Evolution of the Sele River coastal plain (southern Italy) during the Late Quaternary by inland and...

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Rendiconti LinceiSCIENZE FISICHE E NATURALI ISSN 2037-4631 Rend. Fis. Acc. LinceiDOI 10.1007/s12210-012-0165-5

Evolution of the Sele River coastalplain (southern Italy) during the LateQuaternary by inland and offshorestratigraphical analyses

Pietro P. C. Aucelli, Vincenzo Amato,Francesca Budillon, Maria RosariaSenatore, Sabrina Amodio, CarmineD’Amico, Simone Da Prato, et al.

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LAND SEA INTERACTION IN CAMPANIA (ITALY)

Evolution of the Sele River coastal plain (southern Italy)during the Late Quaternary by inland and offshorestratigraphical analyses

Pietro P. C. Aucelli • Vincenzo Amato • Francesca Budillon • Maria Rosaria Senatore •

Sabrina Amodio • Carmine D’Amico • Simone Da Prato • Luciana Ferraro •

Gerardo Pappone • Elda Russo Ermolli

Received: 19 November 2011 / Accepted: 11 January 2012

� Springer-Verlag 2012

Abstract The late Quaternary evolution of the Sele River

coastal plain (Salerno Gulf, southern Italy) was investi-

gated through integrated stratigraphical, chronological and

palaeoecological analyses. The main environmental chan-

ges were ascribed to glacio-eustatic variations leading to

rapid ingressions alternating with coastal progradations.

The marked marine ingression of MIS 5.5 is testified by

palaeoridges now cropping out 4 km inland at 11/13 m

a.s.l. (Gromola palaeoridge). The eustatic minimum of MIS

2 is testified by lower shoreface deposits in the offshore

core record and in the seismic profiles at 120/130 m below

sea level. This prolonged sea-level fall was interrupted by

at least three rapid sea-level rises, probably related to MIS

5.3, 5.1 and 3. The evidence of the first two sea level rises

are represented by shoreface deposits in the inland S1 core

(30 m thick, 3 m a.s.l., 1.5 km inland). The highstand of

MIS 3 was identified by seismic profiles as onlapping

marine deposits. The shore deposits at 100 m b.s.l were

tentatively attributed to the lowstand of MIS 4. After the

lowstand of MIS 2, the Sele Plain was newly flooded due to

the rapid Post Glacial sea-level rise. This ingression caused

the inland migration of a barrier-lagoon system and stop-

ped at approximately 5.5 ky BP. From that moment the

shoreline started prograding up to the present position

probably due to the decrease in the sea-level rise rates and

This paper is an outcome of the FISR project VECTOR (Vulnerability

of the Italian Coastal Area and Marine Ecosystem to Climate changes

and their role in the Mediterranean carbon cycles), subproject

VULCOST (VULnerability of COaSTal environments to climate

changes) on: ‘‘Land–sea interaction and costal changes in the Sele

River plain, Campania’’.

P. P. C. Aucelli � S. Amodio � G. Pappone

Dipartimento di Scienze per l’Ambiente, Universita di Napoli

Parthenope, Centro direzionale, isola c4, 80143 Naples, Italy

e-mail: [email protected]

S. Amodio


G. Pappone


V. Amato (&) � C. D’Amico

Dipartimento di Scienze e Tecnologie per l’Ambiente e il

Territorio, Universita del Molise, C.da Fonte Lappone,

86090 Pesche (IS), Italy


C. D’Amico


F. Budillon � L. Ferraro

Istituto per l’Ambiente Marino Costiero, CNR, Calata Porta di

Massa, 80133 Naples, Italy


L. Ferraro


M. R. Senatore

Dipartimento di Scienze per la Biologia, la Geologia e

l’Ambiente, Universita degli Studi del Sannio,

Via Dei Mulini 59A, 82100 Benevento, Italy


S. Da Prato

Istituto di Geoscienze e Georisorse, CNR, Via Moruzzi 1,

56124 Pisa, Italy


E. Russo Ermolli

Dipartimento ARBOPAVE, Universita degli Studi ‘‘Federico II’’

di Napoli, Via Universita 100, 80055 Portici, Italy


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Rend. Fis. Acc. Lincei

DOI 10.1007/s12210-012-0165-5

Author's personal copy

to the volcaniclastic supplies from the Neapolitan volca-

noes, especially from the AD 79 Vesuvius eruption, also

recorded in the subbottom chirp profiles.

Keywords Late Quaternary � Sele Plain � Sea-level

changes � Facies analysis � Seismostratigraphy �Land–sea correlation

1 Introduction

Sea-level changes represent a significant factor in con-

trolling the evolution of coastal environments over geo-

logical times. Reconstructing palaeo-sea levels has been

attracting increasing interest in the last years due to the

deep impact of global warming on people living along the

coasts (Lambeck et al. 2011; IPCC 2007; Rahmstorf

2007; Siddall et al. 2006; Pirazzoli 1996). For this reason,

relatively tectonically stable areas are the best places for

this kind of research. In these areas, biological and sed-

imentological markers of the Last Interglacial (Marine

Isotopic Stage 5.5, hereinafter MIS 5.5) and Holocene

(MIS 1) sea level highstand phases are clearly recogni-

zable inland (Orru et al. 2011; Coltorti et al. 2010;

Ferranti et al. 2006; Antonioli et al. 2004; Lambeck et al.

2004; Antonioli et al. 1999), while markers of the low-

stand phases (MIS 2 and 4) can be recognized both off-

shore and inland at a considerable depth from the present

ground level (Spampinato et al. 2011; Caruso et al. 2011;

Wheatcroft and Drake 2003; Waelbroeck et al. 2002; Plint

and Nummedal 2000).

The Sele Plain/Salerno Gulf half-graben represents an

excellent area for integrated studies on the Quaternary

stratigraphic records. In fact the studies on the late Qua-

ternary morpho-stratigraphy allowed the palaeobeach

deposits of the Last Interglacial period to be recognized at

ca. 4 km inland, ca. 11/13 m a.s.l. (Brancaccio et al. 1987;

Russo and Belluomini 1992), covered by dune sands of the

Gromola-S.Cecilia-Arenosola-Aversana palaeoridges

(hereinafter GP). Moreover, the beach deposits of the

Holocene highstand are found at ca. 1.5 km inland, covered

by dune sands of the Laura palaeoridge (Brancaccio et al.

1988; ISPRA 2009; Amato et al. 2011). Other beach

deposits were recognized between 0.8 km inland and the

present shoreline, covered by dune sands of the Sterpina

palaeoridges (Brancaccio et al. 1988; ISPRA 2009; Amato

et al. 2011). The offshore sector of the Salerno Gulf shows

a wide continental shelf extending up to 15–25 km from

the present coast. Here shoreface deposits, recording the

eustatic minimum of the Last Glacial Maximum, were

found offshore in seismic and core data at ca. 8–10 km

from the present-day shoreline and at ca 110/120 m below

s.l. (Budillon et al. 1994).

In order to reconstruct the variations of the coastal and

marine palaeoenvironments due to the palaeoclimatic

changes between MIS 5 and MIS 1, a land–sea integrated

stratigraphic study was carried out, combining information

from three seismic profiles interpreted on the base of two

gravity cores (C1213 and C101), with a 30-m deep core

(S1) drilled inland at 1.5 km from the present coast. Facies

analysis was applied to all cores, also supported by pal-

aeoecological data, sequence-stratigraphic interpretation

and tephro-chronologic and 14C age constraints.

2 The inland and offshore geologic and geomorphologic

setting

The alluvial-coastal plain of the Sele River displays up to

2,400 m of post-orogenic sediment infill, accumulated in a

coastal half-graben, extending offshore in the deep Salerno

Gulf (ISPRA 2009 with references). This tectonic depres-

sion is bounded to N-NE by the horsts of the Lattari and

Picentini mountains and to the S-SE by the Cilento

mountains (Fig. 1). The submerged topography of the

Salerno Gulf displays an asymmetrical shape: a narrow

shelf domain develops down to 120–130 m around the

large submarine Salerno Valley, whereas a shelf 25 km

large and 180 m deep, surrounds the Cilento shore south of

the Sele River mouth, controlled by shallow rocky out-

crops. This physiography largely reflects the structural

configuration, mainly controlled by the Capri Master Fault

to the north (CMF in Fig. 1) and the Sele line to the south.

The Sele Plain–Salerno Gulf half-graben was charac-

terized by extensional tectonics since the Late Miocene–

Lower Pliocene (Brancaccio et al. 1987; Ortolani et al.

