Middle Pleistocene Vertebrate-Bearing Fluvial Deposits of the Ceriti Mts Area, Latium Coast (Central Italy)

Geologica Romana 39 (2006), 27-38

MIDDLE PLEISTOCENE VERTEBRATE-BEARING FLUVIAL DEPOSITS OF THE CERITI 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, Italy e-mail: [email protected] 2 Dipartimento di Scienze della Terra, Università degli Studi di Roma “La Sapienza”, P.le A. Moro 5, 00185 Rome 3 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 Torino 7 Soprintendenza Archeologica per l’Etruria meridionale

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). The outcropping succession is, from base to top, composed of terrigenous and carbonate fluvial deposits, travertines and ~ 410 ka old pyroclastites. The fluvial deposits form an aggradational river terrace, belong to an ancient risen alluvial-coastal plain and sedimented close to the palaeocoast. Two fossiliferous levels have been discovered 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 mosbachensis, 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 first discovery 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 approximately 0.26 mm/a uplift rate in the Ceriti Mts basin.

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

INTRODUCTION faces of the terraces are widely used to estimate the rate Ancient fluvial deposits forming aggradational river of uplift along the Latium coast (Karner et al., 2001a; terraces can be used as markers of uplift (Maddy, 1997; Giordano et al., 2003; De Rita et al., 2002). Finally, sev- Van den Berg & Van Hoof, 2001; Westaway, 2001), in eral vertebrate-bearing fossiliferous sites have been dis- particular if sedimentation took place close to palaeo- covered within the fluvial-deltaic and coastal sediments coasts (Burbank & Anderson, 2001). In many cases of the Roman Basin (Milli et al., 2004; Milli & Palombo, these deposits are interbedded with shallow marine and 2005). transitional sediments or with volcanites, in general It is here presented a new site of palaeontologic and chronologically well constrained by biostratigraphy or biochronologic interest, the Cerveteri-Monte Li Pozzi radiometric age data. Moreover, fluvial deposits com- site (CMLP site hereafter), where terraced fluvial monly bear vertebrate fossil remains (Bridge, 2003), deposits crop out, more than 3 km inland from the pres- which may constitute local assemblages of biochrono- ent-day coastline and some 5 km NW from Cerveteri logic relevance and may be used as correlation tool with (Fig. 1). Paleontologic, sedimentologic and elevation marine isotope stages (Bridgland & Schreve, 2001). data of fluvial sediments are used to provide information These three conditions, presence of river terraces, on chronostratigraphy and paleoenvironmental aspects interlayering of fluvial deposits with marine ones and of the site and on local uplift. volcanites, and occurrence of faunal assemblages in river sediments are present in many Italian Neogene- Quaternary sedimentary basins and in particular in the METHODS Roman Basin, along the eastern Tyrrhenian Sea coast (Latium Region) (Fig. 1). Here, in fact, the basin fill is The CMPL palaeontologic site corresponds to an exca- partly composed of terraced fluvial deposits interbedded vation conducted by the “Soprintendenza Archeologica with coastal marine, volcanic and volcano-sedimentary per l’Etruria meridionale” in collaboration with the successions (Conato et al., 1980; Milli, 1997; Karner & Università degli Studi di Roma “La Sapienza” and CNR- Marra, 1998). Moreover, elevation data from top sur- Istituto di Geologia Ambientale e Geoingegneria. The 28 Geologica Romana 39 (2006), 27-38 MANCINI et al.

A P E N N 14 IN Lake Sabatini Tolfa Mts Bracciano E N Tolfa Mts Mts S

Ceriti 1 Ceriti 12 13 MMtsts 4 10 teri 9 11 erve 2 5 Fig. 3a C 3 Rome 6 7

8 iver Alban I er R ta Tib ROMAN Hills ly BASIN T yr Rome rh 42¡ 15 en LATIUM 16 i an 17 S ea 38¡ 10 km 12¡ 16¡

1 Selected fossiliferous sites: 9 ) Monte Mario 1) Cerveteri-Monte Li Pozzi 10) Sedia del Diavolo 2 2) Torre in Pietra 11) Saccopastore 3) Castel di Guido 12) Cava Nera Molinario 3 4) Polledrara 13) Redicicoli 4 5) Malagrotta 14) Capena 6) Ponte Galeria 15) Fontana Ranuccio 5 7) San Cosimato 16) Isernia-La Pineta 8) Vitinia 17) Notarchirico

Fig. 1 - Simplified geological map of the Roman Basin, with location of selected fossiliferous sites. Legend: 1) subaeral volcanic and volcano-sedimentary successions (Late Pliocene-Late Pleistocene); 2) marine and non-marine sedimentary successions (Late Miocene-Holocene); 3) marine, carbonate and siliciclastic successions (Trias-Middle Miocene); 4) normal fault; 5) buried normal fault. excavation is located on the eastern flank of Monte Li fronts perpendicular to it. This good exposure enables Pozzi, a N-S oriented hill with planar top surface at 136 physical stratigraphic analysis and 3D facies reconstruc- m a.s.l., at the interfluve between Fosso Sassetara to the tion to be made (Fig. 2), as well as collection of fossil east and Fosso Perazzetta to the west. The excavation is remains and preliminary taphonomic observations. rectangular in plan view and presents two floors, at 118 Facies analysis has been conducted following the stan- and 121 m, separated by a major step. Each floor corre- dard methods of field geology (Miall, 1996; 2000). In sponds to a fossiliferous level. The main front of the exca- particular for terrigenous fluvial deposits it has been fol- vation is 7 m in length and is oriented N20°E, with minor lowed in part the Architectural Element Analysis of Miall (1996), while environmental models of calcareous tufa from Pedley (1990) have been considered for facies analysis on travertines.

