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Volume 43,r. 1-2r2004
of the
Proceeding
]" MEETIIVG OF THE ITALIAI{ OSTRACODOL(
,,IIVMEMORY OF GIULIAIVORUGG
Rimini, February I 2-I 4, 2003
Editors:
Elsa Gliozzi
Antonio Russo
MTJCCHI MODENA
Bollenino delh Societi Paleontologica Italiana
r ssN0375-763314r-r57
+l (r-2),2004
2 pls.
Modena,Novembre2004
New insights on the Quaternary stratigraphy of tl
deduced by borehole investigations
Barbara DRI-L'ANToNIA*
Alessandro CInvPALIxI*
Alessandro Bossto*
Libero MtcHpl-ucclo
Gi
Francesco Paolo BoxnDoNNA*
* Dipartimento di Scienze della Terra, Universit) di Pisa, Italy
- o
Studio di geologia L. Michelucci, Livorno, Italy
Radiometricages,Liuorno, t
KEY WORDS - Quaternary,Snatigraphy,Micropalaeontologlr,
drilt
ABSTRACT - Thispaper reportsthe main resultsgf q" integratedstu.dyofI 5 boreholes
Despite this area is o"i if the'most extensiuelystudied 9f thi Coastal Turcayy (Cennal ltat
"pahchina"
the subsurfacistratigrapb is still imperfectlykitow". T\t prest
deposits(beach"rocks),
sectorof the'Pisa
iln of Liuorio, locatedon the'eustaticLiuirno Terraie'nia the southernmost
-Grondo
obserut
performedinclufud lithological-sedimentological
fui Lupi" erosionalscarp.Analyses
allowedto
and radiocarbohdating. Stratigraphitit ;"itrfretution of the I5 inu/stigatedboreholes
Particuhrb i
of which can be ,oorlitrd wirt formatiort oLtrropping"in North-tVestirn Tuscany.
belowtie Eutyrrhenian'pirtfilrA" lAyerof a relatiuelythlck marineiucc'
io rorfirm the presence
successio,ojptors to inilude two units io far unrecognized
In a/dition, the Lower Pleistocene
phaseof thi Santernian-EmilianUgle
sedimentsreferableto the regressiue
-of and a secondiarine t
Aurila puncticruciara) a
the Sicilian"o, the basisof Foth osiacodfiunot (commonoclutrenttt
'Groida
dei LLpi" scarp,we re!
Zone"). Finatly in a sinile boreholedr;lted in proximity of ,hq
o tyih of probabk Uppe, Pleistocineage 0
but might likely represent
needfurther i'ntuestigatiois,
In tie Pisa Phin dimain, *, ,ttoidtd braikislt-continenialttdi*trts (wit6 lo*t, leuelsof proba-b
Historical coastaldepositsclosethe succesiion.On
sandsreferableto the Wrsilian transgression.
Quatrri?ry stat1sropb of the Liuirno sunoundingsand tugtit that this area undertpentt
preuiouslyrecognized.
RIASSTINTO- [Nuovi dati sulla Stratigrafiadel Quaternariodell'areadi Livorno emers
principali
risubati emersidallo studio multitrisciplinareA; t S sondaggiffittuati nel sonosuolo
'delle
pl* studiate delk Tbscanamarittima Qnlia Cennale), topratilno-"Per i ben noti depq,sit
sonosLoloi a tuttbgt Ancort pococonosciuta.Queyo studio inieressaun'irta comPrendentila c
da ur
Liuorno e il settortTi* meridiinaledelh Pianui di Pisa. Questidue domini sono'separati
analisi
dei Lupi". Le inlagini effettuateincludono osseruAzionilitologicqsedimentologiche,
L'interfretuzionett itigrofito dei I 5 sondaggiindagati ha permusodi ri9onorcgrt.7principali u
confoi*izioni ffiorant; illta TbsianaNord-Occidentale.Nel domlnio del Ter
essere'correhte
';:ffi,Li:';:i#'h,i,!;:,:l:::),!;";:",r;:,1"",!#'T';
?::,f:,:':{:#:,:;"u#',
ffi::,'/::
regressiuadel ciclo Santerniano-Emiliono i ,, secondo ciclo marino del PleistoceneInferiore,..
"ftomtke
fot,
presenza di Aurila puncticruciata) e delle nannoflore ("Zqna a lmall Gephyrocapsa ).
'delk
"Gronda
dei Lupi", sono sta:ti incontrati sedimenti da costieri a naisizionali. Qu
,rorpoto
ulteriori'indagini, powbbero irrrrc l'espressionedi un cich di probabile etd pleistocenica superir
Eutirreniana.'Netfa Plarura di Pisa, ioro stati indiuiduati seiimenti contiientali e di ambient
riferibili al PleistoceneSuperiore, che sono ffoncati dn sabbie ascriuibili alh trasgressioneWrsiliar
eii storica. I dati acquisti hanno consentito di ffinare la stratigrafa full'area il Lirorno e sugc
quanto finora noto.
INTRODUCTION
The Quaternary successionof the Livorno
surroundings (Tuscany, Central Italy) is one of the
most exteniively studied of the Coastal Tuscany (e.8.
Bacci et al., 1939; Malatesta, 1942; Barsotti et al.,
1974; Mazzanti, 1984, 1987, 1995, 2001 cum bib.;
Lazzarorro et al., 1990; Dall'Antonia 6{ Mazzanti,
"panchina"
2001), especially for the well known
deposits (b-eachrocks) related to the marine high stand
of-the last interglacial (Barsotti et al., 1974; Hearry et
Al., 1986; Federici 6( Mazzanti, 1995; Mauz, 1999).
Systematic analysesbased on well data were carried
out by Galletti Fancelli (1979) and Fancelli et al.
( 1986) on Holocene deposits of the southern sector
of the alluvial Pisa Plain (just North of Livorno). In
particular the latter paper revised about 2000 welliosr of old boreholes,-dfilledfor water research.These
sifnificant studies, however, are not supported by
dJtailed palaeontological analysesand lack exhaustive
taC-dating
chronological constriins, the only available
(Ferrara
et
being performed more than 40 years ago
al., 1i59, I 96 1). As a consequence,the subsurface
stratigraphy of the Livorno area is still imperfectly
known and controversial.
\With the aim to fill this gap of knowledge, rD
r42
B, DALL:ANTONIA,A. CIAMPALINI, L. MICHELUCCI, G. ZANCHETA, A, BOSyO, EP BONADONNA
extensive study of 15 borehole cores was undertaken.
The main results of these preliminary investigations
are discussedin this paper.
GEOLOGICALSETTING
In the North-'Western Tuscany, where the study
area is located (Text-fig. l), four main morphological
domains, which correspond to as much geological and
(Lazzarotto et al., 1990) can be easily
strucrural settings
-the
Pisa Plain made up of Upp.!
recognized: I)
"polycyclic"
Pleisiocene-Holocene deposits; II) the
eustatic Livorno Terrace, formed mostly during the
"Euryrrhenian"
transgression (Orygen isotope stage,
Ois 5.); III) the Livorno hills and Pisahills comPrising
mainly Lower-Middle Pliocene and Lower Pleistocene
marine deposits, with minor amount of continental
terraced l\4iddle-Upper Pleistocenesediments; IV) the
Livorno mountains, mostly made up of MesoCaino zorc sandstones, carbonates, argillites and
ophiolites belongitg to the Ligurian and Tuscan
naPPes.
-Th:
present.study focuseson a small area, which
comprises the ciry of Livorno, located on the Livorno
Terrice and the southernmost sector of the Pisa Plain.
