
2973
4W
DS
18
573
01
4211
716
301
801
416
83
365
5970
4W
DS
19
569
201
1207
418
602
101
414
982
964
961
6W
DS
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
3)
(04
2)
(01
3)
(00
1)
(00
2)
(01
)(0
39)
(01
1)
(02
5)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
References
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Hughen K A Overpeck J T Peterson L C amp Trumbore S 1996 Rapid climate changes inthe tropical Atlantic region during the last deglaciation Nature 380 5153
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Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
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Larsen G 2000 Holocene volcanism in Iceland and tephrochronology as a tool in volcanologyIn Iceland 2000 modern processes and past environments Keele University UK
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European tephrochronological framework for Termination 1 799
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Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
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Rose N L Golding P N E amp Battarbee R W 1996 Selective concentration and enumerationof tephra shards from lake sediment cores Holocene 6 243246
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Santacroce R 1987 Somma Vesuvius Quad Ric Sci 114 252
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Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 801
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Sweatman T R amp Long J V P 1969 Quantitative electron microprobe analysis of rock formingminerals J Petrol 7 332379
Turney C S M 1998 Extraction of rhyolitic ash from minerogenic lake sediments J Paleolim-nol 19 199206
Turney C S M amp Lowe J J 2001 Tephrochronology In Tracking environmental changes inlake sediments physical and chemical techniques (ed W M Last amp J P Smol) DordrechtKluwer Academic
Turney C S M Harkness D D amp Lowe J J 1997 The use of microtephra horizons tocorrelate Lateglacial lake sediments successions in Scotland J Quat Sci 12 525531
Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
van den Bogaard P amp Schmincke H 1985 A widespread isochronous Late Quaternary tephralayer in central and northern Europe Geol Soc Am Bull 96 15541571
van den Bogaard B Dordeg er W Sandgren P amp Schmincke H-U 1994 Correlating theHolocene records Icelandic tephra found in Schleswig-Holstein (northern Germany) Natur-wissenschaften 81 554556
Vernet G amp Raynal J-P 2001 Tephrostratigraphy of the Limagne revisited Implications forLateglacial and Holocene Prehistory In Tephras chronology archaeology (ed E Juvignparae ampJ-P Raynal) pp 111116 Dossiers de lrsquo ArchparaeoLogis no 1 France
Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
Vezzoli L 1991 Tephra layers in Bannock Basin (eastern Mediterranean) Mar Geol 1002134
von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
Walker M J C Bjorck S Lowe J J Cwynar L C Johnsen S Knudsen K-L WohlfarthB amp INTIMATE Group 1999 Isotopic events in the GRIP ice core a stratotype for the LatePleistocene Quat Sci Rev 18 11431150
Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
802 S M Davies and others
Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
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786 S M Davies and others
The new data indicate clearly that the NYT originated from the Campanian volcaniccentre
In the interval between the dispersal of the NYT (ca 120 14C ka BP) and 95 14Cka BP there appear to have been as many as 34 eruptions in the Campi Flegrei caldera(Di Vito et al 1999) Of these only one appears to have been detected widely in theregion the Pomici Principali (also termed the Agnano Formation or C-1 tephra inmarine records (Paterne et al 1988) This was the product of the highest magnitudeeruption from this epoch and is dated to between 976 sect 300 and 1032 sect 50 14C kaBP (Delibrias et al 1979 Di Vito et al 1999) or to 122 varve ka BP based on theMonticchio varve chronology (Allen et al 1999) It is trachytic in composition andappears to have had a mainly eastwards dispersal
The Mercato Tephra dated to ca 80 14C ka BP and originally analysed usingEDS has a phonolitic composition and is believed to have been generated by Vesu-vius (Paterne et al 1988) New WDS data obtained from reference samples col-lected from an exposure to the west of Naples support these conclusions (table 1 andAppendix A) The silica content of the WDS analyses are ca 3 lower than thoseobtained using EDS (table 1) which may reregect the fact that the EDS data werenormalized
The only tephra listed in table 1 that is thought to have originated from the AeolianIslands is the Pollara pumice also referred to as the E2 tephra in marine sequences(Paterne et al 1986 1988) The limited geochemical data available so far suggest itto be the only Italian tephra listed in table 1 that is rhyolitic in composition Littlemore is known about this ash which has not been recorded extensively except thatits age is estimated to be ca 130 14C ka BP (Keller 1980)
5 Extending the known distributions of European tephras
Figure 2 summarizes schematically the known distributions of three of the tephrasreferred to in the preceding section the VA the LST and the NYT Following theintroduction of a laboratory method that enables the detection of micro-tephra parti-cles in mineral-rich sediment the VA has been traced to sites that are located muchfarther south (into The Netherlands) and east (as far as St Petersburg) than thedistribution limits based on occurrences of visible layers of the ash As a result con-tinental sequences over a much larger area in northern Europe can now be correlateddirectly with marine and ice-core records using the VA as a time-parallel marker
This suggests therefore that other prominent ash layers such as the LST andNYT should also be detectable over larger tracts of Europe than is presently thecase if suitable sites are examined for the presence of micro-tephra horizons To testthis assertion we examined lake sediment deposits of Last Termination age froma site in the northern Apennines in order to establish whether the NYT could bedetected in micro-tephra form The site selected Prato Spilla `Crsquo lies well to thenorth of the localities in central and southern Italy and in the Adriatic Sea fromwhich visible records of the NYT have been reported Prato Spilla `Crsquo lies at an alti-tude of ca 1350 m in the Appennino Parmense ca 60 km south of Parma and 15 kmeast of Pontremoli The site contains a continuous sediment sequence spanning theLast Termination and most of the Holocene Detailed pollen and coleopteran strati-graphical records which have been radiocarbon dated have been published for thissite (Lowe 1992 Ponel amp Lowe 1992 Lowe amp Watson 1993)
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European tephrochronological framework for Termination 1 787
Figure 6 Light microscope photograph of an NYT glass shard from Prato Spilla Crsquosequence assigned on geochemical grounds to the NYT
The methods adopted for sub-sampling of the Prato Spilla `Crsquo sequence for thequantishy cation of glass shard concentrations and for subsequent electron microprobeanalysis of selected glass shards followed those described elsewhere (Turney 1998)In summary contiguous samples of 1 cm stratigraphic interval were extracted fromthe sequence to establish presenceabsence of glass shards Each of the 1 cm3 blocksin which tephra particles was detected was then examined with more care andshard concentrations were quantishy ed for each sub-sample Micro-tephra particleswere detected in shy ve samples (shy gure 6) but were predominantly clustered around500 cm in the part of the sequence assigned on pollen-stratigraphic grounds to theLate Glacial Interstadial or the `Allerfrac12drsquo|indeed the part of the succession in whichthe NYT would be expected to occur Peak concentrations of micro-tephra particlesreach 225 shards cmiexcl3 and are conshy ned to a single 1 cm thick sample in the sequencewhich probably represents the time of maximum deposition of the ash
Electron microprobe measurements based on WDS were obtained from the surfacesof 21 separate glass shards extracted from the sample with peak shard concentrations(Appendix A) Since only EDS measurements were available for the NYT prior to thepresent study we also obtained WDS measurements from 17 shards extracted fromthe visible layer of NYT that is exposed on Procida Island which lies in the type-locality for the NYT close to the city of Naples (Appendix A) The results providenot only a more comprehensive geochemical dataset for the NYT than was previ-ously available but also a consistent basis for comparison with the Prato Spilla `Crsquodataset All of the WDS data reported here (Appendix A) were measured at the samelaboratory (Tephrochronology Analytical Unit University of Edinburgh) using thesame sample pretreatment and preparation protocol The WDS results for the NYTdinoter to a minor degree from the EDS results (table 1 and Appendix A) especiallywith respect to the amounts of silica aluminium and calcium measured The EDS
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788 S M Davies and others
4 8FeO ()
TiO
2 (
) Neapolitan Yellow Tuff(Procida)Neapolitan Yellow Tuff(Prato Spilla lsquoCrsquo)
0
1
2
3
40 50 60 70
MgO
(
)
SiO2 ()
K2O
(
)
40 50 60 70
0
04
08
4
8
12
SiO2 ()
(a)(b)
(c)
Figure 7 Bi-plots of SiO2 K2 O SiO2 MgO and FeOTiO2 for the WDS analyses obtainedfrom glass shards of the NYT from Procida (Naples) and Prato Spilla Crsquo Means and standarddeviations are shown
results show a higher degree of statistical scatter than the WDS measurements whichmay reregect the fact that the data were normalized combined with the inreguence ofvariation in water content between shards
There is a very close correspondence between the WDS data for the Prato Spilla `Crsquomicro-tephra shards and those obtained from the type-material near Naples (shy g-ure 7) The geochemical data strongly suggest therefore that the NYT is representedat the Prato Spilla `Crsquo site by a discrete layer of micro-tephra particles This conclu-sion is compatible with the pollen-stratigraphic data from the site and accords withage estimates for the NYT (ca 120 14C ka BP) obtained from other sites (Paterneet al 1990)
These results encourage us to believe that many if not all of the tephras listedin table 1 will be detectable over much larger tracts of Europe than is presently thecase if appropriate research is undertaken to detect layers of micro-tephra particlesin selected sites The authors are presently engaged in a major continent-wide pro-gramme of research in collaboration with a number of European research groupsdesigned to test this hypothesis The focus in this research is on those parts of Europewhere we expect to shy nd overlapping `apronsrsquo of tephra deposition originating fromthe Italian Eifel Massif Central and Icelandic provinces For example a number ofsites in parts of southern France northern Italy and perhaps western Switzerlandmay have received inreguxes of micro-tephra originating from the Italian and Eifelprovinces and perhaps also from the Massif Central Sites in parts of Germany Den-mark and southern Sweden for example may in turn have received tephra depositsfrom both of the Icelandic and Eifel provinces If this proves to be the case then thestage will be set for the construction of a tephrostratigraphical framework for Europewhich will enable Last Termination sequences to be correlated on a continent-widebasis using micro- and visible tephra layers as time-parallel stratigraphic markersFurthermore there is also the possibility that other tephras remain to be discovered
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European tephrochronological framework for Termination 1 789
those which either because of the magnitude or nature of some volcanic eruptionswere distributed over parts of Europe in micro-tephra form only
6 European tephrostratigraphy and the chronology of eventsduring the Last Termination and Early Holocene
One of the crucial issues in Late Quaternary palaeoenvironmental research thatremains to be resolved is the degree to which climatic events inferred from oceanicterrestrial and ice-core records were synchronous during the Last Termination andEarly Holocene If the ice-core records provide realistic estimates of the rates anddurations of climatic events during this period then comparisons between individ-ual records have to be enotected with at least a decadal precision The problem thispresents and the role that tephrostratigraphy can play in resolving some of thedimacr culties involved are put into perspective in shy gure 8
Figure 8 shows some of the data used to calibrate radiocarbon dates (the LakeSuigetsu and Cariaco Basin datasets) plotted against the GRIP ss08c ice-core recordof macr 18O variations The latter has been selected by the INTIMATE group as an arbi-trary and temporary standard for this period and used to deshy ne an event stratig-raphy scheme (shy gure 1) for the Last Termination (see Bjorck et al 1998 Walker etal 2001) As has been alluded to in earlier sections of this paper the uncertaintiesassociated with all of the dating methods currently employed preclude precise com-parisons of ice-core marine and terrestrial records Oceanic and terrestrial recordsmostly rely upon radiocarbon dating locally supplemented in a few cases by varvechronology Imprecisions in radiocarbon dates can arise through site-specishy c fac-tors (eg hard-water or mineral carbon errors in freshwater sequences and reservoirerrors in marine sequences) sample selection laboratory measurements of 14C activ-ity and other factors (Lowe amp Walker 2000) Further imprecision may be introducedby the calibration of radiocarbon dates since the uncertainties in the dataset usedto calibrate pre-Holocene radiocarbon dates INTCAL98 are far higher than forthe Holocene which is based on dendro-calibration (Stuiver et al 1998) There arealso uncertainties anotecting varve chronologies while the ss08c ice-core chronologyfor the Last Termination dinoters signishy cantly from the GISP2 record and indeedfrom other models of the GRIP record (Lowe et al 2001) Published comparisonsbetween ice-core marine and terrestrial records for the Last Termination seldom takeinto account the true magnitude of the dating uncertainties involved and frequentlyemploy circular reasoning
Figure 8 shows the positions on the radiocarbon time-scale of 20 of the tephrasdiscussed earlier in this paper these being the ones for which reasonably conshy dentradiocarbon age estimates can be made (though these will be subject to revised esti-mates in the future) A high number of these occur in the period 14080 14C kaBP but we conshy dently anticipate the discovery in the future of additional tephras(perhaps in micro-tephra form only) which will date to the period 185140 14C kaBP Tephras detected in the GRIP ice core over the same time-interval are plottedon the calendar time-scale in shy gure 8 By providing key `time-linesrsquo between recordstephrostratigraphy can help to resolve some of the dating uncertainties referredto earlier by for example enabling direct comparisons of discrepant age estimatesobtained using dinoterent methods (cf Litt et al 2001) It can also provide estimatesof the magnitudes of the reservoir errors that anotected various marine sectors at dif-
Phil Trans R Soc Lond A (2002)
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790 S M Davies and others
-44
-40
-36
-32
cale
ndar
yea
rs B
P
8000
9000
10 0
00
11 0
00
12 0
00
13 0
00
14 0
00
15 0
00
16 0
00
17 0
00
18 0
00
14C age (BP)
VA
SA
Un
Un
Un
Un
Un
BF
Hol
ocen
eG
S-1
GI-
1aG
I-1b
GI-
1cG
I-1d
GI-
1eG
S-2
aG
S-2
bG
S-
2c
Bor
robo
l
La
Nug
egravere
Laa
cher
See
God
ivel
le 5
amp I
-TH
OL
-2
Puy
de D
ocircme
I-T
HO
L-1
Saks
unar
vatn
Houmlg
stor
psm
osse
nU
lmen
er M
aar
amp L
3574
radiocarbon dated European tephra horizons
Cho
pine
Kili
an V
asse
tM
erca
to
God
ivel
le 4
Pom
ici P
rinc
ipal
i amp V
edde
Polla
ra p
umic
eK
OL
-GS-
2 amp
GS
-2B
AS-
12
3
GS
-2B
AS-
4 U
nita
dei
Tef
raSu
peri
ori amp
laye
r Y
-1
Gre
enis
h
L9
20 0
0018
000
16 0
0014
000
12 0
0010
000
-44
-40
-36
-32
800
600
400
200 0
GISP2 volcanicsulphate conc (ppb)
1000
Nea
polit
an Y
ello
w T
uff
GISP2 18O (permil) dGRIP 18O (permil) d
Figure 8 For description see opposite
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European tephrochronological framework for Termination 1 791
ferent times through a comparison of radiocarbon dates obtained from marine andterrestrial horizons in which the same tephra has been detected (see for exampleAustin et al 1995 Bondevik et al 2001 Haregidason et al 2000) Tephrostratigraphymay provide an independent test of suggestions that some of the climatic changesduring the Last Termination were time-transgressive as illustrated for some appar-ently contrasting climatic trends in Iceland Britain and NW Russia (Lowe 2001) Ofparticular importance as far as establishing `leadsrsquo and `lagsrsquo in climatic changes isconcerned are the tephra records from the Greenland ice cores The discovery of theVedde and Saksunarvatn ashes in the GRIP record (Gronvold et al 1995) alreadyprovides a basis for making direct comparisons between marine terrestrial and ice-core records It is a matter of some urgency that the incidence of tephra depositsin the Greenland ice cores be more fully explored in the hope that this will lead tothe recognition of additional time-parallel links between the ice-core records on theone hand and oceanic and terrestrial records on the other An investigation of thenew NordGRIP record for this purpose is currently in progress (S M Davies 2002unpublished data)
Finally a fuller and more reshy ned tephrostratigraphical scheme for Europe will alsohave other applications It will provide an important database for those investigatingthe timing and frequency of volcanic eruptions in Europe during the past 20 000 yror so as well as of the geochemical evolution of the dinoterent volcanic centres overthat period A fuller record of the distribution of micro-tephras may also provideinformation on atmospheric circulation patterns during the dispersal and depositionperiods as well as on the nature and altitude of the eruption columns which mayin turn provide inferences about magma viscosity
This paper is a contribution to the INTIMATE project of the INQUA Palaeoclimate Com-mission and the work is supported by a Leverhulme Trust Research project (grant allocationnumber F07537C) entitled Testing hypotheses of rapid climate change using tephrochronol-ogyrsquo SMDrsquo s contribution was completed during possession of a NERC PhD studentship(GT 0499ES162) We are extremely grateful to Dr Peter G Hill for his assistance withthe EPMA analyses at the Tephrochronology Analytical Unit University of Edinburgh We alsothank Dr G Mastrolorenzo (Vesuvius Observatory) and Miss G Swindle for assistance duringthe macreld investigations in Naples Thanks are also expressed to two anonymous reviewers forcomments on an earlier draft
Appendix A
Table 2 shows the major oxide concentrations of NYT glass shards from Procidaand Prato Spilla `Crsquo and of the Mercato Tephra from the Naples area (see x 4 forsite context) All oxides are shown as weight and total iron is expressed as FeO
Figure 8 Radiocarbon calibration curve for Termination 1 and the Early Holocene compared with theGRIP macr 18 O event stratigraphy the GRIP ss08c and GISP2 macr 18 O records (wwwngdcnoaagov) andknown tephra horizons from this period The shaded areas represent the cooler climatic episodes andare labelled with the Greenland stratotype terminology (Bjorck et al 1998) Where radiocarbon agesare reported in table 1 as a range the mean is given here Abbreviations for GRIP horizons are asfollows Un unknown (approximate positions are given (S Johnsen 2001 personal communication))SA Saksunarvatn Ash VA Vedde Ash BF Black Feather Sulphate concentrations from the GISP2record are also shown (Zielinski et al 1996) Open circles denote radiocarbon calibration data fromLake Suigetsu (Kitagawa amp van der Plicht 2000) Filled circles denote radiocarbon calibration data fromCariaco Basin assuming a marine reservoir age of 420 14 C yr (Hughen et al 1998)
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792 S M Davies and others
Tab
le2
Majo
roxi
de
con
cen
trati
on
sof
NY
Tgl
ass
shard
sfr
om
Pro
cida
an
dP
rato
Spil
laC
rsquoan
dof
the
Mer
cato
Tep
hra
from
the
Naple
sare
a(s
eex4
for
site
con
text
)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
roci
da)
1584
204
0177
634
201
106
828
635
197
5969
1W
DS
2598
603
9178
027
101
204
924
244
583
4965
8W
DS
3586
604
5173
631
100
805
924
342
183
0951
9W
DS
4583
903
9177
933
000
906
924
540
486
9958
3W
DS
5605
106
8179
126
901
204
923
243
086
1976
4W
DS
6591
704
5177
332
801
006
425
740
887
8968
0W
DS
7581
804
1178
031
501
107
125
640
086
9956
1W
DS
8589
504
2179
533
701
506
926
740
987
5970
4W
DS
9592
003
9178
135
101
007
026
443
585
7972
7W
DS
10
591
404
2174
631
601
105
723
442
482
6957
0W
DS
11
593
403
6177
131
301
506
726
439
188
5967
6W
DS
12
588
103
8176
128
100
505
525
141
583
4952
1W
DS
13
577
003
8176
533
500
807
228
140
384
8952
0W
DS
14
586
004
7179
735
300
706
827
842
984
6968
5W
DS
15
588
104
2180
629
400
505
924
937
993
0964
5W
DS
16
579
603
9178
536
501
308
228
836
087
1959
9W
DS
17
580
103
9177
631
500
907
327
039
488
9956
6W
DS
mea
n588
104
2177
631
901
006
525
940
686
9962
8
sd
(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(07
8)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 793
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
rato
Spil
laC
rsquo)
1552
105
4177
247
401
914
38
735
578
9951
1W
DS
2557
305
7179
845
701
512
640
136
581
5960
6W
DS
3595
004
4173
724
302
003
117
652
877
8950
7W
DS
4575
704
2179
433
001
406
627
043
083
6953
7W
DS
5599
904
0178
826
401
304
421
841
688
4966
5W
DS
6591
103
8177
826
601
105
022
443
888
8960
2W
DS
7565
304
5180
939
501
410
532
535
791
8962
1W
DS
8597
606
9180
826
501
604
821
546
684
6970
7W
DS
9571
805
6179
939
801
109
932
240
883
6964
7W
DS
10
588
603
7176
527
601
104
721
042
487
7953
3W
DS
11
559
404
9180
544
501
812
339
435
878
6957
2W
DS
12
594
704
0181
328
301
705
522
144
785
6967
9W
DS
13
611
103
7187
016
900
802
419
938
195
9975
8W
DS
14
599
204
4181
128
601
404
620
844
986
6971
6W
DS
15
601
204
4177
328
302
004
722
446
385
5972
1W
DS
16
595
104
5176
428
801
504
722
744
884
3962
8W
DS
17
603
704
1177
825
101
503
520
348
181
2965
3W
DS
18
558
704
5179
647
401
813
139
836
879
0960
7W
DS
19
589
602
8178
830
901
606
622
436
091
8960
5W
DS
20
553
606
3178
647
401
913
840
136
978
0956
6W
DS
21
579
004
0175
739
000
708
328
338
286
7959
9W
DS
mea
n582
804
6179
033
401
507
427
341
484
8962
1
sd
(1
87)
(01
0)
(02
7)
(09
2)
(00
4)
(03
9)
(08
0)
(04
9)
(05
0)
(07
0)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
794 S M Davies and others
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)
1575
202
7194
219
701
101
016
374
766
9951
8W
DS
2575
802
9194
523
902
201
520
273
564
5959
0W
DS
3574
301
4205
219
101
100
416
481
266
1965
2W
DS
4575
500
7206
018
002
000
415
181
669
3968
6W
DS
5580
000
9208
018
601
300
515
883
367
1975
5W
DS
6571
001
0206
016
101
600
515
078
967
1957
2W
DS
7577
501
1201
117
101
500
620
675
655
4950
5W
DS
8573
700
9212
717
101
900
815
187
564
2973
9W
DS
9580
301
3208
715
801
400
824
81
754
1968
1W
DS
10
574
400
6211
18
402
00
516
480
567
8971
6W
DS
11
577
200
7214
212
501
200
829
879
247
962
6W
DS
12
572
200
9211
217
301
501
15
980
465
9966
3W
DS
13
571
800
7210
417
402
201
16
184
467
2971
2W
DS
14
567
300
9208
916
901
400
917
383
262
5959
3W
DS
15
568
600
8205
918
202
101
414
682
666
6960
8W
DS
16
572
501
1211
318
202
01
215
884
364
5970
9W
DS
17
572
901
2212
916
502
101
215
883
667
2973
4W
DS
18
573
01
4211
716
301
801
416
83
365
5970
4W
DS
19
569
201
1207
418
602
101
414
982
964
961
6W
DS
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
3)
(04
2)
(01
3)
(00
1)
(00
2)
(01
)(0
39)
(01
1)
(02
5)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
References
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802 S M Davies and others
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Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 787
Figure 6 Light microscope photograph of an NYT glass shard from Prato Spilla Crsquosequence assigned on geochemical grounds to the NYT
The methods adopted for sub-sampling of the Prato Spilla `Crsquo sequence for thequantishy cation of glass shard concentrations and for subsequent electron microprobeanalysis of selected glass shards followed those described elsewhere (Turney 1998)In summary contiguous samples of 1 cm stratigraphic interval were extracted fromthe sequence to establish presenceabsence of glass shards Each of the 1 cm3 blocksin which tephra particles was detected was then examined with more care andshard concentrations were quantishy ed for each sub-sample Micro-tephra particleswere detected in shy ve samples (shy gure 6) but were predominantly clustered around500 cm in the part of the sequence assigned on pollen-stratigraphic grounds to theLate Glacial Interstadial or the `Allerfrac12drsquo|indeed the part of the succession in whichthe NYT would be expected to occur Peak concentrations of micro-tephra particlesreach 225 shards cmiexcl3 and are conshy ned to a single 1 cm thick sample in the sequencewhich probably represents the time of maximum deposition of the ash
Electron microprobe measurements based on WDS were obtained from the surfacesof 21 separate glass shards extracted from the sample with peak shard concentrations(Appendix A) Since only EDS measurements were available for the NYT prior to thepresent study we also obtained WDS measurements from 17 shards extracted fromthe visible layer of NYT that is exposed on Procida Island which lies in the type-locality for the NYT close to the city of Naples (Appendix A) The results providenot only a more comprehensive geochemical dataset for the NYT than was previ-ously available but also a consistent basis for comparison with the Prato Spilla `Crsquodataset All of the WDS data reported here (Appendix A) were measured at the samelaboratory (Tephrochronology Analytical Unit University of Edinburgh) using thesame sample pretreatment and preparation protocol The WDS results for the NYTdinoter to a minor degree from the EDS results (table 1 and Appendix A) especiallywith respect to the amounts of silica aluminium and calcium measured The EDS
Phil Trans R Soc Lond A (2002)
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788 S M Davies and others
4 8FeO ()
TiO
2 (
) Neapolitan Yellow Tuff(Procida)Neapolitan Yellow Tuff(Prato Spilla lsquoCrsquo)
0
1
2
3
40 50 60 70
MgO
(
)
SiO2 ()
K2O
(
)
40 50 60 70
0
04
08
4
8
12
SiO2 ()
(a)(b)
(c)
Figure 7 Bi-plots of SiO2 K2 O SiO2 MgO and FeOTiO2 for the WDS analyses obtainedfrom glass shards of the NYT from Procida (Naples) and Prato Spilla Crsquo Means and standarddeviations are shown
results show a higher degree of statistical scatter than the WDS measurements whichmay reregect the fact that the data were normalized combined with the inreguence ofvariation in water content between shards
There is a very close correspondence between the WDS data for the Prato Spilla `Crsquomicro-tephra shards and those obtained from the type-material near Naples (shy g-ure 7) The geochemical data strongly suggest therefore that the NYT is representedat the Prato Spilla `Crsquo site by a discrete layer of micro-tephra particles This conclu-sion is compatible with the pollen-stratigraphic data from the site and accords withage estimates for the NYT (ca 120 14C ka BP) obtained from other sites (Paterneet al 1990)
These results encourage us to believe that many if not all of the tephras listedin table 1 will be detectable over much larger tracts of Europe than is presently thecase if appropriate research is undertaken to detect layers of micro-tephra particlesin selected sites The authors are presently engaged in a major continent-wide pro-gramme of research in collaboration with a number of European research groupsdesigned to test this hypothesis The focus in this research is on those parts of Europewhere we expect to shy nd overlapping `apronsrsquo of tephra deposition originating fromthe Italian Eifel Massif Central and Icelandic provinces For example a number ofsites in parts of southern France northern Italy and perhaps western Switzerlandmay have received inreguxes of micro-tephra originating from the Italian and Eifelprovinces and perhaps also from the Massif Central Sites in parts of Germany Den-mark and southern Sweden for example may in turn have received tephra depositsfrom both of the Icelandic and Eifel provinces If this proves to be the case then thestage will be set for the construction of a tephrostratigraphical framework for Europewhich will enable Last Termination sequences to be correlated on a continent-widebasis using micro- and visible tephra layers as time-parallel stratigraphic markersFurthermore there is also the possibility that other tephras remain to be discovered
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European tephrochronological framework for Termination 1 789
those which either because of the magnitude or nature of some volcanic eruptionswere distributed over parts of Europe in micro-tephra form only
6 European tephrostratigraphy and the chronology of eventsduring the Last Termination and Early Holocene
One of the crucial issues in Late Quaternary palaeoenvironmental research thatremains to be resolved is the degree to which climatic events inferred from oceanicterrestrial and ice-core records were synchronous during the Last Termination andEarly Holocene If the ice-core records provide realistic estimates of the rates anddurations of climatic events during this period then comparisons between individ-ual records have to be enotected with at least a decadal precision The problem thispresents and the role that tephrostratigraphy can play in resolving some of thedimacr culties involved are put into perspective in shy gure 8
Figure 8 shows some of the data used to calibrate radiocarbon dates (the LakeSuigetsu and Cariaco Basin datasets) plotted against the GRIP ss08c ice-core recordof macr 18O variations The latter has been selected by the INTIMATE group as an arbi-trary and temporary standard for this period and used to deshy ne an event stratig-raphy scheme (shy gure 1) for the Last Termination (see Bjorck et al 1998 Walker etal 2001) As has been alluded to in earlier sections of this paper the uncertaintiesassociated with all of the dating methods currently employed preclude precise com-parisons of ice-core marine and terrestrial records Oceanic and terrestrial recordsmostly rely upon radiocarbon dating locally supplemented in a few cases by varvechronology Imprecisions in radiocarbon dates can arise through site-specishy c fac-tors (eg hard-water or mineral carbon errors in freshwater sequences and reservoirerrors in marine sequences) sample selection laboratory measurements of 14C activ-ity and other factors (Lowe amp Walker 2000) Further imprecision may be introducedby the calibration of radiocarbon dates since the uncertainties in the dataset usedto calibrate pre-Holocene radiocarbon dates INTCAL98 are far higher than forthe Holocene which is based on dendro-calibration (Stuiver et al 1998) There arealso uncertainties anotecting varve chronologies while the ss08c ice-core chronologyfor the Last Termination dinoters signishy cantly from the GISP2 record and indeedfrom other models of the GRIP record (Lowe et al 2001) Published comparisonsbetween ice-core marine and terrestrial records for the Last Termination seldom takeinto account the true magnitude of the dating uncertainties involved and frequentlyemploy circular reasoning