GEOLOGICAL FRAMEWORK The Roman Basin and the northern-central Latium coastal belt

The Roman Basin widens for more than 70 km in the NW-SE direction along the coastal region of Latium and is of tectono-sedimentary origin. It was formed after the SW-NE directed extension that affected the western margin of the northern-central Apennines since Late Miocene, in concomitance with the opening of the backarc Thyrrenian Sea Basin (Funiciello & Parotto, 1978; Malinverno & Ryan, 1986; Patacca et al., 1990; Fig. 2 - Cerveteri Monte Li Pozzi site: view of the excavation. A-E are the facies described in the text and featured in fig.4. Bar scale is 2 m Cavinato & De Celles, 1999). The Roman Basin is sub- in height. divided into horsts and minor grabens or half-grabens, MIDDLE PLEISTOCENE VERTEBRATE-BEARING FLUVIAL ... Geologica Romana 39 (2006), 27-38 29 mainly bounded by NNW-SSE and NE-SW trending 1994a,b) is of great interest for reconstructing the normal faults. Pliocene and Pleistocene sedimentologic, volcanic and The fill of the Roman Basin (Funiciello & Parotto, tectonic evolution of northern Latium. This basin is 1978; Barberi et al., 1994; Funiciello, 1995; Marra et al., located in the north-westernmost margin of the Roman 1995), only considering sedimentary successions, is Basin and comprises the CMLP fossiliferous site (Figs. composed of: 1) at the base, Lower Pliocene to Lower 1 and 3a). Pleistocene sequences, of shelf marine and coastal envi- Morphologically, the Ceriti Mts area is a hilly region ronments and up to 1 km in thickness. They cover with with maximum elevation of 430 m a.s.l. and is elongat- angular unconformity syn-orogenic, Meso-Cenozoic ed in the NNW-SSE direction. This area is bounded to successions and recorded phases of tectonic subsidence, the west by a narrow coastal plain, no more than 2 km interrupted by short-term phases of localised uplift. 2) wide and with inner margin at about 15 m a.s.l. The plain Middle Pleistocene to Holocene fluvial, coastal and shal- is laterally contiguous to the Tiber River delta plain to low marine sediments, which were deposited under a the SSE. The present-day river drainage in the Ceriti Mts tectonic regime of regional uplift. area is represented by short streams roughly flowing in Furthermore, in northern and central Latium a wide- the NNE-SSW direction. spread, subaeral volcanism developed at different time In the hilly area two main belts are recognised: 1) an intervals: Late Pliocene, late Early Pleistocene and eastern belt, which is characterised by an almost N-S Middle-Late Pleistocene (Locardi et al., 1977; Barberi et directed alignement of acid lava domes, Late Pliocene in al., 1994; Cavinato et al., 1994; Funiciello, 1995; Marra age (De Rita et al., 1994a); 2) a western belt, where three et al., 1998; Karner et al., 2001b). This volcanism is main morphological terraces are recognised and which mainly represented by pyroclastic products, interbedded border the coastal plain. These terraces correspond to with the sedimentary sequences. Related magmatism, as depositional surfaces, gently dip seaward and are sepa- a whole, locally enhanced the regional trend of uplift. rated by steep erosional scarps. The first, upper terrace The regional uplift acted as long term control (> 1 dips from 150 to 130 m a.s.l., from the inner margin to Ma) on sedimentation, volcanism and landscape evolu- the outer edge. The second terrace dips from 80 to 50 m tion in Latium since the late Early Pleistocene (see also a.s.l. The third, lower terrace is a subplanar surface with Mancini & Cavinato, 2005). Uplift rates decrease along inner margin at about 40 m a.s.l. the NE-SW direction, from the axis of the Apennines to Structurally, the Ceriti Mts basin is interpreted as a the coastal belt, i.e. from values in the range of 0.30- NE-SW trending half-graben (De Rita et al., 1994a,b), 0.50 mm/y to 0.10-0.25 mm/y (D’Agostino et al., 2001, which is bounded to NW by a system of SW-NE and with references). This uplift was probably due to isosta- SSW-NNE directed and SE dipping normal faults (Fig. tic rebound after the ENE directed compression of the 3a). The footwall block corresponds to the Monti della Apenninic Chain or to mantle upwelling (Barberi et al., Tolfa ridge, where Mesozoic to Paleogene marine silici- 1994; Cavinato & De Celles, 1999; D’Agostino et al., clastic and carbonate successions crop out (Accordi and 2001). Carbone, 1988; Civitelli and Corda, 1988, with refer- Sedimentation and morphological evolution of the ences). The hanging-wall block comprises both the northern-central coastal belt of Latium also results from Mesozoic and Paleogene successions and overlaying the concomitance of glacio-eustatic and climatic con- Neogene and Quaternary sedimentary sequences and trols with regional uplift, during the Middle Pleistocene- volcanic deposits (Fig. 3b). Holocene (Dai Prà, 1978; Conato et al., 1980; Milli, The oldest Neogene sediments are transgressive 1997; Karner & Marra, 1998; Marra et al., 1998; Karner Messinian conglomerates, covered by Lower-Middle at al., 2001a; De Rita et al., 2002; Giordano et al., 2003; Pliocene pelites, sands and regressive conglomerates. It Carobene, 2004). These shorter term controls, 100 ka follows the Upper Pliocene lava of the Ceriti Mts spaced, led to the deposition of several, IV order, raised Volcanic Complex, and a series of four Quaternary depo- depositional sequences, each bounded by a main uncon- sitional sequences and Middle Pleistocene volcanites. formity. Each sequence, or in some cases several verti- Each depositional sequence is bounded at the base by a cally stacked sequences, correspond to a single aggrada- major erosional unconformity and at the top by a depo- tional, fluvial-coastal terrace, which record one or more sitional surface. The latter corresponds to one of the phases of relative sea-level rise. Depositional top sur- above mentioned morphological terrace or to the present faces of these aggradational terraces commonly corre- day coastal plain, in the case of the last sequence. spond to terraced surfaces, mark sea level highstands The first sequence is composed, in the lower part, of and are locally used for estimation of uplift rates fluvial sands and gravels, the “Puntoni fluvial deposits” (Bordoni & Valensise, 1998; Karner et al., 2001a; sensu De Rita et al. (1994a) (Fig. 3 a-b). These fluvial Giordano et al., 2003). sediments are only referred to the Early Pleistocene because of the presence of reworked Upper Pliocene vol- The Ceriti Mts basin stratigraphy canites and the absence of any resedimented Middle Pleistocene volcanites. However, the new paleontologic Among the minor grabens and half-grabens of the findings within these sediments at the CMLP site allow Roman Basin, the Ceriti Mts basin (De Rita et al., a partial attribution to Middle Pleistocene to be proposed 30 Geologica Romana 39 (2006), 27-38 MANCINI et al.

