Stratigraphy and stage boundaries in reference sections of the Upper Cretaceous Chalk in the east of...

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Cretaceous Research 26 (2005) 157e169

Stratigraphy and stage boundaries in reference sectionsof the Upper Cretaceous Chalk in the east of theParis Basin: the ‘‘Craie 700’’ Provins boreholes

Francis Robaszynskia,*, Bernard Pomerolb, Edwige Masurec,Jean-Pierre Bellierc, Jean-Francois Deconinckd

aFaculte Polytechnique de Mons, 9 rue de Houdain, 7000 Mons, BelgiquebUniversite Paris e Val de Marne, Avenue du General de Gaulle, 94010 Creteil, France

cDepartement de Geologie sedimentaire-micropaleontologie, Universite P. et M. Curie, ESA 7073 CNRS,

4 place Jussieu, T 56, 4eme etage, 75252 Paris Cedex 05, FrancedUniversite de Bourgogne, UMR 5561 CNRS, Biogeosciences, 6 Boulevard Gabriel, 21000 Dijon, France

Received 17 February 2003; accepted in revised form 5 October 2004

Available online 11 March 2005

Abstract

The Provins boreholes (Poigny: Craie 701, and Sainte-Colombe: Craie 702) drilled in 1999 as part of the ‘‘Craie 700’’ projectinitiated by the Paris Basin Geologists’ Association provide reference sections for the Upper Cretaceous of the eastern part of theParis Basin. The lithology of the Cretaceous drilled at Poigny and Sainte-Colombe is presented in two logs displaying major litho-

events that provide lines of correlation. Bio-events are expressed by the appearance/disappearance of index species of fossils.Foraminifera give a biozonation close to that defined by previous work on the Anglo-Paris Basin. Some of these bio-events providea second set of lines useful for correlation. From the results of these lithobiostratigraphic studies, stage boundaries from the UpperAlbian to the Campanian have been located with a maximum uncertainty of a few metres.

The main results are as follows: (1) below the Tertiary cover, the sedimentation of the Chalk seems to have been continuous: nomajor hiatuses have been identified from the Campanian down to the Cenomanian; (2) the Upper Albian was reached at the base ofthe Sainte-Colombe Borehole; (3) in this borehole, the stages have approximately the following thicknesses: Upper Albian

‘‘Vraconian’’ (Vraconnien) (13 m), Cenomanian (58 m), Turonian (180 m), Coniacian (80 m), Santonian (70 m), Campanian (217 m;about 265 m at Poigny); (4) the Chalk succession is 40e50 m thicker at Poigny than at Sainte-Colombe; (5) lines of correlation basedon litho- and bio-events and stage boundaries are sub-parallel; (6) a 17-m-thick dolomitic body occurring only in the Sainte-

Colombe Borehole is located at the transition between the lower and upper parts of the Campanian; (7) clay-rich beds correspondingto kaolinite-bentonites used for long-distance correlations are recognized in the Turonian and are very accurate marker beds.

Three tectonic phases are evident in the two boreholes. The pre-Ilsede phase is discrete in the Middle Turonian. The early Ilsedephase begins in the lower part of the Coniacian. The main Ilsede phase reduces the thickness of the middle part of the Coniacian

(foraminiferal biozone S/b thin or absent). The Wernigerode phase seems to have reduced the thickness of the upper part of theSantonian (?lack of crinoid zones). The development of a thick dolomitic body in the Sainte-Colombe Borehole, and the presence ofbored surfaces bounding the same stratigraphic interval in the Poigny Borehole, may be related to the Peine phase, active between

the early and late Campanian.� 2005 Elsevier Ltd. All rights reserved.

Keywords: Upper Cretaceous; Chalk; Paris Basin; Stage boundaries; Bio-events; Tectonic phases

* Corresponding author.

E-mail address: [email protected] (F. Robaszynski).

0195-6671/$ - see front matter � 2005 Elsevier Ltd. All rights reserved.

doi:10.1016/j.cretres.2004.10.003

mailto:[email protected]

http://www.elsevier.com/locate/CretRes

158 F. Robaszynski et al. / Cretaceous Research 26 (2005) 157e169

1. Introduction

The ‘‘Craie 700’’ programme was initiated during the1990s by the Paris Basin Geologists’ Association and theFrench Compagnie Generale de Geophysique. Two deepboreholes were drilled in 1999 in the Chalk of the ParisBasin, close to Provins, at Poigny and Sainte-Colombe(Fig. 1), where the Chalk succession reaches its maximumthickness (more than 600 m). The main objective was toidentify the origin of variations in the velocity of seismicwaves in the chalks because for the past 50 yearspetroleum exploration using seismic reflection has beenfaced with this problem (Hanot and Renoux, 1991;Megnien and Hanot, 1997; Hanot and Thiry, 1999;Hanot, 2000). The boreholes were continuously coredwith recovery reaching 98%. Coring was stopped ata depth of 700 m in the Cenomanian at Poigny and in theUpper Albian (‘‘Vraconian’’) at Sainte-Colombe.

The most striking feature is the occurrence of a 17-m-thick dolomitic development located at a depth of 168e185 m in the Sainte-Colombe Borehole, while the samestratigraphic interval drilled at Poigny shows the usualchalk.

The continuously cored succession provides anexceptional opportunity to describe the lithology andto study macro- and microfossil assemblages, includingammonites, inoceramids, echinoids, brachiopods, fora-minifera and dinoflagellate cysts. Some ostracods werefound, and the rich nannofossil content was also studied(Janin, 2000). Preliminary results were presented in June2000 at the French Academy of Sciences and partly

published in a special issue of the Bulletin d’Informationdes Geologues du Bassin de Paris (Megnien and Hanot,2000). Since that publication (Robaszynski and Bellier,2000; Robaszynski et al., 2000), several stratigraphicinterpretations of lithological units, key marl seams andforaminiferal biozones have been improved and corre-late better with those of southern England.

