P44_copertina_R_OK C August 20-28,2004 Florence -Italy Field Trip Guide Book - P44 G. Roghi,F. Russo L. Keim,F. Mauer, C.Neri,N.Preto,A.Riva, Associate Leaders:P. Brack,P. Gianolla, Leader: M.Stefani ARCHITECTURE OF THEDEPOSITIONAL FLUCTUATIONS ANDTHESHAPING RELATIVE SEA-LEVEL CARBONATE PRODUCTION, DOLOMITES: PLATFORMS OFTHE TRIASSIC CARBONATE 32 Volume n°5-fromP37toP54 GEOLOGICAL CONGRESS Post-Congress nd INTERNATIONAL P44 18-06-2004, 14:40:21 The scientific content of this guide is under the total responsibility of the Authors

Published by: APAT – Italian Agency for the Environmental Protection and Technical Services - Via Vitaliano Brancati, 48 - 00144 Roma - Italy

Series Editors: Luca Guerrieri, Irene Rischia and Leonello Serva (APAT, Roma)

English Desk-copy Editors: Paul Mazza (Università di Firenze), Jessica Ann Thonn (Università di Firenze), Nathalie Marléne Adams (Università di Firenze), Miriam Friedman (Università di Firenze), Kate Eadie (Freelance indipendent professional)

Field Trip Committee: Leonello Serva (APAT, Roma), Alessandro Michetti (Università dell’Insubria, Como), Giulio Pavia (Università di Torino), Raffaele Pignone (Servizio Geologico Regione Emilia-Romagna, Bologna) and Riccardo Polino (CNR, Torino)

Acknowledgments: The 32nd IGC Organizing Committee is grateful to Roberto Pompili and Elisa Brustia (APAT, Roma) for their collaboration in editing.

Graphic project: Full snc - Firenze

Layout and press: Lito Terrazzi srl - Firenze

P44_copertina_R_OK D 26-05-2004, 15:11:36 Volume n° 5 - from P37 to P54

32nd INTERNATIONAL GEOLOGICAL CONGRESS

TRIASSIC CARBONATE PLATFORMS OF THE DOLOMITES CARBONATE PRODUCTION, RELATIVE SEA-LEVEL FLUCTUATIONS AND THE SHAPING OF THE DEPOSITIONAL ARCHITECTURE

AUTHORS: M. Stefani1, P. Brack2, P. Gianolla1, L. Keim3, A. Mastandrea4, F. Mauer5, C. Neri1, N. Preto6, E. Ragazzi6, A. Riva1, G. Roghi7, F. Russo4

1 Università di Ferrara - Italy 2 ETH, Zürich - Switzerland 3 Boze Autonome Provinz - Italy 4 Università di Calabria - Italy 5 Petroleum Institute - Abu Dhabi 6Università di Padova - Italy 7CNR Padova - Italy

Florence - Italy August 20-28, 2004

Post-Congress P44

P44_R_OK A 4-06-2004, 11:29:14 Front Cover: Middle Triassic, clinostratifi ed slope breccias forming the southern portion of the Catinaccio-Rosengarten Massif, here visible in a spectacular summer sunset light.

P44_R_OK B 4-06-2004, 11:29:17 TRIASSIC CARBONATE PLATFORMS OF THE DOLOMITES CARBONATE PRODUCTION, RELATIVE SEA LEVEL FLUCTUATIONS AND THE

SHAPING OF THE DEPOSITIONAL ARCHITECTURE P44

Leader: M. Stefani Associate Leaders: P. Brack, P. Gianolla, L. Keim, F. Mauer, C. Neri, N. Preto, A. Riva, G. Roghi, F. Russo