Figure 8 shows the positions on the radiocarbon time-scale of 20 of the tephrasdiscussed earlier in this paper these being the ones for which reasonably conshy dentradiocarbon age estimates can be made (though these will be subject to revised esti-mates in the future) A high number of these occur in the period 14080 14C kaBP but we conshy dently anticipate the discovery in the future of additional tephras(perhaps in micro-tephra form only) which will date to the period 185140 14C kaBP Tephras detected in the GRIP ice core over the same time-interval are plottedon the calendar time-scale in shy gure 8 By providing key `time-linesrsquo between recordstephrostratigraphy can help to resolve some of the dating uncertainties referredto earlier by for example enabling direct comparisons of discrepant age estimatesobtained using dinoterent methods (cf Litt et al 2001) It can also provide estimatesof the magnitudes of the reservoir errors that anotected various marine sectors at dif-
Phil Trans R Soc Lond A (2002)
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790 S M Davies and others
-44
-40
-36
-32
cale
ndar
yea
rs B
P
8000
9000
10 0
00
11 0
00
12 0
00
13 0
00
14 0
00
15 0
00
16 0
00
17 0
00
18 0
00
14C age (BP)
VA
SA
Un
Un
Un
Un
Un
BF
Hol
ocen
eG
S-1
GI-
1aG
I-1b
GI-
1cG
I-1d
GI-
1eG
S-2
aG
S-2
bG
S-
2c
Bor
robo
l
La
Nug
egravere
Laa
cher
See
God
ivel
le 5
amp I
-TH
OL
-2
Puy
de D
ocircme
I-T
HO
L-1
Saks
unar
vatn
Houmlg
stor
psm
osse
nU
lmen
er M
aar
amp L
3574
radiocarbon dated European tephra horizons
Cho
pine
Kili
an V
asse
tM
erca
to
God
ivel
le 4
Pom
ici P
rinc
ipal
i amp V
edde
Polla
ra p
umic
eK
OL
-GS-
2 amp
GS
-2B
AS-
12
3
GS
-2B
AS-
4 U
nita
dei
Tef
raSu
peri
ori amp
laye
r Y
-1
Gre
enis
h
L9
20 0
0018
000
16 0
0014
000
12 0
0010
000
-44
-40
-36
-32
800
600
400
200 0
GISP2 volcanicsulphate conc (ppb)
1000
Nea
polit
an Y
ello
w T
uff
GISP2 18O (permil) dGRIP 18O (permil) d
Figure 8 For description see opposite
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 791
ferent times through a comparison of radiocarbon dates obtained from marine andterrestrial horizons in which the same tephra has been detected (see for exampleAustin et al 1995 Bondevik et al 2001 Haregidason et al 2000) Tephrostratigraphymay provide an independent test of suggestions that some of the climatic changesduring the Last Termination were time-transgressive as illustrated for some appar-ently contrasting climatic trends in Iceland Britain and NW Russia (Lowe 2001) Ofparticular importance as far as establishing `leadsrsquo and `lagsrsquo in climatic changes isconcerned are the tephra records from the Greenland ice cores The discovery of theVedde and Saksunarvatn ashes in the GRIP record (Gronvold et al 1995) alreadyprovides a basis for making direct comparisons between marine terrestrial and ice-core records It is a matter of some urgency that the incidence of tephra depositsin the Greenland ice cores be more fully explored in the hope that this will lead tothe recognition of additional time-parallel links between the ice-core records on theone hand and oceanic and terrestrial records on the other An investigation of thenew NordGRIP record for this purpose is currently in progress (S M Davies 2002unpublished data)
Finally a fuller and more reshy ned tephrostratigraphical scheme for Europe will alsohave other applications It will provide an important database for those investigatingthe timing and frequency of volcanic eruptions in Europe during the past 20 000 yror so as well as of the geochemical evolution of the dinoterent volcanic centres overthat period A fuller record of the distribution of micro-tephras may also provideinformation on atmospheric circulation patterns during the dispersal and depositionperiods as well as on the nature and altitude of the eruption columns which mayin turn provide inferences about magma viscosity
This paper is a contribution to the INTIMATE project of the INQUA Palaeoclimate Com-mission and the work is supported by a Leverhulme Trust Research project (grant allocationnumber F07537C) entitled Testing hypotheses of rapid climate change using tephrochronol-ogyrsquo SMDrsquo s contribution was completed during possession of a NERC PhD studentship(GT 0499ES162) We are extremely grateful to Dr Peter G Hill for his assistance withthe EPMA analyses at the Tephrochronology Analytical Unit University of Edinburgh We alsothank Dr G Mastrolorenzo (Vesuvius Observatory) and Miss G Swindle for assistance duringthe macreld investigations in Naples Thanks are also expressed to two anonymous reviewers forcomments on an earlier draft
Appendix A
Table 2 shows the major oxide concentrations of NYT glass shards from Procidaand Prato Spilla `Crsquo and of the Mercato Tephra from the Naples area (see x 4 forsite context) All oxides are shown as weight and total iron is expressed as FeO
Figure 8 Radiocarbon calibration curve for Termination 1 and the Early Holocene compared with theGRIP macr 18 O event stratigraphy the GRIP ss08c and GISP2 macr 18 O records (wwwngdcnoaagov) andknown tephra horizons from this period The shaded areas represent the cooler climatic episodes andare labelled with the Greenland stratotype terminology (Bjorck et al 1998) Where radiocarbon agesare reported in table 1 as a range the mean is given here Abbreviations for GRIP horizons are asfollows Un unknown (approximate positions are given (S Johnsen 2001 personal communication))SA Saksunarvatn Ash VA Vedde Ash BF Black Feather Sulphate concentrations from the GISP2record are also shown (Zielinski et al 1996) Open circles denote radiocarbon calibration data fromLake Suigetsu (Kitagawa amp van der Plicht 2000) Filled circles denote radiocarbon calibration data fromCariaco Basin assuming a marine reservoir age of 420 14 C yr (Hughen et al 1998)
Phil Trans R Soc Lond A (2002)
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792 S M Davies and others
Tab
le2
Majo
roxi
de
con
cen
trati
on
sof
NY
Tgl
ass
shard
sfr
om
Pro
cida
an
dP
rato
Spil
laC
rsquoan
dof
the
Mer
cato
Tep
hra
from
the
Naple
sare
a(s
eex4
for
site
con
text
)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
roci
da)
1584
204
0177
634
201
106
828
635
197
5969
1W
DS
2598
603
9178
027
101
204
924
244
583
4965
8W
DS
3586
604
5173
631
100
805
924
342
183
0951
9W
DS
4583
903
9177
933
000
906
924
540
486
9958
3W
DS
5605
106
8179
126
901
204
923
243
086
1976
4W
DS
6591
704
5177
332
801
006
425
740
887
8968
0W
DS
7581
804
1178
031
501
107
125
640
086
9956
1W
DS
8589
504
2179
533
701
506
926
740
987
5970
4W
DS
9592
003
9178
135
101
007
026
443
585
7972
7W
DS
10
591
404
2174
631
601
105
723
442
482
6957
0W
DS
11
593
403
6177
131
301
506
726
439
188
5967
6W
DS
12
588
103
8176
128
100
505
525
141
583
4952
1W
DS
13
577
003
8176
533
500
807
228
140
384
8952
0W
DS
14
586
004
7179
735
300
706
827
842
984
6968
5W
DS
15
588
104
2180
629
400
505
924
937
993
0964
5W
DS
16
579
603
9178
536
501
308
228
836
087
1959
9W
DS
17
580
103
9177
631
500
907
327
039
488
9956
6W
DS
mea
n588
104
2177
631
901
006
525
940
686
9962
8
sd
(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(07
8)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 793
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
rato
Spil
laC
rsquo)
1552
105
4177
247
401
914
38
735
578
9951
1W
DS
2557
305
7179
845
701
512
640
136
581
5960
6W
DS
3595
004
4173
724
302
003
117
652
877
8950
7W
DS
4575
704
2179
433
001
406
627
043
083
6953
7W
DS
5599
904
0178
826
401
304
421
841
688
4966
5W
DS
6591
103
8177
826
601
105
022
443
888
8960
2W
DS
7565
304
5180
939
501
410
532
535
791
8962
1W
DS
8597
606
9180
826
501
604
821
546
684
6970
7W
DS
9571
805
6179
939
801
109
932
240
883
6964
7W
DS
10
588
603
7176
527
601
104
721
042
487
7953
3W
DS
11
559
404
9180
544
501
812
339
435
878
6957
2W
DS
12
594
704
0181
328
301
705
522
144
785
6967
9W
DS
13
611
103
7187
016
900
802
419
938
195
9975
8W
DS
14
599
204
4181
128
601
404
620
844
986
6971
6W
DS
15
601
204
4177
328
302
004
722
446
385
5972
1W
DS
16
595
104
5176
428
801
504
722
744
884
3962
8W
DS
17
603
704
1177
825
101
503
520
348
181
2965
3W
DS
18
558
704
5179
647
401
813
139
836
879
0960
7W
DS
19
589
602
8178
830
901
606
622
436
091
8960
5W
DS
20
553
606
3178
647
401
913
840
136
978
0956
6W
DS
21
579
004
0175
739
000
708
328
338
286
7959
9W
DS
mea
n582
804
6179
033
401
507
427
341
484
8962
1
sd
(1
87)
(01
0)
(02
7)
(09
2)
(00
4)
(03
9)
(08
0)
(04
9)
(05
0)
(07
0)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
794 S M Davies and others
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)
1575
202
7194
219
701
101
016
374
766
9951
8W
DS
2575
802
9194
523
902
201
520
273
564
5959
0W
DS
3574
301
4205
219
101
100
416
481
266
1965
2W
DS
4575
500
7206
018
002
000
415
181
669
3968
6W
DS
5580
000
9208
018
601
300
515
883
367
1975
5W
DS
6571
001
0206
016
101
600
515
078
967
1957
2W
DS
7577
501
1201
117
101
500
620
675
655
4950
5W
DS
8573
700
9212
717
101
900
815
187
564
2973
9W
DS
9580
301
3208
715
801
400
824
81
754
1968
1W
DS
10
574
400
6211
18
402
00
516
480
567
8971
6W
DS
11
577
200
7214
212
501
200
829
879
247
962
6W
DS
12
572
200
9211
217
301
501
15
980
465
9966
3W
DS
13
571
800
7210
417
402
201
16
184
467
2971
2W
DS
14
567
300
9208
916
901
400
917
383
262
5959
3W
DS
15
568
600
8205
918
202
101
414
682
666
6960
8W
DS
16
572
501
1211
318
202
01
215
884
364
5970
9W
DS
17
572
901
2212
916
502
101
215
883
667
2973
4W
DS
18
573
01
4211
716
301
801
416
83
365
5970
4W
DS
19
569
201
1207
418
602
101
414
982
964
961
6W
DS
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
3)
(04
2)
(01
3)
(00
1)
(00
2)
(01
)(0
39)
(01
1)
(02
5)
Phil Trans R Soc Lond A (2002)
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796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
References
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Allen J R M (and 14 others) 1999 Rapid environmental changes in southern Europe duringthe last glacial period Nature 400 740743
Alley R B (and 10 others) 1993 Abrupt increase in Greenland snow accumulation at the endof the Younger Dryas Nature 362 527529
Andronico D Calderoni G Cioni R Sbrana A Sulpizio R amp Santacroce R 1995 Geo-logical map of Somma Vesuvius volcano Period Mineral 64 7788
Atkinson T C Brireg a K R amp Coope G R 1987 Seasonal temperature in Britain during thepast 22 000 years reconstructed using beetle remains Nature 325 587592
Austin W E N amp Kroon D 1996 Lateglacial sedimentology foraminifera and stable isotopestratigraphy of the Hebridean Continental Shelf northwest Scotland In Late Quaternarypalaeoceanography of the North Atlantic margins (ed J T Andrews W E N Austin HBergsten amp A E Jennings) vol 111 pp 187213 Geological Society of London SpecialPublication
Austin W E N Bard E Hunt J B Kroon D amp Peacock J D 1995 The 14 C age ofthe Vedde Ash implications for Younger Dryas marine reservoir corrections Radiocarbon 375362
Barker D S 1983 Igneous rocks Englewood Clireg s NJ Prentice-Hall
Bennet K D Boreham S amp Sharp M J 1992 Holocene history of environment vegetationand human settlement on Catta Ness Shetland J Ecol 80 241273
Birks H H Gulliksen S Hadeg idason H Mangerud J amp Possnert G 1996 New radiocarbondates for the Vedde Ash and the Saksunarvatn Ash from western Norway Quat Res 45119127
Bjorck J amp Wastegordm ard S 1999 Climate oscillations and tephrochronology in eastern middleSweden during the last glacialinterglacial transition J Quat Sci 14 399410
Bjorck S Ingparaolfsson O Hadeg idason H Hallsdparaottir M amp Anderson N J 1992 Lake Torfadals-vatn a high resolution record of the North Atlantic Ash zone I and the last glacialinterglacialenvironmental changes in Iceland Boreas 21 1522
Bjorck S Walker M J C Cwynar L Johnsen S Knudsen K Lowe J J Wohlfarth Bamp INTIMATE members 1998 An event stratigraphy for the Last Termination in the NorthAtlantic region based on the Greenland ice-core record a proposal by the INTIMATE groupJ Quat Sci 13 283292
Bjorck S Lowe J J amp Walker M J C 2001 Integration of ice core marine and terrestrialrecords of Termination 1 from the North Atlantic region Quat Sci Rev 20 11691274
Bond G C Mandeville C amp Horeg man S 2001 Were rhyolitic glasses in the Vedde Ash andin the North Atlanticrsquo s Ash zone 1 produced by the same volcanic eruption Quat Sci Rev20 11891199
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 797
Bondevik S Mangerud J amp Gulliksen S 2001 The marine 1 4 C age of the Vedde Ash Bedalong the west coast of Norway J Quat Sci 16 37
Bossuet G Richard H Magny M amp Rossy M 1997 A new occurrence of Laacher See Tephrain the central Jura (France) The mire of Le Lautrey C R Acad Sci Paris Sparaer IIa 3254348
Brauer A Endres C Gunter C Litt T Stebich M amp Negendank J F W 1999 Highresolution sediment and vegetation responses to Younger Dryas climate change in varved lakesediments from Meerfelder Maar Germany Quat Sci Rev 18 321329
Brooks S J Mayle F E amp Lowe J J 1997 Chironomid based Lateglacial climatic recon-struction for southeast Scotland J Quat Sci 12 161167
Calanchi N Dinelli E Gasparatto G amp Lucchini F 1996 Etnean tephra layer in Albanolake and Adriatic Sea cores new macrndings of Y-1 layer in the central Mediterranean area ActaVulcan 8 713
Coope G R Lemdahl G Lowe J J amp Walkling A 1998 Temperature gradients in northernEurope during the last glacialHolocene transition (149 ka BP) interpreted from coleopternassemblages J Quat Sci 13 419433
Dansgaard W (and 10 others) 1993 Evidence for general instability of past climate from a250 kyr ice-core record Nature 363 218220
Davies S M Turney C S M amp Lowe J J 2001 Identimacrcation and signimacrcance of a visiblebasalt-rich Vedde Ash layer in a Late-glacial sequence on the Isle of Skye Inner HebridesScotland J Quat Sci 16 99104
Delibrias G Di Paola G M Rosi M amp Santacroce R 1979 La storia eruttiva del complessovulcanico Somma Vesuvio ricostruita dalle successini piroclastiche del Monte Somma RendSoc It Mineral Petrolog 35 411438
Di Vito M A Isaia R Orsi G Southon J de Vita S Drsquo Antonio M Pappalardo L ampPiochi M 1999 Volcanism and deformation since 12 000 years at the Campi Flegrei caldera(Italy) J Volcanol Geophys Res 91 221246
Dugmore A J amp Newton A J 1992 Thin tephra layers in peat revealed by X-radiography JArchaeol Sci 19 163170
Dugmore A J amp Newton A J 1998 Holocene tephra layers in the Faroe Islands Frodskaparrit46 191204
Eastwood A J Pearce N J G Westgate J A Perkins W T Lamb H F amp RobertsN 1999 Geochemistry of Santorini tephra in lake sediments from southwest Turkey GlobalPlanet Change 21 1729
Eirpara sup3 ksson J Knudsen K L Hadeg idason H amp Henriksen P 2000 Lateglacial and Holocenepalaeoceanography of the North Icelandic shelf J Quat Sci 15 2342
Etlicher B Janssen C R Juvignparae E amp Van Leeuwen J F N 1987 Le Haut Forez (MassifCentral France) aprmicroes le Plparaeniglaciaire Wurmien environnement et tparaephra du volcan de LaNugmicroere Bull Ass Fr Etud Quat 4 229239
Frezzotti M amp Narcisi B 1996 Late Quaternary Tephra derived paleosols in central Italyrsquo scarbonate Apennine range stratigraphical and paleoclimatological implications Quat Int3436 147153
Friedrich M Kromer B Spurk M Hofmann J amp Kaiser K F 1999 Paleoenvironment andradiocarbon calibration as derived from LateglacialEarly Holocene tree-ring chronologiesQuat Int 61 2739
Froggatt P C 1992 Standardisation of the chemical analysis of tephra deposits Report of theICCT working group Quat Int 1314 9396
Gronvold K Oskarsson N Johnsen S J Clausen H B Hammer C U Bond G amp Bard E1995 Ash layers from Iceland in the GRIP ice core correlated with oceanic and land sedimentsEarth Planet Sci Lett 135 149155
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
798 S M Davies and others
Hadeg idason H Eirpara sup3 ksson J amp van Kreveld S 2000 The tephrochronology of Iceland and theNorth Atlantic region during the Middle and Late Quaternary a review J Quat Sci 15322
Hoek W Z amp Bohncke S J P 2001 Oxygen isotope wiggle matching as a tool for synchronisingice-core and terrestrial records over Termination 1 Quat Sci Rev 20 12511264
Hughen K A Overpeck J T Peterson L C amp Trumbore S 1996 Rapid climate changes inthe tropical Atlantic region during the last deglaciation Nature 380 5153
Hughen K A Overpeck J T amp Lehman J 1998 A new 14 C calibration data set for the LastDeglaciation Radiocarbon 39 483494
Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
Hunt J B amp Hill P G 1996 An inter-laboratory comparison of the electron probe microanalysisof glass geochemistry Quat Int 3436 229241
Hunt J B amp Hill P G 2001 Tephrological implications of beam sizesample size ereg ects inelectron microprobe analysis of glass shards J Quat Sci 16 105117
Hunt J B Fannin N G T Hill P G amp Peacock J D 1995 The tephrochronology andradiocarbon dating of North Atlantic Late Quaternary sediments an example from the StKilda Basin In The tectonics sedimentation and palaeoceanography of the North Atlanticregion (ed R A Scrutton M S Stoker G B Shimmield amp A W Tudhope) vol 90pp 227248 Geological Society of London Special Publication
Hunt J B Clift P D Lacasse C Vallier T L amp Werner R 1998 Standardisation ofelectron probe microanalysis of glass geochemistry In Proc ODP Scientimacrc Results vol 152pp 8591 College Station TX Ocean Drilling Program
Jakobsson S P 1979 Outline of the petrology of Iceland Jokull 29 5773
Juvignparae E 1987 Deux retombparaees volcaniques tardiglaciaires dans le Cparaezallier (Massif CentralFrance) Bull Ass Fr Etud Quat 13 37
Juvignparae E 1993 Contribution microa la tparaephrostratigraphie du Quaternaire et son application microa lagparaeomorphologie Mparaem Serv Explicat Cartes Gparaeol Min Belg 36 166
Juvignparae E amp Gewelt M 1987 La Narse drsquo Ampoix comme tparaephrostratotype dans la Chasup3 ne desPuys mparaeridionale (France) Bull Ass Fr Etud Quat 29 3749
Juvignparae E Kozarski S amp Nowaczyk B 1995 The occurrence of Laacher See Tephra in Pomera-nia NW Poland Boreas 24 225231
Juvignparae E Bastin B Delibrias G Evin J Gewelt M Gilot E amp Streel M 1996 Acomprehensive pollen and tephra based chronostratigraphic model for the Lateglacial andHolocene period in the French Massif Central Quat Int 3436 113120
Keller J 1980 The island of Vulcano Rend Soc It Mineral Petrolog 36 369414
Keller J Ryan W B F Ninkovich D amp Altherr R 1978 Explosive volcanic activity in theMediterranean over the past 200 000 years as recorded in deep sea sediments Geol Soc AmBull 89 591604
Kitagawa H amp van der Plicht J 2000 Atmospheric radiocarbon calibration beyond 11 900 calBP from Lake Suigetsu laminated sediments Radiocarbon 42 369380
Kvamme T Mangerud J Furnes H amp Ruddiman W F 1989 Geochemistry of Pleistoceneash zones in cores from the North Atlantic Norsk Geol Tids 69 251272
Lacasse C Sigurdsson H Johannesson H Paterne M amp Carey S 1995 Source of Ash zone 1in the North Atlantic Bull Volcanol 57 1832
Langone L Asioli A Corregiari A amp Trincardi F 1996 Age depth modelling through theLate-Quaternary deposits of the central Adriatic Basin In Palaeoenvironmental analysis ofItalian crater lake and Adriatic sediments (ed F Oldmacreld amp P Guilizzoni) vol 55 pp 177196 Memorie dellrsquo Instituto Italiano di Idrobiologia
Larsen G 2000 Holocene volcanism in Iceland and tephrochronology as a tool in volcanologyIn Iceland 2000 modern processes and past environments Keele University UK
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 799
Litt T amp Stebich M 1999 Bio- and chronostratigraphy of the Lateglacial in the Eifel regionGermany Quat Int 61 516
Litt T Brauer A Goslar T Merkt J Balaga K Muller H Ralska-Jasiewiczowa MStebich M amp Negendank J F W 2001 Correlation and synchronisation of Lateglacialcontinental sequences in northern Central Europe based on annually laminated lacustrinesediments Quat Sci Rev 20 12331249
Long D amp Morton A C 1987 An ash fall within the Loch Lomond stadial J Quat Sci 297101
Lotter A F Eicher U Siegenthaler U amp Birks H J B 1992 Lateglacial climatic oscillationsas recorded in Swiss lake sediments J Quat Sci 7 187204
Lowe J J 1992 Lateglacial and Early Holocene lake sediments from the Northern ApenninesItaly|pollen stratigraphy and radiocarbon dating Boreas 21 193208
Lowe J J 2001 Abrupt climatic changes in Europe during the last glacialinterglacial tran-sition the potential for testing hypotheses on the synchroneity of climatic events usingtephrochronology Global Planet Change 603 7384
Lowe J J amp Turney C S M 1997 Vedde Ash layer discovered in a small lake basin on theScottish mainland J Geol Soc Lond 154 605612
Lowe J J amp Walker M J C 2000 Radiocarbon dating the last glacialinterglacial transition(ca 14914 C ka BP) in terrestrial and marine records the need for new quality assuranceprotocols Radiocarbon 42 5368
Lowe J J amp Watson C 1993 Lateglacial and Early Holocene pollen stratigraphy of the northernApennines Italy Quat Sci Rev 12 727738
Lowe J J Birks H H Brooks S J Coope G R Harkness D D Mayle F E SheldrickC Turney C S M amp Walker M J C 1999 The chronology of palaeoenvironmental changesduring the Last GlacialHolocene transition towards an event stratigraphy for the BritishIsles J Geol Soc Lond 156 397410
Lowe J J Hoek W Z amp INTIMATE group 2001 Inter-regional correlation of palaeoclimaticrecords for the Last GlacialInterglacial transition a protocol for improved precision recom-mended by the INTIMATE project group Quat Sci Rev 20 11751187
Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
Mangerud J Lie S E Furnes H Kristiansen I L amp Liquest mo L 1984 A Younger Dryas ashbed in western Norway and its possible correlation with tephra beds from the Norwegian Seaand North Atlantic Quat Res 21 85104
Mangerud J Furnes H amp Jparaohansen J 1986 A 9000 year-old ash bed on the Faroe IslandsQuat Res 26 262265
Martini J 1970 Recherche de retombparaees volcaniques dans le sud-est de la France et la Suisseoccidentale Arch Sci 23 641674
Martini J amp Duret J J 1965 Note preliminaire sur la presence drsquo un niveau de cendres vol-caniques dans des sparaediments post-glaciaires des environs de Genmicroeve Arch Sci 18 587588
Mayewski P A Meeker L D Twickler M S Whitlow S Yang Q Lyons W B amp Pren-tice M 1997 Major features and forcing of high latitudes Northern Hemisphere atmosphericcirculation using a 110 000 year long glaciochemical series J Geophys Res 102 345365
Merkt J Muller H Knabe W Muller P amp Weiser T 1993 The Early Holocene Saksunarvatntephra found in lake sediments in NW Germany Boreas 22 93100
Narcisi B 1993 Segnalazione di un livello piroclastico di provenienza etnea nellrsquo area del Fucino(Italia Centrale) Quaternario 6 8792
Narcisi B 1996 Tephrochronology of a Late Quaternary lacustrine record from the Monticchiomaar (Vulture volcano southern Italy) Quat Sci Rev 15 155165
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on September 20 2011rstaroyalsocietypublishingorgDownloaded from
800 S M Davies and others
Newton A J amp Dugmore A J 1993 Tephrochronology of Core C from Lago Grande di Mon-ticchio In Paleolimnology of European Maar Lakes (ed J F W Negendank amp B Zolitschka)Lecture Notes in Earth Science vol 49 333348 Springer
Oldmacreld F Appleby P G amp Thompson R 1980 Palaeoecological studies of lakes in theHighlands of Papua New Guinea J Ecol 68 457477
Orsi G Drsquo Antonio M de Vita S amp Gallo G 1992 The Neapolitan Yellow Tureg a large mag-nitude trachytic phreatoplinian eruption eruptive dynamics magma withdrawal and calderacollapse J Volcanol Geotherm Res 53 275287
Paterne M Guichard F Labeyrie J Gillot P Y amp Duplessy J C 1986 Tyrrhenian Seatephrochronology of the oxygen isotope record for the past 60 000 years Mar Geol 72259285
Paterne M Guichard F amp Labeyrie J 1988 Explosive activity of the south Italian volca-noes during the past 80 000 years as determined by marine tephrochronology J VolcanolGeotherm Res 34 153172
Paterne M Labeyrie J Guichard F Mazaud A amp Maitre F 1990 Fluctuations of the Cam-panian explosive volcanic activity (south Italy) during the past 190 000 years as determinedby marine tephrochronology Earth Planet Sci Lett 98 166174
Pawse A Beske-Diehl S amp Marshall S A 1998 Use of magnetic hysteresis properties andelectron spin resonance spectroscopy for the identimacrcation of volcanic ash a preliminary studyGeophys J Int 132 712720
Pearce N J G Westgate J A amp Perkins W T 1996 Developments in the analysis of singleglass shards in volcanic deposits by laser ablation ICP-MS quantitative and single internalstandard multi-element methods Quat Int 3436 213227
Pearce N J G Westgate J A Perkins W T Eastwood W J amp Shane P 1999 Theapplication of laser ablation ICP-MS to the analysis of volcanic glass shards from tephradeposits bulk glass and single shard analysis Global Planet Change 21 151171
Pilcher J R amp Hall V A 1992 Towards a tephrochronology for the Holocene of the north ofIreland Holocene 2 255259
Ponel P amp Lowe J J 1992 Coleopteran pollen and radiocarbon evidence from the Prato Spillarsquo Drsquo succession N Italy C R Acad Sci Paris Sparaer II 315 14251431
Rose N L Golding P N E amp Battarbee R W 1996 Selective concentration and enumerationof tephra shards from lake sediment cores Holocene 6 243246
Ruddiman W F amp Glover L K 1972 Vertical mixing of ice rafted volcanic ash in NorthAtlantic sediments Geol Soc Am Bull 83 28172836
Ruddiman W amp McIntyre A 1981 The North Atlantic Ocean during the last deglaciationPalaeogeogr Palaeoclimatol Palaeoecol 35 145214
Santacroce R 1987 Somma Vesuvius Quad Ric Sci 114 252
Sarna-Wojcicki A 2000 Tephrochronology In Quaternary geochronology methods and applica-tions (ed J S Noller J M Sowers amp W R Lettis) AGU Reference shelf vol 4 pp 357377Washington DC American Geophysical Union
Sejrup H P Sjiquest holm J Furnes H Beyer I Eide L Jansen E amp Mangerud J 1989Quaternary tephrochronology on the Iceland Plateau north of Iceland J Quat Sci 4 109114
Sikes E L Samson C R Guilderson T P amp Howard W R 2000 Old radiocarbon agesin the southwest Pacimacrc Ocean during the last glacial period and deglaciation Nature 405555558
Stein R Nam S-I Grobe H amp Hubbersten H 1996 Late Quaternary glacial history andshort term ice rafted debris deg uctuations along the East Greenland continental marine In LateQuaternary palaeoceanography of the North Atlantic margins (ed J T Andrews W E NAustin H Bergsten amp A E Jennings) pp 135151 Geological Society London SpecialPublication
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 801
Stuiver M amp Grootes P M 2000 GISP2 oxygen isotope ratios Quat Res 53 277284
Stuiver M Reimer P J Bard E Beck J W Burr G S Hughen K A Kromer BMcCormac G Van der Plicht J amp Spurk M 1998 INTCAL 98 radiocarbon age calibration24 0000 cal BP Radiocarbon 40 10411083
Sweatman T R amp Long J V P 1969 Quantitative electron microprobe analysis of rock formingminerals J Petrol 7 332379
Turney C S M 1998 Extraction of rhyolitic ash from minerogenic lake sediments J Paleolim-nol 19 199206
Turney C S M amp Lowe J J 2001 Tephrochronology In Tracking environmental changes inlake sediments physical and chemical techniques (ed W M Last amp J P Smol) DordrechtKluwer Academic
Turney C S M Harkness D D amp Lowe J J 1997 The use of microtephra horizons tocorrelate Lateglacial lake sediments successions in Scotland J Quat Sci 12 525531
Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
van den Bogaard P amp Schmincke H 1985 A widespread isochronous Late Quaternary tephralayer in central and northern Europe Geol Soc Am Bull 96 15541571
van den Bogaard B Dordeg er W Sandgren P amp Schmincke H-U 1994 Correlating theHolocene records Icelandic tephra found in Schleswig-Holstein (northern Germany) Natur-wissenschaften 81 554556
Vernet G amp Raynal J-P 2001 Tephrostratigraphy of the Limagne revisited Implications forLateglacial and Holocene Prehistory In Tephras chronology archaeology (ed E Juvignparae ampJ-P Raynal) pp 111116 Dossiers de lrsquo ArchparaeoLogis no 1 France
Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
Vezzoli L 1991 Tephra layers in Bannock Basin (eastern Mediterranean) Mar Geol 1002134
von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
Walker M J C Bjorck S Lowe J J Cwynar L C Johnsen S Knudsen K-L WohlfarthB amp INTIMATE Group 1999 Isotopic events in the GRIP ice core a stratotype for the LatePleistocene Quat Sci Rev 18 11431150
Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
Phil Trans R Soc Lond A (2002)
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802 S M Davies and others
Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
Phil Trans R Soc Lond A (2002)
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788 S M Davies and others
4 8FeO ()
TiO
2 (
) Neapolitan Yellow Tuff(Procida)Neapolitan Yellow Tuff(Prato Spilla lsquoCrsquo)
0
1
2
3
40 50 60 70
MgO
(
)
SiO2 ()
K2O
(
)
40 50 60 70
0
04
08
4
8
12
SiO2 ()
(a)(b)
(c)
Figure 7 Bi-plots of SiO2 K2 O SiO2 MgO and FeOTiO2 for the WDS analyses obtainedfrom glass shards of the NYT from Procida (Naples) and Prato Spilla Crsquo Means and standarddeviations are shown
results show a higher degree of statistical scatter than the WDS measurements whichmay reregect the fact that the data were normalized combined with the inreguence ofvariation in water content between shards
There is a very close correspondence between the WDS data for the Prato Spilla `Crsquomicro-tephra shards and those obtained from the type-material near Naples (shy g-ure 7) The geochemical data strongly suggest therefore that the NYT is representedat the Prato Spilla `Crsquo site by a discrete layer of micro-tephra particles This conclu-sion is compatible with the pollen-stratigraphic data from the site and accords withage estimates for the NYT (ca 120 14C ka BP) obtained from other sites (Paterneet al 1990)
These results encourage us to believe that many if not all of the tephras listedin table 1 will be detectable over much larger tracts of Europe than is presently thecase if appropriate research is undertaken to detect layers of micro-tephra particlesin selected sites The authors are presently engaged in a major continent-wide pro-gramme of research in collaboration with a number of European research groupsdesigned to test this hypothesis The focus in this research is on those parts of Europewhere we expect to shy nd overlapping `apronsrsquo of tephra deposition originating fromthe Italian Eifel Massif Central and Icelandic provinces For example a number ofsites in parts of southern France northern Italy and perhaps western Switzerlandmay have received inreguxes of micro-tephra originating from the Italian and Eifelprovinces and perhaps also from the Massif Central Sites in parts of Germany Den-mark and southern Sweden for example may in turn have received tephra depositsfrom both of the Icelandic and Eifel provinces If this proves to be the case then thestage will be set for the construction of a tephrostratigraphical framework for Europewhich will enable Last Termination sequences to be correlated on a continent-widebasis using micro- and visible tephra layers as time-parallel stratigraphic markersFurthermore there is also the possibility that other tephras remain to be discovered
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 789
those which either because of the magnitude or nature of some volcanic eruptionswere distributed over parts of Europe in micro-tephra form only
6 European tephrostratigraphy and the chronology of eventsduring the Last Termination and Early Holocene
One of the crucial issues in Late Quaternary palaeoenvironmental research thatremains to be resolved is the degree to which climatic events inferred from oceanicterrestrial and ice-core records were synchronous during the Last Termination andEarly Holocene If the ice-core records provide realistic estimates of the rates anddurations of climatic events during this period then comparisons between individ-ual records have to be enotected with at least a decadal precision The problem thispresents and the role that tephrostratigraphy can play in resolving some of thedimacr culties involved are put into perspective in shy gure 8
