FACIES 36 37-56 PI. 11-16 4 Figs. ERLANGEN 1997

Platform Margins, Microbial/Serpulids Bioconstructions and Slope-to-basin Sediments in the Upper Triassic of the ' Unit' (Lucania and , Southern )

Anna Climaco, Maria Boni, Alessandro lannace and Valeria Zamparelli, Napoli

KEYWORDS: PLATFORMCARBONATES - INTRAPLATFORMBASIN - TURBIDITIC CARBONATES - ORGANIC RICH FACIES - REEFS - MICROBIALITES- SERPULIDS - CALABRIA(SOUTHERN ITALY) - UPPER TRIASSIC

SUMMARY margin with buildups and related basinal sediments exists. These sedimentary and paleoecological features match The Upper Triassic carbonates of the area comprised well with those found in the intraplatform basins of the between Maratea (Lucania) and (Calabria) Dolomia Principale, as well as with other coeval facies in have been studied. They have been grouped into six Southern Apennines, Central Apennines, Southern Alps facies assemblages which, in turn, define two depositional and in Southern Spain. Altogether, this evidence suggests systems: that in the Norian time both Southern Alps and Apennines 1) a platform margin depositional system, compris- experienced a very similar tectonic evolution and compara- ing algae- bivalves- bearing dolomites (A1), Megalo- ble paleoceanographic conditions, characterised by the for- dontid-bearing limestones and dolomites (A2), dololutites mation of numerous intraplatform throughs with restricted and stromatolitic/bioclastic dolomites. (A3); circulation, the latter influencing the bottom conditions as 2) a slope to basin depositional system comprising: well as the marginal communities. The margins of these buildup-facies, talus breccia and coarse to fine doloarenites restricted basins, differently from the typical Dachstein (B1), coarse to fine doloarenites and dark laminated reefs of the Upper Triassic Tethys, were dominated by dololutites (B2), dark laminated dololutites (B3). microbial-serpulid communities. The algal and bivalve dolomites represent typical peritidal platform sediments arranged in cyclical pat- 1 INTRODUCTION terns formed as shoal barrier and back-reef deposits periodically emerged and deformed in tepee structures. In the present paper we will concentrate in detail on the The outer margin of the platform was colonised by subject of the Upper Triassic platform to basin transition in peculiar bioconstructions dominated by microbialites Northern Calabria and Lucania. This subject was firstly and serpulids; little sponges occur less frequently, whereas raised by our research group after the recent discovery of rare corals have been found only in some turbiditic beds. slope facies in these regions (IANNACE et al., 1993), and Along the slope, in a distance that can be estimated shortly accounted for in a previous contribution (IA~rnACEet in 5 or 6 km, the coarse breccias give way to coarse al., 1994). This paper, mainly based on the Ph.D. thesis of turbidites, then finer turbidites and finally to dark, A. CuraACO (1996), gives a complete description of the organic-rich micrites. Most of the floatstone and associ- Upper Triassic of the area comprised between Maratea ated turbidites imply a fault- controlled slope. The (Lucania) and Praia a Mare (Calabria). laminated texture and the high O.M. (Organic Matter) Despite the strong tectonic disturbance and the low bio- content of the latter facies quite obviously point to a stratigraphic resolution, a highly diversified depositional basin with poorly oxygenated bottom waters. system has been put into evidence in the whole area, which In the uppermost Triassic there is an indication of a changes radically theprevious simplepaleogeographic models regressive trend, evidenced by the progradation of the based, during Upper Triassic, on a monotonous, long last- platform facies. At that time a back-reef area was char- ing history of peritidal sedimentation. acterised by Megalodontid prairies alternated to areas of A similar evolution of thoughts has already occurred in sandy bioclastic transport. However, due to the poor the geological knowledge of Upper Triassic of Southern biostratigraphic record and intense cataclasis, no defi- Alias and Central Apennines, where the formerly believed nite evidence of a well-structured Rhaetian platform peritidal dolomites of Upper Triassic age (Dolomia Principale)

Address: Dr. A. Climaco, Prof. Dr. M. Boni, Dr. A. Iannace, Prof. Dr. V. Zamparelli, Dipartimento di Scienze della Terra, Largo San Marcellino, 10, 1-80138 Napoli; Fax. 39 - 81 - 552 56 11 38 have been demonstrated to contain also sediments depos- authors in several areas and interpreted as bioherms, but ited in tectonically controlled basins (JADOULet al., 1992). the bulk of the dolomites was generally referred to shal- Therefore, with the data presented in this paper we would low water, lagoonal environment. A distinction between like to stress that a common tectonic and paleogeographic darker and lighter carbonate facies was also observed history was experienced during Upper Triassic in most (BURTON, 1971, p. 53), butno interpretation was proposed sedimentary domains now represented in many Italian for the fact. carbonate successions. The presence of marginal stromatolitic bioconstructions was also indicated by D'ARGE~aO (1966) but this first 2 GEOLOGICAL SETTING mention, based on limited outcrops, was never followed by extensive research. According to the "Structural Model of Italy" (B~GI et Subsequent research works in the area only dealt with al., 1991), the following tectonic units can be recognised regional or applied geology aspects (A~ODIO-MORELtJet in the Miocenic Apenninic nappes of northern Calabria al, 1976; IE~O et al., 1992), never paying more than a and Lucania (from bottom to top): cursory attention to the sedimentology of Upper Triassic - San Donato Unit; dolomites. - Alburno-Cervati Unit; Only very recently, following the work of IAN~CE - Verbicaro Unit. (1991) in the Lattari Mountains, where many different - Frido Unit types of Norian-Rhaetian platform marginal facies have The Frido Unit consists of metasediments of oceanic been described, was proposed that margin-to-slope facies affinity. The first three units mostly consist of carbonate had eventually to occur also in the Verbicaro succession successions deposited on the Apulian passive continental of Northern Calabria (IAr~ACE, 1993): in fact, this as- margin during Meso-Cenozoic. sumption was confirmed shortly later (IANNACE et al. The San Donato and Alburno-Cervati Units, separated 1993, 1994). by a normal fault (BARBIERI et al., 1984), consist of Triassic to Miocene sediments deposited in a carbonate 4 METHODOLOGICAL REMARKS platform environment (BOUSQUET& GRANDJACQUET,1969; D'ARGF.~aO et al., 1973; AMODto-MORELLIet al., 1976). The stratigraphic and sedimentologic investigation of The Verbicaro Unit rests tectonically over both the the Upper Triassic facies in Calabria has been limited San Donato Unit and the Alburno-Cervati Unit (Fig. 1). It quite significantly by the effects of the strong tectonic was defined by BOUSQUET• GRANDJACQUET(1969), and activity characterising most of these successions, coupled comprises the dcaille de Praia a Mare, (recognised by with the traditionally poor biostratigraphic content of the GRANDJACQUET, 1961) and other similar successions more platform carbonates of this age. to the south, formerly believed to be parautochthonous. In fact, thick, continuos successions are rare through- This unit has been interpreted as resulting from the defor- out the whole area and generally limited to platform mation of transitional domain between a carbonate plat- facies. In these kind of facies, the fossil content only form to a basin, unknown in outcrop (D'ARGEr~O et al., allows a very broad differentiation between Lower-Mid- 1973). However, this conclusion has been based only on dle Norian and Upper Norian-Rhaetian, the latter marked the Jurassic to Paleogene part of the succession because by the appearance of Triasina hantkeni (see below). No the significance of the Triassic sediments was never local marker has been found to allow a correlation based addressed in detail. on purely lithologic or 'event stratigraphy' criteria. The situation is even worse for the slope facies. The 3 PREVIOUS STUDIES well bedded nature of these carbonate facies made them highly susceptible to be affected by numerous shear planes The widespread occurrence of Upper Triassic (Norian- and pervasive brittle fracturing. In fact, many extensive Rhaetian) dolomites, comparable to the Hauptdolomit outcrop areas consist of cataclastic, deeply eroded, dark (Dolomia Principale) of the Alps, has been known in dolomites, sometimes developing calanchi features. northern Calabria (Southern Italy) since the end of the last For these reasons, the field investigations have been century (CORTESE, 1895). conducted with different degrees of detail in distinct Particularly, the papers of CORTESE (1895) and DI areas: hundreds of m of platform successions have been Sa'EFANO (1904), despite some stratigraphic discrepancies, measured at m scale, whereas fragments of slope facies and related disagreement between the two authors, are the successions have been surveyed at a dm scale (Fig. 2). first source of objective descriptions and sound data, Total thickness evaluations in the platform facies can be which can still be successfully used in modem research. only affected by the presence of normal faults; on the The extensive geological mapping performed in the contrary, an exact evaluation of the thicknesses of the sixties by C. Grandjacquet (in BtrRTON, 1971) and DA~A~ slope facies is impossible, and therefore these can be only (1970), while representing the first modern and still valu- roughly estimated. Moreover, to avoid false reconstruc- able cartographic document for Northern Calabria, added tions of the facies assemblages geometry, we restricted very few details to the knowledge of the Triassic dolom i tes. the analysis of the depositional systems only to the out- Dasycladacean-rich dolomites were mentioned by these crops belonging to the same tectonic unit, as indicated in 39