1979), along NW–SE and NE–SW faults. The collapse is

evidenced by the deposition of the so-called Conglomerati

di Eboli, a thick and widespread clastic unit (Early Pleis-

tocene in age). The latter is in part deeply buried in the

external sector of the plain and in the offshore sector, and

in part is largely exposed inland, along the NW margin of

the plain (Fig. 1). At the beginning of Middle Pleistocene,

the geomorphology of the plain was re-shaped by normal

and transtensional faults (Fig. 1). Part of the area carrying

Early Pleistocene fanglomerates was uplifted, while a large

part of the Plain continued to subside, accommodating the

so-called Battipaglia-Persano Supersynthem (BP in Fig. 1;

ISPRA 2009). This unit, which is up to some hundred

meters thick, covers a large part of the most internal sector

of the plain forming wide depositional terraces lying at

16–18 m a.s.l., close to the modern coast, and at 100 m

a.s.l. or more close to the mountain foot. Thickness and

facies distribution of the supersynthem’s lower part suggest

that its deposition was accompanied by subsidence and by

NW-ward tilting (ISPRA 2009).


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The subsidence sharply decreased when the transgres-

sion witnessed by the Gromola-S.Cecilia-Arenosola-Aver-

sana palaeoridges (GP in Fig. 1) occurred (Last

Interglacial; MIS 5; Brancaccio et al. 1988; Russo and

Belluomini 1992).

This eustatic transgression first formed clayey-silty and

peaty transitional (lagoon to palustrine) deposits and then

sandy beaches. The back-barrier domains were filled up

with marshy and fluvio-palustrine sediments when the sea-

level rise stopped and aeolian sands finally accumulated on

the coastal ridges. Remnants of the back-barrier terrace

related to these highstand phases are preserved in the

modern landscape at 11–14 m a.s.l., while the coeval

shoreface sediments occur up to 13 m a.s.l. and the dunes

up to 23 m a.s.l. This chrono-altimetrical data of the MIS 5

palaeo-sea level allowed the plain to be considered slightly

uplifting during the last 120–100 ky (Brancaccio et al.

1988; Barra et al. 1998, 1999; ISPRA 2009).

Near Paestum, in the SE sector of the plain and near

Pontecagnano in the NW sector, the MIS 5 transgression

was limited by the pre-existing prominent lobes of the

Travertini di Cafasso-Seliano (ISPRA 2009; Amato et al.

2009a) and of the Travertini di Faiano-Pontecagnano

(D’Argenio et al. 1983; Amato et al. 2009a, b), respectively

(Fig. 1).

During the Last Glacial regression the Sele Plain was

mainly subjected to floodplain conditions, when the fall of

the sea level caused a strong shoreline progradational phase

(Budillon et al. 1994). To the late part of the Post Glacial

transgression and to the following period of highstand is

finally due the deposition of the most external sector of the

plain. The early Holocene shows a clear transgressive trend

while the late Holocene has a progradational trend. The

transgression trend was pre-announced by lagoon deposits,

whose basal part was radiometrically dated to around

9,000 years BP (Barra et al. 1998, 1999; ISPRA 2009). The

peak of ingression occurred at about 5,300 years BP and

formed the innermost part of the Laura coastal ridge (up to

1.5 km from the present coastline; LP in Fig. 1). The

progradational trend added more advanced Laura ridges

(probably other three, dated from 5.3 to 3.6 ky BP) and the

Sterpina ridges (I and II, dated from 2.6 ky BP to about

2.0 ky BP; Brancaccio et al. 1986, 1988; Barra et al. 1998,

1999; ISPRA 2009).

The shelf sector hosts the seaward front of the Sele,

Tusciano (TR in Fig. 1), Picentino (PR in Fig. 1) and

Fig. 1 Simplified geological map of the Salerno Gulf–Sele Plain

area. 1) Pre-Quaternary bedrock; 2) Eboli Conglomerates (Early–

Middle Pleistocene); 3) marine, continental and transitional deposits

of the Battipaglia-Persano SuperSynthem (BP) (Middle–Late Pleis-

tocene); 4) fluvial-marshy deposits (Late Pleistocene–Holocene); 5)

travertine deposits (Middle Pleistocene–Holocene); 6) Gromola-

S.Cecilia-Arenosola-Aversana sandy barriers (GP) (Late Pleistocene,

MIS 5); 7) Laura-Sterpina sandy barriers (LP) (Holocene); 8) Main

faults (CMF Capri Master Fault); 9) location of inland (S1) and

offshore (C101, C1213) cores; 10) seismic lines (GNS12, CSal 5,

CSal 2) location. PR Picentino River, TR Tusciano River, SRSolofrone River


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Solofrone-Capo di Fiume (SR in Fig. 1) rivers’ alluvial

deposits. Coastal and alluvial domains prograded 15 km

seawards starting from MIS 5, in step with the general

retreat of the sea level during the Last Glacial Maximum

(MIS 2). Successively the shelf underwent drowning,

following the Late Pleistocene–Holocene transgression

(Budillon et al. 1994; Buccheri et al. 2002; Iorio et al.

2009; Sacchi et al. 2009). Consequently, the stratigraphic

pattern of the Sele River plain consists of a thick Late

Pleistocene prograding wedge topped by a marked

erosional unconformity, which, in turn, underlies the

lithosomes that were formed between 18 and 5 ky. The late

Holocene depositional unit consists of a wedge whose

thickness decreases toward the shelf edge. The most

impressive late Holocene event was caused by the AD 79

Vesuvius eruption (Lirer et al. 1973; Buccheri et al. 1994;

Sacchi et al. 2005; Insinga et al. 2008), that settled a thick

pumiceous lapilli layer, which now provides a well rec-

ognizable stratigraphic marker within the shelf and the

upper slope sediments.

3 Materials and methods

3.1 Inland core

A new deep core (30 m thick) was drilled in the inner part

of the Laura palaeoridge (40�27.3230N, 14�38.1710E,

2.85 m a.s.l., S1 in Fig. 1), using a dry-continuous

mechanic coring that allowed a 10 cm diameter core to be

extracted. The core was preserved in six coring-box, now

kept at IAMC-CNR Naples warehouses. Here, the core was

analyzed to define color, texture, grains size, shape and

composition, fossil content, sedimentary and diagenetic

structures. All these features were taken into account to

define lithofacies and their association, according to the

Unconformity Boundary Stratigraphic Unit method

(UBSU, after Salvador 1994). The most significant layers

were sampled for laboratory analyses, such as palaeoe-

cology (mollusk, ostracoda and benthic foraminifera

assemblages) palynology and 14C AMS datings, in order to

interpret at the best, the lithofacies organizations and their

chronology, and finally, the original depositional environ-

ments (Fig. 2).

3.2 Mollusks

Qualitative and quantitative malacological analyses were

carried out on 58 samples of the S1 core. Shells of each

sample were identified and counted. Taxonomy of the

species follows both the World Register of Marine Species

(WoRMS) database for marine and brackish taxa (accessed

at http://www.marinespecies.org on 2011-06-27) and the

Italian Ministry of Environment’s Checklist of the Italian

Fauna (accessed at http://www.faunaitalia.it/checklist/ on

2011-06-27) for non-marine taxa. Ecology of marine and

brackish species was defined after Peres and Picard (1964)

and Peres (1982); while for non-marine species we follow

Kerney (1999). A malacological diagram (Fig. 3) based on

numerical data was essayed; the diagram deals with the

number of shells related to species recovered from each

sample. As the different samples recorded a great vari-

ability in the total number of shells, ranging from more

than 1,400 to less than 5, percentages of species are not

considered for the construction of the diagram, that allows

to recognize several mollusk zones (related to different

environments), in accordance with the major faunal chan-

ges through the sequence.

3.3 Benthic foraminifera

The foraminiferal analysis was carried out on a total of 20

samples collected at approximately 100 cm intervals of the

S1 core (Fig. 2). Almost 300 g of sediment was wet-sieved

through 125 lm, dried at 60�C and then weighed. In the

present study data from [125 lm size fraction were ana-

lyzed. When abundant, the sediments were split by a

microsplitter in small portions for counting foraminifera.

Species determination was mainly based on studies con-

cerning the Mediterranean benthic fauna (Sgarrella and

Moncharmont Zei 1993; Fiorini and Vaiani 2001). For the

genus Ammonia, we referred to Carboni and Di Bella

(1996). Because of the general scarcity of foraminifera,

only qualitative analysis was performed on benthic species.