The objectives of this paper are to present the mainlitho- and bio-events identified throughout the strati-graphic succession and to propose stage boundarieswithin, and correlations between, the two boreholes.

2. Lithology and litho-events

The cores were first described in detail at a scale of1/20 (Bernaux et al., 1999) and then simplified at a scaleof 1/100 (Pomerol, 2000; Robaszynski, 2000). The mainlithological units are presented below for the twoboreholes: Poigny 701 and Sainte-Colombe 702.

2.1. Poigny Borehole

The Cretaceous recovered beneath the Tertiary cover,from 34.75 to 700 m comprises 11 lithological units,including some key marker beds previously describedfrom outcrops in the Anglo-Paris Basin (nineteenthcentury authors and, more recently, Robaszynski et al.,1980; Bailey et al., 1983, 1984; Gale et al., 1988;Mortimore et al., 2001, with extensive literature). Fromtop to bottom, the units are (Fig. 2):

Brussels

Vosg

es

Morvan

ArmoricanMassif

Boulonnais

Belgium

Tours

Rouen

Paris500

Orléans Seine

700

600

400

300

200

Late Cretaceousoutcrop limits

700

Central Massif

isopachsof the chalk

Normandy

100 km

N

English Channel

Provins

Troyes

Mons

PoignySte Colombe

Fig. 1. Location of Poigny and Sainte-Colombe Boreholes on a map showing isopachs of the Chalk.

159F. Robaszynski et al. / Cretaceous Research 26 (2005) 157e169

Rotalipora

Globorotalites

C/c

S/a

T/c

T/b

T/a

TU

RO

NI

AN

CEN

OM

ANIA

N

S. polonica

Reuss.szajn. praec.

Gavel.cristata

S/clow.

S/cup.

S/d

SAN

TON

IAN

CO

NIA

CIA

N

R. szaj.pr.

G.clementiana

S/f

S/g

low

erpa

rt

B.decor

G.stellig.

G.mont.

B.inc.

S/h

S/i

S/k

S/j

CA

MP

AN

IA

N

upp e

rpa

rt

POIGNY 701

37.6

48.253.4

6470.379.1

89.3

100.4

109.4116.3124

134.1

143.5

153.2

163.5172

185.6

197.9

58.1

316.2

304.5293.9

284.4

273.9

263.8

242.4239.1234.2

220.1

209.6

405.2

393.6

381.9

371.1

362.7

351.8

340.1

328.4

251.4

499.5

487.1

477.5

465.2

454.2445.5435.5

424.9416.9

579.9

566.9564.1

548.4

537.6

526.6519.2510.1

615.9609.9

598.9

652.5

628.05

640.3

651.8

672.15670.8664.7

685.1

mic

rite

spic

ules

Gavel.

spRotalipora

cushmani

Dicarinella

sp.

Globorotalites

sp.

cf. Stensioeina

sp.(

prim

.)Globotruncana

gr. bulloides

Marginotruncana

cfpseudolinneiana

Stensioeinagranulata

cf.kelleri

Globorotalites

gr.michelinianus

Osangularia

spp.

Reussella

gr.kelleri

Gavelinellaarnagerensis

Stensioeinapol onica

Gavelinellacristata

Cib.beaumont

R.sz.praec

Gavel inellastelligera

Gavelinellacl ementiana

Gavelinellaclementiana

(sm

ooth

)Stensioeina

gr.pommerana

Verneuilina

sp.

Globotruncana

gr.arca

Bolivinoidesdecoratus

Gavelinella

cf.usakensis

Gav.monterelensi s

Cibic.voltziana

Neoflabellinapraereticul ata

Bolivinoides

gr.australis

(5pu

st.)

Bolivinaincrassata

Gl oborotal iteshi ltermanni

Bolivinoides

gr.austral is( 6

pust

.)

..

grey chertylimestones

nodular flaserchalk

calcisphereand flaser

chalk with marlseams

Magas

chalk without flint

Old Nore Marl

tubular flint

Cal

cisp

here

s

S/e

thin sectionsInoc. crippsi

ph.ph.

700

674.2

654.6

646.6

622.1

grey, marly chalk

grey, flaser limestone

Mytiloides

Plenus Marls

600

Caburn Marls

Southerham M.breccia hg

520.7

508.1

448.4

BridgewickMarls

Lewes tubular flint

500

“marbled”chalk

Streakychalk

bored marly horizonnodules

427.6Shoreham Marllong, grey bioturb.

nodules

flintychalk

Zoophycos

flints

Cladoceramus

345

371

flintychalk

Zoophycos

flints

long, grey bioturb.

paramoudraflints

Zoophycos

flints

chalkwith

scatteredflints

flintychalk

164

140

soft whitechalk withfew flints

bored surfaces

bored surfaces

carious flint

lithological units and marker-beds foraminifera34.75 m

200

300

100

400

.. .

Micraster sp.

ZoophycosCuilfail

S. granulata granulata

R. cf. kelleri T/S

S/b

S.granulatagranul ata

glauc. phosph.

M.M.

Chalkwithout

flint

285

X

X

X

X

X

X

X X

XX

XX

X

X

X

X

X

X

poorly preservedoccurrence

X

chalk

phosphate nodules levelchertnodulesflasersbored level

marl seamsdolomiteZoophycos flintflintsmarly chalk

sandy limestones

Fig. 2. The Poigny Borehole: lithological units, bio-events, foraminiferal biozones and inferred stage boundaries.


34.75e140 m. Soft white chalk with a few flints. Thisis a bioturbated chalk with scattered black flints in theupper half of the unit and very rare flints in the lowerhalf. Between 92 and 106 m numerous specimens ofMagas chitoniformis (Schlotheim) (ZM. ‘‘pumilus’’auct.) were found.