Fig. 1. Geological map and Upper Triassic facies assemblage distribution in the studied area. 1: Algae- bivalves- bearing dolomites (A1); 2: Megalodontid-bearing limestones and dolomites (A2); 3: Monte Cifolo dolomites (A3); 4: Buildup-facies, talus breccia and coarse to fine doloarenites (B1) and Coarse to fine doloarenites and dark laminated dololutites (B2); 5: Dark laminated dololutites (B3); 6: Jurassic to Miocene part of Verbicaro and Alburno-Cervati Units; 7: Quaternary. After CL~ACO (1996). 40

Fig. 2. Schematic sedimentological logs and their correlations. The full description of the successions can be found in CLIM^CO(1996).

Fig. 1, and corresponding to the ,,dcaille de Praia a Mare" B - Slope to basin depositional system: of GRANDJACQUET (1961). Recent seismic profiles B1 - Buildup-facies, talus breccia and coarse to (MosXARD~NI & MERtZr~X, 1986) confirm that all these fine doloarenites; outcrops can be viewed as belonging to a relatively coher- B2 - Coarse to fine doloarenites and dark laminated ent tectonic slice. In this way, even with a poor dololutites; biostratigraphic control, the vertical and lateral facies B3 - Dark laminated dololutites. relationships can be used as a reliable tool for correlation and basin reconstruction. In Fig. 1 the facies assemblages distribution is shown. Another point to stress is that, due to the strong The boundary between them have to be taken as quite recrystallization of the lithotypes, very little information arbitrary because of the frequent inter fingering of facies could be extracted from thin section studies. As a conse- (among B1, B2 and B3), or because of superimposed late quence, even though some 400 thin sections have been (epigenetic?)dolomitization masking the lithofacies bounda- observed, the most reliable informations have been gath- ries (between A1 and A2). The two depositional systems ered mainly through a careful study of the best field should be probably taken as lithostratigraphic units,ranked exposures which, in some cases, are undoubtedly spec- as groups, whereas some of the facies assemblages could tacular. represent mappable members. The studied sections are presented in Fig. 2 as syn- thetic logs. The full descriptions can be found in CUMACO 5 FACIES DESCRIPTION (1996). The studied facies can be grouped, regardless of their age, into six assemblages which, in turn, define two 5.1 Algae- bivalves- bearing dolomites (A1) depositional systems (CLIMACO, 1996): This facies assemblage is dominated by 1 to 6 m-thick beds of white-grey massive dolomites alternated with A - Platform margin depositional system: some cm to 1 m laminated fenestral dolomites. The latter A1 - Algae- bivalves- bearing dolomites; beds can be deformed in m-sized mega-tepee structures. A2 - Megalodontid-bearing limestones and dolo- The best example of these facies association occurs at mites; Monte Rotonda (Lucania), particularly along the road cut A3 - Dololutites and stromatolitic/bioclastic of the Strada Statale n ~18 along the Noce river, where the dolomites. 41

basal part of the succession is beautifully exposed. Other extended successions are present at Monte Cocuzzata. Spectacular outcrops of the tepee-bear- ing facies occur along the shore at Marina di Maratea .9 (IAt~ACE, 1993). Similar facies have been observed also at , Monte Cerviero and Campotenese, at the southern edge of the Pollino massif. In the lower part of the Monte Rotonda succes- t2 sion and at Marina di Maratea, dasycladaceans-rich "2 facies are abundant (PI. 11/2,7). They consist of two types of microfacies. The first is represented by packstone/wackestone in which the algae are associ- ated to bivalves, gastropods, foraminifers, poro- r stromata, micritic intraclasts and peloids. The most abundant species identifiedare Griphoporella curvata (GOMaEL) and Poikiloporella duplicata P~A. The identified foraminifers include Aulotortus sinuosus o~ WEVNSCHF.NK, Aulotortus friedli (KRISTAN-TOLL- MANN),Aulotortus sp., Trocholina sp., G lomospirella sp., Endoteba sp., Ammodiscidae and 'Trochammi- .9