Figure 8 shows some of the data used to calibrate radiocarbon dates (the LakeSuigetsu and Cariaco Basin datasets) plotted against the GRIP ss08c ice-core recordof macr 18O variations The latter has been selected by the INTIMATE group as an arbi-trary and temporary standard for this period and used to deshy ne an event stratig-raphy scheme (shy gure 1) for the Last Termination (see Bjorck et al 1998 Walker etal 2001) As has been alluded to in earlier sections of this paper the uncertaintiesassociated with all of the dating methods currently employed preclude precise com-parisons of ice-core marine and terrestrial records Oceanic and terrestrial recordsmostly rely upon radiocarbon dating locally supplemented in a few cases by varvechronology Imprecisions in radiocarbon dates can arise through site-specishy c fac-tors (eg hard-water or mineral carbon errors in freshwater sequences and reservoirerrors in marine sequences) sample selection laboratory measurements of 14C activ-ity and other factors (Lowe amp Walker 2000) Further imprecision may be introducedby the calibration of radiocarbon dates since the uncertainties in the dataset usedto calibrate pre-Holocene radiocarbon dates INTCAL98 are far higher than forthe Holocene which is based on dendro-calibration (Stuiver et al 1998) There arealso uncertainties anotecting varve chronologies while the ss08c ice-core chronologyfor the Last Termination dinoters signishy cantly from the GISP2 record and indeedfrom other models of the GRIP record (Lowe et al 2001) Published comparisonsbetween ice-core marine and terrestrial records for the Last Termination seldom takeinto account the true magnitude of the dating uncertainties involved and frequentlyemploy circular reasoning
Figure 8 shows the positions on the radiocarbon time-scale of 20 of the tephrasdiscussed earlier in this paper these being the ones for which reasonably conshy dentradiocarbon age estimates can be made (though these will be subject to revised esti-mates in the future) A high number of these occur in the period 14080 14C kaBP but we conshy dently anticipate the discovery in the future of additional tephras(perhaps in micro-tephra form only) which will date to the period 185140 14C kaBP Tephras detected in the GRIP ice core over the same time-interval are plottedon the calendar time-scale in shy gure 8 By providing key `time-linesrsquo between recordstephrostratigraphy can help to resolve some of the dating uncertainties referredto earlier by for example enabling direct comparisons of discrepant age estimatesobtained using dinoterent methods (cf Litt et al 2001) It can also provide estimatesof the magnitudes of the reservoir errors that anotected various marine sectors at dif-
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
790 S M Davies and others
-44
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00
14 0
00
15 0
00
16 0
00
17 0
00
18 0
00
14C age (BP)
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amp I
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amp L
3574
radiocarbon dated European tephra horizons
Cho
pine
Kili
an V
asse
tM
erca
to
God
ivel
le 4
Pom
ici P
rinc
ipal
i amp V
edde
Polla
ra p
umic
eK
OL
-GS-
2 amp
GS
-2B
AS-
12
3
GS
-2B
AS-
4 U
nita
dei
Tef
raSu
peri
ori amp
laye
r Y
-1
Gre
enis
h
L9
20 0
0018
000
16 0
0014
000
12 0
0010
000
-44
-40
-36
-32
800
600
400
200 0
GISP2 volcanicsulphate conc (ppb)
1000
Nea
polit
an Y
ello
w T
uff
GISP2 18O (permil) dGRIP 18O (permil) d
Figure 8 For description see opposite
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 791
ferent times through a comparison of radiocarbon dates obtained from marine andterrestrial horizons in which the same tephra has been detected (see for exampleAustin et al 1995 Bondevik et al 2001 Haregidason et al 2000) Tephrostratigraphymay provide an independent test of suggestions that some of the climatic changesduring the Last Termination were time-transgressive as illustrated for some appar-ently contrasting climatic trends in Iceland Britain and NW Russia (Lowe 2001) Ofparticular importance as far as establishing `leadsrsquo and `lagsrsquo in climatic changes isconcerned are the tephra records from the Greenland ice cores The discovery of theVedde and Saksunarvatn ashes in the GRIP record (Gronvold et al 1995) alreadyprovides a basis for making direct comparisons between marine terrestrial and ice-core records It is a matter of some urgency that the incidence of tephra depositsin the Greenland ice cores be more fully explored in the hope that this will lead tothe recognition of additional time-parallel links between the ice-core records on theone hand and oceanic and terrestrial records on the other An investigation of thenew NordGRIP record for this purpose is currently in progress (S M Davies 2002unpublished data)
Finally a fuller and more reshy ned tephrostratigraphical scheme for Europe will alsohave other applications It will provide an important database for those investigatingthe timing and frequency of volcanic eruptions in Europe during the past 20 000 yror so as well as of the geochemical evolution of the dinoterent volcanic centres overthat period A fuller record of the distribution of micro-tephras may also provideinformation on atmospheric circulation patterns during the dispersal and depositionperiods as well as on the nature and altitude of the eruption columns which mayin turn provide inferences about magma viscosity
This paper is a contribution to the INTIMATE project of the INQUA Palaeoclimate Com-mission and the work is supported by a Leverhulme Trust Research project (grant allocationnumber F07537C) entitled Testing hypotheses of rapid climate change using tephrochronol-ogyrsquo SMDrsquo s contribution was completed during possession of a NERC PhD studentship(GT 0499ES162) We are extremely grateful to Dr Peter G Hill for his assistance withthe EPMA analyses at the Tephrochronology Analytical Unit University of Edinburgh We alsothank Dr G Mastrolorenzo (Vesuvius Observatory) and Miss G Swindle for assistance duringthe macreld investigations in Naples Thanks are also expressed to two anonymous reviewers forcomments on an earlier draft
Appendix A
Table 2 shows the major oxide concentrations of NYT glass shards from Procidaand Prato Spilla `Crsquo and of the Mercato Tephra from the Naples area (see x 4 forsite context) All oxides are shown as weight and total iron is expressed as FeO
Figure 8 Radiocarbon calibration curve for Termination 1 and the Early Holocene compared with theGRIP macr 18 O event stratigraphy the GRIP ss08c and GISP2 macr 18 O records (wwwngdcnoaagov) andknown tephra horizons from this period The shaded areas represent the cooler climatic episodes andare labelled with the Greenland stratotype terminology (Bjorck et al 1998) Where radiocarbon agesare reported in table 1 as a range the mean is given here Abbreviations for GRIP horizons are asfollows Un unknown (approximate positions are given (S Johnsen 2001 personal communication))SA Saksunarvatn Ash VA Vedde Ash BF Black Feather Sulphate concentrations from the GISP2record are also shown (Zielinski et al 1996) Open circles denote radiocarbon calibration data fromLake Suigetsu (Kitagawa amp van der Plicht 2000) Filled circles denote radiocarbon calibration data fromCariaco Basin assuming a marine reservoir age of 420 14 C yr (Hughen et al 1998)
Phil Trans R Soc Lond A (2002)
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792 S M Davies and others
Tab
le2
Majo
roxi
de
con
cen
trati
on
sof
NY
Tgl
ass
shard
sfr
om
Pro
cida
an
dP
rato
Spil
laC
rsquoan
dof
the
Mer
cato
Tep
hra
from
the
Naple
sare
a(s
eex4
for
site
con
text
)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
roci
da)
1584
204
0177
634
201
106
828
635
197
5969
1W
DS
2598
603
9178
027
101
204
924
244
583
4965
8W
DS
3586
604
5173
631
100
805
924
342
183
0951
9W
DS
4583
903
9177
933
000
906
924
540
486
9958
3W
DS
5605
106
8179
126
901
204
923
243
086
1976
4W
DS
6591
704
5177
332
801
006
425
740
887
8968
0W
DS
7581
804
1178
031
501
107
125
640
086
9956
1W
DS
8589
504
2179
533
701
506
926
740
987
5970
4W
DS
9592
003
9178
135
101
007
026
443
585
7972
7W
DS
10
591
404
2174
631
601
105
723
442
482
6957
0W
DS
11
593
403
6177
131
301
506
726
439
188
5967
6W
DS
12
588
103
8176
128
100
505
525
141
583
4952
1W
DS
13
577
003
8176
533
500
807
228
140
384
8952
0W
DS
14
586
004
7179
735
300
706
827
842
984
6968
5W
DS
15
588
104
2180
629
400
505
924
937
993
0964
5W
DS
16
579
603
9178
536
501
308
228
836
087
1959
9W
DS
17
580
103
9177
631
500
907
327
039
488
9956
6W
DS
mea
n588
104
2177
631
901
006
525
940
686
9962
8
sd
(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(07
8)
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 793
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
rato
Spil
laC
rsquo)
1552
105
4177
247
401
914
38
735
578
9951
1W
DS
2557
305
7179
845
701
512
640
136
581
5960
6W
DS
3595
004
4173
724
302
003
117
652
877
8950
7W
DS
4575
704
2179
433
001
406
627
043
083
6953
7W
DS
5599
904
0178
826
401
304
421
841
688
4966
5W
DS
6591
103
8177
826
601
105
022
443
888
8960
2W
DS
7565
304
5180
939
501
410
532
535
791
8962
1W
DS
8597
606
9180
826
501
604
821
546
684
6970
7W
DS
9571
805
6179
939
801
109
932
240
883
6964
7W
DS
10
588
603
7176
527
601
104
721
042
487
7953
3W
DS
11
559
404
9180
544
501
812
339
435
878
6957
2W
DS
12
594
704
0181
328
301
705
522
144
785
6967
9W
DS
13
611
103
7187
016
900
802
419
938
195
9975
8W
DS
14
599
204
4181
128
601
404
620
844
986
6971
6W
DS
15
601
204
4177
328
302
004
722
446
385
5972
1W
DS
16
595
104
5176
428
801
504
722
744
884
3962
8W
DS
17
603
704
1177
825
101
503
520
348
181
2965
3W
DS
18
558
704
5179
647
401
813
139
836
879
0960
7W
DS
19
589
602
8178
830
901
606
622
436
091
8960
5W
DS
20
553
606
3178
647
401
913
840
136
978
0956
6W
DS
21
579
004
0175
739
000
708
328
338
286
7959
9W
DS
mea
n582
804
6179
033
401
507
427
341
484
8962
1
sd
(1
87)
(01
0)
(02
7)
(09
2)
(00
4)
(03
9)
(08
0)
(04
9)
(05
0)
(07
0)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
794 S M Davies and others
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)
1575
202
7194
219
701
101
016
374
766
9951
8W
DS
2575
802
9194
523
902
201
520
273
564
5959
0W
DS
3574
301
4205
219
101
100
416
481
266
1965
2W
DS
4575
500
7206
018
002
000
415
181
669
3968
6W
DS
5580
000
9208
018
601
300
515
883
367
1975
5W
DS
6571
001
0206
016
101
600
515
078
967
1957
2W
DS
7577
501
1201
117
101
500
620
675
655
4950
5W
DS
8573
700
9212
717
101
900
815
187
564
2973
9W
DS
9580
301
3208
715
801
400
824
81
754
1968
1W
DS
10
574
400
6211
18
402
00
516
480
567
8971
6W
DS
11
577
200
7214
212
501
200
829
879
247
962
6W
DS
12
572
200
9211
217
301
501
15
980
465
9966
3W
DS
13
571
800
7210
417
402
201
16
184
467
2971
2W
DS
14
567
300
9208
916
901
400
917
383
262
5959
3W
DS
15
568
600
8205
918
202
101
414
682
666
6960
8W
DS
16
572
501
1211
318
202
01
215
884
364
5970
9W
DS
17
572
901
2212
916
502
101
215
883
667
2973
4W
DS
18
573
01
4211
716
301
801
416
83
365
5970
4W
DS
19
569
201
1207
418
602
101
414
982
964
961
6W
DS
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
3)
(04
2)
(01
3)
(00
1)
(00
2)
(01
)(0
39)
(01
1)
(02
5)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
References
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Hughen K A Overpeck J T Peterson L C amp Trumbore S 1996 Rapid climate changes inthe tropical Atlantic region during the last deglaciation Nature 380 5153
Hughen K A Overpeck J T amp Lehman J 1998 A new 14 C calibration data set for the LastDeglaciation Radiocarbon 39 483494
Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
Hunt J B amp Hill P G 1996 An inter-laboratory comparison of the electron probe microanalysisof glass geochemistry Quat Int 3436 229241
Hunt J B amp Hill P G 2001 Tephrological implications of beam sizesample size ereg ects inelectron microprobe analysis of glass shards J Quat Sci 16 105117
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Juvignparae E amp Gewelt M 1987 La Narse drsquo Ampoix comme tparaephrostratotype dans la Chasup3 ne desPuys mparaeridionale (France) Bull Ass Fr Etud Quat 29 3749
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Juvignparae E Bastin B Delibrias G Evin J Gewelt M Gilot E amp Streel M 1996 Acomprehensive pollen and tephra based chronostratigraphic model for the Lateglacial andHolocene period in the French Massif Central Quat Int 3436 113120
Keller J 1980 The island of Vulcano Rend Soc It Mineral Petrolog 36 369414
Keller J Ryan W B F Ninkovich D amp Altherr R 1978 Explosive volcanic activity in theMediterranean over the past 200 000 years as recorded in deep sea sediments Geol Soc AmBull 89 591604
Kitagawa H amp van der Plicht J 2000 Atmospheric radiocarbon calibration beyond 11 900 calBP from Lake Suigetsu laminated sediments Radiocarbon 42 369380
Kvamme T Mangerud J Furnes H amp Ruddiman W F 1989 Geochemistry of Pleistoceneash zones in cores from the North Atlantic Norsk Geol Tids 69 251272
Lacasse C Sigurdsson H Johannesson H Paterne M amp Carey S 1995 Source of Ash zone 1in the North Atlantic Bull Volcanol 57 1832
Langone L Asioli A Corregiari A amp Trincardi F 1996 Age depth modelling through theLate-Quaternary deposits of the central Adriatic Basin In Palaeoenvironmental analysis ofItalian crater lake and Adriatic sediments (ed F Oldmacreld amp P Guilizzoni) vol 55 pp 177196 Memorie dellrsquo Instituto Italiano di Idrobiologia
Larsen G 2000 Holocene volcanism in Iceland and tephrochronology as a tool in volcanologyIn Iceland 2000 modern processes and past environments Keele University UK
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 799
Litt T amp Stebich M 1999 Bio- and chronostratigraphy of the Lateglacial in the Eifel regionGermany Quat Int 61 516
Litt T Brauer A Goslar T Merkt J Balaga K Muller H Ralska-Jasiewiczowa MStebich M amp Negendank J F W 2001 Correlation and synchronisation of Lateglacialcontinental sequences in northern Central Europe based on annually laminated lacustrinesediments Quat Sci Rev 20 12331249
Long D amp Morton A C 1987 An ash fall within the Loch Lomond stadial J Quat Sci 297101
Lotter A F Eicher U Siegenthaler U amp Birks H J B 1992 Lateglacial climatic oscillationsas recorded in Swiss lake sediments J Quat Sci 7 187204
Lowe J J 1992 Lateglacial and Early Holocene lake sediments from the Northern ApenninesItaly|pollen stratigraphy and radiocarbon dating Boreas 21 193208
Lowe J J 2001 Abrupt climatic changes in Europe during the last glacialinterglacial tran-sition the potential for testing hypotheses on the synchroneity of climatic events usingtephrochronology Global Planet Change 603 7384
Lowe J J amp Turney C S M 1997 Vedde Ash layer discovered in a small lake basin on theScottish mainland J Geol Soc Lond 154 605612
Lowe J J amp Walker M J C 2000 Radiocarbon dating the last glacialinterglacial transition(ca 14914 C ka BP) in terrestrial and marine records the need for new quality assuranceprotocols Radiocarbon 42 5368
Lowe J J amp Watson C 1993 Lateglacial and Early Holocene pollen stratigraphy of the northernApennines Italy Quat Sci Rev 12 727738
Lowe J J Birks H H Brooks S J Coope G R Harkness D D Mayle F E SheldrickC Turney C S M amp Walker M J C 1999 The chronology of palaeoenvironmental changesduring the Last GlacialHolocene transition towards an event stratigraphy for the BritishIsles J Geol Soc Lond 156 397410
Lowe J J Hoek W Z amp INTIMATE group 2001 Inter-regional correlation of palaeoclimaticrecords for the Last GlacialInterglacial transition a protocol for improved precision recom-mended by the INTIMATE project group Quat Sci Rev 20 11751187
Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
Mangerud J Lie S E Furnes H Kristiansen I L amp Liquest mo L 1984 A Younger Dryas ashbed in western Norway and its possible correlation with tephra beds from the Norwegian Seaand North Atlantic Quat Res 21 85104
Mangerud J Furnes H amp Jparaohansen J 1986 A 9000 year-old ash bed on the Faroe IslandsQuat Res 26 262265
Martini J 1970 Recherche de retombparaees volcaniques dans le sud-est de la France et la Suisseoccidentale Arch Sci 23 641674
Martini J amp Duret J J 1965 Note preliminaire sur la presence drsquo un niveau de cendres vol-caniques dans des sparaediments post-glaciaires des environs de Genmicroeve Arch Sci 18 587588
Mayewski P A Meeker L D Twickler M S Whitlow S Yang Q Lyons W B amp Pren-tice M 1997 Major features and forcing of high latitudes Northern Hemisphere atmosphericcirculation using a 110 000 year long glaciochemical series J Geophys Res 102 345365
Merkt J Muller H Knabe W Muller P amp Weiser T 1993 The Early Holocene Saksunarvatntephra found in lake sediments in NW Germany Boreas 22 93100
Narcisi B 1993 Segnalazione di un livello piroclastico di provenienza etnea nellrsquo area del Fucino(Italia Centrale) Quaternario 6 8792
Narcisi B 1996 Tephrochronology of a Late Quaternary lacustrine record from the Monticchiomaar (Vulture volcano southern Italy) Quat Sci Rev 15 155165
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Newton A J amp Dugmore A J 1993 Tephrochronology of Core C from Lago Grande di Mon-ticchio In Paleolimnology of European Maar Lakes (ed J F W Negendank amp B Zolitschka)Lecture Notes in Earth Science vol 49 333348 Springer
Oldmacreld F Appleby P G amp Thompson R 1980 Palaeoecological studies of lakes in theHighlands of Papua New Guinea J Ecol 68 457477
Orsi G Drsquo Antonio M de Vita S amp Gallo G 1992 The Neapolitan Yellow Tureg a large mag-nitude trachytic phreatoplinian eruption eruptive dynamics magma withdrawal and calderacollapse J Volcanol Geotherm Res 53 275287
Paterne M Guichard F Labeyrie J Gillot P Y amp Duplessy J C 1986 Tyrrhenian Seatephrochronology of the oxygen isotope record for the past 60 000 years Mar Geol 72259285
Paterne M Guichard F amp Labeyrie J 1988 Explosive activity of the south Italian volca-noes during the past 80 000 years as determined by marine tephrochronology J VolcanolGeotherm Res 34 153172
Paterne M Labeyrie J Guichard F Mazaud A amp Maitre F 1990 Fluctuations of the Cam-panian explosive volcanic activity (south Italy) during the past 190 000 years as determinedby marine tephrochronology Earth Planet Sci Lett 98 166174
Pawse A Beske-Diehl S amp Marshall S A 1998 Use of magnetic hysteresis properties andelectron spin resonance spectroscopy for the identimacrcation of volcanic ash a preliminary studyGeophys J Int 132 712720
Pearce N J G Westgate J A amp Perkins W T 1996 Developments in the analysis of singleglass shards in volcanic deposits by laser ablation ICP-MS quantitative and single internalstandard multi-element methods Quat Int 3436 213227
Pearce N J G Westgate J A Perkins W T Eastwood W J amp Shane P 1999 Theapplication of laser ablation ICP-MS to the analysis of volcanic glass shards from tephradeposits bulk glass and single shard analysis Global Planet Change 21 151171
Pilcher J R amp Hall V A 1992 Towards a tephrochronology for the Holocene of the north ofIreland Holocene 2 255259
Ponel P amp Lowe J J 1992 Coleopteran pollen and radiocarbon evidence from the Prato Spillarsquo Drsquo succession N Italy C R Acad Sci Paris Sparaer II 315 14251431
Rose N L Golding P N E amp Battarbee R W 1996 Selective concentration and enumerationof tephra shards from lake sediment cores Holocene 6 243246
Ruddiman W F amp Glover L K 1972 Vertical mixing of ice rafted volcanic ash in NorthAtlantic sediments Geol Soc Am Bull 83 28172836
Ruddiman W amp McIntyre A 1981 The North Atlantic Ocean during the last deglaciationPalaeogeogr Palaeoclimatol Palaeoecol 35 145214
Santacroce R 1987 Somma Vesuvius Quad Ric Sci 114 252
Sarna-Wojcicki A 2000 Tephrochronology In Quaternary geochronology methods and applica-tions (ed J S Noller J M Sowers amp W R Lettis) AGU Reference shelf vol 4 pp 357377Washington DC American Geophysical Union
Sejrup H P Sjiquest holm J Furnes H Beyer I Eide L Jansen E amp Mangerud J 1989Quaternary tephrochronology on the Iceland Plateau north of Iceland J Quat Sci 4 109114
Sikes E L Samson C R Guilderson T P amp Howard W R 2000 Old radiocarbon agesin the southwest Pacimacrc Ocean during the last glacial period and deglaciation Nature 405555558
Stein R Nam S-I Grobe H amp Hubbersten H 1996 Late Quaternary glacial history andshort term ice rafted debris deg uctuations along the East Greenland continental marine In LateQuaternary palaeoceanography of the North Atlantic margins (ed J T Andrews W E NAustin H Bergsten amp A E Jennings) pp 135151 Geological Society London SpecialPublication
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on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 801
Stuiver M amp Grootes P M 2000 GISP2 oxygen isotope ratios Quat Res 53 277284
Stuiver M Reimer P J Bard E Beck J W Burr G S Hughen K A Kromer BMcCormac G Van der Plicht J amp Spurk M 1998 INTCAL 98 radiocarbon age calibration24 0000 cal BP Radiocarbon 40 10411083
Sweatman T R amp Long J V P 1969 Quantitative electron microprobe analysis of rock formingminerals J Petrol 7 332379
Turney C S M 1998 Extraction of rhyolitic ash from minerogenic lake sediments J Paleolim-nol 19 199206
Turney C S M amp Lowe J J 2001 Tephrochronology In Tracking environmental changes inlake sediments physical and chemical techniques (ed W M Last amp J P Smol) DordrechtKluwer Academic
Turney C S M Harkness D D amp Lowe J J 1997 The use of microtephra horizons tocorrelate Lateglacial lake sediments successions in Scotland J Quat Sci 12 525531
Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
van den Bogaard P amp Schmincke H 1985 A widespread isochronous Late Quaternary tephralayer in central and northern Europe Geol Soc Am Bull 96 15541571
van den Bogaard B Dordeg er W Sandgren P amp Schmincke H-U 1994 Correlating theHolocene records Icelandic tephra found in Schleswig-Holstein (northern Germany) Natur-wissenschaften 81 554556
Vernet G amp Raynal J-P 2001 Tephrostratigraphy of the Limagne revisited Implications forLateglacial and Holocene Prehistory In Tephras chronology archaeology (ed E Juvignparae ampJ-P Raynal) pp 111116 Dossiers de lrsquo ArchparaeoLogis no 1 France
Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
Vezzoli L 1991 Tephra layers in Bannock Basin (eastern Mediterranean) Mar Geol 1002134
von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
Walker M J C Bjorck S Lowe J J Cwynar L C Johnsen S Knudsen K-L WohlfarthB amp INTIMATE Group 1999 Isotopic events in the GRIP ice core a stratotype for the LatePleistocene Quat Sci Rev 18 11431150
Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
802 S M Davies and others
Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 789
those which either because of the magnitude or nature of some volcanic eruptionswere distributed over parts of Europe in micro-tephra form only
6 European tephrostratigraphy and the chronology of eventsduring the Last Termination and Early Holocene
One of the crucial issues in Late Quaternary palaeoenvironmental research thatremains to be resolved is the degree to which climatic events inferred from oceanicterrestrial and ice-core records were synchronous during the Last Termination andEarly Holocene If the ice-core records provide realistic estimates of the rates anddurations of climatic events during this period then comparisons between individ-ual records have to be enotected with at least a decadal precision The problem thispresents and the role that tephrostratigraphy can play in resolving some of thedimacr culties involved are put into perspective in shy gure 8
Figure 8 shows some of the data used to calibrate radiocarbon dates (the LakeSuigetsu and Cariaco Basin datasets) plotted against the GRIP ss08c ice-core recordof macr 18O variations The latter has been selected by the INTIMATE group as an arbi-trary and temporary standard for this period and used to deshy ne an event stratig-raphy scheme (shy gure 1) for the Last Termination (see Bjorck et al 1998 Walker etal 2001) As has been alluded to in earlier sections of this paper the uncertaintiesassociated with all of the dating methods currently employed preclude precise com-parisons of ice-core marine and terrestrial records Oceanic and terrestrial recordsmostly rely upon radiocarbon dating locally supplemented in a few cases by varvechronology Imprecisions in radiocarbon dates can arise through site-specishy c fac-tors (eg hard-water or mineral carbon errors in freshwater sequences and reservoirerrors in marine sequences) sample selection laboratory measurements of 14C activ-ity and other factors (Lowe amp Walker 2000) Further imprecision may be introducedby the calibration of radiocarbon dates since the uncertainties in the dataset usedto calibrate pre-Holocene radiocarbon dates INTCAL98 are far higher than forthe Holocene which is based on dendro-calibration (Stuiver et al 1998) There arealso uncertainties anotecting varve chronologies while the ss08c ice-core chronologyfor the Last Termination dinoters signishy cantly from the GISP2 record and indeedfrom other models of the GRIP record (Lowe et al 2001) Published comparisonsbetween ice-core marine and terrestrial records for the Last Termination seldom takeinto account the true magnitude of the dating uncertainties involved and frequentlyemploy circular reasoning
Figure 8 shows the positions on the radiocarbon time-scale of 20 of the tephrasdiscussed earlier in this paper these being the ones for which reasonably conshy dentradiocarbon age estimates can be made (though these will be subject to revised esti-mates in the future) A high number of these occur in the period 14080 14C kaBP but we conshy dently anticipate the discovery in the future of additional tephras(perhaps in micro-tephra form only) which will date to the period 185140 14C kaBP Tephras detected in the GRIP ice core over the same time-interval are plottedon the calendar time-scale in shy gure 8 By providing key `time-linesrsquo between recordstephrostratigraphy can help to resolve some of the dating uncertainties referredto earlier by for example enabling direct comparisons of discrepant age estimatesobtained using dinoterent methods (cf Litt et al 2001) It can also provide estimatesof the magnitudes of the reservoir errors that anotected various marine sectors at dif-
Phil Trans R Soc Lond A (2002)
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790 S M Davies and others
-44
-40
-36
-32
cale
ndar
yea
rs B
P
8000
9000
10 0
00
11 0
00
12 0
00
13 0
00
14 0
00
15 0
00
16 0
00
17 0
00
18 0
00
14C age (BP)
VA
SA
Un
Un
Un
Un
Un
BF
Hol
ocen
eG
S-1
GI-
1aG
I-1b
GI-
1cG
I-1d
GI-
1eG
S-2
aG
S-2
bG
S-
2c
Bor
robo
l
La
Nug
egravere
Laa
cher
See
God
ivel
le 5
amp I
-TH
OL
-2
Puy
de D
ocircme
I-T
HO
L-1
Saks
unar
vatn
Houmlg
stor
psm
osse
nU
lmen
er M
aar
amp L
3574
radiocarbon dated European tephra horizons
Cho
pine
Kili
an V
asse
tM
erca
to
God
ivel
le 4
Pom
ici P
rinc
ipal
i amp V
edde
Polla
ra p
umic
eK
OL
-GS-
2 amp
GS
-2B
AS-
12
3
GS
-2B
AS-
4 U
nita
dei
Tef
raSu
peri
ori amp
laye
r Y
-1
Gre
enis
h
L9
20 0
0018
000
16 0
0014
000
12 0
0010
000
-44
-40
-36
-32
800
600
400
200 0
GISP2 volcanicsulphate conc (ppb)
1000
Nea
polit
an Y
ello
w T
uff
GISP2 18O (permil) dGRIP 18O (permil) d
Figure 8 For description see opposite
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 791
ferent times through a comparison of radiocarbon dates obtained from marine andterrestrial horizons in which the same tephra has been detected (see for exampleAustin et al 1995 Bondevik et al 2001 Haregidason et al 2000) Tephrostratigraphymay provide an independent test of suggestions that some of the climatic changesduring the Last Termination were time-transgressive as illustrated for some appar-ently contrasting climatic trends in Iceland Britain and NW Russia (Lowe 2001) Ofparticular importance as far as establishing `leadsrsquo and `lagsrsquo in climatic changes isconcerned are the tephra records from the Greenland ice cores The discovery of theVedde and Saksunarvatn ashes in the GRIP record (Gronvold et al 1995) alreadyprovides a basis for making direct comparisons between marine terrestrial and ice-core records It is a matter of some urgency that the incidence of tephra depositsin the Greenland ice cores be more fully explored in the hope that this will lead tothe recognition of additional time-parallel links between the ice-core records on theone hand and oceanic and terrestrial records on the other An investigation of thenew NordGRIP record for this purpose is currently in progress (S M Davies 2002unpublished data)
Finally a fuller and more reshy ned tephrostratigraphical scheme for Europe will alsohave other applications It will provide an important database for those investigatingthe timing and frequency of volcanic eruptions in Europe during the past 20 000 yror so as well as of the geochemical evolution of the dinoterent volcanic centres overthat period A fuller record of the distribution of micro-tephras may also provideinformation on atmospheric circulation patterns during the dispersal and depositionperiods as well as on the nature and altitude of the eruption columns which mayin turn provide inferences about magma viscosity
This paper is a contribution to the INTIMATE project of the INQUA Palaeoclimate Com-mission and the work is supported by a Leverhulme Trust Research project (grant allocationnumber F07537C) entitled Testing hypotheses of rapid climate change using tephrochronol-ogyrsquo SMDrsquo s contribution was completed during possession of a NERC PhD studentship(GT 0499ES162) We are extremely grateful to Dr Peter G Hill for his assistance withthe EPMA analyses at the Tephrochronology Analytical Unit University of Edinburgh We alsothank Dr G Mastrolorenzo (Vesuvius Observatory) and Miss G Swindle for assistance duringthe macreld investigations in Naples Thanks are also expressed to two anonymous reviewers forcomments on an earlier draft
Appendix A
Table 2 shows the major oxide concentrations of NYT glass shards from Procidaand Prato Spilla `Crsquo and of the Mercato Tephra from the Naples area (see x 4 forsite context) All oxides are shown as weight and total iron is expressed as FeO
Figure 8 Radiocarbon calibration curve for Termination 1 and the Early Holocene compared with theGRIP macr 18 O event stratigraphy the GRIP ss08c and GISP2 macr 18 O records (wwwngdcnoaagov) andknown tephra horizons from this period The shaded areas represent the cooler climatic episodes andare labelled with the Greenland stratotype terminology (Bjorck et al 1998) Where radiocarbon agesare reported in table 1 as a range the mean is given here Abbreviations for GRIP horizons are asfollows Un unknown (approximate positions are given (S Johnsen 2001 personal communication))SA Saksunarvatn Ash VA Vedde Ash BF Black Feather Sulphate concentrations from the GISP2record are also shown (Zielinski et al 1996) Open circles denote radiocarbon calibration data fromLake Suigetsu (Kitagawa amp van der Plicht 2000) Filled circles denote radiocarbon calibration data fromCariaco Basin assuming a marine reservoir age of 420 14 C yr (Hughen et al 1998)
Phil Trans R Soc Lond A (2002)
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792 S M Davies and others
Tab
le2
Majo
roxi
de
con
cen
trati
on
sof
NY
Tgl
ass
shard
sfr
om
Pro
cida
an
dP
rato
Spil
laC
rsquoan
dof
the
Mer
cato
Tep
hra
from
the
Naple
sare
a(s
eex4
for
site
con
text
)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
roci
da)
1584
204
0177
634
201
106
828
635
197
5969
1W
DS
2598
603
9178
027
101
204
924
244
583
4965
8W
DS
3586
604
5173
631
100
805
924
342
183
0951
9W
DS
4583
903
9177
933
000
906
924
540
486
9958
3W
DS
5605
106
8179
126
901
204
923
243
086
1976
4W
DS
6591
704
5177
332
801
006
425
740
887
8968
0W
DS
7581
804
1178
031
501
107
125
640
086
9956
1W
DS
8589
504
2179
533
701
506
926
740
987
5970
4W
DS
9592
003
9178
135
101
007
026
443
585
7972
7W
DS
10
591
404
2174
631
601
105
723
442
482
6957
0W
DS
11
593
403
6177
131
301
506
726
439
188
5967
6W
DS
12
588
103
8176
128
100
505
525
141
583
4952
1W
DS
13
577
003
8176
533
500
807
228
140
384
8952
0W
DS
14
586
004
7179
735
300
706
827
842
984
6968
5W
DS
15
588
104
2180
629
400
505
924
937
993
0964
5W
DS
16
579
603
9178
536
501
308
228
836
087
1959
9W
DS
17
580
103
