Of the Carnian Stage

Rivista Italiana di Paleontologia e Stratigrafia volume I u) numero 1 tavole 1-10 pagne 37-78 Aprrle 1999

THE PRATI DI STUORES/STUORES \TIESEN SECTION (DOLOMITES, ITALY): A CANDIDATE GLOBAL STRATOTYPE SECTION AND POINT FOR THE BASE OF THE CARNIAN STAGE

CARME,LA BROGLIO LORIGAI, SIMONETTA CIRILLI2, VITTORIO DE ZANCHE], DONATO DI BARI4, P]ERO GIANOLLA], G]AN FRANCO LAGH14, \íILLIAM LowRIEs, STEFANo MANFRIN]. ADELAIDE MASTANDREA4, PAOLO MIETTOs, GIOVANNI MUTTbNI5, CLAUDIO NERI1, RENATO POSENATO', MARIACARMELA RECHICHI4, ROBE,MO RETTORI2 & GUIDO ROGHI3

Receioed August 20, 1998; accepted February 23, 1999

Key-*^ords: Carnian, Biostratigraphy, Ammonoids, Conodonts, rari brachiopodi sono limitati aila pane medio superiore della sezio- Palynomorphs, Foraminifers, Gastropods, Bivalves, Brachiopods, Mi- ne (Kaninckina leonbardi, Retzia sp.), dove pure si rrovano nove spe- crocrinoids, Holothurians, Magnetostratigraphn Sequence stnti cie di gasteropodi. Un picco di diversità tassonomica molto netto ri- graphy, Dolomites, Southern Alps. guarda i foraminiferi bentonici isolati e le scleriti di oloturie ed è palese nella parte superiore delia Subzona a Duatina cf. canadensis. Riassunto. \il/iesen La sezione di Prati di Stuores/Stuores (For- In panicolare, vi compaiono scleriti finora segnalate nella Subzona ad mazione di San Cassiano), affiorante nei dintorni di Pralongià, a S$l Aon. le variazioni in frequenza e drversità tassonomica di queste fau- di San Cassiano/St. Kassian, sul versante meridionale del crinale che ne mìnori suggeriscono condizioni anaerobiche-disaerobiche del fon- separa la Val Badia/Abtei dalln Val (BL), @Z) Cordevole è nota come dale nella pane rnedio-inferiore della sezione (O-105 m), quindi una sezione tìpo del Cordevolico. In tempi recenti sono stati individuati tendenza ad ossigenazione più stabile nella pane superiore. La ma- al di sotto della tradizionale Zona ad Aon, numerosi livelli am- con gnetostratigràfia mostra quattro intervalli a polarità normale e rre a monoidi della Subzona a Regoledanus (Zona aProrrachyceras), seguiti polarità inversa. La base della Subzona a Daxatina cf. canadensis è da altri dove compaiono in panicolare i generi Daxatina (Daxatina prossima alf intervallo di polarità noimale S2n. Dal confronto con i sp., D. cf. canadensi), Clionitites e Trac/ryceras, quest'ultimo rappre- dati paleomagnetici della coeva sequenzà di Mayerling (Austria), ri sentato da specie diverse da T aon, Daxatina, genere ritenuto tìpico sulta che il tasso di sedimentazione a Stuores è circa otto volte supe- delle medie ed alte latitudini, risulta pertanto cosmopolita e Tiachyce. riore a quello dei carbonati pelagici della serie austriaca e che h pri ras) taxon delle medie e basse latitudini, viene confermato in livelli ma presenza di D. cf. canadensis può cadere nella pane inferìore della che precedono le faune ad Aon. Nella sezione è stata definita una Zona a Diebeli della suddetta serie. Sulla base degli ammonoic{i, degli nuova unità. biostratigrafica, 1a Subzona a Daxatina cf. canadensis altri gruppi fossili e dei dati rnagnetostratigrafici unìt:rrnente ai requr- (Zona a Trachyceras) Carnico, nella presenf,r riferibile al quale sono siti storici, si propone rl FAD di Daxatina corne mr.ker della base "Anolcites" anche ex gr. laricus, fustoceras n. sp. A, Asklepioceras e del Carnico e la sezione di Prati di Stuores. come GjSP del lìrnite Muensterites. Il FAD di Daxatina viene indicato come marker del li- Ladinico-Carnico. mite inferiore dell'unità. Tale limite cade all'interno della Fm. di San Cassiano, pochi rnetri al di sopra del limite con la Fm. di La Valle. Abstact. The Prati di Stuores/Stuores -Wiesen section (Dolo- La comparsa di Tiacltyceras aon ne segna il limite superiore. La subzo- mites, Italy) is proposed as a candidate Global Stratotype Section and na è individuabile anche in altre sezioni delle Dolomiti. I conodonti, Point for the base of the Carnian Stage. In addition to being a fa- molto scarsi in tutta la sezione fino a mlncare nella pane bassa della mous, richly fossiliferous localitn it includes the type-section of the Subzona a D. cf. canadensis, si inquadrano nella Zona di associazione Cordevolian substage. The section is located near Pralongià, along a Budurnignatus diebeli. GondoLeLla poLygnatbiformis, segnalata nella the southern slope of the crest selìrr!Ìting the Badia/Abtei and Corde- Subzona ad Aon, manca sia nella Subzona a Regoledanus sia in quella vole valleys. Below the levels witb Tiaclryceras d.on, the secrion con- a D. cf. canadensis; il suo significato di marker della base del Carnico, tains a rich ammonoid fauna that characterizes the upper parr of rhe come proposta in questo lavoro risulta discutibile. Nella ricca palino- Regoledanus Subzone and subsequently records the first àppearances flora presente poco sopra il FAD di Dautina sr individua la fase a of the mìd-high latitude genus Daxatina (Daxatina sp., D. cf. canaden" vigens -densus, già segnalata nella Subzona ad Aon. I foraminiferi ben- sls) and of traditional Tracbyceras wìth species different from T actn. tonici (sezioni sottili e iavati) sono rappresentati da specie nore so- Therefore, the Daxatina cf. canadensis Subzone is recognised above prattutto nel Carnico della Tetide. Alcune specie ad affinità carnica the Regoledanus Subzone. Very rare conodonts of the Budurwignatus sono già presenti al di sotto della prina comparsa di Daxatina (es. group and species of Gladigondolella from the diebeli Assembl.age Gsollbergella spiroLoculiftrmis). I bivalvi appartengono a tre morfotipi Zone occtr. GondoleLla polygnathtfurmis, already known from the di Posidoniidi ("Posid.onia" uengensis, "P" cf , uengensis, ? Halobia).I Aon Subzone, is absent. Palynornorphs, foraminifers, gastropods, bi-

1) Dipanimento di Scienze Geologiche e Paleontologiche - Università di Ferrara - Corso Ercole I d'Este, 32 - 44laA Ferrara E-mail: [email protected] 2) Dipartimento di Scienze della Terra - Università di Perugia -Ptazza dell'Università - 06100 Perugia. 3) Dipartimento di Geologia, Paleontologia e Geofisica - Università di Padova - Via Giotto, 1 - 35132 Padova. 4) Dipartimento di Scienze della Terra - Sezione Paleontologia - Università di Modena - Via Università,4 - 41100 Modena. 5) Institute of Geophysics - ETH Hoenggerberg - 8093 Zùrich. 38 C. BrogLio Loriga et al.

Fig. 1 - Location of the Prati di Stuores/Stuores ^ Cassiano\9 Sliesen area PIZ LA VILLA rnd sr rarigrephic secrions. ,' .2078t8/ ì- t/ l \q Sections 1 and 1 bis corre- _-_a spond to rhe column in Fig. I I and 13. Section 2 corre- I ,i sponds to the Stuores $íre- "."Í):N] sen section in Urlichs (1974, i >-( /-\!, ) /Q 1.994) and to section SW5 in ''lt ly- )) Neri et al. (1995). \r\\! ge, in lccordance wirh rhe gui- |I \\ /;-- *d--=\\ ,!"- \ delines for establishment of GSSP (Remrne er al., 1996). The Stuores section consists of .1, two parts (Fig. 1, and 3). The 'westernmost part, herein named valpafo a section l. corresponds exactJy SETISASS with section SV4 of Neri et al. ,l (1995) and with the section i1lu- \ ..-----".. . \ Q 1"" 2 3Km strated by De Zanche & Gianol- la (1995) and by Mietto Er Man- frin (1995b). The latter extends wIr*N downward for about 20 m below stake 1, which marks the base of the section described in this paper. The top of section L may be correlated to a short section (section 1 bis) located slightly to the east and separa- ted from section i by faults of modest throw. Section 2 lies further to the east and corresponds to the Stuores Wiesen section of Urlichs (1974, 1994) and to section SW5 of Neri et al. (1995). Due ro recronic omis- sion, the base of secrion 2 can- j\Frl\^./ \ \.r-.< / not be correlated with the top r P SoOm of section 1bis. Further details t:: on the relationships between the Stuores section as used he- vaives, brachiopods, microcrinoids and holothurian sclentes were stu- rein and the section in Urlichs (1974, 1994), s/ere given died. Variations in frequency and taxonomic diversity of these faunas by Neri et al. (1995). In the present paper, rhe rerm suggest anaerobic-disaerobic bottom conditions for the lower-middle pan of the section (0-105 m), followed by a more stable oxygen con- section 1 and lbis refers ro the Prati di Stuores/Stuores \Wiesen tent in the upper portion. Magnetostratigraphy showed four intervals section. The section supplied a rich ammonoid with normal polarity and three interuals with reversed polarity. The fauna which predates the first appearance of Tiaclryceras Daxatina cf. canadensis Subzone falls close to the normal polarity and includes the genus Daxatina, a taxon particuiarly interval S2n. The present study proposes the FAD of the cosmopoli- significant in global correlations (Mietto Manfrin, trn genus Daxatina xs the marker of the base of the Carnian Stage, & placing it at a lower stratigraphic level than previously indicated in 1995a, b). This cosmopolitan genus allows correlations the Stuores area. The Prati di Stuores section is proposed as GSSP of between different paleolatitudinal provinces. The use of the Ladinian-Carnian bounciarv. its first appearance as a criterion for recognizing the base of the Carnian Stage is proposed, which would pla- ce this boundary at a stratigraphic level lower than pre- lntroduction. viously adopted in the same area (cf. Urlichs, 1974, The Prati di Stuores/Stuores ltriesen section (Do- 1994; Krystyn, 1978). lomites, Italy) is proposed as a candidate Global Strato- The Stuores section 1 was marked permanently type Section and Point for the base of the Carnian Sta- with twenty stakes to permit accurate localisation of the Prati di Stuores section, a GSSP candidate 39

. Pruri di Stuores,/Sruores Wi.- sen section at the head of the Cordevole valley. Setfsqss

sampling sites. Other fossil groups, magnetostratigraphy varian Alps near Berchtesgàden, less than 20 km south and sequence stratigraphy were investigated recently, of Salzburg (e.g. Allasinaz, 1964). Differences and/or discrepancies with previous studies No substantial modifications were made to this (e.g. Mretto & Manfrin, 1995b; De Zanche & Gianolla, scheme until the sixties. when stratigraphic research re- .work 1995; GianolIa, 1995; Roghi, 1995) may result from the sumed with the of Jacobshagen (1961), Allasinaz re-measurement and standardization of the stratigraphic (1964), Tozer (1967), Kozur (1976) and others. On the section. The Authors responsible for the various fields basis of the major bioevent philosophy, Krystyn (1928) of study are indicated at the beginning of each chapter. considered the distinction between the Aon and Aonoi- des zones to be of little importance. He proposed a sub- division of the Carnian strge into two parrs, the lower Historical Background. corresponding to the sr"rbstage, pius the Cordevo- (Carmela Broglio Loriga) Julian lian, and comprising the Aonoides, Austriacum and "Sr- The name Carnian was introduced in 1869 by renites" Zones, and the upper corresponding to the Tu- Mojsisovics to define the stratigraphic interwal corre- valian. This proposal was rejected by Bizzarini et al. sponding to the Trachyceras aonoides Zone. Mojsisovics (1986) and Urlichs (1994). On the basis oi ammonoid (1869) listed six iocalities, ar rhat time under Austro- biostratigraphy in the Southern Alps, and particularly Hungarian ru1e, where these rocks crop out. Flowever, in the Prati di Stuores section, Urlichs (1.974, 1994) con- the origin of the name Carnian (Karnische StufQ ís un- sidered the original zonal statement of Mojsisovics to be cerrain. According to Tozer (1967, 1984) it derives from stiil valid and therefore maintained the use of the Cor- the province of Carinthia (Kàrnten), within which the devolian substage. locality of Raibl (ancient name of Cave del Predil), ex- The criterion adopted by most workers for reco- .was piicitly indicated by Mojsisovics, situated. Alternati- gnizing the base of the Carnian has been the first appea- vely, GaetanL (1995), though referring to the Raibl suc- rance of the genus Tiacbyceras. This event is believed to cession in Carnia, considers that the name derives from occur at the base of the Aon Subzone/Zone in the the Carnian Alps, although the section actually occurs Tethyan domain, while in North America it lies within in the Julian Alps. the Desatoyense Zone (Tozer, 1967, 1984, 1994). Mojsisovics, Waagen & Diener (1895) redefined Mietto & Manfrin (1995a, b) defined a strati- the Carnian Stage within their chronostratigraphic revi- graphic interw;l, charecterised by Daxatina, Clionitites sion of the Triassic, and subdivided it into the Cordevo- and species of Tracbyceras different from Z aon, whtch, lian, Julian and Tuvalian substages, corresponding rein the Stuores section, is located below the traditional spectively to the Tiachycerts aon, T aonoides anà Tiopites base of the Carnian. These biostratigraphic data encou- subbul/atus ammonoid zones. The term Cordevolian is raged these two authors to suggest that the base of the derived from the Cordevole Valley in the Dolomites, Carnian should be placed at a lower stratigraphic level. near the head of which the Stuores section occurs. The thus including the upper part of the Frankites regoleda- name Julian comes from the Julian Alps, in which the nus Zone (Krystyn tn ZapÍe, 1983) in the Cernian, a Raibl/Cave del Predil section mentioned above occurs, zone usually considered Ladinian and correlated with and Tuvalian is derived from Tuval. a locality in the Ba- the Frankites sutherlandi Zone of North Americ.r. C. Broglio Loriga et al.

