Italiana di Paleontologia e Stratigrafia volume

Key-uords: Stratigraphy, Mammal fauna, Plio-Pleisrocene
boundary, Central Italy

Rìassunto. Lo studio della successione geologica affiorante a
M.te Riccio ha consentito di del:ineare una ricostruzione dell'evoluzione
dell'area per il Plio-Pleistocene. Lanalisi stratigrafica indica il passaggio
da un ambiente marino poco pro{ondo durante il Pliocene, a cosriero
durante il Pleistocene Inferiore (testimoniato da evidenti linee di riva) a
condizioni continentali nella parte aka del Pleistocene Inferiore.

Lanalisi di resti di mammiferi provenienti da un livello sovra-
stante depositi marini ("Macco" auct.) ha permesso di riferire I'asso-
cìazione faunistica al Villafranchiano superiore (Unità Faunistica
Tasror correlabile alì'inizio del Pleisrocene. È qu.rr, l: prima .egna-
lazione di una fauna a mammiferi del Pleistocene Inferiore nel Lazro
settentrionale.

Abstacts. The geological evolution of the area of M.te Riccio
for the Plio-Pleistocene time span has been pointed out. The M.te Ric-
cio area was probably an high during Gelasian-Santernian times. The
stratigraphical sequence shows the passage from a coastal marine envi-
ronment during Pliocene, ro a coasral environment during Earlv Pleis-

numero paglne

tocene (testifìed by evidences of shorelines) ro conrinental conditions
during the upper part of Pleistocene. The analysis of the mammal
bones coming from a level overlying a marine formation ("Macco"
auct.) allow us to ascribe the faunal association to the late Vil-
lafranchian (Tasso F.U.) referable to the beginning of the Pleistocene.
It is the first signalation of an Early Pleistocene mammal fauna in the
Northern Latium.

Geological background.

The sequence outcropping in the Monte Riccio
area is already known in the literature (Fazzini et aI.,
1972; Colalongo et al., 1,973; Conti et al., 1983). These
authors pointed out detailed studies of the Early and
Middle Pliocene parts, \ /hile the Late Pliocene-Early
Pleistocene parts were mainly studied in a closely area,
named Macchia della Turchina (Conato & Dai Pra, 1980;
Carboni Er Palagi, 1997) (Fig.1).

GEOLOGICAL EVOLUTION AND BIOCHRONOLOGICAL EVIDENCES OF THE
MONTE RICCIO SECTION (TARQUINIA, CENTRAL ITALY)

ILARIA MAZZINI, PAOLO PACCARA, CARMELO PETRONIO S. RAFFAELE SARDELLA

Receixed January 4, 200A; accepted May 9,2AAA

-L

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Studi di Roma "La Sapienza"
pet ro nì o (q;'axrma. u niro m a f . it ;

Fig. 1 - Geological skerch map (mo-
dified frorn Conato Er Dai
Pra, 1980): a) Alluvial depo-
sits (Holocene); b) Marine
deposits rich in volcanoclas-
tic material (Middle Pleisto-
cene); c) Marine deposits of
Macchia della Turchina se-
quence (Early Pleistocene);
d) Clays and marls with
Cladocora cdespitosa (Ea,rly
Pleistocene); e) Ignimbrites
of Vulsini and Tolfa intrusive
volcanics (Late Pliocene-
Middle Pleistocene); f) Bio-
detritical calcarenites and
limestones ("Macco", Mid-
dle-Late PlioceneT: g) gre) 5h
-blue clays (Early Pliocene);
i) iocation of the srte.

- Piazzale A. Moro,5 100185 Rorna. Email
Sardella: sardella@axrma.uniromal.it

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FII" Eo lliÍ]e llTìillnt Ns f__ln *i

- Dipartimento di Scienze della Terra, Universirà degli
Mazz-rni: ilcaa4rpronet.it; Paccara: p.paccara@)libero.it; Petronìo:



248

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5

a.s.1., a se ries of transgressive events of in.rrine shallow
waters ascribed generically to Middle-Late Pliocene and
Early Pleistocene for the presence of Bulimina etnea in
the upper levels.