9177
631
500
907
327
039
488
9956
6W
DS
mea
n588
104
2177
631
901
006
525
940
686
9962
8
sd
(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(07
8)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 793
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
rato
Spil
laC
rsquo)
1552
105
4177
247
401
914
38
735
578
9951
1W
DS
2557
305
7179
845
701
512
640
136
581
5960
6W
DS
3595
004
4173
724
302
003
117
652
877
8950
7W
DS
4575
704
2179
433
001
406
627
043
083
6953
7W
DS
5599
904
0178
826
401
304
421
841
688
4966
5W
DS
6591
103
8177
826
601
105
022
443
888
8960
2W
DS
7565
304
5180
939
501
410
532
535
791
8962
1W
DS
8597
606
9180
826
501
604
821
546
684
6970
7W
DS
9571
805
6179
939
801
109
932
240
883
6964
7W
DS
10
588
603
7176
527
601
104
721
042
487
7953
3W
DS
11
559
404
9180
544
501
812
339
435
878
6957
2W
DS
12
594
704
0181
328
301
705
522
144
785
6967
9W
DS
13
611
103
7187
016
900
802
419
938
195
9975
8W
DS
14
599
204
4181
128
601
404
620
844
986
6971
6W
DS
15
601
204
4177
328
302
004
722
446
385
5972
1W
DS
16
595
104
5176
428
801
504
722
744
884
3962
8W
DS
17
603
704
1177
825
101
503
520
348
181
2965
3W
DS
18
558
704
5179
647
401
813
139
836
879
0960
7W
DS
19
589
602
8178
830
901
606
622
436
091
8960
5W
DS
20
553
606
3178
647
401
913
840
136
978
0956
6W
DS
21
579
004
0175
739
000
708
328
338
286
7959
9W
DS
mea
n582
804
6179
033
401
507
427
341
484
8962
1
sd
(1
87)
(01
0)
(02
7)
(09
2)
(00
4)
(03
9)
(08
0)
(04
9)
(05
0)
(07
0)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
794 S M Davies and others
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)
1575
202
7194
219
701
101
016
374
766
9951
8W
DS
2575
802
9194
523
902
201
520
273
564
5959
0W
DS
3574
301
4205
219
101
100
416
481
266
1965
2W
DS
4575
500
7206
018
002
000
415
181
669
3968
6W
DS
5580
000
9208
018
601
300
515
883
367
1975
5W
DS
6571
001
0206
016
101
600
515
078
967
1957
2W
DS
7577
501
1201
117
101
500
620
675
655
4950
5W
DS
8573
700
9212
717
101
900
815
187
564
2973
9W
DS
9580
301
3208
715
801
400
824
81
754
1968
1W
DS
10
574
400
6211
18
402
00
516
480
567
8971
6W
DS
11
577
200
7214
212
501
200
829
879
247
962
6W
DS
12
572
200
9211
217
301
501
15
980
465
9966
3W
DS
13
571
800
7210
417
402
201
16
184
467
2971
2W
DS
14
567
300
9208
916
901
400
917
383
262
5959
3W
DS
15
568
600
8205
918
202
101
414
682
666
6960
8W
DS
16
572
501
1211
318
202
01
215
884
364
5970
9W
DS
17
572
901
2212
916
502
101
215
883
667
2973
4W
DS
18
573
01
4211
716
301
801
416
83
365
5970
4W
DS
19
569
201
1207
418
602
101
414
982
964
961
6W
DS
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
3)
(04
2)
(01
3)
(00
1)
(00
2)
(01
)(0
39)
(01
1)
(02
5)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
References
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Hughen K A Overpeck J T Peterson L C amp Trumbore S 1996 Rapid climate changes inthe tropical Atlantic region during the last deglaciation Nature 380 5153
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Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
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European tephrochronological framework for Termination 1 799
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Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
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Rose N L Golding P N E amp Battarbee R W 1996 Selective concentration and enumerationof tephra shards from lake sediment cores Holocene 6 243246
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Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 801
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Turney C S M 1998 Extraction of rhyolitic ash from minerogenic lake sediments J Paleolim-nol 19 199206
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Turney C S M Harkness D D amp Lowe J J 1997 The use of microtephra horizons tocorrelate Lateglacial lake sediments successions in Scotland J Quat Sci 12 525531
Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
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Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
Vezzoli L 1991 Tephra layers in Bannock Basin (eastern Mediterranean) Mar Geol 1002134
von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
Walker M J C Bjorck S Lowe J J Cwynar L C Johnsen S Knudsen K-L WohlfarthB amp INTIMATE Group 1999 Isotopic events in the GRIP ice core a stratotype for the LatePleistocene Quat Sci Rev 18 11431150
Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
Phil Trans R Soc Lond A (2002)
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802 S M Davies and others
Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
Phil Trans R Soc Lond A (2002)
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790 S M Davies and others
-44
-40
-36
-32
cale
ndar
yea
rs B
P
8000
9000
10 0
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11 0
00
12 0
00
13 0
00
14 0
00
15 0
00
16 0
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17 0
00
18 0
00
14C age (BP)
VA
SA
Un
Un
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BF
Hol
ocen
eG
S-1
GI-
1aG
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GI-
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Saks
unar
vatn
Houmlg
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3574
radiocarbon dated European tephra horizons
Cho
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Kili
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Pom
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-44
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800
600
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GISP2 volcanicsulphate conc (ppb)
1000
Nea
polit
an Y
ello
w T
uff
GISP2 18O (permil) dGRIP 18O (permil) d
Figure 8 For description see opposite
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 791
ferent times through a comparison of radiocarbon dates obtained from marine andterrestrial horizons in which the same tephra has been detected (see for exampleAustin et al 1995 Bondevik et al 2001 Haregidason et al 2000) Tephrostratigraphymay provide an independent test of suggestions that some of the climatic changesduring the Last Termination were time-transgressive as illustrated for some appar-ently contrasting climatic trends in Iceland Britain and NW Russia (Lowe 2001) Ofparticular importance as far as establishing `leadsrsquo and `lagsrsquo in climatic changes isconcerned are the tephra records from the Greenland ice cores The discovery of theVedde and Saksunarvatn ashes in the GRIP record (Gronvold et al 1995) alreadyprovides a basis for making direct comparisons between marine terrestrial and ice-core records It is a matter of some urgency that the incidence of tephra depositsin the Greenland ice cores be more fully explored in the hope that this will lead tothe recognition of additional time-parallel links between the ice-core records on theone hand and oceanic and terrestrial records on the other An investigation of thenew NordGRIP record for this purpose is currently in progress (S M Davies 2002unpublished data)
Finally a fuller and more reshy ned tephrostratigraphical scheme for Europe will alsohave other applications It will provide an important database for those investigatingthe timing and frequency of volcanic eruptions in Europe during the past 20 000 yror so as well as of the geochemical evolution of the dinoterent volcanic centres overthat period A fuller record of the distribution of micro-tephras may also provideinformation on atmospheric circulation patterns during the dispersal and depositionperiods as well as on the nature and altitude of the eruption columns which mayin turn provide inferences about magma viscosity
This paper is a contribution to the INTIMATE project of the INQUA Palaeoclimate Com-mission and the work is supported by a Leverhulme Trust Research project (grant allocationnumber F07537C) entitled Testing hypotheses of rapid climate change using tephrochronol-ogyrsquo SMDrsquo s contribution was completed during possession of a NERC PhD studentship(GT 0499ES162) We are extremely grateful to Dr Peter G Hill for his assistance withthe EPMA analyses at the Tephrochronology Analytical Unit University of Edinburgh We alsothank Dr G Mastrolorenzo (Vesuvius Observatory) and Miss G Swindle for assistance duringthe macreld investigations in Naples Thanks are also expressed to two anonymous reviewers forcomments on an earlier draft
Appendix A
Table 2 shows the major oxide concentrations of NYT glass shards from Procidaand Prato Spilla `Crsquo and of the Mercato Tephra from the Naples area (see x 4 forsite context) All oxides are shown as weight and total iron is expressed as FeO
Figure 8 Radiocarbon calibration curve for Termination 1 and the Early Holocene compared with theGRIP macr 18 O event stratigraphy the GRIP ss08c and GISP2 macr 18 O records (wwwngdcnoaagov) andknown tephra horizons from this period The shaded areas represent the cooler climatic episodes andare labelled with the Greenland stratotype terminology (Bjorck et al 1998) Where radiocarbon agesare reported in table 1 as a range the mean is given here Abbreviations for GRIP horizons are asfollows Un unknown (approximate positions are given (S Johnsen 2001 personal communication))SA Saksunarvatn Ash VA Vedde Ash BF Black Feather Sulphate concentrations from the GISP2record are also shown (Zielinski et al 1996) Open circles denote radiocarbon calibration data fromLake Suigetsu (Kitagawa amp van der Plicht 2000) Filled circles denote radiocarbon calibration data fromCariaco Basin assuming a marine reservoir age of 420 14 C yr (Hughen et al 1998)
Phil Trans R Soc Lond A (2002)
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792 S M Davies and others
Tab
le2
Majo
roxi
de
con
cen
trati
on
sof
NY
Tgl
ass
shard
sfr
om
Pro
cida
an
dP
rato
Spil
laC
rsquoan
dof
the
Mer
cato
Tep
hra
from
the
Naple
sare
a(s
eex4
for
site
con
text
)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
roci
da)
1584
204
0177
634
201
106
828
635
197
5969
1W
DS
2598
603
9178
027
101
204
924
244
583
4965
8W
DS
3586
604
5173
631
100
805
924
342
183
0951
9W
DS
4583
903
9177
933
000
906
924
540
486
9958
3W
DS
5605
106
8179
126
901
204
923
243
086
1976
4W
DS
6591
704
5177
332
801
006
425
740
887
8968
0W
DS
7581
804
1178
031
501
107
125
640
086
9956
1W
DS
8589
504
2179
533
701
506
926
740
987
5970
4W
DS
9592
003
9178
135
101
007
026
443
585
7972
7W
DS
10
591
404
2174
631
601
105
723
442
482
6957
0W
DS
11
593
403
6177
131
301
506
726
439
188
5967
6W
DS
12
588
103
8176
128
100
505
525
141
583
4952
1W
DS
13
577
003
8176
533
500
807
228
140
384
8952
0W
DS
14
586
004
7179
735
300
706
827
842
984
6968
5W
DS
15
588
104
2180
629
400
505
924
937
993
0964
5W
DS
16
579
603
9178
536
501
308
228
836
087
1959
9W
DS
17
580
103
9177
631
500
907
327
039
488
9956
6W
DS
mea
n588
104
2177
631
901
006
525
940
686
9962
8
sd
(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(07
8)
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 793
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
rato
Spil
laC
rsquo)
1552
105
4177
247
401
914
38
735
578
9951
1W
DS
2557
305
7179
845
701
512
640
136
581
5960
6W
DS
3595
004
4173
724
302
003
117
652
877
8950
7W
DS
4575
704
2179
433
001
406
627
043
083
6953
7W
DS
5599
904
0178
826
401
304
421
841
688
4966
5W
DS
6591
103
8177
826
601
105
022
443
888
8960
2W
DS
7565
304
5180
939
501
410
532
535
791
8962
1W
DS
8597
606
9180
826
501
604
821
546
684
6970
7W
DS
9571
805
6179
939
801
109
932
240
883
6964
7W
DS
10
588
603
7176
527
601
104
721
042
487
7953
3W
DS
11
559
404
9180
544
501
812
339
435
878
6957
2W
DS
12
594
704
0181
328
301
705
522
144
785
6967
9W
DS
13
611
103
7187
016
900
802
419
938
195
9975
8W
DS
14
599
204
4181
128
601
404
620
844
986
6971
6W
DS
15
601
204
4177
328
302
004
722
446
385
5972
1W
DS
16
595
104
5176
428
801
504
722
744
884
3962
8W
DS
17
603
704
1177
825
101
503
520
348
181
2965
3W
DS
18
558
704
5179
647
401
813
139
836
879
0960
7W
DS
19
589
602
8178
830
901
606
622
436
091
8960
5W
DS
20
553
606
3178
647
401
913
840
136
978
0956
6W
DS
21
579
004
0175
739
000
708
328
338
286
7959
9W
DS
mea
n582
804
6179
033
401
507
427
341
484
8962
1
sd
(1
87)
(01
0)
(02
7)
(09
2)
(00
4)
(03
9)
(08
0)
(04
9)
(05
0)
(07
0)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
794 S M Davies and others
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)
1575
202
7194
219
701
101
016
374
766
9951
8W
DS
2575
802
9194
523
902
201
520
273
564
5959
0W
DS
3574
301
4205
219
101
100
416
481
266
1965
2W
DS
4575
500
7206
018
002
000
415
181
669
3968
6W
DS
5580
000
9208
018
601
300
515
883
367
1975
5W
DS
6571
001
0206
016
101
600
515
078
967
1957
2W
DS
7577
501
1201
117
101
500
620
675
655
4950
5W
DS
8573
700
9212
717
101
900
815
187
564
2973
9W
DS
9580
301
3208
715
801
400
824
81
754
1968
1W
DS
10
574
400
6211
18
402
00
516
480
567
8971
6W
DS
11
577
200
7214
212
501
200
829
879
247
962
6W
DS
12
572
200
9211
217
301
501
15
980
465
9966
3W
DS
13
571
800
7210
417
402
201
16
184
467
2971
2W
DS
14
567
300
9208
916
901
400
917
383
262
5959
3W
DS
15
568
600
8205
918
202
101
414
682
666
6960
8W
DS
16
572
501
1211
318
202
01
215
884
364
5970
9W
DS
17
572
901
2212
916
502
101
215
883
667
2973
4W
DS
18
573
01
4211
716
301
801
416
83
365
5970
4W
DS
19
569
201
1207
418
602
101
414
982
964
961
6W
DS
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
3)
(04
2)
(01
3)
(00
1)
(00
2)
(01
)(0
39)
(01
1)
(02
5)
Phil Trans R Soc Lond A (2002)
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796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
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Di Vito M A Isaia R Orsi G Southon J de Vita S Drsquo Antonio M Pappalardo L ampPiochi M 1999 Volcanism and deformation since 12 000 years at the Campi Flegrei caldera(Italy) J Volcanol Geophys Res 91 221246
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Dugmore A J amp Newton A J 1998 Holocene tephra layers in the Faroe Islands Frodskaparrit46 191204
Eastwood A J Pearce N J G Westgate J A Perkins W T Lamb H F amp RobertsN 1999 Geochemistry of Santorini tephra in lake sediments from southwest Turkey GlobalPlanet Change 21 1729
Eirpara sup3 ksson J Knudsen K L Hadeg idason H amp Henriksen P 2000 Lateglacial and Holocenepalaeoceanography of the North Icelandic shelf J Quat Sci 15 2342
Etlicher B Janssen C R Juvignparae E amp Van Leeuwen J F N 1987 Le Haut Forez (MassifCentral France) aprmicroes le Plparaeniglaciaire Wurmien environnement et tparaephra du volcan de LaNugmicroere Bull Ass Fr Etud Quat 4 229239
Frezzotti M amp Narcisi B 1996 Late Quaternary Tephra derived paleosols in central Italyrsquo scarbonate Apennine range stratigraphical and paleoclimatological implications Quat Int3436 147153
Friedrich M Kromer B Spurk M Hofmann J amp Kaiser K F 1999 Paleoenvironment andradiocarbon calibration as derived from LateglacialEarly Holocene tree-ring chronologiesQuat Int 61 2739
Froggatt P C 1992 Standardisation of the chemical analysis of tephra deposits Report of theICCT working group Quat Int 1314 9396
Gronvold K Oskarsson N Johnsen S J Clausen H B Hammer C U Bond G amp Bard E1995 Ash layers from Iceland in the GRIP ice core correlated with oceanic and land sedimentsEarth Planet Sci Lett 135 149155
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
798 S M Davies and others
Hadeg idason H Eirpara sup3 ksson J amp van Kreveld S 2000 The tephrochronology of Iceland and theNorth Atlantic region during the Middle and Late Quaternary a review J Quat Sci 15322
Hoek W Z amp Bohncke S J P 2001 Oxygen isotope wiggle matching as a tool for synchronisingice-core and terrestrial records over Termination 1 Quat Sci Rev 20 12511264
Hughen K A Overpeck J T Peterson L C amp Trumbore S 1996 Rapid climate changes inthe tropical Atlantic region during the last deglaciation Nature 380 5153
Hughen K A Overpeck J T amp Lehman J 1998 A new 14 C calibration data set for the LastDeglaciation Radiocarbon 39 483494
Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
Hunt J B amp Hill P G 1996 An inter-laboratory comparison of the electron probe microanalysisof glass geochemistry Quat Int 3436 229241
Hunt J B amp Hill P G 2001 Tephrological implications of beam sizesample size ereg ects inelectron microprobe analysis of glass shards J Quat Sci 16 105117
Hunt J B Fannin N G T Hill P G amp Peacock J D 1995 The tephrochronology andradiocarbon dating of North Atlantic Late Quaternary sediments an example from the StKilda Basin In The tectonics sedimentation and palaeoceanography of the North Atlanticregion (ed R A Scrutton M S Stoker G B Shimmield amp A W Tudhope) vol 90pp 227248 Geological Society of London Special Publication
Hunt J B Clift P D Lacasse C Vallier T L amp Werner R 1998 Standardisation ofelectron probe microanalysis of glass geochemistry In Proc ODP Scientimacrc Results vol 152pp 8591 College Station TX Ocean Drilling Program
Jakobsson S P 1979 Outline of the petrology of Iceland Jokull 29 5773
Juvignparae E 1987 Deux retombparaees volcaniques tardiglaciaires dans le Cparaezallier (Massif CentralFrance) Bull Ass Fr Etud Quat 13 37
Juvignparae E 1993 Contribution microa la tparaephrostratigraphie du Quaternaire et son application microa lagparaeomorphologie Mparaem Serv Explicat Cartes Gparaeol Min Belg 36 166
Juvignparae E amp Gewelt M 1987 La Narse drsquo Ampoix comme tparaephrostratotype dans la Chasup3 ne desPuys mparaeridionale (France) Bull Ass Fr Etud Quat 29 3749
Juvignparae E Kozarski S amp Nowaczyk B 1995 The occurrence of Laacher See Tephra in Pomera-nia NW Poland Boreas 24 225231
Juvignparae E Bastin B Delibrias G Evin J Gewelt M Gilot E amp Streel M 1996 Acomprehensive pollen and tephra based chronostratigraphic model for the Lateglacial andHolocene period in the French Massif Central Quat Int 3436 113120
Keller J 1980 The island of Vulcano Rend Soc It Mineral Petrolog 36 369414
Keller J Ryan W B F Ninkovich D amp Altherr R 1978 Explosive volcanic activity in theMediterranean over the past 200 000 years as recorded in deep sea sediments Geol Soc AmBull 89 591604
Kitagawa H amp van der Plicht J 2000 Atmospheric radiocarbon calibration beyond 11 900 calBP from Lake Suigetsu laminated sediments Radiocarbon 42 369380
Kvamme T Mangerud J Furnes H amp Ruddiman W F 1989 Geochemistry of Pleistoceneash zones in cores from the North Atlantic Norsk Geol Tids 69 251272
Lacasse C Sigurdsson H Johannesson H Paterne M amp Carey S 1995 Source of Ash zone 1in the North Atlantic Bull Volcanol 57 1832
Langone L Asioli A Corregiari A amp Trincardi F 1996 Age depth modelling through theLate-Quaternary deposits of the central Adriatic Basin In Palaeoenvironmental analysis ofItalian crater lake and Adriatic sediments (ed F Oldmacreld amp P Guilizzoni) vol 55 pp 177196 Memorie dellrsquo Instituto Italiano di Idrobiologia
Larsen G 2000 Holocene volcanism in Iceland and tephrochronology as a tool in volcanologyIn Iceland 2000 modern processes and past environments Keele University UK
Phil Trans R Soc Lond A (2002)
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Litt T amp Stebich M 1999 Bio- and chronostratigraphy of the Lateglacial in the Eifel regionGermany Quat Int 61 516
Litt T Brauer A Goslar T Merkt J Balaga K Muller H Ralska-Jasiewiczowa MStebich M amp Negendank J F W 2001 Correlation and synchronisation of Lateglacialcontinental sequences in northern Central Europe based on annually laminated lacustrinesediments Quat Sci Rev 20 12331249
Long D amp Morton A C 1987 An ash fall within the Loch Lomond stadial J Quat Sci 297101
Lotter A F Eicher U Siegenthaler U amp Birks H J B 1992 Lateglacial climatic oscillationsas recorded in Swiss lake sediments J Quat Sci 7 187204
Lowe J J 1992 Lateglacial and Early Holocene lake sediments from the Northern ApenninesItaly|pollen stratigraphy and radiocarbon dating Boreas 21 193208
Lowe J J 2001 Abrupt climatic changes in Europe during the last glacialinterglacial tran-sition the potential for testing hypotheses on the synchroneity of climatic events usingtephrochronology Global Planet Change 603 7384
Lowe J J amp Turney C S M 1997 Vedde Ash layer discovered in a small lake basin on theScottish mainland J Geol Soc Lond 154 605612
Lowe J J amp Walker M J C 2000 Radiocarbon dating the last glacialinterglacial transition(ca 14914 C ka BP) in terrestrial and marine records the need for new quality assuranceprotocols Radiocarbon 42 5368
Lowe J J amp Watson C 1993 Lateglacial and Early Holocene pollen stratigraphy of the northernApennines Italy Quat Sci Rev 12 727738
Lowe J J Birks H H Brooks S J Coope G R Harkness D D Mayle F E SheldrickC Turney C S M amp Walker M J C 1999 The chronology of palaeoenvironmental changesduring the Last GlacialHolocene transition towards an event stratigraphy for the BritishIsles J Geol Soc Lond 156 397410
Lowe J J Hoek W Z amp INTIMATE group 2001 Inter-regional correlation of palaeoclimaticrecords for the Last GlacialInterglacial transition a protocol for improved precision recom-mended by the INTIMATE project group Quat Sci Rev 20 11751187
Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
Mangerud J Lie S E Furnes H Kristiansen I L amp Liquest mo L 1984 A Younger Dryas ashbed in western Norway and its possible correlation with tephra beds from the Norwegian Seaand North Atlantic Quat Res 21 85104
Mangerud J Furnes H amp Jparaohansen J 1986 A 9000 year-old ash bed on the Faroe IslandsQuat Res 26 262265
Martini J 1970 Recherche de retombparaees volcaniques dans le sud-est de la France et la Suisseoccidentale Arch Sci 23 641674
Martini J amp Duret J J 1965 Note preliminaire sur la presence drsquo un niveau de cendres vol-caniques dans des sparaediments post-glaciaires des environs de Genmicroeve Arch Sci 18 587588
Mayewski P A Meeker L D Twickler M S Whitlow S Yang Q Lyons W B amp Pren-tice M 1997 Major features and forcing of high latitudes Northern Hemisphere atmosphericcirculation using a 110 000 year long glaciochemical series J Geophys Res 102 345365
Merkt J Muller H Knabe W Muller P amp Weiser T 1993 The Early Holocene Saksunarvatntephra found in lake sediments in NW Germany Boreas 22 93100
Narcisi B 1993 Segnalazione di un livello piroclastico di provenienza etnea nellrsquo area del Fucino(Italia Centrale) Quaternario 6 8792
Narcisi B 1996 Tephrochronology of a Late Quaternary lacustrine record from the Monticchiomaar (Vulture volcano southern Italy) Quat Sci Rev 15 155165
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Newton A J amp Dugmore A J 1993 Tephrochronology of Core C from Lago Grande di Mon-ticchio In Paleolimnology of European Maar Lakes (ed J F W Negendank amp B Zolitschka)Lecture Notes in Earth Science vol 49 333348 Springer
Oldmacreld F Appleby P G amp Thompson R 1980 Palaeoecological studies of lakes in theHighlands of Papua New Guinea J Ecol 68 457477
Orsi G Drsquo Antonio M de Vita S amp Gallo G 1992 The Neapolitan Yellow Tureg a large mag-nitude trachytic phreatoplinian eruption eruptive dynamics magma withdrawal and calderacollapse J Volcanol Geotherm Res 53 275287
Paterne M Guichard F Labeyrie J Gillot P Y amp Duplessy J C 1986 Tyrrhenian Seatephrochronology of the oxygen isotope record for the past 60 000 years Mar Geol 72259285
Paterne M Guichard F amp Labeyrie J 1988 Explosive activity of the south Italian volca-noes during the past 80 000 years as determined by marine tephrochronology J VolcanolGeotherm Res 34 153172
Paterne M Labeyrie J Guichard F Mazaud A amp Maitre F 1990 Fluctuations of the Cam-panian explosive volcanic activity (south Italy) during the past 190 000 years as determinedby marine tephrochronology Earth Planet Sci Lett 98 166174
Pawse A Beske-Diehl S amp Marshall S A 1998 Use of magnetic hysteresis properties andelectron spin resonance spectroscopy for the identimacrcation of volcanic ash a preliminary studyGeophys J Int 132 712720
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Pearce N J G Westgate J A Perkins W T Eastwood W J amp Shane P 1999 Theapplication of laser ablation ICP-MS to the analysis of volcanic glass shards from tephradeposits bulk glass and single shard analysis Global Planet Change 21 151171
Pilcher J R amp Hall V A 1992 Towards a tephrochronology for the Holocene of the north ofIreland Holocene 2 255259
Ponel P amp Lowe J J 1992 Coleopteran pollen and radiocarbon evidence from the Prato Spillarsquo Drsquo succession N Italy C R Acad Sci Paris Sparaer II 315 14251431
Rose N L Golding P N E amp Battarbee R W 1996 Selective concentration and enumerationof tephra shards from lake sediment cores Holocene 6 243246
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Ruddiman W amp McIntyre A 1981 The North Atlantic Ocean during the last deglaciationPalaeogeogr Palaeoclimatol Palaeoecol 35 145214
Santacroce R 1987 Somma Vesuvius Quad Ric Sci 114 252
Sarna-Wojcicki A 2000 Tephrochronology In Quaternary geochronology methods and applica-tions (ed J S Noller J M Sowers amp W R Lettis) AGU Reference shelf vol 4 pp 357377Washington DC American Geophysical Union
Sejrup H P Sjiquest holm J Furnes H Beyer I Eide L Jansen E amp Mangerud J 1989Quaternary tephrochronology on the Iceland Plateau north of Iceland J Quat Sci 4 109114
Sikes E L Samson C R Guilderson T P amp Howard W R 2000 Old radiocarbon agesin the southwest Pacimacrc Ocean during the last glacial period and deglaciation Nature 405555558
Stein R Nam S-I Grobe H amp Hubbersten H 1996 Late Quaternary glacial history andshort term ice rafted debris deg uctuations along the East Greenland continental marine In LateQuaternary palaeoceanography of the North Atlantic margins (ed J T Andrews W E NAustin H Bergsten amp A E Jennings) pp 135151 Geological Society London SpecialPublication
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on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 801
Stuiver M amp Grootes P M 2000 GISP2 oxygen isotope ratios Quat Res 53 277284
Stuiver M Reimer P J Bard E Beck J W Burr G S Hughen K A Kromer BMcCormac G Van der Plicht J amp Spurk M 1998 INTCAL 98 radiocarbon age calibration24 0000 cal BP Radiocarbon 40 10411083
Sweatman T R amp Long J V P 1969 Quantitative electron microprobe analysis of rock formingminerals J Petrol 7 332379
Turney C S M 1998 Extraction of rhyolitic ash from minerogenic lake sediments J Paleolim-nol 19 199206
Turney C S M amp Lowe J J 2001 Tephrochronology In Tracking environmental changes inlake sediments physical and chemical techniques (ed W M Last amp J P Smol) DordrechtKluwer Academic
Turney C S M Harkness D D amp Lowe J J 1997 The use of microtephra horizons tocorrelate Lateglacial lake sediments successions in Scotland J Quat Sci 12 525531
Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
van den Bogaard P amp Schmincke H 1985 A widespread isochronous Late Quaternary tephralayer in central and northern Europe Geol Soc Am Bull 96 15541571
van den Bogaard B Dordeg er W Sandgren P amp Schmincke H-U 1994 Correlating theHolocene records Icelandic tephra found in Schleswig-Holstein (northern Germany) Natur-wissenschaften 81 554556
Vernet G amp Raynal J-P 2001 Tephrostratigraphy of the Limagne revisited Implications forLateglacial and Holocene Prehistory In Tephras chronology archaeology (ed E Juvignparae ampJ-P Raynal) pp 111116 Dossiers de lrsquo ArchparaeoLogis no 1 France
Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
Vezzoli L 1991 Tephra layers in Bannock Basin (eastern Mediterranean) Mar Geol 1002134
von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
Walker M J C Bjorck S Lowe J J Cwynar L C Johnsen S Knudsen K-L WohlfarthB amp INTIMATE Group 1999 Isotopic events in the GRIP ice core a stratotype for the LatePleistocene Quat Sci Rev 18 11431150
Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
802 S M Davies and others
Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 791
ferent times through a comparison of radiocarbon dates obtained from marine andterrestrial horizons in which the same tephra has been detected (see for exampleAustin et al 1995 Bondevik et al 2001 Haregidason et al 2000) Tephrostratigraphymay provide an independent test of suggestions that some of the climatic changesduring the Last Termination were time-transgressive as illustrated for some appar-ently contrasting climatic trends in Iceland Britain and NW Russia (Lowe 2001) Ofparticular importance as far as establishing `leadsrsquo and `lagsrsquo in climatic changes isconcerned are the tephra records from the Greenland ice cores The discovery of theVedde and Saksunarvatn ashes in the GRIP record (Gronvold et al 1995) alreadyprovides a basis for making direct comparisons between marine terrestrial and ice-core records It is a matter of some urgency that the incidence of tephra depositsin the Greenland ice cores be more fully explored in the hope that this will lead tothe recognition of additional time-parallel links between the ice-core records on theone hand and oceanic and terrestrial records on the other An investigation of thenew NordGRIP record for this purpose is currently in progress (S M Davies 2002unpublished data)
Finally a fuller and more reshy ned tephrostratigraphical scheme for Europe will alsohave other applications It will provide an important database for those investigatingthe timing and frequency of volcanic eruptions in Europe during the past 20 000 yror so as well as of the geochemical evolution of the dinoterent volcanic centres overthat period A fuller record of the distribution of micro-tephras may also provideinformation on atmospheric circulation patterns during the dispersal and depositionperiods as well as on the nature and altitude of the eruption columns which mayin turn provide inferences about magma viscosity
This paper is a contribution to the INTIMATE project of the INQUA Palaeoclimate Com-mission and the work is supported by a Leverhulme Trust Research project (grant allocationnumber F07537C) entitled Testing hypotheses of rapid climate change using tephrochronol-ogyrsquo SMDrsquo s contribution was completed during possession of a NERC PhD studentship(GT 0499ES162) We are extremely grateful to Dr Peter G Hill for his assistance withthe EPMA analyses at the Tephrochronology Analytical Unit University of Edinburgh We alsothank Dr G Mastrolorenzo (Vesuvius Observatory) and Miss G Swindle for assistance duringthe macreld investigations in Naples Thanks are also expressed to two anonymous reviewers forcomments on an earlier draft
Appendix A
Table 2 shows the major oxide concentrations of NYT glass shards from Procidaand Prato Spilla `Crsquo and of the Mercato Tephra from the Naples area (see x 4 forsite context) All oxides are shown as weight and total iron is expressed as FeO
Figure 8 Radiocarbon calibration curve for Termination 1 and the Early Holocene compared with theGRIP macr 18 O event stratigraphy the GRIP ss08c and GISP2 macr 18 O records (wwwngdcnoaagov) andknown tephra horizons from this period The shaded areas represent the cooler climatic episodes andare labelled with the Greenland stratotype terminology (Bjorck et al 1998) Where radiocarbon agesare reported in table 1 as a range the mean is given here Abbreviations for GRIP horizons are asfollows Un unknown (approximate positions are given (S Johnsen 2001 personal communication))SA Saksunarvatn Ash VA Vedde Ash BF Black Feather Sulphate concentrations from the GISP2record are also shown (Zielinski et al 1996) Open circles denote radiocarbon calibration data fromLake Suigetsu (Kitagawa amp van der Plicht 2000) Filled circles denote radiocarbon calibration data fromCariaco Basin assuming a marine reservoir age of 420 14 C yr (Hughen et al 1998)
Phil Trans R Soc Lond A (2002)
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792 S M Davies and others
Tab
le2
Majo
roxi
de
con
cen
trati
on
sof
NY
Tgl
ass
shard
sfr
om
Pro
cida
an
dP
rato
Spil
laC
rsquoan
dof
the
Mer
cato
Tep
hra
from
the
Naple
sare
a(s
eex4
for
site
con
text
)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
roci
da)
1584
204
0177
634
201
106
828
635
197
5969
1W
DS
2598
603
9178
027
101
204
924
244
583
4965
8W
DS
3586
604
5173
631
100
805
924
342
183
0951
9W
DS
4583
903
