The end of the Lago-Mare time in the SE Valdelsa Basin (Central Italy): interference between local tectonism and regional sea-level rise

Laura ABBAZZI Dipartimento di Scienze della Terra, Università di Firenze, via G. La Pira 4, I-50121 Firenze (Italy)

Marco BENVENUTI Dipartimento di Scienze della Terra, Università di Firenze, and Istituto di Geoscienze e Georisorse, C.N.R, c/o Dipartimento di Scienze della Terra, Università di Firenze, via G. La Pira 4, I-50121 Firenze (Italy)

Maria Elena CECI Dipartimento di Scienze Geologiche, Università di Roma Tre, Largo San Leonardo Murialdo 1, I-00146 Roma (Italy)

Daniela ESU Dipartimento di Scienze della Terra, Università di Roma “La Sapienza”, Piazzale Aldo Moro 5, I-00185 Roma (Italy)

Costanza FARANDA Dipartimento di Scienze Geologiche, Università di Roma Tre, Largo San Leonardo Murialdo 1, I-00146 Roma (Italy)

Lorenzo ROOK Francesca TANGOCCI Dipartimento di Scienze della Terra, Università di Firenze, via G. La Pira 4, I-50121 Firenze (Italy)

Abbazzi L., Benvenuti M., Ceci M. E., Esu D., Faranda C., Rook L. & Tangocci F. 2008. — The end of the Lago-Mare time in the SE Valdelsa Basin (Central Italy): interference between local tectonism and regional sea-level rise. Geodiversitas 30 (3) : 611-639.

ABSTRACT A multi-disciplinary study has been carried out on a Late Neogene succession exposed in the SE portion of the Valdelsa Basin (Strolla Creek, Central Italy). Th e succession consists of upper Tortonian-Messinian sediments, unconform- ably overlain by uppermost Messinian-Pliocene deposits, accumulated in al- luvial, lacustrine and marine environments. Previous studies on this succession hypothesized a sudden marine fl ooding of the upper Messinian Lago-Mare realm in the earliest Zanclean in apparent agreement with the Mio-Pliocene transition

GEODIVERSITAS • 2008 • 30 (3) © Publications Scientifi ques du Muséum national d’Histoire naturelle, Paris. www.geodiversitas.com 611 Abbazzi L. et al.

recorded elsewhere in the Mediterrranean Basin. Data from this study suggest a more complex stratigraphy recording a local depositional evolution possibly driven by interference between uplift, relief denudation and eustacy. Th e sedi- ments encompassing the Mio-Pliocene transition have been included into the Borro Strolla synthem, furtherly subdivided into three sub-synthems. Th e Borro Strolla synthem has been dated as uppermost Messinian-earliest Zanclean based on the integration of physical stratigraphy, facies analysis and biochronology of non-marine fossil assemblages in part documented for the fi rst time. Th e oc- currence in the lower Borro Strolla Synthem of the gerbil Debruijnimys sp. and the murid Stephanomys aff . S. donnezani (Depéret, 1890) with Pliocene affi nity KEY WORDS represents the most important novelty in the composition of a mammal fauna Late Messinian, otherwise similar to other Italian late Messinian sites. Th e co-occurrence of ter- early Zanclean, Lago-Mare, restrial molluscs from the same sediments gives further biochronologic constrains non-marine fossil supporting the calibration of the Borro Strolla synthem to the latest Messinian- assemblages, earliest Zanclean. Th e Borro Strolla stratigraphic section then is discussed in facies analysis, Valdelsa Basin, the framework of local to regional events which marked the transition from the Central Italy. Messinian to Pliocene.

RÉSUMÉ La fi n du Lago-Mare dans la partie SE du bassin de Valdelsa (Italie centrale) entre tectonique locale et remontée du niveau marin régional. Une étude multidisciplinaire a été réalisée sur les dépôts néogènes (alluviaux, lacustres et marins) du sud-est du bassin de Valdelsa (Italie centrale). Ces sédiments, datés du Tortonien supérieur-Messinien inférieur, sont surmontés, en discontinuité, par des sédiments du Messinien supérieur-Pliocène. Cette étude suggère que ces dépôts résultent de l’interaction de phénomènes locaux tels que la surrection et la dénu- dation des reliefs ainsi que l’eustasie plutôt que du changement drastique dû à la transgression du Zancléen inférieur sur le Lago-Mare, enregistrée en Méditerranée. Ces sédiments, déposés à la transition du Mio-Pliocène correspondent au synthème de Borro Strolla (qui comprend trois sub-synthèmes). Il a été daté Messinien supé- rieur-Zancléen inférieur grâce à l’analyses de coupes, d’études sédimentologiques (étude de faciès), et de la biochronologie établie sur les associations de faunes non-marines, montrant elles-mêmes de nouveaux éléments. La découverte, dans la partie inférieure du synthème de Borro Strolla, du gerbillidé Debruijnimys sp. MOTS CLÉS et du muridé Stephanomys aff . S. donnezani (Depéret, 1890) à affi nité pliocène est Messinien supérieur, un élément nouveau dans cette association faunistique qui correspond par ailleurs Zancléen inférieur, Lago-Mare, à celle observée en Italie dans les sites du Messinien supérieur. D’autre part, la pré- associations fossiles non- sence de mollusques terrestres dans ces mêmes sédiments permet aussi d’attribuer marines, le synthème de Borro Strolla au Messinien supérieur-Zancléen inférieur. Les attri- analyses de faciès, Bassin de Valdelsa, butions stratigraphiques établies pour le synthème de Borro Strolla sont corrélées Italie centrale. aux événements locaux et régionaux enregistrés à la limite Messinien-Pliocène.

INTRODUCTION by a well-known sequence of dramatic palaeo- environmental changes though not unanimously Th e period encompassing the latest Miocene-earliest interpreted in terms of sedimentary successions, Pliocene was marked in the Mediterranean region including thick evaporites, chronology and forcing

612 GEODIVERSITAS • 2008 • 30 (3) Th e end of the Lago-Mare time in the SE Valdelsa Basin (Italy)

factors (see recent review in Rouchy & Caruso 2006). at local scales the circumediterranean margins A late Messinian catastrophic sea-level fall aff ecting with consequent control on the depositional pat- the whole Mediterranean Basin is generally accepted terns in several Messinian basins (Boccaletti et al. following the seminal papers on the Messinian Salin- 1990b). Th e basins developed on the western side ity Crisis (MSC) (Hsü et al. 1973, 1975, 1978; Cita of the Northern Apennines (Central Italy) bear the et al. 1978). Nevertheless, in the last 15 years such sedimentary record of these events outlining the a dramatic sea-level fall has been considered to have interference between local tectonism and sea-level occurred either diachronically or synchronously in changes occurred in the late Messinian. Angular marginal and deeper areas, in a time-span ranging unconformities within the evaporite-bearing suc- from about 7 to 5.6 Ma (see review of alternative cessions and resedimented evaporites, in fact, record time and facies models for the MSC in Rouchy & the active uplift and erosion of the basin margins Caruso 2006 and Manzi et al. 2007). At the end of across and following to the Salinity Crisis (Testa & the Messinian, between 5.59 and 5.33 Ma (Krijgsman Lugli 2000). Th e Mio-Pliocene transition has been et al. 1999), a dilution of a hyperaline Mediterranean described in many Tuscan basins as stratigraphi- Basin determined the formation of a low-salinity sea cally concordant (Bossio et al. 1993) equating the known as the “Lago-Mare” realm (Ruggieri 1962, local Lago-Mare replacement by normal marine 1967a, b). Th e sedimentary successions referred to condition to the sudden, catastrophic, refi lling of this latest Messinian setting, widely recognized in the Mediterranean Basin. Nevertheless, locally this many circum-mediterranean basins and including transition may be stratigraphically more complex resedimented and primary evaporites and clastic hinting to interplay of eustacy and tectonism on deposits, bear a typical palaeontological signature the depositional dynamics. characterized by molluscs, ostracods and dynocysts Th is paper summarizes a case study in which a with a marked Paratethyan affi nity (for a review see previously reported concordant contact between Orszag-Sperber 2006). Th is feature has fed a debate Lago-Mare and open marine sediments is only which is still in large part open, around the latest apparent. Specifi cally, data from integrated strati- Messinian connections among the Paratethys, the graphic and palaeontological analyses carried out Mediterranean and the Atlantic basins (Orszag-Sperber in the SE Valdelsa Basin (Strolla Creek area, central 2006). Finally, the restored connection between the Tuscany), indicate complex stratigraphic relations Atlantic Ocean and the Mediterranean Basin, at the among marine and non-marine deposits which beginning of the Pliocene, determined the sudden escape the picture of the Mio-Pliocene transition replacement of the Lago-Mare realm with open and recorded elsewhere in the Mediterranean area. deep marine conditions. Th ese events had a great impact on the structure and composition of the circum-mediterranean biotas forcing large-scale fau- GEOLOGICAL SETTING nal exchanges, local extinction, palaeobiogeographic OF THE VALDELSA BASIN isolation, etc. (Benson 1976, 1984). Such a sequence of events was mostly controlled Th e study area is located in the southeastern end by tectonically-driven sea-level changes, related of the Valdelsa Basin (Fig. 1), a 25 km wide and to the temporary closure and re-opening of the 60 km long NW-SE trending depression, bounded Gibraltar Strait, and by high-frequency climatic by the Monte Pisano-Poggio del Comune ridge to fl uctuations (Bertini 1994, 2006; Butler et al. the SW, and the Monte Albano-Monti del Chianti 1995; Orszag-Sperber et al. 2000; Rouchy et al. ridge to the NE and SE and fi lled with more than 2001; Griffi n 2002). Th e latter determined cyclo- 2000 m thick Neogene and Quaternary sediments themic development of the Messinian successions (Ghelardoni et al. 1968). exposed in the Mediterranean area. Th e active tec- Th e substratum of these deposits (Fig. 1B) is com- tonic setting related to the late collision between posed on the SW of Late Paleozoic-Jurassic phyllites, the Africa and Europe plates, was also aff ecting quartzites, evaporites and carbonates (Adria basement