3.4 Ostracods

Thirty-seven samples were prepared for ostracod analysis

of the S1 core (Fig. 2). Samples were disaggregated in

warm water (95�C) adding hydrogen peroxide, washed

through a 63-lm sieve, and finally dried at 110�C. In order

to facilitate palaeoecologic interpretation, semi-quantita-

tive analyses were performed, including both juvenile and

adult specimens. Ostracod frequencies were calculated for

200 g of dried sediment. The analysis of the population

structure of each species was performed in order to

Fig. 2 Sedimentological log of the inland core S1. Columns show

from the left to the right: (a) selected samples used for 14C datings and

palaeoecological analyses (mollusks, benthic foraminifera, ostracods,

pollens); (b) grain size log; (c) lithofacies, as indicated in Table 1,

where their detailed descriptions are shown; (d) vertical distribution

of the main mollusk, ostracod and benthic foraminifera assemblages;

(e) depositional environments, also suggested by vertical evolution of

lithofacies; (f) systems-tract interpretation as suggested by retrogra-

dational and progradational facies trends (SB sequence boundary,

MFS maximum flooding surface); (g) marine isotope stages (MIS)

interpretation. See details in the text of the inland data

c


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http://www.marinespecies.org

http://www.faunaitalia.it/checklist/


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Fig. 3 Malacological diagram from the inland core S1. Crosses represent single shells


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separate autochthonous from displaced species (Gliozzi

2000). The autoecological data of each species and their

interpretation were performed following different authors

(e.g. Colalongo 1969; Athersuch et al. 1989; Montenegro

and Pugliese 1995; Gliozzi and Mazzini 1998; Meisch

2000).

3.5 Pollen

Only four samples were collected for pollen analysis of the

S1 core, due to unsuitable lithology (Figs. 2, 4). For each

sample, 10 g of sediment were treated with HCl and HF for

mineral dissolution. Physical enrichment procedures, such

as ZnCl2 separation and ultrasound sieving, were realized

in order to concentrate the pollen grains in the residue. The

most peaty samples were boiled in KOH 10% before being

processed. Quantitative pollen analysis was only possible

on three core samples, since the sample at -12.20 m was

barren. Ca. 300 pollen grains were counted in each sample

and 42 taxa were identified. The main sum used for the

calculation of arboreal (AP) and nonarboreal pollen (NAP)

percentages excluded marsh and water plants (including

Typha and Potamogeton), spores, algae and indeterminate

grains.

3.6 Offshore cores

The gravity core C1213 was collected in 2003 at a depth of

152 m (40�26.1330N, 14�45.9500E) (Fig. 1) and about

4.7 m of marine sediment were retrieved. The core was cut

in 1 m-long sections and split in two halves in order to

allow visual description and sediment physical measure-

ments at IAMC-CNR laboratories.

The gravity core C101 was collected in 1984 at a depth

of 87 m (40�33.0670N; 14�47.1660E) (Fig. 1) and entered

the marine sediment within the shelf down to 4.30 m bsf.

3.7 Seismic data

The subbottom profiles were acquired in 2002 using a

Chirp Cap II profiler on board of the R/V Urania, during

the acquisition of data for a geologic cartographic project

by IAMC-CNR (Fig. 1). Chirp seismic system in based on

a frequency-modulated source (FM), pinging within the

2–7 kHz band. The single channel Uniboom profiles were

shot by a EG&G mod. 230 (PSU230) Power Supply, each

150 ms at 300 J, on board of R/V Bannock during a cruise

carried out by the Earth Science Department of Naples

University in 1984.

The conversion of two-way travel time to real depth was

obtained assuming an average velocity of about

1,550 m s-1 below the sea floor (Carlson et al. 1986). The

vessel positioning was achieved by a 12-channel DGPS, a

motion sensor and a gyrocompass in order to perform a

real-time correction during the 2002 survey while a Loran

C positioning was used during the acquisition of Uniboom

profiles in 1984. Subbottom profiles investigated the shelf

record by about 60 ms two-way travel time, c. 50 m

beneath the sea floor. Maximum vertical resolution does

not exceed 30–40 cm. The Uniboom signal penetrated the

Fig. 4 Pollen diagram from core S1. Taxa percentages are plotted

against depth


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first 80 ms two-way travel time, c. 60 m bsf, and achieved

a vertical resolution of about 70 cm.

Seismic lines were interpreted considering reflection

geometries, relative lateral terminations among reflectors

and seismic facies analysis, according to standard seismo-

stratigraphic, echo facies interpretation (Damuth 1980;

Vail 1987) and sequence-stratigraphic criteria on conti-

nental margins (Posamentier and Allen 1999; Plint and

Nummedal 2000).

3.8 Radiometric datings

An age-depth model of the S1 drilled succession was built

thanks to radiometric dating of three biological sea-level

markers: Cerithium vulgatum, Cerastoderma glaucum and

Donax trunculus. The shells were analyzed at the CIRCE-

DSA-SUN laboratory (Center for Isotopic Research on

Cultural and Environmental heritage, Environmental Sci-

ence Department, Second University of Naples). 14C ages

were calibrated using the Calibration data set, intcal09.14c

of Reimer et al. (2009).

The age model of the C101 core is based on AMS 14C

dating performed at CIRCE-DSA-SUN Laboratory on

mixed planktonic foraminifera shells from four collected

samples. Radiocarbon ages were converted into calendar

ages through intracal09.14c (Reimer et al. 2009). The fall

deposits of the 79 AD Vesuvius eruption were considered

as chronological reference.

4 Results

4.1 The S1 core

4.1.1 Mollusks

A total of 101 mollusk taxa were recovered, including 33

bivalves, 66 gastropods and 2 scaphopods. All the identi-

fied species were previously reported for modern non-

marine, marine and lagoonal settings of the Mediterranean

area. Figure 3 provides a malacological diagram divided in

the following mollusk zones.

• Zone S1A (from -29.7/-29.8 to -28.8/-29 m; from

-25.3/-25.5 to -24.6/-24.8 m): polytypic marine

assemblages consisting mainly of Antalis dentalis,

Chamelea gallina, Corbula gibba, Donax semistriatus,

Tellina nitida, Timoclea ovata, Bittium sp., Pyramidel-

loidea spp. and Turritella communis. Shell fragments

are abundant and often rounded. Taxa of the unstable

mud biocoenosis (MI; infralittoral and circalittoral) of

Peres and Picard (1964) dominate; infralittoral elements

of the upper clean-sand (SFS; bathymetry: 0–2.5 m),

of the fine, well-sorted sand (SFBC; bathymetry:

2.5–25 m) and of the Posidonia meadows biocoenoses

(HP; bathymetry: 0.5–40 m) are also present.

• Zone S1B (from -28.5/-28.65 to -25.8/-26 m; from

-24.1/-24.3 to -23.25/-23.4 m; from -22.1/-22.3

to -20.1/-20.3 m): mixed polytypic marine and

oligotypic brackish assemblages. Besides the interval

from -22.1/-22.3 to -20.1/-20.3 m, both marine

shells and their fragments, altered and dissolved, are

frequent. Species of the marine assemblages are the

same of the zone S1A. Generally low diversity and low

abundance characterize the brackish assemblages;

shells are well preserved. Bittium reticulatum, an

euryhaline component of HP biocoenosis, also spread-

ing over brackish environments, and Hydrobia sp.,

typical of the lagoonal eurythermal and euryhaline

biocoenosis (LEE), prevail. Abra segmentum (LEE),

Parvicardium exiguum (LEE) and Rissoidae spp. (HP)

are present as associated elements.

• Zone S1C (sample -22.6/-22.8 m): abundant frag-

ments and reworked marine shells. Species of the MI

biocoenosis (A. dentalis, C. gibba, T. communis)

prevail; other species such as Glycymeris sp. (SFBC),

Nuculana pella, T. ovata and Ringicula sp. are rare and

represented only by fragments.

• Zone S1D (from -19.6/-19.8 to -18.6/-18.8 m): rare

fragments and broken specimens (Cardiidae indet.,

B. reticulatum, Rissoidae indet.).

• Zone S1E (from -18.1/-18.3 to -15.1/-15.3; sample

-12.1/-12.3 m): rich oligotypic brackish assemblages

dominated by B. reticulatum (HP) and Hydrobia sp.

(LEE). Also represented are A. segmentum (LEE),

Cerastoderma glaucum (LEE), Loripes lacteus (LEE),

P. exiguum (LEE), and some taxa requiring higher

salinity conditions, such as Cerithium vulgatum, Pyra-

midelloidea spp., Pusillina spp. (HP) and Rissoa spp.

(HP). Specimens of freshwater gastropods (Acroloxus

lacustris, Bithynia tentaculata, Gyraulus spp., Lymnaea

(Radix) peregra, Physa (Physella) acuta and Valvata

piscinalis), typical of environments with still or slow-

moving waters, and a fair number of marine infralittoral

species locally occur.

• Zone S1F (from -14.7/-14.9 to -12.6/-12.8 m):

mixed marine and oligotypic brackish assemblages.

Marine elements are reworked (e.g. C. vulgatum,

C. gallina, C. gibba, Donax spp., Glycymeris sp.);

and shells of the brackish assemblages (A. segmentum,

B. reticulatum, C. glaucum, Hydrobia sp., Pusillina

spp.) are both preserved and reworked. Rare Cochli-

cella conoidea, a terrestrial species typical of dune

environments, and V. piscinalis, a freshwater gastropod,

also occur. Shell oxidation may be locally observed.

