INTRODUCTION
The northern side of the northern Apennines has never been considered worthy of attention with respect to the Paleogene larger foraminifera. This is due to the widespread outcropping of terrigenous turbidites and lacking of carbonate platform deposits, which are instead well-represented in the Southern Alps (especially Berici and Lessini Mountains, in the Veneto region).
Nevertheless, scanty records of resedimented larger foraminifera have been reported in the past (Serpagli, 1962, 1964; Petrucci, 1963; Petrucci & Barbieri, 1966;
Sirotti, 1966; Papani, 1967), even in some flyschoid formations from the Emilian side of the northern Apennines. Indeed, the larger foraminifera reported are rare and clearly redeposited out from their environment of life, but they represent the only witness of some still- unknown carbonate platforms.
New material from three formations (Loiano Fm., Montepastore Fm., and Monte Sporno Flysch) has been collected to study the larger foraminifera. Moreover, some of the specimens studied by Sirotti (1966) have been re-determined referring mainly to the monographs of Schaub (1981) and Less (1987).
Aim of this work is to give new data about the larger
foraminiferal assemblages of those formations, with a particular attention to their biostratigraphic and paleo- geographic significance. Regarding the biostratigraphy, we refer to the Shallow Benthic Zones (SBZ) of Serra- Kiel et al. (1998).
GEOLOGICAL SETTING
The Northern Apennines is a complex fold-and-thrust belt originated mainly from the collision between the Sardinia-Corsica Massif and the Apulia (or Adria) microplate (Elter, 1960; Boccaletti et al., 1971;
Boccaletti & Guazzone, 1972; Reutter & Groscurth, 1978).
The tectonic deformation involved different Meso- Cenozoic paleogeographic domains (Ricci Lucchi &
Ori, 1985; Bettelli et al., 1989; Carmignani et al., 2004), namely the Tuscan-Umbria Domain (Apulia microplate), the Ligurian Domain (mainly oceanic), the Subligurian Domain (thinned crust of the Apulia margin close to the oceanic crust), the Epiligurian Domain (sediments deposited over the deformed Ligurian units starting from the Middle Eocene), and the Neogene-Quaternary Succession, filling up the foreland basin.
NEW DATA ON RESEDIMENTED LARGER FORAMINIFERA FROM SOME PALEOGENE FORMATIONS OF THE NORTHERN APENNINES (ITALY)
Cesare A. Papazzoni & Paolo Zoboli
Dipartimento di Scienze della Terra, Università di Modena e Reggio Emilia, Largo S. Eufemia 19, I-41100 Modena, Italy papazzoni.cesareandrea@unimore.it
ABSTRACT - The Paleogene larger foraminifera from some flyschoid formations of the Emilian side of the northern Apennines were restudied. The presence of larger foraminifera in this area has been usually neglected, both for their rarity and for the clear redeposition of the tests out from the environment of life.
Starting from the known occurrences, we restudied the Paleogene larger foraminifera from the Loiano Formation, the Montepastore Formation (formerly known as Coscogno Flysch or Coscogno Limestone), and the Monte Sporno Flysch.
The larger foraminifera identified showed usually the same age in the same samples, so the assemblages are substantially contemporary. Moreover, the ages of the assemblages are consistent with the ages determined with different tools.
The assemblage with Nummulites anomalus, N. beaumonti, N. incrassatus, N. problematicus, N. variolarius, Discocyclina radians radians, Orbitoclypeus varians varians, Asterocyclina stella stella, Asterocyclina stellata stellaris allow to assign a Bartonian age (SBZ 18) to the upper part of the arenaceous member of the Loiano Fm.
Its lower part, with Nummulites alponensis, N. maximus, N. millecaput, N. variolarius, Operculina parva, Discocyclina radians radians, Orbitoclypeus douvillei chudeaui, Asterocyclina stella stella, Asterocyclina stellata stellaris is probably of Middle-Late Lutetian age (SBZ 15-16), even if some reworking is here probable. The assemblages collected from the Montepastore Fm. and from the Monte Sporno Flysch contain Alveolina cf.
ellipsoidalis, A. moussoulensis, Glomalveolina cf. pilula, Orbitolites biplanus, Nummulites praecursor, Ranikothalia sp., Discocyclina archiaci bakhchisaraiensis. They are both attributed to the Lower-Middle Ilerdian (SBZ 6-7, basal Eocene). It is worthy noting that some authors suggested a strict correlation between these formations.
