Rivista Italiana di Paleontologia e Stratigrafia YOlUme lUJ numero 2 tavole 1-2 pagrne 173-1,82 Settembre 1997 CONODONT BIOSTRATIGRAPHY OF THE LATE TRIASSIC SEQUENCE oF MONTE COCUZZO (CATENA COSTIERA, CALABRIA, ITALY) ADELAIDE MASTANDREA*, FABIO IETTO*+, CLAUDIO NERI*** & FRANCO RUSSO**** Key-uords: Catena Costiera Calabrese, Basin deposits, Cono- donts. Norian. Rhaetian. Riassunto. Nel presente lavoro sono riponati i risultati preli- minari di uno studio biostratigrafico, basato sui conodonti, dei terre- ni carbonatici triassici della Catena Costiera Calabrese, affioranti nel- la finestra tettonica di Monte Coctzzo. La successione studiata (Colle del Crapio) si è depositata in contesti di piede scarpata/bacrno ed ha fornito faune a conodonti ricche e ben presenate. Sono riconoscibili due biozone: la prirna, nella pane inferiore-media dell'unità, è marca- 'ta dt EpigondoleLla slwahensis e può essere riferita al Norico supe- riore (Sevatiano); la seconda è caratterizzata da MisikelLa bernsteini, in associazione con M. postbernsteini, ed ha un inquadramento cronostra- tigrafico pir\ controverso. Secondo Krystyn (1990) e Golebiowshi (1990) potrebbe essere riferita al Sevatiano sommitale (Norico supe- riore), mentre per Kozur 6c Mock (1991) Ia comparsa di M posthcrnsrcini rndicherebbe il passaggio al Rerico. Abstact. Preliminary results are reponed from rn investiga- tion of the conodont associations found in the Late Triassic carbona- te succession of the so-called "Catena Costieru Calabrese" that crops out in the tectonic window of Monte Cocrzzo. The succession of Colle del Crapio consists of alternating carbonate mud, breccia and calciturbidites deposited in a toe-of-slope to basin setting and con- tains rich and well-preserved conodont faunas penaining to two bio- zones. The iower zone is characterised by the occurrence o{ Epigon- doleLla sloz,ahensls and may be referred to the Late Norian (Sevatian). The upper zone is characterised by Misikella bernsteini associated wrth M. postbernsteinì. The chronostratigraphic setting of the latter zone is more controversial, as it may be regarded as latest Sevatian (Upper Norian) according to Krystyn (1990) and Golebiowski (1990), while according to the zonation of Kozur 6c Mock (1991) the first occurrence of M, postbernsteini marks the beginning of the Rhaetian stage. Introduction. This paper is the first contribution on conodont stratigraphy of the Late Triassic succession cropping our in the so-called Monte Cocuzzo tectonic uindotu Auct., pertaining ro the "Catena Costiera Calabrese" and loca' ted west of Cosenza. The succession, mainly consisting of strongly do- lomitized carbonate rocks, has been interpreted by Amodio Morelli et aI. (1976) as a rracr of the African margin of Apulia, cropping our as a recronic window below the thrust sheets perraining ro rhe "Calabrian (Calabridi) units" (Ogniben, 1969). The stratigraphic section studied .was measured and sampled near Colle del Crapio (Fig. 1). The section is 73 m thick, including the upper part of rhe "Interme- diate Complex or Monte Cocvzzo Complex" and the lower part of the "Upper Complex or Colle del Crapio- Valle delle Pernici Complex" of Ietto et al. (1995) (Fig. 2). Observations on the same stratigraphic interval were also made in a quarry on the southern