I lÉ lÉ | € lforaminifers]s I t I I Fig.l str.rtigr.rphicposirionorrhe | - els'ìlEiF16]Èl mosrpaleonrologicsrtnpres lbis I p'ri I r=: I F I U E I b È | H I È I ì | .l throughout the di | ,oo 15 1 I S I' .U | 3 I } 1 È l- sruoressecrron(seereblesr- I l--l-l ].*rol I S. ] | È 1- I S lcl zforthecornpletes:mple | ,".i--f--l- ]swzsl I I i I ' ILL' Posirion). Stakes =, isgztl I I I i I I I l--,)- fzz ! | | I ] ,.^ | E l'*'] I I I I I I cresrrrabout2l5Om,downro tn o''" ahitude I É E i l,**, I . l,n.*oo [..*,o.r,l I'n"*oo I r" ol- 1980 m. It then continues beyond the crest and | ,ro-]€ É i l;::Wf i i 1,,.*u.* | i'**'..1 i j ra >""S ffi lr*,*i"-"'" i 1,..*0.,,r.*,r.rl"t*'oi'."'o.u ' .nd, ar the foot of the Richrho- | ,*F+ i | | i i | 1 fenRiffandtheSettsass(Fig.t). I F IEWó' lll:WJI I l17sw60 lrzsw+.ao i i?sw60 I I The section is accessible via foot- rz path no' 23 Flotel I >,*-ffi l'*' lì;;;ì; l.*"o,o.o l,u"*,,0]'"*o'o i i,,.*,'.] ] c'A'I' from - ,] pralongià towards Sertsass, a few E i l,u.*,uol Itu.*r.o ],u.*u.* I,u"*uolru.*ro ] 1b-1OF1a6-|==! | ]'**..*l I lOl hundredmetresEsEofPizStuo- "*ol,u.*'oi res (218i m)' Pralongià mav be ] ro o-,.0_13 E=2 ] I l"*'u'o l,o.*,u],0.*0.*l llnWl::] | | .*"1 I I 1,..*rì1,**,.1 l_l reachedbychair-iiftorbydirt I ll ] I I li3swsor I I ]t-l roadbothfromsanCassiano/St. t3 o-^^ I 12ol.7# ].*r, I l'rt*'oori ] | Kassiun and Corvara (Badia/Ab- | | sw.oo-.--' I I I ,,swoo q6 tei Valley) and from Arabba i V:- | ]'r.*', l,rr*..,, ',.*o.o I i >..^ jswzn j'oswvrr (Cordevole 111-12 tto l=> ] ,0.*ro 'to"*u*,0.*0.,|1::yg:: ]""*"] i i Valley). l---l._ | ] ]swuuo.o i I I r'-r 10>'u n,o, + i I lswulo i I i+ i i l.*,,,..u ]n"*'o l**.* ] ]'.*'" I i tithostrarigraphy 9 > Fù{rzr I É i:w:n ;"",^,,, ,.*roo I ,"-,.,-- tD (VittorioDeZanche. no $ i':*n i;;;; i**" ;;;;; ."*.. ]!:;1: ' piero Gianolra & cr.'rdio Neri) , gF ]$ r"*,.i"*t l ! ,.*o.oolr.*,oul, , *€ . prati i FSBlfi i,*ouo i 1ìilí3i i^-., i The di Stuores /Stuo_ tf- i I i::y:^'"1"",^,."^ res viesen section is famous I to' ' ,, ] i i o-] | ffi ]r*, llSWÀ%'] l|ÈWiig'pSWlt'1 1 ,r.""r., to the ctassical works by u.*,, Irau,'rr.r (1834), \rissmann & I u o + ].*u I b:W6ff 1..*..F*,'] | I * ]+ ] uo.*u, 1 1O I Mùnster (184i), Klipstein (1845), uo l##u1. pSWlí;3 - Laube_(186e), Mojsisovics (1882), I >- E i.*,"..]*-" ,.*,,, ut*'oo.",^,."" ] | so-J---T ,.. i I i u.*ro | I | and Ogilvie (1S93), in which i.*ou.o],.*u 1 331?î3 l5sw610 | peoloq + --]!.q.d-l l'.'*|:Swxli!l]li;.,,"-.. I uo*= 1s-w4l l*..,. ::::: l= f.,f:;:;,::'il:?ii*:r::j,,Jj: i;.-,i XSWI38 The locality is also in the i f- E lo.*,,, I ffi;; i o .- .o 'l- swr"-cl ir."' , ifg;l o.*ono io"*to [:yi1 tvpe-rrea of rhe San Cassi;no - ' 3sw" j..*,- (Ú i H l.*nuo iiiWl: ';;i';; 113#ii É;., defined by wissmann i r o ,'ffi ].*, [il:Ji [*;: ];il;; ,*,.. |]il;: ] I flùzissmann & Múnster, 1841) as I 2swts*60 l-^..,..^^ ,"*.n Schichten aon SI. Cassìan and =+ ,U)i 2 > 10 ffi , 2.-". ru;l::' ..*oo , j subsequently named Cassianer é swe4.5 ,"*o.u i,"*o"o rsw+.s ] | Schicbten. The San Cassiano ' 'l Fm. lsw,os lìÈilióé8 ,"*oo Fm. b.isin.rl l=- i ] 'swo.o l-r--1 is a unit, subdivided bv ogilvie Gordon (leoo) l+ i:WS: I I I E ,.]_+ ill I ] I ] I lE intotwo-".,,be..,"tower;(un. -: rereCassianerschicbren,Ucs) .eol'T I I i I ] i S i i i i i Et y.d."upper" (Obere Cassianer Definition of the base of the Carnian. lithologic features and paleontologic contents. The IJCS overlie the La valle Fm' (although their boundary The Prati di stuores/stuores wiesen section. rhe Stuores section lies near pralongià, along the :il"::'Jîl,j;::::1L::ir;::'J:,t'Jl1::::::::;:; southern slope of the crest that separates the BadialAbtei turbidity volcanoarenites. According to Urlichs (1974), and Cordevole valleys. The section is located within a the OCS orzerl ie thc hioL"st voicanoarenitic layer wide, deepiy eroded gully cut into the rtop. u.r*"."ìn. ft'q*rl"riri;;r;;;';i'i"t",, of muddy beds, sit- Prati di Stuores section, a GSSP candidate +1

Teb. 1 - Arnmonoid distribution in the Prati di Stuores sections 1 and Lbis. The layer URL 1b is located at the base of section 2 (cf- Urlichs, 1994); o :open nomenclàture. tstones and maris, with some limestone intercalations. \fendt (1.977) and Marinelli (1980), the La Valle Subsequently, this lithostratigraphic definition vzas Fm./San Cassiano Fm. boundary (at 1.5 m from the challenged by De Zanche et aI. (1.993), De Zanche &. base of stake 0, Fig. 3) is marked by the appearance of Gianolla (1995) and Neri et al. (1.995) because paleogeo- oolitic turbidites, which indicate the progradation of a graphy, i.e. the distance of the volcanic shoreline, con- carbonate platform (Cassian Dolomite). trols the presence and/or the amount of volcanic debris The over 200 m thick alternations of siliciclastic within the La Valle and San Cassiano Fm. As a conse- and carbonate turbidites, deposited in a relatively deep quence, the volcaniclastic content does not seem to be a basin, together with the absence of unconformities and significant characteristic at the basin scale. the gradual upward increase in sedimentation rate and Considering the iithology, mainly grey and dark carbonate content, show that the Prati di Stuores sec- grey marls with intercalations of volcanoturbidites (La tion records a marked continuity of sedimentation. No Vaile Fm.) crop out in the lower part of the section, sudden or significant facies changes may be perceived while in the upper part brov/n and yellowish marls with either in the entire section or especially within the in- carbonate turbidites gradually prevail (San Cassiano terval including the proposed Ladinian/Carnian bound- Fm.). In agreement with Richthofen (1860), Fùrsich & ary (base of bed SV4, Tab. 1). 42 C. Broglio Loriga et al.

Synsedimentary tectonics seem to be absent. Some 5 - in considering the occurrence of the Carnian minor slumps recognizable in the upper part of the sec- taxon TiacLryceras, the Julian age was suggested for the tion do not interfere with the continuity of the section. Daxatina cf. canadensis Subzone (Mietto & Manfrin, 1995a, b). Furthermore, new material from Prati di Stuores Biostratigraphy and sections outside the Stuores area (Mietto & Man- frìn, 1995b) allowed a re-evaluarion of the specimens at- The ammonoid biostratigraphy of the Ladi- tributed previously fo"Anolcites" ex gr. laricus (Mojsiso- ni'an/Carnían boundary sequence, particularly the in vics). The main result is that the genus kstoceras occurs Stuores secrion, was discussed by Urlichs (1974, 1994) from the upper Neumayri Subzone, through the Regole- and Mietto & Manfrin (1995a, b); the conodont biostra- danus Subzone to the upper part of the Daxatina cf. tigraphy was documented formerly by Neri et al. (1994, canadensis Subzone (Fig. a), exrending the previousiy 1995, 1996) and Mastandrea et al. (1997). The present known range (Mietto Ec Manfrin, 1995a) and permìtting study inciudes the biostratigraphic data of a segmenr un- more accurate correlations with North America (Tozer, derlying the Aon Zone. Research on ammonoids, cono- 1994). Consequently, Zestoceras cf. nitidum Tozer occurs donts and palynomorphs from Ladinian-Carnian strati- in the upper Neumayri Subzone (F.ig. +) and the ranges graphic sections of the Dolomites is stiil in progress, but of Z. ex gr. enode (Tozer) a,nd Z. alf . enode correspond the present paper summarizes the knowledge to date. to the lower and upper parts of the Regoledanus Subzo- ne, respectiveiy (Fig. 4). Finally, Zestoceras n. sp. A (cf. Ammonoids and ammonoid biozones. Mietto & Manfrin, 1995b, pl. 2, figs. 4-6) comes from (Stefano Manfrin & Paolo Mietto) beds which contain also Daxatina sp. and D. cf. canadensis (Frg.4, and 13; Tab. 1). The Stuores section yielded many ammonoids (29 Specimens such as that illustrated in Mietto & levels), particularly from beds below the interval studied Manfrin (1995b: pl. 2, {ig.3) are retained as "Anolcitei' Urlichs (1974, by 1994). The fauna was illustrated by ex gr. /aricus, which is typical also of the Daxatina cf. Mietto & Manfrin (1995b), bur new material has been canadensis Subzone and is preceded, in the upper part collected (Pl. 1, and 2) and a revised ammonoid distribu- of the Regoledanus Subzone,.by a faintly ornamented is presented tion in Table 1. form here identified as "Ano/cites" cf. laricus. The most significant ammonoid events recorded At the base of the Daxatina cf. canadensis Subzo- in the Stuores section are as follows. ne, the genus Daxatina with Daxatina sp. and Daxatina 1- The genus Daxatina, prevrously known in the cf . canadensis ('Whiteaves) and "Anolcites" ex gr. laricus mid-high latitudes, occurs also in the Tethyan domain; appear. Clionitites and Tracbyceras lrepresented by Tia- 2 - species of the low-intermediate latitudes genus chyceras bipunctatum (Mùnster)] appear at 52.2 m and TiacÌryceras, different from T don aÍe found in levels o1- 61.5 m, from the base of rhe section, respecrively. der than previously known; The lower boundary of the Daxatina cf. canaden- 3 - the uppermost Regoledanus Ladinian Subzone sis Subzone lies within the San Cassiano Formation, .rr (Protrachyceras Zone) pars and Daxatina cf. canadensis 43.5 m above its boundary with the underlying La Valle Subzone (Trachyceras Zone) were recognised in the seg- Formation. The ammonoid fauna recovered below 45 m ments 12 to 45 m and 45-194.3 m respectively; (bed SW4, Tab. 1) corresponds to the fauna of horizon - 4 the correlation of the Daxatina cf. canadensis C of the Regoledanus Subzone sensu Mtetto & Manfrin Subzone with the upper Sutherlandi Zone from British (1995b), as indicated by the association of Frankites aper- Columbia is ìustified: razs (Mojsisovics), [ranging from -7 m (bed SVOa) rc 79.3

PLATE 1

Ammonoids from the Prati di Stuores/Stuores rViesen sectron.