• Zone S1G (sample -11.55/-11.70 m): mixed mollusk

assemblage with marine and brackish species.


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B. reticulatum (HP) prevails, and is followed by

C. gallina (SFS and SFBC), Caecum sp., Lucinella

divaricata (SRPV = upper muddy sands in sheltered

areas biocoenosis; bathymetry: 0–1 m), Hydrobia sp.

(LEE), D. semistriatus (SFS) and C. vulgatum. Shell

fragments are abundant; individuals of some species are

strongly reworked (B. reticulatum, C. vulgatum); others

are in a good state of preservation (Caecum sp.,

C. gallina, Hydrobia sp., L. divaricata). Rare Gyraulus

sp. and Succinea sp. testify some freshwater input.

• Zone S1H (from -11.1/-11.3 to -10.6/-10.8 m):

fragments and specimens of marine species (B. reticul-

atum, C. glaucum, C. gallina, Donax spp., L. divari-

cata), are generally poor represented and reworked.

• Zone S1I (from -10.1/-10.3 to -4.1/-4.3 m): marine

infralittoral assemblages dominated by infaunal and

filter feeders bivalves. Shell fragments are common;

specimens are not abundant. C. gallina (SFS and

SFBC), D. semistriatus (SFS), Glycymeris sp. (SFBC)

and L. divaricata (SRPV) prevail. Rare individuals and

fragments of non-marine species (Ancylus fluviatilis,

V. piscinalis and Hygromiidae indet.) locally occur.

• Zone S1L (from -3.6/-3.8 to -3.1/-3.3 m): few and

rounded marine shell fragments, and one specimen of

L. divaricata (SRPV).

• Zone S1M (from -2.6/-2.8 to -1.6/-1.8 m): rare

marine and terrestrial shell fragments.

• Zone S1N (sample -1.10/-1.30 m): few shell frag-

ments of terrestrial gastropods and one specimen of

C. conoidea.

4.1.2 Benthic foraminifera

From the bottom to the top of the core two associations

have been individuated (Fig. 2)

• Association A1: (from -29.90/-30.00 to -21.40/

-21.50 m): the benthic association is characterized

by the prevalence of Ammonia beccarii (Linn.) and

subordinately by the species A. tepida (Linn.), Elphi-

dium crispum (Linn.), E. macellum (Fichtel and Moll),

Peneroplis pertusus (Forskal) and Quinqueloculina spp.

All taxa are present with low percentages except in

sample -28.70/-28.80 m in which A. beccarii and

A. parkinsoniana are more abundant. A. beccarii, is

present in all samples and it is indicative of a shallow-

marine environment characterized by sandy bottoms

(Sgarrella and Moncharmont Zei 1993). Jorissen (1988)

found that this species is very abundant in the Adriatic

Sea along a belt parallel to the Italian coast at a water

depth of less than 20 m, where the highest abundance is

found between 15 and 20 m in the samples with

intermediate percentages of organic matter. The species

is totally absent in the area in front of the main Po

outlets. E. crispum, E. macellum and P. pertusus are

shallow-marine species that are commonly found as

epiphytic (Blanc-Vernet 1969; Langer 1993) and do not

tolerate high concentrations of organic matter. The

assemblage found in this interval suggests an area not

directly influenced by the river run-off and mainly

characterized by coarse substrate.

• Association A2: (from -17.35/-17.50 to -11.35/

-11.50 m): taxa are dominated by very few specimens

of the genus Ammonia. While the sample at -16.35/

-16.50 m is characterized by the highest values of

A. tepida (Cushman) and E. granosum (d’Orbigny).

E. granosum is considered by Jorissen (1988) as

inhabitant of a near-shore zone (7.5–25 m water depth),

with coarse substrata poor in organic matter; it is also

reported from lagoon and shallow-marine settings

(Zampi and D’Onofrio 1987; Albani and Serandrei

Barbero 1990; Bellotti et al. 1994). A. tepida is common

in shallow-marine environments, lagoons and deltas

(Almogi-Labin et al. 1992; Favry et al. 1998; Abu-Zied

et al. 2007); it can also be indicative of moderately

restricted conditions (Debenay et al. 2005). A. tepida

(referred to as A. parkinsoniana forma tepida by Jorissen

1988) has a very close relation to run-off systems and has a

strong correlation with high percentages of organic matter.

All taxa present in this interval are common in shallow-

marine environments subjected to fluvial influence.

4.1.3 Ostracoda

Basing on ostracod assemblages, the S1 core may be

divided from the bottom to the top in seven intervals

(Fig. 2). In the first interval the ostracods are abundant both

in species diversity and in number of specimens with an

association typical of shallow-marine environments. The

third interval is characterized by an oligotypic association,

indicative of brackish water, with a very low number of

specimens per sample. The ostracod assemblage of the fifth

interval is characterized by a relatively high species

diversity and abundant valves, typical of oligo to mesoh-

aline shallow-water environments (lagoon). The changes in

the ostracod associations are due to salinity variations. On

the contrary, the following interval is characterized by

relatively low species diversity and low number of speci-

mens; these taxa are typical of shallow-marine environ-

ments. The other intervals are barren.

4.1.4 Pollen

Pollen analysis results are presented in a detailed pollen

diagram (Fig. 4) where all the recognized taxa show their


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percentage values plotted against depth. The arboreal taxa

percentage (AP/Tot curve in Fig. 4) oscillates between 80

and 90% giving the image of a very dense forested land-

scape (intra alias Heim 1970) in which the main arboreal

elements were deciduous Quercus, Alnus, Carpinus and

Corylus. These trees do not show important variations

along the diagram, they probably represent the main ele-

ments of a forest association established on humid soils.

Vegetation associations dominated by Alnus, Corylus,

Carpinus and Ulmus now characterize high humidity

environments linked to microclimatic conditions, well

represented all over Italy (Pedrotti and Gafta 1996). These

elements are also commonly present in alluvial environ-

ments of temperate regions in central Europe (Polunin and

Walters 1987) where they form plain-wood strips, by now

relicts in Italy and almost disappeared from southern Italy,

a part from the hygrophilous woods of Mount Circeo

(Stanisci et al. 1998).

It is very interesting from a phytogeographic and bio-

climatic point of view the constant presence of Vitis sp.

The species vinifera, as its wild representative, are now

associated with the above-mentioned arboreal elements in

thermophilous humid forests from central to southern Italy

(Pignatti 1982) even if the wild representative is in constant

regression all over Europe (Arnold et al. 1998).

Small amounts of Abies, Fagus and Betula are the

only representatives of the mountain vegetation belt.

Mediterranean elements are mainly represented by

Quercus ilex and by minor percentages of Olea, Phillyrea

and Pistacia.

Poaceae are the main representatives of the herbaceous

elements; their percentages are always below 10%. The

constant presence of Cyperaceae, water plants and spores

indicates the persistence of humid environments around the

site. In sample -17.20 the presence of a dinoflagellate cyst

suggests the possible connection to sea water.

A very similar vegetation association, dominated by a

deciduous forest on humid soils with Vitis as brushwood

element, characterized the Holocene climatic optimum

(8,354–8,524 cal yr BP) in the Vendicio plain, near For-

mia, about 100 km north of Naples (Aiello et al. 2008).

Here, the dated level was sampled at a core depth corre-

sponding to ca. 16 m below the present sea level. In the S1

core the levels sampled for pollen analysis correspond to

ca. 13–14 m b.s.l. and thus their stratigraphical position is

consistent with an early–middle Holocene age.

4.1.5 Facies analysis

On the whole, 23 lithofacies, organized in 8 lithofacies

associations, were identified and their detailed descriptions

are summarized in Table 1. The vertical stratigraphic

evolution of the S1 core (Fig. 2) is here briefly described.

The lowermost interval (-30.00/-28.30 m) is charac-

terized by bioclastic sands where marine fossil fauna are

rich and diversified, indicating a high-energy shallow-

marine environment, corresponding to the infralittoral zone

(S2 and S3 lithofacies).

From -28.30 to -25.80 m depth, coarse to fine muddy

sands with bioclasts, locally intercalated to gravels, occur

(SB1 and SB2 lithofacies); marine fauna is dominant, but

associated with brackish species indicating, on the whole, a

shallow-marine environment with freshwater input.

After a thin interval made of very altered and oxidized

reddish-brown silty sands showing diagenetic structures

related to an emersion phase (CP2 lithofacies, ephemeral

coastal plain), the shallow-marine conditions are re-estab-

lished as shown by coarse sands and gravels with typical

shallow-marine fauna (S2 and S4 lithofacies), which in turn

pass upward to sands and gravels with marine and subor-

dinately brackish fauna (SB lithofacies association, up to

-23.10 m depth). Then, a second interval (0.15 m thick)

characterized by the CP1 lithofacies, testifies to a new

emersion surface.