Introduction (Gaetani et al. 1981, Senowbari-Daryan et al., 1993; Gianolla P. and Stefani M. Russo et al., 1998b, 2000), the biostratigraphic The spectacular Triassic outcrops of the Dolomites and chronological framework was substantially have been playing a major role in the understanding refi ned (Brack & Rieber, 1993; Mietto and Manfrin, of the carbonate platforms since the XIX Century, 1995a), the sequence stratigraphic understanding as witnessed by a the huge number of publications, was enhanced through basin-platform correlation mainly written by German, English, French and and refi ned dating (Gianolla et al., 1998a and Italian speaking geologists. The seminal studies references herein). During the last 20 yr, the origin by Richthofen (1860) and Mojsisovics (1879) of the platform-top sedimentary cyclicity (Figure already recognized the “reef” nature of the 1.2) has triggered a hot debate, particularly on the Dolomite platforms, described their steep slope interpretation of the Latemar Platform (Goldhammer clinostratifi cations (Ueberguss-Schichtung), and et al., 1990; Brack et al., 1996; Egenhoff et al., provided a fi rst bio-chrono-stratigraphic framework 1999; Preto et al., 2001), without, for the time being, (Figure 1.1). After a somewhat extenuate research reaching any eventual conclusion. period during the fi rst half of the XX century, great The Dolomites Region is placed at the junction attention was refocused on the Dolomites successions between German, Italian and Ladin speaking areas through the last 40 years. During this time interval, and each individual place is therefore often described a fi rst geometric and sequence stratigraphic synthesis by three quite different names (e.g. Rosengarten = was achieved (Bosellini, 1984), the major role of the Catinaccio = Cadenàc, second c pronounced as in non coralline bioconstructors and the importance of child), the use of which is still triggering sensitive the synsedimentary cementation were recognized socio-political emotions. The intrinsic stratigraphic

Figure 1.1 - The Mojsisovics’ (1879) “prophetic” geological profi le of the visited Cernera – Crepa de Formìn carbonate platforms. The geometric relationships between the depositional bodies are essentially depicted as in the modern P37 to P54 n° 5 - from Volume interpretation, even if some minor brittle tectonic structures are missing and the chonological interpretation provided by the original German text is somewhat different form the modern one. Moving from SW to NE, observe the fault, presently considered as an overthrusting of Permian evaporites (a Bellerophon Schichten) onto Middle Triassic volcanogenic units (g Augitporphyrtuffe), the Anisian Upper Serla Plafrorm (Unterer Mushelkalk), the low relief Contrìn Platform (d Oberer Mushelkalk) interfi ngering with Dont Fm basinal beds (e Buchensteiner Schichten), the aggradational-retrogradational uppermost Anisian Cernera Platform (g Wengener Dolomit), which was terminated by an early drowning and onlapped by terrigenous and volcanoclastic beds (f Augitporphyrtuffe and g Wengener Schichten), followed by basinal argillaceous-calcareous beds (Cassianer Schichten), shallowing up into a Cassian platform (h Cassianer Dolomit). For further explanation see introduction and Day 4 texts.