"Gronda
dei Lupi",
A scarp, which is locally known as
separatesthe Livorno Terrace from the Pisa Plain.
Aicordirg to Lazzarotto et Al. (1990) and Mazzanri
Text-fig. I - Main morphological and structural domains of
Nonh-'W'eti.tn Tir"scanyand location of the study area
(redrawn from Lazzarotto et al., 1990).
(2001), this scarp has a complex origin. The northeastern sector is probably related to fluvial erosion
during the marine low stand of the Last Glacial and
the south-western part to marine erosion during the
Holocene ma><imumtransgression.
The present-day knowledge of the PlioceneQuaterniry stratisraphy of ,lt. ,investigated area is
summ arned in Tei't-dgt' 2a-b (redrawtt "id simplified
from Mazzanti, 1987).
Text-fig. 2a shows an ideal section berween the
Pisa Plain and the Livorno hills. The Quaternary
Livorno hills successionis char acterrzedby three main
informal formations (Barsotti et al., 1974; Bossio et
dl., 1981; Mazzanti, 1984; Lazzarotto et al., 1990;
Marroni et Al., 1990; Bossio et al., 1993; Pasquinucci
et al., 2001). From the base they are: 1) the Lower
Pleistocene(Santernian-Emilian) Sandsand Clays with
Arctica islandica, which rests transgressivelyon the preQuate rnary substratum, represented by the Middle
Pliocene Yellow Sands; 2) the Lower Pleistocene
(Emilian) Nugola Vecchia Sands, representing the
regressivephase of the Santernian-Emilian rycle; 3)
the primarily continental Middle PleistoceneFattoria
delle Pianacceformation. To the North the Pisa Plain
succession (Text-fig. 2a) is the result of rwo main
sedimentary cycles separated by an erosive phase
originated during the marine low stand of the Last
Glicial Ma,ximum (Mazzanti, 1987, 2001; Federici 6{
Mazzanti, 1995). The older succession develoPed
during the Upper Pleistoceneand comprises_theArno
and Serchio Gravels, the Aeolian Sands of Coltano
and the Sands and Muds of Vicarello (Lazzarotto et
dl., 1990). The younger Upper Pleistocene-Holocene
successioncomprisescontinental and marine deposits,
the latter being related to the Versilian transgression
and subsequentphases.
Text-fi g. 2b shows the main stratigraphical features
of the Livbrno Terrace. As previously mentioned the
Livorno Terrace formed during the marine high stand
of the last interglacial, i.e. Ois 5e or Euryrrhenian
(Shackleton, 1987, Hearry et al., 1986; Federici &
Mazzanti, 1995; Mauz, I99r, which originated a few
meter-tick calcarenitic layer ("panchina") yielding
"senegalese"
or Strombus fossil community
locally
"panchina"
(Barsotti et al., 1974). This
layer ("panchina
I") is covered by thin continental deposits referred to
as Ardenza Sands and Rio Maggiore Conglomerates
(Lazzarorroet al., 1990). A thinner second calcarenitic
level ("panchina II"), mainly of aeolian facies,is locally
intercal-atedin the continental succession.Accorditg
to the recent work of Mauz (1999) at Buca dei Corvi
(near Castiglioncello, about 15 hn S of Livorno) and
in agreemJttt with the supposition of Federici 6c
"panchina"
layer would
Mazianti (I99r, the second
correspond to the Ois 5c. This successionwas well
documented in the spectacularsection of the dry-dock
"Torre
of
del Fanale" (Barsotti et al., 1974), excavated
in the harbour of Livorno about thirry years ago and
no longer visible.
r43
NEW INSIGHTS ON THE QUATERNARY
STRATIGRAPHYOF THE LIVORNOARfu
LIVORNOHILLS
(Fattoria Pianacce Terrace)
PISA PLAIN
2a
@
Yellow Sands fm.
(Middle Pliocene)
")-fii:surrace
-'-*-if,"gre
ssivesurface
2b
Livorno
LIVORNO TERRACE
3
+-.
.1 ,F-.*-{
Pliocene-Lower Pleistocene sediments
.v
4
Text-fig. 2
a) Ideal section berween the Pisa Plain and the Livorno hills: I ) Sands and Clays with Arct
Sands; 3) Fattoria delle Pianacce continental deposits; 4) Arno and Serchio Gravels; 5) fluvi
Sandsof Coltano; 6b) Sandsand Muds ofVicarello; 7) Holocene fluvial sediments; 8) Holocene r
of the Versilian transgression (redrawn and simplified from Mazzanri, 1987).
"panchina
I"; 2) calcareniti,
b) Stratigraphical featuresof the LivornoTerrace: l) calcarenitic layer
Sands and Rio Maggiore Conglomerates; 4) sediments of the Versilian transgression (redrawr
1987).
In the area of the city of Livorno, which is
investigatedin the present study, the substratum below
"panchina"
layer is made up of Pliocene-Lower
the first
"Torre
Pleistocenedeposits.Notably, in the spectacular
del Fanale" Section it consists of a Lower Pleistocene
marine succession(.". 15 m-thick) dipping of about
15' toward Northwest. Barsotti et al. (1974) assigned
"late
Calabrian"
these basal marine sediments to the
on the basisof the co-occurrenceof the bivalve Arctica
islandica (Linnaeus) and the benthonic foraminifer
Hyalinea baltica (Schroeter). A more detailed
biostratigraphical constrain was later provided by
Gianelli et al. (1982), who referred the successionto
the lower Emilian (Helicosphaerasellii Zone of the
calcareousnannofossils).
MATERTALS
AND METHODS
On the whole 15 continuously cored boreholeswere
investigated (Text-fig. 3). Boreholes depth varies on
averagefrom 20 to 25 m, the deepest borehole pen-
etrates down to -34 m below s.l. (depth will be
throughout referred to sea level).
Analyses performed were primarily based on
lithological-sedimentologicd observations,which took
lnto account colour sediments,grain size, presenceof
sedimentary structures and also the macrofaunal
content. Micropalaeontological analyseswere carried
out on a selectedset of about one hundred samples,
which could be considered representativeof the main
different lithologies recognized. Investigations were
focused chiefly on ostracods,but comprised partly also
benthonic foraminifers (planktonic forms are usually
absent or extremely rare) and occasionally calcareous
nannofossils.Data from thesegroups and from remains
of molluscs, echinoids, charophytes, seeds,etc. were
used for biostratigraphical purpose and palaeoenvironmental reconstruction. Specifically, biostratigraphical significance of the ostracod fauna is based
primarily upon papers by Ruggieri and co-workers.
Among these there are Ruggieri (1950, I952a, b,
1953a, b, 1954, 1972, 1973a, b, I975a, b, I976a,
r44
B. DALLANTONIA, A. CIAMPALINI,L. MICHELUCCI, G. ZANCHETru, A. BOSSIO,F,PBONADONNA
1977, 1978), Aruta & Ruggieri (1983) and particularly Ruggieri ( 1980), which provided a list of species
useful for the stratigraphy of the Italian Pleistocene.