140e164 m. Soft chalk without flints. This biotur-bated unit is bounded by two slightly bored surfaces atthe top and bottom. A breccia-like level is present at158.30 m and may represent an incipient hardground.This unit is considered to be equivalent to the dolomiticbody of the Sainte-Colombe Borehole on the basis ofkey foraminiferal entries.

164e185 m. Flinty chalk. This is a unit of off-whitechalk with grey bioturbation. The upper third ischaracterized by Zoophycos flints and the lower thirdby some vertical flints looking like small paramoudras.The base is bounded by a marl seam 3e4 cm thickinterpreted as Old Nore Marl.

285e448.40 m. Flinty chalk. This unit can be sub-divided into four subunits: (1) the upper part consists of60 m of hard chalk with flint bands and some Zoophycosflints; long grey bioturbations are present at 320e322 m;a crinoid fragment was found near the top where theSantonian/Campanian boundary may be situated; (2)26 m of chalk without flints, the base being markedby numerous inoceramid fragments (Platyceramus gr.mantelli?, ?Cladoceramus cf. undulatoplicatus, indicatingthe basal Santonian); (3) 56.60 mof hard chalk with blackand grey flints in about 15 m in the middle part, and longgrey bioturbations in the lower part, resting on a slightlybored horizon equivalent to the Shoreham Marl, whichoccurs in the lower part of the Santonian; (4) 20.80 m ofwhite chalk with hard nodules in the lower part.

448.40e508.10 m. ‘‘Marbled’’ chalk. In the upperpart, several metres of grey, streaky chalk without flintscan be interpreted as the Cuilfail Zoophycos Beds,representing the uppermost Turonian. Below is a greyishhard chalk with large grey bioturbations and some flintsat the base.

508.10e520.70 m. Chalk with tubular flints. Indescending order the following were recorded from thelevels noted: 508.20 m, some zoned tubular flints;510.50 m, hard nodular chalk, flints and Zoophycos;512.50 m, zoned tubular flints that may correlate withthe Lewes Tubular Flint; 513 m, nodules and breccia-like hard chalk; 515 m, fragments of Micraster sp.;517 m, nodules and breccia-like hard chalk. The LewesMarl is missing above this unit.

520.70e622.10 m. Calcisphere and flaser hard chalkwith numerousmarl seams. This unit consists of 101.40 mof a very hard chalk including at least 22 marl seams andfour nodular and breccia-like bands. The hardness islinked to the calcisphere content and to the very highdegree of diagenesis by compaction. From the top,several marl seams of volcanic origin are recognized

and documented below (kaolinite clay with negativeEuropium anomaly, cf. Deconinck et al., 2005): 523 m,Bridgewick Marl; 550.50 m, Caburn Marl; 566.70 m,Southerham Marl. As there are no definite criteria, it ismore difficult to attribute with certainty the other marlseams but it is very likely that the Glynde, New Pit,Malling and Gun Gardens Marls are represented.

622.10e646.60 m. Nodular flaser chalk. This isa succession of very hard flaser chalk, nodular, withmany inoceramid bioclasts (0.5e1.5 cm). Four marllayers (or concentrations of flasers) are noted at 624.90,630.70, 633.30 and 636.50 m. This lithologic unitroughly correlates with the Grand Blanc-Nez Forma-tion, named in 1980 in the Boulonnais cliffs (Robaszyn-ski et al., 1980), with which the Holeywell Beds(Mortimore, 1983, 1986: later the Holeywell NodularChalk Member; Bristow et al., 1997) correspond.

646.60e654.60 m. Grey marly chalk. The marly na-ture of this unit is clearly evident on resistivity andgamma-ray logs where it has the shape of the PlenusMarl (uppermost Cenomanian). This interpretation isconfirmed by the highest occurrence of the planktonicforaminiferan Rotalipora cushmani (Morrow) at651.80 m and the presence of ‘‘filaments’’ at 652.60 m(planktonic micro-bivalves, elsewhere frequent in thePlenus Marl). Unfortunately, none of the beds definedby Jefferies (1963) in the Plenus Marl of the Anglo-ParisBasin is differentiated.

654.60e674.20 m. Grey flaser limestone. This isessentially composed of calcispheres cemented withcalcite and partly with dolomite. The base is markedby a conglomerate 40 cm thick consisting of 2e5-cmlimestone pebbles and 2e8-mm phosphatic and glauco-nite grains. A marl seam is present at 660.40 m.

674.20e700 m. Grey, cherty limestone. This is a veryhard grey limestone, with opalescent bluish cherts andsome silicified sponge and bivalve fragments. In thinsections it shows, in a carbonate-marl-silt background,some calcispheres, quartz grains, bivalve bioclasts, andglauconite and phosphate grains. Two glauconitic gravellevels are present at 680.60 and 690.90 m. A fragment ofInoceramus cf. crippsi was noted at 697 m.

2.2. Sainte-Colombe Borehole

In the Cretaceous succession, cored from 82.40 to700 m, 11 lithological units showing thicknesses andcharacteristics equivalent to those of the PoignyBorehole are recognized (Fig. 3). However, the lower-most part of the succession (659.40e685.40 m), corre-sponding to the grey limestones with cherts, overlies anadditional unit (685.80e700 m) that consists of greylimestones containing common quartz grains, spongespicules and silicified bivalves. This facies may be anequivalent of the ‘‘gaize’’ that crops out in the easternpart of the Paris Basin. In addition, the dolomitic body


S/d

S/c

S/k

S/j

?S/iS/h

S/g

S/f

S/e

?T/b

T/c

S/a

?S/bS/c

upper

lower

CA

MP

AN

IA

NSA

NTO

N.

CO

NIA

CIA

NT

UR

ON

IA

NC

ENO

M.

A LB.

low

er

pa

rtu

pp

er

pa

rtT/S

Rotalipora

INOCERAMIDS : I. labiatus (debris)

C/c

T/a

STAGESDepth SAINTE - COLOMBE 702

100

200

300

400

500

600

700

m +42.10

ammonites

I. crippsi

Mytiloides mytiloides

O. cuvieri

Inoceramuscuvieri

Micraster sp.