Fig. 1 c[. Protr'rclrycera.s sp. Sample S\f3b.1, Regoledanus Subzone. Fig.2-7 Zestoceras n. sp. A. Fig. 2) satnple PSR10.9; Fig.3) sample PSR8.2; Fig.4) sample PSR3.oe; Fig, 5) slnple PSR6.1; Fig. 6) sample PSRl1.1a; Fig. 7) sample PSR3.42; Daxatina cf. canadensìs Subzone. Fig. 8-10 Clionitites sp. Fig. 8) sample PRS3.6b; Fig. 9) sample PSR3.36; Fig. 1O) sample PSR3.32; Daxatine cf. canadensis Subzone. Ftg. 17-12 - "Anolcites" ex gr. laricus (Mojsisovic$. Fig. 11) sample PSR3.43; Fig. 1J) sample SV4.2; Daxetina cf. canadensis Subzone. Fig. 13 Zestoceras aff. enode (Tozer). Sample SrV2.1, Regoledanus Subzone. f19.1+-r) - Muensterites sp. Fig. 14) sample S\17B.1; Fig. 15) sample S\W10.10, note the surure; Daxatina cf. canadensis Subzone. Fig. 16 Asklepioceras sp. Sample S\í10.3, Daxatina cf. canadensis Subzone. Fig. 17 Frankites apertus (Mojsisovics). Sample PSR8.1, Daxatina cf. canadensis Subzone.

Aì1 figures x 1; all specimens are illustrated here for the first time; for other material from the Pratì di Stuores section see Mietto & Manfrin (1995a, b). Pt. 1 Prati di Stuores section, a GSSP candidate +) C. Broglio Loriga et al.

^_bFis.4 - R.rn"e ch.rn .i the most si- LADINIAN CARNIAN gnificant uppermost Ladi- DAXATINA nian-lowermost Carnian am- cf. monoids from Prati di Stuo- CANADENSIS res and correlated sections in the Dolornites.

This subzone was recognised ,rlso in other similar sections throughout the Badia/Abtei Valley (Col da Oi, Kerpatscha, Col de Frea near Gardena Pass), in the area of Campolongo Pass (Bec de Roces, Crep de Mont), and in the eastern Dolomites (Rio Cuzze near Borca di Cado- re), rs mentioned partly in Mietto & Manfrin (1995b). The...'r.'*."^^'|'' oredatinp o[ the first appearance of the genus Tiachyce- ras within the Daxatina cf. canadensis Subzone allows the subu- nit to be placed at the base of the Trachyceras Zone o{ Mietto & Manfrin (1995a, b); this includes the T. aonoides Zone sensu Kry- styn (1978). Although in the Stuores section, Tiaclryceras oc' curs a few meters above the FAD of Daxatína, the high sedimenta- m (bed PSR8, Tab. 1)1, together wrth Zestoceras aff. eno- tion rate supports the idea that the FAD of Tiachyceras is de and probable Protracbyceras sp. (Fig. 13). However, ,E nearly coincident with the appearance of Daxatina. apertus, associated with an ammonoid assemblage of the Some specim eîs of Daxatina exhtbit the suture line uppermost Daxatina cf. canadensis Subzone lBadiotites (Mietto Ec Manfrin, 1995b, fig.6), but only one specimen e12x (Mùnster), Daxatina ? sp., Tiaclrycerds sp., Clionitites of Tiaclryceras from the same interval shows unequivocal basi/eus (Mùnster) and Sirenotrachyceras sp.], was collec- traces of the suture. The specimen ol Tiaclryceras mîtenste- ted also from an isolated layer (bed S\fl11) which crops d (Wissmann), illustrated in Pl. 2, fig. 2, shows the first out near the small church of Pralongià (see Mietto Er lateral saddle triangular in shape, elongated and frilled. Manfrin, 1.995b). Other specimens in which the suture line is not clearly The upper boundary of the subzone is located at evident were referred to Tiaclryceras on the basis of their 1.94.3 m in section 1 bis (Fig. 1, and 13), which yielded morphologic features. Tozer (1994) noted that Daxatina a specimen of a probable Tiachyceras aon (Mij'nster). The shows close morphologic similarity to Trachyceras, but Daxatina cf. canadensis Subzone is 149.3 m thick in the the two genera are clearly differentiated on the basis of Stuores section, reflecting a high sedimentation rate. their suture line, which is of ceratitic type in Daxatina

PLATE 2 Ammonoids frorn the Prati di Stuores/Stuores Sliesen section.

Fig. 1 - Tiaclryceras bipunctatunt (Mùnster). Sample 5\16.la, Daxatina cf. canadensis Subzone. Fig. 2-5 - Tiaclryceras mumsteri (lfissmann). Fig. 2) sample PSR3.dt1, collected between PSR3 and PSRS; Fig. 3) sample PSR5.1, a) positive, b) negative; Fig.4) sarnple PSR1O.15; Fig.5) sample PSR3.33, a) complete specimen, b) the same specirnen but wrthout the outer whorl, c) nght side of the outer whorl, d) left side of the outer whorl; Daxatina cf. canadensis Subzone. Fig.6-9 - Daxatina sp. Fig. 6) sample PSR4.1; Fig. 7) sample PSR3.dt2, collected between PSR3 and PSR8, a) negative .'entral area, b) -^";.;"- .'--..'l area Fig. 8) sample PSR1b.1; Fig. 9) sample S\f5b.7; Daxatina cf. canadensìs Subzone. Fig. 10-11 - Daxatina cf. canadensis (Vitheave$. Fig. 10) sample SW10.11, note the suture; Fig. 11) sample SV10.1; Daxatina cf. canadensis Subzone.

All figures x 1; except for exemplars 2 and 11, all specimens are illustrated here for the first time; for other materiel see Mietto 8c Manfrin (i995a, b). Pl.2 Prati di Stuores section. a GSSP candidate 45 C. Broglio Lorìga et al.

a Fig.5 - A comparison betn'een the À,l|ietto & Manfrin, Tozer, l994 vlark et al., 1992 ui 1995a, b I amrnonoid scales adopted in f g 3ì Southern Alps, Canada and z 1 2 3 d 8 ò >xEF Arctrc Ocean, with the most z SOUTHERN BRITISH SVALBARD :è CEF srgnificant bio-events at the f ALPS COLUMBIA 3€F traditional and proposed La- z :vÉ^ E f (I dinian-Carnrrn bo,,rd.rru z TBACHYCERAS TRACHYCERAS STOLLEYITES E. AQN DESATOYENSE TENUIS $Èîîltî 12 oounoary O zo Frcnkiles DAXATINA sutheilandi DAXATINA cf. CANADENSIS z CANADENSIS u z Daxatina F canaoensts af 2 z t! F. sutherlandi 1-2-3 1-21?) 1_2 boundary F 1-2Q) FHANKITES Y INDIGIRITES ó z Frankiles f REGOLEDANUS TOZERI fI glaDer z J I o ,PFìOTRACHYCERAS' ,4ACLEARNOCEBAS NEUMAYRI MACLEAFìNI J and of ammonitic type, with triangular elongated saddles, graphic units mentioned above, pertaining to different do- rn Tiacbyceras. The characteristic presence in Tiaclryceras oÍ mains, does not seem to coincide perfectiy. two serried orders of spines adjacent to the ventral furrow Some discrepancies in the vertical range of some and forming a typical raised structure is a further differen- taxa (i.e., Asklepioceras, Muensterite) may be only appa- tiating feature. In Daxatina rhe ventral area is quite different. In particular. the pllcemenr oI the Clionitites, Tra- rent, and raised furrow boundaries bearing spines are clryceras and Daxatina association in the Desatoyense nearly absent. Moreover, Tiaclryceras is generally more fi- Zone (:base of the C.rrnian sensu Tozer, 1994) is not nely and more regularly ornamented than Daxatina. supported by the stratigraphic data; in addition, in the Prati di Stuores section the same genera appear and are Ammonoid correlations. associated inside the Daxatina cf. canadensis Subzone. is (Stefano Manfrin & Paolo Mietto) It very important ro note that in the Boreal domain (Barents Sea, Svalbard, Sverdrup Basin), the Daxa- The ammonoid fauna succession in the Stuores tina canadensis Zone is currently used as a unit correia- section and in other localities of the Southern Alps table with the Sutherlandi Zone from Canada and rvith (Mietto & Manfrin, 1995b) records some bioevents the Nathorstites Zone from Siberia (Mork, Embry & which occur (in homotaxis) also in exrra-rerhyan areas Veitschat, 1989; Mark, Vigran & Hochuli, 1,99A; Mork (British Columbia; Svalbard) (Fig S) et al., I992a, b; Weitschat & Dagys, 1989). 'Ihe correla- The occurrence of genera with widespread ro co- tion of this zone from the Boreal domain with the smopolitan distribution allows the tethyan biozones to Daxatina cf. canadensis Subzone of the Tethys and with be correlated with those defined in Canada (British Co- Subzone 2 (except its basal part) of the Sutherlandi lumbia) by Tozer (1,967;1,99a). Zone from Canada thus appears strongiy plausible.

Tn .roreemcnr 11995r/ J4, h\ *ith Mietto & Manfnn \,, vl, The proposal to identify the LadinianlCarnian the Neumayri Subzone is considered equivalent to rhe boundary with the FAD of Daxatina is supported also Maclearni Zone or at least to the Subzones 2 and 3 as by the areal distribution of the taxon. Tozer (1994), due to the presence of Maclearnoceras in In fact, the genus is known as a characteristic r.rxon association with Liardites (Fig. 4 and 5). of the Boreal domain. Bòhm referred the taxon to " Daza- The appearance of Frankites, which marks the base sonites" (Arctic Ocean, Bjarnoya; DA3, 9A4). The type of the Regoledanus Subzone, makes this tethyan unlt corre- species "Tiachyceras" canadense \íhiteaves 1889 was found latable with Subzone 1 of the Sutherlandi Zone from Ca- in the Liard River, British Columbia (cf. also Smith, L927; nada. The appearance of Daxatina in the Daxatina cf. ca- Mclearn, \947a, b; Tozer, 1967, 1994). The same genì-rs nadensis Subzone makes plausible the correlation of this was noted in Alaska by Martin (1916), while Arkell, tethyan unit with Subzone 2 of the Sutherlandi Zone from Kurnmel & Wright (1957) considered the genus as typical Canada, sensu Tozer (1994). As a matter of fact, Daxatina of the mid-high latitude. The occurrence of Daxatina in appears within Subzone 2 and is preceded at the base of the the Southern Alps and also in the Himalaya (L. Krystyn, same subzone by the appearance of Frankites sutherlandi pers. comm.) makes it the only cosmopolitan genus of the (Mcl-earn). Therefore, the correlation of the biostrati- Ladinian-Carnian boundary interval. Prati di Stuores section, a GSSP candidate