nidae'. A second facies consists of grainstone par- .O ticularly rich in large (1 to 5 cm!) thalli ofdasycladacean algae, encrusted by microbialites and cemented by isopachous fibrous dolomite (PI. 11/2,7). The thalli are generally relatively isoriented along bedding with no particular depositional texture. More abundant at Monte Cocuzzata, Serra Vingiolo and in the upper part of Monte Rotonda are bivalves- .9 and gastropods-bearing massive dolomites. The rock is represented by a white-grey dolomite, generally heavily recrystallized, in which the only notable feature is represented by moulds of weathered out shells. This is the classic facies where the first researchers recognised the fossils Worthenia solitaria and Gervillea exilis, typical of the Dolomia Principale facies. The microfacies is not very different from that occurring in the algal packstone/wackestone, except for the reduced abundance of algae. The fenestral fabric form dm- to few m-thick interlayers of fine-grained, laminated dolomite. The microfacies are represented by mudstone or micro- bial bindstone, always rich in fenestrae and birdseye t- cavities. Platy intraclasts are frequent, as well as pisolites (P1.11/3). The latter sometimes are found as in situ formed crusts. Particularly spectacular in this facies assem- blage are the tepee structures and their associated cements. Both mature tepees (PI. 11/1) and senile ~o tepees (tepee-derived breccias) have been observed. The synsedimentary deformation can affect up to O 1m of fenestral facies and is always associated to ~ non-isopachous crusts of laminated cements. In some

cases, where the thickness of the deformed strata is O

reduced, only the presence of stratabound cement O crusts witnesses the existence of this kind of phe- O nomenon. The constant association of the tepee with fenestral facies and pisolites define them as peritidal ~h tepees formed during subaerial exposures at the platform margin. 42

Within the subtidal beds of the tepee facies occurring The microfacies present mainly consist of bioclastic at the Marina di Maratea beach, some fragments of iso- packstone/grainstone (PI. 11/8) and minor wackestone lated, Thecosmilia-type corals as well as thamnasteroid with bivalves and gastropods associated to a well differ- colonies have been found. entiated microfaunaand microfloracomprising foraminifers As already observed by IANNACE (1993), the non- (Triasina hantkeni MAJZON, Aulotortus sinuosus WEvr4- isopachous cement crusts are cut by a second generation SCrmNK,Aulotortus sp., Auloconuspermodiscoides OBER- of cements which are dominated by radial-fibrous tex- r~,USER, Glomospirella sp.), dasycladacean algae (Gripho- tures (P1. 11/4). In the road cut of the Strada Statale n~ 8 porella curvata (Gt~r~mEL) and porostromata. The dasy- these late cements are seen cutting several tens of meters cladacean algae may be locally the dominant fossil re- of the succession (PI. 11/1); therefore a direct genetic link mains, particularly in those layers alternated with strom- to the tepee formation can be discarded. They were pre- atolites. Oncoids can be locally abundant. In a few exam- cipitated in fractures which opened after than a consider- ple, herringbone cross stratification has been observed. able part of the marginal area had been built and ce- This monotonous succession of massive limestone is mented. In this respect, this confirms their possible freatic, rarely interrupted by some dm-thick beds of laminated, late origin, already suggested by IANNACE (1993), fenestral facies. These are normally calcareous-dolomitic but in this case the dolomite is fine-grained and texture 5.2 Megalodontid-bearing limestones and preserving. The microfacies are represented by peloidal dolomites (A2) mudstone and microbial bindstone, always presenting a laminated fenestral porosity. This facies assemblage is characterised by massive It is particularly important to mention that in this beds of limestone, partially or totally dolomitized, in facies have been locally observed din-sized irregular which numerous sparry and thick shells occur (PI. 11/5). cavities filled with botryoidal, radial fibrous calcite. These They can be up to 20 cm long, the most common size being cements, which obviously replace former aragonite ones, around 10 cm, and can be found disarticulated or as were found by IANNACE (I993) at the same stratigraphic complete unbroken individuals. Their morphology gener- position in the nearby mountains around Brefaro (Maratea). ally suggests that they belong to the family Megalodontidae, Larger outcrops, with the same kind of cements, have even though also other families could be represented. been described in the Lattari Mountains and, even though This Megalodontid-bearing lithofacies is present in their exact origin remains still controversial, have been the upper part of the Serra di Castrocucco, Monte Roton- interpreted so far as formed at a platform margin setting. da and Monte S. Angelo successions but its best outcrop It is important to stress here that this Megalodontid- occurs along the sea-shore at Cala la Secca, near Castrocucco bearing limestone is particularly important because it has village. Another outcrop is found at Monte Cucuzzata, been described in several areas of Southern Apennines tectonically resting over cataclastic dolomites of the facies (CIWTA, 1964; DE CASTRO1988; IAr~ACE, 1989; BARATrOLO assemblage B 1. & PARErZrE, 1991; POSENATO & IE~O, 1995), always in The whole facies assemblage is relatively monoto- association with a foraminifers assemblage comprising nous, being dominated by massive calcareous beds more the species Triasina hantkeni, which is considered the or less dolomitized. Typically, late diagenetic dolomite Upper Norian-Rhaetian index species (MARcOLrX et al., replaces the limestone pervasively, along discordant fronts, 1993 and references therein). Similar facies occur in the and has a coarse-grained, non mimetic texture. These same stratigraphic position also in Southern Alps ('Strati features have been shown to be typical of this lithofacies a Triasina', BOSELLINI& BROGLIO-LORIGA,1965), indicat- in the whole Mediterranean area (IANNACE& FRISIA, 1994). ing that this lithofacies, easily recognised in the field, is a