From -23.00 to -21.00 m depth, medium sands to gravels

with rounded and discoidal pebbles and cobbles are docu-

mented; a dominant brackish fauna or barren sediments occur

(M lithofacies association, mouth bar of estuarine/delta). The

upper interval up to about -15.30 m depth is dominated by

muddy sediments with organic matter and brackish fossil

fauna, living in still waters with soft bottoms (L1 and L2

lithofacies, open to sheltered lagoon environment).

The following interval (from -15.30 to -11.75 m),

limited by two erosional surfaces, is characterized by

gravels passing gradually to muds; here brackish fauna is

associated to freshwater (characeans) and terrestrial (gas-

tropods) species. On these bases, the sediments could be

interpreted as a flooded tidal delta or as a washover fan

formed on the landward margin of a barrier island (WF

lithofacies association). After open marine conditions came

back by a coarse reworked horizon with polygenic grains

(mollusks and travertine fragments, S6 and S5 lithofacies,

from -11.75 to -10.40 m depth), followed by a thick

interval (from -10.40 to -3.90 m) with abundant coarse to

medium sands locally intercalated with silty horizons (S

lithofacies association, upper shoreface environment).

Here, the marine species are more frequent than the

brackish ones but, on the whole, the fossil fauna is less rich

and diversified than in the lower part of S1 core.

From -3.90 to -1.60 m depth, planar and cross-lami-

nated silty sands, locally oxidized, with rare fragments of

marine bivalves, together with terrestrial gastropods, indi-

cate a foreshore/backshore deposit (FB1 and FB2 lithofa-

cies), followed by fossilized and pedogenized beach dune

ridge deposits and recent aeolian sands of coastal plain

(D and CP lithofacies associations, from -1.60 to 0 m).


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Table 1 S1 land core: lithofacies, lithofacies association and their environmental interpretation

Lithof.

assoc.

Lithofacies Environ. interpretation

CP CP1 Reddish-brown medium-fine and coarse silty sands with abundant altered shell fragments.

Note the strong oxidation of sediments

Coastal plain

CP2 Paleosol: brownish sandy mud with organic matter and plant material

CP3 Volcaniclastic deposits formed by greenish altered cinerite with rare whitish-grey pumice. The

thickness is about 5 cm

D D1 Dark-brown medium-fine silty sands with rounded and subrounded lithic fragments topped by

roots and humified material

Beach dune ridge

D2 Greyish muddy medium sands with pedoconcretions and burrows filled by dark muddy sandy

matrix. Rare Cochlicella conoidea and fragments of indeterminate terrestrial mollusks are

present

FB FB1 Whitish-grey medium-fine silty sands and rare muddy levels; rounded and discoidal lithic and

calcareous granules locally occur; planar and cross laminations are present. Fragments of

indeterminate terrestrial mollusks and rare fragments of marine bivalves have been

recognized

Foreshore/backshore

FB2 Gravelly coarse-medium sands with rounded and discoidal lithic and biogenic (bivalves)

fragments

S S1 Planar laminated centimeter levels of alternating grey sandy silts, muds and medium-fine

sands. Detrital mineral grains are recognized: quartz, mica and others. Shallow-marine fossil

associations are poor and oligotypic with rare gastropods, benthic foraminifera (rare

Ammonia) and ostracods (rare Aurila, Loxoconcha, Argilloecia sp.). This lithofacies only

occurs in the holocenic interval

Upper shoreface

S2 Grey medium-fine silty sands with abundant bioclasts (mollusks, anellids, echinoids, corals);

nodules of organic matter locally occur. Sometimes planar laminations are recognized.

Mollusks fauna (Antalis dentalis, Turritella communis, subordinated Chamelea gallina,Corbula gibba, Donax semistriatus, Bittium sp. etc.), also as rounded bioclasts, indicate

marine environment with high-energy. Ostracofauna is rich and diversified: Cytherettasubradiosa, Carinocythereis antiquata, Semicytherura incongruens, Cytheridea neapolitana,Pontocythere turbida, with rare Hiltermannicythere turbida, Cytheretta adriatica, Costa spp.

Benthic foraminifera association is dominated by Ammonia beccarii, subordinately Ammoniatepida, Elphidium crispum, Elphidium macellum, Peneroplis pertusus and Quinqueloculinaspp. are present. All fossil associations are poor and oligothipic in the holocenic interval

S3 Dark-grey gravelly muddy sands (medium-coarse sand grains) with abundant bioclasts

(mollusks, anellids, echinoids, bryozoans and rare corals); granules and pebbles are

subrounded and discoidal. Organic matter and altered volcanic material locally occur. Fossil

associations are the same as that in the S2 lithofacies, but some brackish mollusks (Bittiumreticulatum and Hydrobia sp.) are associated. On the whole, fossil fauna are scarce and less

diversified in the holocenic interval

S4 Coarse sands and gravels with scarce silty matrix. Clasts are represented by granules, pebbles

and cobbles (max. 3 cm in size). Mollusk association is represented by Chamelea gallina,Donax semistriatus, Glycymeris sp. and Bittium sp. with rare form of Hydrobia sp. Benthic

foraminifera are rare or absent; the genera Ammonia is dominant. Ostracod association is

poor and oligotypic (rare Aurila, Loxoconcha, Argilloecia sp.).

S5 Coarse-medium reworked sands and polygenic gravels with abundant whole and fragmented

mollusks (Chamelea gallina, Donax semistriatus, very abundant Bittium sp.), rare ?travertine

fragments; very rare Ammonia occur; ostracod association is poor and oligotypic (rare Aurila,

Loxoconcha, Argilloecia sp.). This lithofacies is only documented in the holocenic interval

S6 Coarse reworked sands and polygenic gravels with abundant whole and fragmented mollusks

(Chamelea gallina, Donax semistriatus, Lucinella divaricata, Bittium sp., Caecum sp., and

Hydrobia sp.), echinoid spines. Some characeans (oogons) are locally documented.

Ostracods association is composed of Cyprideis torosa and Loxoconcha elliptica, also with

Candona neglecta, C. angolata, Aurila woodwardi, Prionocypris zenkeri and Xestoleberis sp.

Very rare Ammonia occur. This lithofacies is only documented in the holocenic interval


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4.1.6 Chronology

The C1 sample (Donax trunculus, 9.70 m from the top,

-6.85 m below s.l.) gave a 14C age of 4,582 ± 50 years

BP for the S4 lithofacies (calibration: 95% r2 at

5,346 ± 33 years BP). The C2 sample (Cerastoderma

glaucum, 17.20 m, 14.35 m below s.l.) gave a 14C age of

10.073 ± 49 years BP for the L1 lithofacies (calibration:

95% r2 at 11,660 ± 218 years BP), while the 14C age of

the C3 sample (Cerithium vulgatum, 18.20, 15.35 m below

Table 1 continued

Lithof.

assoc.

Lithofacies Environ. interpretation

SB SB1 Whitish-grey coarse to fine muddy sands with bioclasts and organic matter. More altered

volcanoclastic material also occurs. Mollusk associations are marine (Antalis dentalis,Turritella communis, Chamelea gallina, Lentidium mediterraneum, Bittium sp.) and brackish

(Cerastoderma glaucum, Hydrobia sp. Abra segmentum); the marine shells are more altered

and dissolved while the brackish ones are well preserved. Ostracods and benthic foraminifera

associations are the same as that in the S2 lithofacies

Upper shoreface/brackish

SB2 Whitish-grey coarse-medium sands and gravels with scarce silty sand matrix; bioclasts are

common. Also here the marine mollusk shells are partly altered and dissolved. More altered

volcanoclastic material occurs. Fossil associations are the same as that in the SB1 lithofacies

WF WF1 Dark-grey medium-fine muddy sands with volcanoclastic material and oligotyphic brackish

(Abra segmentum, Cerastoderma glaucum, Bittium reticulatum and Hydrobia sp.) and

reworked marine molluscks. Some oogones of characeans occur. Ostracod associations are

dominated by Cyprideis torosa and Loxoconcha elliptica associated with Candona neglecta,

C. angolata, Aurila woodwardi, Prionocypris zenkeri e Xestoleberis sp. Rare or totally absent

Ammonia.

?Flood tidal delta or

washover fan in brackish

lagoon

WF2 Grey medium-coarse muddy sands with pebbles; integral and fragmented reworked shells of

marine and brackish mollusks (Bittium sp. Pusillina lineolata, and Hydrobia sp.) occur. Few

oogons of characeans and rare terrestrial gastropods (Cochlicella conoidea) are present;

oxidation locally occur. Ostracod and benthic foraminifera associations are the same as that

in the WF1 lithofacies

WF3 Grey muddy gravels with subrounded and discoidal polygenic pebbles and abundant

fragmented shells of brackish (Abra segmentum, Cerastoderma glaucum, Bittium sp.

