INTRODUCTION

Ancient fluvial deposits forming aggradational riverterraces can be used as markers of uplift (Maddy, 1997;Van den Berg & Van Hoof, 2001; Westaway, 2001), inparticular if sedimentation took place close to palaeo-coasts (Burbank & Anderson, 2001). In many casesthese deposits are interbedded with shallow marine andtransitional sediments or with volcanites, in generalchronologically well constrained by biostratigraphy orradiometric age data. Moreover, fluvial deposits com-monly bear vertebrate fossil remains (Bridge, 2003),which may constitute local assemblages of biochrono-logic relevance and may be used as correlation tool withmarine isotope stages (Bridgland & Schreve, 2001).

These three conditions, presence of river terraces,interlayering of fluvial deposits with marine ones andvolcanites, and occurrence of faunal assemblages inriver sediments are present in many Italian Neogene-Quaternary sedimentary basins and in particular in theRoman Basin, along the eastern Tyrrhenian Sea coast(Latium Region) (Fig. 1). Here, in fact, the basin fill ispartly composed of terraced fluvial deposits interbeddedwith coastal marine, volcanic and volcano-sedimentarysuccessions (Conato et al., 1980; Milli, 1997; Karner &Marra, 1998). Moreover, elevation data from top sur-

faces of the terraces are widely used to estimate the rateof uplift along the Latium coast (Karner et al., 2001a;Giordano et al., 2003; De Rita et al., 2002). Finally, sev-eral vertebrate-bearing fossiliferous sites have been dis-covered within the fluvial-deltaic and coastal sedimentsof the Roman Basin (Milli et al., 2004; Milli & Palombo,2005).

It is here presented a new site of palaeontologic andbiochronologic interest, the Cerveteri-Monte Li Pozzisite (CMLP site hereafter), where terraced fluvialdeposits crop out, more than 3 km inland from the pres-ent-day coastline and some 5 km NW from Cerveteri(Fig. 1). Paleontologic, sedimentologic and elevationdata of fluvial sediments are used to provide informationon chronostratigraphy and paleoenvironmental aspectsof the site and on local uplift.

METHODS

The CMPL palaeontologic site corresponds to an exca-vation conducted by the “Soprintendenza Archeologicaper l’Etruria meridionale” in collaboration with theUniversità degli Studi di Roma “La Sapienza” and CNR-Istituto di Geologia Ambientale e Geoingegneria. The

MIDDLE PLEISTOCENE VERTEBRATE-BEARING FLUVIAL DEPOSITS OF THECERITI MTS AREA, LATIUM COAST (CENTRAL ITALY)

Marco Mancini1, Maria Rita Palombo2,1, Carmelo Petronio2,1, Raffaele Sardella2,1,Claudia Bedetti3, Luca Bellucci4, Emanuele Di Canzio3, Caterina Giovinazzo5,

Mauro Petrucci6 and Flavia Trucco7

1 CNR Istituto di Geologia Ambientale e Geoingegneria, Via Bolognola 7, 00138 Rome, Italye-mail: marco.mancini@igag.cnr.it

2 Dipartimento di Scienze della Terra, Università degli Studi di Roma “La Sapienza”, P.le A. Moro 5, 00185 Rome3 Collaboratore scientifico esterno c/o Dipartimento di Scienze della Terra, Università di Roma “La Sapienza”

4 Dottorato di Ricerca in Paleontologia, consorzio tra Università di Modena e Reggio Emilia, di Bologna e di Roma “La Sapienza”5 Dottorato di Ricerca in Scienze della Terra, Università degli Studi di Roma “La Sapienza”

6 Dottorato di Ricerca in Scienze della Terra, Università degli Studi di Torino7 Soprintendenza Archeologica per l’Etruria meridionale

Geologica Romana 39 (2006), 27-38

ABSTRACT - It is here presented a Middle Pleistocene fossiliferous site, the Cerveteri Monte Li Pozzi(CMLP) site, located in the Ceriti Mts area, within the wider Roman Basin (Latium coast, central Italy). Theoutcropping succession is, from base to top, composed of terrigenous and carbonate fluvial deposits, travertinesand ~ 410 ka old pyroclastites. The fluvial deposits form an aggradational river terrace, belong to an ancientrisen alluvial-coastal plain and sedimented close to the palaeocoast. Two fossiliferous levels have been discov-ered inside: the lower level, where Elephas (Palaeoloxodon) antiquus and Axis sp. ? A. eurygonos were found;the upper level with E. antiquus, Stephanorhinus cf. S. hundsheimensis, Dama cf. D. clactoniana, Arvicola mos-bachensis, Testudo sp.. The faunal assemblage as a whole indicates the middle-late Galerian Mammal Age,approximately 600-500 ka, and may be correlated with the MIS 15 or MIS 13. This fossil assemblage is the firstdiscovery of Galerian fauna in the Ceriti Mts area and thus represents a new Local Fauna.

On the basis of lithostratigraphic, biochronologic and elevation data, it is possible to estimate an approximate-ly 0.26 mm/a uplift rate in the Ceriti Mts basin.

KEY WORDS: Middle Pleistocene, Italy, fluvial deposits, mammal fossil assemblage, uplift.

excavation is located on the eastern flank of Monte LiPozzi, a N-S oriented hill with planar top surface at 136m a.s.l., at the interfluve between Fosso Sassetara to theeast and Fosso Perazzetta to the west. The excavation isrectangular in plan view and presents two floors, at 118and 121 m, separated by a major step. Each floor corre-sponds to a fossiliferous level. The main front of the exca-vation is 7 m in length and is oriented N20°E, with minor

fronts perpendicular to it. This good exposure enablesphysical stratigraphic analysis and 3D facies reconstruc-tion to be made (Fig. 2), as well as collection of fossilremains and preliminary taphonomic observations.