Subsequentstudies-or unpublished researchof the
preseni authors have been took into account to check
ihe reliabiliry of marker ostracod species(seeappendix
for details on the stratigraphicaldistribution of marker
species).Calcareousnannofossilsanalyseswere carried
out by Dr. Agata Di Stefano (Dipartimento di Scienze
Geologiche,Univ. Catania, Italy); the biozonal scheme
adopted is that of Rio et al. ( I 990). Finally, 7
radiocarbon dating (AMS and conventional, performed
b y C e n t r e f o r I s o t o p e R e s e a r c h , U n i v e r si t y o f
Groning€o, The Netherlands) from wood or mollusc
shells were util ized to provide a reliable
chronostratigraphical framework (T"b. I ) for the
younger deposits.Dates on marine shells and remains
of Poiidonii oceanicahave been corrected for the marine
reservoir effect, that can be reasonablyassumedto be
ca. 400 yr for the whole middle-upper Holocene of
the Mediterraneansea (Siani et al., 2000, 2001).
O
The stratigraphicalreconstruction herein proposed
took into account the previous studies on the subsurface geology of the Livorno surroundings mentioned
above and-assumedas a k.y section the successionof
"Torre
del Fanale" in the harbour of
the dry-dock of
Livorno, describedby Barsotti et al. (1974).
RESULTS
The multidisciplin ary lithological, palaeontological
and geochronologicalstudiesrevealedthat the 15 cores
analyzeddisplay a highly variable range of lithologies
and faunal associations.However, single lithofacies have
been schematicallygrouped into 7 main stratigraphical
units, some of which can be correlatedwith formations
outcropping in North-western Tirscany. Lithology of
single borehole and stratigrap.hicalcorrelation of rhe 7
units recognized are shown in Text-fig. 4. The units
are described below from base to top; stratigraphical
and palaeoenvironmentalconsiderationsare also provided.
Boreholes
\"ro?Yol?Hl1,",,
Text-fig.3
Location of the | 5
investigated boreholes.
STRATIGRAPHYOF THE LIVORNOARE/
NEW INSIGHTS ON THE QUATERNARY
Laboratory
Sample
NO
NO
Material
Borehole
Depth
'"C-age yr
(m below s.l.)
BP
-r9.3
> 50,300
6ttCpon
7oc
GrN-26356
CZI2
Wood frag.
F
GrN-26355
BZOS
Wood frag.
G
-8
GrN-26610
CLI2ASI
Posidonia
C
-8.4
1 4 8 0! 4 0
- r 3.98
CI
oceanica
CZOI
Posidonia
A
3.2
l5 l0 t 100
-t2.21
B
-9.6
+ 45
1330
-t3.23
E
-7.5
4930+ 60
I
-10.4
> 45.000
GrN-2661I
r45
> 40.700
oceanica
GrA-20211
GrA- 19972
C L I S S 2 C Posidonia
I
oceanico
CZO652
Marine
shells
GrA-21608
DLOIDC
Marine
shells
UNn I
Description Unit I includes rwo subunits (1A
and 1B).-subunit 1A is characterizedmainly by sandy
silts (borehole N) and bluish- grey clays and silry clays
(boreholesO, B Q); the marimum cored thickness is
about 17 m. Locally (borehole Q) sandy horizons with
marine fossil remains (among molluscs Nuculana,
Turritella, Conus, Bittium) occur. Uppermost levels of
this subunit are abruptly overlain by sedimentsof Unit
3 and are characterized by colour banding and
calcareous nodules, which suggest an episode of
subaerial exposure (palaeosol).A single exception is
borehole N, where Subunit 1A passesupwards to
coarser sediments referable to Unit 2. Microfaunal
content of Subunit 1A is not thoroughly homogeneous.
Samples from borehole N usually bear scarce to
moderately rich associations.Planktonic foraminifers
(Globigerinida) are extremely rare; benthonic
foraminifers are represented primarily by the genus
AmmoniA, includitg usually both ,4. beccarii(Linnaeus)
and A. tepida (Cushman), Elphididae (ElPhidium) and
locally Miliolidae. The moderately diversified ostracod
a s s o c i a t i o n sa r e c h a r a c t e r i z e d b y t h e c o m m o n
occurrence of the euryhaline species Cyprideis torosa
(Jones)and the marine nearshoreopportunistic species
Pontocythereturbida (Mtiller). Aurila conuext (Baird),
Kollmann, Semicytherurt
Cytheridea "?llktafa
incongruens (M tiller) are subordinately present;
occasionally also Callistocythereflauidofusca (Ruggieri)
and Aurila cymbotformis (Seguenza) are wellcontain also a few
r e p r . e s e n t e d .Y " , . y
:3pples.
specimens of the brackish speciesLoxoconchaelliptica
Brady and rare representativesof the fresh water genera
Thb. I - Radiometric ages technical
data ('aC-ages are not
corrected for the marine
reservoir effect).
Ilyocypris and/or Candona; rare charophyr" oospores
were found at -14.5 m. In borehole Q assemblages
are rather rich and diversified. Fragments of marine
bivalves,gastropodsand echinoids are common. Planktonic foraminifers (Globigerinida and Globorotalida)
are relativelywell represented;marine benthonic forms
are very abundant ind highly diversified; Miliolidae,
Elphididae, Textulariidae, Discorbidae (Valuulineria)
and Cibicidae (Cibicides) are locally frequent. Ostracod assemblagesconsist of marine nearshore ta>(aand
Aurilinae attain a significant portion of the fauna,
among them there areAuril^a conuex*,A. foll^ Ruggieri
and subordinately A. gr. hesperiarRuggieri, A. punctata
(Mtinster) , A. cymbaeformisand A. cf.fastigataUliczny.
In the uppermost sample, the fauna includes also frequent Urocythereisspp. and very few juveniles of
Cyprideis torosa and the fresh water genus_
In boreholes O and P fragments of
Pseud.ocAnd.onA.
marine bivalves, gastropods and echinoids are widespread. Benthonic foraminifers usually dominate the
microfauna, whereas planktonic foraminifers (mainly
Globigerinida) are scatterlypresent.In borehole O foraminifers are primarily represented by Miliolidae,
Discorbidae (Valuulineria) and Hyalinea baltica is notably present. In borehole P Miliolidae, Bolivinidae
(Boliuina) and Cassidulinidae (Cassidulina) dominate.
The major components of the usually abundant ostracod fauna are forms rypical of open marine conditions. They are Krithe praetexta (Sars), Cytheropteron
ruggierii Pucci, Loxoconc/ta subrugosa Ruggieri, L.
mutabilis Ciampo and Cytherelh uulgata Ruggieri; locally Aurila cymbaeformis and Carinoualua testudo
(Namias) are relatively well represented.
Subunit I B includes silt-sand alternations (bore-
146
L. MICHELUCCI, G. ZAT{CHETA,,
B. DALL:ANTONU, A. CI,,4,A4PALINI,
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STRATIGRAPHYOF THE LIVORNOARfu
NEW INSIGHTS ON THE QUATERNARY
holes I, G, H), fine/medium sands (borehole I) and
clay-fine to coarsesand alternations (borehole L). The
morimum thicknessis about 20 m. Samplesfrom this
subunit yield a very scarceand moder?tgly preserved
microfauna. Assemblagesare dominated by the brackish foraminifer Ammonia tePida,but contain atso_v9ry
few representativesof Ammonia beccarii, Elphidid.ae
(Elphilium), Nonionidae (Florilus) and Miliolidae. The
ostracod fauna is extremely poo r. Aurilo ty*baeformis,
Costa edwardsi (Roemer) (juveniles), Cyprldeis torosa
sP.(jt(juveniles), Pontqcythereturbida, Pseudocand.ona
veniles), Xestolebiriscommunis Mtiller were recorded.
Only a single sample (from borehole H; -14.00 m) is
chaiacterizJd by t relatively rich fauna with dominant
Ammonia tepidn; the ostracod fauna consistsprimarily
of Loxoconchaelliptica and Cyprideistorosa(some specimens are tuberculate).
