T-- Rivista Italiana di Paleontologia e Stratigrafiavolu volume 103 numero I tavole 11 pagrne 39-52 Aprile 1997
CONODONT BIOSTRATIGRAPHY OF THE S.CASSIANO FORMATION SURROUNDING THE SELLA MASSIF (DOLOMITES, ITALY): IMPLICATIONS FOR SEQUENCE STRATIGRAPHIC MODELS OF THE TRIASSIC OF THE SOUTHERN ALPS
ADELAiDE MASTANDREA'I, CLAUDIO NERI'I* & FRANCO RUSSO*>I'i
Key-uords: Conodonts, Biostratigraphl Sequence Stratrgraphy, Upper Triassic of the Dolomites based on two generations of Cassian S. Cassiano Formation, Ladinian, Dolomites. platforms is clearly inadequete to describe the actual successlon,
Riassunto. Lo scopo del presente lavoro è la definizione del contesto cronostratigrafico della Formazione di S. Cassiano interdigi- lntroduction. tata con i depositi clinostratificati di scarpata della piattaforma cassia- na del Gruppo di Sella. Sono state studiate numerose sezioni, sia dal The Sella Massrf consists of an isolated, atoll-like, punto di vista sedimentologico che biostratigrafico; tre di queste, si. deeply dolomitized carbonate platform (Cassian Dolo- tuate in prossimità dei passi Sella e Gardena, hanno fornito faune a mite), overlain by the horizontal beds of the Raibl and Conodonti stratigraficamente significarive, attribuibili alla Zona a die- Dolomia Principale Formations, respecrively Late Car- beLi sensu Krystyn (1983), indicativa della pane piu alta del Ladinico superiore. Ne consegue che la piattaforma cassiana del Sella, che in nian and Norian in age (Fig. I and 2). Due to irs spec- base ai rapponi geometrico-stratigrafici è necessariamente coeva ai de- tacuiar exposure and almost complete absence of tecto- positi bacinali della Fonnazione di S. Cassiano, è anch'essa di età nic deformation, the Sella Massif has been the object of ladinica terminale (in contrasto con la tradizionale attribuzione al several studies, and its depositional geometries and the Carnico). Dal mornento che vari lavori hanno documentato l'esisten- za, nell'area delle Dolomiti, di piattaforme carbonatiche posr-vulcani- stratigraphic relationships between basin and platform che pii) z,ecchie (es.: i Denti di Terra Rossa) e più giwani (es.: le piat- sediments have been well defined (Mojsisovics, 1829; Re- taforne del Nuvolau e del Lagazuoi), sì possono trarre le seguenti ithofer, 7928; Leonardi & Rossi, 1957; Bosellini et al., conclusioni: a) le successioni post-vulcaniche e cassiane delle Dolomi- 1980; Boselliní, 1982; 1984; Kenter, L990; Bosellini Ee ti sono decisamente pi,ì complesse e caraftertzzafe da pirì generazioni di piattaforme di quanto non si ritenesse; b) un modello stratigrafico- Neri, 1991). sequenziale del Ladinico superiore-Carnico delle Dolomiti, basato su The studies cited above clearly demostrated that due sole generazioni di piattaforme cassiane, non è ulteriormenre so- the Sella Platform is an isolated buildup, composed stenibile; c) la cornplessità stratigrafica delle Dolorniti occidentali nel mainly of clinostratified slope deposits (breccias and me- Ladinico-Carnico è fonemente controllata dal segnale tettonico (che sovrasta quello eustatico), e quindi il modello sequenziale che si può gabreccias), radially prograding from a central nucleus costruire in quest'area non è proponibile come standard globale. represented by an undated, probably Eariy Ladinian, carbonate core (Bosellini & Neri, 1991). The clinoforms Abstract. The strarigraphy and age of the S. Cassiano Forma- interfinger at the base with the S. Cassiano Fm., which tion outcropping around the Sella Massif (Dolornites, Nonhern ltaly) consists were investigated. The unit interfingers with slope deposits penai- of aiternating marly pelites, platform-derived ning to the Cassian carbonate platform of the Sella Massif. Several calciturbidites and olistolith swarms, and blackish sand- stratigraphic sections were analyzed from a sedimentologic and bio- stones derived from the erosion of volcanic areas. stràtigraphic perspecrive. Three sections (Sella Pass Ia and Ib, Garde- The age of the Sella Platform and coeval S. Cassia- ne Pass) yielded stratigraphically significant conodont faunas refera- no Formation has been regarded as Ladinian-Carnian ble to the diebeli Assemblage Zone sensu Krysryn (1983) of latest La- by dinian age. Therefore, the Sella Cassian Platform traditionally regar- Leonardi (1967). The subsequent recognition of different ded as a typical Carnian buildup, is also latest Ladinian in rge. The generations of carbonate platforms (pre- and post-volca- occurrence of post-volcanic carbonate platforms older (e.g. Denti di nics, Bosellini & Rossi, 1974) led to rhe idea that the Terra Rossa) tnd younger (e.g., the Nuvolau and Lagazuoi platforms) "Cassian" platforms (post-volcanics) pertain to the Car- rhan the Selle Platform, suggests thet: a) the post-volcanic and Cas- sian succession of the Dolomites is far more compiex than traditio- nian. Some authors, however, (e.g., Assereto et a!., !977; nally thought and b) a sequence stràtigraphic model of the Middle- Bizzarini & Braga, 1982; Fois Er Gaetani, 1980) followed
'f Dipartirnento Screnze della Terra, lJniversità di Modena, via Università, 4, I-41100 Modena. 'f'r Dipanrrrento di Scienze Geologiche e Paleontologiche, Uni'ersità di Ferrara, C.so Ercole I d'Este,32, I-44100 Ferrara. '''"f Dipanimento di Screnze della trra, Università della Calabria, I-87030, Arcavacarr di Rende (Cosenzr). 40 A. Mastandrea, C. Neri & F. Russo
Sciliar^ Cortina Arabba ! d'Ampezzo Catinaccio^ \_
Predazzo
Fìo 1 Index-map of the area studied with the toponyms quoted in the text, cass,an F-.:-f r'/ 'z ffi Dolomils l-. . ..1 WenqenBeds the works of early German geologists (Mojsisovics, car&na mn ffi Megabrtrcn L:j-i-! voba-'cr )'--/-23 3a 1829; Ogilvie, 1893; Ogilvie Gordon, 1929) and distin- t guished a lower member of the S. Cassiano Fm. of Late ffi s.cassianoFm. \ Ladinian age and an upper member of Carnian age. As a consequence, a portion of the Cassian Dolomite is con- Fig. 2 - Simplified geologic map of the Sella Massif, showing the sidered Upper Ladinian in age. location of the stratigraphic sections. The post-Cassian for- mations have been omitted. Ia and Ib, Pass Recent interpretations of the sequence strati- Sella sections; II, Murfreit section; III, Gardena Pass section; IV Val Me- graphic organization of the Cassian succession (Bosellini sdì section; V, Campolongo Pass section. Key: 1, direction Er Doglioni, L988; Masetti et a1., 1991; Bosellini, 1991; of progradation of the Sella Platform; 2, tnce oÍ the strati- De Zanche et a1., 1993) are based on two generations of graphic sectionsl J, faults; 3r, ovenhrust. Cassian platforms. In the present paper, v/e supply age data for the 1. The western sector (i.e., Selle Pass, Fig.2) is characterized Cassian successions of the Sella Massif based on cono- by a poorly exposed succession consisting of alternating marl, marly to pure micrite, bioclastic calcarenite and breccia, and olistolith donts and supported by the ammonoid findings repor- swarms, locally organized in thickening- and coarsening-upward (CQ ted by Neri et al. (1.994), Mietto & Manfrin (1995a,b) sequences (lr4asetti et al., 1991). This succession overlies a volcanicla- rVengen and Baracca (1996). stic sequence penaining to the Formation, from which it is separated by an horizon about 25-30 m thick consisting of turbiditic coarse sandstones and conglomerates. with carbonate and volcanic The S. Cassiano Formation around the Sella Massif. clasts, alternating with lens-shaped ruditic debris flows and carbonate olistolith swarms (Fig. 3 and 4). The S. Cassiano Formation of this The San Cassiano Formation consists of pelites area contains a significant amount of volcaniclastic sandstones and mi- and marls alternating with micrites and gravity-displaced croconglomerates. The volcaniclastic input increases southward, resul- ting in a \lengen-like succession that interfingers and panly replaces carbonates (calciturbidites and debrites) derived from the the S. Cassiano Formation, which is usually more rich in carbonate adjacent Cassian platforms. Variable amounts of volcani- lithotypes. clastic turbidites, fed by remnant, inactive volcanic 2. The S. Cassiano Formation of the nonhern flank of the highs, may be intercalated in the succession. The volca- Sella Massif (from Murfreit to Colfosco, Fig. 2) contains a thick chan- neled megabreccia body (Gardena Megabreccia), described by Bosellini niclastic content is quite low in the type area of the for- et a1. (1980), Bosellini (1982; 198a) end Bosellini 6c Neri (1991). h mation (S. Cassiano, Pralongià, Stuores $fliesen) or in consists of several megabeds formed by chaotically arranged carbonate the sorroundings of Cortina, while it is significant to olistoliths and ranges in thickness from a few tens of metres (Gardena the west (i.e., southern slope of Sasso Piatto Mt., we- Pass) to about 200 m (Murfreit). The Gardena Megabreccia subdivides the S. Cassiano deposits into two units, underlying and overlying the stern flank of Sella Massif), near the Buffaure-Monzoni megabreccia respectively (Fig. 5). P redazzo volcanic district. The lower unit consists of an acyclical alrernation of shales, On the basis of volcaniclastic content and overall marls, carbonate and volcanoclastic turbidites, ruditic debrites, Ienses stntigraphic organization, three kinds of successions, of carbonate megabreccia a few metres thick. The prominent charac- teristic of this succession is the frequent occurrence of: a) chaotic or characterrzing different areas, may be recognized within poorly organized gravity-displaced deposits (slump deposit, mud-flov', the S. Cassiano Formation surrounding the Sella Massif debris-flow); b) unconformities related to slump and slide scars; c) (Fig. i) small tensional synsedimentary faults with metre-size tenical displace- Conodont biostratigraphy of the S. Cassiano Formation +1