Facies analysis has been conducted following the stan-dard methods of field geology (Miall, 1996; 2000). Inparticular for terrigenous fluvial deposits it has been fol-lowed in part the Architectural Element Analysis ofMiall (1996), while environmental models of calcareoustufa from Pedley (1990) have been considered for faciesanalysis on travertines.

GEOLOGICAL FRAMEWORK

The Roman Basin and the northern-central Latiumcoastal belt

The Roman Basin widens for more than 70 km in theNW-SE direction along the coastal region of Latium andis of tectono-sedimentary origin. It was formed after theSW-NE directed extension that affected the western mar-gin of the northern-central Apennines since LateMiocene, in concomitance with the opening of thebackarc Thyrrenian Sea Basin (Funiciello & Parotto,1978; Malinverno & Ryan, 1986; Patacca et al., 1990;Cavinato & De Celles, 1999). The Roman Basin is sub-divided into horsts and minor grabens or half-grabens,

MANCINI et al.28 Geologica Romana 39 (2006), 27-38

Fig. 2 - Cerveteri Monte Li Pozzi site: view of the excavation. A-E arethe facies described in the text and featured in fig.4. Bar scale is 2 min height.

Fig. 1 - Simplified geological map of the Roman Basin, with location of selected fossiliferous sites. Legend: 1) subaeral volcanic and volcano-sed-imentary successions (Late Pliocene-Late Pleistocene); 2) marine and non-marine sedimentary successions (Late Miocene-Holocene); 3) marine, car-bonate and siliciclastic successions (Trias-Middle Miocene); 4) normal fault; 5) buried normal fault.

12¡ 16¡

Tolfa Mts

CeritiMts

Rome

Italy

15

1617

38¡

42¡

Rome

APENNINES

AlbanHillsTiber River

ROMANBASINTyrrhenian Sea

CeritiMts

LATIUM

LakeBracciano

1

Fig. 3a2

3

4

5

6 7

8

910 11

12 13

14

1) Cerveteri-Monte Li Pozzi

9 ) Monte Mario

8) Vitinia

7) San Cosimato

6) Ponte Galeria5) Malagrotta

4) Polledrara

3) Castel di Guido2) Torre in Pietra

14) Capena

13) Redicicoli

12) Cava Nera Molinario

11) Saccopastore

10) Sedia del Diavolo

Cerveteri

15) Fontana Ranuccio16) Isernia-La Pineta

17) Notarchirico

SabatiniMtsN

10 km

1

2

3

4

5

Selected fossiliferous sites:

Tolfa Mts

mainly bounded by NNW-SSE and NE-SW trendingnormal faults.

The fill of the Roman Basin (Funiciello & Parotto,1978; Barberi et al., 1994; Funiciello, 1995; Marra et al.,1995), only considering sedimentary successions, iscomposed of: 1) at the base, Lower Pliocene to LowerPleistocene sequences, of shelf marine and coastal envi-ronments and up to 1 km in thickness. They cover withangular unconformity syn-orogenic, Meso-Cenozoicsuccessions and recorded phases of tectonic subsidence,interrupted by short-term phases of localised uplift. 2)Middle Pleistocene to Holocene fluvial, coastal and shal-low marine sediments, which were deposited under atectonic regime of regional uplift.

Furthermore, in northern and central Latium a wide-spread, subaeral volcanism developed at different timeintervals: Late Pliocene, late Early Pleistocene andMiddle-Late Pleistocene (Locardi et al., 1977; Barberi etal., 1994; Cavinato et al., 1994; Funiciello, 1995; Marraet al., 1998; Karner et al., 2001b). This volcanism ismainly represented by pyroclastic products, interbeddedwith the sedimentary sequences. Related magmatism, asa whole, locally enhanced the regional trend of uplift.

The regional uplift acted as long term control (> 1Ma) on sedimentation, volcanism and landscape evolu-tion in Latium since the late Early Pleistocene (see alsoMancini & Cavinato, 2005). Uplift rates decrease alongthe NE-SW direction, from the axis of the Apennines tothe coastal belt, i.e. from values in the range of 0.30-0.50 mm/y to 0.10-0.25 mm/y (D’Agostino et al., 2001,with references). This uplift was probably due to isosta-tic rebound after the ENE directed compression of theApenninic Chain or to mantle upwelling (Barberi et al.,1994; Cavinato & De Celles, 1999; D’Agostino et al.,2001).

Sedimentation and morphological evolution of thenorthern-central coastal belt of Latium also results fromthe concomitance of glacio-eustatic and climatic con-trols with regional uplift, during the Middle Pleistocene-Holocene (Dai Prà, 1978; Conato et al., 1980; Milli,1997; Karner & Marra, 1998; Marra et al., 1998; Karnerat al., 2001a; De Rita et al., 2002; Giordano et al., 2003;Carobene, 2004). These shorter term controls, 100 kaspaced, led to the deposition of several, IV order, raiseddepositional sequences, each bounded by a main uncon-formity. Each sequence, or in some cases several verti-cally stacked sequences, correspond to a single aggrada-tional, fluvial-coastal terrace, which record one or morephases of relative sea-level rise. Depositional top sur-faces of these aggradational terraces commonly corre-spond to terraced surfaces, mark sea level highstandsand are locally used for estimation of uplift rates(Bordoni & Valensise, 1998; Karner et al., 2001a;Giordano et al., 2003).