Stratigraphical and palaeoenuironmental remarhs
OstracoJ"tiociations recorreredin Subunit 1A include
a number of taxa, which are relevant for
biostratigraphical purpose. These -significant taxa,
which usually occuf paichily and in low numbers' can
be divided in rwo distinct grouPs: 1) speciesknown
from the Pliocene, which d-isappearedby the end of
the Lower Pleistocene (Sicilian), i.e. Aurila
bullapunctata extumefacta lJliczny' (very rare) , A.
cymb'atformis (rare to frequent), A. lanceaeformls
lJliczny (very rare), A. pigadiana Sissingh (very rare),
A. pun'ctata (rare to common), Carinoualua testudo(rare
to'frequent) , Flexus rriebeli (Ruggieri) (very rare); 2)
taxa, which to date are not known to occur prior to
(Brady) (very
the Pleistocene, i.e. Aurila arborescens
('neY rare),
(Mtiller)
rare) , Cytherelloidea sordida
(very
Ruggieri
L.
rubritincta
rare)
Loxoconiha elliptica
,
( v e r y r a r e ), L r u b r u g g s a ( r a r e t o f r e q u e n t ) ,
(lr.ry rare),
Neocytherid.eis
fasciqta (Brady S{ Robertson)
Palmoconcha-turbida (Mtiller) (rare to frequent),
subspiralis (Brady, Closskey F Robertson)
Prorytherid.eis
(".t1' rare). Finalfy,^ single sample (boreholeN; -18.5
m) is characterizedby thE occurience of Aurila fauorita
Ruggieri (very rare), known from the Emilian-Sicilian
interval (Ruggieri, 1980)The co-occurrenceof the rwo grouPs of ostracod
speciesmentioned above allows to refer Subunit 1A to
th. Lower Pleistocene.In addition, the Presenceof
Hyalinea baltica allows to exclude a Santernian $e. Qr
sediments encountered in borehole O (R.tggieri 6{
Sprovieri, 1978). Finally, it is-worth mentiolilg that
nb palaeontological data in favour of a Sicilian €e
harrebeen recor:dedin Subunit 1A. It follows that this
subunit can be reasonably referred to the Emilian.
similar
t?4 l.ty
Comparison with the. ":1*y
"Torre
del Fanale",which
successlonof the dry dock of
has been assignedto the lower Emilian, corroborates
our inference.
Faunalcontent of Subunit 1B is not highly suitable
to provide reliable age constrains. However, the cooccurrence, although at distinct levels, of Aurila
r47
a Lower
rymbaeformisand Loxoconchqelliptlca suggests
Pl.irtol.tt. ase. Further informltion can derive from
consideration on the stratigraphical position of this
subunit. In this respect,it must be taken into account
that sediments of^ Subunit 1A, encountered in the
southernmost boreholesof the Livorno Terracedomain,
dip towards Northwest (Barsotti .e.tal., I97 4) and that
Subunit 1B, drilled in northward boreholes,is overlain
by the Sicilian Unit 2 (seebelow)..This implies that
Subunit I B can be reasonablyplaced berweenSubunit
1A and Unit 2 and therefore asiigned to the late Lower
Pleistocene(Emilian).
Micro-macrofaunal content indicatesthat sediments
of Subunit 1A formed in a shallow marine environment
with p.redo.minantlynormal salinities (most of the
successlondocumented in borehole Q) and subordinate
local influences of fresh-brackishwaters (borehole N
and top of the successionin borehole Q)..Assemblages
from bbreholesO and P can be interpreted as reflecting
a local transition to relatively deeper environments or
colder bottom water conditions.
The pauciry of the fauna recoveredin Subunit I B
together^with the dominance of Ammonia tepida "tt4
loially, among ostracods of Loxoconchy elliptica and
Cyprideis turosa, are characteristic of unfavourable
p"l".oenvironmental conditions, mosdy referableto a
brackish water setting.
UNtr 2
Description- This unit is documented in boreholes
E H, I, L, M, N and presumablyalso in borehole G.
Lower levelsconsist mainly of coarse(loc"lly fine) sands
and gravelswith sparsepebbleswith a thicknessvaryi.g
froni 4 meters to a few decimetres. These coarse
sediments are overlain by a fairly variable succession,
which includes fine silry iands (boreholeM), fine sands
passingupwards to silts (borehole H) and clays,locally
itrt.r.ilat^.d with gravels, followed by fit-. to coarse
sands (boreholeJI, L). Unit 2, which shows a
maximum thickness of about 12 m, is documented
also at the bottom of borehole F by silry sands (1 mthick). On the basis of lithological affinities and
geometric position, sands ryi,L grivels recoveredfrom
17.7 to -1^0.5 m in borehole Glt'n. been included in
the present unit. Unit 2 is normally-abrqPdy overlain
by
' cilcarenitic deposits ("panchina" layer) of Uni r 3.
from a- few exCeptions,samPles from this
Apart
^display
unit
- a rich faunal content. Fragments of
echinoids, and marine molluscs are frequent.
Planktonic foraminifers (mainly Globigerinida) are
occasionallypresent and are relatively abundant only
in silty-cl'ayey levels. Benthonic foraminifers are
represented mostly by the - gelus . Ammonia
(piedominantly A. beccarii and subordinately, in
bbreholes H, i, and N, A. tepida), Miliolidae and
Elphididae (Elphidium). Discorbidae (Valuulineria) and
Nonionidae (Florilus) can be frequent in silry-cl ayey
sediments. Sample collected at -f 8.6 m in borehole
r48
B. DALL:ANTONIA,A, CIAMPALINI,L, MICHELUCCI, G. ZANCHETru, A. BOSSrc,EP BONADONNA
M is characterized by the presenceof Hyalinea baltica.
Ostracod faunas are often highly diverse and
comprise almost exclusively marine forms . Aurila
rymbaeformis, A. punctata, Cytheridea neapolitnna,
Lo*otincha ouulata (Costa),- L. subrugosi, Krithe
praetexta, Palmoconclta turbida are among the most
Trequent and recurrent taxa. Bosquetina d.entata
jonesi (Baird) and Aurila
(Mtiller), Pterygocythereis
puncticruciata Ruggieri are particularly abundant in
borehole I, H and M respectively. Rare fresh and
brackish water ostracods (..g. Candona Sp., Ilyocypris
sp., Cyprideis toros*, Loxoconcha ellipticd were found
only in boreholesH, I, and N.
Stratigraphical and palaeoenuironmental remarks
fu for Subunit 1A, ostiacod assemblagesrecovered in
Unit 2 are indicative of a Lower Pleistoceneage. This
is documented by the co-occurrence of rypical
Quaternary species, i. e. Loxoconclta elliptica, L.
subrugosa, Nto ty th erideisfasciata, Palmoconclt a tur bida,
Procytherideis subspiralis, with Pliocene-Lower
Pleisiocene species (Aurik bullapunctatd extumefact*,
A. cymbaeformis,A. lancaeaformis,A. pigadiana, A.
punctata, Carinoualua testudo, Flexus triebeli,
-Pachycaud.ites
Other
Ruggieri).
attenuata
biostratigraphical significant ostracod taxa are Aurila
puncticriciita and Aurila fauoriya, which are restrained
"cold
guest"
to the Emilian-Sicilian interval, and the
Muellerina problematica (Seguenza), known only from
the Lower Pleistocene(Ruggieri, 1980). These species
are usually p^resenl, it very .low numbers, with the
exception of Aurila punctimuciata. According to
Rugfieri ( 1980) this speciesis rare in the Emilian and
bec-oln.r frequent only in the Sicilian. A Sicilian age
for sedimentl pertainitg to Unit 2 is supported also
by calcareous nannofossils analysi_s.Associations
recoveredin boreholesM and F are referable,although
"small
GephyrocaPsa
affected by reworki^g, to the
Zone".