GEODIVERSITAS • 2008 • 30 (3) 613 Abbazzi L. et al.

and Tuscan units) thrusted by sandstones, limestones or “Argille Azzurre-lower part”) referred to the lower- and claystones, Late Cretaceous-Paleogene in age most Pliocene Discoaster variabilis-Sphaeroidinellopsis (Ligurid units). Oligocene Macigno sandstones biozones. Th is unit is in turn unconformably capped (Tuscan units) dominate on the NE side, whereas by paralic gravels passing upward to shallow marine limestones and claystones of Ligurid units form the sands (“units C-D” or “Conglomerati di Casa Stieri”) eastern and southeastern margins of the basin. and clays (“unit E” or “Argille Azzurre-upper part”) Th e tectonic origin of the Valdelsa Basin, as well as referred to the middle Pliocene. Th e local succes- of the several basins west of the Northern Apennines, sion is topped by shallow marine sands (“unit F” or feeds a debate between supporters of “extensional” “Sabbie di Talciona”), in erosive contact with “unit E”, (Trevisan 1952; Sestini 1970; Martini & Sagri 1993; ascribed to the middle Pliocene as well on the basis Carmignani et al. 1994; Elter & Sandrelli 1994) and of the fossiliferous content. “compressional” (Bernini et al. 1990; Boccaletti et al. According to Benvenuti & Degli Innocenti (2001) 1990a, 1995; Boccaletti & Sani 1998; Bonini & Sani the middle Pliocene units C-F correspond to the 2002) models. Th ese basins (Fig. 1A), fi lled with up- Certaldo (“units C-E”) and Ponte a Elsa (“unit F”) per Miocene-Pliocene fl uvio-lacustrine and shallow- synthems whereas unit B may represent part of an marine deposits (central basins sensu Martini & Sagri older synthem (Borro Strolla synthem, see below) 1993) or exclusively with middle Pliocene-Pleistocene within the Valdelsa Basin Pliocene succession. fl uvio-lacustrine and fl uvial deposits (peripheral basins sensu Martini & Sagri 1993) a few hundreds meters up to 2500 m thick, are, in fact, alternatively interpreted LOCATION AND STRATIGRAPHY as grabens/half-grabens or thrust-top basins. OF THE STROLLA CREEK AREA Th e basin-fi ll development during the Messinian SE VALDELSA BASIN was regulated by a major regional relief, the Mid Tuscan Ridge (Fig. 1A), representing a signifi cant Th e study area is located near Poggibonsi, 45 km SE physiographic divide. Several basins developed on the to Florence (Fig. 3). Th is is a hilly area stretching along east of this ridge, such as the Valdelsa Basin, did not the western side of the Chianti Mounts, drained by experience evaporitic deposition during the Salinity two small tributaries of the Elsa river, the Carfi ni and Crisis maintaining fully terrestrial environments Strolla creeks respectively. Along the Strolla Creek, up to the early Pliocene. On the contrary, west of good exposures of the Neogene deposits are available this ridge, marine ingression since early Messinian thanks to extensive quarrying of gravel and sand. favoured accumulation of gypsum and salts. On the NNE of the study area the Mio-Pliocene From a stratigraphic point of view the Neogene deposits rest unconformably on the pre-Neogene sediments exposed in the Valdelsa Basin, mostly of substratum forming the Chianti Ridge. Upper Pliocene age, have been recently (Benvenuti & Degli Mio cene sediments, unconformably overlain by the Innocenti 2001) included in a stratigraphic frame- Pliocene succession, crop out to a limited extent work based on fi ve main unconformity-bounded in the study area but they are widely exposed in units (synthems: International Subcommission on the nearby Casino Basin (Lazzarotto & Sandrelli Stratigraphic Classifi cation 1994). 1977; Bossio et al. 2001). Th e fi eld recognition of In the Strolla Creek valley a succession including unconformities or inferences on unconformable the Miocene-Pliocene transition has been described transitions supported by facies relations and bio- by Bossio et al. (1993, 2001; Fig. 2). Th e basal term of chronologic considerations allowed to subdivide this succession consists of non-marine clays (“unit A” uppermost Messinian-earliest Zanclean deposits or “Casino clays” respectively by Bossio et al. 1993 into three unconformity-bounded units consisting and 2001) ascribed to the uppermost Messinian on of various lithofacies associations (see Benvenuti & the base of the non-marine ostracod and mollusc as- Degli Innocenti 2001 for a similar approach) in- semblages. According to Bossio et al. (1993, 2001) this dicative of diff erent paleoenvironments developed unit is conformably overlain by marine clays (“unit B” in this area.

614 GEODIVERSITAS • 2008 • 30 (3) Th e end of the Lago-Mare time in the SE Valdelsa Basin (Italy)

A N N G M ITALY FPP Lucca FlorencePRATOMAGNO VP C CHIANTI RIDGE VE MID TUSCAN RIDGE VA Leghorn TF Vol Arezzo Cec Cas Siena Middle Pleistocene Rad Ser VC to recent deposits Early Pleistocene SR deposits Vel Mbam Rib Pliocene deposits BC Late Tortonian- Messinian deposits Late Burdigalian- Grosseto Tortonian deposits Pre-neogene units Bolsena Lake Alb Magmatic rocks 50 km

B Axis of anticline 2000 Isobates of the top 500 of the substratum (m)

Serchio River CHIANTI MOUNTS

500 500 2000 PISANI MOUNTS Arno River Pesa River N 1000 200 0 Val d'Elsa Alluvial deposits (Pleistocene-Olocene) 1000 Elsa River Basin 50 Marine and continental 0 deposits (Plio-Pleistocene) Marine and paralic deposits (lower-middle Pliocene) study area Iano - Poggio de Fluvio-lacustrinel deposits (upper Miocene) Late Paleozoic-Jurassic basement Casino Ba

l Comune Ridge Ligurid limestones sin Substratum Ligurid and Subligurid units 20 km Tuscan Tuscan units Metamorphic units

FIG. 1. — A, Schematic distribution of Neogene-Quaternary basins west of the Northern Apennines (dotted line borders area in B); B, schematic geology of a portion of central Tuscany including the Valdelsa and the Casino basins (after Benvenuti & Degli Inno- centi 2001). Isobates of the top substratum after Ghelaroni et al. (1968). Abbreviations: Plio-Quaternary basins: C, Casentino Basin; FPP, Firenze-Prato-Pistoia Basin; G, Garfagnana Basin; M, Mugello Basin; VA, Upper Valdarno Basin; VC, Valdichiana Basin; Mio- Quaternary basins: Alb, Albegna Basin; BC, Baccinello-Cinigiano Basin; Cec, Cecina Basin; Cas, Casino Basino; Mbam, Monte- bamboli Basin; Rad, Radicondoli Basin; Rib, Ribolla Basin; Ser, Terrazzano Basin; SR, Siena-Radicondoli Basin; TF, Tora-Fine Basin; VE, Valdelsa Basin; Vel, Velona Basin; Vol, Volterra Basin; VP, Viareggio-Pisa Basin.

GEODIVERSITAS • 2008 • 30 (3) 615 Abbazzi L. et al.

Bossio et al. 1993 Bossio et al. 2001 This study

F

E Pst PE Middle

Piacenzian D Pa C CR PS

PLIOCENE B Pa Lower

Zanclean BS3 BS2 BS1 McL1 MsQ A MbG UM2 MaC

UM1

Messinian Mc Mc Upper MIOCENE MaF Mc

Tortonian McL

FIG. 2. — Comparison among different stratigraphic framework established for the Neogene deposits in the Strolla Creek area. Legend for codes: A-F, see text. Abbreviations: BS1-3, sub-synthems within the Strolla Creek synthem; CR, Certaldo synthem; MaC, Ca- sino Clays; MaF, Torrente Fosci Clays; MbG, Grotti Breccias; Mc, Caprareccia Sandstones; McL, Podere Luppiano Conglomerates; McL1, Lilliano Conglomerates; MsQ, Quercegrossa Sandstones; Pa, Argille Azzurre; PE, Ponte a Elsa synthem; PS, Casa Stieri Con- glomerates; Pst, Talciona Sand; UM1, upper Tortonian-lower Messinian lacustrine deposits; UM2, Messinian Lago-Mare deposits.