Plate 11 Upper Triassic carbonates of Verbicaro Unit (Lucania and Calabria, Southern Italy). Norian and Rhaetian platform margin facies. Fig. 1. Dolomitic beds with tepee structure (top left) cut by a cement-filled dyke (right). Monte Rotonda. Fig. 2. Hand specimen of Dasycladaceans-rich bed. Monte Rotonda. Fig. 3. Pisolitic micro facies with polygonal fitting and reverse grading found alternated to Dasycladaceans beds. Norian, Monte Rotonda, sample AC 347. Fig. 4. Radial-fibrous dolomitic cements, probably after former aragonite, filling vertical fractures in platform dolomites (see PI. 11/1). Monte Rotonda. Sample AC 351. xl.5. Fig. 5. Megalodontid sparitic shells in dolomitic limestones. Upper Norian-Rhaetian. Cala la Secca. Coin is 2.3 cm in diameter. Fig. 6. Partly dolomitized limestones with flat pebbles and synsedimentary cements of supratidal environment. Upper-Norian-Rhaetian. Cala La Secca. Fig. 7. Griphoporella curvata (Gt3r~mEL) packstone with large dissolution cavities filled by sparry dolomite. Lower-Middle Norian. Monte Rotonda. Sample AC 354. x 8 Fig. 8. Bioclastic grainstone with foraminifers (Triasina hantkeni, Aulotortus sinuosus) and algae (Griphoporella curvata). Upper Norian-Rhaetian, Cala la Secca. Sample AC 469. x 9 Plate 11 43 44 reliable marker for the Uppermost Triassic in platform tectonic fracturing. These occurrences, while allowing carbonates throughout Italy, in agreement with a common detailed observations and a good amount of sampling, practice at the end of last century (CoaTESE 1895). where not apt for a true stratigraphic study. The breccias are very heterogeneous in terms of shape 5.3 Dololutites and stromatolitic/bioclastic and size of the clasts. The latter can vary from some dolomites (A3) centimetres to some meters across (PI. 12/1,2) and gener- ally appear floating in a finer matrix. Their shape is The upper part of the Monte Cifolo section contains a generally very irregular: they can vary from angular to peculiar facies assemblage which is not represented in any sub-spherical, the edges being always quite rounded. other area. The clasts mostly consist of microbial boundstone, The facies is represented by fine-grained dolomitic representing resedimented fragments of organic buildups. mudstone, in beds up to I m thick, generally homogene- Occasionally, among them also white to grey, sometimes ous or showing a very faint, planar lamination. Locally, laminated or stromatolitic fragments occur, the latter they may be brecciated, the clasts showing a good polygo- quite obviously derived from the platform interior. nal fitting. No fossils are normally present in this facies. The buildup-derived clasts are generally irregular, Alternating with these dolomites, other types of facies sometimes mammillary in shape (PI. 12/1,2,4). The pre- Occur: vailing macrofabric consists of a dark, thrombolitic or- - stromatolitic bindstone and mudstone with sheet ganic network in which are scattered ram- to 1 cm-sized, cracks and fenestrae; dendroid cavities filled with grey internal sediment and - bioclastic packstone and wackestone. The bioclasts white, isopachous fringes of dolomitic cements (P1.12/3). consist of Griphoporella curvata (Gt~r~mEL), bivalves, Quite often, these microbial aggregates are enveloped by ostracods, gastropods, Au!otortid foraminifers; stromatolitic crusts. In this case, a different fabric may - pisolitic dolomites represented both by beds with develop in which tuberoid thrombolitic-stromatolitic or- pisoids with polygonal fitting and by irregular layers with ganic aggregates form a quite open network filled with a festoons of laminated, non-isopachous fibrous cements muddy sediment (P1.12/4), less frequently with cm-thick enveloping clasts of mudstone or algal packstone. isopachous fibrous cement crusts. At present, we do not know the meaning of these two different kinds of fabric, 5.4 Buildup-facies, talus breccia namely if they correspond to different organisms or to and coarse to fine doloarenites (B1) different growth morphologies controlled by hydrody- namic factors. The most abundant facies in the central part of the The microbial crusts often envelope isolated or gre- investigated area is represented by various types of breccia garious serpulids (P1. 12/4; P1. 13/1,2,3) or even articu- and other finer resedimented deposits. The breccia depos- lated bivalve shells. Locally (northern side of Serra di its are particularly significant because is mainly in their Castrocucco), serpulids can form large aggregates in clasts that the presence of bioconstructions at the margin which all individuals are in vertical growth position and of the Norian platform is recorded. Only in a few outcrops parallel to each other. In some outcrops (La Spartosa, (i. e. Bocca della Cappella) there is limited evidence of in Bocca della Cappella), little sphinctozoan sponges have situ bioconstructions. been found (PI. 14), also encrusted by microbial laminae. The breccia deposits are particularly well exposed at Nevertheless, the main organic component of the bound- Serra di Castrocucco and in the lower part of Monte stones is represented by the crusts themselves, indicating Cifolo, where they occur in well ordered, stratigraphic that the biomass of these paleoenvironment was largely succession. In other areas, such as La Spartosa locality, dominated by microbial organisms. spectacular outcrops can be found despite a pervasive All the components of these facies are made up of

Plate 12 Upper Triassic carbonates of Verbicaro Unit (Lucania and Calabria, Southern Italy). Upper slope breccias, bioconstructions and associated facies. Norian Fig. 1. Unsorted, probably talus breccia with large rounded clasts of microbial boundstone. Bocca della Cappella. Fig. 2. Unsorted, mud supported breccia with cobble-sized fragments of microbial boundstones. Monte Cifolo. Fig. 3. Detail of a field exposure of a typical exemple of a network of thrombolitic microbialite with cavities filled by internal geopetal sediments and isopachous crusts of white sparry dolomite. Bocca della Cappella, coin is 2.3 cm in diameter. Fig. 4. Irregular, mammillary framework of a thrombolitic-stromatolitic microbialite. Intra-framework space is filled with lighter coloured internal sediment. Within the encrusted portion serpulids are frequently found. Bocca della Cappella. Fig. 5. Concentric, oncoidal-type microbial encrustations on the weathered surface of a loose cobble. Bocca della Cappella. Coin is 2.3 cm in diameter. Fig. 6. Wavy laminated and cross-bedded facies in the fine to medium grained bioclastic dolomites associated to brecciated bioconstructions. M.Cifolo. Coin is 2.3 cm in diameter. Plate 12 45 46 dolomite. This is generally quite coarse, probably in brecciated dolomites, up to 10 m thick. These are heavily consequence of the low-grade metamorphism affecting recrystallized and show no internal structures. The the successions of the Verbicaro Unit. Quite frequently, microfacies are represented by inlyabioclastic rudstone. irregular patches of quartz, generally following the lami- The clasts frequently include disarticulated bivalve shells. nation of the crusts, have been found. In thin section they The matrix consists of pseudospar, resulting from the are represented by mega- and microquartz filling the recrystallization of a former micrite. network cavities. The poor sorting of the breccia clasts, together with the 5.5 Coarse to fine doloarenites absence of any textural structuration and abundance of and dark laminated dololutites (B2) matrix, suggest that most of these deposits suffered little, if any transport. The rounded edges of many clasts do not The landscape between the village and Praia a contrast with this assumption in that they may have been Mare is dominated by deeply eroded hills, mostly consist- inherited from the bioconstruction shape itself and/or ing of black, finely bedded and heavily cataclastic dolomites. indicate fragmentation of scarcely lithified materials. Some good observations have been performed on various In some cases, particularly in the outcrops of Bocca segments of the stratigraphic successions, outcropping della Cappella, the boundstones form blocks some meters along the road from Praia to Aieta. Similar lithologies large. Probably, these large boulders were deposited as occur a!so in the Papasidero and areas, some tens single, loose blocks derived from nearby in-situ biocon- of kms south-east. structions. However, some very large boundstone blocks The succession is organised in half to two m-thick from the same locality probably represent single in-situ beds of coarse doloarenites, alternating with dark beds of buildups, not only because of their large size, but also much finer detrital dolomites (PI. 15/1). Slumps and because their lower contact does not deform the underly- slump-breccias are quite frequent (Pl. 15/3,5). ing, laminated sediments (as detrital boulders should do). The coarser beds have sharp, erosional lower contacts, The lack of lateral continuity in the outcrop made with occasional evidence of reworking of the substrate in often difficult such investigations; nevertheless, we are the lower part of the same beds. A broad grading of the quite confident that most of the outcrops found at Bocca deposit is observed, the upper part being finer graded (PI. della Cappella and on the southern flank of Serra di 15/2,4). The bioclastic components include mainly thin Castrocucco represent in situ bioconstructions whereas shelled bivalves, as well as gastropods, crinoids, serpulids, many breccia deposits of the surrounding areas formed dasycladaceans (Griphoporella curvata), foraminifers very close to the site where the buildups grew up. (Aulotortus sinuosus WEYNSC~mt~,Agathammina austro- Most breccia deposits (western Serra di Castrocucco, alpina K~STAN-Tot~MArCN,Variostoma sp., Endoteba sp., lower part of Bocca della Cappella, Monte Cifolo) are 'Trochamminidae', Ammodiscidae) and microproblem- intercalated with graded bioclastic, coarse to fine atica. Some beds provided an interesting coral-rich fauna doloarenites. These are organised in bed-sets some dm- to (CLIMACO, 1994), including Pinacophyllum sp., Disticho- few m-thick, composed of several doloarenite levels, with phyllia sp., Coryphyllia sp. and Retiophyllia sp. an erosional lower boundary and grading up into dark These beds are intercalated with dark, well bedded mudstone. The bioclasts are frequently represented by organic-rich dolomites. The single beds are 1 to few cm- thin, single bivalve shells, less than 1 cm long. More thick and consist of bioclastic, fine-graded doloarenites. often, undifferentiated skeletal debris is observed. In the The lower limit is generally sharp, whereas the upper one latter facies slumps and slump-breccias are very frequent, grades into darker dololutites. with sometimes clasts of the laminated doloarenites scat- tered in the breccia bodies. 5.6 Dark laminated dololutites (B3) In a few cases (upper part of Serra of Castrocucco section and upper part of Bocca della Cappella sections) South of the Praia a mare village (in the localities of S. the breccias are associated to massive beds of grey micro- Nicola Arcella beach, Fiuzzi, La Mantinera and Isola di