a La Tolfa Mts 487 m 1

2 495 m B

Sasso 430 m 3

Ceriti 4 Mts 5

137 m 6 Santa Severa 7

Tyrrhenian 8 Sea Coastal plain N 1 km A 9

10 11 12 13

WSW ENE S Volcanic deposits Travertines N b (Middle Pleistocene) (Middle Pleistocene) 400 Puntoni Unit fluvial deposits (Early-Middle Pleistocene) CMLP section 300 (Fig. 4) terraced fluvial deposits (late Middle Pleistocene) 200 terraced fluvial and coastal deposits (Late Pleistocene) 100 Alluvial and coastal deposits (Holocene) 0 m a.s.l.

Limestone and sandstone (Mesozoic-Paleogene)

A B

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 (Middle Pleistocene); 4) volcanic and volcano-sedimentary deposits of the Sabatini Volcanic Complex (Middle Pleistocene); 5) Travertines (Middle Pleistocene); 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. (see below). which is related to the acme of the volcanic activity of The upper part of the first sequence is composed of the Sabatini Mts District, occurred between 400 and 300 travertines, or cool freshwater tufa sensu Pedley (1990), ka (Barberi et al., 1994). which form a 5 km2 wide and SW dipping wedge. They The second sequence is composed of Middle Pleisto- are related to perched hydrothermal springs, aligned cene fluvial sediments, sands and gravels of the “Fosso along the NE-SW directed faults (Fig. 3a). The top sur- Zambra fluvial deposits” sensu De Rita et al. (1994a), face of travertines gently slopes from 250 to 150 m a.s.l. with top depositional surface corresponding to the second in the eastern part of the outcrop, while it is in the range morphological terrace. of 150-130 m in the coastal belt where it corresponds to The third sequence comprises alluvial sands and grav- the first morphological terraced surface. The travertines els, interfingered with coastal and shallow marine sands are overlain by a few metres-thick pyroclastic cover, and calcarenites. The coastal marine deposits are rich in MIDDLE PLEISTOCENE VERTEBRATE-BEARING FLUVIAL ... Geologica Romana 39 (2006), 27-38 31 a subtropical and warm seawater mollusc assemblage ones (Isernia FU) birds, amphibians and reptiles, with Stombus bubonius Lmk (Dai Prà, 1978; Bordoni & Arvicola mosbachensis, Allocricetus bursae, ‘‘Hyaena Valensise, 1998), indicative of the MIS 5.5 (the prisca’’, Hippopotamus ex gr. H. antiquus and Ovis Thyrrenian substage). The last sequence corresponds to ammon antiqua have been reported, together with ele- the Upper Pleistocene-Holocene coastal plain deposits. phants, equids, rhinoceroses, cervids and bovids (Palombo, 2004). Younger late Galerian faunal assemblages (Fontana Ranuccio FU, roughly correlated to 13- BIOCHRONOLOGICAL REMARKS 11 MIS) are less numerous: scanty fossil remains of Stephanorhinus sp. and Bos primigenius have been Reconstructing the Neogene-Quaternary biostratigra- found in the Ponte Galeria area (Fig. 1), whereas typical phy in non-marine environments and recognizing taxa of the Fontana Ranuccio FU, such as Cervus ela- “boundaries” between successive faunal complexes is a phus eostephanoceros, have been uncovered in the vol- problematic task. The discontinuity in the continental caniclastic sediments cropping out at Cava Nera sedimentary record, environmental conditions, tapho- Molinario, within the urban area of Rome (Fig. 1) (Di nomic and sampling biases are responsible for the fact Stefano & Petronio, 1993). that the stratigraphic order of the highest and lowest The Aurelian complex includes several faunal assem- occurrences, the stratigraphic data, of remains within a blages found in fluvial and fluvio-palustrine deposits given geographic area does not necessarily reflect the ascribed to the Torre in Pietra FU (sensu Palombo et al., temporal order of their actual first/last appearances, the 2004). This complex is characterized, among the others, palaeobiological events, in the time. Actually, relative or by the occurrence of Ursus spelaeus, Canis lupus, absolute deposition