slope of Monte Cocuzzn (Fig. 1). The little data on the age of this succession availa- ble to date were based on benthic fossils, such as the dasycladacean green alga Griphoporella cuntata (Giimbel, 1972) Pia, L915, occurring in the Upper Complex of Colle del Crapio (Ietto et aI., 1993) and referred to the Late Triassic (Norian-Rhaetian) (Barattolo et al., 1993). The finding of a rich conodont fauna in the sec- tion studied allows more accurate biostratigraphic da- ting. Two distinct conodont biozones were recognized within the relatively thin interval sampled. The stratigraphic section Lithostratigraphy and sedimentology. The stratigraphic section studied (Fig. Z) inciudes, from a lithostratigraphic view point, the upper part of the "Intermediate Complex" and the lower part of the "Upper Complex" of Ietro et al. (1993; 1995). 'f Istiruto di Paleontologia, Università di Modena, via Università,4, I-41100 Modena. 'f" Dipanimento di Scienze della Terra, Università Federico II, Largo S. MarcelLno, 10, I-80138 Napoli. ',"" Dipanimento di Scienze Geologiche e Paleontologiche, (Jnrversità di Ferrara, C.so Ercole I d'Este,32, I-44100 Ferrara o'r+* Dipartimento di Scienze della Terra, Universirà della Calabria, I-82030, Arcavacata di Rende (Cosenza). 174 A. Mastandrea, F. Ietto, C. Neri & F. Russo Intermediate Complex. The Intermediate Complex (52 m, excluding a not precisely determinable lower tract of the complex) con- sists mainly of dark grey to blackish dolostone with mi- nor marly interlayers. The main iithofacies are as fol- lows. a - Black dolomicrite with minor thin (mm- to cm-thick) fine-grained, graded dolomite intercalations, interpreted as fine, distal or starved, turbidites embed- ded into basin lime mudstone. b - Coarse grained dolostone, deriving from the dolomitization of a calcarenite and a fine breccia, for- ming individual beds 3-4 ro 30-40 cm thick, with erosio- nal base, normai grading, even lamination and, occasio- nally, current ripples. These beds are interpreted as tur- bidites (usually T"6); they are either amalgamated or se- parared by centimetre-thick dolomicritic interlayers. The grains are usually too deepiy recrystallized to be recogni- zable; however, in some rare case, bioclasts such as dasy' clads (Gryphoporella sp.) or fragments of microbialitic boundstone can be observed. Calabrian (Calabridi) crystalline-metamorphtc units Carbonate complex Border of lhe lectonic window Sampled outcrops : a. Colle del Crapio seclron b. quarry south of M. Cocuzzo Fig. 1 A, Location map of the area studied; B, Structural units and location of the ourcrops sampled. c - Doiomitic breccia, mainly with flat clasts, for- ming beds ranging in thickness from 50-60 cm to 2-3 m; clasts are mainly represented by tabular fragments of beds, 1-5 cm thick and 20-50 cm wide. They consist both of basinal dark dolomicrite (lithofacies a) and of calciturbidites (ithofacies b); platform-derived clasts are more rare, usually smali in size (4-5 cm) and consist of microbialite boundstone (stromatolitelike laminite with associated skeletal cyanobacteria and encrusting forami- nifers). The breccia bodies show quite different degrees oÍ organization, ranging from chaotic mud-supported deposits (mud flows) to normal-graded, clast-supported beds capped by laminated doioarenite (turbidites). Late- ra1 and vertical transition between siumped beds and flar pebble breccia is frequent. These lithofacies are frequently organized into coarsening-up sequences, mainly made of facies a and b, or, more rareln into fining-up sequences. The intervals dominated by flat clast breccia do not show any defined organisation. Moreover, the tract of the Intermediate Complex studied does not show a clear vertical evolu- tion, although an upward increase in the amount of breccia occurs. The frequent occurrence of slumped ho- [] [l *-:::1 r v :Fiurnefreddo :=:= î------------j** Gririard X ! a) U X J U F o F z Conodont biostratigraplry of Monte Cocuzzo : 'z- - 175 .cc l0 .cc9 .CC 8 . CC 5 .CC 48 .CC 4A oCC 4 - 2_ o CC 1 rizons and chaotic deposits consisting of tabular slabs derived from slope deposits in the upper part of the unit may indicate a pronounced slope instability, proba- bly due to synsedimentary tectonics. Upper Complex. Only the lowermost paft of the Upper Complex (20 m) was investigated. This unit is very poorly expo- sed, due to the abundance of marls intercalated in the succession. Outcrops consist of dm-thick blackish dolo- mite, represented by both dolomitized mudstone and calciturbidites, and of yellow to grey dolomitic marls. Poor exposure makes facies analysis and paleoenviron- mental interpretation difficult, but according to the avai- lable data the overall depositional setting indicates a ba- key Fig. 2 - Colle del Crapio stratigraphic sectton. Key: 1) dolostone; 2 and 3) marly dolostone and dolomitic limestone; 4 and 5) fine-grained doloarenites; and dolomitic calcarenites; 6 and 7) coarse-grained dolostone and dolomitic limestone; 8 and 13) dolomitic breccia with platy laminated clasts; 9 and 18) dolomitic breccia with marly clasts; 1O) alrerna- ting lithologies; 11) marls; 12) slumped deposits; 14) thin turbidites; 15) coarse amalga- mated turbidites; 16) carbona- te mud (possibly dolomiti- zed); 17) marlylpelitic mud; 19) slump; 20) erosive surface; 21) normal grading; 22) even lamination; 23) small scale crosslamination; 24) covered interual; 25) sample. sinal environment. The unit records a marked reduction in the carbonate gravitational sedimenration and an in- crease in pelite input. Biostratigraphy. The Conodont fauna. Nine samples, with a minimum weight o{ 7 kg, were collected in the Coile del Crapio section. Six were obtained from the Intermediate Complex and three from the Upper Complex (Fig Z). Two additional sam- ples collected from ^ qu rry south of Mr. Cocuzzo, ar the boundary between the Intermediate and Upper Complex, were consistent with the data from Colle del 25 24 23 22 21 20 19 18 17 16 15 - -) a LO L/ O A. Mastandrea, F, Ietto, C. Neri G F. Russo Rarniform elements of conodonts in the Colle Crapio. Four samples taken from the underlying Lower Complex (Serra Mezzana) yielded large mono-specific collections of Epigondolella slwakensis. All the samples from Colle del Crapio were col- lected from black dolomicrites, quasi-stoichiometric and very rich in organic matter (Russo F. et ai. in prepara- tion), with thin graded intercalations interpreted as fine turbidites. The samples yielded a very rich conodont fauna, well preserved as single elements or less frequen- tly as clusters. Conodonts showed a colour