Plate 13 Upper Triassic carbonates of Verbicaro Unit (Lucania and Calabria, Southern Italy). Microfacies of the clasts of the brecciated or resedimented buildups. Norian. Fig. 1. Biogenic framework with serpulids surrounded by thrombolitic microbial matrix. The irregular, intraframework cavities are filled by isopachous cement crusts. Bocca della Cappella. Sample AC 535. x3 Fig. 2. Bafflestones with a large amount of serpulids encrusted by microbial laminae. Bocca della Cappella. Sample AC 536. x 10 Fig. 3. Thrombolitic-peloidal boundstone with serpulids. Bocca della Cappella. Sample AC 547. x 4.5 Fig. 4. Oncoidal microbial crust surrounding serpulids. A stage of organic encrustation after oncoid formation is evident, followed by the precipitation of dolomitic isopachous cement fringes. Bocca della Cappella. Sample AC537. x 1.7 Fig. 5. Detail of serpulids surrounded by microbial crusts. Bocca della Cappella. Sample AC 74. x 15 Plate 13 47 48

Dino), the doloarenites become much less frequent in the 7 THE DEPOSITIONAL MODEL dark dolomites. The successions are here dominated only by the finer and more organic-rich sediments. Mudstone Our tridimensional model for the depositional setting and wackestone with faint grading are the prevailing of the facies types is presented in Fig. 4. It is based mostly lithofacies. Locally, some marly, brown weathered levels on the geological section of Fig. 3. We believe that in this or thin carbonaceous seams are present. section, even considering offsets due to alpine tectonics, As in the case of the previous facies, the thickness of the former Triassic facies relationships are still preserved. these successions is difficult to assess, but at least two However, it must be emphasised that the proposed hundred meters of these dark, fine-grained carbonates model is heavily influenced by those made in Southern outcrop around San Nicola ArceUa. Alps by JAootrL et al. (1992) and TRor,mzr'rn & BOTTOm (1993). In these areas similar facies are found which, because of a milder tectonic shortening, are still organised 6 BIOSTRATIGRAPHY after their original depositional setting, thus allowing a AND CORRELATION CRITERIA more reliable interpretation of the basin dynamics. The Norian-Rhaetian biostratigraphy of platform car- In the followingchapters we will discuss the depositional bonates is based on the algae and foraminifersbiozonation. model, developed from our data, and organized for two The main foraminifers generally quoted in the platform time slices, in accord to the poor stratigraphic resolution carbonates of the Tethys realm belong to the Aulotortidae allowed by the foraminifers biostratigraphy: Norian and and Ammodiscidae family (ZA~ar~-'n, 1976; PILLER,1978; Upper Norian-Rhaetian. GAZDZICra, 1983; POISSONet al. 1985; SALAJet al. 1988; DE CASTRO 1990; KAMOUN et al., 1994; ZA~,a'A~LLIet al., 7.1 Norian 1995). Only the appearance of Triasina hantkeni allows to identify the Upper Norian-Rhaetian (MARCOtJX et al., The Norian depositional system is well constrained by 1993). the available data. In fact, both dasycladacean-dolomite Among dasycladacean algae, one of the most common and microbialites-bearing breccias can be dated as Lower- in the Norian-Rhaetian stage is the Griphoporella curvata Middle Norian because they are found below the Triasina (GOMBEL) (PI. 11/7). hantkeni-bearing Megalodontid limestone. Moreover, The presence of Poikiloporella duplicata Pin (PI. 16/ comparable breccia bodies are found intercalated within 12,13), a Ladinian-Carnian species (GRANIER& DELOVV~E, dolomitic turbidites, while all the resedimented dolomites 1994), (generally reported in association with Clypeina become gradually finer grained toward the SSW, the besici PAnaac in the Carnian limestones, OaT 1967, 1972) finest sediment being represented by the dark dolomicrites in the lower part of the Monte Rotonda succession, in of Fiuzzi. Thus, these deposits can be reasonably dated as association with Griphoporella curvata,Aulotortus sinuosus Norian, too. andA.friedli (an assemblage typical of Norian-Rhaetian The lateral interfingering of all these facies can be stages), raises some problems. According to this datum, easily explained as corresponding to the transition from the range of P. duplicata should be extended to the the platform edge to the basin. Particularly, as we will Norian, but further research is in progress on this point. discuss below, while the algal dolomites represent the The correlations between the various dolomitic inner margin sediments, the breccia bodies and the turbidites successions are based, above all, on the presence of correspond to the upper and middle-lower ones, and the Triasina hantkeni (facies assemblage A2). This foramini fer, laminated micrites to the basinal deposits. in associations with Aulotortus sinuosus and Griphoporella curvata, has allowed to refer to the Norian-Rhaetian the 7.1.1 Algal and bivalve dolomites association of facies A2. The stratigraphic superposition of the Triasina hantkeni The algal and bivalve dolomites and related facies -bearing facies A2 over both the platform dolomites (A 1), represent typical peritidal platform sediments arranged in and the slope breccia facies at Serra di Castrocucco (B 1), cyclical patterns. We have already pointed up (IANN^CEet has allowed to refer these facies assemblages to the al., 1994) that they formed in the inner marginal area. This Lower-Middle Norian. earlier inference can be confirmed here, based on the