Stratigraphic section.

The stratigrrphical study has been carried out on
different quarries located at different heights in 1ocalit,v
Monte Riccio. The stratigraphical section illustrated in
Fig. 2 is a synthesis of al1 the outcrops. In Fig. 3 the
upper quarry is illustrated. Numbers in both figures
refers to the follou.ing description, top to the bottom.

6) Grey clay characterised by a clastic level at the
base and organised in channelised bodies. Locally a
complete alteration in caolinite is evident, probably due
to hydrothermal fluids circulation, (0.5-2 m) .

5) Conglomerate in abundant s:rndy matrix. Ciasts
are marly, calcareous, of calcarenites and flint; their
dimensions reach 20-cm of diameter. An erosive surface
is evident at the bottom, (0.15-1.5 m) .

4) Coarse ocraceous sand, clast-supported u'ith
cemented levels. Conglomerate in lenses and levels. In
the upper part, sub-horizontai parallel structures are vis-
ible. Locally lenses of pebbles with crossing sets are
present. Clasts are constituted by marly limestone and
intrusive volcanic material. Fragments of marine mol-
luscs are often found. At the base it is characterised bv
clasts of intrusive volcanic hying on ln unconformity
surface, N dipping, (0.a-3 m).

3) Biodetritical coarse sands, r.vith abundant silty-
clay matrix in the upper part. Calcareous sandy concre-
tions and srnalÌ clayey lenses are often found. High fre-
quency of molluscs remains and abundant internal
rnoulds of marine molluscs in the upper part. Vithin this
level abundant vertebrate remains were found. A slight-
ly undulated surface is at the base, (3-4m) .

2) Alternance of conglomerates and sands consti-
tuted, respectivel,v, by well sorted, round caicarenites
clasts (25-30 cm of di.rmeter) rnd biodetritical, coarse
sands. In the last centimetres some clasts of micritic
limestone are present. The molluscs frequency is very
loq (1.5 m) . The passage to the underlying level is
gradual.

1) Alternance of cemented and loose caicareous
biodetritical coarse sands. They contain a rich malaco-
fauna and have a horizontal stratification, (12 m). At the
top it is characterised by intense karstic processes and
by the increasing occurrence of clasts.

Levels 2 and 3 (Fìg. z) were fonnerly referred to
the "Macco" aocÍ.. (Fazzini et a1., 1972; Carboni et a1.,
1994) . From our point of view the conglomerate facìes
of level 2 testifies the beginning of the Santernian
regression and it is a typicai beach facies, with a rocky

6

é

<d

Fig. 2 - Geological log: a) unconformit,v surface; b) molluscs
remains; c) mammal bones; d) crossing beddìng; e) intru-
sive volcanic pebbles (clark) and marl)-limestones pcbblcs;
f) "Macco" pcbblct; g1 sandr .rnd clal-cr- ìntcryaìs; h) biode-
tritical calc:rrenitic interr.als.

Fazzini et aL (tWZ) describe the Calcare di Tar-
quinia (called "Macco" in Central Italy, where it rvidely
outcrops) as an alternating sequence of biodetritical
sands and calcarenites. They assigned it to a dubitative
time interval that spans from Early Pliocene to the lower
part' of Middle Pliocene. Overlying the "Macco" they
found a level of cemented, coarse, calcareous sands
atsigned to Late Pliocene-Early Pìei:tocene. CongJom-
erates in sandy matrix ("Conglomerati di incerta
attribuzione") locally close the sequence but they are
not assigned to a precise stratigraphic interval.

Colalongo et al. (tlll) identified a srratigraphical
disconformity b,v means of the foraminifer assemblages.
The disconformity was referred to late Early Pliocene
and late Middle Pliocene time interval llacuna medio-
pliocenica).