alteration in- dex (CAI) of 5 (Epstein et al. 1.977). Conodont occurrences and vertical ranges are gi- ven in Fig. 3. Discussion. Fauna 1 - Samples CC1 to CC5 from Colle del Crapio (Fig. 3) yielded a rich monospecific conodont assemblage exclusively containing specimens of Epigon- dolella slwakensis (Kozur) emend. Budai & Kovacs, 1986 (Fig. 3). This species is very abundant (approximately 530 platform elements and some clusters) and well pre- served. Mostly broken specimens of ramiform elements (i..., prioniodiniform, enantiognathiform, hideodelli- form, and hibbardelliform) of the apparatus were also found. Budai Er Kovacs (1986) and Kovacs & Nagy (1989) reported the presence of Epigondolella slwakensls from the Rezi Dolomite Formation of Keszthely Mts. and Fe- kete-hegy Limestone Formation ("Avicuia limestone") of Pilis Mts. in the Balaton Highland (Hungary) where it ranges from Upper Alaunian to Sevatian. The E. slwa' kensis population described by these authors includes elements with great morphological variability, similar to those observed in the Colle del Crapio fauna. Orchard (1,983, 1,991) recognised a significant mor- phological variety in the Epigondolella population of the Norian of British Columbia and therefore defined four conodont biozones in the Columbianus Zone (Ammo- nite Standard Scale of Canada, Tozer,1994), correspon- ding to the Middle Norian (Alaunian 2 and 3 sensw Kry- styn in Zapfe,1983). COLLE DELCRAPIO SECTION È F bÈ - FEFFÈ=EEE * È È E È 9È E x; ÈÉ É fi s É Fio i rCC 10 .CC 9 .cc 8 .cc 6 .LL 5 rCC 48 oCC 4A .cc 4 .LL I Occurrence and venical rrnge del Crapio section. PLATE 1 Upper Norian conodonts from Colle del Crapio (Monte Cocuzzo) section (CC). Eq. f-l EpigondoleLla sloaakensis (Kozt4 1972) emend. Budai & Kovacs, 1986. 1) upper view, IPUM 25715, CC1, x 80. 2) upper view, IPUM 25716, CC4, x 80. 3) lateral view, IPUM 25717, CCl, x 80. 4) oblique lateral view, IPUM 25718, CC4, x 1OO. 5a) upper view; 5b) lower view, IPIJM 25719, CC4, x 80. 6) upper view, IPUM 25720, CCl, x 80. Z) upper view, IPUM 25721, CC4, x 80. 8) lateral view, IPUM 25722, CC6, x 80' 9) lower view, IPUM 25723' CCI' x 80' Fig. 10 - Enantiognathiform elements, IPUM 25724' CC4, x 100. Fig. 11, 12- Hibbardelliformelernent. i1) IPUM 25725,CC10,x200. 12)IPUM25726, CC4A,x 150 Fig. 13 ' Grodelliform element, IPUÌI{ 25727 ' CC10' x 100' ril.r+,rs- prioniodiniformelements. 14) IPUM25728,CC4,x1OO. 15) IPUM.?5729,CC4B,x70. r;g.to,tz- Hindeodelliformelemenrs. 16)IPUM25730,cc9,x100. 17) IPUM2573l,CC4B,x10O. Fig, 18 - Panicuiar o{ the pit of EpigondolelLa slwabmsis, fig' 9, x 800' X 'J at U rr'. rrl X F-.1 (^) U f! F F z Conodont biostratigraphl of Monte Cocuzzo Krystyn (in Zapfe, 1983) Kryslyn, t980; 1988 Kozur, l9E9; Kozur s Mock, 1991 z E I (f Marshi posthernsteini delrei rhaetica ultima Stuezenbaumi paucdentata poslhemsteini steinbergensis z É. z z Ua '6 f q Reliculalus hemsteini hemsteini - andrusovi ouinque- DUnclalus bidentata bidentata z z f [Iacer posÍeraE n.sp. D Hogani postera oo ó AMN/ONOID ZONE€ CONODONT ZONES 178 A. Mastandrea, F. Ietto, C. Neri G F. Russo Fig.4 - Biostratigraphic zonations based on ammonoids and cono- donts of the Upper Norian and Rhaetian stages. Roghi et al. (1995) noted, in the E. slwakensis po- pulation collected in the Dolomia di Forni (Carnia), an evolutionary trend similar to the one described by Or- chard (1983; 1991) tn two differenr species, E. postera and E serrulata. On the basis of this observation they referred the Dolomia di Forni to the Alaunian (Middle Norian). According ro Kozur (1972; 1989) and Kozur Er Mock (1991) Epigondolella slwahensis is a typical Seva- tian (Upper Norian) species. Its main occurrence marks the upper part of the E. bidenwa Zone and its disappea- rance corresponds to the lower boundary of the Misikel- la hernsteini-Paruigondolella andruswl Assemblage Zone (sensu Kozur & Mock, l99I) of the uppermosr Sevarian (Fig. a), This species has been reported also from the Calcari Selctferi of the late Sevatian age in the Lagonegro Basin, southern Italy (Amodeo et al., 1993). Fauna2. In sample CC6 specimens of Epigondolel- la slouahensls (Kozur) occur together with Misikella postbernsteini Kontr & Mock. The occurrence o{ M. posthernsteini earlier rhan M. hernsteini (which firsr ap- pears in sample CC8) is problematic, since M. posthernsteinl is thought to have evolved from the latter. Samples CC8, CC9 and CC10, from the Upper Complex, yielded a conodonr fauna composed exclusi- vely of the genus Mísikella, represented by M. hernsteini and M. posthernsteinl associated with ramiform elemenrs. The first species is quanritatively dominant over rhe se_ cond. Transitional forms between M. lternsteiní and M. posthernsteinl occur in sample CC8 (Fig. 3). Misikella bernsteini (Mostler) has been considered typical of the Suessi Zone (Upper Norian)(Mostler er al., 1,978; Gazdztcki et aI., 1979; Kovacs & Kozur, 19gO), as well as the Stuerzenbaumi Subzone (Lower Rhaetian) in the Zlambach Marls and Koessen Beds of the North- ern Calcareous Alps (Krystyn, 1980; Golebiowski, L986; 1ee0). Misikella postbernsteinl was originally described from the I-ower Rhaetian in the Zlambach Beds of Maly Mlynsky vrch (Slovakia) by Kozur & Mock (192a). Sin- ce then it has been reported many times from strati- graphic successions attributed ro rhe Upper Norian and/or Rhaetian of Europe and Japan (Mostler et a1., 1978; Gazdzícki, 1978; Gazdzicki et al., 1979; Kovacs & Kozur, 1980; Isozaki 8c Matsuda, 1982; Krystyn, 1980, 1988; Golebiowski, 1,986, 199A; Gulio, 1996). Recently, M. postbernsteini was collected from the uppermost Tri- assic (Crickmayí Zone) of Canada (Orchard, 1991). M. posthernstetni rs generally considered a species characteristic of the Rhaetian. FIowever, according ro Krystyn (1990) and Golebiowski (1990) it appears from the uppermost Sevatian (Suessi Zone); and the predomi- nance of M. hernsteini on M. posthernsteini is diagnostic of the uppermost Noriar age. Kozur & Mock (1991) suggesr that the first occur- rence of M. postbernsteíni can be used as a marker ro define the Norian,/Rhaetian boundary, an event easily recognisable in the Tethyan successions. In this case, most of rhe Cochloceras suessi ammonoid zone would be- long to the Rhaetian. On the other hand, Krystyn (1988, 1990) defined the base of the Rhaetian in the Hallstatt region as the first occurrence of " Cboristoceras" baueri (Stuerzenbau- mr Zone). This corresponds, in terms of conodont bio- stratigraphy, to the Last Occurrence Datum (LOD) of PLATE 2 Upper Norian/Early Rhaetian conodonts from Colle del Crapio (Monte Cocuzzo) section (CC). Fig. 1-6 - Misikella hernsteini (Mostler, 1967). l) oblique lateral view, IPUM 25732, CC9, x 100. 