dates for sediment in which the low- Megaloceros giganteus, Cervus elaphus (advanced est and highest occurrences of fossil remains are docu- form) and Dama dama. mented, respectively correspond only to the ante quem The presence at Monte Li Pozzi of two fossiliferous or post quem time of the actual origination and extinc- levels older than 400 ka (see in the following) is of par- tion bioevents in a given geographic area (Palombo, ticular interest since it may improve our knowledge 2004, with references therein). about the middle-late Galerian mammalian faunas from Nonetheless, the classic criteria on which biochron are the Roman Basin. based, such as absence/presence of particular taxa, faunal turnovers, the evolutionary stage of taxa belonging to a well-defined phyletic lineage or typical taxa associa- DATA FROM THE FOSSILIFEROUS SITE tions, are the only available tools that enable us to build Facies analysis a chronological scheme. In some cases, the occurrences of particularly long stratigraphic sequence permits to Seven informal sedimentary and volcanic units are better constrain the temporal range of such biochrons. distinguished, from unit A to G (Fig. 4), each correspon- In this regard, the detailed facies and sequence strati- ding to a single lithofacies or to a facies assemblage. graphic analyses, carried out in the last years on deposits Unit A- It comprises the lower fossiliferous level. It is holding Pleistocene vertebrate fossil remains of the up to 2.5 m thick and is composed of light brown, mas- Roman Basin, have allowed the establishment of a sive sandy silts, interfingered with fine to coarse sands regional and local chronostratigraphic framework which and gravels. The silt contains scattered bones of mam- sets some physical and temporal limits to the occurrence mals, small rizholithes and subrounded calcareous nod- of faunal complexes, in agreement with the biochrono- ules, up to 5 cm long. It is interlayered with planar hori- logic setting proposed for the mammal faunas in the zons of reddish or green clay, 10 cm in thickness and Italian peninsula (Milli & Palombo 2005, and references bearing bones. These horizons are interpreted as weakly therein). Accordingly, in the Roman Basin two major developed paleosols. faunal complexes have been recognised: the ‘‘Galerian’’ The sands are poorly sorted and rich in silty and clayey and the ‘‘Aurelian’’ complexes (Milli & Palombo, 2005). matrix. They are mostly composed of quartz, muscovite The Galerian complex mainly includes faunal assem- and sanidine, and less frequently of biotite, magnetite and blages essentially found in barrier island-lagoon deposits pyroxene. Poorly preserved sets of through cross-bedded and subordinately in fluvio-lacustrine and palustrine laminae have been observed, which indicate paleocurrent deposits that can be ascribed to the Italian Slivia and directions from NNW to SSE. The sands contain a tusk of Isernia Faunal Units (FUs hereafter) (middle Galerian Elephas (Palaeoloxodon) antiquus Falconer & Cautley, Mammal Age, Gliozzi et al, 1997; Palombo, 2004) as which is oriented in a transverse direction to the paleocur- testified by stratigraphic and palaeontological data (Milli rents. This suggests partial mobilization of the fossil & Palombo, 2005). In the older local faunas (Slivia FU) remain by currents. inter alios Crocuta crocuta, Mammuthus trogontherii, The gravels crop out in the southernmost sector, are Equus altidens, Stephanorhinus hundsheimensis, clast-supported, are rich in coarse sandy matrix and form ‘‘Praemegaceros’’verticornis, Megaloceros savini, Axys a massive lenticular bed, interpreted as a small channel- eurygonos, Cervus elaphus acoronatus, Hemibos galeri- fill deposit, 1 m in lenght and 30 cm in thickness. anus and Bison schoetensacki occur. From the younger Pebbles and cobbles, with diameters up to 7 cm, are well 32 Geologica Romana 39 (2006), 27-38 MANCINI et al.