Pusillina lineolata and Hydrobia sp.) and subordinately reworked marine mollusks. Few

oogons of characeans occur. Ostracod and benthic foraminifera associations are the same of

the WF1 lithofacies

L L1 Dark-grey laminated mud with rare polygenic coarse sands; abundant brackish (Bittiumreticulatum and Hydrobia sp.) and subordinate freshwater (Armiger crista, Bityniatentaculata, Valvata piscinalis) mollusks, living in still waters with soft bottom, are

documented. An oxidated and altered greenish pumice horizon (10 cm thick) occur. Ostracod

fauna is dominated by Cyprideis torosa and Loxoconcha elliptica and associated with

Candona neglecta, C. angolata, Aurila woodwardi, Prionocypris zenkeri and Xestoleberis sp.

Benthic foraminifera association is characterized by Ammonia tepida, Elphidium granosumand deformed Ammonia tepida. Pollen analysis shows deciduous main arboreal elements

(Quercus, Alnus, Carpinus, Corilus) representing a near forest association on humid soils;

herbaceous elements are Poaceae (\10%), Cyperaceae, water plant, spores, rare

dinoflagellate cysts, indicating humid environment connected to sea water

Brackish lagoon

L2 Dark-grey silty clay with abundant coarse to fine sand intercalations; mollusks are not

abundant or rare (Bittium sp., Hydrobia sp. Cardiidae indeter., Rissoa sp.), sometimes

oxidated. Ostracod fauna is the same as that in the L1 lithofacies. Rare Ammonia or totally

absence of benthic foraminifera occur

M M1 Greenish grey medium-fine silty sands alternated with rounded and discoidal gravels or sandy

silts. Mollusks association is dominated by brackish forms (Bittium reticulatum, Hydrobiasp., Abra segmentum, Cerastoderma glaucum, Loripes lacteus, Pusillina lineolata, Rissoaspp.); the ostracods are Cyprideis torosa and Loxoconcha elliptica, subordinately Aurilawoodwardi. Very rare Ammonia beccarii

?Mouth bar of estuary/delta

M2 Muddy sandy gravels, locally oxidated, and medium-coarse sands with abundant reworked and

dissolved marine shells. Fossil associations are the same as that in the M1 lithofacies

M3 Dark-grey muddy gravels with subrounded and rounded pebbles and cobbles (until to 8 cm in

size), locally rich in organic matter. Fossil associations are the same as that in the M1

lithofacies


123


s.l.) was 9,568 ± 39 years BP for the L2 lithofacies (cal-

ibration: 95% r2 at 10,968 ± 180 years BP).

The ages obtained from the C2 and C3 samples are not

in agreement with the stratigraphy. The bias could be due

to reworking of this part of the core during the drilling, to

reworking of the dated mollusk shells into the sediments

or to a dating error. Nevertheless, these chronologic-data

allowed the lagoon environments (L1 and L2 lithofacies)

to be referred to as the beginning of the Holocene, while

the transition to the upper shoreface was established about

5,300 years ago. In this way, if there are no dating errors,

it is possible to constraint the upper part of the S1 suc-

cession (from L1 and L2 lithofacies to the top) into the

Holocene.

4.1.7 Environmental model and sequence stratigraphy

According to the above integrated approach based mostly

on sedimentological and palaeoecological data, it has been

essayed the reconstruction of the palaeoenvironmental

evolution of the southern sector of the Sele Plain during the

Late Pleistocene–Holocene interval. To this purpose we

have taken into account also the literature of the last

10 years (cfr. Barra et al. 1999; ISPRA 2009). The envi-

ronmental model, that we propose, corresponds to a coastal

plain with a fluvial mouth passing to the open sea through a

lagoon-barrier island system, sometimes crossed by was-

hover fans and/or channels.

In addition, the detailed sedimentological and strati-

graphic analyses allowed us to individuate the retrograda-

tional and progradational coastal systems by applying the

sequence stratigraphy approach to the S1 core (Fig. 2),

even though radiometric datings are not available for the

lower part of the core. We propose that the base of the S1

reaches the Late Pleistocene Highstand (MIS 5), where the

more open marine lithofacies occur. In this interval, about

7 m thick, two main sequences were individuated, with the

lower not complete downwards. The following estuarine/

delta deposits (about 3 m thick) correspond to a lowstand

system, formed during the prolonged sea-level fall (MIS4–

MIS2 interval) that reached -120 m during the Last Gla-

cial Maximum, c. 20 ky BP (Siddall et al. 2006; Lambeck

et al. 2011; Waelbroeck et al. 2002; Caruso et al. 2011).

This is a very condensed interval characterized at the base

by erosion, meteoric diagenesis and reworking of coastal

sediments. The subsequent Holocene marine transgression

is testified by lagoon deposits (transgressive system), fol-

lowed by a very short progradation phase associated to

flood tidal delta/washover fan sediments (highstand sys-

tem); the latter are topped by a new sequence boundary

corresponding to an erosional surface. In the upper 12 m, a

fourth sequence was individuated corresponding to a beach

dune prograding system, still active at present. On the

whole, the third and fourth sequences clearly record the

Holocene sea-level rise (MIS1).

4.2 The offshore data

4.2.1 The C101 and C1213 cores

The C1213 core (Fig. 5) entered a marine succession

whose textures and biological assemblage give indication

of a progressively shallowing upward environment in the

lower 170 cm (A) and of an increasingly deep environment

in the uppermost 320 cm (C). Between them a 15 cm thick,

well-sorted, fine sand deposit with shell fragments (B) is

included, being underlain by a sharp irregular surface.

The A unit is composed of two fining upward horizons:

the lower one (sub-unit A1) includes at the base a poorly

sorted, mud-sustained deposit with bryozoans, sponges and

mollusk shells; the upper one (sub-unit A2) shows at the

base a mud-sustained, poorly sorted bed made by rhodolit-

bearing pebbles, bryozoans and mollusk shells.

The C unit consists, from the base to the top, of a 60-cm-

thick, mud-sustained, poorly sorted heterometric bioclastic

sand, whose grains are fining upwards, and of a homoge-

neous marine mud which holds two volcaniclastic deposits:

the deepest one (sub-unit C1) is a 15-cm-thick, dark-grey

ash deposit dispersed within an olive-grey muddy matrix,

slightly bioturbated and bounded by blunt surfaces; the

shallowest (sub-unit C2) is 45 cm thick and is made up of

coarse white and grey pumiceous lapilli, above a sharp and

regular surface; these distinctive lithofacies match well

with analogous tephra found in several cores in the Salerno

Gulf and respectively correlated to the AD 79 Vesuvius

Plinian eruption and to the 2.7–3.3 ky BP Somma-Vesu-

vius activity (AP eruptions; Insinga et al. 2008).

The B unit displays textures and bioclastic content

typical of a lower shoreface deposit; therefore, it registers

the shallowest marine environment within the core sedi-

ment record. Based on its stratigraphic position and litho-

logic features it can be related to the LGM lowstand, i.e. to

the stage of maximum retreat of the shoreline. On the basis

of lithofacies analysis and stratigraphic markers it is pos-

sible to infer to the base of the core a relative age as old as

MIS 3, since it passes through the lower shoreface deposit

(B) relative to the maximum glacial lowstand condition

(MIS 2) and reaches a former deposit that stands for a mid-

shelf environment (A2) and inner-shelf environment (A1).

The C101 core (Fig. 5) entered a marine succession

mostly consisting of fine siliciclastic deposits. The basal

unit (A) is constituted of mud deposits that include several

thin layers of well-sorted silt and lenses of fragmented

shells (mainly mollusks and echinoids). A 17-cm-thick

volcaniclastic deposit (sub-unit A1) occurs between 281 and

302 cm, composed of normally graded, fine to very fine


123


black ash which well correlates to the analogous deposit

(sub-unit C1) occurring in C1213 core, on the base of its

lithologic features and stratigraphic position. According to

Iorio et al. (2004), Insinga et al. (2008) and Sacchi et al.

(2009), these tephra, settled in the Salerno Gulf shelf owe

its origin to the 2.7–3.3 BP Somma-Vesuvius activity

Fig. 5 Sedimentological logs of the offshore cores C1213 and C101.

Graphic columns illustrate the lithological characteristics of the two

cores divided in units on the base of grain sizes, textures, organogenic

components and sedimentary structures (see key legend). The three

columns on the right represent: the depositional environment, as

derived by vertical evolution of lithostratigraphic characteristics; the

systems tract as deduced by the seismic data interpretation (FSST

falling stage systems tract, LST lowstand systems tract, TSTtransgressive systems tract, MFS maximum flooding surface, HSThighstand systems tract) and the marine isotope stages (MIS)

interpretation. The three blue lines evidence the correlated intervals

between the two cores. Location of C1213 and C101 cores is also

shown in the upper right (stratigraphy of C1213 from ISPRA, 2009

modified). See the text for further information


123


(AP eruptions). Nevertheless, the occurrence of parallel

lamination toward the top deposit, the concentration of shell

fragments and the dubious age dating at 4.4 ky cal BP at

293 cm bsf (Table 2), let us to infer that this volcaniclastic

deposit underwent reworking processes in this sector of the

shelf.