9177
933
000
906
924
540
486
9958
3W
DS
5605
106
8179
126
901
204
923
243
086
1976
4W
DS
6591
704
5177
332
801
006
425
740
887
8968
0W
DS
7581
804
1178
031
501
107
125
640
086
9956
1W
DS
8589
504
2179
533
701
506
926
740
987
5970
4W
DS
9592
003
9178
135
101
007
026
443
585
7972
7W
DS
10
591
404
2174
631
601
105
723
442
482
6957
0W
DS
11
593
403
6177
131
301
506
726
439
188
5967
6W
DS
12
588
103
8176
128
100
505
525
141
583
4952
1W
DS
13
577
003
8176
533
500
807
228
140
384
8952
0W
DS
14
586
004
7179
735
300
706
827
842
984
6968
5W
DS
15
588
104
2180
629
400
505
924
937
993
0964
5W
DS
16
579
603
9178
536
501
308
228
836
087
1959
9W
DS
17
580
103
9177
631
500
907
327
039
488
9956
6W
DS
mea
n588
104
2177
631
901
006
525
940
686
9962
8
sd
(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(07
8)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 793
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
rato
Spil
laC
rsquo)
1552
105
4177
247
401
914
38
735
578
9951
1W
DS
2557
305
7179
845
701
512
640
136
581
5960
6W
DS
3595
004
4173
724
302
003
117
652
877
8950
7W
DS
4575
704
2179
433
001
406
627
043
083
6953
7W
DS
5599
904
0178
826
401
304
421
841
688
4966
5W
DS
6591
103
8177
826
601
105
022
443
888
8960
2W
DS
7565
304
5180
939
501
410
532
535
791
8962
1W
DS
8597
606
9180
826
501
604
821
546
684
6970
7W
DS
9571
805
6179
939
801
109
932
240
883
6964
7W
DS
10
588
603
7176
527
601
104
721
042
487
7953
3W
DS
11
559
404
9180
544
501
812
339
435
878
6957
2W
DS
12
594
704
0181
328
301
705
522
144
785
6967
9W
DS
13
611
103
7187
016
900
802
419
938
195
9975
8W
DS
14
599
204
4181
128
601
404
620
844
986
6971
6W
DS
15
601
204
4177
328
302
004
722
446
385
5972
1W
DS
16
595
104
5176
428
801
504
722
744
884
3962
8W
DS
17
603
704
1177
825
101
503
520
348
181
2965
3W
DS
18
558
704
5179
647
401
813
139
836
879
0960
7W
DS
19
589
602
8178
830
901
606
622
436
091
8960
5W
DS
20
553
606
3178
647
401
913
840
136
978
0956
6W
DS
21
579
004
0175
739
000
708
328
338
286
7959
9W
DS
mea
n582
804
6179
033
401
507
427
341
484
8962
1
sd
(1
87)
(01
0)
(02
7)
(09
2)
(00
4)
(03
9)
(08
0)
(04
9)
(05
0)
(07
0)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
794 S M Davies and others
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)
1575
202
7194
219
701
101
016
374
766
9951
8W
DS
2575
802
9194
523
902
201
520
273
564
5959
0W
DS
3574
301
4205
219
101
100
416
481
266
1965
2W
DS
4575
500
7206
018
002
000
415
181
669
3968
6W
DS
5580
000
9208
018
601
300
515
883
367
1975
5W
DS
6571
001
0206
016
101
600
515
078
967
1957
2W
DS
7577
501
1201
117
101
500
620
675
655
4950
5W
DS
8573
700
9212
717
101
900
815
187
564
2973
9W
DS
9580
301
3208
715
801
400
824
81
754
1968
1W
DS
10
574
400
6211
18
402
00
516
480
567
8971
6W
DS
11
577
200
7214
212
501
200
829
879
247
962
6W
DS
12
572
200
9211
217
301
501
15
980
465
9966
3W
DS
13
571
800
7210
417
402
201
16
184
467
2971
2W
DS
14
567
300
9208
916
901
400
917
383
262
5959
3W
DS
15
568
600
8205
918
202
101
414
682
666
6960
8W
DS
16
572
501
1211
318
202
01
215
884
364
5970
9W
DS
17
572
901
2212
916
502
101
215
883
667
2973
4W
DS
18
573
01
4211
716
301
801
416
83
365
5970
4W
DS
19
569
201
1207
418
602
101
414
982
964
961
6W
DS
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
3)
(04
2)
(01
3)
(00
1)
(00
2)
(01
)(0
39)
(01
1)
(02
5)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
References
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Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
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Phil Trans R Soc Lond A (2002)
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802 S M Davies and others
Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
792 S M Davies and others
Tab
le2
Majo
roxi
de
con
cen
trati
on
sof
NY
Tgl
ass
shard
sfr
om
Pro
cida
an
dP
rato
Spil
laC
rsquoan
dof
the
Mer
cato
Tep
hra
from
the
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sare
a(s
eex4
for
site
con
text
)
nS
iO2
TiO
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MgO
CaO
Na
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K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
roci
da)
1584
204
0177
634
201
106
828
635
197
5969
1W
DS
2598
603
9178
027
101
204
924
244
583
4965
8W
DS
3586
604
5173
631
100
805
924
342
183
0951
9W
DS
4583
903
9177
933
000
906
924
540
486
9958
3W
DS
5605
106
8179
126
901
204
923
243
086
1976
4W
DS
6591
704
5177
332
801
006
425
740
887
8968
0W
DS
7581
804
1178
031
501
107
125
640
086
9956
1W
DS
8589
504
2179
533
701
506
926
740
987
5970
4W
DS
9592
003
9178
135
101
007
026
443
585
7972
7W
DS
10
591
404
2174
631
601
105
723
442
482
6957
0W
DS
11
593
403
6177
131
301
506
726
439
188
5967
6W
DS
12
588
103
8176
128
100
505
525
141
583
4952
1W
DS
13
577
003
8176
533
500
807
228
140
384
8952
0W
DS
14
586
004
7179
735
300
706
827
842
984
6968
5W
DS
15
588
104
2180
629
400
505
924
937
993
0964
5W
DS
16
579
603
9178
536
501
308
228
836
087
1959
9W
DS
17
580
103
9177
631
500
907
327
039
488
9956
6W
DS
mea
n588
104
2177
631
901
006
525
940
686
9962
8
sd
(0
71)
(00
7)
(01
8)
(02
8)
(00
3)
(00
9)
(01
8)
(02
5)
(03
8)
(07
8)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 793
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
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Yel
low
Tu
reg(P
rato
Spil
laC
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1552
105
4177
247
401
914
38
735
578
9951
1W
DS
2557
305
7179
845
701
512
640
136
581
5960
6W
DS
3595
004
4173
724
302
003
117
652
877
8950
7W
DS
4575
704
2179
433
001
406
627
043
083
6953
7W
DS
5599
904
0178
826
401
304
421
841
688
4966
5W
DS
6591
103
8177
826
601
105
022
443
888
8960
2W
DS
7565
304
5180
939
501
410
532
535
791
8962
1W
DS
8597
606
9180
826
501
604
821
546
684
6970
7W
DS
9571
805
6179
939
801
109
932
240
883
6964
7W
DS
10
588
603
7176
527
601
104
721
042
487
7953
3W
DS
11
559
404
9180
544
501
812
339
435
878
6957
2W
DS
12
594
704
0181
328
301
705
522
144
785
6967
9W
DS
13
611
103
7187
016
900
802
419
938
195
9975
8W
DS
14
599
204
4181
128
601
404
620
844
986
6971
6W
DS
15
601
204
4177
328
302
004
722
446
385
5972
1W
DS
16
595
104
5176
428
801
504
722
744
884
3962
8W
DS
17
603
704
1177
825
101
503
520
348
181
2965
3W
DS
18
558
704
5179
647
401
813
139
836
879
0960
7W
DS
19
589
602
8178
830
901
606
622
436
091
8960
5W
DS
20
553
606
3178
647
401
913
840
136
978
0956
6W
DS
21
579
004
0175
739
000
708
328
338
286
7959
9W
DS
mea
n582
804
6179
033
401
507
427
341
484
8962
1
sd
(1
87)
(01
0)
(02
7)
(09
2)
(00
4)
(03
9)
(08
0)
(04
9)
(05
0)
(07
0)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
794 S M Davies and others
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)
1575
202
7194
219
701
101
016
374
766
9951
8W
DS
2575
802
9194
523
902
201
520
273
564
5959
0W
DS
3574
301
4205
219
101
100
416
481
266
1965
2W
DS
4575
500
7206
018
002
000
415
181
669
3968
6W
DS
5580
000
9208
018
601
300
515
883
367
1975
5W
DS
6571
001
0206
016
101
600
515
078
967
1957
2W
DS
7577
501
1201
117
101
500
620
675
655
4950
5W
DS
8573
700
9212
717
101
900
815
187
564
2973
9W
DS
9580
301
3208
715
801
400
824
81
754
1968
1W
DS
10
574
400
6211
18
402
00
516
480
567
8971
6W
DS
11
577
200
7214
212
501
200
829
879
247
962
6W
DS
12
572
200
9211
217
301
501
15
980
465
9966
3W
DS
13
571
800
7210
417
402
201
16
184
467
2971
2W
DS
14
567
300
9208
916
901
400
917
383
262
5959
3W
DS
15
568
600
8205
918
202
101
414
682
666
6960
8W
DS
16
572
501
1211
318
202
01
215
884
364
5970
9W
DS
17
572
901
2212
916
502
101
215
883
667
2973
4W
DS
18
573
01
4211
716
301
801
416
83
365
5970
4W
DS
19
569
201
1207
418
602
101
414
982
964
961
6W
DS
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
3)
(04
2)
(01
3)
(00
1)
(00
2)
(01
)(0
39)
(01
1)
(02
5)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
References
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Bjorck J amp Wastegordm ard S 1999 Climate oscillations and tephrochronology in eastern middleSweden during the last glacialinterglacial transition J Quat Sci 14 399410
Bjorck S Ingparaolfsson O Hadeg idason H Hallsdparaottir M amp Anderson N J 1992 Lake Torfadals-vatn a high resolution record of the North Atlantic Ash zone I and the last glacialinterglacialenvironmental changes in Iceland Boreas 21 1522
Bjorck S Walker M J C Cwynar L Johnsen S Knudsen K Lowe J J Wohlfarth Bamp INTIMATE members 1998 An event stratigraphy for the Last Termination in the NorthAtlantic region based on the Greenland ice-core record a proposal by the INTIMATE groupJ Quat Sci 13 283292
Bjorck S Lowe J J amp Walker M J C 2001 Integration of ice core marine and terrestrialrecords of Termination 1 from the North Atlantic region Quat Sci Rev 20 11691274
Bond G C Mandeville C amp Horeg man S 2001 Were rhyolitic glasses in the Vedde Ash andin the North Atlanticrsquo s Ash zone 1 produced by the same volcanic eruption Quat Sci Rev20 11891199
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European tephrochronological framework for Termination 1 797
Bondevik S Mangerud J amp Gulliksen S 2001 The marine 1 4 C age of the Vedde Ash Bedalong the west coast of Norway J Quat Sci 16 37
Bossuet G Richard H Magny M amp Rossy M 1997 A new occurrence of Laacher See Tephrain the central Jura (France) The mire of Le Lautrey C R Acad Sci Paris Sparaer IIa 3254348
Brauer A Endres C Gunter C Litt T Stebich M amp Negendank J F W 1999 Highresolution sediment and vegetation responses to Younger Dryas climate change in varved lakesediments from Meerfelder Maar Germany Quat Sci Rev 18 321329
Brooks S J Mayle F E amp Lowe J J 1997 Chironomid based Lateglacial climatic recon-struction for southeast Scotland J Quat Sci 12 161167
Calanchi N Dinelli E Gasparatto G amp Lucchini F 1996 Etnean tephra layer in Albanolake and Adriatic Sea cores new macrndings of Y-1 layer in the central Mediterranean area ActaVulcan 8 713
Coope G R Lemdahl G Lowe J J amp Walkling A 1998 Temperature gradients in northernEurope during the last glacialHolocene transition (149 ka BP) interpreted from coleopternassemblages J Quat Sci 13 419433
Dansgaard W (and 10 others) 1993 Evidence for general instability of past climate from a250 kyr ice-core record Nature 363 218220
Davies S M Turney C S M amp Lowe J J 2001 Identimacrcation and signimacrcance of a visiblebasalt-rich Vedde Ash layer in a Late-glacial sequence on the Isle of Skye Inner HebridesScotland J Quat Sci 16 99104
Delibrias G Di Paola G M Rosi M amp Santacroce R 1979 La storia eruttiva del complessovulcanico Somma Vesuvio ricostruita dalle successini piroclastiche del Monte Somma RendSoc It Mineral Petrolog 35 411438
Di Vito M A Isaia R Orsi G Southon J de Vita S Drsquo Antonio M Pappalardo L ampPiochi M 1999 Volcanism and deformation since 12 000 years at the Campi Flegrei caldera(Italy) J Volcanol Geophys Res 91 221246
Dugmore A J amp Newton A J 1992 Thin tephra layers in peat revealed by X-radiography JArchaeol Sci 19 163170
Dugmore A J amp Newton A J 1998 Holocene tephra layers in the Faroe Islands Frodskaparrit46 191204
Eastwood A J Pearce N J G Westgate J A Perkins W T Lamb H F amp RobertsN 1999 Geochemistry of Santorini tephra in lake sediments from southwest Turkey GlobalPlanet Change 21 1729
Eirpara sup3 ksson J Knudsen K L Hadeg idason H amp Henriksen P 2000 Lateglacial and Holocenepalaeoceanography of the North Icelandic shelf J Quat Sci 15 2342
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Frezzotti M amp Narcisi B 1996 Late Quaternary Tephra derived paleosols in central Italyrsquo scarbonate Apennine range stratigraphical and paleoclimatological implications Quat Int3436 147153
Friedrich M Kromer B Spurk M Hofmann J amp Kaiser K F 1999 Paleoenvironment andradiocarbon calibration as derived from LateglacialEarly Holocene tree-ring chronologiesQuat Int 61 2739
Froggatt P C 1992 Standardisation of the chemical analysis of tephra deposits Report of theICCT working group Quat Int 1314 9396
Gronvold K Oskarsson N Johnsen S J Clausen H B Hammer C U Bond G amp Bard E1995 Ash layers from Iceland in the GRIP ice core correlated with oceanic and land sedimentsEarth Planet Sci Lett 135 149155
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798 S M Davies and others
Hadeg idason H Eirpara sup3 ksson J amp van Kreveld S 2000 The tephrochronology of Iceland and theNorth Atlantic region during the Middle and Late Quaternary a review J Quat Sci 15322
Hoek W Z amp Bohncke S J P 2001 Oxygen isotope wiggle matching as a tool for synchronisingice-core and terrestrial records over Termination 1 Quat Sci Rev 20 12511264
Hughen K A Overpeck J T Peterson L C amp Trumbore S 1996 Rapid climate changes inthe tropical Atlantic region during the last deglaciation Nature 380 5153
Hughen K A Overpeck J T amp Lehman J 1998 A new 14 C calibration data set for the LastDeglaciation Radiocarbon 39 483494
Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
Hunt J B amp Hill P G 1996 An inter-laboratory comparison of the electron probe microanalysisof glass geochemistry Quat Int 3436 229241
Hunt J B amp Hill P G 2001 Tephrological implications of beam sizesample size ereg ects inelectron microprobe analysis of glass shards J Quat Sci 16 105117
Hunt J B Fannin N G T Hill P G amp Peacock J D 1995 The tephrochronology andradiocarbon dating of North Atlantic Late Quaternary sediments an example from the StKilda Basin In The tectonics sedimentation and palaeoceanography of the North Atlanticregion (ed R A Scrutton M S Stoker G B Shimmield amp A W Tudhope) vol 90pp 227248 Geological Society of London Special Publication
Hunt J B Clift P D Lacasse C Vallier T L amp Werner R 1998 Standardisation ofelectron probe microanalysis of glass geochemistry In Proc ODP Scientimacrc Results vol 152pp 8591 College Station TX Ocean Drilling Program
Jakobsson S P 1979 Outline of the petrology of Iceland Jokull 29 5773
Juvignparae E 1987 Deux retombparaees volcaniques tardiglaciaires dans le Cparaezallier (Massif CentralFrance) Bull Ass Fr Etud Quat 13 37
Juvignparae E 1993 Contribution microa la tparaephrostratigraphie du Quaternaire et son application microa lagparaeomorphologie Mparaem Serv Explicat Cartes Gparaeol Min Belg 36 166
Juvignparae E amp Gewelt M 1987 La Narse drsquo Ampoix comme tparaephrostratotype dans la Chasup3 ne desPuys mparaeridionale (France) Bull Ass Fr Etud Quat 29 3749
Juvignparae E Kozarski S amp Nowaczyk B 1995 The occurrence of Laacher See Tephra in Pomera-nia NW Poland Boreas 24 225231
Juvignparae E Bastin B Delibrias G Evin J Gewelt M Gilot E amp Streel M 1996 Acomprehensive pollen and tephra based chronostratigraphic model for the Lateglacial andHolocene period in the French Massif Central Quat Int 3436 113120
Keller J 1980 The island of Vulcano Rend Soc It Mineral Petrolog 36 369414
Keller J Ryan W B F Ninkovich D amp Altherr R 1978 Explosive volcanic activity in theMediterranean over the past 200 000 years as recorded in deep sea sediments Geol Soc AmBull 89 591604
Kitagawa H amp van der Plicht J 2000 Atmospheric radiocarbon calibration beyond 11 900 calBP from Lake Suigetsu laminated sediments Radiocarbon 42 369380
Kvamme T Mangerud J Furnes H amp Ruddiman W F 1989 Geochemistry of Pleistoceneash zones in cores from the North Atlantic Norsk Geol Tids 69 251272
Lacasse C Sigurdsson H Johannesson H Paterne M amp Carey S 1995 Source of Ash zone 1in the North Atlantic Bull Volcanol 57 1832
Langone L Asioli A Corregiari A amp Trincardi F 1996 Age depth modelling through theLate-Quaternary deposits of the central Adriatic Basin In Palaeoenvironmental analysis ofItalian crater lake and Adriatic sediments (ed F Oldmacreld amp P Guilizzoni) vol 55 pp 177196 Memorie dellrsquo Instituto Italiano di Idrobiologia
Larsen G 2000 Holocene volcanism in Iceland and tephrochronology as a tool in volcanologyIn Iceland 2000 modern processes and past environments Keele University UK
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 799
Litt T amp Stebich M 1999 Bio- and chronostratigraphy of the Lateglacial in the Eifel regionGermany Quat Int 61 516
Litt T Brauer A Goslar T Merkt J Balaga K Muller H Ralska-Jasiewiczowa MStebich M amp Negendank J F W 2001 Correlation and synchronisation of Lateglacialcontinental sequences in northern Central Europe based on annually laminated lacustrinesediments Quat Sci Rev 20 12331249
Long D amp Morton A C 1987 An ash fall within the Loch Lomond stadial J Quat Sci 297101
Lotter A F Eicher U Siegenthaler U amp Birks H J B 1992 Lateglacial climatic oscillationsas recorded in Swiss lake sediments J Quat Sci 7 187204
Lowe J J 1992 Lateglacial and Early Holocene lake sediments from the Northern ApenninesItaly|pollen stratigraphy and radiocarbon dating Boreas 21 193208
Lowe J J 2001 Abrupt climatic changes in Europe during the last glacialinterglacial tran-sition the potential for testing hypotheses on the synchroneity of climatic events usingtephrochronology Global Planet Change 603 7384
Lowe J J amp Turney C S M 1997 Vedde Ash layer discovered in a small lake basin on theScottish mainland J Geol Soc Lond 154 605612
Lowe J J amp Walker M J C 2000 Radiocarbon dating the last glacialinterglacial transition(ca 14914 C ka BP) in terrestrial and marine records the need for new quality assuranceprotocols Radiocarbon 42 5368
Lowe J J amp Watson C 1993 Lateglacial and Early Holocene pollen stratigraphy of the northernApennines Italy Quat Sci Rev 12 727738
Lowe J J Birks H H Brooks S J Coope G R Harkness D D Mayle F E SheldrickC Turney C S M amp Walker M J C 1999 The chronology of palaeoenvironmental changesduring the Last GlacialHolocene transition towards an event stratigraphy for the BritishIsles J Geol Soc Lond 156 397410
Lowe J J Hoek W Z amp INTIMATE group 2001 Inter-regional correlation of palaeoclimaticrecords for the Last GlacialInterglacial transition a protocol for improved precision recom-mended by the INTIMATE project group Quat Sci Rev 20 11751187
Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
Mangerud J Lie S E Furnes H Kristiansen I L amp Liquest mo L 1984 A Younger Dryas ashbed in western Norway and its possible correlation with tephra beds from the Norwegian Seaand North Atlantic Quat Res 21 85104
Mangerud J Furnes H amp Jparaohansen J 1986 A 9000 year-old ash bed on the Faroe IslandsQuat Res 26 262265
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Mayewski P A Meeker L D Twickler M S Whitlow S Yang Q Lyons W B amp Pren-tice M 1997 Major features and forcing of high latitudes Northern Hemisphere atmosphericcirculation using a 110 000 year long glaciochemical series J Geophys Res 102 345365
Merkt J Muller H Knabe W Muller P amp Weiser T 1993 The Early Holocene Saksunarvatntephra found in lake sediments in NW Germany Boreas 22 93100
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Phil Trans R Soc Lond A (2002)
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800 S M Davies and others
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Oldmacreld F Appleby P G amp Thompson R 1980 Palaeoecological studies of lakes in theHighlands of Papua New Guinea J Ecol 68 457477
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Paterne M Labeyrie J Guichard F Mazaud A amp Maitre F 1990 Fluctuations of the Cam-panian explosive volcanic activity (south Italy) during the past 190 000 years as determinedby marine tephrochronology Earth Planet Sci Lett 98 166174
Pawse A Beske-Diehl S amp Marshall S A 1998 Use of magnetic hysteresis properties andelectron spin resonance spectroscopy for the identimacrcation of volcanic ash a preliminary studyGeophys J Int 132 712720
Pearce N J G Westgate J A amp Perkins W T 1996 Developments in the analysis of singleglass shards in volcanic deposits by laser ablation ICP-MS quantitative and single internalstandard multi-element methods Quat Int 3436 213227
Pearce N J G Westgate J A Perkins W T Eastwood W J amp Shane P 1999 Theapplication of laser ablation ICP-MS to the analysis of volcanic glass shards from tephradeposits bulk glass and single shard analysis Global Planet Change 21 151171
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Rose N L Golding P N E amp Battarbee R W 1996 Selective concentration and enumerationof tephra shards from lake sediment cores Holocene 6 243246
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Santacroce R 1987 Somma Vesuvius Quad Ric Sci 114 252
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Sejrup H P Sjiquest holm J Furnes H Beyer I Eide L Jansen E amp Mangerud J 1989Quaternary tephrochronology on the Iceland Plateau north of Iceland J Quat Sci 4 109114
Sikes E L Samson C R Guilderson T P amp Howard W R 2000 Old radiocarbon agesin the southwest Pacimacrc Ocean during the last glacial period and deglaciation Nature 405555558
Stein R Nam S-I Grobe H amp Hubbersten H 1996 Late Quaternary glacial history andshort term ice rafted debris deg uctuations along the East Greenland continental marine In LateQuaternary palaeoceanography of the North Atlantic margins (ed J T Andrews W E NAustin H Bergsten amp A E Jennings) pp 135151 Geological Society London SpecialPublication
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European tephrochronological framework for Termination 1 801
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Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
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van den Bogaard B Dordeg er W Sandgren P amp Schmincke H-U 1994 Correlating theHolocene records Icelandic tephra found in Schleswig-Holstein (northern Germany) Natur-wissenschaften 81 554556
Vernet G amp Raynal J-P 2001 Tephrostratigraphy of the Limagne revisited Implications forLateglacial and Holocene Prehistory In Tephras chronology archaeology (ed E Juvignparae ampJ-P Raynal) pp 111116 Dossiers de lrsquo ArchparaeoLogis no 1 France
Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
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Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
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Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
Phil Trans R Soc Lond A (2002)
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802 S M Davies and others
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Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
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Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 793
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Nea
poli
tan
Yel
low
Tu
reg(P
rato
Spil
laC
rsquo)
1552
105
4177
247
401
914
38
735
578
9951
1W
DS
2557
305
7179
845
701
512
640
136
581
5960
6W
DS
3595
004
4173
724
302
003
117
652
877
8950
7W
DS
4575
704
2179
433
001
406
627
043
083
6953
7W
DS
5599
904
0178
826
401
304
421
841
688
4966
5W
DS
6591
103
8177
826
601
105
022
443
888
8960
2W
DS
7565
304
5180
939
501
410
532
535
791
8962
1W
DS
8597
606
9180
826
501
604
821
546
684
6970
7W
DS
9571
805
6179
939
801
109
932
240
883
6964
7W
DS
10
588
603
7176
527
601
104
721
042
487
7953
3W
DS
11
559
404
9180
544
501
812
339
435
878
6957
2W
DS
12
594
704
0181
328
301
705
522
144
785
6967
9W
DS
13
611
103
7187
016
900
802
419
938
195
9975
8W
DS
14
599
204
4181
128
601
404
620
844
986
6971
6W
DS
15
601
204
4177
328
302
004
722
446
385
5972
1W
DS
16
595
104
5176
428
801
504
722
744
884
3962
8W
DS
17
603
704
1177
825
101
503
520
348
181
2965
3W
DS
18
558
704
5179
647
401
813
139
836
879
0960
7W
DS
19
589
602
8178
830
901
606
622
436
091
8960
5W
DS
20
553
606
3178
647
401
913
840
136
978
0956
6W
DS
21
579
004
0175
739
000
708
328
338
286
7959
9W
DS
mea
n582
804
6179
033
401
507
427
341
484
8962
1
sd
(1
87)
(01
0)
(02
7)
(09
2)
(00
4)
(03
9)
(08
0)
(04
9)
(05
0)
(07
0)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
794 S M Davies and others
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)
1575
202
7194
219
701
101
016
374
766
9951
8W
DS
2575
802
9194
523
902
201
520
273
564
5959
0W
DS
3574
301
4205
219
101
100
416
481
266
1965
2W
DS
4575
500
7206
018
002
000
415
181
669
3968
6W
DS
5580
000
9208
018
601
300
515
883
367
1975
5W
DS
6571
001
0206
016
101
600
515
078
967
1957
2W
DS
7577
501
1201
117
101
500
620
675
655
4950
5W
DS
8573
700
9212
717
101
900
815
187
564
2973
9W
DS
9580
301
3208
715
801
400
824
81
754
1968
1W
DS
10
574
400
6211
18
402
00
516
480
567
8971
6W
DS
11
577
200
7214
212
501
200
829
879
247
962
6W
DS
12
572
200
9211
217
301
501
15
980
465
9966
3W
DS
13
571
800
7210
417
402
201
16
184
467
2971
2W
DS
14
567
300
9208
916
901
400
917
383
262
5959
3W
DS
15
568
600
8205
918
202
101
414
682
666
6960
8W
DS
16
572
501
1211
318
202
01
215
884
364
5970
9W
DS
17
572
901
2212
916
502
101
215
883
667
2973
4W
DS
18
573
01
4211
716
301
801
416
83
365
5970
4W
DS
19
569
201
1207
418
602
101
414
982
964
961
6W
DS
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
3)
(04
2)
(01
3)
(00
1)
(00
2)
(01
)(0
39)
(01
1)
(02
5)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
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Allen J R M (and 14 others) 1999 Rapid environmental changes in southern Europe duringthe last glacial period Nature 400 740743
Alley R B (and 10 others) 1993 Abrupt increase in Greenland snow accumulation at the endof the Younger Dryas Nature 362 527529
Andronico D Calderoni G Cioni R Sbrana A Sulpizio R amp Santacroce R 1995 Geo-logical map of Somma Vesuvius volcano Period Mineral 64 7788
Atkinson T C Brireg a K R amp Coope G R 1987 Seasonal temperature in Britain during thepast 22 000 years reconstructed using beetle remains Nature 325 587592
Austin W E N amp Kroon D 1996 Lateglacial sedimentology foraminifera and stable isotopestratigraphy of the Hebridean Continental Shelf northwest Scotland In Late Quaternarypalaeoceanography of the North Atlantic margins (ed J T Andrews W E N Austin HBergsten amp A E Jennings) vol 111 pp 187213 Geological Society of London SpecialPublication
Austin W E N Bard E Hunt J B Kroon D amp Peacock J D 1995 The 14 C age ofthe Vedde Ash implications for Younger Dryas marine reservoir corrections Radiocarbon 375362
Barker D S 1983 Igneous rocks Englewood Clireg s NJ Prentice-Hall
Bennet K D Boreham S amp Sharp M J 1992 Holocene history of environment vegetationand human settlement on Catta Ness Shetland J Ecol 80 241273
Birks H H Gulliksen S Hadeg idason H Mangerud J amp Possnert G 1996 New radiocarbondates for the Vedde Ash and the Saksunarvatn Ash from western Norway Quat Res 45119127
Bjorck J amp Wastegordm ard S 1999 Climate oscillations and tephrochronology in eastern middleSweden during the last glacialinterglacial transition J Quat Sci 14 399410
Bjorck S Ingparaolfsson O Hadeg idason H Hallsdparaottir M amp Anderson N J 1992 Lake Torfadals-vatn a high resolution record of the North Atlantic Ash zone I and the last glacialinterglacialenvironmental changes in Iceland Boreas 21 1522
Bjorck S Walker M J C Cwynar L Johnsen S Knudsen K Lowe J J Wohlfarth Bamp INTIMATE members 1998 An event stratigraphy for the Last Termination in the NorthAtlantic region based on the Greenland ice-core record a proposal by the INTIMATE groupJ Quat Sci 13 283292
Bjorck S Lowe J J amp Walker M J C 2001 Integration of ice core marine and terrestrialrecords of Termination 1 from the North Atlantic region Quat Sci Rev 20 11691274
Bond G C Mandeville C amp Horeg man S 2001 Were rhyolitic glasses in the Vedde Ash andin the North Atlanticrsquo s Ash zone 1 produced by the same volcanic eruption Quat Sci Rev20 11891199
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Bossuet G Richard H Magny M amp Rossy M 1997 A new occurrence of Laacher See Tephrain the central Jura (France) The mire of Le Lautrey C R Acad Sci Paris Sparaer IIa 3254348
Brauer A Endres C Gunter C Litt T Stebich M amp Negendank J F W 1999 Highresolution sediment and vegetation responses to Younger Dryas climate change in varved lakesediments from Meerfelder Maar Germany Quat Sci Rev 18 321329
Brooks S J Mayle F E amp Lowe J J 1997 Chironomid based Lateglacial climatic recon-struction for southeast Scotland J Quat Sci 12 161167
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Coope G R Lemdahl G Lowe J J amp Walkling A 1998 Temperature gradients in northernEurope during the last glacialHolocene transition (149 ka BP) interpreted from coleopternassemblages J Quat Sci 13 419433
Dansgaard W (and 10 others) 1993 Evidence for general instability of past climate from a250 kyr ice-core record Nature 363 218220
Davies S M Turney C S M amp Lowe J J 2001 Identimacrcation and signimacrcance of a visiblebasalt-rich Vedde Ash layer in a Late-glacial sequence on the Isle of Skye Inner HebridesScotland J Quat Sci 16 99104
Delibrias G Di Paola G M Rosi M amp Santacroce R 1979 La storia eruttiva del complessovulcanico Somma Vesuvio ricostruita dalle successini piroclastiche del Monte Somma RendSoc It Mineral Petrolog 35 411438
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Friedrich M Kromer B Spurk M Hofmann J amp Kaiser K F 1999 Paleoenvironment andradiocarbon calibration as derived from LateglacialEarly Holocene tree-ring chronologiesQuat Int 61 2739
Froggatt P C 1992 Standardisation of the chemical analysis of tephra deposits Report of theICCT working group Quat Int 1314 9396
Gronvold K Oskarsson N Johnsen S J Clausen H B Hammer C U Bond G amp Bard E1995 Ash layers from Iceland in the GRIP ice core correlated with oceanic and land sedimentsEarth Planet Sci Lett 135 149155
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798 S M Davies and others
Hadeg idason H Eirpara sup3 ksson J amp van Kreveld S 2000 The tephrochronology of Iceland and theNorth Atlantic region during the Middle and Late Quaternary a review J Quat Sci 15322
Hoek W Z amp Bohncke S J P 2001 Oxygen isotope wiggle matching as a tool for synchronisingice-core and terrestrial records over Termination 1 Quat Sci Rev 20 12511264
Hughen K A Overpeck J T Peterson L C amp Trumbore S 1996 Rapid climate changes inthe tropical Atlantic region during the last deglaciation Nature 380 5153
Hughen K A Overpeck J T amp Lehman J 1998 A new 14 C calibration data set for the LastDeglaciation Radiocarbon 39 483494
Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
Hunt J B amp Hill P G 1996 An inter-laboratory comparison of the electron probe microanalysisof glass geochemistry Quat Int 3436 229241
Hunt J B amp Hill P G 2001 Tephrological implications of beam sizesample size ereg ects inelectron microprobe analysis of glass shards J Quat Sci 16 105117
Hunt J B Fannin N G T Hill P G amp Peacock J D 1995 The tephrochronology andradiocarbon dating of North Atlantic Late Quaternary sediments an example from the StKilda Basin In The tectonics sedimentation and palaeoceanography of the North Atlanticregion (ed R A Scrutton M S Stoker G B Shimmield amp A W Tudhope) vol 90pp 227248 Geological Society of London Special Publication
Hunt J B Clift P D Lacasse C Vallier T L amp Werner R 1998 Standardisation ofelectron probe microanalysis of glass geochemistry In Proc ODP Scientimacrc Results vol 152pp 8591 College Station TX Ocean Drilling Program
Jakobsson S P 1979 Outline of the petrology of Iceland Jokull 29 5773
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Juvignparae E 1993 Contribution microa la tparaephrostratigraphie du Quaternaire et son application microa lagparaeomorphologie Mparaem Serv Explicat Cartes Gparaeol Min Belg 36 166
Juvignparae E amp Gewelt M 1987 La Narse drsquo Ampoix comme tparaephrostratotype dans la Chasup3 ne desPuys mparaeridionale (France) Bull Ass Fr Etud Quat 29 3749
Juvignparae E Kozarski S amp Nowaczyk B 1995 The occurrence of Laacher See Tephra in Pomera-nia NW Poland Boreas 24 225231
Juvignparae E Bastin B Delibrias G Evin J Gewelt M Gilot E amp Streel M 1996 Acomprehensive pollen and tephra based chronostratigraphic model for the Lateglacial andHolocene period in the French Massif Central Quat Int 3436 113120
Keller J 1980 The island of Vulcano Rend Soc It Mineral Petrolog 36 369414
Keller J Ryan W B F Ninkovich D amp Altherr R 1978 Explosive volcanic activity in theMediterranean over the past 200 000 years as recorded in deep sea sediments Geol Soc AmBull 89 591604