From a palaeoenvironmental viewpoint faunal
conrent of Unit 2 is characteristicof a nearshoremarine
environment with euhaline conditions; a relatively
deeper setting of deposition could be supposed for
^yey leiels. Evidence of a fairly feebG^influence
silry-cl
-fresh-brackish
waters is documented only in
of
boreholesH, I, and N.
UNrr 3
Desription - This unit has been recognized in the
subsurfaie of the Livorno Terrace (boreholesO, B a
and also in more seawardboreholes (boreholes H, I,
L, N). It rypically includes a well cemented calcarenitic
layer, from- a few decimetres to I meter thick (owing
to drillirg activiry this consolidatedlevel is occasionally
reduced io fragments immerse in a sandy matrix) and
a basal .ottglomerate, from I to 2 meter thick
(boreholesI,-O, P). Abundant marine shell remains
are usually present. In borehole P this unit includes
also yellowish fine sands (.". 3 m-thick) with sparse
"panchi.""
laygr qtd marine
fragments of the underlain
molluscs. Data from drilled boreholesclearly indicate
a seawardincreasi.g depth of Unit 3 (from + 1 I m in
borehole a to -7 .5 m in borehole L). Sediments
of this unit are usually not suitable for micropalaeontological analyses;the few most favourable
samples are characterized by a highly heterogeneous
miciofauna with frequent, clearly reworked elements.
and palaeoenuironmental remarks
Snatigraphical
Unit 3 corresponds to the Upper Pleistocene
transgressivedeposits ("panchina' layer) well known
in thE coastal stiip near Livorno and particularly well
"Torre
del Fanale". The
studied in the dry-dock of
calcarenitic layer recovered in our borehole can be
"Torre
"panchina'
layer of
del
correlatedwith the first
Fanale" (Ois 5e, ca. 125,000 yr BP). This is supported
by the manifest marine origin (abundant shell remains)
and consistencyof depths attained in drilled boreholes
"Torre
del Fanale" succession.
with that observed in
Radiocarbon dating of Turritelk shells form fine sands
"panchina
layer" (borehole I)
a few meters below the
EXPLANATION OF PLATE I
- Aurihfauorita Ruggieri.LV (SubunitlA boreholeN; -18,5 -).
Fig. I
- Auriln"arborescens(Erad,f).
6 right view.(SubunitlA boreholeN; -21.5 m).
FiE.2
- Auriln punctata(Mtinster).RV (Unit 2 boreholeM; -18.6 m).
Fig. 3
Ruggieri.4)LV (Unit 2 boreholeM; -18.6 m);7) RV (Unit
Fi[s. 4,7 - Aurila'puncticruciata
- Auriln'knggaeformis
Uliczny.-Lv(SubunitlA boreholeN; -14.5 m).
FiE.5
- Aurila bulkpunctataextumefactaUliczny.
RV (Subunit lA borehol.Q +2.1 m).
Fig.6
8) LV (Unit 2 boreholeM; -16.7 m); 9) RV (Un
Fi[s. 8-9 - Aurila ty*fiqrformis(Seguenza).
LV (Unit 4 boreholeG; -7.3 m).
fi[. tO - Aurik jigadiiza Sissingl't.
- Bythocythere
puncticukiaRuggieri.RV (Unit 2 boreholeM; -18.6 m).
Fig. ll
"bythocytheri"
minima Bonadlce,Ciampo 6( Masoli (x 90). LV (Unit 2 borehole
FG. 12 - MiotypT;dtititaliana Moos. LV (Subunii 78 boreholeA; -2.5 m).
FiE. B
Fig. 14 - Celtii rugosa(Costa).RV (SubunitTB boreholeA; -2.5 m).
Fig. 15 - Flexusniebeli(Ruggieri).LV (SubunitlA boreholeN; -21.5 m).
(Seguenza).
LY (Subunit78 boreholeA; -2.5 m).
rcnapteri-s.1.
Fig. 16 - Ruggreria
& Robertson).LV (Unit 4 boreholeG; -7.3 m).
FiE. 17 - Neocltherideis-farciata(Brady
- Procytherideisiubspiralis
(Brady,Crosskey& Robertson).LV (Subunit lA borehol
FiE. l8
ostracodtaxa.All viewsexternallateral(x 55 unlessoth
of selected
S.E.M. microphorographs
150
B. DALL:ANTONIA,A. CIAMPALINI,L. MICHELUCCI, G. ZANCHETTA,A. BOSSrc,EP BONADONNA
greater than 45,000 yr BP and
have provided "l ,"g.
""rr"Lfpper
Pleistocene age for the
are consistent with
"panchina"
layer.
UNrr 4
Description- This unit has been recoveredonly in
borehole G. It consistsof grey-bluish silry-clayeysands
(l m-thick) with disperseremains of Turritella, which
are overlain by silry sands (c". I.5 m-thick). Lower
levels are characterized by very abundant fragments of
marine molluscs and echinoids. The microfauna consistspredominantly of marine taxa, but euryhaline and
brackish-fresh water forms are relatively well represented. Particularly, benthonic foraminifers are dominated by the genus Ammonia (preval endy A. beccarii
and secondarlll A. rcpidn)and subordinately Elphididae
(Elphidium) and Miliolidae. Ostracod associationsare
quit. rich and diversified, the major comPonents beihg nearshoremarine til(a such as Pontocythereturbida,
Citheridea neapolituna, Loxoconchinae (Loxoconcha
bhirdl Mtiller ,- L. ouulata, L. subrugosa,P. turbida),
Cistacythereis turbida (Mtiller), Costa edwardsi and
Carinorythereiswhitei (Baird). The fauna, however, includes dso Cyprideistorosa(common) and representatives of llyoqtpris and Candona. In ttt. uPPer levels
benthonic foraminifers are representedmainly by A.
beccarii, A. tepida, Elphididae (Elphidium) and
Nonionidae (Florilus).Th^eosffacod assemblageis made
up mosdy by Cyprideis torosA and representatives of
t6. genui llyocyjiis; marine til€ (e.g. Costa ed'ward.si,
Palrioconchi iirbida, Semicytheruri incongruens) are
present in very low numbers.
Stratigraphical and palaeoenuironmental remarks
Unit 4 is-not easily interpretable from a stratigraphical
viewpoint. Ostracod associationsare characterized !y
rypicil Quate rnary species (e.8. Cytherelloideasordida,
Lixoconcha subrugosA, Niocytherideis fasciata,
Palmoconchaturbidi). The lowermost sample (borehole G; -7.3 m) contains in very low numbers also
Pliocene-Lower Pleistocenespecies (i... Aurila
and
clmbaeformis, A. lanceaeformis,-A. pigadiana.)
-*hich
not
does
a
species
Mooi,
italiana
Mioryprideis
-the
Pliocene/Pleistocenebound ary (R,tggieri,
crosi
1980). The co-occurrenceof the abovementioned taxa
indicates reworking. On the whole, microfaunas are
indicative only of J generic Quaternary age.Radio carbon dating of wood fragments from the lowermost
sample provided a minimum age of 40,700 yr BB but
it cinnot be excluded that wood fragments are reworked.