The upper unit (B) starts from 195 to 164 cm bsf with

the tephra layer (sub-unit B1) correlated to the AD 79

Vesuvius eruption composed of angular and sub-angular

white to grey pumice lapilli laying on a basal erosive

contact. This unit is overlain by a normally graded and

reworked deposit consisting of pumice lapilli and ash, mud

supported, with fragmented organism shells up to 149 cm

bsf, thus evidencing synsedimentary reworking processes

(Buccheri et al. 2002; Sacchi et al. 2005) soon after the AD

79 eruption. Between 149 cm and the core top, the unit B is

mainly composed of mud deposits with some thin well-

sorted silty layers and widespread presence of shells,

mainly mollusks, sometimes fragmented.

According to the recognized lithofacies, the depositional

conditions have changed at the core site from a mid to an

outer shelf environment characterized by fine-grained

sedimentation with current influxes able to selected the silt

sediment and to break and drag the organism shells. On the

basis of the 14C datings (Table 2) the sediment-core is

representative of the whole Holocene marine sedimenta-

tion, since about 11.2 ky cal BP.

4.2.2 Seismic data

The very high resolution (VHR) seismic acoustic profile

CSal 5 was shot off the Sele River mouth, up to 40 m of

depth, 2.9 km off the shoreline; the CSal 2 VHR profile

was shot off in between the Tusciano and Picentino river

mouths, up to 20 m of depth, 1.9 km from the coastline.

The GNS12 uniboom profile was run off the Capo di

Fiume-Solofrone streams at a depth of 20 m, 3.6 km

distant from the Paestum coast (Figs. 1, 6).

The seismic lines go far off the present-day sand bars

that lie within 10 m below s.l. (ISPRA 2009). Some evi-

dent stratigraphic horizons can be traced beneath the sea-

floor, across the plain margins and bear a meaningful

stratigraphic reference over the Salerno Gulf and the

surrounding shelf margin. From the seafloor downwards,

they are as follows:

• a shallow unit beneath the seabed, 8–10 m thick, with

typical discontinuous reflectors possibly due to fluid

escape and plastic deformation features or sediment

undulations (Urgeles et al. 2011). Between 40 and 70 m

below s.l., in the central and northern sector of the Bay.

The unit is bounded at the base by a regular and

conformable marine reflector that lies halfway between

the AD 79 Vesuvius tephra and the present-day seabed,

thus not older than about 1 ky (ISPRA 2009);

• the conformable, isochronous, marine reflector related

to the Vesuvius AD 79 Plinian eruption, traceable from

about 22 m of depth, far beyond the shelf break and

largely reported in recent literature on the offshore;

• the diachronic unconformity (LPu) associated to the

increasing land exposure, following the sea-level retreat

since MIS 5.1; it truncates the top of the Late

Pleistocene prograding units, and marks a progressively

longer hiatus landwards. It matches locally with the

ravinement surface, that records the landward shift of

the wave base erosion during the following phase of

sea-level rise. In this case the paralic lithosomes are

missing (Cattaneo and Steel 2003);

• a set of gentle-dipping prograding lithosomes with

sigmoidal reflections above the LPu (4 in the CSal 2; at

least 1 in the CSal 5, Fig. 6), stacking in a retrogressive

arrangement towards the most recent one. The four

prograding set off the TP coast lie 70, 45, 30 and 23 m

deep b.s.l and are, respectively, 6.8, 4.3, 3.1 and 2.5 km

far from the present-day shoreline;

• a laterally continuous prograding unit (Fig. 6), trun-

cated at the top by the LPu, and mostly consisting of a

Late Pleistocene Falling Stage Systems Tract (FSST) in

the mid-shelf and of a lowstand prograding wedge

(LST), seaward (Plint and Nummedal 2000).

The Uniboom profile shows three prograding units

alternating with onlapping units below the LPu (Fig. 7).

This stratigraphic pattern was formerly interpreted as

due to a forced regression of the coastal units driven by the

Late Pleistocene, fourth order sea-level drop following

the Tyrrhenian highstand stage (Budillon et al. 1994).

Table 2 14C dating results of the analyzed samples in C101 core

Sample depth (cm) Lab. DSA Radiocarbon age

(years BP)

Calibrated

age (1 r)

Calibrated age

BP (years BP)

d13C (%)

C101 (-45) -811 860 ± 31 1158–1219 AD 792–631 4 ± 1

C101 (-293) -802 3,911 ± 38 2469–2396 BC 4,419–4,346 0 ± 1

C101 (-358) -804 5,520 ± 45 4445–4420 BC 6,395–6,370 1 ± 1

Mixed planktonic foraminifera shells were used as material to be dated


123


The peak of the retreat accounts for the growth of a shelf-

margin and a mid-shelf littoral body. The latter is shore

parallel and was at least 100 km long, during the last

maximum lowstand phase (LST) (Budillon et al. 2011). At

present, the external front of the two lowermost prograding

wedges lie at a depth of 85 and 110 m, respectively. They

are 700 and 1,200 m wide, as far as may be seen in the

profiles, and both attain a vertical thickness of about 30 m.

The inner portion of the oldest wedge is masked by the

acoustic shadowing due to the overlying, gas rich, sedi-

ments and presumably extends further towards the coast.

5 Discussion

The inland and offshore stratigraphic investigations in the

Sele Plain–Salerno Gulf area were aimed at identifying the

coastal prisms within the shelf and the alluvial-coastal

Fig. 6 Line drawings of the subbottom chirp seismic profiles CSal5

(above) and CSal2 (below). For location see Fig. 1. The units were

identified on the base of the internal reflectors’ terminations and on

their stacking patterns and represents the stratigraphic architecture of

the shelf record from MIS 5 to the present-day (see text for details)


123


plain as well as at detailing their shifts through time and

space, in steps with the relative sea-level changes of the

Late Pleistocene–Holocene (Fig. 8). We base this discus-

sion on both literature data (Budillon et al. 1994; ISPRA

2009; Amato et al. 2011; Amato et al. 2012) as well as on

the identification, offshore and inland, of the transgressive

and regressive phases of the Holocene shorelines. More-

over, well dated tephra layers and 14C ages, allowed us to

identify the main lowstand and highstand phases of the

palaeo-sea levels. In particular, the inland data show that,

before the sedimentation of the Holocene prism, a con-

densed succession (see Fig. 2), including erosive features

linked to a large hiatus developed. This hiatus is here

referred to the eustatic minimum (MIS 2) of the LGM, and,

probably, to MIS 3 and 4. Moreover, a highstand phase was

probably driven by the eustatic maximum of the Last

Interglacial (MIS 5).

The offshore data (seismic lines and cores) show,

beneath the Post Glacial sediment wedge, three coastal

prisms linked to relative lowstand phases interposed to two

short relative rising sea-level phases, testified by onlapping

set of reflectors above the coastal deposits.

Therefore, based on absolute depth of the toplap sur-

faces, the three lowstand phases were tentatively referred to

MIS 5.4, MIS 4 and MIS 2, while the two short relative

highstand phases to the MIS 5.3 or 5.1 and to the MIS 3. In

addition, the inland data (cores and outcrops) allowed the

Last Interglacial sea-level rise to be detailed: in fact, the

remnants of the MIS 5.5 beach deposits of the GP can be

referred to the bottom of the S1 core at ca. 29 m depth

(26 m below s.l.; S2 lithofacies). So, during the Last

Interglacial, while in the GP areas developed beach

deposits, the bottom of the S1 core show marine lithofa-

cies. Moreover, two further short lowstand phases are

recognizable in the lower part of the S1 core. They could

be tentatively related with the MIS 5.4 and MIS 5.2 low

palaeo-sea levels. In fact, the CP1 lithofacies, recognized at

-23 and -20 m a.s.l, testify to two short emersion periods

that could be referred to such marine stages. In the time

span corresponding to MIS 4, MIS 3, and MIS 2, the inland

data recorded a very condensed succession. Mouths of

estuarine/delta environment, marked by several erosonial

surfaces and by oxided horizons. According to Lambeck

and Chappel (2001) and Pirazzoli (1996), during this per-

iod the shoreline was progressively shifted seawards,

reaching the present 120/130 m b.s.l. during the Last

Glacial Maximum of MIS 2.

In the offshore, at the transition between the LGM and

the Post Glacial period the sets of gentle-dipping sigmoidal

reflections, in backstepping above the LPu (Fig. 6), testify

phases of delta front progradation that occurred despite the

rapid sea-level rise (18–6 ka; Lambeck and Chappel 2001).