Conodonts the section still contains Budurcnignatbus and long-range Gladigondolellas (G/. tetbydis, GL rn. malayensi). Budu- \ rwignatbus diebeli and B. mostleri extend up to about s 177 m, together with a broken specimen \ a of Gondolella o which, due to its poor preservation, has an uncertain * Ò \ È classification at species level (G. inclinata vel G. polygna- tt s q Q \ thiformi). o \ t € \ .s E o e \M \ o \ Flowever, it should be noted that G. polygnathtfor- < \ \ \ \ \ o mis was found together with Tiaclryceras near the t\ (l aon 18SW X 5.50 I 2 base of section 2 Ftg. 1), which corresponds to rhe stra- 18SW tX 2.60 totype section of the Cordevolian Substage of Urlichs 18SW 18 70.00 2 (1974). On the basis of data from sections in the Stuores 17SVr' 17 8.10 area, if seems that the FAD o{ Pseudofurnishrus murcta- I?SW VIT 56.00 nus murcianzrs is located slightly below the first occur- 17SW 16 -ì.00 t5sw 164 8.98 4 rence of G. polygnathtformis. Moreover, in the lower I 5SW 14 40.7 8 2 samples of section 2 {rom the Stuores area, B. diebeli r5-16 r2sw 12 116.2s 8 5 4 I 2 ll-12 occurs together with G. po/ygnathi/òrtnis, conftrming lOSW VII 112.55 2 3 5 the overlap of the ranges of these taxa shown in other 8SW 9 90.50 ) I sections within Alpine Europe (Mastandrea er a1., in 8SVr'8 86.50 2 il progress). 5bsw vI 5 8.05 5SW V 4)_J) I 5SVr' 6 42.94 base ofthe 4SW ry 4i.50 Daxatina cf. oanadensis Sbz Ammonoid vs. conodont biozones: comparison and (45 4SW I]I 33,00 m) problems. 4 3SV/ II tió . l:2 7 (Adelaide Mastandrea, Paolo Mietto & Claudio Neri) 2SW I 15.00 The vertical distribution of conodonts and ammo- Tab. 2 - Range chan of conodonts in the Prati di Stuores secrion. noids across the Ladinian /Carnian boundary was discussed by Krystyn (1983) in the Epidaurus secrion (Greece) Conodont biostratigraphy. and, more recently, by Kovacs et al. (1991) in the Fùred (Adelaide Mastandrea) Limestone in the Balaton Highlands (Hungary). These accounts present contrasting The Prati di Stuores section is very poor in cono- sets of data. According (1983), donts. Only eleven out of nineteen samples yielded spe- to Krystyn in the Epidaurus cimens (1-19), and eight taxa .were recognised, among section the conodont assemblage characterised by Budu- which the species of the Buduro.,tignathus group and two roaignatbus diebeli, marker of the diebeli A.-Zone, rs cor- long-range species of the genus Gladigondolella: (GL relatable with the Regoledanus Zone sensu Krystyn tethydis (Huckriede), Gl. rn. rnalayezsis Nogamì. The Bu- (1983). The first occurrence of Gondolella polygnathtfor- duroaignatbus group is represented by B. mungoensk znls is considered to coincide with the base of the Aon (Diebel), B. longobardlcazs (Kovacs), B. diebeli (Kozur & Subzone (Krystyn, 1983). Unfortunately, in this section Mostler) and B. mostleri (Kozur) (P1. 3). All taxa are the ammonoids are scarce and represented only by spe- typical of the diebeli Assemblage Zone of Krystyn cìmens of Tiaclryceras sp. in the Aonoides Zone sensu (1983), vzhich was referred by the author to rhe upper- Krystyn (1,978). The ranges of Buduroaignathus diebeli, inost Ladinian Regoledanus Zone. B. mwngoensis and B. mostleri do not show any overlap The first occurrence of conodonts of the Buduro- with that of G. poLygnatbtformis, even though. on the oignatbus group with GL tethydis is recorded at 26.50 m basis of sections such as the Mayerling section) Austrian from stake 1 (Regoledanus Subzone) [ab. 2 and Fig. Krystyn (in Gallet et a1., 1998) concluded that the Budu- 13). IJnfortunately, the interval between 26.50 and rwignatbus group range extends into the Aonoides about 86 m is barren of conodonts: Budurctuignathus sp. Zone. occurs at sS\lV, 0.35 m above the FAD of Daxztina cf.. Clear evidence of overlap between the ranges of cdnddensis (45 m from stake 1). Budurovignathus and G. polygnathifurmis is supplied by The segment of section between 86.5 m and about the Prati di Stuores section and outcrops from the Apu- 1,49 m is relatively iess poor. Particularly, sample SW12 seni Mts. (Roumania, Kozur, 1980; 1989). Flowever, it is (1,1,6.25 m from stake 1., mid-lower Daxatina cf. canaden- unclear whether the overlap is due mainly to a dow- sis Subzone) contains GL tetlrydis, B. mungoensis, B. lon- nward extension of the range of G. polygnathtformis, be- gobardicus, B. diebeli and B. Tnostleri. The upper part of low the FAD of Tiaclryceras Aon, or to the upward exten- 48 C. Broglio Loriga et al, sion of the range of the Budurwignathus group into the phormis in the beds containing specimens of Frankites Aonoides Zone. apertus (Neri et al., 1995; Mastandrea et a1., 1992; Russo In the Ladinian-Carnian succession of the Balaton et aI., 1997). Highlands, conodonts of the Bwdurwignathws group (in- The problem requires further discussion in order cluding B. diebel) occur with G. polygnatbiftrmis at the to confirm whether the FAD o{ G. polygnathiformis re- base of the Fùred Limestone (Kovacs et al., l99I), which ally corresponds with that of T aon, or whether it is contains Frankites sp., and is thus referable to the Rego- within the upper Regoledanus Zone Auct. (:Daxatina ledanus Zone. The conciusion of Kovacs et al. (1991) is cf. canadensis Subzone). Data from the Stuores area sup- that the base of the Carnian stage shouid be identified pofi the idea that the FAD of G. polygnathiformis and by the first appearance of G. polygnathifurmis, and that T aon are broadly coeval; this interpretation is consi- the Regoledanus Zone is therefore included into the Car- stent with data from Epidaurus, and does not conflict nian. with data from the Mayerling section, Austria (Gallet et Two of the authors (S. Manfrin & P. Mietto) belie- al.,1998). ve that the specimens of Frankites sp. in the Fùred Limestone may pertain to E apertus rather than to E regoledanus. This is supported by a re-evaluation of the Paleontological and paleoecological contributions ammonoid fauna described in Frech (1911) from the same stratigraphic unit. This fauna includes "Tiaclryceras agreement the revised guidelines the (Anolcites) Richthofeni MOJS.", which the two authors In with for establishment global chronostratigraphic standards consider, with some reservations) to be .4 apertus. II thís of (Remane et aI., 1,996), other fossil groups were investiga- interpretation is correct, it would be possible to argue that the FAD of G. polygnathiformis falls within the ted in the staked Prati di Stuores section. Data on Daxatina cf. canadensis Subzone, and that its occurrence palynomorphs, which could be important biostratigraphic tools, and benthic foraminifers, bivalves, ga- at the base of the Aon Subzone in the Prati di Stuores on section 2 (Frg 1) is the result of ecological control. A stropods, brachiopods, microcrinoids and holothurian significant change from anoxic/disoxic to a fully oxyge- sclerites, identified in the interval including the propo- nated basin environment may occur in the upper D. cf. sed Ladinian/Carnian boundary, are presented and di- canadensis Subzone, below the Aon Subzone, as sugge- scussed below. sted by micro- and macrobenthos assemblages. This consideration may support the proposal to draw the Ladi- Palynomorphs. man/Carnian boundary at the base of the Daxatina cf. (Simonetta Cirilli & Guido Roghi) canadensis Subzone, whose lower boundary occurs in the segment unaffected by significant paleoecological Palynologic assemblages from the Stuores section changes, and may thus be regarded as reflecting evolu- were calibrated with the ammonoid zonation and there- tionary control. fore supply a basis for a more detailed chronostrati- .,,,1., Furthermore, there is no agreement among the 614PurL-- ^L;^ rruu/. authors of the paper by Kovacs et al. (1,99I) about the Most of the 36 samples yielded well preserved as- real taxonomy of the conodonts classified as uG. semblages (P1. 4, 5 and 6). A few samples (LCP3, polygnatbrformis". According to Krystyn (pers. comm. to LCP20, SWZ, respectively 31.5 m, 48.4 m and 1,2Q m A. Mastandrea) G. polygnathiformis has never been from stake 1) proved barren of organic matter; others found within the Regoledanus Zone. yielded material deeply affected by diagenetic pyrrrtza- Other data on conodont assembiages from strati- tion and degradation processes. A semiquantitative stu- graphic sections of the Sella Pass, Gardena Pass and dy of organic particles, including palynomorphs and Punta Grohmann confirm the absence of G. polygnathi- palynomacerals, was carried out. The compositional va-

PLATE 3 Conodonts from the Prati di Sruores/Stuores Wiesen section. rrg. r-z Budurwignatbus longobardicus (Kovac$. Fig. 1a) upper view, Fig. 1b) lower view, sample S\X/4/1.2, 15Ox; Fig. 2) upperJateral view, sample S\14l12, 180x. Fig. 3-4 Budurouignathus mostleri (I(ozur). Fig. 3) upper view, sample SW4/12,200x; Fig. 4) lower view, sample SYJ4/72,20ax. Fig.5-6, 10 -Budurwignathus rnungoensis (Diebel). Fig. 5) upper view, sample SW4/L2, 140x; Fig. 6) upper view, sample S\{/4/VII, 150x; Fig. 10) lower view, sample SSí4/VII, 200x. Figs 7, 11 - Budurwignatbus d.iebeli (Kozur & Mostler). Fig.7) upper view, sample S\í4III,200x.; Fig. 11) upper view, sample S\V4IVII, i50x. Fig. 8 GLadigondolelLa tnalayensis maLayensis Nogami. Upper view, sample S$14l18, 150x. Fig. 9 Gladigondolella tetlrydk (Huckriede). Upper view, sample S\X/4/16, 100x. Prati di Stuores section, a GSSP candidate C. Broglio Loriga et aL.

riation in miospore assemblages throughout the section Daxatina cf. canadensis Subzone. Partitisporites noai- is high, both in total abundance and number of species. mundanus is first recorded here ar LCP1 (30 m) and its The palynologic content, with the exception of abundance increases upwards. In addition, Lunansporttes the marine elements, is presented in Tab. 3, summarized acutus and l'leorais*icleia tay/orit occur in the Regoleda- in Fig. 13, and described below. nus Subzone. The most abundant species is the long ranging Ooalipollis pseudoalatus, which rs presenr - Assemblage A (0 to 48.7 m, upper parr of Rego- throughout the section; other sporomorphs are more or ledanus Subzone and lowermosr parr of Daxatina cf. ca- Iess constantly present in variabie percentage nadensis Subzone): it is highly diversified, containing 43 throughout the section (see Tab. 3). species, some of them making their first occurrence wi- Concaaisporites tora/is, Gutboerlìsporites cancello- thin the Stuores section 1 (Tab. 3, samples SVa to sus, Alisporites oeatlts, Densosporites cf. aariomarginatus SVm, 0.5 m to 48.5 m). The most significant first oc- and l{yrtomisporis eraii occur sporadically in the Regole- currences are Enzonalasporites vigens and " Lueckisporites" danus Subzone and disappear in the overlying Daxatina cf. singbii, from sample SWh Qa.I m) and sample cf. canadensis Subzone. The percentage of bisaccates is LCP16 (44.5 m; Tab. 3, and Fig. 13), respectively the high at the base of the section, decreasing slightly to- iast one, just 50 cm below the lower boundary of the wards the Regoledanus/Dax:rtina cf. canadensis subzone Da-xatina cf. canadensis Subzone. Both extend into the boundary, but increasing again in the latter subzone.

PLATE 4 PJvnomorphs frorn the Prati di Stuores./Stuores Viesen section: Assemblage A

Fio 1-2 Enzonalasporites zzgezs Leschik. Fig. 1) sampie S\li; Fig.2) sample LCP16. Fì. 1 "Lueckisporites" cî. singhii Balme. Sample LCP16. Fig. 4 IQrtonisporis eruiiYtn der Eem. Sample LCP12. Duplicisp orites granulatus (Leschik). Sample LCP1.

Fig. 6 Ooa lip o I I is p seud o a latus (Thiergan). Sample SlX/a. Ftg.7 Scllaspora rugcuetuctta Vrn der Eem. Sample LCP l. Fio R-S Utaesporites gadensis Praehauser-Enzenberg. Fig. 8) sample LCP12; Fig. 9) sample LCp14 Aratrisporites fi.rnbriatus (Klau$. Sample LCP1. Frg. 11 Cdldnrcspora tener (Leschrk) Màdler. Sample LCP1. r1g. tt Neoesisporites tallatus De Jersey. Sample LCP16. Podosporites amicus Scheurìne. Sample LCP1.

Except Fig. 6 (300x), all fìgures x50O

PLATE 5

Palynomorphs from the Prati di Stuores,/Stuores Viesen section: Assernblage B

Vallasporites ignacii Leschrk in Krausel & Leschik. Fig. 1a) proximal view, Fig. 1b) distal vieq sarnple S.Wab. "Lueckisporites" cf. singbii Balme. Fig.2) sample LCP17; Fig.3) sarnple SVab. Fio 4-5 Patinasporites denswsreschrk in Krausel & Leschik. Fig. 4) sample sT\fi ; Fig. 5) sample ST\fhx. Fio A-R Enzonalasporites vigensLeschik in Krausel & Leschik. Fig. 6) sample LCP22;Fig.7) sample SWtl; Fig. 8) sample LCp25. F;e I Camerosporites secatus Leschlk in Krausel 6c Leschik. Tetrad, sample S.ù/n. Fig. 10 Retìtulatisporites muricatus Kosenke. S.rmple SVt. Fig. 11 ÍVeylandites mdgmus (Bose 8c Karr) Van der Eern. Sample S\X/21.

Atl tlsures x)uu.

PLATE 6 Palynomorphs from the Prati di Stuores/Stuores \liesen section: Assenblage B

Fig. 1,5 - SeLlaspora ruguuerrucdtd Van der Eem. Fig. 1) sample LCP22;Fig.5) sample Swaa. Fig.2 - Gordonisporafossulata (Balme). Fig.2a) proximal view, Fig.2b) distal view, sample S\ls. Fig. 3 - Uvaesporites gadensis Praehauser-Enzenberg. Sample SlWr. Fig.4 - Uvaesporites sp. A. Sample S$lr. Fìg. 6 - Lycopodiacidites kohenii Van der Eem. Sample SlVn. Fig.7 - Neoraistrickia tayloriiPlayford & Dettmann. Sample S$ls. Fig. 8 - Conoerrucosisporites sp. A. Sample ST\7o. Fig. 9 - Concavisporites crassexinius Nillson. Sample STrVi. Fig. 10 ' Partitisporites nwimundanus morphon (Leschik in Krausel 6c Leschik) Van der Eem. Sample LCP22. Fig. 11 - Duplicisporites granulatus Leschik in Krausel & Leschik. Sample LCP22.