2a) upper view; 2b) lateral view, IPUM 25733, CC9, x 1ZO. 3) lower view, IPUM 25734;4) upper view, IPUM 25735; CC8, x 170. 5) later,rl view, IPUM 25736, CC9, x 100. Fig.6a-b - Misikellabernsteini-Misikellaposthernsteini6a) obliquelateralview;6b)lowerview, IPUM25737,CC9,xI7A. Fig.7-10 - Misihella postbemsteini Kozur 6c Mock, 1974. 7a) upper view; Zb) lateral view; 7c) oblique lateral view; IPUM 25738, CC6, x 170. 8a) lower view; 8b) oblique lateral view; IPUM 25739, CC6, x fiA. 9) upper view, IPUM 25240, CC6, x 170. 10) oblique lateral view, IPUM 25741, CC6, x 170. Fig. 11 - Cluster of Mkikella hernsteini.IPUM 25742, CC10, x 150. Fig. 12, 13 - Clusters of hideodelliform elements. IPUM 25743, CC8, x 150. Fig. 14 - Cluster of Grodella delicatula.IPUM 25744, CC8, x 100. Fig. 15 - Cluster of Epigond.oleLla slmakmsis. IPUM 25745, CC4, x 150. Conodont biostratigraplry of Monte Cacuzzo 180 Epigondolella bidenaa, First Occurrence Datum (FOD) of Misikella rhaetica and M. koessenensis, all species not documented in the Catena Costiera Calabrese. Following the scheme of Kozur & Mock (L991), the conodont fauna from samples CC6 to CC10 could be referred to the Early Rhaetian (M. hernsteini - M. postbernsteinl Subzone, M. postbernsteini Zone), whereas according to Krystyn (1990) it should be ascribed to the latest Norian (Ì4. hernsteini Zone) (Fig a) Conclusions. 1. The lower part of the Colle del Crapio sequen- ce (samples CCl to CC5) is characterised by the occur- rence of Epigondolella slwakensis, a taxon referred to the Aulanian-Sevatian (Middle-Upper Norian) by many aut- hors (Kozur, 1972, 1.989; Budai 6c Kovacs, 1986; Kovacs & Nagy, 7989; Kozur & Mock, 1991; Roghi et a1., rees). 2. The chronostratigraphic attribution of the up- per part of the succession (from samples CC6 to CC10) is more controversial, as it involves the unsolved defini- tion of the Norian-Rhaetian boundary. Samples CC8 to CC10 record the occurrence of the genus Misikella, rep- resented by M. hernsteini and M. posthernsteint. 3. According to many Authors, M. hernsteìnì and M. posthernsteini indicate. an lJpper Norian-Rhaetian A. Mastandrea, F. Ietto, C. Neri & F. Russo REFERENCES age, even if a larye part of the M. posthernsteini range is typically Rhaetian. The presence and abundance of M. hemsteini still at the top of the section, and the absence of diagnostic species such as M. rhaetica and M. koesse- nensis, may indicate that the upper parr of the the Colle del Crapio section (Upper Complex) belongs ro rhe up- permost Norian (Krystyn, 1990; Golebiowski, 1990). On the contÍary, according to the scheme of Kozur Er Mock (1991), the upper part of this section would be regarded as Early Rhaetian in age. 4. Since this preliminary study is based on a sin- gle stratigraphic section, we are not able to address the chronostratigraphic problems connected with the No- rian,/Rhaetian boundary. F{owever, we provide a descrip- tion of the verticai distribution of conodonts within the stratigraphic succession of the "Catena Costiera". Acknooledgements. $7e ere grrteful to A. Nicora (Milano) and M.J.Orchard (Vancouver) for revisions of the original manuscript. Field and printing expenses were supported by a grant of MURST 40o/o and CNR 96.00364 (F Russo, Cosenza). English revision by E. Fois Erickson (Cleveland). Illustrated specimens are housed in the Collections of the Institute of Paleontology, University of Modena IPUM 257 15-257 45) . Amodeo F., Molisso F., Kozur H., Marsella E. & D'Argenio B. (1993) - Age of transitional beds from "Cheny Lime- stones" (calcari con selce) to "Radiolarites" (scisti sili- ..i\ i- tL. r.