Cr. waltersdorf

Volviceramusinvolutus

Cladoceramusundulatoplicatus

O. pilula

Magas

82.40

Cuilfail Beds

dolomitic chalk

687.2

659.4

638.2

630.25

608.9

Southerham M.

Caburn Marl

Bridgewick M.

496.6

509.4

Zoophycosflints

285.4

168

185

Zoophycosflints

Lewes tubul. fl.

Shoreham Marl430.5

369.7

346.1

449.6

M. mytiloides

grey sandylimestone

grey, chertylimestone

nodularflaserchalk

calcisphereand

flaser chalkwith marl

seams

tubular flint

“marbledchalk”

nodules

very few flint

paramoudraflint

scattered flints

soft whitechalk withfew flints

91.8

107.4

121.4

133.6

143153.1162.1165.2

186197208.4

216.8226

238246.9

255266.8274.6281.3

293.75

305.4316.1

328.1

343.6

358.8366.45

377.6

389.5396.8

408.8

420.2

431.6

446.4

470472.3485.7

500.9

516.2

554.65

565.9

580.2584.4591.55600.15607.85609.95611.6617.2626.1630637.6642.3650.35653.6657.65

685.5687.2694.5694.7697.6

AMMONITESPleurohoplites (Pleuroh.) sp.Pleurohoplites (Arraphoceras) cf. studeri

?

Globorotalites

spp.

Osangularia

spp.

Dicari nella&Marg in otruncana

spp.

Gave line llaarnager ensi s

Stensio einapolonica

Ga veline llacristata

Ci bici de sb eaumonti anus

Gavelinellastelligera

Gavelinellaclementiana“typica”

“fila

me n

ts”

Rotalipora

gr.cush mani

Whiteinella

spp.

Praeglobotruncana

spp.

Whiteinella

cf.prae helv eti ca

Bolivinaincrassata

Neofl.praereticulata

Globorotaliteshiltermanni

Bolivinoidesstrigillatus

Bolivinoidesaustralis

Gavellinellamonterelensis

Boli vinoid esdecoratus

Bolivinoidesculverensis

Gavelinellaclementiana“costata”

Ste nsioeinapommerana

Gave linellausa kensis

Reussellaszajn oc haepraecurso r

Stens.exsc.&

exsc.gracilis

Loxostomum

eleyi

Stensioeinag ra nulatagranulata

Globotruncana

cf.bulloides

Stensioeina

gr.granulata

cf.kelleri/levis

G.arnag./(R.cf kelleri)

S. granulata granulata

Stensioeina polonica

R. szajn. praec.

G. cristata

G. clement.

Bol. decor.

G.m.

B.i.

“Vra

coni

an”

O. cordier.

Cib.voltzi ana

lithologic unitsmarker beds

I. virgatus

glauc. phosph.

grey, flaserlimestone

?C. woollgariM. subhercy.

mic

rite

calc

isph

eres

poorly preservedoccurrence

X

thin sections

Early

Mid

d le

Late

flintychalk

Old Nore Marl

flintychalk

Lewes M.

Plenus Marl

O.mantellianaI. pictus

X

X

X

XX

X

X

X

X

X

X

X

X

X

X

X

foraminifera

Fig. 3. The Sainte-Colombe Borehole: lithological units, bio-events, foraminiferal biozones and inferred stage boundaries. For key, see Fig. 2.


responsible for the high seismic velocities occursbetween 168 and 185 m. The 12 lithological units areas follows, from top to bottom:

82.40e168 m. Soft white chalk with few flints. Thesmall brachiopod Magas chitoniformis (ZM. pumilusauct.) is present between 102 and 132 m.

168e185 m. Dolomitic unit. This is a brownish harddolomitic chalk with grey Zoophycos bioturbations andseveral Zoophycos flint levels, as at 173.60 m. The unit isnot present in the Poigny Borehole but may correlatewith the chalk between two slightly bored levels showingthe same entries of Bolivinoides decoratus near the baseand Gavelinella monterelensis at the top. Any dolomiticchalk cited in literature from outcrops in the Paris Basincan be compared to this thick unit.

185e285.40 m. Flinty chalk. Zoophycos flints arepresent in the upper part and paramoudra-like flintsnear the base, which is bounded by a marl seam 2 cmthick interpreted as Old Nore Marl.

285.40e449.60 m. Flinty chalk subdivided into foursubunits: (1) 60.70 m of hard white bioturbated chalkwith Zoophycos flints between 290 and 293.60 m,characteristic of the basal Campanian; numerous frag-ments of Echinochorys sp. in the upper part andMicraster sp. between 325 and 329 m; (2) 23.60 m ofchalk without flints in the upper part but with someflints at the base, which is marked by the presence ofCladoceramus undulatoplicatus at 369.70 m, the markerinoceramid species for the basal Santonian; (3) 60.80 mof bioturbated chalk, with black and grey flints andinoceramid fragments (Platyceramus sp. at 397.60e400.15 m and Volviceramus involutus at 410.20e412.40 m) marking the middle part of the Coniacian.The base rests on a marl layer with Chondrites at430.50 m, very probably equivalent to the ShorehamMarl; (4) 19.10 m of white chalk with flints in the upperpart and nodules in the lower part.

449.60e496.60 m. ‘‘Marbled’’ chalk. Marly streakychalk without flints in the upper part may represent theCuilfail Beds (uppermost Turonian). Near the base, at493.60 m, are hard nodular and breccia-like chalks(hardground?) resting on a marl at 496.60 m interpretedas the Lewes Marl (absent from the Poigny Borehole).

496.60e509.40 m. Chalk with tubular flints. This isa white to grey, bioturbated and flaser-structured chalk,with zoned tubular flints, a hardground (501.75 m) andnodules (505.70 m). The base rests on a marl seam(upper Bridgewick Marl).