^lr llgures xtuu. Pl. 4 Prati di Stuores section, a GSSP candidate ft C. Broglio Loriga et aL. Pl. 6 Prati di Stuores section, a GSSP candidate 5l 54 C. Broglio Loriga et al

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Tab. 5 - Foraminifer (thin section) range chart in the Prati di Stuores sectìon. Number at i right hancl of the sarnple iÈ name refers to the distence ! in metres from the under- à's 5= si lying stake.

lSsw 10.21 )7'7.1 6

Ì 7l.95 Marine elements such as lTsw 12.65 I 65J0 acritarchs (Baltisphaeridium sp. I ?SW 4XO and Micrlrystridium sp.) and fo- l6sw 5 45 raminiferal test linings are gene- ..il.,,,-^^-'-^- The first appearance of E l2sw 10.42 lxw 1r? aigens and "L". c[. singhii tradi- ì rsw 0J5 tionally falls in the Upper Ladi- nian (Scheuring, 1970, 1974, I 12.90 1978; Clement-Westerhof et al., l11o 19741 Schuurm.rn, 1979; I osw 6.45 1977, Visscher et al., 1980; Visscher & Brugmann, 1981; Van der E,em, 1983). According to Van der Eem (1983), the appearance of L. uigens marks the beginning 81.l0 - base of the secatus-oigens (Lon- 8l!0 ol phase Daxatina cl-. canadensis Sbz. 7SW 5.00 gobardian), whereas "L." cf. sin- (4s m) 6sritt 2J0 ghii appears in the upper part of the same phase. 5SW I L90

5S\\' I I JO - Assemblage a (+8.7 ro 160 m, Daxatina cf. canadensis Subzone) contains 37 species. In sample LCP22 (48.7 m), the 45W 7.55 typical Carnian species Patina- sporites densus and Vallasporites 4SW 5.35 ignacii appear, together with cf. 4SW 0.90 4SW 0.60 Concentricisporites bianulatus, 4SW 0.00 [nfernopollenites paruus and 3S\\' 820 as\\'sJo Tiiadkpora modesta. Camerospo- 3SW 4.00 . rites secatus appears in sample lsw o.oo 2SW 8.80 LCP24 (52.3 m), within the Da- :sw 6.90 xatina cf. canadensis Subzone. iSw q:o rsw r.:0 Other characteristic ele- 2SW 0J0 ments are lVey/andites înagmus, tsw9.l0 lsw860 which appears in sample r siv a.eo STVhx (79 m) and Aulisporites astigmosus, from sample SWo lsw 1.90 (7q ) *\ T. tL- I SW O00 \. . .- ,.,). "^^-. most p.ìrt of the subzone, from sample At the Regoledanus/Daxatína cf. canadensis subzo- SWu2 (109 m), rare specimens of c[. Partitisporites ne boundary, an apparent diversification was recorded. maljaukinae are recorded. Other ne'w sporomorph ap- Deltoidospora mesozoicus, Ephedripites primws, Osmunda- pearances in the Daxatina cf. canadensis Subzone are cidites cl. zaellmanii, and[Jztaesporites sp. A (cf. Van der shown in Tab.3. Eem, 1983) first occur just above the boundary and are Marine elements are more common than in the followed, slightly higher, by Concavisporites sp. A (cÍ. Regoledanus Subzone; they include acritarchs (BaLtbr- Van der Eem, 1983) and Reticulatisporites Tnuricatus. sphaeridiurn sp., Micrhystridium sp., Dictyotidium te- Prati di Stuores section, a GSSP candidate 57

nuiornatum), Prasinophytae algae (Cymatiosphaera sp. A from both washed materials and thin sections. The fora- 'and Thsmanites) and foraminiferal test linings. miniferal succession is as follows (Tah.le7 and 8). Previous palynologic studies of the Stuores section A) 0 to 45 m (Regoledanus Subzone). This seg- were cairied out by Van der Eem (1933) who defined ment ranges from stake 0 to the FAD of Daxarina. the base of the aigens-densus phase at the first occurren- Isolated foraminifers ffab. l\ - A rich fauna domi, ce of Patinasporites densus and Vallasporites ígnacii. How- nated by agglutinated forms such as "Endothyra" leueppe- ever, Van der Eem's samples were coliected in younger rl Oberhauser, PalaeolitwonelLa rneridionalis (Luperto), strata (Aon Subzone), from section 2 (Fig. 1), correspon- Ammodiscus cf . infimus (Strickland), A. incertus (d'Orbi- ding to the section in Urlichs (1974). As these forms gny), Glomospirella ? facilis lr{o, Glomospira perplexa occur aiso in the underlying layers (section 1), the base Franke, Reopbax eominutus Kristan-Tollmann, etc., toget- of the oigens-densus phase is now revised and is placed her with Dentalina ex gr. subsiliqua Franke, D. cassiana close base canadensis to the of the Daxatina cf. Subzone Gùmbel, l''lodosaria primitioa Kùbler & Zwing\i, Pseudo- (Tab. \Veylandites magmws, 3 and Fig. 13). Both which nodosaria obconìca (Reuss), Kriptoseptida lelebelsbergi occurs exciusively in the secatus-oigens phase, and Came- (Oberhauser) , knticulina cassiana (Grimbei), L. karnica rosporìtes sec+ttrs, whose first appearance is considered (Oberhauser), etc.; in addition Duostomina biconaexa Lare Ladinian in age (Schuurman, 1977, L979; Visscher Kristan-Tollmann, D. alta Krtstan-Tollmann, D. turboi- Er Krystyn, 1978; Visscher & Brugman, 1981,; Van der dea Krístan-Tollmann and Ophthalmidium c{. exiguum Eem, 1983; Blendinger, 1988; Brugman et al., 1.993;Yar- Kóhn-Zaninetti occur. rinston. 1996). occur within the Daxatina cf. canadensis Thin section (Tab. 8) - In a mudstone layer ar 9.10 Subzone. m the appearance of the Gsollbergel/a spirolocu/tforrnis In summary, the Regoledanus Subzone in the (Oravecz-Sch e{fer), S emimeandro sp ira ex gr. ka rn i ca -p I a - Stuores section is characterised by the first occurrence of nispira (Oravecz-Scheffer) and TizrrigLornina carnica (D+ Enzonalasporites aigens and of " Lueckisporite{' cf. singhii ger) assemblage 'was recorded. Piallina tetbylls Rettori et (ciose to the top of the subzone). Within this ammo- occurs fine-grained noid subzone, significant last occurrences are those of al. first in a unit at 1,9.90 m. The Concavisporites toralis, Guthoerlisporites cancellosus, Den- appearance of Gordiospira triassica lJrosevic was recor- sosporites cf. variomarginatus and l(yrtomisporis eruii. ded at 36.13 m, but this species is absent in the rest of The Daxatina cf. canadensis Subzone is charac- the section. Gsollberge/la spiro/ocultformis occurs terised by the appearances of Patinasporites densus and throughout the succession in both calcarenites and mud- Vallasporites ignacii, together with the occurrences of dy limestones. Turriglomina carnica, when present, is Camerosporttes secatus and \Veylandites rnagmus. Further- more abundant above 29.18 m. In addition, .r solitary more, the Tiiadispora group becomes more diversified specimen of Paheolituonel/a meridionaLis (Luperto) was towards the upper part of the subzone. recognised (+l .Z m from stake 1). All these taxa are In addition, it should also be noted that Assem- small and, at present, known exclusively from the Car- blage B of the Daxatina cf. canadensis Subzone from the nian of western and eastern Tethys. Prati di Stuores section can be correlated with G/H As- Specimens o{ AmmobacuLites, Gheorghianina, Glo- sembiages of the Barents Sea (Hochuli et al., 1989, [ig. mospird, Glomospirella, Duostomina, Endoteba, Ophthal- 2) for the presence of Patinasporites summus and Came- mtdíurn and Reophax may be associated with the fauna rosporites secatus. These boreal assembiages include the mentioned above. Nodosariidae and Textulariidae were presence o{ Daxatina canadensis and are referred to the also noted (Tab. 8). uppermost Ladinian. Flowever, the typical boreal index B) 45 to about 110 rn (Daxatina cf. canadensis taxa of Assemblage G, such as Echinitosporites iliacoides Subzone p.p.). and Retisulcites perforatus (Hochuli et al., 1989), are lac- Isolated foraminifers - Few new taxa gradually ap- king in the palynoflora from the Prati di Stuores section. pear. Most of the foraminifers present at iower levels such as Lenticulina excaoata Terquem, L. bochardi Ter- Benthic foraminifera. quem, Z. karnica (Oberhauser) , Glomospirella herntgordi- (Carmela Broglio Loriga, Donato di Bari & Roberto Rettori) formis Tscherdinzev, etc. persist above 45 m, but the no- The study of foraminifers was carried out both in dosariids, including Dentalina gwernbeli Schwager and thin section and washed material to obtain the most rea- Nodosaria nitidana Brand, become dominant. Other listic assemblages (P1. 7, and Pl. 8). Fifty-one species new taxa belonging to the C)berhauserellidae, such as were extracted from 27 samples of marls and clays, and Schlagerina sp. and OberbauserelLa sp., were identified. twenty taxa were identified in over 300 thin sections Thin section - The changes noted in the assembia- from calcarenitic levels and muddy limestones. ges from this segment are the bloom of S. ex gr. karnica Three segments were distinguished in the Stuores -planispira at 11,3.4 m and the decrease of the taxa pre- section on the base of FO and abundance of the ta-xa sent further below. 58 C. BrogLio Loriga et ,tl. PI.7

PLATE / lsolated foraminifera frorn the Prati di Stuores/Stuores $Tiesen section. Fig. 1 - Paralingulina ploecbingerí (Oberhauser). Sarnple 14SV 1.5,7Ax. Fig. 2 - Nodosaria nitidana Brand. Sample 13S\l 5.0, 60x. Fig.3-4 - LanrelLiconus procerzzs (Liebus). Fig. 3) /5x; Fig.4) 100x; Sample 163\1 11.0. Fig. 5 - Dentalina ex gr. subsiliqua Franke. Sample 14S\l 1.5, 170x. Fig. 6 - Pseudonodosaria obconica (Reuss). Sample 4SIw I.7,70x. Ftg.7 - Ophthalmidiumfusiforme (Trifonova)- Sample 16SW 8.0,90x. Fig. 8 Ophthalmidium Lucidum (Trifonova). Sarnple 18SV 0.5, 100x. Fig. 9 - LenticuLina excd.ldtd. (Terquen). Sample 13S!l 5.0, 60x. Fig. 10 - Duostonr.ina bicontexa Kristan-Tollmann. Sample 14S\f 1.5, 120x. Fig. 11 - GlomospirelLa bemigordiformis (Tscherdynzew). Sample 65\1 1.7, 90x. Fig. 12 - Lenticulinabocbardi (Terquem). Sample 14SW 1.5, 100x. Fig. 13 - "Endotlryra" huepperi (Oberhauser). Sample 14SSf 1.5,100x. Fig. 14 - AuLotortus ex gr. sinuosus (lleynschenk). Sample 16SW 11.0, 230x. Prati di Stuores sectìon, a GSSP candidate 59

;iii&ia a -:tf:

PLATE 8 Forarninifera rn thin section from the Prati di Stuores,/Stuores $liesen section.

Fig. 1 Piallina tetJryd^Frerrorl et al. Sample 2S\l 10.25,420x. Fig. 2 - PaLaeelituoneLla meridionalis (Lupeno). Sampìe 5SV 1.40, 115x. Fig. 3 - LaneLlicctnus multisprrus (Oberhauser). Sample 18S\{ 5.0, 65x. Fig. 4 - LameLliconus procerus (Ltebts). Sample 18S\f 5.0, 100x. Fig. 5 - Gordiospira triassíca Urosevic. Sample 45 $f 17 .55 , 155x. Fig.6-9 - Turriglomina carnica (Dager). Fig.6) sample 3S\f 9.95,420x; Fig.7) sample 1S\il f.iO,42Ox Fig. 8-9 - Semimeandrospira ex gr. karnica-planispira (Ormecz-Scheffer). Fig. 8) sample 1S\l 9.10, 420x; Fig. 9) sample 16S\f 5.45, 420x Fig. 1O-12 - GsoLlbergeLla spiroloculifurmis (Oravecz-Scheffer). Fig. 10,12) sample 1S\7 9.10,420x; Fig. 11) sample 7S1W 5.0,420x. 60 C, Broglio Loriga et al.