The Ceriti Mts basin stratigraphy

Among the minor grabens and half-grabens of theRoman Basin, the Ceriti Mts basin (De Rita et al.,

1994a,b) is of great interest for reconstructing thePliocene and Pleistocene sedimentologic, volcanic andtectonic evolution of northern Latium. This basin islocated in the north-westernmost margin of the RomanBasin and comprises the CMLP fossiliferous site (Figs.1 and 3a).

Morphologically, the Ceriti Mts area is a hilly regionwith maximum elevation of 430 m a.s.l. and is elongat-ed in the NNW-SSE direction. This area is bounded tothe west by a narrow coastal plain, no more than 2 kmwide and with inner margin at about 15 m a.s.l. The plainis laterally contiguous to the Tiber River delta plain tothe SSE. The present-day river drainage in the Ceriti Mtsarea is represented by short streams roughly flowing inthe NNE-SSW direction.

In the hilly area two main belts are recognised: 1) aneastern belt, which is characterised by an almost N-Sdirected alignement of acid lava domes, Late Pliocene inage (De Rita et al., 1994a); 2) a western belt, where threemain morphological terraces are recognised and whichborder the coastal plain. These terraces correspond todepositional surfaces, gently dip seaward and are sepa-rated by steep erosional scarps. The first, upper terracedips from 150 to 130 m a.s.l., from the inner margin tothe outer edge. The second terrace dips from 80 to 50 ma.s.l. The third, lower terrace is a subplanar surface withinner margin at about 40 m a.s.l.

Structurally, the Ceriti Mts basin is interpreted as aNE-SW trending half-graben (De Rita et al., 1994a,b),which is bounded to NW by a system of SW-NE andSSW-NNE directed and SE dipping normal faults (Fig.3a). The footwall block corresponds to the Monti dellaTolfa ridge, where Mesozoic to Paleogene marine silici-clastic and carbonate successions crop out (Accordi andCarbone, 1988; Civitelli and Corda, 1988, with refer-ences). The hanging-wall block comprises both theMesozoic and Paleogene successions and overlayingNeogene and Quaternary sedimentary sequences andvolcanic deposits (Fig. 3b).

The oldest Neogene sediments are transgressiveMessinian conglomerates, covered by Lower-MiddlePliocene pelites, sands and regressive conglomerates. Itfollows the Upper Pliocene lava of the Ceriti MtsVolcanic Complex, and a series of four Quaternary depo-sitional sequences and Middle Pleistocene volcanites.Each depositional sequence is bounded at the base by amajor erosional unconformity and at the top by a depo-sitional surface. The latter corresponds to one of theabove mentioned morphological terrace or to the presentday coastal plain, in the case of the last sequence.

The first sequence is composed, in the lower part, offluvial sands and gravels, the “Puntoni fluvial deposits”sensu De Rita et al. (1994a) (Fig. 3 a-b). These fluvialsediments are only referred to the Early Pleistocenebecause of the presence of reworked Upper Pliocene vol-canites and the absence of any resedimented MiddlePleistocene volcanites. However, the new paleontologicfindings within these sediments at the CMLP site allowa partial attribution to Middle Pleistocene to be proposed

MIDDLE PLEISTOCENE VERTEBRATE-BEARING FLUVIAL ... 29Geologica Romana 39 (2006), 27-38

(see below).The upper part of the first sequence is composed of

travertines, or cool freshwater tufa sensu Pedley (1990),which form a 5 km2 wide and SW dipping wedge. Theyare related to perched hydrothermal springs, alignedalong the NE-SW directed faults (Fig. 3a). The top sur-face of travertines gently slopes from 250 to 150 m a.s.l.in the eastern part of the outcrop, while it is in the rangeof 150-130 m in the coastal belt where it corresponds tothe first morphological terraced surface. The travertinesare overlain by a few metres-thick pyroclastic cover,

which is related to the acme of the volcanic activity ofthe Sabatini Mts District, occurred between 400 and 300ka (Barberi et al., 1994).

The second sequence is composed of Middle Pleisto-cene fluvial sediments, sands and gravels of the “FossoZambra fluvial deposits” sensu De Rita et al. (1994a),with top depositional surface corresponding to the secondmorphological terrace.

The third sequence comprises alluvial sands and grav-els, interfingered with coastal and shallow marine sandsand calcarenites. The coastal marine deposits are rich in

MANCINI et al.30 Geologica Romana 39 (2006), 27-38

0 m a.s.l.

100

200

300

400

A B

N

B

A

La Tolfa Mts

Coastalplain

Santa Severa

Sasso

137 m

487 m

495 m

TyrrhenianSea

Alluvial andcoastal deposits

(Holocene)

terraced fluvialand coastal deposits(Late Pleistocene)

terraced fluvial deposits(late Middle Pleistocene)

Puntoni Unit fluvial deposits(Early-Middle Pleistocene)

WSW ENE S NTravertines(Middle Pleistocene)

CMLPsection(Fig. 4)

Volcanic deposits(Middle Pleistocene)

1 km

CeritiMts

430 m

1

2

3

4

5

6

7

8

9

Limestone and sandstone(Mesozoic-Paleogene)