UPPER MIOCENE DEPOSITS ascribed by various authors to the fi rst lacustrine (UPPER TORTONIAN-MESSINIAN) event in the Casino Basin (“lower lacustrine cycle”, Th e upper Miocene deposits are visible in small Lazzarotto & Sandrelli 1977; “Argille del Torrente outcrops along and around the Strolla Creek (Fig. 3) Fosci”, Bossio et al. 2001). Ostracod assemblages and are represented by muddy sediments includ- (see below), in fact, point to a late Tortonian-early ed within two units (UM1 and UM2). Despite Messinian age, in agreement with the biostrati- stratigraphic transition is not directly visible, an graphic calibration provided by these authors; unconformable contact between the two units is – UM2: greenish-grey clays and silty clays with here suggested (see below): abundant organic matter, vegetal debris, calcareous – UM1: light brown-grey mostly massive silty clays nodules and rich oligohaline mollusc and ostracod bearing calcareous nodules, vegetal debris, ostracod assemblages (see below). Th ese muddy deposits, in valves and scanty mollusc remains. Th ese deposits, the outcrop 1.5 m thick, are prevalently massive observed exclusively in limited outcrops NE and although thin lamination has been locally observed. SE of the Strolla Creek, are correlatable with those Th e mollusc fauna is either sparse in the sediment or

616 GEODIVERSITAS • 2008 • 30 (3) Th e end of the Lago-Mare time in the SE Valdelsa Basin (Italy)

Recent  alluvial  deposits 350 1 Ponte a Elsa synthem 300 Vegi 250 Certaldo synthem (uppermost Zanclean- Poggio 3

lowermost Piacenzian) A’ diVillore Villa rosa Borro Strolla synthem 250 (uppermost Messinian- 200 lowermost Zanclean) UM2 deposits (Messinian) Fizzano UM1 deposits

(uppermost Tortonian- BS3

Creek 250 lowermost Messinian) 200 Strolla Ligurid substratum Bozzagone Carfin Creek fault sample for ostracod analysis 2 San Fabiano Alluvial deposits A Ponte a Elsa synthem BS3 m g Certaldo synthem

7 BS3 m Piaggiole A s BS3 Borro quarry Piaggiole B g Strolla quarry BS2 synthem 1616 BS1 275 1515 UM2 deposits

200 normal fault UM2 Creek Strolla active quarry BS3 BS2 inactive quarry BS3 250 BS1 BS2

225 BS1 Piaggiole B quarry

Borro Strolla BS3 BS3 Piaggiole A quarry BS3

200 BS3

BS3

225 1515

1717 A

175 A’

200 270 m BS3 190 m BS3

Borro Strolla 200  m

FIG. 3. — Schematic geological maps and cross-section of the Strolla Creek area. Abbreviations: g, gravelly lithofacies; m, muddy lithofacies; s, sandy lithofacies.

GEODIVERSITAS • 2008 • 30 (3) 617 Abbazzi L. et al.

BS3-sandy lithofacies BS3-sandy lithofacies

BS3-gravelly BS3-gravelly lithofacies lithofacies

BS3-sandy lithofacies

talus BS3- gravelly lithofacies talus

FIG. 4. — Panoramic view of the sub-synthem BS3 showing the cyclic stacking pattern of fl uvial gravely-sandy lithofacies associations. The outcrop, the Sefi Quarry face affected by a normal fault, is about 45 m high. concentrated in thin horizons. Ostracods are present be accumulated in the southeastern end of the even if scanty. Th e uppermost part of the deposit is Valdelsa Basin simultaneously to similar deposition composed of blackish clays lacking molluscs, rich in the second Casino’s lake. Deposits lithologically in organic matter and sulphur concretions. Th is and paleontologically equivalent to UM2, in fact, lithofacies is sharply overlain by Zanclean marine have been drilled in the central part (San Miniato clays of sub-synthem BS3 (see below). area) of this basin (Ghelardoni et al. 1968) sug- Th e UM2 unit has been observed exclusively in the gesting that a Lago-Mare-like setting occurred on Piaggiole A quarry (Fig. 3), coinciding with the Bos- a large portion of the Valdelsa Basin during the sio et al. (1993) “unit A”. Successively this unit was latest Miocene. We consider, therefore that the ascribed to the “Argille del Casino” (Bossio et al. 2001), transition bewteen UM1 and UM2, though not considered to record a second lacustrine episode (“upper visible, is marked by an unconformity related to lacustrine cycle”, Lazzarotto & Sandrelli 1977) in the the tectonically-driven transition from the early adjacent Casino Basin. Renewed lacustrine condition Casino Basin to the early Valdelsa-late Casino Basin established in the latter basin following the deformation system (see Discussion). and erosional truncation of UM1 deposits. Angular unconformity within the lacustrine succession of the BORRO STROLLA SYNTHEM (UPPERMOST Casino Basin represents an “intramessinian” uncon- MESSINIAN-LOWERMOST ZANCLEAN) formity of regional signifi cance (see below). Th e deposits included in this study in the Borro New survey of the Casino Basin’s upper Miocene Strolla synthem (BS) were referred by Bossio et al. succession (Benvenuti pers. comm.), indicated that (1993) to the upper Miocene continental gravels the UM2 deposits in the Strolla Creek are at least (“Conglomerati di Lilliano”in Bossio et al. 2001) partially separated from such lithologically equiva- and to “unit B” (“Argille Azzurre-lower part” in lent deposits in the Casino Basin, by a substratum Bossio et al. 2001). Th ese deposits are overlain by high. Th us the UM2 lithofacies is considered to uppermost Zanclean-Piacenzian Certaldo synthem in

618 GEODIVERSITAS • 2008 • 30 (3) Th e end of the Lago-Mare time in the SE Valdelsa Basin (Italy)

N S

Log 1 BS3 Log 2 BS3 BS3 Log 3 Log 4 Log 5 Bs1 BS3 BS3 BS3 BS3 BS3 BS3 BS2 BS3 BS2 BS2 BS2 BS2 BS2 BS3 BS3 BS2 BS1 BS1 BS1 BS1 BS1 BS1 BS1 BS1 approx. 50 m Log 1 Log 4 Log 3

5 Log 2 BS3 BS3 15 Log 5 5 BS3 BS1 5 BS3 10

BS2 BS2 BS2 0 m clay 0 m 10 silt 0 m clay clay 5 BS3 sand silt granules silt sand sand pebble granules boulder granules BS1 pebble pebble 5 boulder boulder BS1 0 m clay silt sand 0 m granules clay pebble silt boulder sand granules pebble boulder colluvial deposits cross-stratification BS3 horizontal stratification terrestrial molluscs BS2 Borro Strolla synthem macrovertebrates vegetal remains BS1 microvertebrates normal faults

FIG. 5. — Photographic sketch, line drawing and correlation of logged sections in the lower-mid portion of the Borro Strolla synthem exposed in the Piaggiole B quarry face (see text). turn capped by the Piacenzian Ponte a Elsa synthem – despite BS is aff ected by normal faults (Fig. 3), which are not discussed in this paper. BS unconform- off set doesn’t prevent the recognition of its internal ably overlies UM1 deposits whereas the stratigraphic architecture proving limited tectonic displacement. contact with UM2 has not been observed. Neverthe- Nevertheless, a normal fault, visible in the Piaggiole A less, we favour an unconformable transition as well, quarry area, downthrows the BS deposits indicating basing on the following considerations: an original position over the UM2 deposits; – UM2 and the Borro Strolla synthem crop out at – lowermost Zanclean marine clays (Bossio et al. very short distance respectively in the Piaggiole A and 1993, 2001) onlapping UM2 at the Piaggiole A B quarries (Fig. 3). Due to the signifi cant thickness quarry and the fl uvial, gravelly-sandy portion of the of the gravelly-sandy portion of BS, well-exposed BS elsewhere (Fig. 3 see geologic section), represent on the left bank of the Strolla Creek (Fig. 4), a in fact, the uppermost portion of this synthem. stratigraphic onlap of UM2 on these deposits seems We suggest therefore that UM1-UM2 and BS de- highly improbable being, in fact, never documented posits are separated by an high-relief erosional contact (see also Bossio et al. 1993, 2001). Furthermore recording a NW-SE trending deeply incised fl uvial a lateral transition from alluvial gravels and sand valley (see discussion). Th e recognition of low-rank into lacustrine muds in a so short distance, appears erosional surfaces within the BS deposits allowed sedimentologically inconsistent; to establish three sub-synthems (Figs 3; 5).

GEODIVERSITAS • 2008 • 30 (3) 619 Abbazzi L. et al.

TABLE. 1. — Checklist of micro- and macromammal taxa found in are massive fi ning upward to silty sands and dark grey the BS1 and subordinately BS2 sub-synthems. silty clays. Th e latter are characterised by dispersed organic matter, root traces, land and subordinate Artiodactyla Bovidae: Protoryx-Paleorix group freshwater molluscs and scanty vertebrate remains Cervidae: cf. Paracervulus (see below). Th ese deposits are unconformably Giraffi dae: gen. et sp. indet. Insectivora Erinaceidae: Galerix cf. depereti overlain by sub-synthem BS3 deposits. Rodentia Cricetidae: Apocricetus barrierei Gerbillidae: Debruijnimys sp. Sub-synthem BS3 Muridae: Apodemus gudrunae Th is sub-synthem consists of two vertically stacked Centralomys benericettii Stephanomys aff. donnezani lithofacies assemblages well-exposed on the Piag- Sciuridae: gen. et sp. indet. giole B and Sefi quarry faces (Figs 4; 5): Lagomorpha Ochotonidae: Prolagus sorbinii – the lower lithofacies assemblage is mostly represented Leporidae: gen. et sp. indet. by gravely and subordinate sandy deposits arranged in two main fi ning-upward bedsets separated by an erosive surface. Gravels are polymodal, well to moderately, Sub-synthem BS1 clast-supported with abundant coarse grained sandy It is composed of sands and subordinate gravels matrix. Locally gravels are characterised by trough observed exclusively in the Strolla Creek valley at and planar cross-bedding indicating paleocurrent to the base of the Piaggiole B quarry face (Fig. 5). Th e W-SW. Th e sands are coarse-medium grained showing lithofacies association, 1.5-9 m thick, is represented horizontal and trough cross-stratifi cation; by an alternation of greyish-purple coarse-grained – the upper lithofacies assemblage rests on the sands, silty sands, and subordinate gravels. Sands previous one through a sharp surface marked by range from normal graded, horizontal planar and oxidized iron encrustations, gypsum crystals and high-angle cross laminated, to massive in places. Th e concretions. Furthermore it sharply overlies the high-angle cross lamination indicates palaeocurrent UM2 just at the Piaggiole A quarry (see also Bossio from S-SE. Gravels are polymodal, clast-supported et al. 1993, 2001). Th e lithofacies assemblage, up with abundant sandy-silty interstitial matrix in to 40 m thick, is represented by massive grey silty dm-m thick lenticular beds interbedded with sands. clays and silts becoming dominant toward the top. Clast composition is mostly represented by lime- Th ese deposits are characterised by dispersed organic stones deriving from the Ligurid unit that occurs matter and vegetal debris and by a rich fossil marine on the northeastern margin, and subordinately by invertebrate fauna including molluscs, ostracods sandstones, limestones and scanty quartzites sup- (see below) forams and nannofl oras (Bossio et al. plied from the Tuscan unit (Macigno Fm., Calcare 1993, 2001). Bossio et al. (1993, 2001) reported the Cavernoso, Verrucano). Sands and silty sands bear results of a biostratigraphic analysis of this deposit non-marine mollusc and vertebrate fossil fauna (see (“unit B” = Argille Azzurre-lower part) suggesting an below). Th is unit is unconformably overlain by the earliest Pliocene age (Discoaster variabilis-Spaeroi- sub-synthem BS2 deposits. dinellopsis seminulina s.l. biozones).