C) about 130 m to the top (Daxatina cf. canaden- va, 1992; 1993), the Transdanubian Central Range (Ora- sis Subzone p.p.) vecz-Scheffer, 1987), Eastern Serbia (IJrosevic, 1988), the Isolated foraminifers - The taxonomic diversity of Northern Caicareous Alps (Oberhauser, 1957; Kristan- the assemblage suddenly increases. Duostominids and in- Tollmann, 1960; Kóhn-Zaninetti, 1969; Zantnettt, 1969, volutinids are dominant. The first occurrence of involu- 1.976), the Julian Alps (Rettori et a1., 1998), China (He tinids such as Aulotortus ex gr. sinuosus Veynschenk, 1-a- & Yue, 1987;He & Norling, 1991) and Israel (Benjami- melliconws multispirus (Oberhauser) and L. procerus (Lie- ni,1988). bus), is noted at 136.1 m. Opbthalmidiumfusiforrne Qri- 7 - Changes in taxonomic compositions may be par- fonova) and O. lucidwm (Trifonova) appear also for the tly related to ecological factors such as oxygen conrent. first time. Lamelliconus ex gr. eentroplanus (Oberhauser) Autochthonous deep water benthic foraminifers appexrs at 167.5 m. characterise the Stuores section mainly from the base to Other main taxa are Duostornina biconpexa Kri- about 130 m (Regoledanus Subzone, lower Daxatina cf. st an-Toll man n, D ip I o tre m in a a s tr ofi rn br ia ta Kristan-ToIl- canadensis Subzone). The shallow water taxa commoniy mann) Variostoma pralongense Kristan-Tollmann, V exile inhabiting the adjacent platform environment are found Kristan-Tollmann, Papillaria altoconica (Kristan-To11- in the basinal sediments of the San Cassiano Fm. from mann), Papillaria sp.; moreover, a few nodosariaceans, about 131 m to the top of the section and are dominant oberhauserellids and agglutinated forms are present. in the upper Daxatina cf. canadensis Subzone. Thin section - The shallow 'water biota from the According to the relationships between foramini- platform environment (Dolomia Cassiana) such as Tubi- feral test morphology and energy-oxygen level suggested phytes, bryozoans, Cayeuxia, calcareous sponges, thick- by Kahio (1989) and Boudiche & Ruget (1993), Dentali- shelled bivalves, encrusting foraminifers becomes more na, Pseudonodosaria and Nodosaria belong to the elonga- I I f a.^ JDUnOant lrom lJU.,/ò-^ m. ted and cylindric morphotype and Lenticulina to the flattened and At 171..95 m, the foraminiferal assemblage is do- planispiral type. Deep water infaunal ha- have been inferred minated by involutinids (Lamelliconinae) mainly refer- bits for these taxa. Agglutinated and tubular tests red to Larnelliconus muhispirus (Oberhauser) and L. pro- of Glomospira, Glomospirella and Atnmodi- scus perraìn to the epifauna inhabiting shallow deep cerus (Liebus), associated with forms present at iower le- to water during the Early Meso-zoic. The asso- vels in the Prati di Stuores section (Gsollbergella spirolo- morphotype ciation suggests disaerobic and low energy culiformis, Sernimeandrospira ex gr. karnica-planispira, conditions of the Tkrriglomina carnica, Piallina tethydi). Agglutinated sedimentary environment. The duostominid- and involutinid-dominated asso- forms and duostominids are present also. ciations above 130 m to the top of the section (upper The comparison between isolated foraminiferal as- Daxatina cf. canadensis Subzone) may record an increase semblages and those in thin sections allows the fol- in energy and oxygen levels of the environment. lowing remarks to be made. 1, - Au/otortus seems absent in the thin sections. 2 - Prorakusia, lormerly known from the San Cas- Bivalves, gastropods and brachiopods. siano Fm. (di Bari & Laghi, 1994) and from Calcare del (Renato Posenato) Predil (Cordevolian (Rettori 1998) Auct.) et al., is absent Bivalves in the Stuores section are mainiy posido- in the Stuores section. niids. Gastropods are very rare in the lower plrt of the 3 - The Carnian affinity of the foraminiferal as- section, but become reiatively frequent in the upper semblages in the Regoledanus and lower Daxatina cf. ca- part, where they are mostly represented by allochtho- nadensis Subzones is indicated mainly by taxa observed nous specimens. Brachiopods are rare and occur oniy in only in thin section such as Gsollbergella spiroloculifor- the upper part of the section (Tab. 6). mis, Semimeadrospira ex gr. karnica-planispira, Tkrriglo- The majority of posidoniids have only concentric mina carnica and Piallina tetlrydis. undulations or ribs and a long hinge margin (P1. 9, fig. 4 - Assemblages recognised in washed materiais 6). Specimens with the same outline and ornamentation and in thin sections from the upper part of the D. cf. were classified by Kittl (1912; pI. 1, fig. 6-12) as Posido- canadensis Subzone are comparabie mainly because of nia wengensis (Wissmann). However, the generic attribu- the occurrence of involutinids (Lamelliconu). tion of this species is questionable because Posidonia is 5 - The most prominent increase in taxonomic di- characterised by a short hinge line (Cox, 1969). Other versity occurs in the upper Daxatina cf. canadensis specimens with the same outline and concentric orne- Subzone (segment C). mentation bear hardly perceptible radial costellae or 6 - Most species occurring in the Stuores section grooves on the posterior region; these are classified here are recorded in the Carnian strata of Turkey (Altiner & as "Posidonia" cf. uengensls (Pi. 9, [ig. 1,5) and could Zamnetti, 1981; Dager, 1978; Rettori et al., 1993); West represent a juvenile stage of Daonella or a transition to Carpathians (Salaj et a1., 1983), the Balkanides (Trifono- Halobia. Some other rare soecimens. without radial co- Prati di Stuores section, a GSSP candidate 61

Tab.6 - Occurrences of bivalves, bra- ll chiopods and gastropods in I the Prari di Stuores secrion i- 1. Number at right hand of s iÈ the sample name refers to li^ È' :i the distance in metres from * i3 Èì\ ii ì:; the underlying stake. àlÈ È È7s hesis concerning the tolerance of t67-178 posidoniids to low-oxygen values, the latter of rhese environ- have l5-16 mental factors seems to played a dominant role in the pelagic assemblage of the Stuores section. Transported shallow-water

7SW 10.5 forms, associated with au- zqv/!.1 tochthonous bivalve specimens 7SW 3.7 _-++tl o[ Koninckina leonhardi, firsr 6SW 10J occur at 105-115 m; aiiochtho- 1- Daxatina cl. canadensis nous patch reef taxa (corals, Dl- r òoz cosfttus maculosus, etc.) occur at 1,1,5-L25 m. According to Fiirsich & \íendt (1977), the trophic nu- cleus of the K. leonhardi association is represented by low-level suspension feeders which there- steliae or wlth only a posterior groove, have a small and fore needed aerobic conditions at the water-sediment in- narrow anterior auricie (P1. 9, fig. 2); they are tentati- terface" Pelitic intercalations contain "P"" ruengensis be- vely referred to Halobia. More, and better preserved ma- low 147 m, suggesting a likely alternation of disaerobic- terial is necessary to clarify the classification of these aerobic conditions in the water near the bottom in the posidoniids, in particular whether they belong to a sin- interval from 105 to about 150 m. The disappearance of gle or different species, and whether they represent a "P". wengensis and the frequent occurrence of nuculoids juvenile or ancestral stage of Daonella or Halobia. (section 2) above 150 m may suggest a change of the Posidoniid bivalves are considered traditionally as redox boundary which shifted inside the sediments. pseudoplanktic or nectoplanktic forms, even though epi- In conclusion, the depositional environment of the benthic, epibyssate or freeJying habits have been propo- Stuores section corresponds to a basin in which prevai- sed (Wignall Ee Simms, 1990; Aberhan &. Palfy, 1996). ling anaerobic to disaerobic conditions of the bottom wa- Posidoniids frequently occur in iaminated black shale fa- ter occurred in the iower part (from O to 104 m). As the cies associated with nektic forms (cephalopod$. Sedi- sediment filled the basin, water circulation increased lea- mentologic and paleontologic features of the posidoniid- ding to frequent aerobic events (Koninckina beds) alter- bearing layers suggest that they are a marker of lower nated with disaerobic events ("Posl donia" -bearíng marls) disaerobic (low bottom-water oxygen values) communiti- in the middle part (from 10a to 150 m). In the upper es (Allison et al., 1995). part of the section (from 150 to 180 m) more stable aero- In the Stuores section, posidoniids occur mainly bic conditions aliowed the settlement of nuculoids, in the laminated dark grey clay and argillaceous marl which occur frequently in section 2 (Aon Subzone). alternated with tuffites and calcarenites transported to the basin from shallower environments. According to Microcrinoids and holothurian sclerites. Fùrsich & Wendt (1977) Posídonia is a typical element (Gian Franco Laghi and Mariacarmeia Rechichi) of the "pelagic assemblage" of the San Cassiano Fm. which is characterised by the absence of benthic forms Microcrinoids (Crinoidea, Echinodermata) were and the dominance of nektic forms and was deposited in noted formerly from the San Cassiano Fm. but were the deeper parts of the basin. Due to either (1) high studied only recently by Kristan Tollmann (1970) who turbidity, (Z) high water content of the bottom sediment considered the high frequency of these fossiis as an indi- (very soupy substrate) or (3) oxygen-deficient bottom cator of typícal facies of the mid-upper Triassic of the waters, this assemblage lacks benthic suspension feeders Tethys, and compared them with the Jurassic Saccocoma (Fiirsich Er \ù7endt, 1,977). According to the new hypot- Facies (Kristan Tollmann, 197A). 62 C. Broglio Loriga et al.

; l: l-L-È: l{ I lÀìi,* iÈ ì : .!- q :€: ÈÈ l€ S li È ì * <'!ì aoià: + i È È : ri= ì : ùrt!È .È iù ; \ : ì.ì + 3 ù rÈ .!.r.ùlli : ì s ! F i;i ì iì i ì l i i.S: i i i=' :s,:.;ìiììi ]! i l9sw 0.0 r ssw-srr tsswti rTsw 6.0 16SW IL0 l6sw 8.0 l4sw i.5

11SW?.0

base o1' Daxatina cf. canadensis Sbz. (45 m) 64.1 ) l.ò

4SW 9.0 43\ / 5J -"

3SW 2.5 iSw sn

I s,v/ 1.5 lsw 0,0 a

| àD. / Range chart of microcrinoids (left) and holothurran sclerites (right) in the Prati di Stuores section. Number at right hand of the sample narne refers to the distance in metres from the underlying stake.

Bizzarini et al. (1989) and Bizzaríni (1993) then species Calc /amno idea cana/ tfera Kristan-To1lmann (64. 1 investigated the stratigraphic ranges of some taxa in the m), no significant change in the taxa of microcrinoid San Cassiano Fm. particularly from the Prati di Stuores and holothurian assembiages from lower levels is noted. - i.e. the type locality of the several species described by The holothurian sclerites are always very rare. Kristan Tolimann (1,970)- where the traditional Aon 102 - 177.7 m (upper Daxatina cf. canadensis Zone ìs documented. Subzone). A sudden increase in the holothurian sclerite New data from the Prati di Stuores section (Tab. taxa causes a remarkable diversity peak in their assem- 7) record the occurrences of eleven and thirteen taxa of blages at 136.1-138.8 meters. In comparison with the microcrinoids and holothurian sclerites, respectively. On eight genera, each represented by a single species, it is to the basis of the vertical ranges of the taxa and their as- be noted that the gents Tbeelta includes four species. semblage sequences, three segments vvere distinguished Microcrinoids are abundant also as individuals. but no as follows. prominent peak is recorded. 0 - 41.8 m (Regoledanus Subzone). Seven our of In conclusion, the results are as foilows. eleven microcrinoid taxa gradually appear. At 41.8 m, close to the first appearance of Daxatina the assemblage includes Osteocrinus rectus Kristan-Tollmann, O. sah/ibe- Microcrinoids. lensis Kristan-Tolimann, O. acus Kristan-Tollmann, O. 1- The assemblage, apart from minor changes, is sp., Axicrinu.s sp., Nololanx muhinodosa Kristan-Toll- similar to that of the Carnian Aon Subzone; the last mann and Ossicrinus reticulatus Kristan-Tollmann. Only occurrence o{ Osteocrinws acus in the Daxatina cf. cana- two species of holothurian sclerites (Etheridgella pentago- densis Subzone is the mosr prominenr evenr that distin- nia Krtstan, Acanthotheelia spinosa Frizzel & Exline) ap- guishes the two subzones. pear at 30.3-41.8 meters from the base of the section. 2 - The assemblage characteristic of the traditional 45 -1,02 m (lower Daxatina cf. canadensis Subzo- I-ower Carnian becomes complete at the first occurrence ne). Apart from the first occurrence of the single sclerite of Daxatina c[. canadensis. Pl. 9 Prati di Stuores section, a GSSP candidate 63

3 - Osteocrinus rectus is the most frequent taxon, 2 - The same assemblage continues, into the Aon and is found in all the "Osteocrinus Facies". In addition, Subzone but becomes poorer. the other species such as Osteocrinus gestlingensis Kristan Tollmann and O. saklibelensis Kristan Tollmann are 1on- Paleomagnetism. ge-range species. (Giovanni Muttoni & Wi1li:rm Low.rie) Holothurian Sclerites. Paleomagnetic techniques. 1 - A great diversity of the species belonging to the genus Theelia, characterises the upper Daxatina cf. Paleomagnetic samples at Stuores were collected canadensis Subzone. with a portable water-cooled rock drill and oriented

PLATE 9 Posidoniidae in the Prati di Stuores./Stuores $liesen section.