The provenance of the bioclasts is still matter of speculation, given the complete absence of carbonate platform sediments in the surroundings.
KEY WORDS: larger foraminifera, biostratigraphy, resedimentation, Eocene, northern Apennines, Italy.
The formations here considered belong to different domains, so each of them will be briefly described separately.
Loiano Fm.
The Loiano Fm. belongs to the Epiligurian Domain; it is made up of resedimented, mainly coarse-grained sandstones cropping out extensively in the Bologna and Modena provinces. The Loiano sandstones overlay the Monte Venere and the Monghidoro Fms. and is overlaid by the Monte Piano Marls (Bettelli et al., 2002b).
The sandstones, fine to very coarse grained (up to microconglomerates, Bettelli et al., 2002b), whitish to grey in colour, are poorly cemented, with few carbonates and matrix (both <14%). The non-carbonate sand is mainly feldspar (about 50%) and quartz; the K-feldspar (microcline) is more abundant than plagioclase. The coarser-grained fraction is made up by fragments of acidic plutonic rocks (gneiss, granite, etc.). The total absence of epidotes, which are instead largely present in other sandstones from the Northern Apennines, point to a different origin (Gazzi & Zuffa, 1970).
The strata are usually thick, often tabular over decametric distance, but irregular or lenticular over larger extensions. Sometimes there are on the top of the beds thin dark grey clayey levels (Bettelli et al., 2002b).
The Loiano Fm. is interpreted as a turbiditic body with complex geometry, deposited in a pelagic environment, probably under the CCD level. The sandy material came presumably from the Monte Venere Fm. and Monghidoro Fm., which constitute the substrate at the base of the Loiano Fm. (Panini et al., 2002).
Nummulites and orthophragminids (sensu Less, 1987) were first reported by Serpagli (1962) from this unit, then named Rio Giordano Fm., close to Pavullo and Lama Mocogno (Modena province). Serpagli (1962) suggested for this formation a Middle Eocene-
?Oligocene age, in contrast with the Miocene age supposed by previous authors, and stated the larger foraminifera were quite well-preserved. Sirotti (1966) made a first taxonomic description and illustration of this fauna, recognizing 16 different species. He also distinguished three stratigraphic levels, the lowermost one dated to the Middle Lutetian, the second one to a generic Lutetian, and the uppermost one to the Priabonian (due to the recognition of Nummulites cf.
fabianii). The fossils were described as less abundant upwards, with the uppermost levels containing mainly rare specimens of Discocyclina scalaris, and no trace of the transition to the Oligocene was found.
Montepastore Fm.
The Montepastore Fm. is a calcareous-marly turbiditic unit belonging to the Subligurian Domain, cropping out mainly in the Bologna and Modena provinces. It was formerly labelled as Flysch di Coscogno by Serpagli (1964), then re-named as Calcari di Coscogno by
Losacco (1966) and Bettelli et al. (1989), and finally Montepastore Fm. (Panini et al., 2002) on the basis of the structural context (Coscogno tectonic unit: Bettelli et al., 2002a) and of the accompanying formations both in the Bologna and Modena provinces.
The stratigraphic relationships with overlaying and underlaying units are not clear, due to its tectonic displacement (Panini et al., 2002). The Coscogno tectonic unit (Melange di Coscogno according to Bettelli et al., 1989) is made up of different ligurian, subligurian, and epiligurian lithostratigraphic units dismembered and intimately mixed each other. These units have different ages, ranging between the Cretaceous and the early Miocene. The presence in the tectonic unit of some Cenozoic rocks ascribed to the Subligurian Domain suggested (Panini et al., 2002) a correlation between the Montepastore Fm. and the Calcari di Groppo del Vescovo (Barbieri & Zanzucchi, 1963), cropping out in the high Parma Apennines.
The strata are thin to very thick, with a fine- or very fine-grained calcarenitic base passing upwards to cal- careous marls or grey-greenish marls. The calcarenitic levels are sometimes bioclastic, with nummulites, dis- coscyclinas, and alveolinas (Panini et al., 2002).
The calcarenitic levels are made up mainly by calcite (56% to > 95%), with minor quantities of quartz, pyrite (always rare) and rock fragments (Serpagli, 1964).