SELLA TOWEHS
"'i I
* -tl
tocoMoltvA
Fig. 3 - Field sketch of the geometri- cal relationships between the S. Cassiano Formation (sec- tion lb) and the Sella Plat- form at the Sella Pass. F.Tli-...:X L=;= l) S. Cassiano Formation li; ii1,:iiiii';lr l';' 4z 2) Cassian Dolomite ment, sutured by turbidites or pelite layers. All these features may be the volcaniclastic-dominated rVengen Formation and the regarded as evidence of remarkable synsedimentary tectonics, probably carbonate-dominated S. Cassiano Formation. This bound- related to the Triassìc activity of the Gardena Pass Fault (Bosellini & ary is diachronous and consequently prevents the estab- Doglioni, 1988; Bosellini 6c Neri, 1991). The upper unit of the S. Cassiano Formation, a few tens to lishment of a reliable subdivision of the S. Cassiano Fm. about 100 m thick, consists of an organized succession of marls and into members of regional extent. carbonates, forming small CU sequences, in turn piled up according to an orerall CU trend that reflects the progradation of the overlying carbonate platform. At the base, the sequences are represented by peli- The stratigraphic sections and the Conodont faunas. tes evolving upward to micritic limestone (mudstone and wackestone) with turbidites. In the upper pan of the unit, the CIJ sequences rninor Several stratigraphic sections, iocated in the north- are capped by coarse amalgamated calciturbidites and finally by olisto- eastern sectors Sella the Se1- lith swarms. Volcaniclastic sandstones may occur but are quite rare. ern and of the Massif, from 3. The eastern and southeastern sectors of the Sella Massif, la Pass to Arabba (Fig. Z) were investigated. Three of from Corvara to Arabba (Fig. 2), are characterized by stratigraphic suc- these sections (Sella Pass Ia and Ib; Gardena Pass; Fig. 4 cessions very similar in facies pattern and venical evolution to the S. and 5) yielded significant conodont faunas, evenly di- Cassiano Formation of the type area. These successions consist of piles of thickening, coarsening-upward cycles, a few metres thick, composed stributed from the the bottom to the top. A further sec- in the lower pan by pelites and marls that grade upward to micritic tion (Arabba) gave only scattered and poor conodont limestones (interpreted as periplatform mud, Masetti et al., 1991) and assemblages, substantially confirming the age data from then to calciturbiditic units. The volcaniclastic input is negligible and, the Sella and Gardena Pass sections. Other sections mea- in general, the terrigenous colnponent is almost exclusively repre- sented by pelites. As a whole, the succession constitutes : major CU sured and sampled at Pordoi Pass, Corvara and Bec da sequence, reflecting the progradation of the carbonate platform. The Rozes (Fig. 2) were barren of conodonts. Bec da Rozes thickness of the succession varies greatly, from about 600 m (Arabba yielded ammonoid faunas indicative of the Regoledanus section, southwestern side of the Livinè valley) to a little more than Zone (Neri et aI., 1994;Baracca, 1996). 1OO m @ec da Rozes section, northeastern side of the Livinè valle,v, Fig. 2), According to Bosellini er rl., (tesl) this rbrupt change in thic- kness is due to the synsedimentary activity of the Livinè Fault, that Sella Pass sections. Th'o panly overlapping sections from strongly controlled the thickness of the volcanic succession (mainly the Sella Pass area were measured (Fig. 2,3 and 4). Both are composed represented by volcanic-derived clastics) and Vengen-S. Cassiano (p.p.) at the base of coarse volcaniclastic sandstones with ruditic lenses, con- formations, and was eventually sutured by the Sella buildup. taining volcanic clasts and carbonrte olistoliths. This unit is followed upward by cyclic alternations of marly pelites and marly to pure lime- The data outlined above indicate that the sedi- stones (mudstone and wackestone). Following a rough corrsening-up trend, the top of the incomplete section Ia and the middle-upper part mentary features of the Cassian succession in the inve- of section Ib are characterized by the occurence of coarse bioclastic stigated areà are cleariy influenced by synsedimentary calciturbidites. The upper pan of section Ib also contains several car- tectonics as well as by the inherited paleogeography (i.e., bonate olistolith svuarms and eventually grades into the clinostratified the iocation of the relic volcanic highs undergoing ero- slope deposits of the carbonare platform. Volcaniclastic sandstone and sion). As a result, the basin deposits show remarkable microconglomerates occur repeatedly in both sections. The basinal deposits of section Ib are clearly interfingered with lateral facies changes over a very shor-t distance, It is the- the clinostratifi"d ,lop" deposrts of the Selh Platform (Fig. 3) that is refore very difficult to physically correlate the S. Cassia- here characterized by climbing progradation (Bosellini, 1984). From no successions around the Sella Massif and aiso to trace the geometric relationships it is apparent that the age of the Sella unambiguously the lithostratigraphic boundary between Platform is necessarily the same age of the S. Cassiano Formation. 42 A. Mastandrea, C. Neri & F. Russo
Eleven samples collected from the two sections (Fig. a) yielded dian) (Fig. 6). In the Epidaurus (Greece) sequence .8. stratigraphically significant conodonts. The fauna includes: mostleri and B. diebeli are distinctive of the Late Longo- Budurw ignatbus mungoens is (Diebel) bardian and disappear at the base of the Carnian toget- Budurwignathus diebeli (Kozur 6c Mosrler) her with B. mungoensls (Krystyn, 1983). The presence of Budurou ignatb us m o st L e r i ff.ozur) Budurnignathus cf . longobardiczs (Kovacs) B. diebeli in the Late Longobardian has been reported Budurouignatbus sp.A also from the Himalayas (Chhabra & Kumar, 1992). (Huckrreàe) GIad igondo lelLa teúrydis Kozur (1980, 1989) maintains, on rhe basis of Gladigondolella malayensis malayensis Nogami data from the Apuseni Mts. (Romania), that B. diebeli is G ondo lella foltata inc linata Kovacs Pseudofumishius nrurcianus praecursor Gtllo & Kozur not present in the rnungoensis A.2., but it is restricted Mietto 6c Manfrin (1995a) reponed the occurrence in this sec- to the Cordevolian (: Sutherlandi - Aonoides Zones) ammonoids of the Regoledanus Subzone sezsz Mietto and tion of (Fig. 6), where it occurs together wíth Metapolygnathus Manfrin. polygnathrfornls (Budurov & Stefanov) and M. adpole Gardena Pass section. The S. Cassiano Fm. of the Gardena (Hayashi). Pass section contains the Gardena Megabreccia, that subdivides the On the contrary, Krystyn (1983) considers the ap- formation into the two units described above (Fig. 5). The lower unit pearance oÍ B. diebeli, aîd M. polygnathformis diachro' is about 80 rn thick but its base is not exposed. The upper unit is longobardian and almost completely covered and, as for the lo*e. unit, its thickness is nous events, starting from the Late not precisely determinable; its base , however, is represented by cyclic the base of the Carnian, respectively. The appearance of irlternations of marly pelites and micritrc limestones. M. polygnatiformis rs considered isochronous with that samples collected below and above the Gardena Megabrec- Six of Trachyceras aon. cia yielded the following conodont fauna (Fig. 5): Data from the Dolomites seem to confirm Kry- B udurou ignathus mungo ens is (Diebel) Budurwignathus diebeli (Kozur & Mostler) styn's (1983) conclusion. Since in the Dolomites B. die- Budurwignatbus mo stleri (Koz\r) Aell is associated with B. mostleri and B, mwngoensis aîd G ladigondol el la tetlry dk (Huckriede) never with M. polygnathiformis, the latter occurring in G I ad igondolcl la n talayens is n a lay ensis Nogami aon (Neri et a1.,7995). Reithofer (1928, p. 542) reponed a specimen of Traclryceras re- beds containingT goledanun (sic) frorn Col de Masores, corresponding to the upper prn of the Gardena Pass section described here. Mietto & Manfrin (1995a) reponed rhe occurrence of ammonoid faunas referable to the Regole- Systematic Paleontology drnus Subzone tnd Daxatina cf. canadensís Subzone sensrz Mietto and Manfrin from the same section.These subzones correspond respecti- vel,v to the lower and upper part of the Regoledanus Zone sensu Kry- Genus Budurooignathus Kozur, 1988 styn (in Zapfe, 1983).