Conti et al. (1983) described, within the "Macco",
a Pliocene,4 mpbistegina level recognised in Central Italy
rnd rhet refer ir rn rhe nnner nîrr.'f rhe Midd]e
Pliocene.

Both Conato Er Dai Pra (1980) and Carboni &
Palagí (1997,1998) indicated at an altitude of over 80 m

L Mazzini, P Paccara, C. Petronio G R Sardella

.v1 a

bs

"?o

| 
--l

r-:::clts-l



Gec,/ctgical ei.,olutictrt of the Monte Riccio section

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---a-.ì--l=-
.-4*I-'---!;2

-ì

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Fig. 3 - Stretigraphy of the M.te Riccio quarrv: numbers correspond to clescription in the text

coast (made of Macco) behind. Level 3 testifies a lagoon
environment where the detritus conlponent is abundant.
There is not a cle:rr unconformity surface between levels
2 and 1, (Fig. 3) but observations on other sections of
the quarry and on nearby outcrops allon- to say that the
M.te Riccio area s..as probably a morphological high dur-
ing Gelasian-Santernian times (Bettelli et al., 1980). In
fact, in M.te Riccio and C.le Pisciarello levels 2 and 3 are
always found while in the surroundings they lack com-
p1etel;- :ind level I is directly overlaid by level 4 or cor-
related levels. In this case, an evident erosive surface
nrarks the prssxge between the tr.o. Probably the
emplacement of the Tolfa dornes, during the upper part
of the Gelasian period (De Rita er aI., 1.997), took part in
rhe nroqressive risinq of the area and the relative seajJ't l"lj't)
lowering until the development of coastal lagoons and,
finally, of continental conditions.

In level 2, at a height of around 125 m a.s.l., the
presence of Litbophaga boreholes induces to the follow-
ing considerations: since level 4 testifies the last evi-
dence of marine deposition, this coastline should be
chronologically linked to ievels 5 and 6 or even younger.

Moreover in deposits correlated to levels 5 and 6 several
teeth of Equus ahide,7.r were found (unpublished data)
while volcanic material from the Volsini-Sabetini com-
plex is completely absent, constraining these levels to
the late Early Pleistocene. Since ievel 5 contains volcanic
intrusive pebbles coming from the Tolfa intrusion, the
lower boundary could be the emplacement and subse-
quent erosion of the Tolfa dome occurred after Late
Pliocene (De Rita et aI., 1997). The deposits related to
this coastline are found near Tarquinia, laying directly
oYer the Macco (cf. Fig. 1, d) .

Marine faunas.

Samples from levels 6 and 5 were analysed but
they u'ere completely barren.

In level ,l fragments of marine molluscs are fre-
quent. In some cases it was possible to recognise Ostrea
sp. and PecLen sp. remains.

In level 3, together with the bone bearing level,
some internal moulds of bivalves were found. In clayey



254 L Mazzini. P Paccara. C. Petronio & R. Sard,ella

ienses an oligospecific assemblage, constitute by
Cyprideis torosa (Jones) was found. The first appearance
of this ostracod species is generally referred to the
beginning of the Early Pleistocene (Bossio, pers. com.).
Foraminifer species with very different palaeoecological
characteristics form an assemblage affected by intense
reworking.

Level 2 is characterised by the presence ol Litbo-
pbaga boreholes on Macco clasts. The orientation of the
boreholes a11ows to assume that they are in life position.

Level t has the same elements (very abundant pec-
tinids and ostreid) recognised by Compagnoni (1966) in
the Macco at Palo.

The taxa represented in this leve1 are: Ostrea
(Ostrea) lamellosa Brocchi, Cblamys (Aequipecten)
opercularis Linnaeus, Chlamys (Aequipecten) seniensis
Lamarck, Chlamys (Chlamys) multistriata (Poli),
Pecten (Pecten) jacobaeus (Linnaeus), Pecten (Pecten)
bipartitus (Foresti), Pecten (Flabellipecten) flabellì-
formis (Brocchi).