Further data can derive from consideration on the
geometric position of this unit. It has been recovered
Snly in th. borehole drilled in proximity of the
"Gionda
dei Lupi" erosional scarp, which seParates
the Livorno Teirace from the Pisa Plain. In this
"panchina"
layer is lacking and at more
borehole, the
or lessthe same depths at which it occurs in southward
boreholes,we recoveredsediments of Unit 4. Unit 4
is comprised berween coarse sediments tentatively
referred to the Sicilian Unit 2 and Subunit 7b
(Holocene). fu a consequence,it can be supposedthat
deposition of Unit 4 took place afrer the deposition
and subsequent erosion of the Upper ?leistocene
"panchitd'
p,erlrapsalso,of pTt of the Sicilian
layer
?ttd
successlon.On the whole, available data suggestthat
"panchina"
laygr (Ois 5.),
Unit 4 is younger than the
In addition, Unit 4 cannot be younger than Unit 6
(seebelow), therefore we tentatively refer this unit to
the Upper
-ihe Pleistocene.
lower levels, the abundant shelly material
In
and the composition of the microfauna are indicative
of a very shlllow marine environment with a near
source of fresh water input. Upwards the dominance
of fresh-brackishwater forms documents ^ transition
to a predominant brackish environment.
UNrr 5
Unit 5 can be divided into two
Description
subunirs (5A and 5B). Both were recoveredaboveUnit
EXPLANATIONOF PLATE2
- Loxoconcha
rubritinctaRuggieri.RV (Unit 2 boreholeN; -5.2 m).
Fig. I
minima Miillei.-LV (Unit 2 boreholeI; -10.4 m).
Fig.2 - Loxoconcha
ellipticaBrady.RV (Subunit78 boreholeA; -5.2 m).
Fig. 3 - Loxoconcha
paialtek Mtifier. RV (Unit 2 boreholeI; -10.4 m).
Fig.4 - Loxoconcha
turbida (Mtiller). RV (Subunir 78 boreholeA; -5.2 m).
Fig. 5 - Palmoconcha
Ruggieri.RV (Unit 2 boreholeH; -6.5 m).
subrugosa
Fig. 6 - Loxoconcha
anenuataRuggieri(x 55). RV (Unit 2 boreholeI; -l1.7 m).
Fig.7 - Pachycaudites
Fig. 8 - Muilhrina problematica(Se[uenza).LY (Unit 2 boreholeH; -10.0 m).
Stambolidis(x 55). RV (Unit 2 boreholeH; -8.5 m).
ihrakienszi
Fig. 9 - Cytherelln
praua(Baird)(x 55). RV (Subunir.78 boreholeF; -5.1 m).
Fig. l0 - Tbnedocythere
Fig. I I - Cypridiistoroia(Jones)(x 40). RV (Subunit1A boreholeN; -21.5 -).
sordida(Mtiller) (* 55).LV (SubunitlA boreholeQ; +10.6m).
Fig. 12 - Cytherelloidea
laeuis(Mtiller). RV (Unit 6 boreholeB; -23.5)
F i g .1 3 - Cyclocypris
Fig. 14 - Candina neshctaSars(x 40). RV (Unit 6 boreholeB; -26.5 m)
F i g . t 5 - Ilyoc.ypris
si6ba (Ramdohr)(x 55). RV (SubunitTB boreholeA; -2.5 m).
S . E . M .-i.rop6otog"raphsof selectedostracodtaxa.All viewsexternallateral(x 90 unlessotherwisesl
r52
B. DALL:ANTONIA,A. CIAMPALINI,L. MICHELUCCI, G, ZANCHETA, A. BOSSIO
3 in boreholesdrilled in the Livorno Terrace (O, B a
boreholes).The lower Subunit 5A comprises mottled
silt or clay-sand alternations with sparse carbonate
glaebulesand coarsesandy gravels (1-5 m-thick). The
basalcontact with Unit 3 is usually sharp. Subunit 58
comprises sands and reddish silty sands with
millimetric nodules of manganese. Rare levels of
gravelly sand are also present. Both the subunits are
barren of fossils.
Snatigraphical and palaeoenuironmental remarks
The geometric position of this unit with respect to
Unit 3 indicates an age younger than the Ois 5e. The
environmental interpretation of Unit 5 is facilitated
by sections exposed on the Livorno Terrace. Subunit
5A shows an alternation of decametric sheet-like
gravelly deposits with silry sands. Some gravel bodies
show fining upward organization and a concaveerosive
basal surface. Overall, Subunit 5A accumulated in an
a l l u v i a l p l a i n e n v i r o n m e n t c h a r a c t e r iz e d b y
palaeochannels with gravelly bedload transport.
Subunit 58 shows clear feature of weathered deposits;
gravel levels are less frequent than in the previous
subunit. It likely representsan environment dominated
by superficial alteration with sporadic supply of
sediments from ephemeral streams.
UNrr 6
Description - This unit comprises sandy silts and
silry-cl ayey sands recovered from -7 to -31 m in the
northern boreholes (boreholesA, B, C, D, E, F); the
maximum cored thickness is about 15 m. Carbonate
glaebules,plant remains, non-marine shells are
common throughout; charophy," oospores are often
present. Unit 6 is sharply overlain by Unit 7. In
boreholes D, E and F lower levels of this unit are
usually characterized by fresh water molluscs (e.g.
Bithynia, Ancylus, and Pisidium) and land snails (e.g.
Carychium, Wrtigo, Vallonia, Punctum, Limax, and
Tbstacella).Fresh water ostracods are locally well
represented; they belong mainly to llyocypris and
Candona, includitg Pseudocandonacompressa(Koch),
and subordinately to Cycloryprislaeuis (Mtiller) and
Pseudocand,ona
spp. In the upper levels, land snails
are still present; they are represented mainly by
Carychium and to a lesser extent by Vallonia, Discus
and Monacha, whereas fresh water ostracods become
extremely rare. The only fresh water mollusc species
is Qtmnea.
Faunal content of boreholes B and C differs only
slightly from that above described. Remains of fresh
water gastropods (Bithynia and Valuata)and land snails
(Carychium and Limax) were found patchily also in
theseboreholes.Microfaunas are usu"lly very poor and
include marine and brackish (e.g. Ammonia tepid.a,
Protelphidium) benthonic foraminifers and very rare,
reworked planktonic forms; ostracods comprise freshbrackish water taxa and locally very rare marine forms.
Only two samples(borehole B; -26.5 m and borehole
C; -16.4 m) yielded a rich fresh water ostracod fauna
(comprising adults of Candona neglecmSars). Fairly
abundant benthonic foraminifers with dominant
Ammonia tepida were recoveredat -22.9 m in borehole
C and at -24.5 m in borehole B.
Snatigraphical and palaeoenuironmental remarhs
Radiocarbon dating from wood fragments collected
in the lower levels of this unit (borehole F; -19.3 m)
indicates an age greater than 50,300 yr BP. The
stratigraphy of this unit indicates that it is older than
Holocene deposits (Unit 7) and younger than Unit 2
of Sicilian age (see borehole F); furthermore, it is
probably also younger than Unit 3 and Unit 4.
Therefore, w€ infer that Unit 6 is still Upper
Pleistocenein age.
Fossil assemblagesrecovered in this unit are
indicative of an alluvial plain environment with
ephemeral water bodies. In the northern boreholes,
the irregular alternation of non-marine and brackish
faunas is considered to reflect tempo rary exchange
berween continental and marine waters.