ù^négro Domain (Southern ltaly). First evidence of Rhaetian conodonts in peninsular Italy. BolL. Sero. Geol. d'ltalia, v. 110(1991), pp. 3-22, Roma. Amodio Morelli L., Bonardi G., Colonna V., Dietrich D., Giunta G., Ippolito F., Liguori V., Lorenzoni S., Paglio- nico A., Perrone V., Piccarretta G., Russo M., Scando- ne P. , Zaneftirr I-orenzoni E. & Zuppetta A. (1976) - LArco CaLabro-peloritano nell'orogene appenninico- maghrebide. Mem. Soc. Geol. It., v. 17, pp. 1-60, Roma. Barattolo F., De Castro P. Er Parente M. (1993) - Some re- marks on GriphoporeLLa cureata (Gúmbel 1872) Pia 1915, dasycladacean green alga from the Upper Triassic. In Barattolo F., De Castro P. & Parente M.(Eds.) - Stu dies on fossil benthic algae. BoLL. Soc. Paleont.1r., spec. v. 1, pp. 23 46,Modetl Budai T. Ec Kovacs S. (1986) - A. rezi Dolomit Rétegtani Helyzete a KeszthelyiHegységben. FòLdt. Int. Evi Jel. 1984-rò1, pp. 17 5-1.9 1., Budapest. Epstein 4.G., Epstein J.B. Ec Harris L.D. (1977) - Conodont alteration - an Index to Organic Metamorphism. GeoL. Suru. Prof. Pap., v.995, pp. 1-22, Vashington. Gazdzickt A. (1978) - Conodonts of the Genus Misikella Kozur & Mock, 1974 from the Rhaetian of the Tatra Mts (Vest Carpahians). Acta PaLaeont. Pol., v. 23, pp. 341-350, Warsavr. Gazdzickt A., Kozur H. 8r Mock R. (1979) - The Norian- Rhaetian boundary in the light of micropaleontological d*a. Geologija, v. 22, pp.7I-1,1,2, Ljubljana. Golebiovrski R. (1986) - Neue Misikellen-Funde (Conodonta) und ihre Bedeutung fùr die Abgrenzung des Rhàt s. str. in den Kòssener Schichten. Sitz. Ber. Akad. Wiss. lVien, math.-nat.Kl., v. 195, pp. 53-65, Vien. Golebiowski R. (1990) - The Alpine Kóssen Formation, a key for European topmost Triassic correlations. A se- quence-and ecostratigraphic contribution to the No- rian-Rhaetian discussion. Albertiana, r'. 8, pp. 25-35, Utrecht. Gullo M. (1996) - Conodont biostratigraphy of uppermost Triassic deep-water calcilutites from Przzo Mondello Conodont biostratigraplry of Monte Cocuzzo 181 (Sicani Mountains): evidence fòr Rhaedan pelagites in Sicily. Palaeogeog., Palaeoclim., Palaeoecol., v. 126, pp. 309-323, Amsterdam. Ietto A., Perri E. & Silvagni C. (1993) - La successione dolo- mitica triassica di Monte Cocuzzo (Catena Costiera, Ca- labria). Atti Acc. Sc. Fis. Mat., v. 60, pp. L47-164, Napoli. Ietto A., Perri E., Ietto F. & Rende L. (1995) - The sequence of Mount Cocrtzzo (Catena Costiera, Calabria) in the dolomitic Trias of the Southern Appennines. Boll. Soc. GeoL. It.,v. lla (1995), pp.215-244, Roma. Isozaki Y. Er Matsuda T. (1982) - Middle and Late Triassic Conodonts from Bedded Chert Sequences in the Mino- Tamba Belt, Southwest Japan. Part 2: Misikella and Par- vigondoLella. J. Geosci.Osaka City Unio., v. 26, pp. 65- 86. Osaka. Kovacs S. Ec Nagy G. (1989) - A Pilis Hegység Aviculas és Halobias Meszkóósszletének Kora. Fòldt. Int. Eoi