1973 Carinella Buduror-, p.799. March er J., p. 2.47. Gonodont biostratigraPhY. 1988 ScpbardieLla No significant biostratigraphic variation in the co- T;'pe species: Polygnatbus nnngoensis Diebel, 1956 nodont fauna was observed in the investigated sections. This can be explained by a high sedimentation rate Pro- Budurovignathus diebeli (Kozur & Mostler, 1971) ducing thick sequences deposited during the time span Pl. 1, fig. s-8 of a single conodont zone. The conodont association of both Sella and Gar- 1971 TàrclogondoLella dìebcli Kozur & l\4ostler, pp. 13-1'1, pl. 2' fig. 1' sections is characterized by Ladinian elements dena Pass : \non rtg, J). snch as: Buduroaignathus mungoensis, B. mostleri and B. 1975 Epigondolella diebeli - Krystyn in Kristan-Tollmann Ec Krystyn' (non 6). diebeli. Specimens oL Pseudofurnish ius murc ianus praecur- p. 273, pl. 2, lig. 5-7, pl. 3, fig. 5 Íig 1980 Metapolygnatbus diebeh - Kov.tcs tc Kozur, pl. 7' frg. 9; pl. 10, sor present in sample PS 6 (Sella Pass section). ^re fíg. 7-9 . Gullo & Kozur (1991) recognized three zones in l98O Carinella diebeli - Krystyn, pl. i 1, fig. 6. the Late Ladinian-Early Carnian, on the basis of the 1983 "EpLgondolalla" diebeli - Krystyn, pl. 8, fig. 7-9. Vrielynck, pp' 123-124, pl. 1, fig. 13-15. evolutionary trend observed within the genus Pseudofur- 1987 CarineLladiebeli- Bndurnignatbus diehcli - Kozur, pl 12' fig. 3. with the conodont L989 nishius. The zones correlate well D9a CarineLla diebeli 'Budurov & Sudar, p. 214, pl. 3, fig. 1-8. standard zonation of Kozur (1980). In particular' accor- 1994 Budurw-rgnatbus díebeLi - Neri er rl., pl. 1' fig. 5. ding to these authors P. murcianus praecttsor is the iast 1995 Buduroarynathus diebeli - Neri et rl., pl. 2, fig 2-a. representative of the bi-platform specimen type and it is by indicative of the higher Longobardian. Remarks. The holotype ol B. diebeli illustrated According to the zonal scheme of Krystyn (1983) Kozur & Mostler (I97I, p|.2, fig. 1) shows strong nodes broad the fauna may be attribuited to the Late Ladinian and developed on both m'argins of the platform and a end- Some of specifically to the upper part of the dìebeli A'Z', which and approximately rectangular posterior 5) have a more rounded corresponds to the Regoledanus Zone (Late Longobar- our specimens (e.g., Pl. 1, fig' Conodont biostratigraplry of tbe S. Cassiano Formation 43
Ia Ib ò h G\ 14 !f u qo 'd 'l rd 'd dk tJo. ia('Eh ! I 'd Q 'rq 'd o .do f v)h È'd r{ b |! E'd tr od0t !rdlJ0 ooro i!'d\X 2 b,q$I{'ru{a EOh .r&u- 3.dOcrOO30q E!EUh\EUE 3 ai .i si Èi c; q; qt "i "" 4 . PS 11/S2 D . PS 10/92 6 7 a @ I a 10
o 1-5 specimens o PS 9/92 o 6-15 o PS 6/92 a>15
Fig.4 - Sella Pass stntigraphic sec- o PS 5/92 tions and distribution of co- nodont species. See Fig. 2 for . PS 4192 . PS 8/92 location. CD, Cassian Dolo- mite. Symbols: see Fig. 4. Symbols: 1) ciinostratified o PS 3/92 slope deposits of the Cassian .PSA92 Dolomite; 2) olistolith swarms; 3) carbonate breccia; o PS 1/92 . PS 7t92 4) volcaniclastic turbidites; 5) carbonate, mainly bioclastic, turbidites; 6) micritic lime- stone; 7) pelites and marls; 8) covered interval; 9) slumps; 1O) conodont sample.