Fig.1 - "Posidonia" cÍ.uengensis (\lissmann).Sample7SW3.7,the specimenatthetophasveryfineradialgroovesandcostellaeonthe nnctcrinr reoinn Fig. 2 - ? Halobia sp. Sample 5S\l 8.0, the specimen on the left has a narrow ridge placed forward of the umbo which may represent the '-"':^- ^"';^l'' thus, it could be classified into HaLobia. However, radial sculpture is only represented by a sharp posterior groove. Fig. 3 - I Halobia sp. Sample /S\l 6.1, the larger specimen, on the right, has very fine radial costellee on the posterior region, but the anterior auricle is lacking. Fig. 4 ? Enteropleura sp. From debris between stakes 16 and 17 Fig. 5 "Posidonia" cÍ. uengensis ($fissmann). Sample 6S\f 10.5, interior surface of a right valve with a posterior radial groove Fig. 6 "Posidonia" c[. uengensis (Sfissmann). Sample 10S$l 4.3,

Scale bar 1 cm. 64 C. Broglio Loriga et aL.

with a magnetic compass. Drilling was performed al- section, whereas in the upper part it drops by about most exciusively in the harder sandstone and siltstone one order of magnitude. The initial susceptibility con- beds, thus resulting in a somewhat coarser sampling in forms to this trend with mean values of 4'.1O-3SI and the marly upper part of the section compared to the 5't10-4SI in the lower and upper part, respectively. A lower sandy-silty part (Fig. 6a). All but two of the 98 sharp decrease in both NRM and susceptibility values 2.5 cm diameter field core samples yielded one standard can be therefore traced within the "Ijntere Cassianer 11 cc specimen for analysis (two samples did not survive Schichten" between 73.3 and 77.3 m above the base of cutting in the laboratory). Paleomagnetic analyses were section (Fig. 6b). Susceptibility varies proportionally to carried out at the paleomagnetic laboratory of ETH Zù- |{RM (Fig. 7), which suggests that both parameters are rich. Stepwise thermal demagnetization treatments and controlled primarily by lithoiogy rather thrn by the measurements of natural remanent magnetization Earth's magnetic fieid intensiry variarions. (NRM) were performed on all specimens in a shielded Paleomagnetic samples typically show the presen- room with ambient fields less than 300nT. Heating and ce, in geographic (in situ) coordinates, of a scllttered low cooling were done in a shielded demagnetizer in which unblocking temperature component of viscous origin ambient fields are less than 5nT. Magnetic remanences consistent with acquisition along the present-day field were measured on a 2G Model 760 3-axis cryogenic ma- direction and/or induced at rendom during drilling or gnetometer mounting DC SQUID sensors. After each cutting. Above this low temperature component, inrer- thermal demagnetization step, the initial susceptibility pretable paleomagnetic directions were obtained ín 93o/o of selected specimens was measured with a Bartington of the 96 specimens. In plrticular. a bipolar charac- MS2 susceptibility bridge to monitor any mineralogicai teristic component oriented in situ north and positive alteration resulting from the heating procedure. Least- (Fig. 8a) or south-southwest and negative (Fig. 8b) was square analysis (Kirschvink, 1980) was used to determine isolated in 72o/" of the specimens in the temperature ran- the component directions of the natural remanent ma- ge between about 200"C and 450oC up ro 550/580"C gnefizafion, chosen by inspection of vector end point (Fig. 6c). In 10% of the specimens the characteristic demagnetograms (Zijderveld, 1967). Mean directions component could be followed up to maximum unbloc- were determined with standard Fisher statistics. The rock king temperatures of 600 to 630'C (Fig. 6c). An additio- magnetic properties were investigated by means of ther- nal l"L0lo of the samples show in situ westerly stable-end- mal unblocking characteristics of orthogonal-axes isother- point trajectories interpreted as transitional directions mal remanent magnefrzation (IRM) (I-owrie, 1990). associated with excursions of the Earth's magnetic fieid or acquired during a polarity reversal. The initial susceptibility often shows a sudden increase above about Paleomagnetic directions. 400-450"C which is related to mineralogical alterations The initial NRM intensity has a mean value o{ during heating (Fig l). FIowever, this alteration did not 0.2't10-4A/m in the volcaniclastic-rich lower oart of the usually hamper the recovery of the characteristic com-

PLATE 10

Microcrinoids and holothurian sclerites from the Prati di Stuores,/Stuores Wiesen section.

Fig. 1,5 - Osteocrinus aczs Kristan-Tollmann. Fig. 1) base of the dorsal spine, lateral view, sample i1 SV 4.0, 13Ox; Fig. 5) needle of the dorsal spine, sample 9SV 7.0,75x. Frg.2-3 - Osteocrinus /ectzs Kristan-Tollmann. Fig. 2) base of the dorsal spìne, lateral view, s:rrnple 11S\W 4.0,100xr Fig.3) rrdial plete, frontal view, sample 8Slf 7.7,4Ax. Fig. 4 - Osteocrinus goestlingensis Kristan-Tollmann. Radial plate, frontal view, sample 6SV 10.0, 50x. Fig.6 - Osteocrinus reticulatus Kristan-Tollmann. Base of the dorsal spine, lateral view, sample 18S\l 0.5, 130x. Fig.7 - Osteocrinus sakliebelensis Kristan-Tollmann. Base of the dorsal spine with radial ring, lateral vieq sarnple 11S\V 4.0, 100x. Fig.8-9 - Nodolanx muhinodosa Kristan-Tollmann. Fig. 8) radial shield, frontal view, sample 11SV 4.0, 4Ox; Fig. 9) aboral shield, frontal vìew, sample 19S\f 0.0, 35x. Fig. 10 - Acantbotbeelia spinosa Frizzel &Exline. Holothurian sclerite, sample 14S\l 3.5, 100x. Fig. 11 - Tbeelia guembeLi Kristan-Tollmann. Holothurian sclerite, sample 11SV 4.0, 170x. Fig. 12 - Axìuinus sp. Brachial plate, lateral view, sample 11SV 4.0, 25x. Fig. 13 - Theelia pralongiaeKristan-Tollmann. Holothurian sclerite, sample 14S1W 3.5, 140x. Fig. 14 - Tbeelia serfa Speckmann. Flolothurian sclerite, sample 14SS0 3.5, 180x. Fig. 15-1ó - Axicrinus alexandri Kristan-Tollmann. Fig. 15) radial shield, frontal vrew, sample 14S\X/ 3.5,35x; Fig. 16) brachial plate, lateral view sample 14SSl 1.5, 40x. Frg. 17 - Tbeelia tubercula Kristan-Tollmann. Holothurian sclerite, sample 14S\7 3.5, 190x. Fig. 18 CalcLigula triassica @rizzel & Exline). Holothurian sclerite, sample 18SV0.5, lOOx. Fig. 19 - Placerotapis subpLanus Kozur & Mostler. Holothurian sclerìte, sample 145\73.5, 180x. Fig.20 - Tulipacrinus sp. Radial ring, ventral view, sample 14S\f3.5,30x. Pl. 10 Prati di Stuores section, a GSSP candidate 65 bb C. BrogLio Loriga et al.

Sample Meters VGP lat Polrity In situ overall mean direction: 1+ 7.70 1.5506 74.5 N Declination 2.0, Inclination 39.8, k:/, a95:5.9, N:89 1+3.20 2.9187 80.9 N 1+ 4.45 4.0588 64.6 N Tilt corrected overall mean direcrion: 1+ 5.90 5.38 14 75.6 N L+7.13 6.5033 64.5 N Declination 359.4, Inclination 16.5,k:7, a95:6, N:89 1+7.73 7.0545 57.7 N L +9.23 8.41.87 75.7 N Tilt corrected mean paleopole calculated àt 46.55N/11.82E (Stuores co- 1 + 9.90 9.4298 73.8 i\ 2+ 1.30 10.406 83.8 1\ ordinates): 2+2.15 11.261. 81.8 t\ Longitude 192.8, Latitude 5 1.9, àp / dn : 3.2/ 6.2 2+ 3.35 1?.467 66.8 t\ 2+4.24 13.321 75.6 N 2+ 5.34 14.426 85.6 N 2+ 5.4A 14.527 76.6 N Tab.8 - Paleomagnetic data from the Prati di Stuores secrion. 2+8.25 1.7.391 84.4 N . "Sample" is paleornagnetic sample; "Meters" is meters 2+8.95 L8.094 45.2 N "VGP 2+ 10.00 19.150 80.7 N from base of secrìon; lat" is latitude of virtual geo- 3 + 0.90 20.050 81.7 N magnetic pole; "Polarity" is polarity interpretation: "N" 3 + 1.74 20.850 69.2 N ('R') is full normal (reversed) i.e. 3 + 4.50 n.654 80.6 N polarity, 3 + 5.50 24.654 81.8 N +90

a)^\ L\u) c) d) e) Suscentibility anJ NRltl Teùpemiurc spectra of the + hard c@rcivity component >lrees samPres Blow-up 5()0"C h l(X)'C nomalized "Ch" componert (oC) +soft coercivity componcnt 0 0.2 0.4 0.6 0 200 400 600

te-l17t2 -111.j11 -176.03 -'.--171.13

l8_t6,9s _l6.es

153 03 - r?-r526r =:ii:;ir5rel

-l$.q:Ut:91

15=ló--*140.78 ----11073 I

-.-.. lr.q I

l{-----ll4.s *-r3{.ó I I

-..... lll.l2 I '.-- 129.3ó _l

i I " lll19,)- tì-rrì^r r I Tcmperaturc "C l1r.0.ll

l16.15 - [=12-il12n -.-.-Lt].ìl

-lll.l5 *10s.35

l0-t04.lt :'...i31:# -1m.70 _ì :, l

8-E{.30

-, - 77,lrl il;fi tliilì::iì::ìiii::!!iXliii!:Ìffi jì!iìllili 7-71 25 73.10 - 7t.91 -

---- 657 ó5.f3 - i ó-ó2.40 _ :l 61.39 -l I I _ 53.0: _i i* F 55.10 g rlr 5b---J2.85 *-- !.85 :-t I t,, J1.a1 .-- Temperature'C - -l Tcmpcralurc oC jl òj rinT 5-4r 78 ------ji:9à a+4.s6 [ I _ i73t

:--- lt.ll ...... :

r28.58

l- 19.15

Érn 2-9.t0

:.91 - l-0.& 68 C. Broglio Loriga et aL.

Fíg.7 - Diagram of normalized su- sceptibillty versus natural re- ( rnanent rnagnetization (NR .//' É M) values for the Prati di c) Stuores samples. The suscep- N .t)...o$ /' ^'{ tibility and NRM intensities t ,/ ^$$"' are normalized with respect - ,t',*trt+ov to their maximum values of, respectively, 3.4'r1O-2Sl and L.7't7a-4A/m. ! n5 a = 0.87555 b=0.0029228 R= 0.91708 () 6 a U) a./ t. a a

(, 0.5 I NRM normalized

Stuores are dominated by a low coercivity and cà. w,Up 580'C maximum unblocking temperature phase interpreted as magnetite, maybe co-existing with subsidiary 600- sulphurs characterised by ca. 32A350oC maximum un- 630 / 580 blocking temperatures (Fig. 6d). Moreover, careful inspection of these curves show that a subsidiary magnetic phase with higher coercivity and unblocking temperature, like hematite, may be also present ar places (e.g. sample 16+8.28, Fig. 6d, e). Such a conclusion supports the previous observation that in a few cases the bipolar characteristic component of NRM could be rraced up to a maximum unblocking temperature of 630"C. A) IN sITU Tick = I mA/m (volume = llcc)

Magnetostratigraphy and magnetostratigraphic correlations.

i6+5.45 A virtual geomagnetic pole (VGP) was calculated for each characteristic component stable endpoint direction after correction for bedding tilt. The latitude of the specimen VGP with respect to the overall mean north paleomagnetic pole was used to delineate the magnetic polarity srratigraphy (Kent et al., 1995). VGP relative latitudes approaching +90oN (-90'N) are interprered as recording normal (reversed) polarity (Fig. 11a, Tab. 8). For polarity magnetozone identification, we adopt the nomenclature used by Kent et al. (1995). We assign integers in ascending numerical order from the base of the IN SITU Tick 0.1 mA./m (volume = I lcc) b) = section to polarity intervals as defined by successive pairs of predominantly normal and predominantly reversed magnetozones. Each ordinal number is prefixed Zrlde:iveld thermal demagnetization diagrams of NRM of by the acronym for the source of the magnetostrati- representative samples frorn the Prati di Stuores section graphy (i.e., "S" for Stuores), and has a suffix for the with normal a) and reversed b) polarity characteristic ma- dominant polarity ("n" is normal, "r" is reversed) of gnetizations. Closed symbols are projections onto the hori- each constituent magnetozone. Polarity intervals that zontal plane and open symbols are projections onto the ver- as tical plane rn in situ coordinates. Demagnetization ternpera- may occur within a magnetozone are referred to tures in "C. submagnetozones and can be labelied in a parallel man- Prati di Stuores section, a GSSP candidate 69

Fig. 9 - Diagram of nornalized susceptibility as {unction of r",-....î,,"" f^. representative samples from Prati di Stuores section. Susceptibili- >| ty is normalized with respect to a maximum value of 1.Z+ 10-251.

0) c/) u.)

N z

600 700 Temperature ("C)

Fig. 10 - Equal-area projections before In Situ Tilt Corrected (in situ) and after bedding Y ;.. tilt correction of the bipolar and transitional charac- ':':1':5.i' o-o'J teristic cornponent which a yielded an overall mean di- " Jl ;'-' o o . a- rection in tilt corrected coor- af,a a_'"-r dinates of Dec. : 359 .+, N=89 N=89 - Inc.: 16.5 for the Prati dì Stuores section. o- oo_ o_a o o_ Ò-& o - oó- o- o ' o- o^u o- o- o oo o-a

ner by assigning to successive pairs of submagnetozones Mayerling (Fig. lZ). Towards the top the correlation be- subordinal integers (ascending upsection) which are then comes less clear. It is possible that the reversed magneto- appended after a decimal point to the higher-order ma- zone S2r at Stuores correlates at Mayerling with a gnetozone designation and given a suffix indicating do- "submagnetozone" located somewhat below 40m and minant polarity. here n;med ?MA4n.lr. lt is worth noting that the The latitude of the VGPs defines at Stuores a "submagnetozone" ?MA,ln.1r at MayerÌing occurs at or lower normal (S1n)-reversed (S1r)-normal (S2n)-reversed very close to a sharp lithological transition located in (S2r)-normal (S3n)-reversed (S3r)-normal (San) magneto- the upper part of the Diebeli conodont zone, between zone sequence (Fig. 1lb). lntermediate VGP latitudes are thinly-bedded limestones below and thickly-bedded preferentially located at polarity transitions. The base of limestones above (see figure 10 in Gallet et al., 1998). the Carnian as defined by the base of the Daxztina cf. Therefore, a hiatus may be present at Mayerling which canadensis subzone falls towards the base of normal ma- encompasses most of the reversed magnetozone s2r at gnetozone S2n. Stuores. If so, the overlying normal magnetozone S3n at On the basis of magnetostratigraphic data and the Stuores corresponds to submagnetozone MA4n.2n at vertical distribution of conodont taxa, the Ladinian/Car- Mayerling, S3r to magnetozone MA4r and, finally, S4n nian boundary at Stuores can be tentatively correlated to submagnerozone MA5n.1n (Fig. 12). This correlation with the coeval Mayerling section from Austria (Gallet et would suggest that the first occurrence of Gondo/elLa a.I., 1998, fig. 11). We propose that the reversed magneto- poLygnatbtformis àt Stuores, presently located in the zone S1r at Stuores correlates with magnetozone MA3r lowermost part of the section 2 (Fig. 1), may be lower, at Mayerling, and that the normai magnetozone S2n at within magnetozone S3n. Moreover, the base of the Stuores corresponds to submagnetozone MA4n.1n at Carnian at Stuores, placed at the first occurrence of 7A C. Broglio Loriga et al.