Kitagawa H amp van der Plicht J 2000 Atmospheric radiocarbon calibration beyond 11 900 calBP from Lake Suigetsu laminated sediments Radiocarbon 42 369380
Kvamme T Mangerud J Furnes H amp Ruddiman W F 1989 Geochemistry of Pleistoceneash zones in cores from the North Atlantic Norsk Geol Tids 69 251272
Lacasse C Sigurdsson H Johannesson H Paterne M amp Carey S 1995 Source of Ash zone 1in the North Atlantic Bull Volcanol 57 1832
Langone L Asioli A Corregiari A amp Trincardi F 1996 Age depth modelling through theLate-Quaternary deposits of the central Adriatic Basin In Palaeoenvironmental analysis ofItalian crater lake and Adriatic sediments (ed F Oldmacreld amp P Guilizzoni) vol 55 pp 177196 Memorie dellrsquo Instituto Italiano di Idrobiologia
Larsen G 2000 Holocene volcanism in Iceland and tephrochronology as a tool in volcanologyIn Iceland 2000 modern processes and past environments Keele University UK
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 799
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Litt T Brauer A Goslar T Merkt J Balaga K Muller H Ralska-Jasiewiczowa MStebich M amp Negendank J F W 2001 Correlation and synchronisation of Lateglacialcontinental sequences in northern Central Europe based on annually laminated lacustrinesediments Quat Sci Rev 20 12331249
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Lotter A F Eicher U Siegenthaler U amp Birks H J B 1992 Lateglacial climatic oscillationsas recorded in Swiss lake sediments J Quat Sci 7 187204
Lowe J J 1992 Lateglacial and Early Holocene lake sediments from the Northern ApenninesItaly|pollen stratigraphy and radiocarbon dating Boreas 21 193208
Lowe J J 2001 Abrupt climatic changes in Europe during the last glacialinterglacial tran-sition the potential for testing hypotheses on the synchroneity of climatic events usingtephrochronology Global Planet Change 603 7384
Lowe J J amp Turney C S M 1997 Vedde Ash layer discovered in a small lake basin on theScottish mainland J Geol Soc Lond 154 605612
Lowe J J amp Walker M J C 2000 Radiocarbon dating the last glacialinterglacial transition(ca 14914 C ka BP) in terrestrial and marine records the need for new quality assuranceprotocols Radiocarbon 42 5368
Lowe J J amp Watson C 1993 Lateglacial and Early Holocene pollen stratigraphy of the northernApennines Italy Quat Sci Rev 12 727738
Lowe J J Birks H H Brooks S J Coope G R Harkness D D Mayle F E SheldrickC Turney C S M amp Walker M J C 1999 The chronology of palaeoenvironmental changesduring the Last GlacialHolocene transition towards an event stratigraphy for the BritishIsles J Geol Soc Lond 156 397410
Lowe J J Hoek W Z amp INTIMATE group 2001 Inter-regional correlation of palaeoclimaticrecords for the Last GlacialInterglacial transition a protocol for improved precision recom-mended by the INTIMATE project group Quat Sci Rev 20 11751187
Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
Mangerud J Lie S E Furnes H Kristiansen I L amp Liquest mo L 1984 A Younger Dryas ashbed in western Norway and its possible correlation with tephra beds from the Norwegian Seaand North Atlantic Quat Res 21 85104
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Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 801
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Stuiver M Reimer P J Bard E Beck J W Burr G S Hughen K A Kromer BMcCormac G Van der Plicht J amp Spurk M 1998 INTCAL 98 radiocarbon age calibration24 0000 cal BP Radiocarbon 40 10411083
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Turney C S M 1998 Extraction of rhyolitic ash from minerogenic lake sediments J Paleolim-nol 19 199206
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Turney C S M Harkness D D amp Lowe J J 1997 The use of microtephra horizons tocorrelate Lateglacial lake sediments successions in Scotland J Quat Sci 12 525531
Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
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van den Bogaard B Dordeg er W Sandgren P amp Schmincke H-U 1994 Correlating theHolocene records Icelandic tephra found in Schleswig-Holstein (northern Germany) Natur-wissenschaften 81 554556
Vernet G amp Raynal J-P 2001 Tephrostratigraphy of the Limagne revisited Implications forLateglacial and Holocene Prehistory In Tephras chronology archaeology (ed E Juvignparae ampJ-P Raynal) pp 111116 Dossiers de lrsquo ArchparaeoLogis no 1 France
Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
Vezzoli L 1991 Tephra layers in Bannock Basin (eastern Mediterranean) Mar Geol 1002134
von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
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Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
802 S M Davies and others
Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
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Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
794 S M Davies and others
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)
1575
202
7194
219
701
101
016
374
766
9951
8W
DS
2575
802
9194
523
902
201
520
273
564
5959
0W
DS
3574
301
4205
219
101
100
416
481
266
1965
2W
DS
4575
500
7206
018
002
000
415
181
669
3968
6W
DS
5580
000
9208
018
601
300
515
883
367
1975
5W
DS
6571
001
0206
016
101
600
515
078
967
1957
2W
DS
7577
501
1201
117
101
500
620
675
655
4950
5W
DS
8573
700
9212
717
101
900
815
187
564
2973
9W
DS
9580
301
3208
715
801
400
824
81
754
1968
1W
DS
10
574
400
6211
18
402
00
516
480
567
8971
6W
DS
11
577
200
7214
212
501
200
829
879
247
962
6W
DS
12
572
200
9211
217
301
501
15
980
465
9966
3W
DS
13
571
800
7210
417
402
201
16
184
467
2971
2W
DS
14
567
300
9208
916
901
400
917
383
262
5959
3W
DS
15
568
600
8205
918
202
101
414
682
666
6960
8W
DS
16
572
501
1211
318
202
01
215
884
364
5970
9W
DS
17
572
901
2212
916
502
101
215
883
667
2973
4W
DS
18
573
01
4211
716
301
801
416
83
365
5970
4W
DS
19
569
201
1207
418
602
101
414
982
964
961
6W
DS
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
3)
(04
2)
(01
3)
(00
1)
(00
2)
(01
)(0
39)
(01
1)
(02
5)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
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Coope G R Lemdahl G Lowe J J amp Walkling A 1998 Temperature gradients in northernEurope during the last glacialHolocene transition (149 ka BP) interpreted from coleopternassemblages J Quat Sci 13 419433
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Davies S M Turney C S M amp Lowe J J 2001 Identimacrcation and signimacrcance of a visiblebasalt-rich Vedde Ash layer in a Late-glacial sequence on the Isle of Skye Inner HebridesScotland J Quat Sci 16 99104
Delibrias G Di Paola G M Rosi M amp Santacroce R 1979 La storia eruttiva del complessovulcanico Somma Vesuvio ricostruita dalle successini piroclastiche del Monte Somma RendSoc It Mineral Petrolog 35 411438
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Dugmore A J amp Newton A J 1998 Holocene tephra layers in the Faroe Islands Frodskaparrit46 191204
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Frezzotti M amp Narcisi B 1996 Late Quaternary Tephra derived paleosols in central Italyrsquo scarbonate Apennine range stratigraphical and paleoclimatological implications Quat Int3436 147153
Friedrich M Kromer B Spurk M Hofmann J amp Kaiser K F 1999 Paleoenvironment andradiocarbon calibration as derived from LateglacialEarly Holocene tree-ring chronologiesQuat Int 61 2739
Froggatt P C 1992 Standardisation of the chemical analysis of tephra deposits Report of theICCT working group Quat Int 1314 9396
Gronvold K Oskarsson N Johnsen S J Clausen H B Hammer C U Bond G amp Bard E1995 Ash layers from Iceland in the GRIP ice core correlated with oceanic and land sedimentsEarth Planet Sci Lett 135 149155
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
798 S M Davies and others
Hadeg idason H Eirpara sup3 ksson J amp van Kreveld S 2000 The tephrochronology of Iceland and theNorth Atlantic region during the Middle and Late Quaternary a review J Quat Sci 15322
Hoek W Z amp Bohncke S J P 2001 Oxygen isotope wiggle matching as a tool for synchronisingice-core and terrestrial records over Termination 1 Quat Sci Rev 20 12511264
Hughen K A Overpeck J T Peterson L C amp Trumbore S 1996 Rapid climate changes inthe tropical Atlantic region during the last deglaciation Nature 380 5153
Hughen K A Overpeck J T amp Lehman J 1998 A new 14 C calibration data set for the LastDeglaciation Radiocarbon 39 483494
Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
Hunt J B amp Hill P G 1996 An inter-laboratory comparison of the electron probe microanalysisof glass geochemistry Quat Int 3436 229241
Hunt J B amp Hill P G 2001 Tephrological implications of beam sizesample size ereg ects inelectron microprobe analysis of glass shards J Quat Sci 16 105117
Hunt J B Fannin N G T Hill P G amp Peacock J D 1995 The tephrochronology andradiocarbon dating of North Atlantic Late Quaternary sediments an example from the StKilda Basin In The tectonics sedimentation and palaeoceanography of the North Atlanticregion (ed R A Scrutton M S Stoker G B Shimmield amp A W Tudhope) vol 90pp 227248 Geological Society of London Special Publication
Hunt J B Clift P D Lacasse C Vallier T L amp Werner R 1998 Standardisation ofelectron probe microanalysis of glass geochemistry In Proc ODP Scientimacrc Results vol 152pp 8591 College Station TX Ocean Drilling Program
Jakobsson S P 1979 Outline of the petrology of Iceland Jokull 29 5773
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Juvignparae E 1993 Contribution microa la tparaephrostratigraphie du Quaternaire et son application microa lagparaeomorphologie Mparaem Serv Explicat Cartes Gparaeol Min Belg 36 166
Juvignparae E amp Gewelt M 1987 La Narse drsquo Ampoix comme tparaephrostratotype dans la Chasup3 ne desPuys mparaeridionale (France) Bull Ass Fr Etud Quat 29 3749
Juvignparae E Kozarski S amp Nowaczyk B 1995 The occurrence of Laacher See Tephra in Pomera-nia NW Poland Boreas 24 225231
Juvignparae E Bastin B Delibrias G Evin J Gewelt M Gilot E amp Streel M 1996 Acomprehensive pollen and tephra based chronostratigraphic model for the Lateglacial andHolocene period in the French Massif Central Quat Int 3436 113120
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Phil Trans R Soc Lond A (2002)
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European tephrochronological framework for Termination 1 799
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Litt T Brauer A Goslar T Merkt J Balaga K Muller H Ralska-Jasiewiczowa MStebich M amp Negendank J F W 2001 Correlation and synchronisation of Lateglacialcontinental sequences in northern Central Europe based on annually laminated lacustrinesediments Quat Sci Rev 20 12331249
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Lowe J J amp Turney C S M 1997 Vedde Ash layer discovered in a small lake basin on theScottish mainland J Geol Soc Lond 154 605612
Lowe J J amp Walker M J C 2000 Radiocarbon dating the last glacialinterglacial transition(ca 14914 C ka BP) in terrestrial and marine records the need for new quality assuranceprotocols Radiocarbon 42 5368
Lowe J J amp Watson C 1993 Lateglacial and Early Holocene pollen stratigraphy of the northernApennines Italy Quat Sci Rev 12 727738
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Lowe J J Hoek W Z amp INTIMATE group 2001 Inter-regional correlation of palaeoclimaticrecords for the Last GlacialInterglacial transition a protocol for improved precision recom-mended by the INTIMATE project group Quat Sci Rev 20 11751187
Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
Mangerud J Lie S E Furnes H Kristiansen I L amp Liquest mo L 1984 A Younger Dryas ashbed in western Norway and its possible correlation with tephra beds from the Norwegian Seaand North Atlantic Quat Res 21 85104
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Phil Trans R Soc Lond A (2002)
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800 S M Davies and others
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Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 801
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von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
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Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
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Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
802 S M Davies and others
Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
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Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
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Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 795
Tab
le2
(Con
t)
nS
iO2
TiO
2A
l 2O
3F
eOM
nO
MgO
CaO
Na
2O
K2O
tota
lE
PM
A
Mer
cato
Tep
hra
(Naple
s)(c
on
t)
20
567
600
9211
417
01
501
14
780
562
1956
7W
DS
21
573
801
4210
516
501
900
814
184
968
1972
WD
S
22
576
100
7208
814
501
200
921
79
856
5959
5W
DS
23
568
200
6209
916
801
800
915
784
664
8963
3W
DS
24
568
501
2204
817
01
901
215
286
466
5962
7W
DS
25
563
400
8208
016
201
500
614
386
862
0953
6W
DS
26
576
500
9208
716
801
700
718
282
462
6968
5W
DS
27
567
501
0211
217
401
800
713
189
265
4967
3W
DS
28
565
301
3209
817
102
000
816
484
565
1962
3W
DS
29
564
501
1207
716
801
900
515
787
764
9960
8W
DS
30
566
401
0204
517
001
801
014
582
664
1952
9W
DS
31
581
700
7210
015
201
900
517
885
460
1973
3W
DS
32
573
200
8203
517
801
600
914
585
165
0962
4W
DS
33
568
001
0208
217
202
000
714
588
061
4961
0W
DS
34
570
100
6210
216
401
600
715
388
165
7968
7W
DS
35
573
201
0209
916
801
601
013
289
964
2970
8W
DS
36
576
201
5207
816
201
900
717
384
460
9966
9W
DS
mea
n572
801
2206
817
501
700
816
682
564
963
8
sd
(0
26)
(00
3)
(04
2)
(01
3)
(00
1)
(00
2)
(01
)(0
39)
(01
1)
(02
5)
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
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Bossuet G Richard H Magny M amp Rossy M 1997 A new occurrence of Laacher See Tephrain the central Jura (France) The mire of Le Lautrey C R Acad Sci Paris Sparaer IIa 3254348
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Brooks S J Mayle F E amp Lowe J J 1997 Chironomid based Lateglacial climatic recon-struction for southeast Scotland J Quat Sci 12 161167
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Coope G R Lemdahl G Lowe J J amp Walkling A 1998 Temperature gradients in northernEurope during the last glacialHolocene transition (149 ka BP) interpreted from coleopternassemblages J Quat Sci 13 419433
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Davies S M Turney C S M amp Lowe J J 2001 Identimacrcation and signimacrcance of a visiblebasalt-rich Vedde Ash layer in a Late-glacial sequence on the Isle of Skye Inner HebridesScotland J Quat Sci 16 99104
Delibrias G Di Paola G M Rosi M amp Santacroce R 1979 La storia eruttiva del complessovulcanico Somma Vesuvio ricostruita dalle successini piroclastiche del Monte Somma RendSoc It Mineral Petrolog 35 411438
Di Vito M A Isaia R Orsi G Southon J de Vita S Drsquo Antonio M Pappalardo L ampPiochi M 1999 Volcanism and deformation since 12 000 years at the Campi Flegrei caldera(Italy) J Volcanol Geophys Res 91 221246
Dugmore A J amp Newton A J 1992 Thin tephra layers in peat revealed by X-radiography JArchaeol Sci 19 163170
Dugmore A J amp Newton A J 1998 Holocene tephra layers in the Faroe Islands Frodskaparrit46 191204
Eastwood A J Pearce N J G Westgate J A Perkins W T Lamb H F amp RobertsN 1999 Geochemistry of Santorini tephra in lake sediments from southwest Turkey GlobalPlanet Change 21 1729
Eirpara sup3 ksson J Knudsen K L Hadeg idason H amp Henriksen P 2000 Lateglacial and Holocenepalaeoceanography of the North Icelandic shelf J Quat Sci 15 2342
Etlicher B Janssen C R Juvignparae E amp Van Leeuwen J F N 1987 Le Haut Forez (MassifCentral France) aprmicroes le Plparaeniglaciaire Wurmien environnement et tparaephra du volcan de LaNugmicroere Bull Ass Fr Etud Quat 4 229239
Frezzotti M amp Narcisi B 1996 Late Quaternary Tephra derived paleosols in central Italyrsquo scarbonate Apennine range stratigraphical and paleoclimatological implications Quat Int3436 147153
Friedrich M Kromer B Spurk M Hofmann J amp Kaiser K F 1999 Paleoenvironment andradiocarbon calibration as derived from LateglacialEarly Holocene tree-ring chronologiesQuat Int 61 2739
Froggatt P C 1992 Standardisation of the chemical analysis of tephra deposits Report of theICCT working group Quat Int 1314 9396
Gronvold K Oskarsson N Johnsen S J Clausen H B Hammer C U Bond G amp Bard E1995 Ash layers from Iceland in the GRIP ice core correlated with oceanic and land sedimentsEarth Planet Sci Lett 135 149155
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
798 S M Davies and others
Hadeg idason H Eirpara sup3 ksson J amp van Kreveld S 2000 The tephrochronology of Iceland and theNorth Atlantic region during the Middle and Late Quaternary a review J Quat Sci 15322
Hoek W Z amp Bohncke S J P 2001 Oxygen isotope wiggle matching as a tool for synchronisingice-core and terrestrial records over Termination 1 Quat Sci Rev 20 12511264
Hughen K A Overpeck J T Peterson L C amp Trumbore S 1996 Rapid climate changes inthe tropical Atlantic region during the last deglaciation Nature 380 5153
Hughen K A Overpeck J T amp Lehman J 1998 A new 14 C calibration data set for the LastDeglaciation Radiocarbon 39 483494
Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
Hunt J B amp Hill P G 1996 An inter-laboratory comparison of the electron probe microanalysisof glass geochemistry Quat Int 3436 229241
Hunt J B amp Hill P G 2001 Tephrological implications of beam sizesample size ereg ects inelectron microprobe analysis of glass shards J Quat Sci 16 105117
Hunt J B Fannin N G T Hill P G amp Peacock J D 1995 The tephrochronology andradiocarbon dating of North Atlantic Late Quaternary sediments an example from the StKilda Basin In The tectonics sedimentation and palaeoceanography of the North Atlanticregion (ed R A Scrutton M S Stoker G B Shimmield amp A W Tudhope) vol 90pp 227248 Geological Society of London Special Publication
Hunt J B Clift P D Lacasse C Vallier T L amp Werner R 1998 Standardisation ofelectron probe microanalysis of glass geochemistry In Proc ODP Scientimacrc Results vol 152pp 8591 College Station TX Ocean Drilling Program
Jakobsson S P 1979 Outline of the petrology of Iceland Jokull 29 5773
Juvignparae E 1987 Deux retombparaees volcaniques tardiglaciaires dans le Cparaezallier (Massif CentralFrance) Bull Ass Fr Etud Quat 13 37
Juvignparae E 1993 Contribution microa la tparaephrostratigraphie du Quaternaire et son application microa lagparaeomorphologie Mparaem Serv Explicat Cartes Gparaeol Min Belg 36 166
Juvignparae E amp Gewelt M 1987 La Narse drsquo Ampoix comme tparaephrostratotype dans la Chasup3 ne desPuys mparaeridionale (France) Bull Ass Fr Etud Quat 29 3749
Juvignparae E Kozarski S amp Nowaczyk B 1995 The occurrence of Laacher See Tephra in Pomera-nia NW Poland Boreas 24 225231
Juvignparae E Bastin B Delibrias G Evin J Gewelt M Gilot E amp Streel M 1996 Acomprehensive pollen and tephra based chronostratigraphic model for the Lateglacial andHolocene period in the French Massif Central Quat Int 3436 113120
Keller J 1980 The island of Vulcano Rend Soc It Mineral Petrolog 36 369414
Keller J Ryan W B F Ninkovich D amp Altherr R 1978 Explosive volcanic activity in theMediterranean over the past 200 000 years as recorded in deep sea sediments Geol Soc AmBull 89 591604
Kitagawa H amp van der Plicht J 2000 Atmospheric radiocarbon calibration beyond 11 900 calBP from Lake Suigetsu laminated sediments Radiocarbon 42 369380
Kvamme T Mangerud J Furnes H amp Ruddiman W F 1989 Geochemistry of Pleistoceneash zones in cores from the North Atlantic Norsk Geol Tids 69 251272
Lacasse C Sigurdsson H Johannesson H Paterne M amp Carey S 1995 Source of Ash zone 1in the North Atlantic Bull Volcanol 57 1832
Langone L Asioli A Corregiari A amp Trincardi F 1996 Age depth modelling through theLate-Quaternary deposits of the central Adriatic Basin In Palaeoenvironmental analysis ofItalian crater lake and Adriatic sediments (ed F Oldmacreld amp P Guilizzoni) vol 55 pp 177196 Memorie dellrsquo Instituto Italiano di Idrobiologia
Larsen G 2000 Holocene volcanism in Iceland and tephrochronology as a tool in volcanologyIn Iceland 2000 modern processes and past environments Keele University UK
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 799
Litt T amp Stebich M 1999 Bio- and chronostratigraphy of the Lateglacial in the Eifel regionGermany Quat Int 61 516
Litt T Brauer A Goslar T Merkt J Balaga K Muller H Ralska-Jasiewiczowa MStebich M amp Negendank J F W 2001 Correlation and synchronisation of Lateglacialcontinental sequences in northern Central Europe based on annually laminated lacustrinesediments Quat Sci Rev 20 12331249
Long D amp Morton A C 1987 An ash fall within the Loch Lomond stadial J Quat Sci 297101
Lotter A F Eicher U Siegenthaler U amp Birks H J B 1992 Lateglacial climatic oscillationsas recorded in Swiss lake sediments J Quat Sci 7 187204
Lowe J J 1992 Lateglacial and Early Holocene lake sediments from the Northern ApenninesItaly|pollen stratigraphy and radiocarbon dating Boreas 21 193208
Lowe J J 2001 Abrupt climatic changes in Europe during the last glacialinterglacial tran-sition the potential for testing hypotheses on the synchroneity of climatic events usingtephrochronology Global Planet Change 603 7384
Lowe J J amp Turney C S M 1997 Vedde Ash layer discovered in a small lake basin on theScottish mainland J Geol Soc Lond 154 605612
Lowe J J amp Walker M J C 2000 Radiocarbon dating the last glacialinterglacial transition(ca 14914 C ka BP) in terrestrial and marine records the need for new quality assuranceprotocols Radiocarbon 42 5368
Lowe J J amp Watson C 1993 Lateglacial and Early Holocene pollen stratigraphy of the northernApennines Italy Quat Sci Rev 12 727738
Lowe J J Birks H H Brooks S J Coope G R Harkness D D Mayle F E SheldrickC Turney C S M amp Walker M J C 1999 The chronology of palaeoenvironmental changesduring the Last GlacialHolocene transition towards an event stratigraphy for the BritishIsles J Geol Soc Lond 156 397410
Lowe J J Hoek W Z amp INTIMATE group 2001 Inter-regional correlation of palaeoclimaticrecords for the Last GlacialInterglacial transition a protocol for improved precision recom-mended by the INTIMATE project group Quat Sci Rev 20 11751187
Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
Mangerud J Lie S E Furnes H Kristiansen I L amp Liquest mo L 1984 A Younger Dryas ashbed in western Norway and its possible correlation with tephra beds from the Norwegian Seaand North Atlantic Quat Res 21 85104
Mangerud J Furnes H amp Jparaohansen J 1986 A 9000 year-old ash bed on the Faroe IslandsQuat Res 26 262265
Martini J 1970 Recherche de retombparaees volcaniques dans le sud-est de la France et la Suisseoccidentale Arch Sci 23 641674
Martini J amp Duret J J 1965 Note preliminaire sur la presence drsquo un niveau de cendres vol-caniques dans des sparaediments post-glaciaires des environs de Genmicroeve Arch Sci 18 587588
Mayewski P A Meeker L D Twickler M S Whitlow S Yang Q Lyons W B amp Pren-tice M 1997 Major features and forcing of high latitudes Northern Hemisphere atmosphericcirculation using a 110 000 year long glaciochemical series J Geophys Res 102 345365
Merkt J Muller H Knabe W Muller P amp Weiser T 1993 The Early Holocene Saksunarvatntephra found in lake sediments in NW Germany Boreas 22 93100
Narcisi B 1993 Segnalazione di un livello piroclastico di provenienza etnea nellrsquo area del Fucino(Italia Centrale) Quaternario 6 8792
Narcisi B 1996 Tephrochronology of a Late Quaternary lacustrine record from the Monticchiomaar (Vulture volcano southern Italy) Quat Sci Rev 15 155165
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
800 S M Davies and others
Newton A J amp Dugmore A J 1993 Tephrochronology of Core C from Lago Grande di Mon-ticchio In Paleolimnology of European Maar Lakes (ed J F W Negendank amp B Zolitschka)Lecture Notes in Earth Science vol 49 333348 Springer
Oldmacreld F Appleby P G amp Thompson R 1980 Palaeoecological studies of lakes in theHighlands of Papua New Guinea J Ecol 68 457477
Orsi G Drsquo Antonio M de Vita S amp Gallo G 1992 The Neapolitan Yellow Tureg a large mag-nitude trachytic phreatoplinian eruption eruptive dynamics magma withdrawal and calderacollapse J Volcanol Geotherm Res 53 275287
Paterne M Guichard F Labeyrie J Gillot P Y amp Duplessy J C 1986 Tyrrhenian Seatephrochronology of the oxygen isotope record for the past 60 000 years Mar Geol 72259285
Paterne M Guichard F amp Labeyrie J 1988 Explosive activity of the south Italian volca-noes during the past 80 000 years as determined by marine tephrochronology J VolcanolGeotherm Res 34 153172
Paterne M Labeyrie J Guichard F Mazaud A amp Maitre F 1990 Fluctuations of the Cam-panian explosive volcanic activity (south Italy) during the past 190 000 years as determinedby marine tephrochronology Earth Planet Sci Lett 98 166174
Pawse A Beske-Diehl S amp Marshall S A 1998 Use of magnetic hysteresis properties andelectron spin resonance spectroscopy for the identimacrcation of volcanic ash a preliminary studyGeophys J Int 132 712720
Pearce N J G Westgate J A amp Perkins W T 1996 Developments in the analysis of singleglass shards in volcanic deposits by laser ablation ICP-MS quantitative and single internalstandard multi-element methods Quat Int 3436 213227
Pearce N J G Westgate J A Perkins W T Eastwood W J amp Shane P 1999 Theapplication of laser ablation ICP-MS to the analysis of volcanic glass shards from tephradeposits bulk glass and single shard analysis Global Planet Change 21 151171
Pilcher J R amp Hall V A 1992 Towards a tephrochronology for the Holocene of the north ofIreland Holocene 2 255259
Ponel P amp Lowe J J 1992 Coleopteran pollen and radiocarbon evidence from the Prato Spillarsquo Drsquo succession N Italy C R Acad Sci Paris Sparaer II 315 14251431
Rose N L Golding P N E amp Battarbee R W 1996 Selective concentration and enumerationof tephra shards from lake sediment cores Holocene 6 243246
Ruddiman W F amp Glover L K 1972 Vertical mixing of ice rafted volcanic ash in NorthAtlantic sediments Geol Soc Am Bull 83 28172836
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Santacroce R 1987 Somma Vesuvius Quad Ric Sci 114 252
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Sikes E L Samson C R Guilderson T P amp Howard W R 2000 Old radiocarbon agesin the southwest Pacimacrc Ocean during the last glacial period and deglaciation Nature 405555558
Stein R Nam S-I Grobe H amp Hubbersten H 1996 Late Quaternary glacial history andshort term ice rafted debris deg uctuations along the East Greenland continental marine In LateQuaternary palaeoceanography of the North Atlantic margins (ed J T Andrews W E NAustin H Bergsten amp A E Jennings) pp 135151 Geological Society London SpecialPublication
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 801
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Stuiver M Reimer P J Bard E Beck J W Burr G S Hughen K A Kromer BMcCormac G Van der Plicht J amp Spurk M 1998 INTCAL 98 radiocarbon age calibration24 0000 cal BP Radiocarbon 40 10411083
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Turney C S M 1998 Extraction of rhyolitic ash from minerogenic lake sediments J Paleolim-nol 19 199206
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Turney C S M Harkness D D amp Lowe J J 1997 The use of microtephra horizons tocorrelate Lateglacial lake sediments successions in Scotland J Quat Sci 12 525531
Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
van den Bogaard P amp Schmincke H 1985 A widespread isochronous Late Quaternary tephralayer in central and northern Europe Geol Soc Am Bull 96 15541571
van den Bogaard B Dordeg er W Sandgren P amp Schmincke H-U 1994 Correlating theHolocene records Icelandic tephra found in Schleswig-Holstein (northern Germany) Natur-wissenschaften 81 554556
Vernet G amp Raynal J-P 2001 Tephrostratigraphy of the Limagne revisited Implications forLateglacial and Holocene Prehistory In Tephras chronology archaeology (ed E Juvignparae ampJ-P Raynal) pp 111116 Dossiers de lrsquo ArchparaeoLogis no 1 France
Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
Vezzoli L 1991 Tephra layers in Bannock Basin (eastern Mediterranean) Mar Geol 1002134
von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
Walker M J C Bjorck S Lowe J J Cwynar L C Johnsen S Knudsen K-L WohlfarthB amp INTIMATE Group 1999 Isotopic events in the GRIP ice core a stratotype for the LatePleistocene Quat Sci Rev 18 11431150
Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
802 S M Davies and others
Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
796 S M Davies and others
Analyses were undertaken on a Cambridge Instruments Microscan V dual spectrom-eter at the Tephrochronology Analytical Unit University of Edinburgh This usedwavelength dispersive spectrometry (WDS) with an accelerating voltage of 20 kV abeam current of 15 nA and a beam diameter of 1 m m A 10 s peak count per elementwas employed with sodium measured in the shy rst and last counting period to monitorany sodium mobilisation A ZAF procedure was applied to correct for counter deadtime atomic number absorption and reguorescence enotects (Sweatman amp Long 1969)Calibration was undertaken using a combinaton of standards of pure metals sili-cates and synthetic oxides and a secondary standard of andradite was also analysedto monitor any drift in the readings
References
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Alley R B (and 10 others) 1993 Abrupt increase in Greenland snow accumulation at the endof the Younger Dryas Nature 362 527529
Andronico D Calderoni G Cioni R Sbrana A Sulpizio R amp Santacroce R 1995 Geo-logical map of Somma Vesuvius volcano Period Mineral 64 7788
Atkinson T C Brireg a K R amp Coope G R 1987 Seasonal temperature in Britain during thepast 22 000 years reconstructed using beetle remains Nature 325 587592
Austin W E N amp Kroon D 1996 Lateglacial sedimentology foraminifera and stable isotopestratigraphy of the Hebridean Continental Shelf northwest Scotland In Late Quaternarypalaeoceanography of the North Atlantic margins (ed J T Andrews W E N Austin HBergsten amp A E Jennings) vol 111 pp 187213 Geological Society of London SpecialPublication
Austin W E N Bard E Hunt J B Kroon D amp Peacock J D 1995 The 14 C age ofthe Vedde Ash implications for Younger Dryas marine reservoir corrections Radiocarbon 375362
Barker D S 1983 Igneous rocks Englewood Clireg s NJ Prentice-Hall
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Birks H H Gulliksen S Hadeg idason H Mangerud J amp Possnert G 1996 New radiocarbondates for the Vedde Ash and the Saksunarvatn Ash from western Norway Quat Res 45119127
Bjorck J amp Wastegordm ard S 1999 Climate oscillations and tephrochronology in eastern middleSweden during the last glacialinterglacial transition J Quat Sci 14 399410
Bjorck S Ingparaolfsson O Hadeg idason H Hallsdparaottir M amp Anderson N J 1992 Lake Torfadals-vatn a high resolution record of the North Atlantic Ash zone I and the last glacialinterglacialenvironmental changes in Iceland Boreas 21 1522
Bjorck S Walker M J C Cwynar L Johnsen S Knudsen K Lowe J J Wohlfarth Bamp INTIMATE members 1998 An event stratigraphy for the Last Termination in the NorthAtlantic region based on the Greenland ice-core record a proposal by the INTIMATE groupJ Quat Sci 13 283292
Bjorck S Lowe J J amp Walker M J C 2001 Integration of ice core marine and terrestrialrecords of Termination 1 from the North Atlantic region Quat Sci Rev 20 11691274
Bond G C Mandeville C amp Horeg man S 2001 Were rhyolitic glasses in the Vedde Ash andin the North Atlanticrsquo s Ash zone 1 produced by the same volcanic eruption Quat Sci Rev20 11891199
Phil Trans R Soc Lond A (2002)
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Bondevik S Mangerud J amp Gulliksen S 2001 The marine 1 4 C age of the Vedde Ash Bedalong the west coast of Norway J Quat Sci 16 37