platform posterior end similar to the specimens from È.d !.{ É oH Ot O O 0{ >> Greece illustrated by Krystyn (1983, pl. 8, fíg.7,8) and bQ U { q 3.É o o 6 referred to B. diebeli. 5! -s: ! aaEoo The outline platform of these specimens resem- o 1301 I + bles that of B. longobardicus (Kovacs) but they have o I I I .l'l I more rounded and stronger marginal B. -a-;==Fr denticles than .Ìt;-l > | -c\'JÀ3 longobardicus. Both forms with a rounded or recrangular I< I ,# roo-l 6 I --'f platform occur in the same samples. Microreticulation to I tcc I -l< I -- . PG 3,/92 covers most of the platform, including nodes, and it is lo i absent only in the adcarinal area. The keel is commonly ll . PG 4/92 -l I bifurcated posterior to the pir. ; lt - Range. Upper Longobardian (Regoledanus Zone), t: I lL I 5o-1 diebeli A.Z. (Krystyn, 1983). Late Ladinian-Early Car- o I t2 | i< I nían (rnungoensis A.Z. - diebeli A.Z.) (: the uppermost 10 | -] Pl. 2, fís. 6 Frg. 5 Gardena Pass stratigraphic section and distribution of conodont species. See Fig. 2 for location. Symbols: see Fig. 4. cf.1983 Maapolygnatbus longobardicas Kovacs, pp. 115-116, pl. 6, fig. 1. Neri G F. Russo 44 A. Mastandrea, C. Zone$ nlunglensis A.Z. - mostleri L,Z.or die' Remarks. The specimens studied share some stmt- Aonoides larities with B. longobardicus, having parallel platform beli A.Z. sensuKozwr 1980. margins, the posterior part of the platform lacking mar- ginal nodes and a broad platform end. They differ from Budurovignathus mungoensis (Diebel, 1956) B. longobardicus in having rounded anterior marginal no- Pl. 1, fig. 9-10 des (two on each side) that do not continue in ridges Polygnatbus mungoensis Diebel, pp. 431-432; pl. 1, fig. 1-20; pl' toward the carina. Furthermore, in lower view, the ba- 1956 2, ftg. I-4; pl. 3' fig. 1; Pl. 4' fig. 1. and flat and has only sal cavity is relatively more broad 1.970 Epigondolella rnungoensk - Huddle, p' 127, fig. 2a-h- slightly raised edges. 1973 Thrdogondolella nurgoensis ntungoensis - van den Boogaard & Range. At present this species is known only Simon, p. 17, pl. 1, fìg. c; pl. 2, fig. a-b. Metapolygnathus mungoensis - Kovacs & Kozur, pl. 7 , fig' 3 . in Northern Flungary' 798a from Upper Longobardian 1989 Buduroaignathus mungocnsis - Kozur, p. 417, pI' 11, fig. 5' pl. 13, fig. 1. 799A Buduro',tignathus mungoensrs - Sadeddin, p. 376, fig' 5 3 (cum Budurovignathus mostle ri (Kozur, 197 2) ryn.). PI. 2, fig. 1-3 l99O SephardielLa mungoensis - March et al., p. 198, pl i, fig. a-p. 1994 Budwwignathus nungoensis - Neri et al., pl. 1' fig. 1. 7995 Budurrnignathus mungoensls - Nert et al., pl. 2, fìg.7'9 1972 EpigondoLeLla rnostleri Kozur in Kozur & Mock, pp' 9-10, pl' 1' fig. 8. strong asymmetry of the posterior l98O Metapolygnathus ntostLeri - Kovacs & Kozur, pl 8' fig 4' Remarks. The 1983 MetapoLygnatbus mostleri - Kovacs, pl. 6, fig' 2' platform distinguishes this species from the other Upper 7983 "EpigondolelLa" mostleri - Krystyn, pl. 8, fig a-6' Ladinian - l,ower Carnian sPecies. diebeLi - Chhabra & Kumar, pl' 4, fig' 10' lgg2 "Epigondolella" The specimens studied show the typical features ntostLeri - Neri et al., 1, fig 3 1994 Budurnignathus Pl. with 1995 Budurnigtzathws tttostleri - Neri et al., pl 2, ftg' 11'12' of B. mungoensisi a marked asymmetric platform marginai nodes, and a distinct free biade and basal cavi- Remarks. A Budurcntgndthus with a symmetrical- ty shifted in the anterior third of the platform' The lar- lobes di- ly pointed platform to the Posterior end; discrete, thin, ger development of one of the posterolateral which the sharp marginal denticles and a Prominent continuous stinguishes this species from B' dtebeli, in the posterior end. carina that extends to the Posterior end of the unit' The platform margins are straight towards there is symmetrical platform of B. mostlerl differs from that of In transitional forms between these two species continuous carina B. n'tungoensls which has one posterolateral lobe more a tendency to develop a posteriorly The ten- strongly developed than the other and stronger' more with an increase in size of the marginal nodes. extend in ridges towards rounded marginal nodes, absent on the Posterior dency of the marginal nodes to lobe with piatform. the carina and to form the second posterior rather pro- The platform outline of. B. mostleri is similar to the beginning of a bifurcated loop appears that of B. japonica japonica (Hayashi) from which B' nounced in some sPecimens. (Mosher, 1968)' mostleri would have developed according to Kozur (in Range. Late Ladinian worldwide to the uP- Kozur & Mock, 1972, p. 1O). B. rnostLeri can be distin- Middle to Late Longobardian (upper Gredleri Zones) mungoensis A'Z' guished lrom B. japonica japonica by the Presence of per part of the Regoledanus (1980), Kozur & denticles on the platform margins. (Krystyn, 1983). According to Kozur Ladi- B. Iongobardicws has a broad, undenticulated Kovacs (1980) this species extends from the Upper (Archelaus - Aon Zones)' platform end and marginal nodes developing into ridges' nian to the Cordevolian Range. Upper part of the Longobardian (Regole- Budurovignathus sp.A danus Zone pars.) tpper part of diebeli A.Z' (Krystyn, Pl. 2, frg.7-9 1983). Upper Longobardian - Cordevolian (Sutherlandi - PLATE 1 Upper Ladinian conodonts from Sella Pass (PS) and Gardena Pass (PG) sections' malayenns rnaLayensis Nogami. 1a) Upper view; lb) lower view; PG 47; x lOO' Fig. 1a-b Gladigond.oLeLLa x PS 2; x 110. 3a) upper vren'; 3b) lower view; 3c) lateral view; PS 4; Fig. 2, 3a-c GondolelLa foliata incLinata Kotacs. 2) ufper rie*; 1 10. view; PS 9; x 130' Fig.4a-b - Gladigondolella teùrydis (Huckriede). 4a) upper view;4b) lateral view; PS 10; x 100' 6) Lower vien'; PG 47; x 100 7a) Upper vrew; Fig. 5, 6, 7a-b, 8a.c - Budurwignatb* d;ibrl; iKo"'. & t'lorit"ù.'s) Upper pG ga) view; 8b) view; 8c) lateral view; PS 3; x 120. 7b) uppei-lateral view; 47; x 1OO. upper .lower Iower view;9c) lateral view; PS 10; x 100 10) upper view; PS Fig.9a-c, 10 - Budur*ign*,tbus nrungoensis (Diebel). l") úip.. ti.*;9t) 11; x 100 +l Pi. i Conodont biostratigrapl4t of the S' Cassiano Formation A. Mastandrea, C. Neri G F. Russo Diagnosis. A Bwdwrwignathus characterized by 1983 Gondolella t'oliata inclinata Kovacs, pp. 110-112, pl. 1, fig. 1-4; pl, 3, fig. 2-4 (cum syn.) prominent, rounded denticles present only on the ante- 1983 GondolelLa inclinata - Krystyn, p. 239, pl. +, fig. l, 2; pl. 5, fig. rior platform margins (two on each side), and a flat, 1, 2; ? pl. 3, fig. 5. broad, undenticulated posterior platform with a promi- 1987 Gondolella inclinata - Vrielynck, pp. 140-141, pl. 4, f;g. 4-9. nent, large denticie that dominates the centre of the po- 1.99A ParagondolelLa inclinata - Catalano et al., pl. 2, ftg.2. 799A ParagondolelLa foliata - Budurov & Sudar, p. 210, pl. 1, frg. 3-6 sterior platform. This denticle is completely separated (holotype of G. foliara inclinata). by a space from the last carinal denticle. 