Daxatina, can be traced at Mayerling in the lower part The lowstand systems tracr (LST) consists mostly of the Diebeli Assemblage- Zone. Finally, the correla- of more or less coarse-grained volcano-sedimentary de- tion proposed here implies that the sedimenrarion rate posits (e.g. Marmolada Conglomerate). Layers including .was of the turbidite sediments at Stuores on average carbonate olistholiths ("Cipit limestones" p.p.) are char- about 8 times higher than that of the pelagic carbonares acteristic. They derive partly from the destruction of at Mayerling. previous carbonate buildups, and partly from carbonare fringing reefs grown on a previous slope during rhe late LST. TST deposits are defined by the strong decrease in Sequence stratigraphy. terrigenous content and the appearance of fine-grained terrigenous-carbonate (Piero Gianolla & Claudio Neri) facies (upper part of the La Valle Fm.). In the Prati di Stuores, the maximum flooding The Prati Stuores di section is illustrative of the surface (mfs) seems to 1ie close to La Valle Fm.,/San Cas- basinal stratigraphy in the wesrern Dolomites after the siano Fm. boundary; it yielded ammonoids belonging l.rte L.rdinian peak in volc.rnic rcriviry (Fig. 13). The up- to the topmost Regoledanus Subzone (sensu Mietto Ec per part of the La Valle Fm. (iowermost part of the sec- Manfrin, 1995b). In the basinal areas rhe Car 1 HST records tion) a marked decrease in sedimentary supply corresponds to the lower part of the San Cassiano Fm., and consists of calcilutites, marls and claystones. A pro- interfingered with the Cassian Doiomite 1 (De Zanche gressive upward increase in shallow-water carbonate con- et aL, 1.993). In carbonate shelf areas, the next sequence tent and a new increase in volcano-sedimentary supply boundary (SB) is placed ar the rop of the eroded and (San foliow Cassiano Fm.). The carbonate supply re- karstified Cassian Dolomite 1; in basinal areas, the Car cords the progradation of a carbonate platform (Dolomi 2 SB falls at the strong increase of clastic supply which te), while siliciclastics indicate the presence of a near is also recorded in the upper pert of the Prati di Stuo- volcano-terrigenous coastline. reslStuores Viesen (cf. Urlichs, 1974, 1994), i.e. above The sequence stratigraphy of the crucial interval, biocalcarenitic and oolitic turbidites (Car 1 HST). including the Ladinian/Carman boundary, has already In the Prati di Stuores/Stuores Wiesen secrlon, been taken into consideration by many authors characterised by a high sedimentation rate, the proposed (Brandner, 1.984, 1.991; Doglioni et aL, L990; Bosellini, Ladinian/Carnian boundary lies within the Car 1 earìy 1991; Masetti a1., 1991; et Yose, 1,991;De Zanche et a1., HST. In correlated sections with low sedimentauon rate 1993; Neri et al., 1.994, 1996; Mastandrea er aI., 1997; throughout the Dolomites, it likely falls very close to Gianolia, 1995; Gianolia et a1., 1998). On the who1e, the maximum flooding surface (mfs). most of these authors agree a sequence on stratigraphy The possibility of correlating the Car 1 DS over a setting including a LST and a TST made up by the La great distance indicates its chronostratigraphic value. ValÌe Fm. and a HST documented by the progradation In the eastern part of the Northern Calcareous of a carbonate platform and equivalent basinal deposits Alps, the Car 1 DS can be recognised within the Rei- oi rhe San Cassiano Formarion. flinger Kalk. Taking the Scheiblinggraben secrion as a According to De Zanche et al. (1993) and Gianol- reference (Mostler & Scheuring, 1974; Krystyn, 1991), (1995), la the whole Prati di Stuores/Stuores \íiesen sec- the Daonella lommeli-bearing marls represent the LST, belongs tion to the Car 1, 3rd order, depositional se- and the overlying cherty limestones (FS 19 to FS 18) quence (DS). The Car 1 DS includes the La Valle Fm., and the radiolarian micritic limestones correspond to the lower part of the San Cassiano Fm. and the Cassian the TST and the HST, respectively. The overlying shales Dolomite 1. represent the Car 2 LST. On the basis of conodonts, rhe In the Dolomites the Car L sequence boundary Ladinian/Carnian boundary should fa1l just above sam- (SB) corresponds to a regional unconformity. In the car- D1e 'tr) tv. bonate shelf areas it is represented by a major erosion In the western part of the Northern Calcareous and karst surface lying on top of the Sciliar Dolomite 3 Alps, the Car 1 DS may be correlated with the L4 DS or the oldest carbonate platform. In the basinal areas in Rúffer & Zùlcke (1,995). the Car 1 SB is an important submarine erosional surfa- In the German domain, the Car 1 DS corre- ce on lJpper Ladinian volcanics or volcaniclastics; local- sponds to part of the K2 DS (Hauptsandstein-Obere 1y the erosion cuts deeply into older, underlying units. Lettenkeuper-Grenzdolomit-iower part of the Gipskeu-

pl^r F;. 1 I ^f th. '.1.tivs VGP latitudes of the characteristic component as a function of stratrgraphic position with polarity interpretation for the Prati di Stuores section. Magnetic polarity zones (i.e. magnetozones) are shown by filled (open) bars for norrnal (reversed) polarity; single-sample polarity zones are sho-n by half bars. Transitional VGPs are represented by shaded bars. Thichness is expres- sed in meters from the stake 1. Prati di Stuores section, a GSSP candidate 71

a) b) Vinual Geomagncric Polc lÀtitude (") Silmples Ii:'i"Hr' I fl,"',,'i,1"'"u ffirrunsilional Vfrp,'t .lrt.r .rt p"lr -45 0 ì.15 ffipolrrity -z\rrtytrrn.rtion

,- _-- _^ _ t73t7 ---'17601

_ l7l 5, -l?t.tl lE _166.9i _ t6ó.ei

03 -_153

L7-L5r6s n -iiìò.t.1

_ tJ3.0t -[393

t6-1f0 lE rr0.78 - B30J t4-L-ì4.ú -lrt.6r 1l -ll1

120 120 S3n -ì16t5 l:-|110 rl - '-111.t5 S2r

t0-lot r5 :iiì,l:il_t0l.6l 100 93.17 - q: e-rj (rr - irl 9r 1l _ r)l óJ

8_81.10

1)rr 80 77.1) a a _ 7t.ll

--- ó6 5l -. ó5.13 (.) 6-ó1.40 ''. ólll61.03 61.19 ,* - 59.19 60(, 53.15 -,,,,,- 56 75 5J1) - .5J10 5b-51.85 5t 35 - \/n x -sltl d . -- 1737 ló9i -''_-.. J5 t5 t jtli rr " i-rr7R :l- !r 4l) S1r _ ó.1 t-r I L_l___ '1 t-:8.58 /

_ luu5 ro l_ 19.15

'' il16

ì_9 l0 ?rll

L-0.m 72 C. Broglio Loriga et aL.

Moyerling, Austrio l E o l9

E ó o tr o E o o I

180

ló0

S3r 140 o. !

S3n 120 c S2r a o o

80 Drop in NR[,4 o .q And SusceDt tl ii/ E oo

c !:

o ,a o

o o : Siuores, ltoly .q E ! o ! o o b co C -s É

E E c

Fig. il Comparison of magnetostratigraphic and biostratigraphic data from this study and the MayerLng section from Austria (Gallet et a1., 1998) for the Ladinian/Carnian boundary of the Tethys realm. Biostratigraphy at Mayerling is based on conodonts. Polarity nomenclature at Mayerling is here informally introduced for clarity because it was nor formally established in Gallet et al. (1998, fig. 10). 'We follow for Mayerling the system described for the Stuores section which we prefer to the system consisting of letrers in ascending alphabetical order from the base of section which was used in Broglio Loriga et al. (1998, fig. 3) and in the composire rnîgnerosrrÀri- graphic scale of Gallet et al. (1998, fig. 12). Magnetic polarity intervals MF-, MG+, MH-?, MI+, ML- and MM+ rn Broglio Loriga et al. (1998) correspond to MA3r, MA4n.1n, ìMA4n)1r, MA4n.2n, MA4r and MA5n.1n in this paper, respectively. The thicl

lbis

r.- lr E Stakes # I i3 s LL : -, ÈE € o 19> 9q o

SAn t'-l-T- 18>-', 3 l---: :-:-- o a N 17> N .cl i '1 s o 5-16 > @ I (E 14 p s3r .9 e .9 ci o € r-I !) z 3 13> I G € ol l S3n o G q 'A o o 1't-12 > s2r p A I g o .e g > 10> Ò : G c 3 t: x 9> s g o o P p * B> eH t ftt .p I *3 S E t- I àó I 7> O ES F I ls 6> * (u

6 5b> O S2n l I

a I 5> ".P os Slr 3$ z 4> s' (g sI 3> ,A : Conodonts Pollen a z 2> and spares 1> o - . open nom€nclalure =tII

Ammonoids I ffiTE (ú full normal lransilional lull reversed gap oi dala J polarily polarity polarity at polafity (g lrans[0n J

Fig. 13 - A synthesis of the rnain stratigraphic results in the Prati di Stuores section. Lithostratigraphic colurrns correspond to the sections 1 and 1 bis in Fig. 1. Numbers end triangles on the left indicate the stakes. Ammonoid, conodont and palynomorph distributron refer to selected taxa.

per) in the sequence stratigraphy framework of the Ger- Keuperkporites baculatus, referred to the uppermost Ladi- man Triassic by Aigner & Bachmann (1,992). The rest of nian (Brugman et a1., 1993). On the other hand, Brug- the K2 DS (: upper part of the Gipskeuper) forms a man (1983) pointed out that the appearance of Enzona- new DS (Car 2). Palynomorphs allow the correlation of lasporites aigens rn the lower part of the Gipskeuper the upper part of the La Valle Fm. (Car 1 TST) and the (HST), also occurs in the Prati di Stuores section. Obere Lettenkeuper, which both bear the characteristic Prati di Stuores section, a GSSP candidate 73

,fl r.l 1 ois _-ìri PH | Rr ,1, I i î"

Stakes T---:r Ì lt î LL !-- i o 19> :l =i--:=î i fi c I Rr'.n frr= i 18 >'"' 3 F.--= i o -

:l N 17> Ì I g,a I ì hir 1 3 .ol i q) o 15-16 > E i S3r È I tt (E 14 > .9 e '-tl, c z 0) E 13> 3 I T'(! oi o 5Jn ,q o îÍ 11-12 ol > s2r o g.g i o .a >.i 10> Ò i Q G I : (g -c p x 9> : (E & g o o ,. .ò s o B (E B> e f; l *e È ) I E 7> ìo És F ls 6> ÈR- Nó 5b> qJJ S2n ri Ei 5> $.i S/r ei z 4> fi sI

3> 'S Conodonts Pollen z 2> and spores 1> 51n o o oDen nomenclalure

Ammonoids Iffi ftE lullnormal lransilional lull reversed gap ol dala J polaily polarity polarily at polarity Iranslon

_^bF;ù _"I 1 - a "..-tL-";. ^{ .he main stratigraphic results in the Pratr di Stuores section. Lithostratrgraphic colurnns correspond to the sections 1 and 1 bis in Fig. 1. Numbers and triangles on the left indicate the stakes. Ammonoid, conodont and palynomorph distribution refer to selected taxa.

per) in the sequence stratigraphy framework of the Ger- Keuperisporites baculatus, referred to the uppermost Ladi- man Triassic by Aigner & Bachmann (1992). The rest of nian (Brugman et al., 1993). On the other hand, Brug- the K2 DS (: upper part of the Gipskeuper) forms a man (1983) pointed out that the appearance of Enzona- new DS (Car 2). Palynomorphs allow the correlation of lasporites aigens ín the iower part of the Gipskeuper the upper part of the La Valle Fm. (Car 1 TST) and the (HST), also occurs in the Prati di Stuores section. Obere Lettenkeuoer. which both bear the characteristic Prati di Stuores section, a GSSP candiclate 75

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