10 11 12

b

a

13

Fig. 3a - Geological map of the Ceriti Mts basin (partly modified after De Rita et al., 1994a). Legend: 1) alluvial and coastal sediments (Holocene);2) Upper Pleistocene fluvial and coastal sediments: gravels and cemented sands (panchina); 3) Fosso Zambra Unit: fluvial gravels and sands (MiddlePleistocene); 4) volcanic and volcano-sedimentary deposits of the Sabatini Volcanic Complex (Middle Pleistocene); 5) Travertines (MiddlePleistocene); 6) Puntoni Unit: fluvial sands and gravels (Early-Middle Pleistocene); 7) volcanites of the Ceriti Volcanic Complex (Late Pliocene); 8) marine gravels, sands and pelites (Late Miocene-Middle Pliocene); 9) marine sandstone and limestone (Mesozoic-Paleogene); 10) normal fault;11) CMLP fossiliferous site; 12) geological cross section; 13) hydrothermal spring. Fig. 3b - Geological cross section of the Ceriti Mts basin.

a subtropical and warm seawater mollusc assemblagewith Stombus bubonius Lmk (Dai Prà, 1978; Bordoni &Valensise, 1998), indicative of the MIS 5.5 (theThyrrenian substage). The last sequence corresponds tothe Upper Pleistocene-Holocene coastal plain deposits.

BIOCHRONOLOGICAL REMARKS

Reconstructing the Neogene-Quaternary biostratigra-phy in non-marine environments and recognizing“boundaries” between successive faunal complexes is aproblematic task. The discontinuity in the continentalsedimentary record, environmental conditions, tapho-nomic and sampling biases are responsible for the factthat the stratigraphic order of the highest and lowestoccurrences, the stratigraphic data, of remains within agiven geographic area does not necessarily reflect thetemporal order of their actual first/last appearances, thepalaeobiological events, in the time. Actually, relative orabsolute deposition dates for sediment in which the low-est and highest occurrences of fossil remains are docu-mented, respectively correspond only to the ante quemor post quem time of the actual origination and extinc-tion bioevents in a given geographic area (Palombo,2004, with references therein).

Nonetheless, the classic criteria on which biochron arebased, such as absence/presence of particular taxa, fau-nal turnovers, the evolutionary stage of taxa belonging toa well-defined phyletic lineage or typical taxa associa-tions, are the only available tools that enable us to builda chronological scheme. In some cases, the occurrencesof particularly long stratigraphic sequence permits tobetter constrain the temporal range of such biochrons.

In this regard, the detailed facies and sequence strati-graphic analyses, carried out in the last years on depositsholding Pleistocene vertebrate fossil remains of theRoman Basin, have allowed the establishment of aregional and local chronostratigraphic framework whichsets some physical and temporal limits to the occurrenceof faunal complexes, in agreement with the biochrono-logic setting proposed for the mammal faunas in theItalian peninsula (Milli & Palombo 2005, and referencestherein). Accordingly, in the Roman Basin two majorfaunal complexes have been recognised: the ‘‘Galerian’’and the ‘‘Aurelian’’ complexes (Milli & Palombo, 2005).

The Galerian complex mainly includes faunal assem-blages essentially found in barrier island-lagoon depositsand subordinately in fluvio-lacustrine and palustrinedeposits that can be ascribed to the Italian Slivia andIsernia Faunal Units (FUs hereafter) (middle GalerianMammal Age, Gliozzi et al, 1997; Palombo, 2004) astestified by stratigraphic and palaeontological data (Milli& Palombo, 2005). In the older local faunas (Slivia FU)inter alios Crocuta crocuta, Mammuthus trogontherii,Equus altidens, Stephanorhinus hundsheimensis,‘‘Praemegaceros’’ verticornis, Megaloceros savini, Axyseurygonos, Cervus elaphus acoronatus, Hemibos galeri-anus and Bison schoetensacki occur. From the younger

ones (Isernia FU) birds, amphibians and reptiles,Arvicola mosbachensis, Allocricetus bursae, ‘‘Hyaenaprisca’’, Hippopotamus ex gr. H. antiquus and Ovisammon antiqua have been reported, together with ele-phants, equids, rhinoceroses, cervids and bovids(Palombo, 2004). Younger late Galerian faunal assem-blages (Fontana Ranuccio FU, roughly correlated to 13-11 MIS) are less numerous: scanty fossil remains ofStephanorhinus sp. and Bos primigenius have beenfound in the Ponte Galeria area (Fig. 1), whereas typicaltaxa of the Fontana Ranuccio FU, such as Cervus ela-phus eostephanoceros, have been uncovered in the vol-caniclastic sediments cropping out at Cava NeraMolinario, within the urban area of Rome (Fig. 1) (DiStefano & Petronio, 1993).

The Aurelian complex includes several faunal assem-blages found in fluvial and fluvio-palustrine depositsascribed to the Torre in Pietra FU (sensu Palombo et al.,2004). This complex is characterized, among the others,by the occurrence of Ursus spelaeus, Canis lupus,Megaloceros giganteus, Cervus elaphus (advancedform) and Dama dama.

The presence at Monte Li Pozzi of two fossiliferouslevels older than 400 ka (see in the following) is of par-ticular interest since it may improve our knowledgeabout the middle-late Galerian mammalian faunas fromthe Roman Basin.

DATA FROM THE FOSSILIFEROUS SITE

Facies analysis

Seven informal sedimentary and volcanic units aredistinguished, from unit A to G (Fig. 4), each correspon-ding to a single lithofacies or to a facies assemblage.

Unit A - It comprises the lower fossiliferous level. It isup to 2.5 m thick and is composed of light brown, mas-sive sandy silts, interfingered with fine to coarse sandsand gravels. The silt contains scattered bones of mam-mals, small rizholithes and subrounded calcareous nod-ules, up to 5 cm long. It is interlayered with planar hori-zons of reddish or green clay, 10 cm in thickness andbearing bones. These horizons are interpreted as weaklydeveloped paleosols.