ed boulders, essentially composed of: encrusted trunks, 136 m a.s.l. Matrix supported, up to 60 cm in lenght, branches and leaves. Frequent car- G massive Middle bonate oncoids are also found. These basal deposits are gravels Pleistocene volcanic overlain by lenses of calcareous grey sand, with root and Brown tuff volcano- traces and peat fragments, and by a 50 cm thick tabular with pumice sedimentary bed of intraclast tufa (Pedley, 1990). This tufa is well (Tufi stratificati deposits varicolori di cemented and is partly intercalated with phytoherm F La Storta Fm) boundstones, cylindrical in shape, 30 cm high and form- 131 m ing a large carbonate barrage. Buried terraced surface The basal deposits are interpreted as channel-fill facies. Gravels, with plant fragments, correspond to the Gp lithofacies sensu Miall (1996) and was presumably deposited on a lateral accreted bar in a fairly high flow Middle Pleistocene condition. Subsequent encrustation of reworked plants travertines occurred under a weaker water flow regime. The overlaying calcareous sands are interpreted as pedogenised E floodplain deposits, covered by the barrage; this was formed under weak, WNW-ESE directed flows, in shal- 123 m Floodplain and low-water channels. 2nd D fluvial channel Unit C - It corresponds to the second fossiliferous fossiliferous deposits level C level, where a skeleton of Elephas antiquus is found B Main unconformity (Fig. 5). This directly lays over the carbonate barrage. 1st The separating surface between unit B and C is erosion- Floodplain and Puntoni fossiliferous Fluvial al, is carved into the tufa and sands and represents the level fluvial channel A deposits Deposits base of ribbon-like structures. These channels are 1.5 m (Early-Middle 118 m Pleistocene) wide, 50 cm deep and N45°W oriented, and are filled with massive, dark grey sandy silts, rich in ferromagnesian minerals and with scattered travertine boulders, 20 Fig. 4 - Stratigraphic-sedimentologic log of the CMPL site. A-G are the units, lithofacies and lithofacies assemblages, described in the text. cm long. The silts are laterally continuous with a thin veneer, 2 cm thick, of cross-laminated coarse sands, rounded and composed of limestone, chert and sand- which incompletely covers the fossil remains. stone, which belong to the mesozoic-cenozoic forma- This unit is interpreted as a single mud flow deposit tions outcropping in the Monti della Tolfa ridge. An iso- that filled small intrabarrage channels and mobilized in lated, rhyolite boulder, subspheric in shape and 30 cm in part the fossil bones. diameter, was found near the tusk; it should belong to the Unit D - It is composed of massive, coarse carbonate nearest Mt Ceriti lava domes, no more than 1 km far sands, 1 m thick, composed of detrital fragments of from the site to NNE. travertine and quartz. It contains root traces and frag- Unit A is a fluvial facies assemblage: silts and fine sands mentary rests of small terrestrial gasteropods. This unit are interpreted as floodplain or leeve deposits, respective- is interpreted as a pedogenised floodplain deposit. ly FF and LV elements, in the classification of Miall Unit E - It is composed of an aggradational to progra- (1996). They are in part pedogenically modified, as it is dational travertine facies assemblage, totally 8 m in thick- indicated by root traces, concretions and paleosols. ness. The basal surface is planar-horizontal and deposi- Coarser sediments are considered as channel-related tional, in the north-eastern part of the excavation, where facies (CH element). Paleocurrent data, measured from travertines cover in aggradation the unit D; it becomes clast imbrications, indicate flow direction from NNW, subvertical and partly erosional to the South. Clastic tufa from the Tolfa Mts ridge, in accordance with the litholog- deposits, as well as phytoherm boundstones and frame- ic provenance of clasts. The bones recovered in this unit stones (Pedley, 1990), are recognised. In particular were probably in part transported or mobilized by flows recumbent macrophytes indicate general southward above the overbank area. directed flows, coming from the hydrothermal springs Unit B - It is up to 2 m thick and lays over the unit A, sited at 1 km from the CMPL site, to the North (Fig. 3a). from which is separated through a deeply incised ero- Travertines of the unit E form small morphological sional surface. Above the surface it crops out a basal lag, terraces, separated by 1-3 m high scarps, and are attrib- 50 cm in thickness and composed of massive gravel and uted to the barrage or the distal perched springline facies phytoclast tufa (Pedley, 1990). The gravel fills NW-SE models sensu Pedley (1990) and Pedley et al. (2003), directed paleochannels, 2 m wide and 50 cm deep. Clasts prograding on alluvial plain deposits. are calcareous and arenitic and are up to 10 cm in diam- Unit F - It is a 2.5 m thick, massive volcaniclastic eter; their main axes are mostly isooriented along the deposit, composed of dark brown scoriaceous ashes, preferential W-E direction. The freshwater tufa forms a with white and grey pumice. It also contains thin hori- 50 cm thick, tabular bed and consists of variously orient- zons of leucite crystals altered in yellow-whitish anal- MIDDLE PLEISTOCENE VERTEBRATE-BEARING FLUVIAL ... Geologica Romana 39 (2006), 27-38 33

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 the N-S direction. The sandy matrix is rich in ferromagnesian minerals. This deposit is interpreted as an ancient talus.