The analysis of the macrofossii record in level 1
("Macco" auct.) shows some variations in the different
taxa frequency. The lower part of the deposit is charac-
terised by high equitabilitl. of pectinids, while the upper
part is marked bv the great .rbundlnce o[ rhe species
Cblamys (A.) opercularis and Chlamys (A.) seniensis.
The upper part of the biocalcarenite is characterized also
by the high frequency of fragments of Ditrupa cornerl
(Linnaeus). These data suggests r progressive lowering
of the sea leve1 and a relative increasing of the environ-
mental instability during the deposition of level 1.

Ostracods relative to the base of 1evel 1 are charac-
terised by a iov' specific diversity and low frequency (10
species assigned to 6 genera). At the rop rhe frequency
is medium-1ow but the specif-ic diversity rises (25 species
assigned to 19 genera). The palaeoecological indications
allow defining a marine infralittoral environmenr, wirh
dominant species Loxoconcha oowlata (Costa) and Auri-
la cf . Awrila (Aurila) convexd (Baird).

In levels 2 and I the forams assemblage is charac-
terised mainly by benthic species such as Ammonia spp.,
Elpbidium spp., Florilus boueanus (d'Orbigny) and rare
Lobatula lobatula (Valker & Jacob), typical of the infra-
littoral environment.

Mammal fauna.

Almost the totality of the mammal bones have
been collected from the top the calcarenites and from
the detritic clays overlying level 1 ("Macco" auct.)
(Figg. 2; 3). Unfortunately the large mammal remains
(elephants and rhinos) have been destroyed during the
qlrarry works. Some Testudo sp. remains were found too.
The followins taxa have been checked:

Fig. a - Sus s*ozzii Nla;or, fragmertary mandiblc with P/3, P/,1,
M/1, M/2: e) latcrai vicw, b) occlr.rsal vier..

Prolagus sp., Elephantidae cf. Mammuthus merid-
ionalìs (Nesti), Sus strozzi Major, Hippopotamus antiqu-
zs Desn:rarest, Leptobos cf . Leptobos etruscus (Falconer),
Procapreolus sp., Eucladoceros ctenoides (Nesti), ,4xis
n e s tiì (Maj or), S tep h an orh in u s cf . S t ep b an orh in u s etr u s c u s
(Falconer), Equus stenonis Cocchi, Vwlpes cf. Vulpes
alopecoides Ma.jor, Canis etruscrzs Falconer and Megan-
tereon cultridezs (Cuvier p artim).

Prolagus sp.

Only two fragmentary molars represent this
taxon but the scantiness of the fossil record do not
allow any further taxonomic consideration. The genus
occurred in the early Villafranchian (Arondelli) to the
late Villafranchian of Upper Valdarno (Gliozzt et a1.,
reeT).

Elephantidae cf. Mammuthus meridionalls (Nesti)
Some juvenile diaphysis of limb bones and a den-

tal lamina are referable to this family. The thickness of
the enamel of the tooth is similar ro those of the speci-
men of Mammuthus meridionalìs of the late Villafranchi-
an faunas.

Sus strozzii Major
A fragmentary mandible with P/3, P/4,M/1,M/2

(Fig. a) and a metapodial showing the typical features
of this species represent the taxon. This suid quite
commonly occurs in the middle and late Viliafranchian
faunas.



Geological epolution of the Monte Riccio section 251

a) Leptobos cl. Leptobos etntscus (,.7ìaLconer): proxirnrl and
distal ephiphysis of a metacarp:rl bo're (front.rl r-icr); b)
Axis nestii (lvlajor): mctatarsal bone (frontal vier').