1.992 Neogondolella inclinata - Chhabra Ec Kumar, p1. a, fig.8-11, 13, The carina, composed of large denticles, ends at tf. L994 NeogondoLella incLinata - Neri et al., pl. 1, fig. 4. about half of the platform length. A small pit is located foliata 7995 NeogondoleLlafoliata inclinata - Neri et al., pl. 2, fig. 10, 1,4,20. beneath the anterior third of the platform; the keel is wide and flat with slightly raised edges. Remarks. The specimens studied show the typical Description. Slightly asymmetrical platform, with characteristics of G. foliata incltnata. They are slender, denticles on the anterior margins. The posterior two elongated with thickened upturned margins and a basal piatform is flat, broad and undenticulated, with a pro- edge always arched before the pit. minent, large denticle in its centre. This denticle is com- According to Kovacs (1983, p. 111) G. foliata incli- pletely separated by a large space from the last carinal nata evolved from GondoLe/la excelsa (Mosher); the latter denticìe. is distinguished by its high anterior carina) flar platform A microreticulation covers the margins of the and never upturned margins. Krystyn (1983, p. 239) ele- platform, including the marginal denticles, but it is ab- vated this subspecies to species, whereas Budurov 6c Su- sent in the adcarinal area. The free blade shows its maxi- dar (1990, p. 210) consider G.foliata inclinata as a syno- mum height in the anterior part and is composed of nym of G.foliata (Budurov). four or five denticles that form a convex crest. The cari- Range. Base of Longobardian to Late mun' na is composed of large denticles that end at about mid- Ju|ian, goensis - Z. (upper Gredleri Zone to up- length of the platform. In profile, the unit is arched and A.Z awrtformis (Kovacs E{ Kozur, 1980; Kovacs, turned down anteriorly. per Austriacum Zone) The lower surface has a small pit in the anterior 1983; Krystyn, 1983). third of the platform and the keel is wide, flat with sii- ghtly raised edges. Large elements (e.g. Pl. 2, fig. 9) show Genus Pseudofurntshius Yan den Boogaard', 7966 an increased platform with posterolateral expansion. Type species: Pseudofurnishius tnurcianus Van den Boogaard, 1966 Remarks. Budurwignathus sp. A differs frorn Bw' duroaignathus longobardiuzs in having a broad posterior platform with one prominent denticle at its centre, and Remarks. Diebel (1956, p. 432) found some specr- rounded anterior rnarginal denticles. Furthermore, in mens from Cameroon that he assigned to Spathognatbo' profile the former is much more arched posteriorly. .8. dus ? sp.inc. In the description he regarded as anterior mungoensis and .8. diebeli have a denticulated platform the part with the platforms and opposite to the inclina- and a continuous carina that extends to the posterior tion of the denticles of the blade. Van den Boogaard end of the piatform. (1966) established for these forms the genus Pseudofwr- Range. Upper Longobardian (diebeli A'Z^ sensu nishtus. He considered the platforms as posterior and Krystyn, 1983). Buduroatgnathus sp. A occurs in associa- suggested an orientation opposite to that proposed by tion with Buduroaignathus mungoensis, B. mostlerl, B. c[. Diebel. Some authors (Sadeddin, 1990; Gullo & Kozur, longobardicus and Gladigondolella tethydts. 1.989; 1991,, Sadeddin Ec Kozur, 1992; Eicher & Mosher, 1924) fo11ow Diebel's orientation, others favor Van den Gondolella foliata inclinata Kovacs, 1983 Boogaard's (Huddle, 1970; Van den Boogaard & Simon, Pl. 1, fig. 2-3 1973; Ramovs, 1977). PLATE 2 lJpper Ladrnian conoclonts from Sella Pass (PS) and Gardena Pass (PG) sections PS x 140. 3e) Upper Fig. 1a-b, 2, 3a-b Budurrrtignat|ttts ntostl.ert (Kozur). 1a) Upper vren'; lb) ion'er r,rer'; PS 8l x 15C.2) l,.rrerai view; 3; viev'; 3b) upper- laterrl viewl PS 3; x 14C. vrewl 4c) lateral vrer'.5) Later;rÌ vrex'; PS Fig. 4 r-c, 5 Pseudofurníshtus murcldnus prdecursor Gulio Ec Kozur. 4a) Upper view; 4b) lower 6r x 140. 11C' Fig. 6a-b Buciurougnathrs cf. l.ongobartiiczs (Kovecs). 6a) Upper vien'; 6b) loo'er vien'; PS 8; x lower vtew; 8c) iater,ri uew; PS 8; Fig. 7a-b, 8a-c, 9a-d - Bu;urooi-gnathus sp.A. 7.r) Upper view; 7b) lateral view; PS 8; x 130. 8a) Upper viev; 8b) x 130. 9a) upper Yier,; 9b) lower wiew; 9c) leteral vrew; 9d) lateral-lower view; PS 8; x 100. Pl. 2 Conociont biostratigrapby of the S. Cassiano Formation 48 A. Mastandrea, C. Neri €r F. Russo In our opinion the orientation proposed by Die- In the Stuores-Wiesen secrion (Pralongià, Dolomi- bel prevents confusion and it is consistent with other tes) mono-platform forms of Pseudofurnishius mwrcmnus platform elements. occur in beds containtng Tiachyceras aon. Range. Middle-Late Longobardian (middle and up- Pseudofurnishius murcianus praecursor per part o{ mwngoensis A.Z. sensuKoztr 1980). Gullo & Kozur.1.991. PL 2, fig. 4-5 Discussion on the straiigraphic setting of the Cas- sian platforms. 7980 Pseudofurnishius murcianus n.subsp. Kovacs 6c Kozur, pl. 7, î.ig. 6. The data reported above indicare rhar the S.Cassia- 1997 Pseudofurnishius murcianus praecursor Gullo & Kozrr, p. 77, pl. no Formation surroundine the Sella .1, fig. 9; ? pl. 5, fig. 1, 2. Massif is Late Ladi- 1994 Pseudofumìsbius murcianus praecrlrsor - Neri et al., pl. 1, fig. 2. nian in age. This conclusion raises the question of the corre- Remarks. Subspecies of Pseudofurnishius murcianus lation between the various Cassian platforms of the Do- with a reduced, narrow outer platform, often denticula- lomites (Fig. Z). ted and sometimes longer than the inner ones. Gullo & According to the currenr stratigraphic interpreta- Kozur (1991,, p. 77) established this subspecies on mare- tion, the "Cassian" (or post-volcanic) succession of the rial from the Sosio Vallev ( Sicily) and Spain. The aut- Dolomites is characterized by tzoo generations of carbo- hors chose as holotype the specimen iilustrated by Ko- nate platforms, either referred to the Late Ladinian-Car- vacs & Kozur 1980, pI. Z, fig. 6 as Pseudofurnishius mur- nian p.p. interval (Assereto et aI., 1977; De Zanche et cianus n.subsp. from Spain. The holotype of Pseudofur- al., 1993), or considered to be confined within the Car- nishius murcianus pldecursor is relatively stumpy and nian (Cordevolian-Julian) (Bosellini & Doglioni, 1988; shows a well developed inner platform with 5-6 denti- Masetti et al., 1991). cles on its surface. The outer platform is reduced to a The data presented in this paper, as weil as a re- row of denticles along the blade. Both platforms exrend view of data from the literature, indicate rhàt the strati- towards the anterior end. Our specimens, instead, are graphic succession between the Ladinian volcanics and very narroq slender, with a quite wide inner platform, the Raibl Formation is far more complex than pre- characterized by six denticles, two of which are situated viously thought. The post-volcanic succession of the on the platform margin, whereas the outer platform is Western Dolomites is characterized by several, though very reduced, rudimentarn with only one denticle. On not necessarily isochronous, episodes of growth and re- the lower surface, the basal cavity beneath the inner treat of carbonate platforms. The older post-voicanic platforrn is located anteriorly, a little before the midsec- platforms are documented in the Sciliar-Cime di Terra- tion of the r,rnit, and extends anteriorly and posteriorly rossa area (Brandner, 1991; Brandner er al., 1991; Yose, but does not reach the posterior end. In the paratype 