The tectonic dismembered profoundly this formation, wich at present crops out only on areas wide some tens of meters.
Serpagli (1964) firstly reported the presence of several larger foraminifera, among which Alveolina, Nummu- lites, and Discocyclina, within the turbiditic beds of the Coscogno Flysch (= Montepastore Fm.). He also recognized some smaller benthic foraminifera, such as Rotalia, Elphidium, and Cuvillierina. It is noteworthy the first record of the genus Cuvillierina in Italy (Petrucci, 1963) comes from the Monte Sporno Flysch (see below), correlated by Serpagli (1964) with the Coscogno Flysch.
Monte Sporno Flysch
The Monte Sporno Flysch is a mainly calcareous turbiditic unit belonging to the Ligurian Domain, cropping out mainly in the Parma province (Baganza and Parma valleys). It is overlaid by the Monte Piano Marls, whereas the underlaying units were not observed (Martini & Zanzucchi, 2000).
The turbiditic beds of the Monte Sporno Flysch are either siliciclastic, carbonatic, or mixed, but the carbonate fraction prevails. The terrigenous component of the arenitic beds is mainly quartzy, with subordinate feldspar and rock fragments. Carbonatic bioclasts are often present and sometimes abundant. The cementation by calcite is common, but the matrix contain also a detrital component with silt, clay, and micrite (Fontana et al., 1998).
The unit is subdivided into three informal members,
from bottom to top:
a) Membro di Rio Brugnara (fSp1), with a thickness of 200-220 m. Marly clays, reddish in colour, with occasional fine- to medium-grained arenaceous inter- calations, passing upwards to marls with intercalated calcarenitic beds, often graded (Petrucci & Barbieri, 1966; Cerrina Feroni et al., 2005).
b) Membro di Armorano (fSp2), with a thickness of 1250-1300 m. Marly limestones and limestones, whitish in colour, alternating with light grey marls, in strata up to 5 m thick. This lithology is intercalated with sandstones, calcarenites, and marly pelites in thin to medium layers. Chert nodules are present (Petrucci &
Barbieri, 1966; Martini & Zanzucchi, 2000; Cerrina Feroni et al., 2005).
c) Membro di Calestano (fSp3), with a thickness of 330 m. In comparison with the latter, the marly beds are more frequent (Petrucci & Barbieri, 1966).
The flute casts, groove casts and load casts observed in different localities of the Parma and Baganza valleys show a general direction E-W, with provenance from west (Vinci, 1964).
Petrucci & Barbieri (1966) noted the abundance of foraminifera and microfossils in general; they mentioned, among the larger foraminifera, Nummu- litidae, Alveolinidae, Discocyclinidae and generic
“Orbitoidacea”. Nevertheless, the authors retained the transport and reworking of the tests does not allow their use as biostratigraphic tools. Near Vernasca (Piacenza pre-Apennines) Papani (1967) described a “nummulitic”
calcareous-marly flysch, correlatable with the Monte Sporno Flysch, containing Nummulites sp., Alveolina sp., Discocyclina sp., and Cuvillierina sp., together with several planktonic foraminifera. The latter indicate a Middle-Late Eocene age for this unit. More recently, Fontana et al. (1998) re-examined the Monte Sporno Flysch and reported abundant Paleocene-Eocene microfossils, with planktonic (Globigerina, Globo- rotalia) and benthonic foraminifera (Discocyclina, Miliolidae, Alveolina).
MATERIALS AND METHODS
The sampling has been made starting from the localities cited in the literature.
The Loiano Fm. has been sampled close to Pavullo nel Frignano and Frassineti (Modena province), on the right side of the Rio Giordano creek, along the road going from the main Via per Polinago to the locality Monzone (Fig.
1). Three samples labelled RG 0601, RG 0602, and RG 0603 have been collected from this area; they roughly correspond to the samples 4-7 of Sirotti (1966). The bad outcrops, together with the homogeneous appearance of the rocks, did not allow the reconstruction of any stratigraphic column; anyway, the linear distance between the first and the last sample do not exceed 100 m.
Moreover, we found a new locality (Poggiale near Monzuno, exactly at the km 3 of the Strada Provinciale 59) in the Bologna Apennines (Fig. 1) where the Loiano sandstones contain larger foraminifera never mentioned in the literature. Two samples labelled POG 0602 and POG 0603 have been collected practically on the same stratigraphic level, some 50 m far each other.