Sub-synthem BS2 Th e lithofacies association included in this sub- PALEONTOLOGICAL ANALYSES synthem is exposed exclusively in the Piaggiole B quarry (Fig. 5) and consists of gravels grading up- Th e material is house in the Science Department ward to coarse-grained sands, silty sands and silty of the University of Firenze. clays. Gravels are polymodal, clast-supported with abundant grey sandy matrix and showing a clast MAMMALS composition similar to sub-synthem BS1. Clast im- A not abundant mammal assemblage has been brication indicates a provenance from SE. Th e sands recovered at Strolla Creek, with at least 12 taxa

620 GEODIVERSITAS • 2008 • 30 (3) Th e end of the Lago-Mare time in the SE Valdelsa Basin (Italy)

AB C E H

D F I G

FIG. 6. — Small mammals recovered from Borro Strolla synthem: A, Galerix cf. depereti Crochet, 1986, left M3 (DST-BS-07); B, Apocri- cetus barrierei Mein & Michaux, 1970, left M1 (DST-BS-05); C, Debruijnimys sp. right mandible with M1-M2 (DST-BS-08); D, Apodemus cf. gudrunae van de Weerd, 1976, right M2 (DST-BS-09); E, F, Centralomys benericettii De Giuli, 1989, left M1 and M2 (DST-BS-10); G, Stephanomys aff. donnezani Depéret, 1890, left M1 (DST-BS-11); H, Prolagus sorbinii Masini, 1989, right P3 (DST-BS-06); I, Sciu- ridae indet., M3 (DST-BS-12). Scale bar: 1 mm.

documented (Table 1). Fossils, on the whole col- (Fig. 7A), one of the younger representatives of lected in the Piaggiole B quarry, come mostly from the Muntiacinae group in Europe and one of the deposits of the BS1 sub-synthem (from sediments better known cervids in France during the Ruscin- of the BS2 sub-synthem, only remains of the ocho- ian Mammal Age (Dong 1990, 1996; cf. Azanza tonid Prolagus Pomel, 1853 are occurring). 2000), occurs in some Italian localities referred to the Th e greater part of fossils belongs to micromammals latest Turolian (e.g., Baccinello V-3, Abbazzi 2001; (Fig. 6) with an insectivore, six rodents and two Monticino quarry and Casino Basin, Abbazzi & lagomorphs; the ochotonid Prolagus sorbinii Masini, Azanza 2000; Gallai 2002). Th e bovids Palaeoryx 1989 (Fig. 6H) is the best represented taxon. Gaudry, 1861 and Protoryx Forsyth Major, 1891 Th e completeness of the mammal fossil record is (Fig. 7B, C) well-known from Greek and Turk- low and both the large and small mammal samples ish localities during the middle and late Miocene cannot be considered fully representative of the (Solounias 1981; Köhler 1987), are also reported original assemblage. Th e contribution of mammals in Spain (Alcalà 1994) during the latest Miocene to the palaeoclimatic and palaeoenvironmental and early Pliocene. reconstructions is therefore of limited value, taking Th e occurrence of a very large giraff e (Fig. 7D, E), also into account that some taxa are not completely comparable in size to Helladotherium Gaudry, 1860 located in a precise systematic scheme; on the other from Greece, is an interesting new datum because hand more signifi cant are the biochronological this group of ruminants is not known from not en- setting and the paleobiogeographic considerations demic Neogene Italian sites. However, it does not deriving from the mammal remains. allow any biochrological conclusion. In fact, large Th e Strolla Creek mammal assemblage, suggests sized giraff es, widespread during the late Mio cene, palaeobiogeographic connections with western are still present in the Pleistocene in eastern Europe Europe, fi tting the general aspect of a fauna at the (cf. Geraads 1998a), while the occurrence of a dubi- Mio-Pliocene boundary. Indeed, the cervid Para- ous sivatheriine is reported from France in the early cervulus Teilhard de Chardin & Trassaert, 1937 Pliocene (Montpellier, MN14 unit; Guerin 1986).

GEODIVERSITAS • 2008 • 30 (3) 621 Abbazzi L. et al.

Also the micromammal fauna shows a transitional nor in the Spanish ones. As a matter of fact, the character (Rinaldi 2003) partially comparable with large size – the length of M1 falls at the largest other latest Messinian mammal assemblages such as extreme of the range of the type sample of D. julii those from Monticino, in Central Italy (Marabini & from Asta Regia and it is signifi cantly larger than Vai 1989). Indeed some of the taxa occurring in the African species – and the large anteroconid are Strolla Creek are also present in the fi llings of the associated to the well-developed posterolofi d and karst fi ssures in the gypsum within the Monticino to the very brachyodont dental crown (Fig. 6C). quarry (De Giuli 1989; Masini 1989; Rook 1992), Taking into account the unknown morphological correlated to the latest Messinian Colombacci variability and the possibility of endemism, we refer Fm: Galerix aff . depereti Crochet, 1986 (Fig. 6A), the Strolla Creek gerbil to Debruijnimys sp. Apocricetus cf. barrierei Mein & Michaux, 1970 Th e occurrence of gerbils in the Neogene of Italy (Fig. 6B), Apodemus cf. gudrunae van de Weerd, is not, however, a novelty: Gerbillidae gen. et sp. 1976 (Fig. 6D), Centralomys benericettii De Giuli, indet. is fi rstly reported from the latest Messinian 1989 (Fig. 6E, F) and Prolagus sorbinii Masini, 1989 Ciabot Cagna site (Piedmont, Cavallo et al. 1993). (Fig. 6H). However, the murid Stephanomys Schaub, However, the scarcity of the material – only a M3 1938, which is documented at Monticino by the has been been found at Ciabót Cagna – prevents species S. debruijni De Giuli, 1989, is represented at any comparison with our remains. Strolla Creek by remains (Fig. 6G) which are closer To sum up, we believe that the occurrence of to the Pliocene species S. donnezani Depéret, 1890 gerbil attributable to the genus Debruijnimys, as (e.g., from the French site Sète; Adrover 1986), and well as its association with the murid Stephanomys, another important diff erence is the occurrence of represented by a species (Stephanomys aff . donnezani) a representative of the Rodentia family Gerbillidae more evolved than the latest Messinian one, could Gray, 1825 (Fig. 6C); the latter form needs a more be indicative of a latest Messinian-earliest Zanclean extensive discussion. Th e dispersal of these rodents age for the BS1 sub-syntem. from Africa towards Spain is indeed one of the Very general palaeoenvironmental inferences can main events related to the Messinian Salinity Crisis be drawn from the mammalian assemblage, which (Wessel 1998, 1999; Agustí 1999). are however in agreement with those derived from Th e morphology of the gerbil remains from Strolla other sources of informations (e.g., molluscs, see Creek is comparable to that of the genus Debruijni- below). Indeed an environment with wooded areas mys Castillo & Agustí, 1996. Th is genus has been and more open spaces is suggested by the occur- defi ned by Castillo & Agustí (1996) on the material rence of the cervid on one hand, and of the large from the middle Pliocene locality Asta Regia (MN sized giraffi d and Debruijnimys sp. on the other; 15 biochronological unit), which has been referred modern gerbils are in fact widespread in the desertic to the species D. julii Castillo & Agustí, 1996. De- and sub-desertic regions of Africa and central and bruijnimys occurs also as an indetermined species western Asia (cf. Tong 1989). (Debruijnimys sp.) in other latest Miocene-early Pliocene Spanish localities (Bacochas 1, cf. Sesé 1989; MOLLUSCS Caravaca 1, cf. Bruijn 1974; Alcoy, cf. Castillo & UM2 deposits Agustí 1996; Agustí 1999; Agustì & Casanovas-Vilar A signifi cant rich oligo-mesohaline mollusc assem- 2003). An origin of the European species of Debru- blage is recorded from unit UM2 sampled in the ijnimys by migration from North Africa during the Piaggiole A quarry (Fig. 8). It is composed of aquatic late Messinian is further supported by the occurrence prosobranch gastropods belonging to the families of D. davidi (Geraads, 1998) in the latest Miocene/ Neritidae Rafi nesque, 1815, Melanopsidae H. & early Pliocene locality Lissasfa (Morocco) (Geraads A. Adams, 1854 and Hydrobiidae Troschel, 1857 1998b; Agustí & Casanovas-Vilar 2003). and bivalves belonging to the families Cardiidae Th e Strolla Creek gerbil shows a mosaic of char- Lamarck, 1809 (Lymnocardiinae Stoliczka, 1871) acters which does not occur in the African sample, and Dreissenidae Gray in Turton, 1840.

622 GEODIVERSITAS • 2008 • 30 (3) Th e end of the Lago-Mare time in the SE Valdelsa Basin (Italy)

C

A

B

D

E

FIG. 7. — Large mammals recovered from Borro Strolla synthem: A, Paracervulus sp., left M1, occlusal view (DST-BS-02); B, C, Protoryx- Paleoryx group (DST-BS-03); B, frontals with horn cores; C, left metatarsus; D, E, Giraffi dae indet., distal end of metapod (DST-BS-04). Scale bars: A, D, E, 2 cm;B, C, 10 cm.