H ipp op otamus antiquu s Desmarest
A partially crushed fragment of the sku1l u'ith the

temporal and the upper part of the occipital bones, rvith
the linea nucalis testify the occurrence of the hippo. The
short sagittal crest forms a wide acute angle with the
frontal plan. This morphology and the large size .rre
characteristic features of this species, which widespread
in Italy from Africa in the Early Pleistocene (late Vil-
lafranchian, Tasso F.U., Petronio, 1986) . It seems to sur-
vive in Europe until the beginning of the Late Pleis-
tocene (Mazza, 1991; Petronio, 1995).

Leptobos cf. Leptobos etruscus (Falconer)

The occurrence of a slender bovid is testified by
two frontal bones with the basis of the horn core, some
jugal teeth, the proximal and the distal ephiphysis of a
meracarpal (Fig. 5a) . The size and the morphological
features of the metacarpal bone of the specimen from
Monte Riccio shon' great similarities with the fossil
record of Leptobos etruscus from Olivola and Upper
Vaidarno studied by Masini (1989), while the late Vil-
lafranchian Leptobos vallisarni and Bison (Eobison)
depiulii show more b'isontine features.

Leptobos etruscus characterised the late Vil-
lafranchian (Olivo1a-Farneta F.U.) (Gliozzi et al., 1997).

Procapreolus sp.
The occurrence of the roe deer in the Early Pleis-

tocene deposits of Italy is not well defined. This cervid
is repre sented bv a fragn-rent of the frontal bone with the
basal part of the antler. The roedeer is a very rare ele-
ment in the villafranchian faunas. It occurs in the Cava
Toppetti deposit referred to the end of Pliocene, Costa
S. Giacomo F.U. (Abbazzi et aI., 1992), r'hile there are
no sLlre data about the late Villafranchian faunas.

Eucladoceros ctenoides (Nesti)
The occurrence of this large cervid is testified by

the basal part of an antler (Fig. 6b), some molar teeth, a

a) Stephanorhinus cf. Stephanorbinus etuscus (Falconer):
distal part of a humerus (posterior view); b) Eucladoceros
ctenoides (Nesti): basal part of an antler (lateral vicw)

Fio A



252

distal end of a tibia and a calcaneum of a juvenile speci-
men. In particular, the size and the peculiar morphology
of the antler allow taxonomic considerations. The rose is
rounded in shape, with a diameter of Z0 mm; rhe outer
tine is strong and starts directly from the rose. It forms
with the beam a moderately obtuse angle. A very peculiar
inner tine is placed between the bean-r and the ourer tine,
very simiiar to the other specimens of Eucladoceros
ctenoides (Azzaroli &'Mazza, 1992). This species, associ-
ated with Eucladoceros dicranios, is a quite common ele-
ment of Lhe Upper Vlldarno depositr and chrracterises
the Oiivola and Tasso F.U. (Gliozzi et aL, 1997).

Axis n'estìi (Major)
Several metapodials (Fig. 5b), some fragmentary

lirnb bones, a great number of jugal teeth rnd the basal
part of an antler testify thc occurrence of this cervid.
The slenderness of the limb bones, the index of the
metapodials, the morphology of the antler and the teeth
allow to refer these fossil to Axis nestii, which, from a
biochronological point of vieq characterises the earliest
late Villafranchian faunas (Olivola and Tasso F.U.) (Di
Stefano & Petronio, 1998).

Stepbanorbinus cf. Stephanorhinus etruscus (Falconer)
A fragmentary humerus (Fig. 6a), radius and tibia

testify the occurrence of a rhino. The morphological fea-
tures (i.e. the slenderness of the diaphyses) and the size
are close to those of the specimens collected from the
Upper V.rldarno and Vrl di Chiena deposits iM.rzza.

L Mazzini, P Paccara, C. Petronio & R. SardelLa

Fig. / Fquu, stclottit Corclrr:
nr.rndìblc.r7 l.rtcr.rl ries: br
occlusal r.ier'.