The sands are poorly sorted and rich in silty and clayeymatrix. They are mostly composed of quartz, muscoviteand sanidine, and less frequently of biotite, magnetite andpyroxene. Poorly preserved sets of through cross-beddedlaminae have been observed, which indicate paleocurrentdirections from NNW to SSE. The sands contain a tusk ofElephas (Palaeoloxodon) antiquus Falconer & Cautley,which is oriented in a transverse direction to the paleocur-rents. This suggests partial mobilization of the fossilremain by currents.

The gravels crop out in the southernmost sector, areclast-supported, are rich in coarse sandy matrix and forma massive lenticular bed, interpreted as a small channel-fill deposit, 1 m in lenght and 30 cm in thickness.Pebbles and cobbles, with diameters up to 7 cm, are well

MIDDLE PLEISTOCENE VERTEBRATE-BEARING FLUVIAL ... 31Geologica Romana 39 (2006), 27-38

rounded and composed of limestone, chert and sand-stone, which belong to the mesozoic-cenozoic forma-tions outcropping in the Monti della Tolfa ridge. An iso-lated, rhyolite boulder, subspheric in shape and 30 cm indiameter, was found near the tusk; it should belong to thenearest Mt Ceriti lava domes, no more than 1 km farfrom the site to NNE.

Unit A is a fluvial facies assemblage: silts and fine sandsare interpreted as floodplain or leeve deposits, respective-ly FF and LV elements, in the classification of Miall(1996). They are in part pedogenically modified, as it isindicated by root traces, concretions and paleosols.Coarser sediments are considered as channel-relatedfacies (CH element). Paleocurrent data, measured fromclast imbrications, indicate flow direction from NNW,from the Tolfa Mts ridge, in accordance with the litholog-ic provenance of clasts. The bones recovered in this unitwere probably in part transported or mobilized by flowsabove the overbank area.

Unit B - It is up to 2 m thick and lays over the unit A,from which is separated through a deeply incised ero-sional surface. Above the surface it crops out a basal lag,50 cm in thickness and composed of massive gravel andphytoclast tufa (Pedley, 1990). The gravel fills NW-SEdirected paleochannels, 2 m wide and 50 cm deep. Clastsare calcareous and arenitic and are up to 10 cm in diam-eter; their main axes are mostly isooriented along thepreferential W-E direction. The freshwater tufa forms a50 cm thick, tabular bed and consists of variously orient-

ed boulders, essentially composed of: encrusted trunks,up to 60 cm in lenght, branches and leaves. Frequent car-bonate oncoids are also found. These basal deposits areoverlain by lenses of calcareous grey sand, with roottraces and peat fragments, and by a 50 cm thick tabularbed of intraclast tufa (Pedley, 1990). This tufa is wellcemented and is partly intercalated with phytohermboundstones, cylindrical in shape, 30 cm high and form-ing a large carbonate barrage.

The basal deposits are interpreted as channel-fillfacies. Gravels, with plant fragments, correspond to theGp lithofacies sensu Miall (1996) and was presumablydeposited on a lateral accreted bar in a fairly high flowcondition. Subsequent encrustation of reworked plantsoccurred under a weaker water flow regime. The over-laying calcareous sands are interpreted as pedogenisedfloodplain deposits, covered by the barrage; this wasformed under weak, WNW-ESE directed flows, in shal-low-water channels.

Unit C - It corresponds to the second fossiliferouslevel, where a skeleton of Elephas antiquus is found(Fig. 5). This directly lays over the carbonate barrage.The separating surface between unit B and C is erosion-al, is carved into the tufa and sands and represents thebase of ribbon-like structures. These channels are 1.5 mwide, 50 cm deep and N45°W oriented, and are filledwith massive, dark grey sandy silts, rich in ferromagne-sian minerals and with scattered travertine boulders, 20cm long. The silts are laterally continuous with a thinveneer, 2 cm thick, of cross-laminated coarse sands,which incompletely covers the fossil remains.

This unit is interpreted as a single mud flow depositthat filled small intrabarrage channels and mobilized inpart the fossil bones.

Unit D - It is composed of massive, coarse carbonatesands, 1 m thick, composed of detrital fragments oftravertine and quartz. It contains root traces and frag-mentary rests of small terrestrial gasteropods. This unitis interpreted as a pedogenised floodplain deposit.

Unit E - It is composed of an aggradational to progra-dational travertine facies assemblage, totally 8 m in thick-ness. The basal surface is planar-horizontal and deposi-tional, in the north-eastern part of the excavation, wheretravertines cover in aggradation the unit D; it becomessubvertical and partly erosional to the South. Clastic tufadeposits, as well as phytoherm boundstones and frame-stones (Pedley, 1990), are recognised. In particularrecumbent macrophytes indicate general southwarddirected flows, coming from the hydrothermal springssited at 1 km from the CMPL site, to the North (Fig. 3a).

Travertines of the unit E form small morphologicalterraces, separated by 1-3 m high scarps, and are attrib-uted to the barrage or the distal perched springline faciesmodels sensu Pedley (1990) and Pedley et al. (2003),prograding on alluvial plain deposits.