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Volume n° 5 - from P37 to P54 P44 - P44 Leader: M.Stefani preserving thissignifi has chosennottoimposehispersonalopinions, Stefani), whilethoroughlyreviewing thepaper, diverging geologicalviews; theguideeditor(M. scientifi authors themselves enjoy different linguisticand stratigraphic pictureoftheDolomites. The guide nevertheless feltcompelledtostillgive anarticulate chrono-sequence stratigraphicterminology, but we made someeffort tosimplifytheintricatelitho-bio- the Dolomitesquiteacomplex oneindeed. We have combine tomake thestratigraphicterminologyof and theglottologicalcomplexity ofthearea variety, thelonglastinggeologicalresearchhistory units willbevisitedduringthetrip. surfaces, theinterpretationofwhich hastriggeredahoddebate, throughthelast20years.Coevalplatform andbasinal Figure 1.2- A spectacularviewofthecyclicLatemarplatform-top succession,punctuatedbyhighfrequencyemersion platforms oftheDolomitesgrew inquite anactive their large depositionalgeometry. The carbonate slope andplatformfacies, always framedwithin The excursion will beaimedatillustratingbothbasin, clarify any discussion. view ofthespectacularoutcrops oftheregion will to somedegree of complexity; wehopethattheactual research initsmaking,attherisktoexpose thereader richness andasaway toillustratethegeological c backgroundsandhave sometimeexpressed cant diversity asascientifi c anisotropy thatwas tosignifi and massive magmatism,inducingalithospheric and magmaticevents including:(i)Permianrifting Tethys Ocean. The region recordsseveral tectonic of apassive continentalmargin oftheMesozoic deriving formthecomparatively gentlydeformation belonging tothemuchlarger Alpine Chainand 2000), anonmetamorphicsouth-vergent thrustbelt 1987; Castellarinetal.,1998;&Cantelli, portion oftheSouthern Alps (Figure1.3,Doglioni, The DolomiteMountainsformthecentral-northern Regional tectonicsetting Day 5). relief, terrigenous-carbonateunits(Falzarego area, The youngervisitedunitsconsistofCarnianlow volcanic (Sella,Day3)isolatedhighreliefplatforms. pre- (Cernera,Day4;Marmolada,6)andpost- Day 1;Seceda,Odle,2),tomove then onother pre-volcanic platformandbasincarbonates(Schlern from westtoeast,startingwith Anisian-Ladinian a Middle Triassic magmaticevent. The tripwillmove structural framework andwereseverely affected by cnl infl cantly une the uence 26-05-2004, 15:21:35 P44_R_OK 5 just non-palinspasticrepresentationofthepresent-day sketches hereafterillustrated(Figure1.6)aretherefore Marmolada area(Day6). The “palaeogeographic” area diffi detailed palaeogeographicreconstructionofthe and thestructuraltelescopingcombinetomake the signifi deformation. The and generatinglarge overthrusting andstrike slip in nature,affecting theregion during Tertiary times of compressional Alpine deformation,mainlybrittle the visitedarea.(iv) Several superimposedphases times, withoutproducingany known magmatismin into thewestern Tethys opening,duringJurassic rifting, startingintheUpper Triassic andclimaxing visited carbonateplatforms.(iii)Continentalmargin dynamics playedamajorroleintheshapingof the deformationfollowed. This Middle Triassic (Sloman, 1989). A lateLadinianslowing down of Cima Pape) andasignifi induced epicrustalintrusions(Monzoni,Predazzo, into amagmaticevent. The short-lived Ladinianevent differential subsidenceandupliftingclimaxing (trans-) tensionaltectonics,associatedwith Triassic and Alpine evolution. (ii)Middle Triassic cult, asforinstancevisibleinthevisited Figure 1.3-Structuralscheme oftheDolomitesandsurroundingSouthernalpineregion. cant shoshoniticvolcanism cant tectonicshortening TRIASSIC CARBONATEPLATFORMSOFTHEDOLOMITES PRODUCTION, RELATIVESEALEVELFLUCTUATIONSANDTHE SHAPING OFTHEDEPOSITIONALARCHITECTURE variability (carbonateversus basinalunits). which islargely infl which isvisibleinthespectacularregional landscape, several massive glacialepisodes,theimprintingof the Quaternarytimes,whichsaw thedevelopment of generated duringthelast5millionyears,even during region. A large portionofthepresentelevation was Tertiary basalticdikingisknown fromtheDolomites distribution ofthestratigraphicunits.Onlyminor however lackingintheeasternDolomites. The locally exceeding 2000m;thesevolcanites are Porphirit, mainlyriodaciticinnature,withthickness of athickvolcanic package,theBozenerQuartz (trans-) tensionalriftingresultedintheaccumulation eroded, toformtheregional basement. The Permian metamorphosed Palaeozoic rockswereupliftedand Carboniferous Variscan orogeny, deformedand one forthestudyofthisperiod.Following the Triassic formations,makingtheregion aclassical but theareaissharplydominatedbyimpressive includes PermiantoCretaceousunits(Figure1.4), The stratigraphicframework oftheDolomites Regional Stratigraphy (After Castellarinetal.(1981)–modifi uenced bythe strongstratigraphic ed ). 5 -