Palaeontologic data

The fossil vertebrate remains recovered from the two fossiliferous levels in the Monte Li Pozzi stratigraphic succession (Fig. 4) can be regarded as the first Galerian local faunal assemblage discovered in the Ceriti Mts basin and can contribute to better determine the chronostratigraphic attribution of the sequence. In the lower level (unit A), Elephas (Palaeoloxodon) Fig. 5 - Almost complete skeleton of Elephas (Palaeoloxodon) antiquus (Falconer & Cautley) from the second fossiliferous level. Bar is 120 antiquus and Axis sp.? A. eurygonos (Azzaroli) were cm long. found; in the upper level (unit C) Testudo sp., Arvicola mosbachensis (Schmidtgen), E. antiquus, Stephano- cime. Close to the top, root traces and terrestrial gas- rhinus cf. S. hundsheimensis (Toula), and Dama cf. D. teropods, such as Helix pomatia L. and other helicidae, clactoniana (Falconer) are present. are present. This unit may be interpreted as a pyroclastic Elephas antiquus from unit A is represented by a well flow deposit in part pedogenically modified at the top. preserved, slightly compressed and rather complete tusk The abundant presence of leucite and pumices is typical, (maximal length about 3200 mm). in the Ceriti Mts area, of the Tufi stratificati varicolori di Axis remains correspond to a fragmentary antler and a La Storta formation (Bonadonna & Bigazzi, 1970; metatarsal bone lacking the proximal epiphysis (Fig. 6 c- Bigazzi et al. 1973; De Rita et al., 1993). Recently this d). The morphology of the antler, slightly curved and unit has been dated 410 ± 1 ka (Karner et al., 2001b). with no deep grooves, and the morphological features Unit G - It is composed of 1.5 m of matrix-supported, and dimension of the metatarsal (Transversal Distal massive gravels. Clasts are up to 10 cm in diameter, in Diameter (TDD) = 37 mm; Medial Transversal Diameter

Fig. 6 - Selected material of the faunal assemblage: a) antler fragment of Dama cf. D. clactoniana (Falconer); b) distal part of left humerus of Stephanorhinus 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. 34 Geologica Romana 39 (2006), 27-38 MANCINI et al.

(MTD) = 32 mm) suggest to refer these specimens to servative features characterising the genus Arvicola in Middle Pleistocene advanced representatives of Axis the Mediterranean area (Röttger, 1987). Accordingly, on eurygonos (Di Stefano and Petronio, 2003). the basis of just one molar, the hypothesis of a younger In the unit C, Elephas antiquus is present with a quite age can not be completely ruled out. complete, slightly unarticulated skeleton (Fig 5). A partial anatomical connection of the vertebrae and the zeu- Summary on stratigraphy of CMLP gopodial elements can be recognised. Although only preliminary observations have been carried on, such tapho- All the lithostratigraphic units outcropping at CMLP nomical setting suggests that the elephant carcass could can be referred to the middle part of Middle Pleistocene be buried in sediment under low energy depositional (Fig. 4) basing on the fossil content and on the upper conditions or submitted to mud flow. The skull, large constraint of the Tufi stratificati varicolori di La Storta, sized, shows a typical wide and triangular fan; esoccipi- 410 ± 1 ka old (Karner et al., 2001b). Unit A is part of a tal bones are protruding. The skull apex and the brain- terrigenous fluvial depositional system, with volcanic case are not preserved. Two upper and two lower molar pebbles of the Cerite District, and is thus referred to the teeth (M3?) are present and in part are still hidden in the “Puntoni Fluvial Deposits” of De Rita et al. (1994a). sediment. Approximate in situ measurements, such as Units B to D are part of a mixed carbonatic and terrige- average enamel thickness from the lingual side of five nous fluvial system, evolving upward to a sole carbonate laminae and lingual laminar frequency, have been car- system (unit E); units B to E are referred to “Middle ried out on a left lower molar. These measurements fit Pleistocene travertines”. with the variability field of the Italian Middle Pleisto- The erosive surface that separates the “Puntoni Fluvial cene Elephas antiquus specimens (Palombo, 1986; Deposits” from the “Middle Pleistocene travertines” is Palombo & Ferretti, 2005). considered as a relevant unconformity, developed in a A fragmentary antler, with a flattened part, of a fallow fluvial environment (Fig. 4). On the other hand, the top- deer is referred to Dama cf. D. clactoniana since its mor- most surface of the “Middle Pleistocene travertines” at phology, size and stoutness (Fig. 6a). about 130 m a.s.l. is a terraced surface, the first morpho- The occurrence of a rhinoceros is testified by a distal logical terraced surface in the Ceriti area, buried below part of a large left humerus (TDD = 143 mm) (Fig. 6b). the tuffs and so younger than 410 ka circa. Units F and An attribution to Stephanorhinus cf. S. hundsheimensis G represent one of the westernmost, peripheral outcrops is suggested by the relative development of the trochlea of the Sabatini Mts Volcanic District. and condyli, the morphology of the distal medial side of As far the climatic stratigraphy is concerned, several diaphysis plus epiphysis and of the coronoid fossa sedimentologic and paleontologic features from units groove, and by the dimension and proportions of the A-E of CMLP, such as the presence of paleosols and of bone (Fortelius et al., 1993). a widespread travertine sedimentation (see also Pedley Arvicola mosbachensis from unit C is represented by a et al., 2003) and the occurrence of taxa like E. antiquus, 3.5 mm long, left M1 (lower first molar) (Fig. 7). The S. hundsheimensis, Axis sp. and Testudo sp., are consis- SDQ value is approximately 125, where SDQ is the tent with a temperate-warm and relatively humid paleo- Schmeltz Dicken Quotient, i.e. enamel thickness quo- climate. These data suggest for the sedimentary units A- tients calculated from the thickness of the leading and E the attribution to one or more interglacial stages of the trailing edges of dentine triangle (Heinrich 1982). Such middle part of Middle Pleistocene, such as the Marine a value, following Maul et al. (1998, 2000), is consistent Isotope Stages 15, 13 and 11. Moreover, the Tufi strati- with an attribution to the early-middle Toringian small ficati varicolori di La Storta were deposited in con- land Mammal Age, roughly correspondent to Marine comitance with the MIS 11, which is considered climat- Isotope Stage 13. Nonetheless, this biochronologic indi- ically similar to the Present Interglacial (Loutre & cation has to be considered with caution, since the con- Berger, 2003; Kukla, 2005, with references).