Unit F - It is a 2.5 m thick, massive volcaniclasticdeposit, composed of dark brown scoriaceous ashes,with white and grey pumice. It also contains thin hori-zons of leucite crystals altered in yellow-whitish anal-

MANCINI et al.32 Geologica Romana 39 (2006), 27-38

Floodplain andfluvial channel

deposits

A

BC

D

E

Matrix supported,massivegravels

Brown tuffwith pumice

(�Tufi stratificativaricolori di

La Storta� Fm)

MiddlePleistocenetravertines

Floodplain andfluvial channel

deposits

1stfossiliferous

level

2ndfossiliferous

level

136 ma.s.l.

123 m

118 m

131 m

PuntoniFluvial

Deposits(Early-MiddlePleistocene)

MiddlePleistocene

volcanicand

volcano-sedimentary

deposits

F

G

Main unconformity

Buried terraced surface

Fig. 4 - Stratigraphic-sedimentologic log of the CMPL site. A-G arethe units, lithofacies and lithofacies assemblages, described in the text.

cime. Close to the top, root traces and terrestrial gas-teropods, such as Helix pomatia L. and other helicidae,are present. This unit may be interpreted as a pyroclasticflow deposit in part pedogenically modified at the top.The abundant presence of leucite and pumices is typical,in the Ceriti Mts area, of the Tufi stratificati varicolori diLa Storta formation (Bonadonna & Bigazzi, 1970;Bigazzi et al. 1973; De Rita et al., 1993). Recently thisunit has been dated 410 ± 1 ka (Karner et al., 2001b).

Unit G - It is composed of 1.5 m of matrix-supported,massive gravels. Clasts are up to 10 cm in diameter, in

general poorly rounded, and are composed of limestone,sandstone, chert, and of dark grey or red volcanic scoriae.The main axes of clasts are in general oriented along theN-S direction. The sandy matrix is rich in ferromagnesianminerals. This deposit is interpreted as an ancient talus.

Palaeontologic data

The fossil vertebrate remains recovered from the twofossiliferous levels in the Monte Li Pozzi stratigraphicsuccession (Fig. 4) can be regarded as the first Galerianlocal faunal assemblage discovered in the Ceriti Mtsbasin and can contribute to better determine the chronos-tratigraphic attribution of the sequence.

In the lower level (unit A), Elephas (Palaeoloxodon)antiquus and Axis sp.? A. eurygonos (Azzaroli) werefound; in the upper level (unit C) Testudo sp., Arvicolamosbachensis (Schmidtgen), E. antiquus, Stephano-rhinus cf. S. hundsheimensis (Toula), and Dama cf. D.clactoniana (Falconer) are present.

Elephas antiquus from unit A is represented by a wellpreserved, slightly compressed and rather complete tusk(maximal length about 3200 mm).

Axis remains correspond to a fragmentary antler and ametatarsal bone lacking the proximal epiphysis (Fig. 6 c-d). The morphology of the antler, slightly curved andwith no deep grooves, and the morphological featuresand dimension of the metatarsal (Transversal DistalDiameter (TDD) = 37 mm; Medial Transversal Diameter

MIDDLE PLEISTOCENE VERTEBRATE-BEARING FLUVIAL ... 33Geologica Romana 39 (2006), 27-38

Fig. 5 - Almost complete skeleton of Elephas (Palaeoloxodon) antiqu-us (Falconer & Cautley) from the second fossiliferous level. Bar is 120cm long.

Fig. 6 - Selected material of the faunal assemblage: a) antler fragment of Dama cf. D. clactoniana (Falconer); b) distal part of left humerus ofStephanorhinus cf. S. hundsheimensis (Toula), on the left posterior view, on the right anterior view; c) antler fragment of Axis sp. ? A. eurygonos(Azzaroli); d) metatarsus of Axis sp. ? A. eurygonos. Bar scale is 50 mm long.

(MTD) = 32 mm) suggest to refer these specimens toMiddle Pleistocene advanced representatives of Axiseurygonos (Di Stefano and Petronio, 2003).

In the unit C, Elephas antiquus is present with a quitecomplete, slightly unarticulated skeleton (Fig 5). A par-tial anatomical connection of the vertebrae and the zeu-gopodial elements can be recognised. Although only pre-liminary observations have been carried on, such tapho-nomical setting suggests that the elephant carcass couldbe buried in sediment under low energy depositionalconditions or submitted to mud flow. The skull, largesized, shows a typical wide and triangular fan; esoccipi-tal bones are protruding. The skull apex and the brain-case are not preserved. Two upper and two lower molarteeth (M3?) are present and in part are still hidden in thesediment. Approximate in situ measurements, such asaverage enamel thickness from the lingual side of fivelaminae and lingual laminar frequency, have been car-ried out on a left lower molar. These measurements fitwith the variability field of the Italian Middle Pleisto-cene Elephas antiquus specimens (Palombo, 1986;Palombo & Ferretti, 2005).

A fragmentary antler, with a flattened part, of a fallowdeer is referred to Dama cf. D. clactoniana since its mor-phology, size and stoutness (Fig. 6a).

The occurrence of a rhinoceros is testified by a distalpart of a large left humerus (TDD = 143 mm) (Fig. 6b).An attribution to Stephanorhinus cf. S. hundsheimensisis suggested by the relative development of the trochleaand condyli, the morphology of the distal medial side ofdiaphysis plus epiphysis and of the coronoid fossagroove, and by the dimension and proportions of thebone (Fortelius et al., 1993).