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Volume n° 5 - from P37 to P54 P44 - P44 Leader: M.Stefani (Modifi Haupdolomite (DP);Dachstein Limestone(CD);CalcariGrigi(CG);Rosso Ammonitico (RA);PuezMarl(MP)- Cassiano Fm.(SC);CassianDolomite(DC);Heiligkreuz/Dürrenstein (DD);RaiblFm.(R);DolomiaPrincipale/ (h), Chaoticmegabrecciae(Ch),dykes (d);La Valle/Wengen Fm.(FM,LV), MarmoladaConglomerate(MC);San Buchenstein Fm.(B);ZoppèSandstone(Z);Sciliar/Schlern Fm(SD); Volcanics (V):pillow lava(p), hyaloclastites Evaporites (Be); Werfen Fm.(W);BraiesGroup(GB); Richthofen Conglomerate(CR); ContrinFm.(C);Livinallongo/ (g); BasalConglomerate(BC); Acidic Volcanites (P);GardenaSandstone(GS);BellerophonFm:Black limestone(Bl), Figure 1.4-Schematic sketch ofthecentral-western Dolomitesstratigraphicsuccession. Metamorphics(m);Granite ed afterBosellinietal.1996). 26-05-2004, 15:21:41 P44_R_OK 7 with encrustingandproblematicaorganisms platforms, richindasycladaceanalgae, associated (Contrìn Fm)developed (Figure1.6a). These areas, whereshallow water carbonateplatforms brought backmarineenvironments tothewestern During alater Anisian phase,renewed transgression Carnian infi of theDolomites(Figure1.6a-e),uptoeventual basinal conditionsthendominatedtheeasternportion Bivera and Ambata Fms),developed. Longlasting recorded byterrigenous-carbonatesuccessions(Dont, sea-level risingtrend,andbasinalenvironments, systems eventually drowned, becauseofageneral of theDolomites.Intheseorientalareas,platform therefore mainlyrecordedonlyintheeasternportion (Bosellini, 1968,Day3). The two oldergenerationsare erosion phase,locallyreachingdown thePermian areas experienced asignifi active throughouttheeasternDolomites,western the middle-upper Anisian, whilesubsidencewas associated withcontinentalconglomerates.During sequences, punctuatedbyemersionunconformities, framework andbelongingtodifferent depositional Fm, grown withinanincreasinglyactive tectonic Monte RiteFm,UpperSerlaDolomiteandContrìn three generationsofcarbonateplatforms,known as grading intoevaporitic environments, gave way to tidal fl In theearlyMiddle Triassic, afi Anisian platforms by evaporitic mineraloccurrence. generally recordaridclimaticcondition,aswitnessed record differential subsidence. The Lower Triassic subsidence, but their uppermostportionstartsto period ofspatiallyuniform,comparatively moderate These ratherlaterallyuniformsuccessionswitnessa chronostratigraphic schemeattheendofvolume). subdivided intoseveral depositionalsequences(cf. emersion episodesenablethesesuccessionstobe an average thicknessof300-400m.Repeated marine carbonateandterrigenousdeposits,showing a complex storm-dominatedsuccessionofshallow- region. The Lower Triassic (Werfen Fm)consistsof providing themajortectonicdetachmentlevel ofthe evaporites andcarbonates(BellerophonFm), then triggeredtheaccumulationofshallow marine Neri, 1997). Transgression fromthePalaeothethys di Val Gardena–GroednerSandstein, Massari& started withLatePermianfl sedimentary accumulationthroughouttheDolomites at unit(Lower SerlaDolomite),laterally lling oftheaccommodation space. cant upliftingandsubaerial uvial redbeds(Arenarie TRIASSIC CARBONATEPLATFORMSOFTHEDOLOMITES rt widespread rst PRODUCTION, RELATIVESEALEVELFLUCTUATIONSANDTHE SHAPING OFTHEDEPOSITIONALARCHITECTURE ( comparatively moisterconditions. plant associations,dominatedby