All the samples from the Loiano Fm. have been washed to extract the larger foraminifera tests.
Moreover, some specimen from the original sampling of Sirotti were retrieved in the collections of the Dipartimento del Museo di Paleobiologia e dell’Orto botanico of Modena and Reggio Emilia University.
These specimens have been re-studied to update their taxonomic attribution.
The Montepastore Fm. (Fig. 1) has been sampled in locality Coscogno, close to Pavullo nel Frignano (Modena province), along the road Strada Provinciale 22 di Sant’Antonio going towards the road Fondovalle del Panaro (COS 0601, COS 0602, and COS 0603); on the same road near the locality Festà (COS 0604 and COS 0605); and in locality Cà Giuliana (Ospitaletto), about 6 km north of Coscogno (COS 0606). The same formation has been sampled in a small outcrop about 1 km south-east of Vedegheto near Savigno (Bologna province; VED 0601). All the samples come from hard limestones, so they were studied by means of thin sections.
The Monte Sporno Flysch (Fig. 2) has been sampled in its middle part (fSp2in Petrucci & Barbieri, 1966), trying to recognize the coarser calcarenites where the larger foraminifera are more probably contained. We took 7 samples, labelled BN 01, BN 02, CAL 0601, CAL 0602, CAL 0603, CAL 0604, and CAL 0605, all along the road Strada Provinciale 15 between Calestano and Ravarano (Parma province), in the Baganza River valley.
All the samples come from hard limestones (sometimes with silicified levels), so they were studied by means of thin sections.
Fig. 1 - Location map of the sampled outcrops of the Loiano Fm.
(squares) and Montepastore Fm. (triangles) in the Modena and Bologna provinces.
LARGER FORAMINIFERAL ASSEMBLAGES AND AGES
Although the larger foraminifera always show clear signs of transport and redeposition, the reconstruction of the assemblages point generally to a quite well-defined age for each sample or group of samples from the same
formation. Here following are the results of the taxonomic recognition or re-determination, together with the ages in terms of Shallow Benthic Zones (SBZ) after Serra-Kiel et al. (1998).
Loiano Fm.
To compare the assemblages, we will start by discussing the material studied and figured by Sirotti (1966). He grouped his 14 samples into 4 assemblages:
a) samples 1-6, ascribed to the Middle Lutetian;
b) samples 7-8, ascribed to a generic Lutetian;
c) sample 9, ascribed to the Upper Eocene;
d) samples 10-14, containing only “Discocyclina scalaris” (= Orbitoclypeus varians varians), no age suggested.
According to the new taxonomic determination (Tab.
1) we can re-define the latter as follows:
a) samples 1-6, SBZ 15-16 (upper Middle-Upper Lutetian)
b) samples 7-8, SBZ 15? (upper Middle Lutetian?) c) sample 9, SBZ 18-20? (Upper Bartonian-Upper Priabonian?);
d) samples 10-14, SBZ 18-20? (Upper Bartonian- Upper Priabonian?).
The ages of the last two assemblages are to some
Fig. 2 - Location map of the sampled outcrops of the Monte Sporno Flysch in the Parma province (Val Baganza).
Tab.1 - List of the species figured by Sirotti (1966), with updated taxonomic determination.
extent speculative, since no specimens from the samples 9-14 have been figured by Sirotti (1966), except for
“Nummulites cfr. fabianii” from sample 9.
Unfortunately, this specimen is a quite worn equatorial section, showing only the first 7-8 whorls which, according to Papazzoni (1998), do not allow us to distinguish between N. “ptukhiani” and N. fabianii. It could be either of Middle Eocene (Upper Bartonian, SBZ 18) or of Late Eocene (Priabonian, SBZ 19-20) age.
One of us (P.Z.) also found unfigured specimens coming from the Sirotti’s collection (Figs. 3a, 3c). They contain among others some taxa not cited in the
publication, such as Nummulites maximus and N. aff.
biarritzensis, possibly indicating the SBZ 17-18 (Bartonian).
The samples collected by us near Monzone have been taken along the road roughly between the samples 4 and 7 of Sirotti (1966), so they should represent the same level.