Indeed, the stacking pattern of reflectors and the reciprocal

stratigraphic position let them to be referred to as the

Transgressive System Tract. The offlap break of each

reflector within the prograding set gives an indication of

the wave-cut terrace depth associated with the toplap ter-

mination (and thus coastal sediment bypass) and may be

indicative of a 10–20 m higher sea level. This assumption

is mostly qualitative and derives from the local wave

Fig. 7 Line drawing of the Uniboom profile at 300 J. For location see Fig. 1, and text for details. Modified from Budillon et al. (1994)


123


climate (assumed that it has been constant through time)

over a ky-based temporal scale, which may deepen the

theoretical depth of closure (Immenhauser 2009) to an

effective one, as deep as k/2 (k being the wave length

period during exceptional storm condition).

Along the Salerno Gulf coast the theoretical depth of

closure in fair-weather conditions does not exceed 8–10 m

(Budillon et al. 2006; Ferrante et al. 2011). It is believed that

normal regression may even occur during transgressive

stages if fluvial sediment supply overcomes the coastal

accommodation space (e.g., Cattaneo and Steel 2003) in a

time span of rapidly changing morphoclimatic conditions

(Einsele 1996). Nevertheless, delta front off the Tusciano

River mouth is surprisingly thicker than the prograding delta

front relative to MIS 2 off the Sele river mouth. This evi-

dence may be accounted for by the observation that during

the Glacial Maximum peak the Sele River flowed directly

along the slope. Indeed, a net of channel features is still

preserved on the seabed slope, possibly due to fluvial bed-

load yield, as gravity and inertia flows from the former river

mouth. As a consequence, a deep detached fan-delta grew up

at the slope foot of the Salerno Valley (Fig. 9) and only a thin

delta front formed south of the river mouth, where a large,

smoothly deepening shelf was present at that time, acting as

base level for the delta front foreset progradation.

This marked seaward delta front could have favored the

formation of the barrier-lagoon system. In fact, the Holo-

cene landward prograding of the latter could have started as

spit bars attached to the delta fronts, to evolve subsequently

as coastal bars, before being fixed by dune vegetation, just

when the rate of sea-level rise decreased.

During these regressive trends and in the early Holocene

sea-level rise, a high amount of organic matter accumu-

lated as a result of the seaward and landward migrations of

the barrier-lagoon system. The consequent free methane

gas in the sediments masks the acoustic signal along ver-

tical confines, even at low pore pressure concentration

(Garcıa-Gil et al. 2011) and fluid-escape features within

shallow shelf marine unit (Trincardi et al. 2004) are often

linked to the external front of the biogenic shallow-gas-

charged sediment, as recorded in seismic lines (CSal5 in

Figs. 6, 7). Therefore, gas-bearing sediments may be

associated to estuarine and lagoonal depositional environ-

ment, tracing the boundary of high organic content in the

muddy facies.

As to the Holocene, the inland data allow a better cor-

relation and the identification of the transition from the low

to highstand, the Maximum Flooding (MF) surfaces, or MF

zones, and the progradational phase. The chronology of the

transition is established by 14C ages that fix the transgres-

sion at the beginning of the Holocene, the MF at ca. 5,5 ky

BP, while, starting from this moment, the Sele Plain pro-

graded until it reached the present shoreline.Fig

.8

Inte

rpre

tati

ve

geo

log

ical

sect

ion

acro

ssth

eco

res,

bas

edo

nse

ism

icp

rofi

les

and

sho

win

gth

ela

nd

–se

aco

rrel

atio

no

fth

eli

tho

faci

esan

dth

eir

chro

no

log

y.

Th

ere

dd

ash

edli

ne

sho

ws

the

sea-

lev

eltr

end

sfr

om

MIS

5to

the

pre

sen

t.In

par

ticu

lar,

the

lan

d–

sea

stra

tig

rap

hic

alco

rrel

atio

nal

low

edth

eid

enti

fica

tio

no

fth

eM

IS5

.5,M

IS5

.3an

dM

IS5

.1h

igh

stan

ds

asw

ell

asth

eM

IS4

,

MIS

3an

dM

IS2

low

stan

ds,

the

Ho

loce

ne

hig

hst

and

that

ori

gin

ated

mig

rati

ng

lan

dw

ard

bar

rier

-lag

oo

nsy

stem

san

dfi

nal

lyth

eH

olo

cen

ep

rog

rad

atio

nal

tren

dth

atg

ener

ated

mig

rati

ng

seaw

ard

bar

rier

-lag

oo

nsy

stem

s.N

ote

that

du

rin

gth

eH

olo

cen

eit

isp

oss

ible

toid

enti

fya

firs

tp

has

eo

fla

nd

war

dm

igra

tio

no

fth

etr

ansi

tio

nal

(bea

chan

db

arri

er-l

ago

on

)sy

stem

sd

uri

ng

earl

y-m

idd

le

Ho

loce

ne,

foll

ow

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ya

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on

of

the

abo

ve

syst

ems

du

rin

gth

ela

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olo

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e.T

he

da

shed

gre

enli

ne

rep

rese

nts

the

corr

elat

ion

of

the

79

AD

tep

hra

thro

ug

hth

eco

res


123


The normal regression trend of the shoreline was more

accentuated during historical times (last 2,500 years)

because it was supported by the emplacement of the distal

fall deposits related to Neapolitan volcanoes eruptions,

mainly the AD 79 event, and by the increasing man-

induced impact on vegetation and on alluvial-coastal

sectors.

Data correlation allows some palaeogeographical and

palaeoenvironmental aspects to be detailed for the Holo-

cene transgression and progradation phases. In particular,

at the beginning of the Holocene, the transgression was fast

and favored the landward migration of the barrier-lagoon

system, up to the maximum ingression that occurred at ca.

5,5 ky BP and reached the position of the Laura palaeo-

ridges. Then, the barrier-lagoon system migrated mainly

seaward. The presence of lagoons during the early Holo-

cene is confirmed by pollen data from the Sele Plain as well

as from very similar vegetation associations characterizing

the Holocene climatic optimum of other Tyrrhenian allu-

vial-coastal plains (Aiello et al. 2008). A different age of

the passage from a retrogradational to aprogradational

trend can be inferred for the sector of the plain between the

Tusciano and Picentino rivers, on the base of the CSal2

seismic profile. Here, the backstepping of the shore per-

sisted until approximately 3.0 ky BP, probably due to the

different vertical tectonic behaviour of the plain, during

Holocene times. In fact,according to Pappone et al. (2012)

and Vilardo et al. (2009), the dx sector of the Sele plain

is undergoing subsidence, while the sx sector should be

tectonically stable or slightly uplifting.

6 Final remarks

To summarize the above data presentation and interpreta-

tion we have assembled in Fig. 9 the main late Quaternary

Fig. 9 Salerno Gulf–Sele Plain palaeogeographical sketches from

MIS 5.5 to the present-day, showing the supposed shoreline position

and some palaeoenvironmental interpretations, derived by inland and

offshore stratigraphical data. 1) lagoon deposits, 2) sandy beach

deposits, 3) MIS 5 beach and dune deposits, 4) travertine deposits, 5)

pro-delta deposits, 6) black dashed lines indicate presumed palaeo-

channels of the Sele and Tusciano rivers, created during the sea-level

falls, 7) cores cited in the text


123


paleogeographical features of the Sele plain/Salerno valley,

tentatively, reconstructed through the correlation of inland

and offshore data.

Starting from MIS 5.5, when the shoreline had reached

the GP, at ca 4 km inland with a palaeo-sea level of

11/13 m above s.l., the shoreline strongly prograded, until

reaching 120/130 m below s.l. (Lambeck and Chappel

2001) during the eustatic minimum of MIS 2. This long-

time lasting of sea level fall was interrupted by three short

rise periods which could be tentatively referred to MIS 5.3,

5.1 and MIS 3. In fact, if the palaeo-shorelines of MIS 5.3

and 5.1 can be located some km seawards from the S1 core,

as suggested by seismic data, two sea-level falls were

recognized in the lower part of the S1 core, at ca 20 m

below s.l. (CP lithofacies layers). These layers, testifying a

short emersion, could have formed during the MIS 5

lowstand phases, as supposed by seismic offshore data, that

show shore deposits at ca. 80 m below s.l. As to the

Holocene, the palaeo-shorelines of the maximum trans-

gressive phase can be located ca. 1.5 km inland, in proxi-

mity of the Laura palaeoridge, when the barrier-lagoon

system was at its maximum retrogradation stage, approxi-

matively at 5.5 ky BP. Then, the shoreline prograded and

the barrier-lagoon system migrated seaward, reaching the

present position. The Sterpina dune system can be related

to this moment when the stasis of the progradation allowed

the formation of the pre 2.5 ky Sterpina I ridge and then the

sin AD 79 Sterpina II ridge (Amato et al. 2012; Alberico

et al. 2011).

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