GEODIVERSITAS • 2008 • 30 (3) 623 Abbazzi L. et al.

Th e gastropods are represented by few species with recorded Italian Lymnocardiinae taxa (Di Geronimo a high number of specimens: Th eodoxus mutinensis et al. 1989; Esu 2007). Dreissena ex gr. D. rostri- D’Ancona, 1869, Saccoia etrusca Capellini, 1880, formis, an upper Miocene species of Paratethyan Saccoia fontannesi Capellini, 1880 and Melanopsis origin (Archambault-Guezou 1976), also points to narzolina D’Archiac, 1846. Th e bivalves are domi- oligohaline oxygenated waterbody. Th e Paratethyan nated by several species of Lymnocardiinae: Euxini- genera Chartoconcha Andrussov, 1908 and Psilodon cardium subodessae Sinzov, 1877, Pseudocatillus cf. Cobalcescu, 1883 are new for the Italian fauna. P. pseudocatillus Barbot de Marny, 1869, Pontalmyra Since the ecology of Lymnocardiinae and Dreisse- partschi Mayer, 1871, Chartoconcha sp., Prosodac- nidae is linked to low salinity, spreading of suitable nomya sturi sabbae Andreescu, 1975, Psilodon cf. habitat in depositional systems of marginal settings P. haueri Cobalcescu, 1883, Psilodon cf. P. munieri characterized by increasing freshwater infl ux after Stefanescu, 1896 and other taxa in a fragmentary the “salinity crisis” favoured their dispersal into the state of preservation. Dreissenidae are represented Mediterranean area from the Paratethyan realm. by one species: Dreissena ex gr. D. rostriformis Des- Indeed the well-preserved and diversifi ed mollusc hayes, 1832. assemblage from the Strolla Creek UM2 deposits Th e gastropods T. mutinensis, S. etrusca and indicates the occurrence of a shallow water oligo- S. fontannesi are typical extinct endemic elements, mesohaline environment characterized by a latest occurring in hypo-oligohaline oxygenated shallow Messinian “Lago-Mare” biofacies in that area. water enviroments of Italian basins from the late Tortonian-early Messinian to the latest Messin- Sub-synthems BS1 and BS2 ian (Ghetti et al. 2002 and references therein). Sands of sub-synthem BS1 and the uppermost muds Melanopsis narzolina is widespread in the hypo- of BS2, both sampled in the Piaggiole B quarry, oligohaline enviroments of several upper Miocene bear non-marine mollusc assemblages character- basins of the Mediterranean area and in Italy where ized by some pulmonate gastropods. Th e common it occurs in latest Messinian deposits; it seems to recorded species are Carychium tridentatum Risso, be also present in lower Pliocene deposits of east- 1826, Physa sp., Acanthinula aculeata O. F. Müller, ern Europe (Romania and Slavonia) (Wenz 1929, 1774, Cernuella sp., whilst Parmacella sp., Trunca- 1942; Esu 1980). tellina callicratis Scacchi, 1833, a fragment of the Th e subfamily Lymnocardiinae is very important aquatic prosobranch Melanopsis sp., is exclusive of for palaeobiogeographic inference, being its numer- BS1, and Oxychilus sp. and Cepaea sp., have been ous representatives widespread since the Oligocene found only in BS2. in the western and eastern Paratethys (Nevesskaya On the whole this fauna is composed of species of et al. 2001). Th e genera and species belonging to diff erent habitats with a medium degree of aridity this subfamilty recorded from Strolla Creek deposits and developed under temperate-warm conditions: are of particular palaeoecologic, chronostratigraphic C. tridentatum and A. aculeata occur commonly in and palaeobiogeographic interest. Th ey characterize damp and wooded places, whilst T. callicratis, Parma- the latest Messinian Lago-Mare biofacies with low cella sp. and Cernuella sp. are elements living in open salinity (oligo-mesohaline) and shallow water oc- drier places (Kerney & Cameron 1979). Physa sp. curring in several latest Messinian deposits (such and Melanopsis sp. require slow running-water. Such as Colombacci Fm.) of the Italian peninsula and type of assemblage, in which the terrestrial taxa are Sicily during the post-evaporitic phase (Esu 2002, dominant, points to mollusc reworking in an envi- 2007). Moreover close relations with the lower ronment liable to fl ooding. Th e recorded species are “Pontian” (Odessian) fauna of the Aegean area known so far since the (early?) Pliocene to Recent and strong affi nity with Paratethyan assemblages (Esu & Ciangherotti 2004) except for the genus of Pontian age from Dacian and/or Euxinian ba- Parmacella Cuvier, 1804 which is known in Italy sin (Andreescu 1977; Popov & Nevesskaya 2000; from Messinian to Early-Middle Pleistocene and Nevesskaya et al. 2001) are pointed out by several is still living in warmer Mediterranean and Middle

624 GEODIVERSITAS • 2008 • 30 (3) Th e end of the Lago-Mare time in the SE Valdelsa Basin (Italy)

A B C

D E F

GHI

J K L

FIG. 8. — Non-marine molluscs from UM2 deposit: A, Euxinicardium subodessae Sinzov, 1877, left valve; B, C, Pseudocatillus pseudocatillus Barbot de Marny, 1869, right valve, interior and exterior view; D, Pontalmyra partschi Mayer, 1871, right valve; E, F, Prosodacnomya sturi sabbae Andreescu, 1975, right valve, exterior and interior view; G, Chartoconcha sp., right valve; H, Psilo- don cf. P. haueri Cobalcescu, 1883, right valve; I, Psilodon cf. P. munieri Stefanescu, 1896, left valve; J, Lymnocardiinae indet., right valve. K, L, non-marine molluscs from BS2 deposit; K, Oxychilus sp., apical view; L, Cepaea sp., apical view. Scale bars: A-C, 3 mm; D-F, J, 4 mm; G-I, 15 mm; K, 1 mm; L, 7 mm.

GEODIVERSITAS • 2008 • 30 (3) 625 Abbazzi L. et al.

East areas (Manganelli & Giusti 1990), as well as correlation of UM1 with the deposits of the fi rst the genus Melanopsis Férussac, 1807, pointing to lacustrine episode in the Casino Basin (Lazzarotto & warm climate and a semi-arid environment. A prob- Sandrelli 1977). Th ey document that the fi rst lake able trend from semi-arid and warm conditions to of the Casino Basin signifi cantly extended to the a more humid climate can be hypothesized for the NW. Th e UM1 ostracod assemblages are dominated time-span deposition of BS1 and BS2, taking into by western European and Mediterranean species in account the occurrence of the genera Parmacella, full agreement with the late Tortonian-early Mes- Truncatellina Lowe, 1852 and Melanopsis only in sianian ostracods recorded in other Tuscan basins. the fi rst sub-synthem BS1. Th e occurrence of Lineocypris spp. and Labiato- candona sp., pertaining to the Paratethyan domain OSTRACODS and not exclusive of UM1 (Belforte and Velona Upper Miocene deposits basins, Devoto 1968; Ghetti et al. 2002; Volterra- Th ree samples have been collected in very small Radicondoli Basin, Bossio et al. 1981; Krstic & outcrops referable to late Miocene, respectively Bossio 1992; Testa 1995; Gliozzi et al. 2007), is located NE and SE of the Strolla Creek: two came tentatively explained by the passive dispersal via from unit UM1 (samples 1 and 2, Fig. 3), whereas aquatic birds from the Paratethyan regions (Ben- the third has been collected at Piaggiole A quarry son 1976; Benson & Rakic-El Bied 1991; Gliozzi within unit UM2. et al. 2007).

UM1 deposits. UM1 samples bear well preserved UM2 deposits. Th e Piaggiole A quarry ostracod as- and rather abundant ostracods (Fig. 9A-E), each semblage (sample 3, Fig. 3) is made of few valves of species represented both by adults and instars, thus Caspiocypris cf. C. pontica Sokac, 1852, Cyprideis sp., considered in situ species. Th e ostracod assemblage Loxocorniculina djafarovi (Schneider in Suzin, 1906) from sample 1 is made of brackish Cytheroidea and Loxoconcha sp. (Fig. 9F-J). Baird, 1908 such as Cyprideis sp. 1, Cyprideis sp. 2, Th e species detected in this sample again point Cyprideis sp. 6 and Loxoconchissa (Loxocaspia) sp. 1. to a brackish (oligo- to mesohaline) waterbody, Th e ostracod assemblage from sample 2 consists, on but the presence of two typical Pontian/Dacian the contrary, mainly of Cypridoidea: Candoninae Paratethyan species such as Caspiocypris cf. C. pon- Kaufmann, 1900 (Lineocypris spp., Candona [Negle- tica and L. djafarovi indicates a very restrict time candona] sp., Fabaeformiscandona sp., Labiatocan- interval corresponding to the latest Messinian dona sp. and Pseudocandona sp.), Cyclocypridinae Lago-Mare biofacies, widespread almost all over the Kaufmann, 1900, (Cypria sp. and Physiocypria sp.) Mediterranean Basin (Carbonnel 1978; Cipollari while Cytheroidea are limited to Cyprideis sp. 6 et al. 1999a, b; Gliozzi 1999; Gliozzi et al. 2002, and Tavanicythere joachinoi Bossio, Gliozzi & Tas- in press). In particular, the presence of L. djafarovi sone, 2004. seems to constrain the age of the deposits to the Despite the open nomenclature of some spe- last latest Messinian precessional cycle (Gliozzi et al. cies, the recognized assemblages suggest the ex- 2006). Th ese results, in full agreement with those of istence of a brackish waterbody characterized by Bossio et al. (1993), which reported a richer Para- slight fl uctuation in salinity. Cyprideis Jones, 1857, tethyan ostracod association from these deposits, Tavanicythere Bossio, 1980 and Loxoconchissa (Loxo- suggest a palaeoenvironmental and chronological caspia) Triebel & Malz, 1969, represent typical correlation with the Argille del Casino and confi rm brackish water dwellers, whereas candonids such as the development of the Lago-Mare realm east of Lineocypris Zalanyi, 1929, and Labiatocandona sp. the Mid Tuscan Ridge. Diff erently from the basins (both typical of upper Miocene Paratethyan depos- located to the west, where the Lago-Mare followed its) tolerate slightly saline waters. Th ese ostracod to pre-existing restricted marine environments assemblages are referable to the late Tortonian-early (Volterra-Radicondoli Basin, Bossio et al. 1978; Messinian (Bossio et al. 2001) and confi rm the Bossio et al. 1981, 1996a, b; Sarti & Testa 1994;