UNrr 7
Description - This unit includes rwo subunits Qn
and 7B). The lower one (Subunft 7A) consistsof fine
to coarsesands(boreholesA, B, C, D, E, F) with local
concentrationsof gravels(boreholesA, B, D), recovered
from a maximum depth of -19.0 m to a minimum
-3.8 m. The qpp.er subunit (Subunit 7B)
depth
.of
comprises alternations of silry sands and sandy silts
often rich in Posidonia oceanicaremains and locally
marine shells.Subunit7B has been recognizedin most
of the investigated boreholes (boreholesA, B, C, D,
E, F, G, H, I, L, N), where it occurs from a maximum
depth of -l 1.6 m ro +1.0 m.
lVith the exception of the uppermost levels,which
can display concentration of marine shells, sands of
Subunit 7A are almost barren of fossils. They
occasionally include (borehole A) rare remains of
echinoids and very scarcemicrofaunas, with possible
local mixing of marine, brackish and fresh water
elements.
Faunal content of the upper subunit is variable.
Levels with Posidonia oceanicaremains are usually rich
in marine gastropods (..g. Aluania, Calliostom*,
Cerithiutrlt, Cerithiopsis, CrytospirA, Cythara, Gibbula,
Hinia, Jujubinus, Tricolia, RissoA,Binium, Turritelln)
and subordinately bivalves (e.g.Acanthocardia,
Chkmys, Dosinia, Ledn, Pectunculus, Wnus, Wnerupis,
Nucula, Tbllina). Microfaunas are abundant and
comprise highly diverse, shallow marine foraminifers
and ostracods (e.g. Aurila conuexA(Baird), Aurila
fallax Ruggieri, Bairdia longeuaginata Miiller,
Bythocytltereminima Bonaduce, Ciampo 6a Masoli,
Costa batei (Brady) , C. edwardsi, Carinocythereiswhitei,
Caudites calceolatus (Costa), Cytberelloidea sordid.a,
STRATIGRAPHYOF THE LIVORNOARE/
NEW INSIGHTS ON THE QUATERNARY
Loxonclta ouulata, L. rhomboidea (Fisher),
Ph lyctocythereglo bosa (Schornikov) , Pontocythere
praua (Baird), Xestoleberis
turbldoi Tbned"ocythere
communis, X. decipiensMtiller).
Remaining sediments locally yielded microfaunas
characterizedby t mixing of marine, brackish and fresh
water forms. Ostracodi can include rare reworked
specimens pertainitg to Cehia rugosa (Costa), Flexus
fiebeli, Miocyprideis italiana, and Ruggieria tetraPtera
(Seguenza).
Snatigraphical and palaeoenuironmental remarks
Radioc"frot dating frbm shell remains collected at
the top of Subunit 7n $orehole E; -6.2 m) provided
an age of 4,530x60 yr BP and allowed to attribute
"Versilian
transgression".
this subunit to the late
Radiometric ages of Posidonia oceanicaremains from
lower levels of Subunit 7B range berween 930x45 yr
and 1 I 10t 100 yr BB indicatitg that deposition of
these sedimentspersistedtill historical age. It is worth
mentioning that bottom of Subunit 7A displays_a
northward increasingdepth (from -7.0 m in borehole
F to -19.0 m in bor-eholeA); on the whole, this holds
true also for Subunit 78 (from -5.8 m in borehole F
to about -11.5 m in boreholesA and B).
On the whole, Unit 7 is interpreted as transgressive
deposits related to the onset of a sandy shore coastal
syitem. Sands with local gravel horizons can be
consideredto representbeach-ridgedeposits;silry sands
and sandy silts with P oceanicamay have accumulated
both in a shorefaceenvironment and in a shallow
m a r i n e s e t t i t g ( D e l l a P i e t i , 1 9 84 ) . T h e l o c a l
occurrence of biackish-fresh water microfaunas mixed
w i t h s h a l l o w m a r i n e a s s o c i a t i o n sa n d r e w o r k e d
elements suggeststhe existenceof zone influenced by
fluvial discharge.
CONCLUSIONS
The multidisciplinary study (lithological and
palaeontological anilyses and radiocarbon dating) of
15 boreholes allowed to refine the Quate rnary
stratigraphy
- t h i s of the Livorno surroundings and suggested
area underwent a more complicated
that
stratigraphical history than previously known (Text-
fig. 5).
Particul arly, in the southernmost boreholes
pertainine to the Livorno Terrace domain we have
b..tr able to confirm the presence below the
"panchina"
layer (Unit 3) of a relatively
Eutyrrhenian
thick marine successionbelongitg to the SanternianEmilian cycle (Subunit 1A). This successionhas been
relativelf well documented in the past literature and,
as previously mentioned, it has been correlated to the
Santernian-Emilian Sandsand Clays with
transgressrve
Arctiia islandict or considered as transitional berween
these and the regressiveEmilian Nugola Vecchia Sands
(Barsotti et al., 1974; Giannelli et al., 1982). The
transition between these formations is still not well
r53
constrained. Stratigraphical inferenceson the Nugola
Vecchia Sands formation, which outcrops about 18
km ENE of Livorno, derive only from a likely
"Montescudaio
Lime stones"
correlation with the
formation, known from the Rosignano basin (about
20 km S of Livorno). The latter formation has been
referred to the Emilian by Galiberti et al. (1982) and
Bartoletti et al. (1986). On the whole, marine sediments of the Santernian-Emilian cycle investigatedin
the present study can be reasonably referred to the
Emilian.
In addition, the Lower Pleistocenesuccessionof
the Livorno subsurface appears to include two
sedimentary units so far unrecognizedin the area.
Specifiially, w€ identified-brackish sediments
(Subunit I B) most likely referable to the regressive
phase of the Santernian-Emilian cycle "ttd thus
correlatable to the Nueola Vecchia Sands formation.
As previously discuss.J rrr"tigraphical considerations
on this brackish successionderives mostly on its
geometric position and in none of the investigated
boreholes we have been able to document a direct
between Subunit 1A and Subunit 1B.
transition
'W'e
have been able to well document a second
marine Lower Pleistocenecycle (Unit 2), which can
be assignedto the Sicilian on the basisof both ostracod
faunas-(common occurrencesof Aurila Puncticruciata)
and calcareous nannofossils ("small GephyrocaPsa
Zone"). In most of the examined boreholes(boreholes
G, H, I, L), marine Sicilian sediments rest on the
regressivephase of the Santernian-Emilian cycle
(Subunit 1B) and only in a single borehole (N) they
overlie marine sediments of Subunit 1A. In coastal
Tuscany, marine Sicilian sediments were previously
known only from the Rosignano area; they are
representedby the Fabbriche Sands formation (about
on the Emilian
30 m thick), which reststransgressively
"Montescudaio
Limestones" formation (Bartoletti et
al., I 986).
Finally, in a single borehole drilled in proximiry of
"Gronda
dei Lupi" erosional scarp (borehole G),
the
we recorded nearshoreto transitional sediments (Unit
4) comprised berween coarse sediments tentatively
referred-to the Sicilian cycle and Holocene sediments
with Posidonia oceanica remains. On the whole,
achieved data seem to suggest that these sediments,
which undoubtedly need further investigations,would
represent ^ cycle of probable Upper Pleistoceneage
"panchina'
(younger
layer).
than the
'r
"panchina"
layer
Su6unit 5A, t..o'n.red above the
in boreholes drilled on land in the Livorno Terrace,
"Rio
Maggiore
may be tentatively correlated to the
Conglomerates" (Lazzarotto et al., 1990). Subunit 58
"Arde
nza Sands"
i s w el l c o r r e l a t a b l e w i t h t h e
(Lazzarotto et al., 1990). These authors suggestedthat
this formation is partly related to aeolian deposition,
but today exposedoutcrops do not show clear evidences
of this. Overall, Unit 5 can be assignedto a generic
Upper Pleistocene.This attribution is corroborated by
B. DALL:ANTONIA,A, CIAMPALINI,L. MICHELUCCI, G. ZANCHETTA,
154
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r-r
STRATIGRAPHYOF THE LIVORNOARE/I
NEW INSIGHTS ON THE QUATERNARY
frequent discoveriesof Middle Palaeolithic Flintstones
in Subunit 58 (Ciampalini, 2002).