1991; Frg. 1. andT). According ro rhese aurhors, two su- illustrated by Gullo & Kozur (1,991., pI. 4, fig. 9) and Catalano et al. (1990, pl. 3, fig. 1) the basal cavity is shifted completely into the posterior part. o AMMONOID CONODONT ZONES AMMONOID o Elements of Psewdofwrnísbius murcianus praecursor o 6 ZONES ZONES o o, have been regarded previously as falling within the vari- 6 f aó a a= (Krystyn,1983) (Kozur, 1 980) a o ability of murcianus (Eicher Mosher, 1974; F'a- P & z z movs, 1,977; Bandel Waksmundski, 1985). z Aonoides 8r On the tadpole J z J Aonoides z diebeli contrary, Gullo 6c Kozur (1991) regarded this subspecies (r l U z Aon Ò (f as a primitive form from which P nturctanus murcnnus o (f o O is derived. ln the latter no outer platform is present. Sutherlandi Regoledanus c!iebeli According to Kozur (1972; 1980; 1989), Van Den z z o z z Boogaard & Simon (1973), Hirsch (1973), Hirsch & f Macleami g z Archelaus mungoensls f d) É. Gerry (1974), Catalano et al. (1990) and Gullo & Kozur mungoensis o co z z Megine (1.989; 1991) the bi-platform are stratigraphically older (5 o J J z than the mono-platform elements. This opinion was G16dleri nungancus Poseldon hungaricus J ) confirmed by the discovery of the stratigraphically ol- dest forms (Pseudofurntshiws sosioensls Gullo & Kozur, Pseudofurntshtus prtscus Sadeddin and Pseudofurnishius Fig.6 - Zonrtron of the Longobardian-Julian (Upper Ladinian- siyaÌaensis Sadeddin & Kozur) that are exclusively of the Lower Carnran) based on :rmmonoids end conodonts .rc- bi-piatform type. cordìng to Krysryn (198J) rnd Kozur (1980). Conodont bios*atigraphy of the S. Cassiano Formation perimposed platforms occur in the post-volcanic succes- Richthofen Riff to the Aon Zone and the lower parr of sion of this area where they interfinger with volcanicla- the Sett Sass platform ro the Aonoides Zone. Mtre re- stic sediments (Marmolada Conglomerare, Wengen For- cently, De Zanche et al. (1993), De Zanche & Gianolla mation). The lo-r'er piatform progrades on a substrate (1995), Gianolla (1995) assigned the Cassian Dolomite 1 represented by volcanic products (piliow-breccia and pil- (Richthofen Riff) to the interval comprising the very lowJavas). These platforms are assigned to the Archelaus top of Regoledanus Subzone, r.he Daxatina c{. canaclensis Zone on the basis of the finding of a specimen pro- of Subzone and the lowermosr part of the Aon Subzone trachyceras archelaus near the top of so-called the (sensu Mietto tr Manfrin, 1995a; 1995b). In the standard "Schlernplateu beds", interpreted as the back-reef depo- stratigraphic scale of the Triassic (Zap[e,19g3), accepted sits of the second post-volcanic piatform (Brandner, by the authors of the present paper, the Daxatina cf. 1997, p.9, fig. 4). canadensis Subzone of Mietto & Manfrin (1995a; 1995b) The younger Cassian platforms are represented by corresponds to the upper part of the Regoledanus Zone. several dolomitic massifs located central-eastern in the Consequently, the Cassian Dolomite 1 is mostly Late Doiomites (Fig. 7): the Richthofen Riff-Sert Sass Mrs., Ladinian in age, although its uppermosr parr may be the Lagazuoi Mt. and its northern and eastern rermina_ attributeci to the Early Carnian. The so called ,,Cassian tions, the Gusela del Nuvolau Mt., the upper carbonate Dolomite 2" (..5., Sett Sass Mt.) is considered Carnian bodies of the Dùrrensrein Mt. (Picco Vallandro) di in age. Chronostratigraphic dara supporting this inter_ (Schlager et al., 1991). Chronostratigraphicaliy, the best pretation are based on: known platforms are probably represented by the the S. Cassiano Formation onlapping the Richthofen ") Riff and Sett Sass Mts. (Fig. 1 and Z), that Richthofen Riff (Urlichs, 1974; 1994); correspond ro rhe Lower and Upper Cassian Dolomite b) the basin succession outcropping at Ctan Zop- (Assereto et a1., 1977) and to the Cassian Dolomite 1 pè-Milieres, near the eastern termination of the Laga- and 2 respectively (De Zanche 1993; et al., De Zanche zuoi platform (Bizzarini & Braga, 1,987; Bízzarini et al., & Gianolla , 1995). Urlichs (1974; 1994) attributed the 1986; 1989); 'I z 3 SCILIAR - SEISER ALM SELLA MASSIF RICHTHOFEN RIFF- SETT SASS ---,t"^J z --' -J :< z Aonoides + | ú Austriacum -----l I Aon ----t l Reooted I z -- | --lI :' z o f1+-1-* v-++++ :1 : Post-volcanic basin successiorr cipil boufdefs volcaniclastic sandslone conglomerate with volcanic pebbles Fig.7 - Chronostratigraphic setting of the Sella platform compared s'rth the successions of Scilier-seiser Alm (from Brandner, 19911 Brandner et al., 1991) and of Sett Sass-Richthof"n Riff (from IJrlíchs 1974;1994; Neri et al., 1995). Abbreviations: SD. Sciliar Dolomite; Lv, Livinallongo Formation; V, volcanics; MCg, Marmolada Conglomerare; Cp, swarÍìs and lenses of carbonate olistoliths (Cipit boulders); lflengen V, Formation; CD, Cassirn Dolomite sensu latu (referred to all the post-volcanic platform$; SC, S. Cassra- no Formrtion; Dù, Dùrrenstein Dolomite; R, Raibl Formation; Dp, Dolomia principele. 50 A. Mastandrea, C. Neri & F. Russo c) the S. Cassiano Formation of the Cortina basin ìowstand deposits cannot be dogmatically accepted, in- lateral to the upper Cassian platform (e.g., the Tamarin ferring that the eustatic conrrol on rhe verrical stacking section, Mastandrea, 1994; Baracca, 1996). of different generations of carbonate platforms cannot On the basis of these sections, the uppermost ge- be unequivocally proven. neration of Cassian platforms may be referred to the The considerable number of post-volcanic carbo- Aonoides and Austriacum Zones of the Julian subst.rge. nate piatform episodes, the frcquent occurrence of car- The Seila Piatform, assigned to the latest Ladinian bonate megabreccia wedges and the wide hiaruses sepa- (Regoledanus Zone), occupies an intermediate position rating the platforms both from their substrate and the between the older and younger carbonate platforms. It overlying formations (Raibi, Dolomia Principale) sug- is younger than the post-volcanic platforms of the Sci- gest that the development of the "Cassian" carbonare liar-Denti di Terrarossa area (Archeiaus Zone) and older bodies occurred in a complex paleogeographic setting. than the latest Cassian platforms such as Sett Sass, Nu- Platforms nucleated on paleohighs, at differenr rimes -'^r^" r t* :- (Frs.7\.It vwLd||, LdbdLuvr,^^^-"^: rt rJ conceivable that a considerable \^ _ò' /' is sometimes difficult to resolve with biostra- chronologic overlapping exists between the Sella tigraphical tools the real succession of events, as rhe Platform and the so called "Cassian Dolomite 1" of De chronologic interval involved is relatively short (a few Zancb.e et al. (1993). Ve have no ilge data on some car- million years). Probably, the rnain conrrol on growth, bonate bodies such as Sass Beccè, at the Pordoi Pass retreat and dismantling of platforms was of recronic na- (Fig. Z). tentatively correlated to the second post-volca- ture, especially in the late Ladinian, at the time of the nic platform of the Denti di Terrarossa area (Fig. 7). huge megabreccia bodies embedded within Wengen-like In conclusion, J conser-vative interpretation sug- deposits. gests at least four episodes of growth of carbonate If rhis interpretarion is correcr, it is clear that the platforms in the Doiomites (Fig. 7). It is thus clear that Cassian succession of the Dolomites cannot be a reliable a sequence stratigraphic model based on two generltions standard for global sequence stratigraphic correlations. of carbonate platforms has to be rejected or significantly modified. A further aspect of the problem regards the Acknoaledgements. type of control on the sequence stratigraphic organíza- The ruthors rre gnreful to G. Leonardi for graphical supporr. tion: eustatic or tectonic? This question also addresses The rn rnrrse rirrl n..1q ;,-^-^..