1988) and the specimen from
Capitonc (TR), Tiber River
Basin (Arnbrosetti, 1972).

Equus stenonis Cocchi
Tl-ris taxon is represented

by an almost completc mandible
tFro 7l , {.".-".r16'-.^.^,'1.
\,,b. ,.i. "td') 

\rltPurJ

and a metapodial. All tl-re teeth,
. ir h rL" """".t i^. ^{ the lclt
I, 2 (lo't by rhe living animal r.
The mandible size f;rlls in the
dimensional field of the speci-
mens from Upper Valdarno. In
n:rricrrlrr. ir is ven rilril,rr in
shape to the holotype from Ter-
ranova (Azzaroli, 1965), and
shows the classical stenonoid
fc;ture': x strong.rnd high hori-
zont.rl branch. rhe ,hape oI the

lower and of the upper profile and e wide, short, r'ery
curved rostrum. All the teeth, including the very strong
canines, are worn and very similar in morphology and in
size to those of the stenonoid horses from Upper Va1-
darno. The chronological range of Eqwus stenonis in Italy
goes from Costa S. Giacomo to Tasso F.U. (Caloi, 1994;
Gliozzi et aI., 1997).

Vulpes cf. Vulpes alopecoides Major
Part of the horizontal branch of a mandible with

the M/2 and M/3 represents this small canid. Both size
and morphology agree with those of the alopecoid fox,
occurring in Italy during middle and late Villafranchian
(Di Stefano et aI., 1994).

Canis etruscus Falconer
A partial Pl1, a fragmentary mandible with M/1

andM/2, and a complete left hand in anatomical connec-
tion (Fig. 8) can be referred to this wolf-1ike dog. The
lower carnassial is moderately worn, but the morphology
of the talonid is very similar to those of the wolves s.l.
The size of the teeth and of the metacarpals of this dog
fall in the àverase of the data of Canis etrwscus from
Olivola and different localities of Upper Valdarno (Torre,
t967),whi\e the coeval Canis arnensls is more reduced in
rize and shows more s]ender metrcarprls.

Azzarolt (1977) considered the first occurrence of
Canìs etruscus in Italy was as onc the biological events,
which characterised the faunal renewal of the late Vil-
lafranchian (the wolf event) . In recent times, Rook &
Torre (1996) referred to Canis c[r. etruscus some fossils

a

.i':*r@&



€* k,.

Scm ': , . ,',,:1.,

Fig. S - (:dnìs etrus(ts Fllconer: left hencl in f,niìtonìjcrl connection.

frorn the middle Villafranchian faunrr of Costa S. Giaco-
mo, l.t.hile ;1 yerv sirrilar canid occurs in the almost
coevai deposit of Senéze (France).

The biochronological distribr-rtion of Canìs etru-
icur ranges frorr Costa S. Giacomo to Farneta F.U.
(Glioz.zr et aI., 1997) .

GeologtcaL e'ao/ution oJ the l'lctnte Riccio section 253

lI egantereon cultriden s (.Clrer partint)
A second right metatarsal can be referred to this

srnilodontine cat. The limb bones of the middle sized
villafranchian felid:rre quitc rare and incompletely
known because the scantiness of the fossil record. The
size and the morphological features arc very sirr-rilar to
that of the specimcn' from Senézc (France), until nour
the mort corrplet,'brrir of cotrp.trirott for thc qenu.
Megantereon (S;irdella, 1998). According to the available
data, Panthera gombaszoegensis shoq,- stronger end
srouter met.rpodi.rls. In Italv Megantereon ex gr. cultri-
dens biochronolosical ranse is Cost:.r S. Giacomo- Pirro
F.U. (Sardella, 1998).

Biochronology.

The n.ran.rmal fauna of Montc Riccio is rn rssoci-
ation referable to the beeinning of late Villafranchian,
Tasso F.U. (fig. 9) (Gliozzi et il..,1997).