DISCUSSION Biochronology of the CMLP fossil fauna

On the basis of thus far available data, the vertebrate fossil content of CMLP site provides a fairly well defined biochronologic indication, that are consistent with the age constraint of the overlaying volcanic deposits, about 410 ka old. The fossil assemblage could in fact be referred at list to the middle Galerian Mammal Age, since the occurrence of a primitive deer (Axis), already present in Early Fig. 7 - Lower first molar of Arvicola mosbachensis (Schimdtgen). Pleistocene faunal assemblages, together with Middle MIDDLE PLEISTOCENE VERTEBRATE-BEARING FLUVIAL ... Geologica Romana 39 (2006), 27-38 35

Pleistocene taxa (Elephas antiquus) (Fig. 8). Apart from In this case, it could be inferred a quite long temporal Axis, that is not recorded from faunas younger than the gap, in the order of 105 years, between the deposition of the Isernia FU, the discovered species are present in the two fossiliferous levels. However, this hypothesis local faunas ascribed to the Isernia FU as well as in can not completely be supported by lithostratigraphy and younger ones, such as Fontana Ranuccio and Torre in facies analysis in estimating the hiatus of the erosive sur- Pietra FUs, respectively in the late Galerian and Aurelian face that separates units B-C from the underlaying unit Mammal Ages. Thus, further considerations are needed A. It should only be reminded that this surface is consid- to investigate the biochronologic significance of the ered as an important unconformity within fluvial CMLP fossil content and the chronostratigraphy of the deposits (Fig. 4), although we have no elements other outcropping succession. than fossils to interpret it as a boundary between two Axis is only found in the CMLP lower level (CMPL 1 hypothetical 4th order sequences. in Fig. 8), which could imply an attribution of this level’s Conversely, both the fossil levels may be attributed: 2) fauna to the Isernia FU, suggesting an age of about 700- to the Isernia FU; or 3) to the Fontana Ranuccio FU. In 600 ka. Indeed, the Isernia FU is mostly based on the both cases we have to suppose that Axis and a quite Isernia-La Pineta and Notarchirico Local Faunas (see advanced morphotypes of Arvicola mosbachensis coex- also Fig. 1), from successions approximately 600 ka old isted at the transition from middle to late Galerian (Lefèvre & Raynal, 1999; Lefèvre et al., 1999; Coltorti Mammal Age. Accordingly, a much shorter time interval et al., 2005). between the two fossiliferous strata, in the order of 103- On the other hand, morphological-evolutionary char- 104 years, is inferred with respect to the first hypothesis. acters of Arvicola mosbachensis, found in the CMLP Whatever the actual biochronologic meaning is, the upper level (CMPL 2 in Fig. 8), are consistent with an CMLP site is the first Galerian site in the Ceriti Mts area attribution to the Fontana Ranuccio FU (MIS 13). For and well fits with a large number of Middle Pleistocene the Fontana Ranuccio Local Fauna, an age of about 460 fossiliferous sites of the Roman Basin (Fig. 8). On the ka has been indicated (Biddittu et al., 1979; 1984). basis of the only palaentological data an age ranging Hence different hypotheses on the biochronologic between 600 and 460 ka BP can be proposed for the sed- meaning of the CMLP fauna can be suggested. 1) Fossils imentary units A-E of the CMLP site, approximately cor- from the lower level may pertain to the Isernia FU and respondent to the time interval between MIS 15 and MIS those from the upper level to the Fontana Ranuccio FU. 12. This biochronological indication is consistent with