Bossuet G Richard H Magny M amp Rossy M 1997 A new occurrence of Laacher See Tephrain the central Jura (France) The mire of Le Lautrey C R Acad Sci Paris Sparaer IIa 3254348
Brauer A Endres C Gunter C Litt T Stebich M amp Negendank J F W 1999 Highresolution sediment and vegetation responses to Younger Dryas climate change in varved lakesediments from Meerfelder Maar Germany Quat Sci Rev 18 321329
Brooks S J Mayle F E amp Lowe J J 1997 Chironomid based Lateglacial climatic recon-struction for southeast Scotland J Quat Sci 12 161167
Calanchi N Dinelli E Gasparatto G amp Lucchini F 1996 Etnean tephra layer in Albanolake and Adriatic Sea cores new macrndings of Y-1 layer in the central Mediterranean area ActaVulcan 8 713
Coope G R Lemdahl G Lowe J J amp Walkling A 1998 Temperature gradients in northernEurope during the last glacialHolocene transition (149 ka BP) interpreted from coleopternassemblages J Quat Sci 13 419433
Dansgaard W (and 10 others) 1993 Evidence for general instability of past climate from a250 kyr ice-core record Nature 363 218220
Davies S M Turney C S M amp Lowe J J 2001 Identimacrcation and signimacrcance of a visiblebasalt-rich Vedde Ash layer in a Late-glacial sequence on the Isle of Skye Inner HebridesScotland J Quat Sci 16 99104
Delibrias G Di Paola G M Rosi M amp Santacroce R 1979 La storia eruttiva del complessovulcanico Somma Vesuvio ricostruita dalle successini piroclastiche del Monte Somma RendSoc It Mineral Petrolog 35 411438
Di Vito M A Isaia R Orsi G Southon J de Vita S Drsquo Antonio M Pappalardo L ampPiochi M 1999 Volcanism and deformation since 12 000 years at the Campi Flegrei caldera(Italy) J Volcanol Geophys Res 91 221246
Dugmore A J amp Newton A J 1992 Thin tephra layers in peat revealed by X-radiography JArchaeol Sci 19 163170
Dugmore A J amp Newton A J 1998 Holocene tephra layers in the Faroe Islands Frodskaparrit46 191204
Eastwood A J Pearce N J G Westgate J A Perkins W T Lamb H F amp RobertsN 1999 Geochemistry of Santorini tephra in lake sediments from southwest Turkey GlobalPlanet Change 21 1729
Eirpara sup3 ksson J Knudsen K L Hadeg idason H amp Henriksen P 2000 Lateglacial and Holocenepalaeoceanography of the North Icelandic shelf J Quat Sci 15 2342
Etlicher B Janssen C R Juvignparae E amp Van Leeuwen J F N 1987 Le Haut Forez (MassifCentral France) aprmicroes le Plparaeniglaciaire Wurmien environnement et tparaephra du volcan de LaNugmicroere Bull Ass Fr Etud Quat 4 229239
Frezzotti M amp Narcisi B 1996 Late Quaternary Tephra derived paleosols in central Italyrsquo scarbonate Apennine range stratigraphical and paleoclimatological implications Quat Int3436 147153
Friedrich M Kromer B Spurk M Hofmann J amp Kaiser K F 1999 Paleoenvironment andradiocarbon calibration as derived from LateglacialEarly Holocene tree-ring chronologiesQuat Int 61 2739
Froggatt P C 1992 Standardisation of the chemical analysis of tephra deposits Report of theICCT working group Quat Int 1314 9396
Gronvold K Oskarsson N Johnsen S J Clausen H B Hammer C U Bond G amp Bard E1995 Ash layers from Iceland in the GRIP ice core correlated with oceanic and land sedimentsEarth Planet Sci Lett 135 149155
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
798 S M Davies and others
Hadeg idason H Eirpara sup3 ksson J amp van Kreveld S 2000 The tephrochronology of Iceland and theNorth Atlantic region during the Middle and Late Quaternary a review J Quat Sci 15322
Hoek W Z amp Bohncke S J P 2001 Oxygen isotope wiggle matching as a tool for synchronisingice-core and terrestrial records over Termination 1 Quat Sci Rev 20 12511264
Hughen K A Overpeck J T Peterson L C amp Trumbore S 1996 Rapid climate changes inthe tropical Atlantic region during the last deglaciation Nature 380 5153
Hughen K A Overpeck J T amp Lehman J 1998 A new 14 C calibration data set for the LastDeglaciation Radiocarbon 39 483494
Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
Hunt J B amp Hill P G 1996 An inter-laboratory comparison of the electron probe microanalysisof glass geochemistry Quat Int 3436 229241
Hunt J B amp Hill P G 2001 Tephrological implications of beam sizesample size ereg ects inelectron microprobe analysis of glass shards J Quat Sci 16 105117
Hunt J B Fannin N G T Hill P G amp Peacock J D 1995 The tephrochronology andradiocarbon dating of North Atlantic Late Quaternary sediments an example from the StKilda Basin In The tectonics sedimentation and palaeoceanography of the North Atlanticregion (ed R A Scrutton M S Stoker G B Shimmield amp A W Tudhope) vol 90pp 227248 Geological Society of London Special Publication
Hunt J B Clift P D Lacasse C Vallier T L amp Werner R 1998 Standardisation ofelectron probe microanalysis of glass geochemistry In Proc ODP Scientimacrc Results vol 152pp 8591 College Station TX Ocean Drilling Program
Jakobsson S P 1979 Outline of the petrology of Iceland Jokull 29 5773
Juvignparae E 1987 Deux retombparaees volcaniques tardiglaciaires dans le Cparaezallier (Massif CentralFrance) Bull Ass Fr Etud Quat 13 37
Juvignparae E 1993 Contribution microa la tparaephrostratigraphie du Quaternaire et son application microa lagparaeomorphologie Mparaem Serv Explicat Cartes Gparaeol Min Belg 36 166
Juvignparae E amp Gewelt M 1987 La Narse drsquo Ampoix comme tparaephrostratotype dans la Chasup3 ne desPuys mparaeridionale (France) Bull Ass Fr Etud Quat 29 3749
Juvignparae E Kozarski S amp Nowaczyk B 1995 The occurrence of Laacher See Tephra in Pomera-nia NW Poland Boreas 24 225231
Juvignparae E Bastin B Delibrias G Evin J Gewelt M Gilot E amp Streel M 1996 Acomprehensive pollen and tephra based chronostratigraphic model for the Lateglacial andHolocene period in the French Massif Central Quat Int 3436 113120
Keller J 1980 The island of Vulcano Rend Soc It Mineral Petrolog 36 369414
Keller J Ryan W B F Ninkovich D amp Altherr R 1978 Explosive volcanic activity in theMediterranean over the past 200 000 years as recorded in deep sea sediments Geol Soc AmBull 89 591604
Kitagawa H amp van der Plicht J 2000 Atmospheric radiocarbon calibration beyond 11 900 calBP from Lake Suigetsu laminated sediments Radiocarbon 42 369380
Kvamme T Mangerud J Furnes H amp Ruddiman W F 1989 Geochemistry of Pleistoceneash zones in cores from the North Atlantic Norsk Geol Tids 69 251272
Lacasse C Sigurdsson H Johannesson H Paterne M amp Carey S 1995 Source of Ash zone 1in the North Atlantic Bull Volcanol 57 1832
Langone L Asioli A Corregiari A amp Trincardi F 1996 Age depth modelling through theLate-Quaternary deposits of the central Adriatic Basin In Palaeoenvironmental analysis ofItalian crater lake and Adriatic sediments (ed F Oldmacreld amp P Guilizzoni) vol 55 pp 177196 Memorie dellrsquo Instituto Italiano di Idrobiologia
Larsen G 2000 Holocene volcanism in Iceland and tephrochronology as a tool in volcanologyIn Iceland 2000 modern processes and past environments Keele University UK
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 799
Litt T amp Stebich M 1999 Bio- and chronostratigraphy of the Lateglacial in the Eifel regionGermany Quat Int 61 516
Litt T Brauer A Goslar T Merkt J Balaga K Muller H Ralska-Jasiewiczowa MStebich M amp Negendank J F W 2001 Correlation and synchronisation of Lateglacialcontinental sequences in northern Central Europe based on annually laminated lacustrinesediments Quat Sci Rev 20 12331249
Long D amp Morton A C 1987 An ash fall within the Loch Lomond stadial J Quat Sci 297101
Lotter A F Eicher U Siegenthaler U amp Birks H J B 1992 Lateglacial climatic oscillationsas recorded in Swiss lake sediments J Quat Sci 7 187204
Lowe J J 1992 Lateglacial and Early Holocene lake sediments from the Northern ApenninesItaly|pollen stratigraphy and radiocarbon dating Boreas 21 193208
Lowe J J 2001 Abrupt climatic changes in Europe during the last glacialinterglacial tran-sition the potential for testing hypotheses on the synchroneity of climatic events usingtephrochronology Global Planet Change 603 7384
Lowe J J amp Turney C S M 1997 Vedde Ash layer discovered in a small lake basin on theScottish mainland J Geol Soc Lond 154 605612
Lowe J J amp Walker M J C 2000 Radiocarbon dating the last glacialinterglacial transition(ca 14914 C ka BP) in terrestrial and marine records the need for new quality assuranceprotocols Radiocarbon 42 5368
Lowe J J amp Watson C 1993 Lateglacial and Early Holocene pollen stratigraphy of the northernApennines Italy Quat Sci Rev 12 727738
Lowe J J Birks H H Brooks S J Coope G R Harkness D D Mayle F E SheldrickC Turney C S M amp Walker M J C 1999 The chronology of palaeoenvironmental changesduring the Last GlacialHolocene transition towards an event stratigraphy for the BritishIsles J Geol Soc Lond 156 397410
Lowe J J Hoek W Z amp INTIMATE group 2001 Inter-regional correlation of palaeoclimaticrecords for the Last GlacialInterglacial transition a protocol for improved precision recom-mended by the INTIMATE project group Quat Sci Rev 20 11751187
Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
Mangerud J Lie S E Furnes H Kristiansen I L amp Liquest mo L 1984 A Younger Dryas ashbed in western Norway and its possible correlation with tephra beds from the Norwegian Seaand North Atlantic Quat Res 21 85104
Mangerud J Furnes H amp Jparaohansen J 1986 A 9000 year-old ash bed on the Faroe IslandsQuat Res 26 262265
Martini J 1970 Recherche de retombparaees volcaniques dans le sud-est de la France et la Suisseoccidentale Arch Sci 23 641674
Martini J amp Duret J J 1965 Note preliminaire sur la presence drsquo un niveau de cendres vol-caniques dans des sparaediments post-glaciaires des environs de Genmicroeve Arch Sci 18 587588
Mayewski P A Meeker L D Twickler M S Whitlow S Yang Q Lyons W B amp Pren-tice M 1997 Major features and forcing of high latitudes Northern Hemisphere atmosphericcirculation using a 110 000 year long glaciochemical series J Geophys Res 102 345365
Merkt J Muller H Knabe W Muller P amp Weiser T 1993 The Early Holocene Saksunarvatntephra found in lake sediments in NW Germany Boreas 22 93100
Narcisi B 1993 Segnalazione di un livello piroclastico di provenienza etnea nellrsquo area del Fucino(Italia Centrale) Quaternario 6 8792
Narcisi B 1996 Tephrochronology of a Late Quaternary lacustrine record from the Monticchiomaar (Vulture volcano southern Italy) Quat Sci Rev 15 155165
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
800 S M Davies and others
Newton A J amp Dugmore A J 1993 Tephrochronology of Core C from Lago Grande di Mon-ticchio In Paleolimnology of European Maar Lakes (ed J F W Negendank amp B Zolitschka)Lecture Notes in Earth Science vol 49 333348 Springer
Oldmacreld F Appleby P G amp Thompson R 1980 Palaeoecological studies of lakes in theHighlands of Papua New Guinea J Ecol 68 457477
Orsi G Drsquo Antonio M de Vita S amp Gallo G 1992 The Neapolitan Yellow Tureg a large mag-nitude trachytic phreatoplinian eruption eruptive dynamics magma withdrawal and calderacollapse J Volcanol Geotherm Res 53 275287
Paterne M Guichard F Labeyrie J Gillot P Y amp Duplessy J C 1986 Tyrrhenian Seatephrochronology of the oxygen isotope record for the past 60 000 years Mar Geol 72259285
Paterne M Guichard F amp Labeyrie J 1988 Explosive activity of the south Italian volca-noes during the past 80 000 years as determined by marine tephrochronology J VolcanolGeotherm Res 34 153172
Paterne M Labeyrie J Guichard F Mazaud A amp Maitre F 1990 Fluctuations of the Cam-panian explosive volcanic activity (south Italy) during the past 190 000 years as determinedby marine tephrochronology Earth Planet Sci Lett 98 166174
Pawse A Beske-Diehl S amp Marshall S A 1998 Use of magnetic hysteresis properties andelectron spin resonance spectroscopy for the identimacrcation of volcanic ash a preliminary studyGeophys J Int 132 712720
Pearce N J G Westgate J A amp Perkins W T 1996 Developments in the analysis of singleglass shards in volcanic deposits by laser ablation ICP-MS quantitative and single internalstandard multi-element methods Quat Int 3436 213227
Pearce N J G Westgate J A Perkins W T Eastwood W J amp Shane P 1999 Theapplication of laser ablation ICP-MS to the analysis of volcanic glass shards from tephradeposits bulk glass and single shard analysis Global Planet Change 21 151171
Pilcher J R amp Hall V A 1992 Towards a tephrochronology for the Holocene of the north ofIreland Holocene 2 255259
Ponel P amp Lowe J J 1992 Coleopteran pollen and radiocarbon evidence from the Prato Spillarsquo Drsquo succession N Italy C R Acad Sci Paris Sparaer II 315 14251431
Rose N L Golding P N E amp Battarbee R W 1996 Selective concentration and enumerationof tephra shards from lake sediment cores Holocene 6 243246
Ruddiman W F amp Glover L K 1972 Vertical mixing of ice rafted volcanic ash in NorthAtlantic sediments Geol Soc Am Bull 83 28172836
Ruddiman W amp McIntyre A 1981 The North Atlantic Ocean during the last deglaciationPalaeogeogr Palaeoclimatol Palaeoecol 35 145214
Santacroce R 1987 Somma Vesuvius Quad Ric Sci 114 252
Sarna-Wojcicki A 2000 Tephrochronology In Quaternary geochronology methods and applica-tions (ed J S Noller J M Sowers amp W R Lettis) AGU Reference shelf vol 4 pp 357377Washington DC American Geophysical Union
Sejrup H P Sjiquest holm J Furnes H Beyer I Eide L Jansen E amp Mangerud J 1989Quaternary tephrochronology on the Iceland Plateau north of Iceland J Quat Sci 4 109114
Sikes E L Samson C R Guilderson T P amp Howard W R 2000 Old radiocarbon agesin the southwest Pacimacrc Ocean during the last glacial period and deglaciation Nature 405555558
Stein R Nam S-I Grobe H amp Hubbersten H 1996 Late Quaternary glacial history andshort term ice rafted debris deg uctuations along the East Greenland continental marine In LateQuaternary palaeoceanography of the North Atlantic margins (ed J T Andrews W E NAustin H Bergsten amp A E Jennings) pp 135151 Geological Society London SpecialPublication
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 801
Stuiver M amp Grootes P M 2000 GISP2 oxygen isotope ratios Quat Res 53 277284
Stuiver M Reimer P J Bard E Beck J W Burr G S Hughen K A Kromer BMcCormac G Van der Plicht J amp Spurk M 1998 INTCAL 98 radiocarbon age calibration24 0000 cal BP Radiocarbon 40 10411083
Sweatman T R amp Long J V P 1969 Quantitative electron microprobe analysis of rock formingminerals J Petrol 7 332379
Turney C S M 1998 Extraction of rhyolitic ash from minerogenic lake sediments J Paleolim-nol 19 199206
Turney C S M amp Lowe J J 2001 Tephrochronology In Tracking environmental changes inlake sediments physical and chemical techniques (ed W M Last amp J P Smol) DordrechtKluwer Academic
Turney C S M Harkness D D amp Lowe J J 1997 The use of microtephra horizons tocorrelate Lateglacial lake sediments successions in Scotland J Quat Sci 12 525531
Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
van den Bogaard P amp Schmincke H 1985 A widespread isochronous Late Quaternary tephralayer in central and northern Europe Geol Soc Am Bull 96 15541571
van den Bogaard B Dordeg er W Sandgren P amp Schmincke H-U 1994 Correlating theHolocene records Icelandic tephra found in Schleswig-Holstein (northern Germany) Natur-wissenschaften 81 554556
Vernet G amp Raynal J-P 2001 Tephrostratigraphy of the Limagne revisited Implications forLateglacial and Holocene Prehistory In Tephras chronology archaeology (ed E Juvignparae ampJ-P Raynal) pp 111116 Dossiers de lrsquo ArchparaeoLogis no 1 France
Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
Vezzoli L 1991 Tephra layers in Bannock Basin (eastern Mediterranean) Mar Geol 1002134
von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
Walker M J C Bjorck S Lowe J J Cwynar L C Johnsen S Knudsen K-L WohlfarthB amp INTIMATE Group 1999 Isotopic events in the GRIP ice core a stratotype for the LatePleistocene Quat Sci Rev 18 11431150
Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
802 S M Davies and others
Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 797
Bondevik S Mangerud J amp Gulliksen S 2001 The marine 1 4 C age of the Vedde Ash Bedalong the west coast of Norway J Quat Sci 16 37
Bossuet G Richard H Magny M amp Rossy M 1997 A new occurrence of Laacher See Tephrain the central Jura (France) The mire of Le Lautrey C R Acad Sci Paris Sparaer IIa 3254348
Brauer A Endres C Gunter C Litt T Stebich M amp Negendank J F W 1999 Highresolution sediment and vegetation responses to Younger Dryas climate change in varved lakesediments from Meerfelder Maar Germany Quat Sci Rev 18 321329
Brooks S J Mayle F E amp Lowe J J 1997 Chironomid based Lateglacial climatic recon-struction for southeast Scotland J Quat Sci 12 161167
Calanchi N Dinelli E Gasparatto G amp Lucchini F 1996 Etnean tephra layer in Albanolake and Adriatic Sea cores new macrndings of Y-1 layer in the central Mediterranean area ActaVulcan 8 713
Coope G R Lemdahl G Lowe J J amp Walkling A 1998 Temperature gradients in northernEurope during the last glacialHolocene transition (149 ka BP) interpreted from coleopternassemblages J Quat Sci 13 419433
Dansgaard W (and 10 others) 1993 Evidence for general instability of past climate from a250 kyr ice-core record Nature 363 218220
Davies S M Turney C S M amp Lowe J J 2001 Identimacrcation and signimacrcance of a visiblebasalt-rich Vedde Ash layer in a Late-glacial sequence on the Isle of Skye Inner HebridesScotland J Quat Sci 16 99104
Delibrias G Di Paola G M Rosi M amp Santacroce R 1979 La storia eruttiva del complessovulcanico Somma Vesuvio ricostruita dalle successini piroclastiche del Monte Somma RendSoc It Mineral Petrolog 35 411438
Di Vito M A Isaia R Orsi G Southon J de Vita S Drsquo Antonio M Pappalardo L ampPiochi M 1999 Volcanism and deformation since 12 000 years at the Campi Flegrei caldera(Italy) J Volcanol Geophys Res 91 221246
Dugmore A J amp Newton A J 1992 Thin tephra layers in peat revealed by X-radiography JArchaeol Sci 19 163170
Dugmore A J amp Newton A J 1998 Holocene tephra layers in the Faroe Islands Frodskaparrit46 191204
Eastwood A J Pearce N J G Westgate J A Perkins W T Lamb H F amp RobertsN 1999 Geochemistry of Santorini tephra in lake sediments from southwest Turkey GlobalPlanet Change 21 1729
Eirpara sup3 ksson J Knudsen K L Hadeg idason H amp Henriksen P 2000 Lateglacial and Holocenepalaeoceanography of the North Icelandic shelf J Quat Sci 15 2342
Etlicher B Janssen C R Juvignparae E amp Van Leeuwen J F N 1987 Le Haut Forez (MassifCentral France) aprmicroes le Plparaeniglaciaire Wurmien environnement et tparaephra du volcan de LaNugmicroere Bull Ass Fr Etud Quat 4 229239
Frezzotti M amp Narcisi B 1996 Late Quaternary Tephra derived paleosols in central Italyrsquo scarbonate Apennine range stratigraphical and paleoclimatological implications Quat Int3436 147153
Friedrich M Kromer B Spurk M Hofmann J amp Kaiser K F 1999 Paleoenvironment andradiocarbon calibration as derived from LateglacialEarly Holocene tree-ring chronologiesQuat Int 61 2739
Froggatt P C 1992 Standardisation of the chemical analysis of tephra deposits Report of theICCT working group Quat Int 1314 9396
Gronvold K Oskarsson N Johnsen S J Clausen H B Hammer C U Bond G amp Bard E1995 Ash layers from Iceland in the GRIP ice core correlated with oceanic and land sedimentsEarth Planet Sci Lett 135 149155
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
798 S M Davies and others
Hadeg idason H Eirpara sup3 ksson J amp van Kreveld S 2000 The tephrochronology of Iceland and theNorth Atlantic region during the Middle and Late Quaternary a review J Quat Sci 15322
Hoek W Z amp Bohncke S J P 2001 Oxygen isotope wiggle matching as a tool for synchronisingice-core and terrestrial records over Termination 1 Quat Sci Rev 20 12511264
Hughen K A Overpeck J T Peterson L C amp Trumbore S 1996 Rapid climate changes inthe tropical Atlantic region during the last deglaciation Nature 380 5153
Hughen K A Overpeck J T amp Lehman J 1998 A new 14 C calibration data set for the LastDeglaciation Radiocarbon 39 483494
Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
Hunt J B amp Hill P G 1996 An inter-laboratory comparison of the electron probe microanalysisof glass geochemistry Quat Int 3436 229241
Hunt J B amp Hill P G 2001 Tephrological implications of beam sizesample size ereg ects inelectron microprobe analysis of glass shards J Quat Sci 16 105117
Hunt J B Fannin N G T Hill P G amp Peacock J D 1995 The tephrochronology andradiocarbon dating of North Atlantic Late Quaternary sediments an example from the StKilda Basin In The tectonics sedimentation and palaeoceanography of the North Atlanticregion (ed R A Scrutton M S Stoker G B Shimmield amp A W Tudhope) vol 90pp 227248 Geological Society of London Special Publication
Hunt J B Clift P D Lacasse C Vallier T L amp Werner R 1998 Standardisation ofelectron probe microanalysis of glass geochemistry In Proc ODP Scientimacrc Results vol 152pp 8591 College Station TX Ocean Drilling Program
Jakobsson S P 1979 Outline of the petrology of Iceland Jokull 29 5773
Juvignparae E 1987 Deux retombparaees volcaniques tardiglaciaires dans le Cparaezallier (Massif CentralFrance) Bull Ass Fr Etud Quat 13 37
Juvignparae E 1993 Contribution microa la tparaephrostratigraphie du Quaternaire et son application microa lagparaeomorphologie Mparaem Serv Explicat Cartes Gparaeol Min Belg 36 166
Juvignparae E amp Gewelt M 1987 La Narse drsquo Ampoix comme tparaephrostratotype dans la Chasup3 ne desPuys mparaeridionale (France) Bull Ass Fr Etud Quat 29 3749
Juvignparae E Kozarski S amp Nowaczyk B 1995 The occurrence of Laacher See Tephra in Pomera-nia NW Poland Boreas 24 225231
Juvignparae E Bastin B Delibrias G Evin J Gewelt M Gilot E amp Streel M 1996 Acomprehensive pollen and tephra based chronostratigraphic model for the Lateglacial andHolocene period in the French Massif Central Quat Int 3436 113120
Keller J 1980 The island of Vulcano Rend Soc It Mineral Petrolog 36 369414
Keller J Ryan W B F Ninkovich D amp Altherr R 1978 Explosive volcanic activity in theMediterranean over the past 200 000 years as recorded in deep sea sediments Geol Soc AmBull 89 591604
Kitagawa H amp van der Plicht J 2000 Atmospheric radiocarbon calibration beyond 11 900 calBP from Lake Suigetsu laminated sediments Radiocarbon 42 369380
Kvamme T Mangerud J Furnes H amp Ruddiman W F 1989 Geochemistry of Pleistoceneash zones in cores from the North Atlantic Norsk Geol Tids 69 251272
Lacasse C Sigurdsson H Johannesson H Paterne M amp Carey S 1995 Source of Ash zone 1in the North Atlantic Bull Volcanol 57 1832
Langone L Asioli A Corregiari A amp Trincardi F 1996 Age depth modelling through theLate-Quaternary deposits of the central Adriatic Basin In Palaeoenvironmental analysis ofItalian crater lake and Adriatic sediments (ed F Oldmacreld amp P Guilizzoni) vol 55 pp 177196 Memorie dellrsquo Instituto Italiano di Idrobiologia
Larsen G 2000 Holocene volcanism in Iceland and tephrochronology as a tool in volcanologyIn Iceland 2000 modern processes and past environments Keele University UK
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 799
Litt T amp Stebich M 1999 Bio- and chronostratigraphy of the Lateglacial in the Eifel regionGermany Quat Int 61 516
Litt T Brauer A Goslar T Merkt J Balaga K Muller H Ralska-Jasiewiczowa MStebich M amp Negendank J F W 2001 Correlation and synchronisation of Lateglacialcontinental sequences in northern Central Europe based on annually laminated lacustrinesediments Quat Sci Rev 20 12331249
Long D amp Morton A C 1987 An ash fall within the Loch Lomond stadial J Quat Sci 297101
Lotter A F Eicher U Siegenthaler U amp Birks H J B 1992 Lateglacial climatic oscillationsas recorded in Swiss lake sediments J Quat Sci 7 187204
Lowe J J 1992 Lateglacial and Early Holocene lake sediments from the Northern ApenninesItaly|pollen stratigraphy and radiocarbon dating Boreas 21 193208
Lowe J J 2001 Abrupt climatic changes in Europe during the last glacialinterglacial tran-sition the potential for testing hypotheses on the synchroneity of climatic events usingtephrochronology Global Planet Change 603 7384
Lowe J J amp Turney C S M 1997 Vedde Ash layer discovered in a small lake basin on theScottish mainland J Geol Soc Lond 154 605612
Lowe J J amp Walker M J C 2000 Radiocarbon dating the last glacialinterglacial transition(ca 14914 C ka BP) in terrestrial and marine records the need for new quality assuranceprotocols Radiocarbon 42 5368
Lowe J J amp Watson C 1993 Lateglacial and Early Holocene pollen stratigraphy of the northernApennines Italy Quat Sci Rev 12 727738
Lowe J J Birks H H Brooks S J Coope G R Harkness D D Mayle F E SheldrickC Turney C S M amp Walker M J C 1999 The chronology of palaeoenvironmental changesduring the Last GlacialHolocene transition towards an event stratigraphy for the BritishIsles J Geol Soc Lond 156 397410
Lowe J J Hoek W Z amp INTIMATE group 2001 Inter-regional correlation of palaeoclimaticrecords for the Last GlacialInterglacial transition a protocol for improved precision recom-mended by the INTIMATE project group Quat Sci Rev 20 11751187
Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
Mangerud J Lie S E Furnes H Kristiansen I L amp Liquest mo L 1984 A Younger Dryas ashbed in western Norway and its possible correlation with tephra beds from the Norwegian Seaand North Atlantic Quat Res 21 85104
Mangerud J Furnes H amp Jparaohansen J 1986 A 9000 year-old ash bed on the Faroe IslandsQuat Res 26 262265
Martini J 1970 Recherche de retombparaees volcaniques dans le sud-est de la France et la Suisseoccidentale Arch Sci 23 641674
Martini J amp Duret J J 1965 Note preliminaire sur la presence drsquo un niveau de cendres vol-caniques dans des sparaediments post-glaciaires des environs de Genmicroeve Arch Sci 18 587588
Mayewski P A Meeker L D Twickler M S Whitlow S Yang Q Lyons W B amp Pren-tice M 1997 Major features and forcing of high latitudes Northern Hemisphere atmosphericcirculation using a 110 000 year long glaciochemical series J Geophys Res 102 345365
Merkt J Muller H Knabe W Muller P amp Weiser T 1993 The Early Holocene Saksunarvatntephra found in lake sediments in NW Germany Boreas 22 93100
Narcisi B 1993 Segnalazione di un livello piroclastico di provenienza etnea nellrsquo area del Fucino(Italia Centrale) Quaternario 6 8792
Narcisi B 1996 Tephrochronology of a Late Quaternary lacustrine record from the Monticchiomaar (Vulture volcano southern Italy) Quat Sci Rev 15 155165
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
800 S M Davies and others
Newton A J amp Dugmore A J 1993 Tephrochronology of Core C from Lago Grande di Mon-ticchio In Paleolimnology of European Maar Lakes (ed J F W Negendank amp B Zolitschka)Lecture Notes in Earth Science vol 49 333348 Springer
Oldmacreld F Appleby P G amp Thompson R 1980 Palaeoecological studies of lakes in theHighlands of Papua New Guinea J Ecol 68 457477
Orsi G Drsquo Antonio M de Vita S amp Gallo G 1992 The Neapolitan Yellow Tureg a large mag-nitude trachytic phreatoplinian eruption eruptive dynamics magma withdrawal and calderacollapse J Volcanol Geotherm Res 53 275287
Paterne M Guichard F Labeyrie J Gillot P Y amp Duplessy J C 1986 Tyrrhenian Seatephrochronology of the oxygen isotope record for the past 60 000 years Mar Geol 72259285
Paterne M Guichard F amp Labeyrie J 1988 Explosive activity of the south Italian volca-noes during the past 80 000 years as determined by marine tephrochronology J VolcanolGeotherm Res 34 153172
Paterne M Labeyrie J Guichard F Mazaud A amp Maitre F 1990 Fluctuations of the Cam-panian explosive volcanic activity (south Italy) during the past 190 000 years as determinedby marine tephrochronology Earth Planet Sci Lett 98 166174
Pawse A Beske-Diehl S amp Marshall S A 1998 Use of magnetic hysteresis properties andelectron spin resonance spectroscopy for the identimacrcation of volcanic ash a preliminary studyGeophys J Int 132 712720
Pearce N J G Westgate J A amp Perkins W T 1996 Developments in the analysis of singleglass shards in volcanic deposits by laser ablation ICP-MS quantitative and single internalstandard multi-element methods Quat Int 3436 213227
Pearce N J G Westgate J A Perkins W T Eastwood W J amp Shane P 1999 Theapplication of laser ablation ICP-MS to the analysis of volcanic glass shards from tephradeposits bulk glass and single shard analysis Global Planet Change 21 151171
Pilcher J R amp Hall V A 1992 Towards a tephrochronology for the Holocene of the north ofIreland Holocene 2 255259
Ponel P amp Lowe J J 1992 Coleopteran pollen and radiocarbon evidence from the Prato Spillarsquo Drsquo succession N Italy C R Acad Sci Paris Sparaer II 315 14251431
Rose N L Golding P N E amp Battarbee R W 1996 Selective concentration and enumerationof tephra shards from lake sediment cores Holocene 6 243246
Ruddiman W F amp Glover L K 1972 Vertical mixing of ice rafted volcanic ash in NorthAtlantic sediments Geol Soc Am Bull 83 28172836
Ruddiman W amp McIntyre A 1981 The North Atlantic Ocean during the last deglaciationPalaeogeogr Palaeoclimatol Palaeoecol 35 145214
Santacroce R 1987 Somma Vesuvius Quad Ric Sci 114 252
Sarna-Wojcicki A 2000 Tephrochronology In Quaternary geochronology methods and applica-tions (ed J S Noller J M Sowers amp W R Lettis) AGU Reference shelf vol 4 pp 357377Washington DC American Geophysical Union
Sejrup H P Sjiquest holm J Furnes H Beyer I Eide L Jansen E amp Mangerud J 1989Quaternary tephrochronology on the Iceland Plateau north of Iceland J Quat Sci 4 109114
Sikes E L Samson C R Guilderson T P amp Howard W R 2000 Old radiocarbon agesin the southwest Pacimacrc Ocean during the last glacial period and deglaciation Nature 405555558
Stein R Nam S-I Grobe H amp Hubbersten H 1996 Late Quaternary glacial history andshort term ice rafted debris deg uctuations along the East Greenland continental marine In LateQuaternary palaeoceanography of the North Atlantic margins (ed J T Andrews W E NAustin H Bergsten amp A E Jennings) pp 135151 Geological Society London SpecialPublication
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 801
Stuiver M amp Grootes P M 2000 GISP2 oxygen isotope ratios Quat Res 53 277284
Stuiver M Reimer P J Bard E Beck J W Burr G S Hughen K A Kromer BMcCormac G Van der Plicht J amp Spurk M 1998 INTCAL 98 radiocarbon age calibration24 0000 cal BP Radiocarbon 40 10411083
Sweatman T R amp Long J V P 1969 Quantitative electron microprobe analysis of rock formingminerals J Petrol 7 332379
Turney C S M 1998 Extraction of rhyolitic ash from minerogenic lake sediments J Paleolim-nol 19 199206
Turney C S M amp Lowe J J 2001 Tephrochronology In Tracking environmental changes inlake sediments physical and chemical techniques (ed W M Last amp J P Smol) DordrechtKluwer Academic
Turney C S M Harkness D D amp Lowe J J 1997 The use of microtephra horizons tocorrelate Lateglacial lake sediments successions in Scotland J Quat Sci 12 525531
Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
van den Bogaard P amp Schmincke H 1985 A widespread isochronous Late Quaternary tephralayer in central and northern Europe Geol Soc Am Bull 96 15541571
van den Bogaard B Dordeg er W Sandgren P amp Schmincke H-U 1994 Correlating theHolocene records Icelandic tephra found in Schleswig-Holstein (northern Germany) Natur-wissenschaften 81 554556
Vernet G amp Raynal J-P 2001 Tephrostratigraphy of the Limagne revisited Implications forLateglacial and Holocene Prehistory In Tephras chronology archaeology (ed E Juvignparae ampJ-P Raynal) pp 111116 Dossiers de lrsquo ArchparaeoLogis no 1 France
Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
Vezzoli L 1991 Tephra layers in Bannock Basin (eastern Mediterranean) Mar Geol 1002134
von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
Walker M J C Bjorck S Lowe J J Cwynar L C Johnsen S Knudsen K-L WohlfarthB amp INTIMATE Group 1999 Isotopic events in the GRIP ice core a stratotype for the LatePleistocene Quat Sci Rev 18 11431150
Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
802 S M Davies and others
Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
798 S M Davies and others
Hadeg idason H Eirpara sup3 ksson J amp van Kreveld S 2000 The tephrochronology of Iceland and theNorth Atlantic region during the Middle and Late Quaternary a review J Quat Sci 15322