626 GEODIVERSITAS • 2008 • 30 (3) Th e end of the Lago-Mare time in the SE Valdelsa Basin (Italy)

A B

D

C

F E

H

G

I J

FIG. 9. — Ostracod valves from UM1 (samples 1, 2, Fig. 3A), UM2 and Borro Strolla synthem-upper part (samples Piaggiole A quarry, Fig. 3B): A-C, sample 1; A, Cyprideis sp. 1, male left valve in lateral external view; B, Cyprideis sp. 2, female right valve in lateral external view; C, Cyprideis sp. 6, male right valve in lateral external view; D-F, sample 2; D, Labiatocandona sp., carapace in left lateral view; E, Tavanicythere joachinoi Bossio, Gliozzi & Tassone, 2004, female right valve in lateral external view; F-J, sample Piaggiole A quarry; F, Loxocorniculina djafarovi Schneider in Suzin, 1906, female left valve in lateral external view; G, Caspiocypris cf. C. pontica Sokac, 1852, female right valve in lateral external view; H, Henryhowella sarsi Müller, 1894, left valve in lateral external view; I, Bythocypris obtusata producta Seguenza, 1880, left valve in lateral view, transmitted light; J, Krithe padovani Colalongo & Pasini, 1988, left valve in lateral view, transmitted light. Scale bars: 0.1 mm.

GEODIVERSITAS • 2008 • 30 (3) 627 Abbazzi L. et al.

Fine Basin, Aldinucci et al. 2005), in the eastern Atlantic and Mediterranean at the beginning of basins, fully or partially isolated from the marine the Pliocene. infl uence, brackish lakes may have been favoured by: 1) the infl ow of saline water generated by the dissolution of the Triassic evaporites (isotopic studies DISCUSSION by Anadón et al. 2002 in the lower Messinian of the Velona Basin); or 2) a partial connection with the Th e stratigraphic revision of the succession encom- Lago-Mare facies, in the specifi c case possibly exist- passing the Mio-Pliocene transition in the Strolla ing in the western portion of the Valdelsa Basin as Creek area allows to focus the discussion on two suggested by core data (Ghelardoni et al. 1968). specifi c aspects.

Sub-synthem BS3 LOCAL DEPOSITIONAL EVOLUTION: No ostracod valves have been recovered in sub- REGIONAL SEA-LEVEL RISE VS LOCAL TECTONISM synthem BS1, BS2 and in the lower part of the Th e stratigraphic relations among the diff erent sub-synthem BS3 deposits. One sample from the units recognized in this study illustrate a complex mudstone on top of sub-synthem BS3 collected depositional dynamic. Non-marine, fl uvial and in the Piaggiole A quarry, provided a scanty but marine conditions established in the Strolla Creek well-preserved marine ostracod assemblage, made area in the following sequence (Fig. 10). of Bythocypris obtusata producta (Seguenza, 1880), Palmoconcha agilis Ruggieri, 1967, Krithe padovani Th e late Tortonian-early Messinian deposition Colalongo & Pasini, 1988, Henryhowella sarsi Müller, and the intramessinian tectonic event 1894 and Macrocypris Brady, 1868. Th is associa- Unit UM1, bearing scanty molluscs and meso-/ tion is very similar to that reported by Bossio et al. oligohaline ostracod assemblages, accumulated (1993, 2001) from the same deposits. during the fi rst fl uvio-lacustrine episode of the Th e lower diversity of this assemblage coupled with Casino Basin in the late Tortonian-early Messinian the presence of marine taxa such as Krithe Brady, (Lazzarotto & Sandrelli 1977; Bossio et al. 2001; Crosskey & Robertson, 1874, Bythocypris Brady, Fig. 10A). Th is evidence indicates that the fi rst Ca- 1880 and Henryhowella Puri, 1957 suggest a rather sino expanded to NW fl ooding an area that succes- deep (outer circalittoral/bathyal) marine environ- sively will pertain to the Valdelsa Basin. Th e upper ment. Th e co-presence of P. agilis (early Messinian Messinian UM2 deposits record the development [Ruggieri 1967b; Aruta 1982] to Zanclean [MPl 2 of a non-marine fl ooded environment (Fig. 10B) or G. margaritae zone] [Nachite 1993]), Bythocypris quite similar to those developing in the same time- obtusata producta (middle Mliocene-early Pleistocene span in other Tuscan basins. In particular such an [Aiello et al. 2000]), H. sarsi (middle Miocene- environment occurred in the nearby Casino (e.g., Present [Bonaduce et al. 1999]) and K. padovani during the second lacustrine episode), Siena basins (Zanclean [MPl 2 or G. margaritae zone] [Ciampo (Lazzarotto & Sandrelli 1977; Bossio et al. 2001) and 1992] to Santernian [MPl 6 or G. infl ata zone] in the central part of the Valdelsa Basin (Ghelardoni [Colalongo & Pasini 1988])point to the Early et al. 1968). Deposition was characterised by sedi- Zanclean. Due to the relatively low resolution of ment settling in quiet shallow waters populated by the Pliocene marine ostracod biostratigraphy, this a diversifi ed benthic invertebrate fauna. Th e mol- age is considered to be in an overall agreement with lusc and ostracod assemblages characterising these that proposed by Bossio et al. (1993, 2001), based deposits show a marked Paratethyan affi nity being on the nannoplankton and planktic foraminifer referable to the latest Messinian Lago-Mare biofacies assemblages. (Esu 2002 and references therein; Gliozzi et al. 2002 Finally, the composition of this assemblage, made and references therein). Th e attribution of UM2 to of a typical Mediterranean-Atlantic stock, attests the Valdelsa Basin rather than to the Casino Basin to the completely restored connection between points to a physical separation established between

628 GEODIVERSITAS • 2008 • 30 (3) Th e end of the Lago-Mare time in the SE Valdelsa Basin (Italy)

the two areas after the deposition and deformation signifi cant role in the setting of mammal fossils. of UM1-“lower lacustrine cycle”/“Argille del Tor- In BS2 the transition from a gravel-bed river to rente Fosci”. Th is “intramessinian” tectonic event low-energy environment is outlined by organic (see below) caused the development of a second matter-rich and terrestrial mollusc-bearing muds. lacustrine setting in the Casino Basin and the Th ese deposits are interpreted as accumulated in a possible activation of the SE Valdelsa Basin where fl oodplain marking the deactivation of the coarse- “Lago-Mare” condition determined the deposition grained transport and deposition. In the thicker of UM2 and similar deposits drilled in the central BS3 sub-synthem two gravel-sand depositional portion of this basin. In particular the physical units record as many phases of decreasing bed- separation of the Casino from the Valdelsa Basin load grain size which refl ect a cyclic shift of the possibly testifi es to an actively growing structural fl uvial style, from gravel- to sand-bed river, as a high tranversal to the basin’s axes. consequence of reduced sediment supply and/or reduced transport capacity, both phenomena com- Th e combination of subsidence pulses and rapidly patible with a relative base-level rise (Shanley & rising sea-level at the Messinian-Pliocene transition McCabe 1994). In the studied case fi ning-upward In the latest Messinian a vigorous fl uvial rejuvena- trend of successive valley fi lls may refl ect the fl u- tion caused the deep incision of the UM1-UM2 vial response to uplift/denudation cycles (Blair & deposits with the development of a N-S trending Bilodeau 1988; Paola et al. 1992; Mutti et al. fl uvial valley about 2 km wide (Fig. 10C). Th e 1996) interfering with a regional sea-level rise western bank of this valley, although disturbed by (see below). Th e uplift/denudation component faults, is located between Piaggiole A and B quar- determined coarse-grained sediment supply to the ries whereas the eastern bank is approximately on fl uvial system during tectonic quiescence whereas the right side of the Carfi ni Creek around Fizzano sediment starving and fi ning derived from the cou- (Fig. 3). Th e valley is fi lled by the Borro Strolla pled eff ect of active uplift of the Chianti Mounts synthem accumulated throughout three major and consequent subsidence of the Valdelsa Basin. stages of alluvial deposition. Palaeocurrent data Th e joined eff ect of subsidence pulses and rapidly indicate the occurrence of tributaries which during rising sea-level at the Miocene-Pliocene transition the deposition of BS1 and BS2 supplied sediments determined periods of high relative base-level in from the SE to the main valley oriented NNE-SSW. the valley controlling the cyclic, fi ning-upward, Th e latter drained toward the SW (Colle Valdelsa fi lling pattern. area) as indicated by palaeocurrent in BS3. A similar, fl uvial, succession occurs in the Casino Th e BS1, BS2 and part of BS3 sub-synthems record Basin (Benvenuti et al. pers. comm.) attesting to three periods of valley aggradation punctuated by the possible coeval development of a fl uvial system erosion (Fig. 5). Th e internal lithofacies architec- draining the former Casino Basin and fl owing to ture in the three sub-synthems is characterised by the ESE (i.e. toward the Siena Basin). It appears fi ning upward trends related to signifi cant change therefore that at the Miocene-Pliocene transition of sediment supply and base level. a watershed between the former Casino and the BS1 sub-synthem records a transition from high Valdelsa basins controlled a diverging drainage. to low-energy channels fi lled with gravels abruptly Such a watershed formed as the consequence of the grading into sands and silty sands. Th e non-marine actively growing tranversal high which conditioned molluscs point to slow fl owing water and to an the Lago-Mare sedimentation in adjacent basins environment liable to fl ooding. A similar conclusion during the late Messinian. can be drawn from the analysis of mammal fossils. Th e low abrasion showed by some bones and, in Th e fl ooding of the Strolla Creek area at the early particular, the presence of articulated limb bones Zanclean maximum sea-level rise indicate that burial occurred soon after the death Th e abrupt marine fl ooding marked by the mollusc- of specimens and that fl uvial transport did not play bearing mudstone sharply resting on UM1-UM2