In the northernmost boreholes belongitg to the
alluvial Pisa Plain dominated by the Arno River
influence, the present study allowed to confirm the
presenceof brackish-continental sediments with lower
Ievels of probable Upper Pleistoceneage (Unit 6).
These sediments are truncated by sands (Subunit 7A),
which can be ascribed to the Versilian transgression
(radiometric age of their top is 4530x60 yr BP) followed by historical coastal deposits (Subunit 7B).
It is worth mentioning that the stratigraphyof Pisa
Plain here discussed shares some interesting features
with the subsurface deposits of the Versilian Plain.
Particularly, a recent revision of old boreholes of the
Versilia Plain (Federici, 1993) and the study of a new
drilling (Antonioli et al., 2000) indicate the presence
of a thick continental successionbelow the marinesands of the Versilian transgression.This continental
successioncan be correlatedwith our Unit 6.
Further future refinement of the stratigraphy of
the Pisa Plain will permit a better reconstruction of
the subsiding history of the various sectorsof this plain
and its relationshipswith the nearby Versilia Plain.
ACKNO\TIEDGEMENTS
grant (F.P.
supportedby MURST ex-60o/o
Research
"lsole"
andby PIC INTERREGIII A Italia-Francia
Bonadonna)
Sardegna-Corsica-Toscana (A. Bossio). The authors gratefully
acknowledge Prof. Renzo Mazzanti for his fruitful suggestions and
comments on an early version of the manuscript and Dr. Agata
Di Stefano for calcareous nannofossils andyses.
rnxoNoMrc
TAXA
AND srRAtc#:)::r,
oN 'ELECTEDosrRACoD
Aurila arborescens(Brady) = Cythere arborescensBrady, 1865
Synonymy and discussion in Athersuch et al. (1985)
Distribution: Pleistocene(Santernian)-Recentfde Ruggieri ( 1980)
las Aurih woodutardii (Brady, 1868)l
Aurila bulhpunctata extumefacta Ulicznf, 1969
Distribution of Aurila bulhpunctatas.l.: Pliocene-Lower Pleistocene
(Sicilian) ftu Ruggieri (1980)
Auriln cymbaeformis (Seguenza) = Cythere cymbaeformis Seguenza,
I 883
Distribution: Pliocene-Lower Pleistocene (Sicilian) fde Ruggieri
r55
(SicilPleistocene
Neogene-Lower
Distribution (Mediterranean):
ian)fide Ruggieri( 1980)
Cehia rugosa(Costa) = CytherinarugosaCosta, 1853
enr.fdt Mostafawi, I 989
Distribut'iotl Pliocene-Pllistoc
sordida (Mi.iller) = CytherellasordidnMi.iller, 1894
Cytherelloidea
(Emilian)-Recent
Distribution: Pleistocene
"frdt Ruggieri(1980)
Flexustriebeli (Ruggieri) = Eucytherettatiebeli Ruggieri, 1962
Synonymyand discussionin Ruggieri(1992)
Distribution: Pliocene-LowerPleistocene
f.de Ruggieri(1992)
elliptica Brady, 1868
Loxoconcha
Synony-y "trd discussionin Athersuch& tVhittaker (1976)
Distribution: Pleistocene-Recenr
fide Athersuch&'W'hittaker
(re76)
rubritincta Ruggieri, 1964
Loxoconcha
Distribution: Pleistoc.n.fE-ilian)-Recentfdt Ruggieri(1980)
subrugosaRuggieri, 1976b
Loxoconcha
Distribution: Pleistocene-Recenr
fde Ruggieri(1978)
Muellerina problematica (Seguenza)= Cythereconcinna?var.
problematicaSeguenza,I 884
("coldguest"?)
Distribution:LowerPleistocene
ffu Ruggieri(1980,
r992)
Miocyprideis italiana Moos, 1962
Distiibution: Pliocenefdt Ruggieri (1980)
Neocytherideis fasciata (Brady & Robertson) = Cytherideis fasciata
Bradv 6c Robertson, 1874
Distribution: Pleistocene(Santernian)-Recentfdt Ruggieri ( 1980)
Pachycauditesattenuata Ruggieri, 1980
Distribution: Pliocene-Lower Pleistocene (Sicilian) fide Ruggieri
( I 980)
Palmoconcha turbida (Mtiller) = Loxoconclta turbida Miiller, 1894
Distribution: Pleistocene(Santernian)-Recentfdc Ruggieri ( 1980)
Procytherideis subspiralis (Brady, Crosskey 6{ Robertson) =
Cltherideis subspirafit Brady, Crosikey & Robertson, 1874
distribution: Pl.irto..tr.-R.. enr fdi Ruggieri (1978)
Ruggieria tetraptera s.l. (Seguenza) = Cythere tetraPtera Seguenza,
l 880
Distribution: Miocene-Pliocene fdt Ruggieri, I 980
A o o e N D U M . R p c o R D S S T G N I F I C A NT o E X T E N DT H E S T R A T I GRAPHICALDISTRIBUTIONOF SOMEOSTRACODSPECIES
Cytherella thrakiensri Stambolidis, 1980: recovered in borehole H
Unit 2-Sicilian; cited from the Recent (Stambolidis, 1980; Aiello
et al., 1996).
Loxoconcha minima Miller, 1894: recovered in borehole I Unit 2Sicilian; cited from the Recent (..g. Miiller, 1894; Puri et al.,
1964; Bonaduce & Pugliese, 1976; Bonaduce et al., 1976; Barra,
l99l cum bib.).
Loxoconcha parallel"a Mtiller, 1894: recovered in boreholes I, H
and N Unif 2-sicilian; cited from the Recent (Mtiller, 1894; Puri
et al., 1964; Bonaduce et al., 1976), but reported as Loxoconcha
cf . paralleh from the Sicilian of Southernmost Apulia (South Italy)
by Bossio et al. (1989).
REFERENCES
(I eSo)
Aurik fauorita Ruggieri, 1975b
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'Plio..tt.
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tocene(Ciampo, 1976)
Aurila pigadiaaa Sissingh,1972
Distribut-ion:Pliocene-LowerPleistocene(Sicilian)rtdt Ruggieri
( l e8o)
Auriln punctata(Mtinster) = Cythere
PunctataMiinster, 1830
Pleistocene(Sicilian)ffu Ruggieri
Distribution: Pliocene-Lower
( I 980)
Aurila puncticruciataRuggieri, 1975b
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DissertationThesis,Monaco, 152 pp.
(manuscript receiued October 23, 2003
accepted March 25, 2004)
Barbara DRU-'ANTONIA
Alessandro CnvPALINI
Giovanni ZnNcHETTA
Alessandro Bosslo
Francesco Paolo BoNnooNNA
Dipartimento di Scienze della Terra
Universith di Pisa
Via S. Maria, 53, 56126 Pisa, Italy
Libero MtcHnluccl
Studio di geologia L. Michelucci
P.zadella Repubblica, 59, Livorno, Italy