Arvicola mosbachensis from unit C is represented by a3.5 mm long, left M1 (lower first molar) (Fig. 7). TheSDQ value is approximately 125, where SDQ is theSchmeltz Dicken Quotient, i.e. enamel thickness quo-tients calculated from the thickness of the leading andtrailing edges of dentine triangle (Heinrich 1982). Sucha value, following Maul et al. (1998, 2000), is consistentwith an attribution to the early-middle Toringian smallland Mammal Age, roughly correspondent to MarineIsotope Stage 13. Nonetheless, this biochronologic indi-cation has to be considered with caution, since the con-

servative features characterising the genus Arvicola inthe Mediterranean area (Röttger, 1987). Accordingly, onthe basis of just one molar, the hypothesis of a youngerage can not be completely ruled out.

Summary on stratigraphy of CMLP

All the lithostratigraphic units outcropping at CMLPcan be referred to the middle part of Middle Pleistocene(Fig. 4) basing on the fossil content and on the upperconstraint of the Tufi stratificati varicolori di La Storta,410 ± 1 ka old (Karner et al., 2001b). Unit A is part of aterrigenous fluvial depositional system, with volcanicpebbles of the Cerite District, and is thus referred to the“Puntoni Fluvial Deposits” of De Rita et al. (1994a).Units B to D are part of a mixed carbonatic and terrige-nous fluvial system, evolving upward to a sole carbonatesystem (unit E); units B to E are referred to “MiddlePleistocene travertines”.

The erosive surface that separates the “Puntoni FluvialDeposits” from the “Middle Pleistocene travertines” isconsidered as a relevant unconformity, developed in afluvial environment (Fig. 4). On the other hand, the top-most surface of the “Middle Pleistocene travertines” atabout 130 m a.s.l. is a terraced surface, the first morpho-logical terraced surface in the Ceriti area, buried belowthe tuffs and so younger than 410 ka circa. Units F andG represent one of the westernmost, peripheral outcropsof the Sabatini Mts Volcanic District.

As far the climatic stratigraphy is concerned, severalsedimentologic and paleontologic features from unitsA-E of CMLP, such as the presence of paleosols and ofa widespread travertine sedimentation (see also Pedleyet al., 2003) and the occurrence of taxa like E. antiquus,S. hundsheimensis, Axis sp. and Testudo sp., are consis-tent with a temperate-warm and relatively humid paleo-climate. These data suggest for the sedimentary units A-E the attribution to one or more interglacial stages of themiddle part of Middle Pleistocene, such as the MarineIsotope Stages 15, 13 and 11. Moreover, the Tufi strati-ficati varicolori di La Storta were deposited in con-comitance with the MIS 11, which is considered climat-ically similar to the Present Interglacial (Loutre &Berger, 2003; Kukla, 2005, with references).

DISCUSSION

Biochronology of the CMLP fossil fauna

On the basis of thus far available data, the vertebratefossil content of CMLP site provides a fairly welldefined biochronologic indication, that are consistentwith the age constraint of the overlaying volcanicdeposits, about 410 ka old.

The fossil assemblage could in fact be referred at listto the middle Galerian Mammal Age, since the occur-rence of a primitive deer (Axis), already present in EarlyPleistocene faunal assemblages, together with Middle

MANCINI et al.34 Geologica Romana 39 (2006), 27-38

Fig. 7 - Lower first molar of Arvicola mosbachensis (Schimdtgen).

Pleistocene taxa (Elephas antiquus) (Fig. 8). Apart fromAxis, that is not recorded from faunas younger than thethe Isernia FU, the discovered species are present inlocal faunas ascribed to the Isernia FU as well as inyounger ones, such as Fontana Ranuccio and Torre inPietra FUs, respectively in the late Galerian and AurelianMammal Ages. Thus, further considerations are neededto investigate the biochronologic significance of theCMLP fossil content and the chronostratigraphy of theoutcropping succession.

Axis is only found in the CMLP lower level (CMPL 1in Fig. 8), which could imply an attribution of this level’sfauna to the Isernia FU, suggesting an age of about 700-600 ka. Indeed, the Isernia FU is mostly based on theIsernia-La Pineta and Notarchirico Local Faunas (seealso Fig. 1), from successions approximately 600 ka old(Lefèvre & Raynal, 1999; Lefèvre et al., 1999; Coltortiet al., 2005).

On the other hand, morphological-evolutionary char-acters of Arvicola mosbachensis, found in the CMLPupper level (CMPL 2 in Fig. 8), are consistent with anattribution to the Fontana Ranuccio FU (MIS 13). Forthe Fontana Ranuccio Local Fauna, an age of about 460ka has been indicated (Biddittu et al., 1979; 1984).

Hence different hypotheses on the biochronologicmeaning of the CMLP fauna can be suggested. 1) Fossilsfrom the lower level may pertain to the Isernia FU andthose from the upper level to the Fontana Ranuccio FU.

In this case, it could be inferred a quite long temporalgap, in the order of 105 years, between the deposition ofthe two fossiliferous levels. However, this hypothesiscan not completely be supported by lithostratigraphy andfacies analysis in estimating the hiatus of the erosive sur-face that separates units B-C from the underlaying unitA. It should only be reminded that this surface is consid-ered as an important unconformity within fluvialdeposits (Fig. 4), although we have no elements otherthan fossils to interpret it as a boundary between twohypothetical 4th order sequences.

Conversely, both the fossil levels may be attributed: 2)to the Isernia FU; or 3) to the Fontana Ranuccio FU. Inboth cases we have to suppose that Axis and a quiteadvanced morphotypes of Arvicola mosbachensis coex-isted at the transition from middle to late GalerianMammal Age. Accordingly, a much shorter time intervalbetween the two fossiliferous strata, in the order of 103-104 years, is inferred with respect to the first hypothesis.