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). 36 Geologica Romana 39 (2006), 27-38 MANCINI et al. the lithostratigraphic constraint given by the overlaying tracted from the present-day elevation datum. Therefore, Tufi stratificati varicolori di La Storta formation, 410 ± the uplift and uplift rate here estimated are fairly specu- 1 ka old (Karner at al., 2001b). lative and affected by incertainities. Nevertheless, it is However, since the vertebrate-bearing fluvial deposits interesting to notice that uplift rates calculated for the and travertines were deposited during interglacials, it is Late Pleistocene-Holocene time interval in the more likely that sedimentation took place within the Cerveteri-Santa Severa area, and based on well defined 600-500 ka time interval, corresponding to the MIS 15- coastal markers of the MIS 5.5, are in the range of 0.19- MIS 13. The top surface of travertines is thus attributed 0.27 mm/y (Bordoni & Valensise, 1998), similar to the to the MIS 13 and is approximately 500 ka old. ones here presented. The Upper Pleistocene-Holocene uplift of the Ceriti area is considered as due to the over- Inferences on local uplift position of volcanically-induced, local uplift to the regional signal of uplift. The CMLP site is located in a uplifted area, which is However, it is our opinion that much more data, con- part of the coastal belt of northern-central Latium. cerning in particular the Middle Pleistocene coastal Chronological and elevation data from the CMLP site deposits and forms, are needed to better estimate times can be used to roughly estimate uplift in this local area. and modes of uplift in the costal range of the Ceriti Mts. In fact, the top surface of travertines, i.e. the first mor- phologic terrace in the Ceriti area, lays at about 130 m a.s.l. and is about 500 ka old (MIS 13). This surface is CONCLUSION depositional and is related to travertines prograding on an ancient alluvial plain. The vertebrate-bearing, fluvial deposits and Considering the closeness of these travertines to the travertines cropping out at the Cerveteri Monte Li Pozzi present-day coastline (Fig. 3a) and assuming for each belong to an ancient, uplifted alluvial plain. These Interglacial a local paleogeographic setting similar to the deposits are referred to the middle part of Middle present one, as it is also testified by the occurrence of Pleistocene, approximately 600-500 ka old, and corre- Upper Pleistocene coastal deposits (MIS 5.5) in the spond to the MIS 15 and 13, on the basis of: 1) their fos- Cerveteri area (Bordoni & Valensise, 1998), it is possi- sil content; 2) the upper lithostratigraphic constraint, ble to infer a closeness of travertines to the former coast- provided by the “Tufi stratificati varicolori di La Storta”, line. It is therefore presumable that the travertines were 410 ± 1 ka old. deposited at the landward margin of the ancient coastal Fossils are found in two different layers, both indicat- plain, during the MIS 13, and at few metres of elevation ing the middle-late Galerian Mammal Age: 1) in the above the former sea level. lower level Elephas (Palaeoloxodon) antiquus and Axis The eustatic sea level at MIS 13 is estimated to be sim- sp.? A. eurygonos are found; 2) in the upper level ilar to the present-day sea level, at 0.0 m with incertaini- Testudo sp., Arvicola mosbachensis, E. antiquus, ties in the ± 10.0 m interval (Pirazzoli, 1991; Murray- Stephanorhinus cf. S. hundsheimensis and Dama cf. D. Wallace, 2002; Siddal et al., in press). So, for the almost clactoniana are found. Fossils from this new paleonto- 500 ka old travertines of the CMPL site, the present ele- logic finding represent the first Galerian faunal assem- vation datum of which is 130 m a.s.l., a 130 ± 10 m uplift blage in the Ceriti Mts area and a new Local Fauna with- might be inferred. This inference is based on the in the wider Roman Basin. assumption that uplift results from the present-day ele- It is here hypothesized that fluvial deposits and vation datum minus the former eustatic sea level posi- travertines have been uplifted to 130 m a.s.l. in the last tion. Within the scenario of an about 130 m high local 500 ka, with uplift rate of about 0.26 mm/y. uplift, which occurred in the last 500 ka, the calculated uplift rate is of about 0.26 ± 0.02 mm/y. ACKNOWLEDGEMENTS - Authors are indebted with Profs. O. However, it should be outlined that these calculations Girotti, B. Mauz and P. Pieruccini and Dr. E. Sacchi for useful do not consider the real elevation a.s.l. of the travertines comments and discussions and with Dr. M. Pavia for the help at 500 ka. This actually is an unknown value, although in paleontological determination. assumed to be close to the former s.l., that should be sub-

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