-l L,. . -.-^f,,t -:view bv A. the meaning of the several wedges of carbonate olisto- Nicora (Milano) and S. Kovacs (Budapest). Englsh revision by E. Fois. liths embedded in the post-volcanic basin succession. As Finrnci.rl support: MURST grant 40olo (E. Serpagli, Modena; pointed out by previous papers (e.g., Yose, 199I), the A. Bosellini, Ferrara) and CNR 96.00364 (F. Russo, Università della classic interpretation of the carbonate megabreccias as Calabria. CS). REFERENCES Assereto R., Bruscir C., Gaetani M. & Jadoui F. (1,977) - The Bizzaríni F., Laghi G.F., Nicosia U. & Russo F. (1989) - Pb-Zn minerabzation in the Triassic of the Dolomites. Distribuzione strartigraficar dei microcrinoidi (Echino- Geological history and genetic intepretation. Ind. Miner., ,.r----,-l --1r- E^"mazione di S. Cassiano (Triassico v. 28, pp. 267-3A2,Roma. superiore, Dolomiti): studio prelimrnare. Atti Soc. Bandel K. & \laksmundski B. (1985) - Trias conodonts from Nat. Mat Modena, r,'. 120, pp. 1-14, Modena. Jordan. Acta GeoL. PoLonica, v. 35, n. 3/4, pp. 288-304, Boogaard M.van den (1,966) Post-Carboniferous conodonts \flarzawa. from south-eastern Spain. Proc. Kon. Ned. Akad. lVet., Baracca A. (1996) - Ammoniti e biostratigrafia dei Ladinico v. 69, pp. 691.-698, Amsterdam. sup.-Carnico delle Dolomiti (Triassico medio-sup., Alpi Boogaard N4.van den & Simon O. (1973) - Pseudofurnishius Meridionali). Tesr di dottorato rnedita, Università di Mo- (Conodonta) in the Triassic of Betic Cordilleras, SE dena. Spatn. Scripta GeoL., v. 16, pp. 1-18, Leiden. Brzzartm F. & Braga G.P. (1987) - Considerazioni bio e litostra- Bosellini A. (1982) - Geologia dei Passi dolomitici clrcostan- tigrafiche sulla Formazione di S. Cassiano (Dolomiti ti il Gruppo del Sella. In Casteilarin A. & Vai G.B. Nord-Orientali, Italia). Studi Tient. Sci. Nat., Acta GeoL., (Eds.) - Guida alla Geologia del Sudalpino Centro- v. 64, pp. 39-56, Trento. orientale. S.G.l. Guide Geologiche Regionali, pp. 267- Btzzarrni F., Laghi G.E, Russo F. & Urlichs M. (1986) - Preli- l/ I, ftoIoqna. minary biostratigraphic correlation between Ampezzo ba- Bosellini A. (1t84) - Progradation geometries of carbonate sin sections and the Cordevolian stratotype (Late Triassic, platform: examples from the Triassic of the Dolomi- Italian Dolom:nes). Laoori Soc. Wneta Sc. Nat., v. 11, pp. tes, northern h.l.lry. Sertimenrology, v. Ji. pp. 1-24, Am- I ')r-rfò- venezla. sterdam. Conodont biostratigraphy of the S. Cassiano Formation 51 Bosellini A. (1991) - Geology of the Dolomites. An Introduc- De Zanche V & Granolla P (1995) - Litostratigrtrfia al limite tton. DoLomieu Conference on Carbonate Platform.s and. Ladinico-Carnico (Sudalpino orientale). Annali [Jniz,er. Dolomitization, pp. 1-43, Ortiser. sità di Ferrara, 5 (Sr.rpplernento), pp. 41-,1g, Ferrara. Bosellini A., Castellarin A., Doglioni C., Gr-ry F., Peri M.C., Eicher D.B. & Mosher L.C. (I974) - Triassic conodonrs frorn Rossi P.M., Simboli G. & Sommavilla E. (1982) - Geo- Sinai and Palestine. Journ. Paleont, v. 48, n. 4, pp.727- logia della conca di Arabba e dei rilievi circostanti. In 739, Tirlsa. Casteliarin A. & Vai G.B. (Eds.) - Guida alla Geologia Fois E. & Gaetant M. (1980) - .fhe northern nargin of the del Sudalpino Centro-orientale. S.G.1. Guide Geolopiche Civetta buiidup. Er,'olution clnring the Ladinian and the Regionali, pp. 243-254, Bologna. Carnian. Ria. It. Paleont. Strat., v. 56, pp. 469-541, Mila- Bosellini A. & Doglioni C. (1988) - Progradation geometries no. of Triassic ciÌrboniìre piatforms of the Dolomites rnd Gianolla P. (1995) - Str:rtigrafia seqr.renziirle el limite Ladinico- their large-scnle physical stretigraphy. AAPG m.ed.iterra- Carnico (Sudalpino orientale). Annali Uniaersità di Fer. nean Basins Conference, Field 7iip, Guidebook 42 pp., rara, 5 (Srpplemento), pp. 49-57, Ferrara. Nice. Gullo M. & Kozur H. (1989) - Pseudofurnishius sostoensts Bosellini A., Lobitzer F{., Brirndner R., Resch W. & Castella- n.sp., :r neq' conodont species from the Late Ladinìan palàont. rin A. (1980)- The complex basins of the C;rlcareous of Sosio valley, n.estern Sicily (Italy). Geol. Mttt. Ibk., v. 16, Alps and p:rleom;rrgins. 26 Im. Geol. Congress, Exc. pp. 2C7-2ll,Innsbruck. 129 C, Abh. Geoi. 8..A.,v. 34, pp. 287-325, Wien. Gullo M. & Koz-ur H. (1991) - Taxonomy, Stratigraphic and Paleogeographic Bosellini A. & Neri C. (1991) - The Sella Platform (Upper significance of the L:rdinian-Early Cirr- niirn conodonr genus Pserrdofirrnishius. Tri:rssic, Dolomites, Italy). Dolontieu Con/èrence on Car- Palaeontographi- ca Al:t. A, r,'. 218, pp. 69-86, Stuttgart. bonate Platfornrs and Dolonitization, GuicJebook Excur- Hirsch F. (1973) sion B. pp. l-30. Ortisei. - Middle Triirssic conodonrs frorn Israel, southern France irnd Spún. Mitt. Ges. Geol. BoseÌlini A. & Rossi R. (1974) - Tri:rssic carbon:rre buildups Berbau.stud., v. 21, pp. 811-828, Innsbruck. of the Dolomites, northern Italy. In Laporte L.F. (Ed.) Hirsch F. & Gerry E. (1974) - Conodont- :rnd Ostracode-bio- Reefs in Time rnd Sprce. 5EP,44 Spec. Publ., r' 18, pp. -friassic stratigraphy of the in Isr:rel. In Ztpfe H. (Ed.) - _U7-ZJJ. lulSiì. Die stratigr:rphie der alpin-mediterr:inen Tri.rs. ó_,reri: Bramdner R. (1991) Geological setting :rnd srr:rrigràphy of Akad. \N/iss. Scbriftenr. Erd-eiss. Kontm., v. 2, pp. 107- the Schlern-Rosengarren buildup and Seiser Alm basin. 114, Vien. In Brandner R., Fliigel E., Koch R. & Yose L.A.- The Huddle J.\f. (1970) - Triassic conodonts from Israei. US. northern margin of the Schlern/Sciliar-Rosengirrten/Ca- GeoL. Surt. Prof. Pap., n.700-8, pp. 1.24-1-3A, Vashington. tinaccio platform. Do/ontieu Conference on Carbonate Kenter J.A.M (1990) - Carbonate platform flanks' slope irngle Platform and Dolontitization, Guidebook. Excursion A, ,rnd sediment fa,bric. Sedintentol.ogy, r'. 37, pp. 777-794, pp. 4-16, Ortisei. Amsterdam. Bnndner R., Fliigel H. & Senowbari-Daryan B. (1991) - Mi- Kov:rcs S. (1983) On the evolution of excelsa-stock in the crofacies of c:rrbonirte slope boulders: indic:rtor of the Upper Ladinian - Crrnirn (Conodonta, Gents Gondo- source area (Middle Triassic: Mahlknecht Cli{f, Western LeLLa, Tria,ssic). Osterr. Akad. lYiss., Scbrtftenr. Erdteiss. Dolornites). Facies, v. 25, pp. 279-296, Erlangen. Komm., r'. 