Whatever the actual biochronologic meaning is, theCMLP site is the first Galerian site in the Ceriti Mts areaand well fits with a large number of Middle Pleistocenefossiliferous sites of the Roman Basin (Fig. 8). On thebasis of the only palaentological data an age rangingbetween 600 and 460 ka BP can be proposed for the sed-imentary units A-E of the CMLP site, approximately cor-respondent to the time interval between MIS 15 and MIS12. This biochronological indication is consistent with

MIDDLE PLEISTOCENE VERTEBRATE-BEARING FLUVIAL ... 35Geologica Romana 39 (2006), 27-38

Fig. 8 - Chronostratigraphic scheme of the Ceriti Mts basin and chronologic distribution of fossils from the CMLP site (partly modified after Gliozzi

et al., 1997, and Milli et al., 2004).

the lithostratigraphic constraint given by the overlayingTufi stratificati varicolori di La Storta formation, 410 ±1 ka old (Karner at al., 2001b).

However, since the vertebrate-bearing fluvial depositsand travertines were deposited during interglacials, it ismore likely that sedimentation took place within the600-500 ka time interval, corresponding to the MIS 15-MIS 13. The top surface of travertines is thus attributedto the MIS 13 and is approximately 500 ka old.

Inferences on local uplift

The CMLP site is located in a uplifted area, which ispart of the coastal belt of northern-central Latium.Chronological and elevation data from the CMLP sitecan be used to roughly estimate uplift in this local area.In fact, the top surface of travertines, i.e. the first mor-phologic terrace in the Ceriti area, lays at about 130 ma.s.l. and is about 500 ka old (MIS 13). This surface isdepositional and is related to travertines prograding onan ancient alluvial plain.

Considering the closeness of these travertines to thepresent-day coastline (Fig. 3a) and assuming for eachInterglacial a local paleogeographic setting similar to thepresent one, as it is also testified by the occurrence ofUpper Pleistocene coastal deposits (MIS 5.5) in theCerveteri area (Bordoni & Valensise, 1998), it is possi-ble to infer a closeness of travertines to the former coast-line. It is therefore presumable that the travertines weredeposited at the landward margin of the ancient coastalplain, during the MIS 13, and at few metres of elevationabove the former sea level.

The eustatic sea level at MIS 13 is estimated to be sim-ilar to the present-day sea level, at 0.0 m with incertaini-ties in the ± 10.0 m interval (Pirazzoli, 1991; Murray-Wallace, 2002; Siddal et al., in press). So, for the almost500 ka old travertines of the CMPL site, the present ele-vation datum of which is 130 m a.s.l., a 130 ± 10 m upliftmight be inferred. This inference is based on theassumption that uplift results from the present-day ele-vation datum minus the former eustatic sea level posi-tion. Within the scenario of an about 130 m high localuplift, which occurred in the last 500 ka, the calculateduplift rate is of about 0.26 ± 0.02 mm/y.

However, it should be outlined that these calculationsdo not consider the real elevation a.s.l. of the travertinesat 500 ka. This actually is an unknown value, althoughassumed to be close to the former s.l., that should be sub-

tracted from the present-day elevation datum. Therefore,the uplift and uplift rate here estimated are fairly specu-lative and affected by incertainities. Nevertheless, it isinteresting to notice that uplift rates calculated for theLate Pleistocene-Holocene time interval in theCerveteri-Santa Severa area, and based on well definedcoastal markers of the MIS 5.5, are in the range of 0.19-0.27 mm/y (Bordoni & Valensise, 1998), similar to theones here presented. The Upper Pleistocene-Holoceneuplift of the Ceriti area is considered as due to the over-position of volcanically-induced, local uplift to theregional signal of uplift.

However, it is our opinion that much more data, con-cerning in particular the Middle Pleistocene coastaldeposits and forms, are needed to better estimate timesand modes of uplift in the costal range of the Ceriti Mts.

CONCLUSION

The vertebrate-bearing, fluvial deposits andtravertines cropping out at the Cerveteri Monte Li Pozzibelong to an ancient, uplifted alluvial plain. Thesedeposits are referred to the middle part of MiddlePleistocene, approximately 600-500 ka old, and corre-spond to the MIS 15 and 13, on the basis of: 1) their fos-sil content; 2) the upper lithostratigraphic constraint,provided by the “Tufi stratificati varicolori di La Storta”,410 ± 1 ka old.

Fossils are found in two different layers, both indicat-ing the middle-late Galerian Mammal Age: 1) in thelower level Elephas (Palaeoloxodon) antiquus and Axissp.? A. eurygonos are found; 2) in the upper levelTestudo sp., Arvicola mosbachensis, E. antiquus,Stephanorhinus cf. S. hundsheimensis and Dama cf. D.clactoniana are found. Fossils from this new paleonto-logic finding represent the first Galerian faunal assem-blage in the Ceriti Mts area and a new Local Fauna with-in the wider Roman Basin.

It is here hypothesized that fluvial deposits andtravertines have been uplifted to 130 m a.s.l. in the last500 ka, with uplift rate of about 0.26 mm/y.

ACKNOWLEDGEMENTS - Authors are indebted with Profs. O.Girotti, B. Mauz and P. Pieruccini and Dr. E. Sacchi for usefulcomments and discussions and with Dr. M. Pavia for the helpin paleontological determination.

MANCINI et al.36 Geologica Romana 39 (2006), 27-38

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Accettato per la stampa: Giugno 2006

MANCINI et al.38 Geologica Romana 39 (2006), 27-38