509.40e608.90 m. Calcisphere and flaser chalk withabout 20 marl seams. Several specimens of Inoceramuscuvieri were found between 566.30 and 593.50 m.

608.90e630.25 m. Nodular flaser chalk with numer-ous bioclasts and a flood of Mytiloides mytiloides(Lower Turonian) between 608.80 and 619.15 m.

630.25e638.20 m. Grey marly chalk (Plenus Marl).Presence of Inoceramus pictus at 635.15 and 645.50 m

(uppermost Cenomanian). The highest planktonicforaminiferan, Rotalipora cushmani, was found in thinsections at 637.60 m.

638.20e659.40 m. Grey flaser limestone. At the baseare two horizons of grey nodular limestone withglauconite and phosphate grains. I. pictus was foundat 645.10 and 645.70 m and Orbirhynchia cf. mantellianaat 648.80 m.

659.40e687.20 m. Grey cherty limestone. A flood offragments of Inoceramus virgatus is present at 667.75 m,and I. crippsi, indicating the basal Cenomanian, wasfound at 668.15 m.

687.20e700 m. Grey sandy limestone (‘‘gaize’’). Thisunit comes below the cherty limestone and was notreached in the Poigny Borehole. Thin sections showsmall quartz grains and sponge spicules. In spite of theirhardness the cores yielded silicified sponges andbivalves, and three fragments of ammonites: two ofPleurohoplites (Pleurohoplites) sp. at 694.50 m and oneof Pleurohoplites (Arraphoceras) cf. studeri (Pictet andCampiche) at 697.60 m. The distribution of the latterform is restricted to the Upper Albian (‘‘Vraconian’’).

2.3. The Turonian clay-rich beds

In the Turonian chalk of north-west Europe, clay-rich beds are common and can be correlated fromEngland to Germany (Wray, 1999; Vanderaveroet et al.,2000). Some of these, including the Glynde, South-erham, Caburn, Bridgewick and Lewes marls, arebentonites. X-ray diffraction analyses of the clayfraction of Turonian clay-rich beds from the Poignyand Sainte-Colombe boreholes reveal an unusualoccurrence of authigenic kaolinite (Deconinck et al.,2005). According to litho- and biostratigraphic data, theSoutherham, Caburn and Bridgewick marls are recog-nized and correlated in both boreholes, whereas theLewes Marl is identified only in the Sainte-ColombeBorehole (Fig. 4).

Thanks to the X-ray diffraction analysis of theTuronian marl-seam marker beds, a re-interpretationof the various marl horizons has been possible, furtherto the publication of Robaszynski (2000).

3. Biostratigraphy and bio-events

During the visual core description of the boreholes,some well-preserved macrofossils were found, some ofwhich have been determined to species. Occasionally,abundant bioclasts may correspond to bio-events.

3.1. Macrofauna and bio-events in theSainte-Colombe Borehole

About 20 horizons contain macrofaunas thatcorrespond to significant bio-events useful for


Fig. 4. Correlation of kaolinite clay-rich beds corresponding to bentonites.

dating. From base to top the occurrences are asfollows:

697.60 m: Pleurohoplites (Arraphoceras) cf. studeri(Pictet and Campiche).

694.50 m: Pleurohoplites (Pleurohoplites) sp.: twoammonites (determined by F. Amedro) indicate a lateAlbian (Z‘‘Vraconian’’, in French, ‘‘Vraconnien’’) age.

668.15 m: Inoceramus crippsi (Mantell), marks thebase of the Cenomanian.

667.75 m: Inoceramus virgatus (Schlueter), typicallyEarly Cenomanian.

648.80 m: ?Orbirhynchia mantelliana (d’Orbigny),Middle Cenomanian.

654.70e645.10e635.15 m: Inoceramus pictus J. de C.Sowerby, uppermost Cenomanian.

619.15e608.80 m: Mytiloides mytiloides (Mantell),Early Turonian.

608.00 m: Orbirhynchia cuvieri sensu Pettit nond’Orbigny, Early Turonian.

605.20 m: Mytiloides subhercynicus (Seitz), typicallyMiddle Turonian.

604.50 m: ?Collignoniceras woollgari (Mantell), baseof the Middle Turonian.

593.50e569.10e566.30 m: Inoceramus cuvieri (J. So-werby), Middle Turonian.

499.00 and 497.20 m: Sternotaxis plana (Mantell),Late Turonian, equivalent of the ‘‘Chalk Rock’’.

482.40 m: ?Micraster sp.444.25 m: ?Cremnoceramus waltersdorfensis (Andert),

topmost Turonian to lower part of the Coniacian.413.40e410.20 m: Volviceramus involutus (J. de C.

Sowerby), middle part of the Coniacian, equivalent tothe ‘‘Craie de Maillot’’.

400.15e397.60 m: Platyceramus sp.369.70 m: Cladoceramus undulatoplicatus (Roemer),

base of the Santonian.274.00e273.00 m: Echinocorys sp., ?Offaster pilula

(Lamarck), lowermost part of the Campanian.132.00e125.00 m: abundant Magas chitoniformis

(Schlotheim)ZMagas ‘‘pumilus’’ auct., upper partof the Campanian, equivalent to the ‘‘Craie deMontereau’’.

109.00e102.00 m: Magas chitoniformis.

Abundant fossils also occur at Poigny, except for the‘‘Vraconian’’ ammonites, as the interval in which theyoccur was not reached in this borehole.


3.2. Foraminiferal biozonation

In both boreholes, foraminifera have been extracteddespite the hardness of most of the chalk samples.The vertical distribution of the significant species(Robaszynski and Bellier, 2000) shows a biozonationsimilar to that proposed byMonciardini and used inmostgeological maps of the Paris Basin (1978, 1980, and inPomerol et al., 1985; cf. Robaszynski andAmedro, 2001).