Jel. 1,987-ró1, pp. 95-129, Budapest. Kovacs S. & Kozur H. (1980) - Stratigraphische Reichweite der wichtigsten Conodonten (ohne Zahnreihencono- donten) der Mittel- und Obertrias. Geol. Palàont .Mitt. Innsbruck., v. 10, pp. 47-78, Innsbruck. Kozur FI. (1972) - Die Conodontengattung Metapolygnatbus HAYASHI 1968 und ihr stratigraphischer Vert. Geol. Palàont. Mitt. Innsbruck., v. 2 (1,1,), pp. 1-37,Innsbruck. Kozur H. (1980) - Revision der Conodonten-zonierung der Mittle-und Obenrias des tethyalen Faunenreichs. Geol. PaLàont Mitt. Innsbruck, v. 10, pp.79-172,Innsbruck. Kozur H. (1989) - Significance of events in Conodont evolu- tion for the Permian and Triassic stratigraphy. Courier Forsch.-lnst.Senckenberg, v. 11,7, pp. 385-408, Frankfurt a.M. Kozur H. & Mock R. (1974) - Misikella posthernsteini n.sp., .iùngste Conodontenart der tethyalen Trias. Cas. min. geol., v. 19, pp. 245-250, Praha. Kozur H. Er Mock R. (1991) - New Middle Carnian and Rhaetian Conodonts from Hungary and the Alps. Stra- tigraphic importance and Tectonic implications for the Buda Mountains and adiacent areas. Jb. Geol. B. -A., v. 134, pp. 27 l-297,'W íen. Krystyn L. (1980) - Triassic conodont localities o{ the Salzkammergut Region (Northern Calcareous Alps). Field Trip B. In Schònlaub H.P. (Ed.) Second European Conodont Symposium (ECOS iI), Guidebook and Ab- srracts. Abh. Geol. B.-A., v. 35, pp. 6i-98, \X/ien. Krystyn L. (1988) - Zur Rhàt-Stratigraphie in den Zamblach- Schichten (vorliufiger Bericht). Sitz. Ber. Akad. lhiss. IVien, matb.-nat.KL., v. 196, pp.21-36 \X/ien. Krystyn L. (1990) - A Rhaetian Stage - Chronostratigraphy, subdivisions and their inrerconrinental correlatton. Al- bertiana, t 8, pp. 15-24, Utrecht. Mostler H., Scheuring B. & Urlichs M. (1973) - Zwr Mega- Microfauna und Mikroflora der Kóssener Schichten (al- pine Obertrias) vom Veissloferbach in Tirol unter be- sonderer Berúcksichtigung der in der suessi- und marsbi- Zone auftretenden Conodonten. Osterr. Abad. lYiss. Schriftenr. Erdutiss. Komm., v. 4, pp. I41-l74,Wren. Orchard M.J. (1983) - Epigondolella populations and their phylogeny and zonation in the Upper Triassic. Fossll and Strata, v. 15, pp. 177-192, Oslo. Orchard M.J. (1991) - Upper Triassic conodonr biochronolo- gy and new index species from the Canadian Cordille- ra. In Orchard M.J. e{ McCracken (Eds.) - Ordovician to Triassic conodont paieontology of the Canadian Cor- dillera. Geol. Suro. Canada BuLl., v. 41.7, pp. 299-335, Ottawa. Ogniben L. (1969) - Schema introduttivo alla geologia del confine calabro-lucano. Mem. Soc. Geol. 1r., v. 8, pp. /t)J-./ bJ. KOma. Roghi G., Mietto P. & Dalla Vecchia F.M. (1995) - Contribu- tion to the Conodont biostratigraphy of the Dolomia di Forni (Upper Triassic, Carnia, NE Italy). Mem. Sci. Geol., v. 47, pp. 1.25-1.33, P;rdova. Tozer E.T. (1994) - Significance of Triassic stage boundaries defined in North America. In Gueaux J. & Baud A. (Eds.) Recent developrnents on Triassic Stratigraphy. Proceedings of the Triassic Symposium, Lausanne, 20- 25 Oct. 1991,, Mèm. de Géologie, v. 22, pp. 1,55-170, Lau- sanne. Zapfe H. (1983) - Das Forschungsprojekt "Triassic of the Tethys Realm' (IGCP Proj.4). Abschlussbericht. Ósterr. Akad. lY'iss. Schrrftenr. Erduisl Komm., v. 5, pp. 7-L6, 'Wien. Received December 19, 1996; accepted May 5, 1997