In fact, the assemblage recognized contains Nummulites sp., N. beaumonti, N. incrassatus, N.
problematicus, N. variolarius, Orbitoclypeus sp., O.
varians scalaris, O. varians varians, Asterocyclina priabonensis, A. stella stella, A. stellata adourensis. This
Fig. 3 - Larger foraminifera from the Loiano Fm. Assemblage characteristic of its lower part. a) Nummulites alponensis Schaub, A form, equatorial section; sample “Molasse di Rio Giordano campioni 2-3”, Sirotti collection; b) Nummulites puigsecensis Reguant & Clavell, A form, equatorial sec- tion; sample POG 0602; c) Nummulites millecaput Boubée, A form, equatorial section; sample “Molasse di Rio Giordano campione 1”, Sirotti col- lection; d) Orbitoclypeus varians (Kaufmann) scalaris (Schlumberger), A form, equatorial section; sample RG 0602; e) Asterocyclina stella stella (Gümbel), A form, equatorial section; sample RG 0602. Scale bar = 1 mm.
Fig. 4 - Larger foraminifera from the Loiano Fm. Assemblage characteristic of the upper part. a) Nummulites cf. gizehensis (Forskål), A form, axial section; sample POG 0603; b) Nummulites incrassatus de la Harpe, A form, equatorial section; sample RG 0602; c) Orbitoclypeus varians varians (Kaufmann), A form, equatorial section; sample POG 0603. Scale bar = 1 mm.
assemblage point to a SBZ 18 (Upper Bartonian), even if with some elements (A. stellata adourensis, maybe A.
stella stella) possibly reworked from the SBZ 15-16.
The assemblage from Poggiale contains Nummulites anomalus, N. beaumonti, N. ex gr. garnieri, N. cf.
gizehensis, N. puigsecensis, Operculina cf. parva, Discocyclina radians radians, Discocyclina trabayensis trabayensis, Nemkovella strophiolata strophiolata, Orbitoclypeus sp., O. varians roberti, O. varians varians, Asterocyclina stellata stellaris.
This assemblage probably contain elements belonging to two different stratigraphic levels: the first from the Middle-Upper Lutetian (SBZ 15-16; Fig. 3) and the other from the Upper Bartonian-Priabonian? (SBZ 18-
Fig. 5 - Larger foraminifera from the Montepastore Fm. a) Alveolina (Glomalveolina) cf. pilula Hottinger, A form, axial section; sample COS 0601; b) Alveolina moussoulensis? Hottinger, A form, oblique centered section; sample COS 0601; c) Orbitolites biplanus Lehmann, A form, axial section; sample COS 0601. Scale bar = 1 mm.
Fig. 6 - Larger foraminifera from the Monte Sporno Flysch. a) Nummulites praecursor de la Harpe, A form, oblique-equatorial section; sample BN 01; b) Alveolina moussoulensis Hottinger, A form, axial section; sample BN 02; c) Cuvillierina sp., A form, axial section;
sample BN 02; d) Discocyclina archiaci (Schlumberger) bakhchisaraiensis Schaub, A form, equatorial section; sample BN 02.
a-c) scale bar = 1 mm; d) scale bar = 0.5 mm.
20?; Fig. 4). The presence of the Priabonian is not confirmed by any diagnostic species, so it remains highly uncertain.
By means of planktonic foraminifera, the basal member of the Loiano Fm. (Membro di Rio Giordano) has been dated to the Middle-Upper Lutetian (upper part of P10-P12; Panini et al., 2002). The age of the upper part of the formation is still uncertain: in a section measured near Albergana (Bettelli et al., 1992) the maximum age seems to be Early Bartonian (P14), because the overlaying Marne di Monte Piano are attributed to this stage in the basal part. Due to the probable lateral heteropy between the formations this age is questionable (Panini et al., 2002).
Montepastore Fm.
Within this formation, one sample (COS 0601) contains some specimens sufficiently well preserved to allow a specific determination (Fig. 5). Here we recognized Nummulites sp., Assilina sp., Operculina sp., Ranikothalia sp., Alveolina moussoulensis?, Alveolina (Glomalveolina) cf. pilula, Orbitolites biplanus, and Asterocyclina sp. In the remaining samples only some Nummulites sp., Operculina sp., Alveolina sp., Discocyclina sp., and Asterocyclina sp. have been recognized. The assemblage points to the SBZ 6-7, or Lower-Middle Ilerdian (early Early Eocene).