Fifteen benthic foraminiferal biozones are distin-guished. Their limits correspond to biohorizons thatcoincide with the lowest and highest occurrences ofparticular species (Figs. 2, 3). Using biozonation andbio-events, it is possible to draw correlations betweenthe boreholes.

The main events are as follows: (1) the highestRotalipora cushmani (Morrow) lies within the PlenusMarls (high Upper Cenomanian); this line is the base ofthe T/a zone; (2) the lowest Reussella cf. kelleriVassilenko or the lowest Gavelinella arnagerensis Sol-akius (ZG. cf. vombensis auct.) is present in the UpperTuronian; base of the T/S zone; (3) the lowest Stensioeinagranulata granulata (Olbertz), above the Turonian/Coniacian boundary; about in the middle of theConiacian; in T/a zone; (4) the lowest Stensioeinapolonica Witwicka, a little below the Coniacian/Santo-nian boundary; base of the upper S/c zone; (5) the lowestReussella szajnochae praecursorDeKlasz, above the baseof the Santonian; base of the S/d zone; (6) the lowestGavelinella cristata GoelZG. pseudoexcolata (Kalinin),senior synonym; within the Santonian; base of the S/ezone; (7) the lowest Gavelinella clementiana (d’Orbigny)forma typicaMarie (Marie, 1941; Teherani, 1968); withinthe lower part of the Campanian; base of the S/g zone;(8) successive lowest Bolivinoides decoratus (Jones): baseS/h, and lowestGavelinella monterelensis (Marie): base S/j; between the lower and upper parts of the Campanian;(9) the lowest Bolivina incrassata Reuss in the upper partof the Campanian; base of the S/k zone.

3.3. Dinoflagellate cyst bio-events

The main bio-events are as follows (Masure, 2000):increasing frequency of Microdinium? crinitum Davey(base of the Cenomanian), extinction of Epelidosphaer-idia spinosa Cookson and Hughes (Middle Cenoma-nian), appearance of the genus Areoligera (upper part ofthe Campanian).

4. Correlation of the boreholes and location

of the stage boundaries

A consistent set of correlation lines between theboreholes is presented, using a combination of litholog-ical units, and litho- and bio-events (Fig. 5). Stage

boundaries of the Cretaceous were discussed during theBrussels Symposium in 1995 and recommendations fortheir definition were summarized in Rawson et al.(1996). However, most of the recommended basalboundary bio-events cannot usually be recognized inboreholes (Robaszynski et al., 2000). Therefore, bio-stratigraphers use lithological marker beds, and fossilsand microfossils associated with the index species whosestratigraphic distribution has been studied at outcrop inthe Anglo-Paris Basin (e.g., Robaszynski et al., 1980;Pomerol et al., 1985; Mortimore and Pomerol, 1987;Hart et al., 1989; Pomerol, 1995; Amedro et al., 1997;Amedro and Robaszynski, 2001a,b; Mortimore et al.,2001). The identification of stage boundaries in the twoboreholes takes into account the recommendationsproposed during the Brussels Symposium (BRU) but isbased largely on data available from outcrops. There-fore, each stage boundary is proposed using a set ofcriteria to constrain the interval within which theboundary should occur. The following abbreviationsare used: FAD, First Appearance DatumZ the lowestoccurrence of a key species; LAD, Last AppearanceDatumZ the highest occurrence of a key species;PROV, Provins boreholes.

Albian/Cenomanian boundaryBRU: FAD Rotalipora globotruncanoides Sigal;

PROV: Sainte-Colombe Borehole only. After visualexamination of both cores and thin sections, nosignificant biostratigraphical elements for dating the‘‘Grey sandy limestone’’ below 687.20 m were foundapart from three ammonite fragments, one of which wasdetermined as Pleurohoplites (Arraphoceras) cf. studeri,a species of the late Late Albian (or ‘‘Vraconian’’: seeAmedro, 2002, for his defence of a Vraconian Stagebetween the Albian sensu stricto and the Cenomanian).The Albian/Cenomanian boundary is placed at687.20 m where there is a glauconitic and phosphaticnodule bed. This is at the lithological change betweena sandy limestone without chert (‘‘gaize’’) below anda limestone with cherts above (which contains I. crippsi,a typical Cenomanian bivalve).

Cenomanian/Turonian boundaryBRU: FAD of Watinoceras devonense Wright and

Kennedy; PROV: above the Plenus Marls and near thebase of the nodular chalk, above the LADs ofRotalipora cushmani and of Inoceramus pictus, and justbelow the FAD of Mytiloides mytiloides.

Turonian/Coniacian boundaryBRU: FAD of Cremnoceramus rotundatus sensu

Troeger non FiegeZCremnoceramus deformis erectus(Meek); PROV: the boundary comes above the‘‘marly streaky chalk’’, which can be interpreted as theCuilfail Zoophycos Beds, and clearly below the lowest

St.g.g.

BIOZONES DINO.

S/k

S/j

S/iS/h

S/g

S/f

S/e

upper

S/cS/b

S/a

T/c

T/b

T/a

C/c

S/d

S/c

lower

BENTHIC FORAM.

R.sz.p.

G.mont.

G.st.

B.dec.

G. cle.

R.cush.

Hd

Es

Mc

Ms

G.cris.

St. pol.

Th

Sp

G.hilt.

B.inc.

Ar.B.aust.

CA

MP

AN

IA

NSA

NT O

N.

CO

NIA

CIA

NT

UR

ON

IA

NC

ENO

MAN

.lo

we

rp

art

up

pe

rp

art

STAGES

R.sz.p.

DINO.. Depth

..

.