Plate 14 Upper Triassic carbonates of Verbicaro Unit (Lucania and Calabria, Southern Italy). Sphinctozoan sponges. Fig. 1. Polished slab showing little sphinctozoan sponges surrounded by microbial crusts with laminated to thrombolitic texture. La Spartosa. Scale in centimetres. Fig. 2-3. Thin sections showing the same structure as Fig. 1. La Spartosa. Samples AC 73 and AC 75. x 1 Fig. 4. Dense bafflestone with serpulids (bottom) and little sphinctozoan sponges. Bocca della Cappella. Sample AC 75a. x 1 Plate 14 49 50

Dsycladacean beds microbial reef debris turbidites mounds talus flow

tepees \

a--, -..< \

INNER UPPER MIDDLE MARGIN SLOPE SLOPE

Fig. 4. Schematicpaleoenvironmental interpretation of the studied facies for the Norian age (from CL~^co, 1996). following evidence: dolomites marked the presence of a periodically emergent a) the closeness to coeval bioconstructed marginal shelf break. IANnACE (1993) also emphasised the abun- facies (at Serra di Castrocucco); dance of synsedimentary cements as an evidence of close- b) the prevalence of high energy microfacies (coarse ness to the open sea. Particularly, he suggested, following skeletal grainstone and packstone); I-IANFORD et al., 1984, that a mechanism of sea water c) the presence of mega-tepees and abundant syn- pumping from the open sea through the barrier into the sedimentary dykes in part of the succession. inner margin domain could be claimed to explain both Considering the point b), we think that the dasycladacean- tepees and cements formation. rich dolomite facies, characterised by the scarceness of Another observation made by IANNACE (1993) is the interparticle mud with respect to the amount of microbial presence of at least two main cement generations. The crusts and fibrous cements, represent shoal barrier depos- first is represented by non-isopachous crusts formed early its. We have never noticed cross stratification to prove during tepee formation; the second, clearly cross-cutting this latter statement, but this could be simply an effect of the first one, is represented by botryoidal cements. the large size and shape of the algal thalli, which does not Observations made along the road cut in the lower part help in recognising such sedimentary structures. of the Noce river valley have shown that this cement The significance of Upper Triassic tepee-bearing generation is clearly related to a fracture network which dolomites as an indicator of inner margin paleoenvironment cut across several meters of bedded succession. The was already discussed by IANNACE (1993). In that paper, resulting ,,cement dykes" quite clearly start as vertical mainly based on successions studied 200 km to the north features but can also propagate horizontally along suit- (Lattari mountains), it was hypothesised that Norian tepee able bedding planes.

Plate 15 Upper Triassic carbonates of Verbicaro Unit (Lucania and Calabria, Southern Italy). Slope facies. Norian. Fig. 1. Laminated, dark beds of coarse to fine doloarenites alternating with light coloured bioclastic dolorudites, Papasidero. Fig. 2. Thin, graded bioclastic beds alternating with organic-rich, laminated ones. Papasidero. Coin r is 2.3 cm. Fig. 3. Slump breccia and debris flow in the black laminated intervals of B2 facies. Bocca della Cappella. Fig. 4. Thin section, showing faint direct grading, sampled in the finer, organic rich levels of the outcrop in Fig. 1. Papasidero. Sample AC46. x 5 Fig. 5. Slumping in the laminated slope deposits. Road to Aieta. Fig. 6. Graded, laminated doloarenites with evidence of sliding (little reverse faults) and mass-flow resedimention. M. Cifolo. Plate 15 51 52

Thus, it can be confidently stated that this phenom- nity (FAGERSTROM,1987). The absolute dominance of enon largely postdates tepee generation and was obvi- these organisms in the bioconstructions of Northern Ca- ously related to tensional fractures cutting a relatively labria, suggests that important environmental stress fac- well lithified platform margin. These fractures were ge- tors were present in the paleoenvironment during their netically linked to the faulting of the shelf break and the growth. When ambient conditions are unfavourable to the onset of basin formation. The absence of such features in development of a well differentiated reef community, the overlying Rhaetian, in fact, restricts their age range to opportunistic species, like serpulids, can develop in anoma- the Norian. lous large amount, during limited period of more favour- The dolomite succession of Serra Vingiolo, which able conditions. The sporadic presence of small sized lacks any tepee and related cements, while showing typi- sponges is another evidence of such limiting conditions. cal planar stromatolites and lower energy microfacies, The existence of restricted conditions in the sedimentary can be ascribed to a more internal, resmcted platform suc- basin is also suggested by the high organic matter content cession. In this respect, it is significant to remember that of the associated slope to basin sediments. CORTESE (1895) correctly stated that only the dolomites of We believe that these buildups grew in the outer Praia d'Aieta (i.e. the Serra Vingiolo dolomites) can be margin/upper slope area, the inner platform margin being actually compared to the Dolomia Principalefacies, whereas occupied by the tepee belt. We base this conclusion on the all the other dolomites of the region should be correlated following elements: to the Dolomia Principale stage. Quite obviously, he was - the association, at Bocca della Cappella, of in situ well aware that all the other dolomites had a different facies! bioconstructed facies with resedimented, dark dolo- arenites; 7.1.2 Bioconstructed facies - the frequent intercalation of the boundstone talus breccia with turbiditic layers; The margin of the basin was colonised by peculiar - the scarcity of cements in the boundstone, respect to bioconstructions dominated by microbialites and serpulids, those found in the algal/bivalve facies ; as witnessed by the boundstone found as resedimented - the absence of subaerial exposure evidence neither in the loose blocks or as debris flows. Sponges were much less boundstone blocks themselves, nor in the associated frequent and always of little size respect to those abundant marginal facies; in the Norian-Rhaetian reef of the Alps (SENoWB:mX- - the upward evolution of the talus breccia of Monte DARYAN, 1990). Corals have been found only in some Cifolo to bioclastic, wavy laminated dolomites, indicat- turbiditic beds and in the platform margin, tepee-bearing ing deposition near the wave-base level. facies. They never occur in association to the microbial- These bioconstructions probably formed low relief serpulid-sponges assemblage. mounds located in the upper part of the slope, probably The collected evidence shows that the bioconstructions below or around normal wave base level. However, as were characterised by a low diversity biota largely domi- they did not include organisms able to make strong wave nated by microbial organisms, probably cyanobacteria. resistant structures, were easily broken by major storms. The most significant metazoan faunistic group is repre- This is probably one of the reasons why only few evidence sented by serpulids. In Upper Triassic reefs of the Teth yan of in situ bioconstruction have been found. and Pacific areas, and in most Phanerozoic reefs, these However, we believe that only some examples of taxa are secondary guild components, playing the role of breccias (Bocca della Cappella) can be interpreted as the binders and encrusters within a well diversified commu- product of such kind of physical deconstruction. Indeed,