Among the planktonic foraminifera reported by Serpagli (1964) there are Morozovella aequa and Globorotalia formosa gracilis. According to Berggren et al. (1995) the first cover the P4-P6 zones, the latter the P6-P7 zones; therefore, the age should be restricted to the P6 zone, or early Early Eocene.
The calcareous nannoplankton assemblages (Panini et al., 2002), with Discoaster lodoensis and D.
barbadiensis, date the Montepastore Fm. to the Early Eocene (NP 12 Zone)-Middle Eocene (Nannotetrina spp. assemblage, NP 15 Zone sensu Perch Nielsen, 1985).
Monte Sporno Flysch
Here the samples CAL 0601-0604 did not bear larger foraminifera, whereas CAL 0605 contains bad-preserved specimens of Alveolina sp., Discocyclina sp., Orbitoclypeus sp., and Asterocyclina sp. The samples BN 01 and BN 02 (Fig. 6) allowed to recognize Nummulites sp., N. praecursor, Operculina sp., Alveolina cf. ellipsoidalis, A. moussoulensis, Orbitolites sp., Discocyclina sp., D. archiaci bakhchisaraiensis, and Cuvillierina sp.
As in the Montepastore Fm., the assemblage indicates the SBZ 6-7 (early Early Eocene).
Petrucci & Barbieri (1966) reported the presence of Morozovella aequa in the middle part of this formation.
As previously mentioned, it spans the P4c-P6b zones (Berggren et al., 1995) or the Late Paleocene-Early Eocene.
Fig. 7 - Ages of the larger foraminiferal assemblages reported on the biostratigraphic scheme of Serra-Kiel et al. (1998). MP = Montepastore Fm.; MS = Monte Sporno Flysch; L1 = lower part of the Loiano Fm.; L2 = upper part of the Loiano Fm.
CONCLUSIONS
The larger foraminiferal assemblages in the three for- mations examined, though always clearly resedimented, do not show consistent differences in age when com- pared to the data obtained by means of planktonic foraminifera or calcareous nannofossils. This allow us to hypothesize the redeposition of the larger foraminifera was penecontemporaneous. Only in the Loiano Fm.
there are strong clues to some degree of reworking, but even in this case the assemblage is consistent with a sin- gle biostratigraphic level (Middle-Upper Lutetian; Fig.
7).
Regarding the Loiano Fm., the younger larger foraminiferal assemblage (SBZ 18, Upper Bartonian) allows to better precise the age of its upper part, which does not contain any other diagnostic fossil, slightly changing the age supposed indirectly by dating the overlaying Marne di Monte Piano Fm., whose base is probably heteropic.
The Montepastore Fm. and the middle part of the Monte Sporno Flysch (Fig. 7) resulted having larger foraminiferal assemblages of exactly the same age (SBZ 6-7). This support in some way the hypothesis of a correlation between these units advanced by Serpagli (1964) and Losacco (1966). Nevertheless, as noted above, the tectonic context seems to support a correlation with the Calcari di Groppo del Vescovo. Our
data are still insufficient to solve this problem.
Another open problem is the provenance of the resed- imented larger foraminifera. The Northern Apennines currently do not show any preserved carbonate platform of Paleogene age.
By means of its petrographic composition, the Loiano Fm. is supposed to come from the Sardinia-Corsica Massif (Bortolotti et al., 1970; Cibin, 1989).
The same provenance has been hypothesized by Sestini et al. (1988) for the Loiano Fm and for the Monte Sporno Flysch.
A different opinion has been advanced by Abbate &
Sagri (1970), who suggested for the Monte Sporno Flysch a provenance from north-west.
In literature we did not found any indication regarding the possible provenance of the Montepastore Fm. The possible connection with the Monte Sporno Flysch could suggest a common source for the sediments.
ACKNOWLEDGEMENTS - We sincerely thank Prof.
Filippo Panini (Università di Modena e Reggio Emilia) for his useful comments on a preliminary version of this paper. Thanks to Prof. Pier Luigi Vercesi (Università di Pavia) for his critical reading of the manuscript.
Contribution to MIUR PRIN project 2004045107 (Palaeo- climatic forcing on building organism communities, carbonate productivity and depositional systems of some Italian Meso- Cenozoic shelf deposits). Bosellini A., coordinator.
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Accettato per la stampa: Settembre 2007