Magas

701 POIGNY

702

SAINTE - COLOMBE

S/d

S/c

S/k

S/j

?S/iS/h

S/g

S/f

S/e

C/c

T/a

?T/b

T/c

S/a

?S/bS/c

50

100

100

200

300

400

500

600

700

200

300

400

500

600

700

upper

lower

m

phosphate + glauconite

highest R. cushmani

nodular chalk

Southerham Marl

Caburn Marl

Bridgewick Marl

echinids

Cuilfail BedsShoreham Marlabundant inoceramidsgrey cherts

abundant inoceramids

Gavelinellacristata

Old Nore MarlBroinsonia.gr. pa

rca

Gavelinellaclementiana

Bolivinoidesdecoratus

?Gavelinellamonterelensis

+116.25

Depth

CA

MP

AN

IA

NSA

NTO

N.

CO

NIA

CIA

NT

UR

ON

IA

NC

ENO

M.

ALB.

Lo

we

rp

art

Up

pe

rp

art

STAGES

Es

Mc

Ms

Ar.

grey cherty limestones

Nodular chalk

Cuilfail Beds

Magas

Chalkwithout

flint

flintsZoophycos

Pleurohoplites (A.)cf. studeri

Inoceramus crippsi

Orbirhynchia

mantelliana

Inoceramus pictus

Mytiloides mytiloides

Orbirhynchia cuvieri

Inoceramus

cuvieri

Sternotaxis planus

Micraster sp.

Cr.waltersdorf

Volviceramus

involutus

Cladoceramus

undulatoplicatus

Offaster pilula

Magas

82.40

34.75

Bolivina.incrassata

Shoreham M.

Lewes Marl

Cuilfail Beds

m

dolomitic chalk

grey flaser limestones

Zoophycos flints

Zoophycos flints

bored surface

687.2

659.4

638.2

630.25

608.9

Southerham Marl

Caburn Marl

Bridgewick Marl

496.6

509.4

Zoophycos

flints

285.4

168

185

Zoophycos

flints

Lewes tubul. fl.

Shoreham Marl430.5

Zoophycosflints

369.7

346.1

Marker Beds

BiozonesB. FORAM.

T/S

Nodular chalk

Marker Beds

Old Nore Marl

In.crippsi

Mytiloides

Southerham Marl

Caburn Marl

Bridgewick Marl

Lewes tubul. fl.

140

164

285

Cladoceram.

448.4

427.6

371

345

622.1

646.6654.6

674.2

breccia hg.

520.7

508.1

“Marbled” chalk

R.cf.k.

T/S

Gbr.

.

449.6

Mytiloides subhercynicus

Pl. M.

Inoceramus virgatus

Plenus marl

Fig. 5. Litho- and biostratigraphic correlation between the Poigny and Sainte-Colombe Boreholes (dinoflagellates: Ar, Areoligera; Es,

Epelidosphaeridia spinosa; Mc, Microdinium ?crinitum; Ms, Microdinum setosum; Sp, Senoniasphaera protrusa; Th, Turnhosphaera hypoflata; Hd,

Heterosphaeridium difficile). For key, see Fig. 2.


Volviceramus, and below the lowest Stensioeina gran-ulata granulata. Within the Coniacian, a marl seamappears to correspond well with the Shoreham Marl,which is approximately the base of the middle part ofthe Coniacian.

Coniacian/Santonian boundaryBRU and PROV: FAD of Cladoceramus undulato-

plicatus, just below the chalk with paramoudra-typeflints and just above the FAD of Stensioeina polonica. Itis noteworthy that C. undulatoplicatus is the onlystandard stage-boundary fossil to be found in the twoProvins boreholes.

Santonian/Campanian boundaryBRU: LAD of Marsupites testudinarius Schlotheim;

PROV: limit clearly below the Old Nore Marl, in thechalk with paramoudra-type and Zoophycos flints, andnear the FAD of Bolivinoides strigillatus; boundarybetween the lower and upper part of the Campanian:PRO: between the FAD of Bolivinoides decoratus andthe FAD of Gavelinella monterelensis.

According to these criteria, the stage boundarieshave been located to within no more than a fewmetres.

5. Dolomitic body, Sainte-Colombe Borehole

The Sainte-Colombe Borehole was drilled in an areacharacterized by a seismic velocity anomaly in the Chalkwhereas the Poigny Borehole is located outside this area(Fig. 1). The chalks recovered at Sainte-Colombe arehardened and contain more Mg. The seismic velocitiesare higher but the same lithological succession isrecognized in both boreholes, except for the occurrenceat Sainte-Colombe of a 17-m-thick unit of dolomitizedchalk which is responsible for a significant increase inthe seismic velocities.

In the Sainte-Colombe Borehole, the dolomiticinterval is located between the FADs of the benthicforaminifera Bolivinoides decoratus and Gavelinellamonterelensis [limit of foraminiferal biozones S/h-S/i,corresponding to the overlap between the ranges of thebelemnites Gonioteuthis quadrata (Blainville) and Be-lemnitella mucronata (Schlotheim)], whereas in thePoigny Borehole, an interval consisting of chalkbounded by bored surfaces is located between thesesame foraminiferal bio-events. The discontinuity isprobably a consequence of the intra-Campanian Peinetectonic phase discussed by Mortimore and Pomerol(1991) and probably responsible for increasing detritalinput of illite (Deconinck et al., 2005). It is noteworthythat this thick dolomitic unit cannot be correlated withany other thick dolomitic unit in outcrops of the ParisBasin.

6. Sedimentation rates and tectonic phases

The linking of data on facies, thicknesses of lithologicbodies, nature of fossil content and development offoraminiferal zones provides a basis for makingobservations on variations in sedimentation rates andon the influence of tectonic phases on sedimentationduring the Late Cretaceous at the Provins borehole sites(Ilsede, Wernigerode and Peine phases as used in theAnglo-Paris Basin by Mortimore and Pomerol, 1997;Mortimore et al., 1998).

AlbianThis stage is represented only in the Sainte-Colombe

Borehole by a 17.30-m succession of sandy limestonesdated as late Late Albian. It corresponds to a marginalfacies (silty quartz, glauconite).