Besicles texa as elephlrrt, rhino rnd some carnl-
vore s, in the faunai association of Monte Riccio .pecies
of great biochronoloeical siqniiicrnce occur such as lep-
tobos etruscus, EtLcladoceros ctenoic/es and Axìs nestiì.
Tlre' c trrr, to gethcr r. ith H ip p op otdùt u s an t iqu u s, which
ri-idespread in Europe during thc late Vill:rfranchian,
clearlv suggest a biochronological collocation in a tin.re
snrn verv clost: to the Plio-Pleistocene boundan'.

In Italt, the occurrcnce of the gentts Procapreolus
h;rs been rccorded only in the carly Mllafranchi;rn fauna
of Montopoli (.Procapreolus cusartus, Montopoli F.U.,
Azz.arolí,!992) and in the middle Villafranch:ian fauna of
C;rva Toppctti (C. S. Giacomo F.U., Abbezzi et al.,
|ee7).

The presen ce ol Procapreolus ín this section
;.rllon's to wide the range of this cervid to the late Vil-
lafranchian.

Fig.9 -Bìochronological fremen.ork
of the niddlc encl late Vil-
lairanchia,r manmal faunas.

\ Biochronological
\ Units\ \\

Faunal List \

MIDDLE
ViLLAFRANCHIAN

LATE
VILLAFRANCHIAN

S. Giacomo F.U.
Olivola

r.u.
Tassq

F.U. I
Farnela

F.U.

Pirro

Prolagus sp.
cI. Mam muthus me ridionalì s
Sus strozzii
Hippopotamus antiquus
Leptabos cf. L- elruscus
Procapreolus sp.
E u c lad oc e ros cte no ide s
Axis nestii
oLúPr ta! tvt ilu tuè ur. o- sr, I
Fó, Jilc ctannnic

Vulpes cf. V. alopecoides
Canls efruscus
M e g ante rean c u ltr i d e n s



254 I. Mazzini, P. Paccara, C

Conclusions.

The peculiar geological evolution of the M.te Ric-
cio - C.le Pisciarello area has allowed the preservation of
levels formerly ascribed to Pliocene marine deposits
("Macco" auct.), here distinguished as overlying the
marine succession. The occurrence in these levels of a
mammal fauna referable to the beginning of the Early
Pleistocene have a great imporrance from both a strati-
graphical and a biochronological point of view. This
mammal fauna is referable, as pointed out above, to the
Tasso F.U., and is the first signalation of an Early Pleis-
tocene mammal fauna in the Northern Latium. It con-
firms the only datum available for the Early Pleistocene
of the area, published by Conato & Dai Pra (1980). In
that work the occurren ce of Bwlimina etnea in the Mac-
chia deila Turchina series suggested an Early Pleistocene
age. Finaily, also the occurrence of the ostracod
Cyprideis torosA, confirms an attribution of the mammal
fauna to the beginning of late Villafranchian.

Petronio & R. Sardella

The Monte Riccio section represents a succession
developing from marine to continental environments.
The occurrence of a mammal fauna within marine sedi-
ments (referred to shallow waters) allows the correla-
tion, not often possibie, between marine and continen-
tal deposits at the Plio-Pleistocene boundary.

Alenowledgments.

Part of this study was carried our during the field work for the
geological map n. 354 Tarquinia, CARG Project, ITALECO and
National Geological Survey.

Special thanks to father Antonio Pascucci for signalling the
presence of vertebrate fauna in the site, to Maurizio Gaetani, Danilo
Torre and Adam Nadachowski for the critical revision of the manu-
script and the useful suggestions. \X/e are grateful to Elsa Gliozzi for
constructive discussions and malacofauna determinations, to Costan-
za Faranda for the ostracod determinarions and to Isabella Palagi {or
the foraminifer dererminaritlns.

Photos by Enrico luliano, Paolo Paccara, Luciano Spinozzi and
Giorgio D'Arpino.

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