Plate 16 Upper Triassic carbonates of Verbicaro Unit (Lucania and Calabria, Southern Italy). Foraminifers and dasycladaceans Fig. 1. Triasina hantkeni MAJZON.Upper Norian-Rhaetian. Serra di Castrocucco. Sample AC 30. x 40 Fig. 2. Aulotortus sinuosus WEYNSCr~rnC. Norian. M.Rotonda. Sample AC 344. x 45 Fig. 3. Aulotortus sinuosus W~YNSCH~rK.Norian. M. Rotonda. Sample AC 344. x 45 Fig. 4. Auloconus permodiscoides OBERHAUSEa. Upper Norian-Rhaetian. M.Rotonda. Sample AC 469. x 42 Fig. 5. Endotriada cf. tyrrenica VACHARD, MARTINI,RETTOaI & ZANINZrTI.Norian. M.Rotonda. Sample AC 43. x 50 Fig. 6. Endoteba ex gr. controversa VACHAP,D & RAZGALLAH.Norian. Monte Rotonda. Sample AC 43. x 55 Fig. 7. Autotortus sinuosus W~scrmrcK Norian. M. Rotonda. Sample AC43. x 38 Fig. 8. Endoteba sp. Norian. Aieta. Sample AC 170. x 50 Fig. 9. Variostoma sp. Norian. M. Rotonda. Sample AC 43. x 30 Fig. 10. Agathammina sp; Norian. Road to Aieta. Sample AC 170. x 50 Fig. 11. Gandinellafalsofriedli SALAJ,Bogzh & SAMUEL.Norian. M.Rotonda. Sample AC 469. x 45 Fig. 12. Poikiloporella duplicata (PIA) Norian. M.Rotonda. Sample AC 343. x 5 Fig. 13. Packstone with Poikiloporella duplicata (PtA). In association Griphoporella curvata fragment of other dasycladaceans and aulotortid foraminifers. Norian. M.Rotonda. Sample AC 345. x 4 Plate 16 53 54 the large size of the clasts and the elevated thickness of the assemblage is concerned, some constraints could arise brecciated facies suggest that most of these deposits when using sequence stratigraphy criteria for correlation. originated during ,,pathologic progradation" (Bos~tarn, In fact, in the Serra di Castrocucco log (Fig. 2), we notice 1989), i. e. as the accumulated debris at the toe ofdownfaulted that Megalodontid limestones follow upper slope breccias. margin. This conclusion, which is mainly drawn by facies This might be an indication of a regressive trend, probably comparison with the already quoted examples of the Alps related to the progradation of the platform, in turn driven (JADOtrL et al., 1992), seems also supported by lateral by a high-stand of relative sea level coupled with a facies change over a short distance at Serra di Castrocucco. slowing of tectonic subsidence. The same trend is present Here, alternating breccias and stratified finer resediments, in the section of Monte Cifolo where the breccia beds are found at the north-west side (Fig. 2), make transition to a followed by fine bioclastic dolomites characterised by thick and monotonous accumulation of only coarse breccias wavy lamination, then followed by A3 facies assemblage, on the southern side. which contains stromatolitic and pisolitic intervals. Direct evidence of synsedimentaryNorian paleofaults Thus, this evidence would suggest a correlation be- is lacking. However, the cement filled dykes found at the tween the Megalodontid limestones and the dololutites base of the Monte Rotonda succession (PI. 11/1) can be and stromatolitic/bioclastic dolomites (A3) of Monte Cifolo. considered an evidence of tensional fracturing of the Actually, the dasycladaceans- and foraminifers-bearing platform margin during the time of slope formation fur- beds of Monte Cifolo A3 dolomites are very similar to the ther to the south. Megalodontid limestones and dolomites, except in that they lack the Triasina hantkeni specie and the large 7.1.3 Slope and basin facies bivalve shells. Considering that the microfacies indicate low hydrodynamic energy, the absence of T. hantkeni Along the slope, in a distance which can be estimated could be only due to unsuitable environment. in 5 or 6 kin, the coarse breccias give way to coarse The resulting paleoenvironmental scenario would im- turbidites, then to finer turbidites and finally to the dark ply a wide shallow shelf characterised by Megalodontid micrites of Fiuzzi. The laminated texture and the high prairies alternated to areas of sandy bioclastic transport. organic matter content of the latter facies quite obviously In the platform areas of eastern Alps this facies has been point to a basin with poorly oxygenated bottom waters. interpreted as formed in near back-reef areas (FxscrmR, In the upper part of the slope, debris flows alternate 1964). However, in the case of Northern Calabria, due to with turbidites, particularly in the Serra di Castrocucco poor biostratigraphic control, no definite evidence of a section. Following some current sedimentary models, this coeval barrier exists. Thus, the alternative interpretation could be ascribed to sea-level oscillation. However, it of an open shelf, probably with a very gentle slope, cannot must be observed that, as the bioconstructed facies did not be ruled out. developed as a continuous barrier, the alternation of coarse and finer facies could be due at least in part to the wandering of the bioconstructed sites, which feeded in 8 CONCLUSIONS turn the coarse detrital deposits, throughout the outer marginal area. The presence of a well structured basinal trough in the Lacking any direct evidence of a well-shaped paleoslope, Norian of Calabria and in part of Lucania (Southern Italy), any attempt of depth estimate would be only speculative. represents a new achievement. Up to the recent past, the However, considering the possible short distance in which Upper Triassic outcrops in this region were interpreted as the platform-to-basin transition was achieved, and the indicative of shallow water, mainly tidal sedimentation. absence of true mega-breccias, the depth of the corre- We can now state that most of the Upper Triassic through- sponding basin should not have exceeded several tens or out this region was deposited in a slope-to-basin environ- few hundreds of meters. ment. In fact, even though we have restricted our analysis to the ~caille de Praia d Mare to avoid miscorrelation with other successions belonging to different tectonic slices 7.2 Upper Norian - Rhaetian (e.g. Papasidero, Grisolia, Mormanno outcrops), we can The reconstruction of the uppermost Triassic paleo- state that also in the latter areas, similar sediments occur. environments raises some problems. In fact, as explained This imply either that the basin was even larger or that above, this geochronologic interval can be truly recog- more than one single through existed within this area in nised only where back-reef, Triaswina hantkeni -bearing Upper Triassic time. Only a careful tectonic analysis limestones are found, i.e. in the platform successions. could solve this point. We