GEODIVERSITAS • 2008 • 30 (3) 629 Abbazzi L. et al.

and BS3 fl uvial deposits eff ectively records the maxi- (Fig. 1A) located west of the Mid Tuscan Ridge and mum Zanclean rise of the sea level that approached bearing evaporites. Here, the pre-evaporitic terres- the Chianti Mounts (Fig. 10D). An inner shelf, trial to shallow marine deposits, including primary dominated by sediment settling and populated by evaporites pre-dating the Salinity Crisis (Benvenuti diversifi ed benthic communities, replaced the fl uvial et al. 1999; Testa & Lugli 2000), are deformed (see environment. Th e lack of transitional environments Moratti & Bonini 1999 and Brogi & Liotta 2005 between the fl uvial and the inner shelf and the pres- for alternative structural interpretations) and un- ence of a circalittoral/bathyal ostracod assemblage conformably overlain, through unconformity Ima, indicate a very rapid marine fl ooding. by clastics and resedimented evaporites. Angular Th e high sea level recorded by these deposits, unconformity Imb (Testa & Lugli 2000; Brogi et reasonably related to the defi nitive re-fi lling of the al. 2002, see also Pascucci et al. 2004 for a diff er- Mediterranean Basin, may have been the last in a ent inter pretation of this stratigraphic transition) succession of fl ooding pulses which concurred to separates two gypsum units which are referred control the facies stacking pattern of the incised respectively to the lower (primary) and upper (re- valley fi ll (see Discussion above). Th e physiography sedimented) evaporites of Sicily and Spain (Testa & of the wide region including central Tuscany and Lugli 2000). Finally unconformity Imc puts in con- the Northern Tyrrhenian Sea, was characterized in tact the upper gypsum unit with a stratigraphically the Late Neogene by several basins separated by complex clastic succession including resedimented structural highs and located at elevations progres- evaporites, gravels, sands, marls and clays (Monte- sively higher toward the Northern Apennines divide. mamboli Group in Testa & Lugli 2000). On the Zanclean sea fl ooding of the innermost portion of whole the upper gypsum and overlying deposits this region, thus, could have been delayed in respect are referred to the Lago-Mare realm (Testa & Lugli with the fl ooding of the lowermost Northern Tyr- 2000; Pascucci et al. 2004). rhenian Basin and adjoined coastal areas. Such a East of the Mid Tuscan Ridge, where the Messin- “threshold eff ect” on sea-level rise, hence on fl uvial ian is represented by fully terrestrial, evaporite-free, base level, may have represented a further control- terrigenous successions, a prominent intramessinian ling factor for the cyclic sedimentary fi lling of the unconformity is also documented. In the Velona Borro Strolla palaeovalley. Basin (Rook & Ghetti 1997; Bonini et al. 1999; Fig. 1B), strongly deformed fl uvio-lacustrine de- THE MESSINIAN AND THE MIO-PLIOCENE EVENTS: posits ascribed to the early Messinian (Ghetti et FROM A LOCAL TO A REGIONAL PERSPECTIVE al. 2002) are angularly overlain by a further al- Th e local stratigraphic architecture of the succes- luvial succession possibly of late Messinian age. sion recording the Mio-Pliocene transition provides As mentioned above a similar unconformity has arguments for a comparison of events at wider been described in the Casino Basin (Lazzarotto & scales. In general terms the Strolla Creek succession Sandrelli 1977; Bossio et al. 2001) separating the records a discontinuous transition from lacustrine deformed upper Tortonian-lower Messinian fl uvio- to fl uvial to open marine settings evidenced by two lacustrine deposits from the second fl uvio-lacustrine signifi cant internal unconformities. Th e basal one succession encompassing the late Messinian. Due separates UM1 from UM2 deposits whereas the to the strong deformation of the underlying upper upper unconformity subdivides UM1-UM2 from Tortonian-lower Messinian units, unconformities the Borro Strolla synthem. in these basins are tentatively correlated with the Occurrence of unconformities in the Messinian Ima of Volterra-Radicondoli Basin, thus pre-dating successions of the Tuscan basins, documented on the Salinity Crisis. Similarly, we equate the inferred both sides of the Mid Tuscan Ridge, is discussed for unconformable contact between UM1 and UM2 in comparison with the studied case (Fig. 11). the Strolla Creek area to unconformity Ima. At least three major “intramessinian” unconformi- Th e unconformity separating UM1-UM2 from ties are recognized in the Radicondoli-Volterra Basin the Borro Strolla synthem documents a further

630 GEODIVERSITAS • 2008 • 30 (3) Th e end of the Lago-Mare time in the SE Valdelsa Basin (Italy)

A CHIANTIMOUNTS ? ? Casino first lake N ? ? ? ? MONTAGNOLASENESE late Tortonian-early Messinian

B ? ? ElsaLago-Mare ? ? ? ? N ? CasinoLago-Mare ? (secondlake) ? transversal growing high late Messinian

C ns

Elsa sea Quercegrossa Valley

Strolla Creek Valley

waterhed N

ElsaArbia-SerbiaBasi latest Messinian-earliest Zanclean

D ns

Quercegrossa Valley Elsa sea

waterhed N Siena sea

ElsaArbia-SerbiaBasi early Zanclean

FIG.10. — A, The Strolla Creek area ( ) is included in the lacustrine Casino Basin; B, a NE-SW trending structural high separates the Casino from the Valdelsa basins, black arrows indicate major supply points; C, the NE-SW high is a watershed for drainage to the Valdelsa and Siena basins respectively; D, at the early Zanclean maximum of sea-level rise the Strolla Creek area is fl ooded.

GEODIVERSITAS • 2008 • 30 (3) 631 Abbazzi L. et al.

event that characterized the end of the Messinian group of Tuscany. Major tectonic pulses in the North- and that can be searched for in other Tuscan basins. ern Apennines thrust belt and related deformation Th e stratigraphically complex Montebamboli Group of the foredeep are suggested for the origin of these (sensu Testa & Lugli 2000), laying on top of several unconformities. Unconformity Im1, in particular, Messinian successions, has been frequently reported marked the beginning of cyclic sedimentation re- to be conformably overlain by lowermost Pliocene corded in the P-ev2 by fl uvio-deltaic sandstone and marine mudstones (Bossio et al. 1993). Th e basal mudstones. Th e cyclothemic arrangement, expressed unconformity of this succession may be related to by fi ning-upward trends within an overall backstep- the Imc of the Volterra-Radicondoli Basin and, due ping fl uvio-deltaic system, is interpreted as the eff ect to the occurrence of several coarse-grained alluvial of precession-dominated climatic cycles which con- units possibly separated by low-rank unconformities. trolled water and sediment discharge in the fl uvial On the northwestern margin of the Volterra Basin, systems of the Northern Apennines during the latest for istance, alluvial gravels (i.e. “Conglomerati delle Messinian (Roveri et al. 2001, 2003). Volpaie”, Lazzarotto et al. 2002), rest unconform- A latest Messinian unconformity, is recognized ably on the “Lago-Mare” deposits being in turn also in other Mediterranean marginal basins (Mo- overlain by lowermost Pliocene marine mudstones. rocco, Spain, Sardinia, Sicily, Israel; Fortuin et al. Th ese alluvial deposits are ascribed to the lowermost 1995; Buchbinder & Zilberman 1997; Rouchy et Pliocene (Lazzarotto et al. 2002), though a latest al. 2003; Cornée et al. 2004; Soria et al. 2005) as- Messinian age could be considered. sociated to non-marine or fully terrestrial deposits Similarly, in the Velona Basin Montebamboli-like resting on the Lago-Mare deposits. Th is evidence alluvial deposits, resting unconformably on top of the suggests that at a regional scale the Mio-Pliocene Messinian succession (Rook & Ghetti 1997), may be transition may have been marked not only by reasonably referred to the Mio-Pliocene transition. rapid massive sea fl ooding as widely documented As already mentioned, a possibly equivalent un- in relatively deep basins of eastern Mediterranean conformity occurs in the Casino Basin separating and Adriatic regions (Rouchy et al. 2001; Roveri the Messinian fl uvio-lacustrine deposits from fl uvial et al. 2001, 2003) but also by base-level lowering gravels and sands possibly encompassing the Mio- and consequent fl uvial incision caused by intense Pliocene transition (Lazzarotto & Sandrelli 1977). tectonic deformation of the circumediterranean In conclusion we suggest that, despite lacking a margins and associated shallow basins. precise chronostratigraphy, further low-rank uncon- formities punctuated the late Messinian in response to a generalised uplift of the basin’s margins and CONCLUSIONS that the youngest one, Imd, could have marked a palaeogeographic transition from lacustrine to Th e study of a clastic succession referred to the Late alluvial settings in some parts of central-southern Neogene and exposed in the SE portion of the Val- Tuscany during the latest Messinian. delsa Basin has been carried out by the integration Two intramessinian unconformities (Im and Im1), of physical stratigraphy, vertebrate and invertebrate occur also in the evaporite-bearing deposits fi lling (ostracods and continental molluscs) palaeontology. the Adriatic foredeep (Roveri et al. 2001, 2003; In particular attention has been focused on the sedi- Fig. 11), and suggest a possible wider signifi cance ments encompassing the Mio-Pliocene transition of tectonic events aff ecting the Northern Apennines and included into the Borro Strolla synthem which during the latest Miocene. Specifi cally, in the fore- represents a composite fi ll of a NE-SW trending deep basin, Im separates primary evaporites from fl uvial valley, incised in upper Messinian Lago-Mare post-evaporitic deposits similarly to the Imb of the deposits, culminating with a marine fl ooding. Th e Tuscan basins. Unconformity Im1 subdividing the fl uvial deposits characterizing the lower portion post-evaporitic succession in two main units (P-ev1 of this synthem bear scanty remains of the gerbil and P-ev2), can be tentatively equated to Imc-Imd Debruijnimys sp. and the murid Stephanomys aff .