5, pp. 1C7-120, Vien. (1973) Budurov K.J. - Carinel/a n.gen. r.rnd revision der Gat- Kovircs S. & Kozur H. (198C) Strltigraphische Reichw-eite tung Gladigondolella (Conodonta). C.R. Acad. Bulg. Sci., der wichtigsten Conodonten (ohne Zahnreihencono- v. ?6, n. 6, pp.799-802, Sophia. donten) der N{ittel - und Obertrils. GeoL. Palàont. Mitt- Budurov K.J. & Sudar M.N. (1990) - Late Triassic Conodont lbh.. y. 13. n. l. pp. 47-zS.lnnsbnrck. Stratigraphy. Cottrier Forsch..lnst. Senckenberg, v. 118, Koznr H. (1972) - Die Conoclonteng2ìtrùng Metapolygnathus pp. 203-239. Frenkfr.rrt ;r. M. Hayashr 1968 und ihr srr:ìrrgraphrscher Wèrt. Geol. Crtirl;rno R., Di Stefano P., Gullo M. & Kozur H. (1990) - Palàont, Mitt. Ibk., r'.2, n. 11, pp. i-37. Innsbruck" Pseudofurntshias (Conoclonta) in peiagrc Late Ladinran - Kozur H. (1980) Revrsion cler Conodontenzonierung der Early Carnian sediments of wesrern Sicily and its strati- Mittel- und Obertri:rs des tethyirlen Faunenreichs. Geol. grrphic and pileogeogruphic significance. BoLL. Soc. Palàont. Mitt, Ibk., v. 10, pp. 79-172.Innsbmck. GeoL. It., v. 109, pp. 91-101, Roma. Kozur FI. (1989) The taxonomy of the gondolellid cono- -Iriassic. Chhabra N.L. td Kumar S. (1992) - Late Scythian rhrough donts in the Permian and Courter Forsch. -[nst. E;rrly Carnian conodont rssemblages and their biostra- Senckenberg, r'. 117, pp. 4C9-469, Fr:rnkfurt a. M. tigraphic irnport:rnce frorn off shore carbonates of Kozur FI. & Mock R. (1972) - Neue Conodonten aus der northern Kumaun, Tethys Himalaya, India. Reo. Micro- Trias der Slon'akei und ihre str;rtigr;rphiscire Bedeutung. paiéont-, v. J5, n. 1, pp.3-21, Peris. Geol. Palìiont. Mitt, Ible,, v. 2, pp. 1-20, Innsbruck. Diebel K. (1956) - Conodonten in der Oberkreide von K:rme- Kozur H. & Mostler H. (1971) - Probleme der Conodonren- rrn. Geologie, t 5, pp. 424-45a,Ber\n. forschung in der Trias. Geoi, Palàont. Mitt. Ibk., v. 1, De Zanche V., Gianolla P, Mietto P., Siorpaes C. & Vail P.R. pp. 1-19, Innsbruck (1993) - Triassic sequence stratigraphy in the Dolomites Kristan-Tollmann E. Ec Krystyn L. (1975) - Die Mikrofauna (IraIy). Mem. Sc. GeoL., v. 45, pp. I-27,Pado:,a. der ladinisch-karnischen I-Iirllstatter kalke von Saklibeli JZ A. Mastandrea, C. Neri & F. Russo (Taurus-Gebirge, Turkei). Sitzung. Osterr. Akad. lYiss. Viesen, Dolomiti). Annali Uniuersitìr di Ferrara, 5 math.-naturleiss. KL., Abt.l, v. 184, pp. 259-340, Vien. (Supplemento), pp. 59-7 4, Ferrara. Krystyn L. (1980) - Stratigraphy of the Hallstatt region. In Ogilvie M.M. (1893) - Contributions to the geology of the 'Slengen Schònlaub H.P. (Ed.) - Second European Symposium. and St. Cassian Strata in Southern Tyrol. ECOS II. Abh. Geol. B.-A.,v.35, pp. 61-98, Wien. Quart. Journ. Geol. Soc., v. 49, pp. 1-78, London. Krystyn L. (1983) - Das Epidaums-Profil (Griechenland)-ein Ogilvie Gordon M.M (1929) - Geologie des Gebietes von Pie- Beitrag zur Conodonten-Standardzonierung des tethya- ve (Buchenstein), St. Cassian und Cortina d'Ampezzo, len Ladin und Unterkarn. Òrterr. Ahad. Wiss. Schriftenr. Jabrb. GeoL. B. Anst., v.79, pp. 357-424,'XIren. F.,1..';," K^** ,- 5,pp. 23 1_258, lfien. Ramovs A. (1977) - Skellettapparat von Pseudofurnishius mur Leonardi P (Ed ) (1967) - Le Dolomiti. Geologia dei monti cianus {Conodontophorida) im Mitteltrias Sloweniensis tra Isarco e Piave. 2 V., 1019 pp., Edizioni Manfrini, (N\l Jugoslawien). N. Jb. Geol. Pàlaont. Abb., v. 3, pp. Rovereto. 36I-399, Stuttgart. Leonardi P. & Rossi D. (1957) - La scogliera coralligena dei Reithofer O. (1928) - Geologie der Sellagruppe (Sùdtiroler Sella nelle Dolomiti occidentali. Ann. Unip. Ferrara, s. Dolomiten). Jb. Geol. Bundensanst., v. 78, pp. 529-579, 9, v. 3, n. 1,, pp. I-36, Ferrara. Wien. March M., Budurov K., Hirsch F. Er Marquez-Aliaga A. Sadeddin \í. (1990) - Pseudofurnishius priscus n.sp. (Conodon- (1988) Sephardiella nov. gen. (Conodonta) emenciation ta) and its stratigraphical significance for the Ladhran of Carinella (Budurov, 1973), Ladinian (Middle Trias- (Middle Triassic) in Jordan. N. Jb. Geol. Pàlaont, Abh., sic). In Ziegler \f (E,d.) - 1st International Senckenberg v. 178, pp. 369-382, Stuttgart. Conference and 5th European Conodont Symposium Sadeddin'W. & Kozur H. (1.992) - Pseudofurnisbius siyalaensis (ECOS V). Contributions I, p^rt 2, Cowrier Forsch. n. sp. (Conodonta) from the Lower Ladinian of \fladi Inst. Senckenberg, v. 7A2, p. 247, Frankfurt a. M. Siyala (|ordan). N. ]b Geol. PàLaont. Mh., pp. 359-368, March M., Budurov K. & Hirsch F (1990) - Sephard.ielLa nov. Stuttgart. gen. (Conodonta), emendation of Carinella (Budurov, Schlager V., Biddle K.T. & Stafleu J. (991) Picco di Vallan- 1973), from the Ladinian (Middle Triassic) type area in dro (Dùrrenstein) A platform-basin transition in Catalonia (N.E. Spain), Sephardic Province. Courier outcrop and seismic moàel. DoLomieu Conference on Forsch.-lnst. Senckenberg, v 118, pp. 197-201, Frankfurt Carbonate PLatform and DoLomitization, Guidebook Ex- a. lvl. cursion B, pp. 1.-22, Ortisei. Masetti D., Neri C. & Bosellini A. (1991) - Deep-water asym- Urlichs M. (1974) - Zur Stratigraphie und Ammonitenfauna metric cycles and progradation of carbonate platforms der Cassianer Schichten von St. Cassian (Dolomiten, governed by high-frequency eustatic osciilations (Trias- Italien). Ósterr. Akad. IYiss. Schriftenr. Erduisl Komm., -fliien. sic of the Dolomites, ltaly). Geology, v. 19, pp. 336-339, v. 2, pp. 2A7-222, Boulder. Urlichs M. (1994) - Tiaclryceras Laube 1869 (Ammonoidea) Mastandrea A,. (1994) - Carnian conodonts from Upper Trias- aus dem lJnterkarn (Obertrias) der Dolomiten (Italien). sic strata of Tamarin section (San Cassiano Fm., Dolo- Stuttgarter Beitr. Naturk., B, n. 217, pp. 1-55, Stuttgart. mites, Italy). Riv. It. Paleont. Strat., v. 100, pp. 493-510, Vrielynck B. (1987) - Conodontes du Trias perimediterra- Milano. neen. Systematique, stratigraphie. Docum. Lab. Géol. Mietto P. & Manfrin S. (1995a) - La successione delle faune ad Lyon,v.97 (1986), pp.1-301, Lyon. ammonoidi al limite Ladinico-Carnico (Sudalpino, Ita- Yose L.A. (1991) - Sequence stratigraphy of mixed carbona- lia). AnnaLi [Jnipersiù di Ferrara,5 (Supplemento), pp. telvolcaniclastic slope deposits flanking the Sciliar 73-35, Ferrara. (Schlern)-Catinaccio buildup, Dolomites, Italy. In Mietto P. & Manfrin S. (1995b) - A high resolution Middle Brandner R., Flùgel E., Koch R. & Yose L.A.- The Triassic ammonoid standard scale in the Tethys Realm. northern margin ol the Schlern,/Sciliar-Rosengar- Preliminary reporr. Ball. Soc. Géol. France, v. 166, pp. ten/Catinaccio platform. Dolomieu Conference on Car' 539-563, Paris. bonate Platform and Dolomitization, Guidebook Excur- Mojsisovics E. M. von (1.879) - Die Dolomit-Riffe von Sùdti sion A, pp. 1.7-39, Ortisei. ro1 und Venetien. Beitriige zur Bildungsgeschicbte cler Al- Zapfe H. (1983) - Das Forschungsprojekt "Triassic of the pen. 559 pp., Vien. Tethys Realm" IGCP Proi.a). Abschlussbericht. Òsterr. Mosher L.C. (1968) - Triassic conodonts from western North Ahad. lYisl Schriftenr. Erdu.,rss. Komm., v. 5, pp. 7-L6, America and Europe and their correlation. Journ. Pa' Wien. leont., v. 42, n. 4, pp. 895-946, Tulsa. Neri C., Mastandrea A., Laghi G.F, Baracca A. Er Russo F. (1994) - New biostratigraphic data on the S. Cassiano Formation around Sella Platform (Dolomites, Italy). Pa- leopelagos, v. 4, PP. 13-21, Roma. Neri C., Russo F., Mastandrea A. & Baracca A. (1995) Lito stratigra{ia, ammonoidi e conodonti della Formazione 1996; accEted 31' 1997 di S. Cassiano: la sezione dei Prati di Stuores (Stuores- Receiaed. Ncnember 12, January