have no direct evidence to ascribe to this time slice Similar platform to basin facies have been recently part of the resedimented breccias and turbidites of Aieta described by IEyro et al. (1995) more to the south, at area, which are cut by multiple shear planes. As a conse- Monte Cocuzzo. Thus, from the Monti Lattari (IArCSA~, quence, we cannot objectively assert that the basin-to- 1989; 1993) and Monti Picentini (Born et al., 1990) to the platform system of Norian age persisted also in uppermost north, to Monte Cocuzzo to the south, there is growing Norian and Rhaetian ages. evidence of Norian basin formation. As far as the stratigraphic position of the A3 facies In all the quoted districts the basinal sediments are 55 characte.rised by high organic content and, with the excep- Buonabitacolo (Soleno, Campania). - In: B ARATTOLO, F., D~ tion of Monte Cocuzzo, by margins colonised by microbialite CASTRO, P. 1~ PARENTE, M. (eds.) (1991): 5th International Symposium on Fossil Algae, Capri (Napoli), Field Trip crusts and serpulids with only minor sponges. These Guidebook., 80-90, 2 Pls., 2 Figs., Napoli sedimentary and paleoecological features match well with BARBIERI , M., DE Vlvo, B., PERRONE, V. & Ttmco E. (1984): those found in coeval intraplat form basins of the Dolomia Strontium Geochemistry of the San Donato Unit barite Principale and equivalent facies in Southern Alps (JAI~W_, mineralization (Calabria, Italy). - Chem. Geol., 45, 279- 1985; TROMBETTA • BoTror,a, 1993; BERRA & JADOUL, 288, 4 Figs., Amsterdam BERRA, F. & JAOOtJL,F. (1996): Norian Scrpulids and microbial 1996) Central Apennines (CmmI~, 1993) as well as in bioconstructions: implication for the platform evolution in Alpujarride, Southern Spain (MARTIN & B~GA, 1987). the Lombardy basin, Southern Alps, Italy. - Facies, 36, Particularly, the peculiar type of microbial/serpulid Erlangen bioconstructions is different from the classic Norian reefs BIGI,G., COSENTINO D., PAROTTO, M., S ARTORIr R., SCANBONE, P., described in the Alps since the middle of last century (and (eds.) (1991): Structural model of Italy. - Quaderni de La Ricerca Scientifica,14,9 maps, Roma(Cons. Naz. Ricerche) then in Sicily) and generally referred to as ,,Dachstein BONI, M., IANNACE, A., KOSTER, J., PARENTE M. (1990): Anoxic reef'' (see FL~3GEL, 1982). Facies in the Upper Triassic of Picenfini Mountains (South- This dichotomy suggests that a strict paleogeographical ern Apennines, Italy).- Boll. Soc. Geol. Ital.,109, 171-185, control existed, during the Norian, on the growth of reefal 6 Figs., Roma associations. The Dachstein-type reefs correspond to well BOSELLINt, A. (1989): Dynamics of Tethyan carbonate plat- forms. - Soc. Econom. Paleontol. and Mineral. Spcc. Pub., diversified communities colonising the margins of the 44, 3-13, 13 figs., Tulsa platforms flanking open marine basins. On the contrary, BOSELLINI,A. & BROGUo-LORmA,C. (1965): Gli S trati a Triasina the microbial-serpulid reefs of Calabria, similarly to those del Gruppo del Sella. - Mem. Geopaleont. Univ. Ferraxa, 1- of the Alps, Apennines and Spain, are associated to 4, 1 Fig. suboxic to anoxic restricted intraplatform basins, as BOUSQUET,J.C. & GRANDIACQUET,C. (1969): Structure de l'Ap&min Calabro-Lucanien (ltalie mdridionale). - C. R. Acad. Sc., evidencedby the laterally equivalent organic-rich sediments 268, 13-16, 3 Figs., Paris (ZArCa'ARELLtet al., 1996). BURTON,A.N. (1971): Carta Geologica Della Calabria 1:25.000. Altogether, these evidence suggests that in the Norian Relazione Generale, Cassa Per I1 Mezzogiorno, Servizio time both Southern Alps and Apennines experienced a Bonifiche, 120 p, 48 Figs. Roma very similar tectonic evolution and comparable pale- CIRmLI, S. (1993): I1 Trias di Filettino-Vallepietra (Appennino Centrale) - Boll.Soc.Geol. Ital., 112, 371-394, 19 Figs., Roma oceanographic conditions, characterised by the formation CIVITAM., (1964): Osservazioni geologiche sui Monti di Maratea, of numerous intraplatform throughs with restricted circu- Lucania meridionale. - Mere. e Note Ist. Geol. Applic. lation, this influencing the bottom conditions as well as Napoli, 9, 1-24, 5 Figs., 1 Geol. Map, Napoli the marginal communities. The understanding of the dy- CLIMACO, A. (1994): Upper Triassic (Norian-Rhaetian) coral namics of these organic-rich facies and related microbial/ fauna in the Verbicaro Unit (Northern Calabria, Southern Italy). - Studi Trentini Scienze Naturali, 69, 51-59, 2 Pls., 1 serpulids communities, is presently in progress (ZAMPARELLI Fig.,Trento et al., 1996). It may provide important clues to the paleo- CLIMACO,A. (1996): Analisi sedimentologico-stratigrafica delle geographic reconstructions of shallow western Tethys by successioni carbonatiche del Trias superiore, affioranti in putting paleoceanographic constraints on the envisaged Lucania (Monti di Maratea) e nella Calabria settentrionale. scenarios. Moreover, it represents an important challenge - Unpublished Tesi di Dottorato di Ricerca, Universit~ di Napoli, 137 p., 23 Pls., 37 Figs. also in terms of oil exploration, when considering the CORaXSE, E. (1895): Descrizione geologica delia Calabria. - importance of Upper Triassic organic-rich dolomites as Mem. Descrittive Carta Geol. d'hal., 9, 510 p. Roma. source rocks for the Italian region (MA'Iq'AVELLI& NOVELLI, DAMIA~a,V. ( 1970): Osserv azioni geologiche in alcune tavolette 1990). del F~ 220 della Calabrianord-occidentale. Parte I: Stxatigrafia. - Boll. Soc. Geol. Ital., 89, 65-80, 7 Figs, Roma D'ARGENIO, B.(1966): Stromatoliti Triassiche della Calabria ACKNOWLEDGEMENTS Settentrionale - Mem. Soc. Geol. Ital., 75, 279-299, 10 Figs., 4 Tab. Napoli This work, which partly represents the Ph.D thesis of D'ARGEr,rIO, B., PESCATOP.E,T. & SC.ANt~t,m (1973): P. Schema A. C., was realised with CNR grant CTB 93.02141 CT05 geologico dell'Appermino meridionale (Campania e Lucania). to M. B. and MURST grants 60% to M. B. and V. Z. Thanks - Atti del Cony.: 'Moderne Vedute sulla geologia dell'Ap- are due to B. Senowbari-Daryan and an anonymous re- pennino', Ace. Naz. Lincei, Quader., 183, 49-72, 5 Figs., 1 Tab., Roma viewer for some helpful suggestions. All the pictures have DE CASTRO, P. (1988): I1 Triassico delle Croci di Acerno in been printed by D. Fiorentino at our Department. Provincia di Salerno. - Atti 74 ~ Congr. Soc. Geol. Ital., Sorrento (Napoli), Italia, 13-17 seUembre: A239-A244, Napoli REFERENCES DE CASTRO, P. 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