632 GEODIVERSITAS • 2008 • 30 (3) Th e end of the Lago-Mare time in the SE Valdelsa Basin (Italy)

Northern Mid Tuscan Apennines Ridge divide Adriatic foredeep

Volterra- Strolla Casino Marginal Deep Deep Chron. Polarity Planktonic Foraminifers Biozone Radicondoli (SE Elsa) basins basins a basins b Age (Ma) MPL 1 shelf shelf hiatus shelf P. Z. fluvial fluvial ??? p-ev2 p-ev2 Imd p-ev2 Lago-mare Lago-mare Lago-mare Im1 Im hiatus c ????? ash layer res-ev p-ev1 res-ev p-ev1 res-ev Non Imb ????? Im distinct. second pr-ev pr-ev res-ev euxinic shales zone ? Casino lake reef euxinic 6 Ima hiatus shales

brackish Messinian

Globorotalia Gilbert conomiozea MIOCENE first Casino lake euxinic shales

?

7 fluvio-lac

G. suterae Tortonian

FIG. 11. — Tentative correlation of Tortonian-Messinian successions across the Northern Apennines region extending the scheme of Roveri et al. (2001) for the Adriatic margin and foredeep basins. Abbreviations: Chron., chronology; P. , Pliocene; Z., Zanclean.

S. donnezani (Depéret, 1890) (both rodents with during the Late Neogene by several basins sepa- Pliocene affi nity) which represent signifi cant nov- rated by structural highs determining a “threshold elties in regard to the latest Messinian mammal eff ect” on the earliest Pliocene sea-level rise which fauna Italian record. Th e co-occurrence of terrestrial may have caused pulsatory variation of the fl uvial molluscs from the same sediments with a Pliocene base level. Th is eff ect may have concurred to the affi nity, gives further biochronologic constrains development of cyclic facies trends in the fl uvial supporting the calibration of the fl uvial deposits portion of the Borro Strolla synthem. to the latest Messinian-earliest Zanclean. Finally, On the whole the Strolla Creek succession records the marine mudstone on top of the synthem were a discontinuous transition from lacustrine to fl uvial calibrated in previous studies to the early Zanclean. to open marine settings evidenced by two signifi - Besides the revised chronological calibration, the cant internal unconformities which may have some Borro Strolla synthem is characterized by a cyclic equivalents in the Northern Apennines region. In facies architecture which is interpreted in terms of particular the occurrence of a latest Messinian un- interplay between variable sediment supply, depend- conformity allows to reconsider the local Messinian- ing on local, tectonically-controlled, relief uplift Zanclean transition as not properly continuous, a and denudation, and regional rise of sea-level. Th e conclusion having possible implications at a wider latter was evidently driven by the earliest Pliocene scale. Th e Mio-Pliocene transition may have been refi lling of the Mediterranean Basin following to the marked not only by rapid massive sea fl ooding as Salinity Crisis. Th e region between central Tuscany commonly documented in the Mediterranean deep and the Northern Tyrrhenian Sea was characterized basins. Tectonic uplift in the marginal areas may

GEODIVERSITAS • 2008 • 30 (3) 633 Abbazzi L. et al.

have locally subtracted accommodation space dur- Systematics and biostratigraphy of the ostracoda of ing the rapid refi lling of the Mediterranean Basin, the Plio-Pleistocene Monte S. Nicola section (Gela, Sicily). Bollettino della Società Paleontologica Italiana favouring erosional truncations and the develop- 39: 83-112. ment of terrestrial environments which, as in the ALCALÁ L. 1994. — Macromamíferos neógenos de la fosa de studied area, may have locally persisted up to the Alfambra-Teruel. Instituto de Estudios Turolienses, Mu- earliest Pliocene. seo Nacional de Ciencias Naturales, Teruel, 554 p. ALDINUCCI M., BIGAZZI G., DALL’ANTONIA B., DA PRATO S., DONIA F., D’ORAZIO M., FORESI L. M., MAZZEI R., RIFORGIATO F., SANDRELLI F. & ZANCHETTA G. Acknowledgements 2005. — Th e upper Messinian post-evaporitic suc- We are grateful to Fabio Ciappelli for the unvaluable cession of Serredi Quarry (southern Tuscany, Italy): help in the fi eld and for the recovery of most large new stratigraphic data and geochronology of an ash mammal remains. Many thanks to C. Angelone layer. Geoacta 4: 67-82. (Rome) for the identifi cation of Leporidae remains ANADÓN P., GHETTI P. & GLIOZZI E. 2002. — Anoma- lous high Sr/Ca ratios in waters in the late Miocene and to J. Agustí (Tarragona) for the suggestions and (Messinian) Velona lacustrine system (central Apen- discussion during the study of the Muridae remains. nines, Italy). Coincident evidence from comparative Th e authors are indebted to A. Bertini and F. Orszag- geochemistry of ostracod and mollusc shells. Chemical Sperber for critical review of the early manuscript Geology 187: 213-230. and for improving text in French. ANDREESCU I. 1977. — Systématique des Lymno cardiidés prosodacniformes. Sous-famille Prosodacninae. Mé- Th is study received fi nancial support from MURST moires de l’Institut de Géologie et de Géophysique, COFIN 2001 project “I molluschi continentali ed Bucharest 26: 5-74. oligoalini del Miocene superiore (Tortoniano/ ARCHAMBAULT-GUEZOU J. 1976. — Étude de Dreis- Messiniano) in Italia” and CNR I.G.A.G. Institute senidae du Néogène européen et revue stratigraphique (to DE) and by fondi d’Ateneo of the University des niveaux correspondants de la Paratéthys. Travaux du Laboratoire de Paléontologie, université d’Orsay, of Florence (to LR and MB). Paris, 359 p. ARUTA L. 1982. — Gli ostracodi del Saheliano (Miocene medio-superiore) di C. Pestavecchia (Bonfornello, REFERENCES Palermo). Bollettino della Società Paleontologica Ita- liana 21: 113-132. ABBAZZI L. 2001. — Cervidae and Moschidae (Mammalia, AZANZA B. 2000. — Los Cervidae (Artiodactyla, Mam- Artiodactyla) from the Baccinello V3 assemblage (late malia) del Mioceno de las Cuencas del Duero, Tajo, Miocene, late Turolian, Grosseto, Italy). Rivista Italiana Calatayud-Teruel y Levante. Memorias del Museo Pale- di Paleontologia e Stratigrafi a 107: 107-123. ontológico de la Universidad de Zaragoza 8: 1-376. ABBAZZI L. & AZANZA B. 2000. — Deer fauna from BENSON R. H. 1976. — Changes in the ostracods of Late Miocene (Messinian) Italian localities, in Les the Mediterranean with the Messinian salinity crisis. Ongulés holarctiques du Pliocène et du Pléistocène. Palaeogeography, Palaeoclimatolology, Palaeoecology 19-22 Septembre 2000. Musée Requien d’Avignon, 20: 147-170. Avignon, abstract volume: 2. BENSON R. H. 1984. — Th e Phanerozoic “crisis” as ADROVER R. 1986. — Nuevas faunas de roedores en el viewed from the Miocene, in BERGGREN W. A. & VAN Mio-Plioceno continetal de la region de Teruel (España). COUVERING J. (eds), Catastrophes and Earth History: Instituto de Estudios Turolienses, Museo Nacional de Th e New Uniformitarism. Princeton University Press, Ciencias Naturales, Teruel, 423 p. Princeton: 437-446. AGUSTí J. 1999. — A critical re-evaluation of the Miocene BENSON R. H., RAKIC-EL BIED K. 1991. — Biodyna- mammal units in western Europe: dispersal events mics, saline giants and late Miocene catastrophism. and problems of correlation, in AGUSTí J., ROOK Carbonates and Evaporites 6: 127-168. L. & ANDREWS P. (eds), Hominoid Evolution and BENVENUTI M. & DEGLI INNOCENTI D. 2001. — Th e Climatic Change in Europe. Volume 1, Th e Evolution Pliocene deposits in the central-eastern Valdelsa Basin of Neogene Terrestrial Ecosystems in Europe. Cambridge (Florence, Italy) revised through facies analysis and University Press, Cambridge: 84-112. unconformity-bounded stratigraphic units. Rivista Ital- AGUSTÍ J. & CASANOVAS-VILAR I. 2003. — Neogene iana di Paleontologia e Stratigrafi a 107: 265-286. gerbils from Europe. Deinsea 10: 13-21. BENVENUTI M., PAPINI M. & TESTA G. 1999. — Sedi- AIELLO G., BARRA D. & BONADUCE G. 2000. — mentary facies analysis in paleoclimatic reconstructions.

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Submitted on 6 February 2007; accepted on 5 May 2007.

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