Cenomanian (Poigny: O53 m; Ste Colombe: ca.57 m).

The three substages of the Cenomanian seem to bepresent in the two boreholes. The presence of I. crippsiand I. virgatus in the hard limestone with cherts in theSte Colombe Borehole supports the existence of theLower Cenomanian, and this is underlined by severalphosphatic nodules and glauconitic horizons that mayrepresent flooding surfaces of the ‘‘Mid Cretaceous’’transgression (at 687.20, 686.40, 665.60 and 659.40 m).Above, at 648.80 m, the limestone without chertcontains a poorly preserved brachiopod that is mor-phologically close to Orbirhynchia mantelliana, a formfrequent in the Middle Cenomanian. Higher up, I .pictusand the Plenus Marls with the highest specimens of R.cushmani indicate the Upper Cenomanian.

This marginal facies of the Cenomanian can becompared to the succession known at St Jouin inNormandy with multiple breaks in sedimentationdemonstrated by the absence of numerous marker bedsthat are present in the Boulonnais, Kent and Westphaliawhere the Cenomanian is about 75.75 and 180 m thick,respectively (Amedro and Robaszynski, 2001b).

Turonian (Poigny: 190 m; Ste Colombe: 182 m).On marker bed and key fossil evidence, the thick-

nesses of the three substages of the Turonian can beestimated as follows (P, Poigny; SC, Ste Colombe):Lower Turonian (nodular chalk) P, 24 m, SC, 21 m;Middle Turonian (ca. below the Southerham Marl), P,52 m, SC, 54 m; Upper Turonian (below about the topof the Cuilfail Beds), P, 115 m; SC, 107 m.

In terms of tectonic phases, the Lower Turoniannodular chalk may represent a pre-Ilsede phase. Atabout the end of the Middle Turonian, the nodularlevels located at 5e10 m below the Southerham Marlare probably the last manifestation of the pre-Ilsedephase. The Upper Turonian is relatively thick by


comparison, for example, with the Boulonnais outcropswhere thicknesses reach about 30 m in the Blanc-Nezcliffs and 45 m in the Caffiers railway cutting. Thereduction in thickness in the latter successions corre-sponds to the Ilsede tectonic phase when subsidence wasmore regular in the Provins area.

ConiacianThe lower part of the Coniacian succession seems to

be reduced and reveals the intervention of the Ilsedetectonic phase through the presence of nodules, prob-ably from hardground(s) above the Cuilfail Beds, andthe lack of the Lewes Marl in the Poigny Borehole.

Near the middle part of the Coniacian deposits, thebenthic foraminiferal biozone S/b is thin, not clearlyevident or possibly missing, and certainly corresponds tothe expression of the main Ilsede tectonic phase, aspreviously reported by Mortimore et al. for the Anglo-Paris Basin (1998, p. 1377).

SantonianeCampanianThe middle part of the Santonian appears to be

expanded as the LAD of Stensioeina polonica and theFADs of Reussella szajnochae praecursor and Gaveli-nella cristata are widely separated. However, above thelatter datum, there is an interval of a few tens of metresup to the Old Nore Marl that should encompass theupper Santonian crinoid zones (Uintacrinus socialis,Marsupites testudinarius) and the basal Campanianzones of Uintacrinus anglicus and Offaster pilula. Noneof these key fossils or their associated faunas wasfound. One of the explanations for their absence mightbe unfavourable ecological conditions during thesedimentation; however, these bio-events are generallyknown throughout northern Europe. Another could bethat the apparent lack of the Santonian crinoidzones might reflect the Wernigerode tectonic phasethat took place during the SantonianeCampaniantransition.

Higher up, the middle part of the Campanian ismarked by the 17-m-thick dolomitic body in the Sainte-Colombe Borehole that correlates with an intervalbounded by two slightly bored surfaces in the PoignyBorehole. These features might be related to the Peinetectonic phase known in the Paris Basin through the‘‘Precy hardground’’, an intra-Campanian key bed(Mortimore and Pomerol, 1996; Hanot and Renoux,1999).

7. Conclusions

The boreholes at Poigny and Sainte-Colombe repre-sent the most complete Upper Cretaceous succession inthe Anglo-Paris Basin and therefore constitute valuablereference sections. Above the upper Upper Albian

(‘‘Vraconian’’), all stages are present with the followingthicknesses. The Cenomanian (ca. 55 m) is slightlythinner and the Turonian thicker (180e200 m) thanin the outer part of the basin. In the Turonian, severalclay-rich beds, including the Southerham, Caburn,Bridgewick and Lewes marls, correspond to kaolinite-bentonites. The Coniacian reaches 75e80 m, the Santo-nian is about 70 m thick, and the Campanian is 265 and217 m thick at Poigny and Sainte-Colombe respectively.

The most striking feature is the occurrence of a 17-m-thick dolomitic body between 168 and 185 m in theSainte-Colombe Borehole. This interval is located atthe transition between biozones S/h-S/i, at the bound-ary between the lower and upper parts of theCampanian. The lateral equivalent at Poigny consistsof chalk bounded by bored surfaces. These featuresprobably result from the Peine intra-Campaniantectonic phase.

From the Turonian to Santonian, the Ilsede tectonicphases are recorded successively in the upper part of theMiddle Turonian, the lower part of the Coniacian(hardground nodules) and the middle part of theConiacian (foraminiferal biozone S/b reduced). Higherup, the Wernigerode phase may have reduced orprevented the deposition of the crinoid zones at theSantonianeCampanian transition.

Acknowledgements

This short presentation of the main stratigraphicalresults of the Provins boreholes (Craie 700 Programme)benefited from the advice of the late Jake Hancock andthe detailed reviews of Christopher Wood and HaydonBailey who greatly improved the manuscript and theEnglish. We are grateful for their kind assistance, andalso to Prof. David Batten for his work on the finalversion of our paper. Francis Amedro is thanked for thedetermination of the Albian ammonites.

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