Hoek W Z amp Bohncke S J P 2001 Oxygen isotope wiggle matching as a tool for synchronisingice-core and terrestrial records over Termination 1 Quat Sci Rev 20 12511264
Hughen K A Overpeck J T Peterson L C amp Trumbore S 1996 Rapid climate changes inthe tropical Atlantic region during the last deglaciation Nature 380 5153
Hughen K A Overpeck J T amp Lehman J 1998 A new 14 C calibration data set for the LastDeglaciation Radiocarbon 39 483494
Hunt J B amp Hill P G 1993 Tephra geochemistry a discussion of some persistent analyticalproblems Holocene 3 271278
Hunt J B amp Hill P G 1996 An inter-laboratory comparison of the electron probe microanalysisof glass geochemistry Quat Int 3436 229241
Hunt J B amp Hill P G 2001 Tephrological implications of beam sizesample size ereg ects inelectron microprobe analysis of glass shards J Quat Sci 16 105117
Hunt J B Fannin N G T Hill P G amp Peacock J D 1995 The tephrochronology andradiocarbon dating of North Atlantic Late Quaternary sediments an example from the StKilda Basin In The tectonics sedimentation and palaeoceanography of the North Atlanticregion (ed R A Scrutton M S Stoker G B Shimmield amp A W Tudhope) vol 90pp 227248 Geological Society of London Special Publication
Hunt J B Clift P D Lacasse C Vallier T L amp Werner R 1998 Standardisation ofelectron probe microanalysis of glass geochemistry In Proc ODP Scientimacrc Results vol 152pp 8591 College Station TX Ocean Drilling Program
Jakobsson S P 1979 Outline of the petrology of Iceland Jokull 29 5773
Juvignparae E 1987 Deux retombparaees volcaniques tardiglaciaires dans le Cparaezallier (Massif CentralFrance) Bull Ass Fr Etud Quat 13 37
Juvignparae E 1993 Contribution microa la tparaephrostratigraphie du Quaternaire et son application microa lagparaeomorphologie Mparaem Serv Explicat Cartes Gparaeol Min Belg 36 166
Juvignparae E amp Gewelt M 1987 La Narse drsquo Ampoix comme tparaephrostratotype dans la Chasup3 ne desPuys mparaeridionale (France) Bull Ass Fr Etud Quat 29 3749
Juvignparae E Kozarski S amp Nowaczyk B 1995 The occurrence of Laacher See Tephra in Pomera-nia NW Poland Boreas 24 225231
Juvignparae E Bastin B Delibrias G Evin J Gewelt M Gilot E amp Streel M 1996 Acomprehensive pollen and tephra based chronostratigraphic model for the Lateglacial andHolocene period in the French Massif Central Quat Int 3436 113120
Keller J 1980 The island of Vulcano Rend Soc It Mineral Petrolog 36 369414
Keller J Ryan W B F Ninkovich D amp Altherr R 1978 Explosive volcanic activity in theMediterranean over the past 200 000 years as recorded in deep sea sediments Geol Soc AmBull 89 591604
Kitagawa H amp van der Plicht J 2000 Atmospheric radiocarbon calibration beyond 11 900 calBP from Lake Suigetsu laminated sediments Radiocarbon 42 369380
Kvamme T Mangerud J Furnes H amp Ruddiman W F 1989 Geochemistry of Pleistoceneash zones in cores from the North Atlantic Norsk Geol Tids 69 251272
Lacasse C Sigurdsson H Johannesson H Paterne M amp Carey S 1995 Source of Ash zone 1in the North Atlantic Bull Volcanol 57 1832
Langone L Asioli A Corregiari A amp Trincardi F 1996 Age depth modelling through theLate-Quaternary deposits of the central Adriatic Basin In Palaeoenvironmental analysis ofItalian crater lake and Adriatic sediments (ed F Oldmacreld amp P Guilizzoni) vol 55 pp 177196 Memorie dellrsquo Instituto Italiano di Idrobiologia
Larsen G 2000 Holocene volcanism in Iceland and tephrochronology as a tool in volcanologyIn Iceland 2000 modern processes and past environments Keele University UK
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 799
Litt T amp Stebich M 1999 Bio- and chronostratigraphy of the Lateglacial in the Eifel regionGermany Quat Int 61 516
Litt T Brauer A Goslar T Merkt J Balaga K Muller H Ralska-Jasiewiczowa MStebich M amp Negendank J F W 2001 Correlation and synchronisation of Lateglacialcontinental sequences in northern Central Europe based on annually laminated lacustrinesediments Quat Sci Rev 20 12331249
Long D amp Morton A C 1987 An ash fall within the Loch Lomond stadial J Quat Sci 297101
Lotter A F Eicher U Siegenthaler U amp Birks H J B 1992 Lateglacial climatic oscillationsas recorded in Swiss lake sediments J Quat Sci 7 187204
Lowe J J 1992 Lateglacial and Early Holocene lake sediments from the Northern ApenninesItaly|pollen stratigraphy and radiocarbon dating Boreas 21 193208
Lowe J J 2001 Abrupt climatic changes in Europe during the last glacialinterglacial tran-sition the potential for testing hypotheses on the synchroneity of climatic events usingtephrochronology Global Planet Change 603 7384
Lowe J J amp Turney C S M 1997 Vedde Ash layer discovered in a small lake basin on theScottish mainland J Geol Soc Lond 154 605612
Lowe J J amp Walker M J C 2000 Radiocarbon dating the last glacialinterglacial transition(ca 14914 C ka BP) in terrestrial and marine records the need for new quality assuranceprotocols Radiocarbon 42 5368
Lowe J J amp Watson C 1993 Lateglacial and Early Holocene pollen stratigraphy of the northernApennines Italy Quat Sci Rev 12 727738
Lowe J J Birks H H Brooks S J Coope G R Harkness D D Mayle F E SheldrickC Turney C S M amp Walker M J C 1999 The chronology of palaeoenvironmental changesduring the Last GlacialHolocene transition towards an event stratigraphy for the BritishIsles J Geol Soc Lond 156 397410
Lowe J J Hoek W Z amp INTIMATE group 2001 Inter-regional correlation of palaeoclimaticrecords for the Last GlacialInterglacial transition a protocol for improved precision recom-mended by the INTIMATE project group Quat Sci Rev 20 11751187
Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
Mangerud J Lie S E Furnes H Kristiansen I L amp Liquest mo L 1984 A Younger Dryas ashbed in western Norway and its possible correlation with tephra beds from the Norwegian Seaand North Atlantic Quat Res 21 85104
Mangerud J Furnes H amp Jparaohansen J 1986 A 9000 year-old ash bed on the Faroe IslandsQuat Res 26 262265
Martini J 1970 Recherche de retombparaees volcaniques dans le sud-est de la France et la Suisseoccidentale Arch Sci 23 641674
Martini J amp Duret J J 1965 Note preliminaire sur la presence drsquo un niveau de cendres vol-caniques dans des sparaediments post-glaciaires des environs de Genmicroeve Arch Sci 18 587588
Mayewski P A Meeker L D Twickler M S Whitlow S Yang Q Lyons W B amp Pren-tice M 1997 Major features and forcing of high latitudes Northern Hemisphere atmosphericcirculation using a 110 000 year long glaciochemical series J Geophys Res 102 345365
Merkt J Muller H Knabe W Muller P amp Weiser T 1993 The Early Holocene Saksunarvatntephra found in lake sediments in NW Germany Boreas 22 93100
Narcisi B 1993 Segnalazione di un livello piroclastico di provenienza etnea nellrsquo area del Fucino(Italia Centrale) Quaternario 6 8792
Narcisi B 1996 Tephrochronology of a Late Quaternary lacustrine record from the Monticchiomaar (Vulture volcano southern Italy) Quat Sci Rev 15 155165
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
800 S M Davies and others
Newton A J amp Dugmore A J 1993 Tephrochronology of Core C from Lago Grande di Mon-ticchio In Paleolimnology of European Maar Lakes (ed J F W Negendank amp B Zolitschka)Lecture Notes in Earth Science vol 49 333348 Springer
Oldmacreld F Appleby P G amp Thompson R 1980 Palaeoecological studies of lakes in theHighlands of Papua New Guinea J Ecol 68 457477
Orsi G Drsquo Antonio M de Vita S amp Gallo G 1992 The Neapolitan Yellow Tureg a large mag-nitude trachytic phreatoplinian eruption eruptive dynamics magma withdrawal and calderacollapse J Volcanol Geotherm Res 53 275287
Paterne M Guichard F Labeyrie J Gillot P Y amp Duplessy J C 1986 Tyrrhenian Seatephrochronology of the oxygen isotope record for the past 60 000 years Mar Geol 72259285
Paterne M Guichard F amp Labeyrie J 1988 Explosive activity of the south Italian volca-noes during the past 80 000 years as determined by marine tephrochronology J VolcanolGeotherm Res 34 153172
Paterne M Labeyrie J Guichard F Mazaud A amp Maitre F 1990 Fluctuations of the Cam-panian explosive volcanic activity (south Italy) during the past 190 000 years as determinedby marine tephrochronology Earth Planet Sci Lett 98 166174
Pawse A Beske-Diehl S amp Marshall S A 1998 Use of magnetic hysteresis properties andelectron spin resonance spectroscopy for the identimacrcation of volcanic ash a preliminary studyGeophys J Int 132 712720
Pearce N J G Westgate J A amp Perkins W T 1996 Developments in the analysis of singleglass shards in volcanic deposits by laser ablation ICP-MS quantitative and single internalstandard multi-element methods Quat Int 3436 213227
Pearce N J G Westgate J A Perkins W T Eastwood W J amp Shane P 1999 Theapplication of laser ablation ICP-MS to the analysis of volcanic glass shards from tephradeposits bulk glass and single shard analysis Global Planet Change 21 151171
Pilcher J R amp Hall V A 1992 Towards a tephrochronology for the Holocene of the north ofIreland Holocene 2 255259
Ponel P amp Lowe J J 1992 Coleopteran pollen and radiocarbon evidence from the Prato Spillarsquo Drsquo succession N Italy C R Acad Sci Paris Sparaer II 315 14251431
Rose N L Golding P N E amp Battarbee R W 1996 Selective concentration and enumerationof tephra shards from lake sediment cores Holocene 6 243246
Ruddiman W F amp Glover L K 1972 Vertical mixing of ice rafted volcanic ash in NorthAtlantic sediments Geol Soc Am Bull 83 28172836
Ruddiman W amp McIntyre A 1981 The North Atlantic Ocean during the last deglaciationPalaeogeogr Palaeoclimatol Palaeoecol 35 145214
Santacroce R 1987 Somma Vesuvius Quad Ric Sci 114 252
Sarna-Wojcicki A 2000 Tephrochronology In Quaternary geochronology methods and applica-tions (ed J S Noller J M Sowers amp W R Lettis) AGU Reference shelf vol 4 pp 357377Washington DC American Geophysical Union
Sejrup H P Sjiquest holm J Furnes H Beyer I Eide L Jansen E amp Mangerud J 1989Quaternary tephrochronology on the Iceland Plateau north of Iceland J Quat Sci 4 109114
Sikes E L Samson C R Guilderson T P amp Howard W R 2000 Old radiocarbon agesin the southwest Pacimacrc Ocean during the last glacial period and deglaciation Nature 405555558
Stein R Nam S-I Grobe H amp Hubbersten H 1996 Late Quaternary glacial history andshort term ice rafted debris deg uctuations along the East Greenland continental marine In LateQuaternary palaeoceanography of the North Atlantic margins (ed J T Andrews W E NAustin H Bergsten amp A E Jennings) pp 135151 Geological Society London SpecialPublication
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 801
Stuiver M amp Grootes P M 2000 GISP2 oxygen isotope ratios Quat Res 53 277284
Stuiver M Reimer P J Bard E Beck J W Burr G S Hughen K A Kromer BMcCormac G Van der Plicht J amp Spurk M 1998 INTCAL 98 radiocarbon age calibration24 0000 cal BP Radiocarbon 40 10411083
Sweatman T R amp Long J V P 1969 Quantitative electron microprobe analysis of rock formingminerals J Petrol 7 332379
Turney C S M 1998 Extraction of rhyolitic ash from minerogenic lake sediments J Paleolim-nol 19 199206
Turney C S M amp Lowe J J 2001 Tephrochronology In Tracking environmental changes inlake sediments physical and chemical techniques (ed W M Last amp J P Smol) DordrechtKluwer Academic
Turney C S M Harkness D D amp Lowe J J 1997 The use of microtephra horizons tocorrelate Lateglacial lake sediments successions in Scotland J Quat Sci 12 525531
Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
van den Bogaard P amp Schmincke H 1985 A widespread isochronous Late Quaternary tephralayer in central and northern Europe Geol Soc Am Bull 96 15541571
van den Bogaard B Dordeg er W Sandgren P amp Schmincke H-U 1994 Correlating theHolocene records Icelandic tephra found in Schleswig-Holstein (northern Germany) Natur-wissenschaften 81 554556
Vernet G amp Raynal J-P 2001 Tephrostratigraphy of the Limagne revisited Implications forLateglacial and Holocene Prehistory In Tephras chronology archaeology (ed E Juvignparae ampJ-P Raynal) pp 111116 Dossiers de lrsquo ArchparaeoLogis no 1 France
Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
Vezzoli L 1991 Tephra layers in Bannock Basin (eastern Mediterranean) Mar Geol 1002134
von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
Walker M J C Bjorck S Lowe J J Cwynar L C Johnsen S Knudsen K-L WohlfarthB amp INTIMATE Group 1999 Isotopic events in the GRIP ice core a stratotype for the LatePleistocene Quat Sci Rev 18 11431150
Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
802 S M Davies and others
Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 799
Litt T amp Stebich M 1999 Bio- and chronostratigraphy of the Lateglacial in the Eifel regionGermany Quat Int 61 516
Litt T Brauer A Goslar T Merkt J Balaga K Muller H Ralska-Jasiewiczowa MStebich M amp Negendank J F W 2001 Correlation and synchronisation of Lateglacialcontinental sequences in northern Central Europe based on annually laminated lacustrinesediments Quat Sci Rev 20 12331249
Long D amp Morton A C 1987 An ash fall within the Loch Lomond stadial J Quat Sci 297101
Lotter A F Eicher U Siegenthaler U amp Birks H J B 1992 Lateglacial climatic oscillationsas recorded in Swiss lake sediments J Quat Sci 7 187204
Lowe J J 1992 Lateglacial and Early Holocene lake sediments from the Northern ApenninesItaly|pollen stratigraphy and radiocarbon dating Boreas 21 193208
Lowe J J 2001 Abrupt climatic changes in Europe during the last glacialinterglacial tran-sition the potential for testing hypotheses on the synchroneity of climatic events usingtephrochronology Global Planet Change 603 7384
Lowe J J amp Turney C S M 1997 Vedde Ash layer discovered in a small lake basin on theScottish mainland J Geol Soc Lond 154 605612
Lowe J J amp Walker M J C 2000 Radiocarbon dating the last glacialinterglacial transition(ca 14914 C ka BP) in terrestrial and marine records the need for new quality assuranceprotocols Radiocarbon 42 5368
Lowe J J amp Watson C 1993 Lateglacial and Early Holocene pollen stratigraphy of the northernApennines Italy Quat Sci Rev 12 727738
Lowe J J Birks H H Brooks S J Coope G R Harkness D D Mayle F E SheldrickC Turney C S M amp Walker M J C 1999 The chronology of palaeoenvironmental changesduring the Last GlacialHolocene transition towards an event stratigraphy for the BritishIsles J Geol Soc Lond 156 397410
Lowe J J Hoek W Z amp INTIMATE group 2001 Inter-regional correlation of palaeoclimaticrecords for the Last GlacialInterglacial transition a protocol for improved precision recom-mended by the INTIMATE project group Quat Sci Rev 20 11751187
Mackie E Davies S M Turney C S M Dobbyn K Lowe J J amp Hill P 2002 The useof Magnetic Separation Techniques to detect basaltic microtephra in last glacialinterglacialtransition (LGIT 1510 ka cal BP) sediment sequences in Scotland Scot J Geol (In thepress)
Mangerud J Lie S E Furnes H Kristiansen I L amp Liquest mo L 1984 A Younger Dryas ashbed in western Norway and its possible correlation with tephra beds from the Norwegian Seaand North Atlantic Quat Res 21 85104
Mangerud J Furnes H amp Jparaohansen J 1986 A 9000 year-old ash bed on the Faroe IslandsQuat Res 26 262265
Martini J 1970 Recherche de retombparaees volcaniques dans le sud-est de la France et la Suisseoccidentale Arch Sci 23 641674
Martini J amp Duret J J 1965 Note preliminaire sur la presence drsquo un niveau de cendres vol-caniques dans des sparaediments post-glaciaires des environs de Genmicroeve Arch Sci 18 587588
Mayewski P A Meeker L D Twickler M S Whitlow S Yang Q Lyons W B amp Pren-tice M 1997 Major features and forcing of high latitudes Northern Hemisphere atmosphericcirculation using a 110 000 year long glaciochemical series J Geophys Res 102 345365
Merkt J Muller H Knabe W Muller P amp Weiser T 1993 The Early Holocene Saksunarvatntephra found in lake sediments in NW Germany Boreas 22 93100
Narcisi B 1993 Segnalazione di un livello piroclastico di provenienza etnea nellrsquo area del Fucino(Italia Centrale) Quaternario 6 8792
Narcisi B 1996 Tephrochronology of a Late Quaternary lacustrine record from the Monticchiomaar (Vulture volcano southern Italy) Quat Sci Rev 15 155165
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
800 S M Davies and others
Newton A J amp Dugmore A J 1993 Tephrochronology of Core C from Lago Grande di Mon-ticchio In Paleolimnology of European Maar Lakes (ed J F W Negendank amp B Zolitschka)Lecture Notes in Earth Science vol 49 333348 Springer
Oldmacreld F Appleby P G amp Thompson R 1980 Palaeoecological studies of lakes in theHighlands of Papua New Guinea J Ecol 68 457477
Orsi G Drsquo Antonio M de Vita S amp Gallo G 1992 The Neapolitan Yellow Tureg a large mag-nitude trachytic phreatoplinian eruption eruptive dynamics magma withdrawal and calderacollapse J Volcanol Geotherm Res 53 275287
Paterne M Guichard F Labeyrie J Gillot P Y amp Duplessy J C 1986 Tyrrhenian Seatephrochronology of the oxygen isotope record for the past 60 000 years Mar Geol 72259285
Paterne M Guichard F amp Labeyrie J 1988 Explosive activity of the south Italian volca-noes during the past 80 000 years as determined by marine tephrochronology J VolcanolGeotherm Res 34 153172
Paterne M Labeyrie J Guichard F Mazaud A amp Maitre F 1990 Fluctuations of the Cam-panian explosive volcanic activity (south Italy) during the past 190 000 years as determinedby marine tephrochronology Earth Planet Sci Lett 98 166174
Pawse A Beske-Diehl S amp Marshall S A 1998 Use of magnetic hysteresis properties andelectron spin resonance spectroscopy for the identimacrcation of volcanic ash a preliminary studyGeophys J Int 132 712720
Pearce N J G Westgate J A amp Perkins W T 1996 Developments in the analysis of singleglass shards in volcanic deposits by laser ablation ICP-MS quantitative and single internalstandard multi-element methods Quat Int 3436 213227
Pearce N J G Westgate J A Perkins W T Eastwood W J amp Shane P 1999 Theapplication of laser ablation ICP-MS to the analysis of volcanic glass shards from tephradeposits bulk glass and single shard analysis Global Planet Change 21 151171
Pilcher J R amp Hall V A 1992 Towards a tephrochronology for the Holocene of the north ofIreland Holocene 2 255259
Ponel P amp Lowe J J 1992 Coleopteran pollen and radiocarbon evidence from the Prato Spillarsquo Drsquo succession N Italy C R Acad Sci Paris Sparaer II 315 14251431
Rose N L Golding P N E amp Battarbee R W 1996 Selective concentration and enumerationof tephra shards from lake sediment cores Holocene 6 243246
Ruddiman W F amp Glover L K 1972 Vertical mixing of ice rafted volcanic ash in NorthAtlantic sediments Geol Soc Am Bull 83 28172836
Ruddiman W amp McIntyre A 1981 The North Atlantic Ocean during the last deglaciationPalaeogeogr Palaeoclimatol Palaeoecol 35 145214
Santacroce R 1987 Somma Vesuvius Quad Ric Sci 114 252
Sarna-Wojcicki A 2000 Tephrochronology In Quaternary geochronology methods and applica-tions (ed J S Noller J M Sowers amp W R Lettis) AGU Reference shelf vol 4 pp 357377Washington DC American Geophysical Union
Sejrup H P Sjiquest holm J Furnes H Beyer I Eide L Jansen E amp Mangerud J 1989Quaternary tephrochronology on the Iceland Plateau north of Iceland J Quat Sci 4 109114
Sikes E L Samson C R Guilderson T P amp Howard W R 2000 Old radiocarbon agesin the southwest Pacimacrc Ocean during the last glacial period and deglaciation Nature 405555558
Stein R Nam S-I Grobe H amp Hubbersten H 1996 Late Quaternary glacial history andshort term ice rafted debris deg uctuations along the East Greenland continental marine In LateQuaternary palaeoceanography of the North Atlantic margins (ed J T Andrews W E NAustin H Bergsten amp A E Jennings) pp 135151 Geological Society London SpecialPublication
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 801
Stuiver M amp Grootes P M 2000 GISP2 oxygen isotope ratios Quat Res 53 277284
Stuiver M Reimer P J Bard E Beck J W Burr G S Hughen K A Kromer BMcCormac G Van der Plicht J amp Spurk M 1998 INTCAL 98 radiocarbon age calibration24 0000 cal BP Radiocarbon 40 10411083
Sweatman T R amp Long J V P 1969 Quantitative electron microprobe analysis of rock formingminerals J Petrol 7 332379
Turney C S M 1998 Extraction of rhyolitic ash from minerogenic lake sediments J Paleolim-nol 19 199206
Turney C S M amp Lowe J J 2001 Tephrochronology In Tracking environmental changes inlake sediments physical and chemical techniques (ed W M Last amp J P Smol) DordrechtKluwer Academic
Turney C S M Harkness D D amp Lowe J J 1997 The use of microtephra horizons tocorrelate Lateglacial lake sediments successions in Scotland J Quat Sci 12 525531
Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
van den Bogaard P amp Schmincke H 1985 A widespread isochronous Late Quaternary tephralayer in central and northern Europe Geol Soc Am Bull 96 15541571
van den Bogaard B Dordeg er W Sandgren P amp Schmincke H-U 1994 Correlating theHolocene records Icelandic tephra found in Schleswig-Holstein (northern Germany) Natur-wissenschaften 81 554556
Vernet G amp Raynal J-P 2001 Tephrostratigraphy of the Limagne revisited Implications forLateglacial and Holocene Prehistory In Tephras chronology archaeology (ed E Juvignparae ampJ-P Raynal) pp 111116 Dossiers de lrsquo ArchparaeoLogis no 1 France
Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
Vezzoli L 1991 Tephra layers in Bannock Basin (eastern Mediterranean) Mar Geol 1002134
von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
Walker M J C Bjorck S Lowe J J Cwynar L C Johnsen S Knudsen K-L WohlfarthB amp INTIMATE Group 1999 Isotopic events in the GRIP ice core a stratotype for the LatePleistocene Quat Sci Rev 18 11431150
Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
802 S M Davies and others
Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
800 S M Davies and others
Newton A J amp Dugmore A J 1993 Tephrochronology of Core C from Lago Grande di Mon-ticchio In Paleolimnology of European Maar Lakes (ed J F W Negendank amp B Zolitschka)Lecture Notes in Earth Science vol 49 333348 Springer
Oldmacreld F Appleby P G amp Thompson R 1980 Palaeoecological studies of lakes in theHighlands of Papua New Guinea J Ecol 68 457477
Orsi G Drsquo Antonio M de Vita S amp Gallo G 1992 The Neapolitan Yellow Tureg a large mag-nitude trachytic phreatoplinian eruption eruptive dynamics magma withdrawal and calderacollapse J Volcanol Geotherm Res 53 275287
Paterne M Guichard F Labeyrie J Gillot P Y amp Duplessy J C 1986 Tyrrhenian Seatephrochronology of the oxygen isotope record for the past 60 000 years Mar Geol 72259285
Paterne M Guichard F amp Labeyrie J 1988 Explosive activity of the south Italian volca-noes during the past 80 000 years as determined by marine tephrochronology J VolcanolGeotherm Res 34 153172
Paterne M Labeyrie J Guichard F Mazaud A amp Maitre F 1990 Fluctuations of the Cam-panian explosive volcanic activity (south Italy) during the past 190 000 years as determinedby marine tephrochronology Earth Planet Sci Lett 98 166174
Pawse A Beske-Diehl S amp Marshall S A 1998 Use of magnetic hysteresis properties andelectron spin resonance spectroscopy for the identimacrcation of volcanic ash a preliminary studyGeophys J Int 132 712720
Pearce N J G Westgate J A amp Perkins W T 1996 Developments in the analysis of singleglass shards in volcanic deposits by laser ablation ICP-MS quantitative and single internalstandard multi-element methods Quat Int 3436 213227
Pearce N J G Westgate J A Perkins W T Eastwood W J amp Shane P 1999 Theapplication of laser ablation ICP-MS to the analysis of volcanic glass shards from tephradeposits bulk glass and single shard analysis Global Planet Change 21 151171
Pilcher J R amp Hall V A 1992 Towards a tephrochronology for the Holocene of the north ofIreland Holocene 2 255259
Ponel P amp Lowe J J 1992 Coleopteran pollen and radiocarbon evidence from the Prato Spillarsquo Drsquo succession N Italy C R Acad Sci Paris Sparaer II 315 14251431
Rose N L Golding P N E amp Battarbee R W 1996 Selective concentration and enumerationof tephra shards from lake sediment cores Holocene 6 243246
Ruddiman W F amp Glover L K 1972 Vertical mixing of ice rafted volcanic ash in NorthAtlantic sediments Geol Soc Am Bull 83 28172836
Ruddiman W amp McIntyre A 1981 The North Atlantic Ocean during the last deglaciationPalaeogeogr Palaeoclimatol Palaeoecol 35 145214
Santacroce R 1987 Somma Vesuvius Quad Ric Sci 114 252
Sarna-Wojcicki A 2000 Tephrochronology In Quaternary geochronology methods and applica-tions (ed J S Noller J M Sowers amp W R Lettis) AGU Reference shelf vol 4 pp 357377Washington DC American Geophysical Union
Sejrup H P Sjiquest holm J Furnes H Beyer I Eide L Jansen E amp Mangerud J 1989Quaternary tephrochronology on the Iceland Plateau north of Iceland J Quat Sci 4 109114
Sikes E L Samson C R Guilderson T P amp Howard W R 2000 Old radiocarbon agesin the southwest Pacimacrc Ocean during the last glacial period and deglaciation Nature 405555558
Stein R Nam S-I Grobe H amp Hubbersten H 1996 Late Quaternary glacial history andshort term ice rafted debris deg uctuations along the East Greenland continental marine In LateQuaternary palaeoceanography of the North Atlantic margins (ed J T Andrews W E NAustin H Bergsten amp A E Jennings) pp 135151 Geological Society London SpecialPublication
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 801
Stuiver M amp Grootes P M 2000 GISP2 oxygen isotope ratios Quat Res 53 277284
Stuiver M Reimer P J Bard E Beck J W Burr G S Hughen K A Kromer BMcCormac G Van der Plicht J amp Spurk M 1998 INTCAL 98 radiocarbon age calibration24 0000 cal BP Radiocarbon 40 10411083
Sweatman T R amp Long J V P 1969 Quantitative electron microprobe analysis of rock formingminerals J Petrol 7 332379
Turney C S M 1998 Extraction of rhyolitic ash from minerogenic lake sediments J Paleolim-nol 19 199206
Turney C S M amp Lowe J J 2001 Tephrochronology In Tracking environmental changes inlake sediments physical and chemical techniques (ed W M Last amp J P Smol) DordrechtKluwer Academic
Turney C S M Harkness D D amp Lowe J J 1997 The use of microtephra horizons tocorrelate Lateglacial lake sediments successions in Scotland J Quat Sci 12 525531
Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
van den Bogaard P amp Schmincke H 1985 A widespread isochronous Late Quaternary tephralayer in central and northern Europe Geol Soc Am Bull 96 15541571
van den Bogaard B Dordeg er W Sandgren P amp Schmincke H-U 1994 Correlating theHolocene records Icelandic tephra found in Schleswig-Holstein (northern Germany) Natur-wissenschaften 81 554556
Vernet G amp Raynal J-P 2001 Tephrostratigraphy of the Limagne revisited Implications forLateglacial and Holocene Prehistory In Tephras chronology archaeology (ed E Juvignparae ampJ-P Raynal) pp 111116 Dossiers de lrsquo ArchparaeoLogis no 1 France
Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
Vezzoli L 1991 Tephra layers in Bannock Basin (eastern Mediterranean) Mar Geol 1002134
von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
Walker M J C Bjorck S Lowe J J Cwynar L C Johnsen S Knudsen K-L WohlfarthB amp INTIMATE Group 1999 Isotopic events in the GRIP ice core a stratotype for the LatePleistocene Quat Sci Rev 18 11431150
Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
802 S M Davies and others
Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
European tephrochronological framework for Termination 1 801
Stuiver M amp Grootes P M 2000 GISP2 oxygen isotope ratios Quat Res 53 277284
Stuiver M Reimer P J Bard E Beck J W Burr G S Hughen K A Kromer BMcCormac G Van der Plicht J amp Spurk M 1998 INTCAL 98 radiocarbon age calibration24 0000 cal BP Radiocarbon 40 10411083
Sweatman T R amp Long J V P 1969 Quantitative electron microprobe analysis of rock formingminerals J Petrol 7 332379
Turney C S M 1998 Extraction of rhyolitic ash from minerogenic lake sediments J Paleolim-nol 19 199206
Turney C S M amp Lowe J J 2001 Tephrochronology In Tracking environmental changes inlake sediments physical and chemical techniques (ed W M Last amp J P Smol) DordrechtKluwer Academic
Turney C S M Harkness D D amp Lowe J J 1997 The use of microtephra horizons tocorrelate Lateglacial lake sediments successions in Scotland J Quat Sci 12 525531
Turney C S M Lowe J J Wastegordm ard S Cooper R amp Roberts S J 2001 The developmentof a tephrochronological framework for the last glacialHolocene transition in NW EuropeIn Tephras chronology archeology (ed E Juvignparae amp J-P Raynal) pp 101109 Dossiers delrsquo ArchparaeoLogis no 1 France
van den Bogaard P 1995 40 Ar39 Ar ages of sanidine phenocrysts from Laacher See Tephra(12 900 yrs BP) chronostratigraphic and petrological signimacrcance Earth Planet Sci Lett133 163174
van den Bogaard P amp Schmincke H 1985 A widespread isochronous Late Quaternary tephralayer in central and northern Europe Geol Soc Am Bull 96 15541571
van den Bogaard B Dordeg er W Sandgren P amp Schmincke H-U 1994 Correlating theHolocene records Icelandic tephra found in Schleswig-Holstein (northern Germany) Natur-wissenschaften 81 554556
Vernet G amp Raynal J-P 2001 Tephrostratigraphy of the Limagne revisited Implications forLateglacial and Holocene Prehistory In Tephras chronology archaeology (ed E Juvignparae ampJ-P Raynal) pp 111116 Dossiers de lrsquo ArchparaeoLogis no 1 France
Vernet G Raynal J P Fain J Miallier D Montret M Pilleyre T amp Sanzelle S 1998Tephrostratigraphy of the last 160 ka in western Limagne (France) Quat Int 4748 139146
Vezzoli L 1991 Tephra layers in Bannock Basin (eastern Mediterranean) Mar Geol 1002134
von Grafenstein U Erlenkauser H Brauer A Jouzel J amp Johnsen S J 1999 A mid Euro-pean decadal isotope-climate record from 15 500 to 5 000 yrs BP Science 284 16541657
Waelbroeck C Duplessy J-C Michel E Labeyrie L Paillard D amp Duprat J 2001 Thetiming of the last deglaciation in North Atlantic climate records Nature 412 724727
Walker M J C 1995 Climatic changes in Europe during the last glacialinterglacial transitionQuat Int 28 6376
Walker M J C Bjorck S Lowe J J Cwynar L C Johnsen S Knudsen K-L WohlfarthB amp INTIMATE Group 1999 Isotopic events in the GRIP ice core a stratotype for the LatePleistocene Quat Sci Rev 18 11431150
Walker M J C Bjorck S amp Lowe J J 2001 Integration of ice core marine and terrestrialrecords (INTIMATE) from around the North Atlantic region an introduction Quat SciRev 20 11691174
Wastegordm ard S Bjorck S Possnert G amp Wohlfarth B 1998 Evidence for the occurrence ofVedde Ash in Sweden radiocarbon and calendar age estimates J Quat Sci 13 271274
Wastegordm ard S Turney C S M Lowe J J amp Roberts S J 2000a The Vedde Ash in NWEurope distribution and geochemistry Boreas 29 7278
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
802 S M Davies and others
Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
802 S M Davies and others
Wastegordm ard S Wohlfarth B Subetto D A amp Sapelko T V 2000b Extending the knowndistribution of the Younger Dryas Vedde Ash into northwestern Russia J Quat Sci 15581586
Wastegordm ard S Bjorck S Grauert M amp Hannon G E 2001 The Mjparaauviquest tn tephra and otherHolocene tephra horizons from the Faroe Islands a link between the Icelandic source regionthe Nordic seas and the European continent Holocene 11 101109
Westgate J A amp Gorton M P 1981 Correlation techniques in tephra studies In Tephra studies(ed S Self amp R S J Sparks) pp 7394 Dordecht Reidel
Witte H J L Coope G R Lemdahl G amp Lowe J J 1998 Regression coeplusmn cients of thermalgradients in northwestern Europe during the last glacialHolocene transition using beetleMCR data J Quat Sci 13 435445
Zielinski G A Mayewski P A Meeker L D Whitlow S I amp Twickler M S 1996 A110 000 year record of explosive volcanism from the GISP2 (Greenland) ice core Quat Res45 109118
Zolitschka B Negendank J F W amp Lottermoser B G 1995 Sedimentological provenance anddating of the Early Holocene volcanic eruption of the Ulmener Maar (Vulcaneifel Germany)Geol Rundsch 84 213219
Phil Trans R Soc Lond A (2002)
on September 20 2011rstaroyalsocietypublishingorgDownloaded from
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