Volzia fl platform areas.Duringthe Anisian, sporomorphand (Moena Fm),conqueringformershallow water then dis-anoxicintraplatformbasinsdeveloped terrigenous-carbonate deposits(MorbiàcFm),but Through thisprogradation,theisolatedpinnacles early Ladinianinterval (cf. FigureRosengarten). phase began, spanningover acomparatively short down considerablyandamassive progradation During theearlyLadinian,subsidenceslowed somewhat thicker thantheirwestern counterparts. the basinalandplatformsuccessionsareindeed the subsidencespeed.IneasternDolomites,both did exist, beinglargely controlledbydifferences in Bubnoffs (m/Myr),but signifi - earlyLadinianbuildups was intheorderof200-400 cf. Day2). The aggradationrateoftheselate Anisian basins (Knollenkalke MboftheLivinallongo Fm, cherty limestoneswereaccumulatedintheadjacent of 800-900m,whilejustafew tensofmetres These platformsrapidlyreachedanaverage thickness Catinaccio, MarmoladaPlatform,Days1,2,6). catch uptherelative sealevel rise(e.g.Latemar, composition) wereonthecontraryabletosurvive and Dolomite orMarmoladaLimestone,accordingtotheir western buildups (referredtoasSciliar-Schlern condensed ammonoid-bearinglimestones. The (Cernera Platform,Day4)andwas covered by in theeasternmoresubsidingportionofregion was terminatedbyanearlydrowning, especially sediments. The upward growth ofseveral buildups still richindasycladaceanand with theformerandwiderContrìnplatforms,being pinnacles initiallysharedmany facies similarities created alarge accommodation space. The aggrading evolution, forcedbyfast regional subsidence,which which weresoontoexperience arapidaggradational environments survived onlyatsmallisolatedhighs, source rocks.Shallow water carbonate-producing source-rock horizon,coeval toactualsubsurface This organic richlevel oftenrepresentsapotential visited duringtheseconddayofexcursion (Seceda). (Livinallongo Fm=BuchensteinerSchichtenp.p.), the baseofdeepeningupbasinalsuccessions system, whileorganic richanoxicsedimentsmarked A regional drowning terminatedtheContrìncarbonate (late Anisian –earlyLadinian Pre-volcanic carbonateplatforms Tubiphytes ), widelyprogradedover basin cant lateralvariations Tubiphytes orae, record ) micritic 7 -

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Volume n° 5 - from P37 to P54 P44 - P44 Leader: M.Stefani (e.g. Marmolada,Day6)andbythedevelopment cementation ofthemargin andupperslopelimestones phase was characterizedbypervasive phreaticmarine pseudo-downlap relationship. The progradational sharp andsub-horizontalingeometry, simulatinga between baseofslopeandbasinalunitsisnormally the basinalaccumulationrates,contactsurface m/Ma. Sincetheprogradationratelargely exceeded of slopewas probablybetween1,400and2,700 Dolomites, theaverage migrationrateofthebase expanded into5-10kmwideplatforms.Inthewestern redefi are stillpoorlydefi Manfrin, 1995.Manyofthesebiostratigraphicunits,aswell asthechronostratigraphic-geochronological subdivisions Figure 1.5- A comparisonofvariousmodernammonoidbiozonationschemes for theTriassic, accordingtoMiettoand ned inthenearfuture.(1-6:candidateboundaries). ned andsomewhatcontroversial innature,especiallyatthesubstagelevel, andwillbeprobably generated bytheerosionofametamorphicbasement accumulation ofturbiditicsands(ArenariediZoppè), whereas theeasternDolomitesweresiteofmassive correlations (Brack&Rieber1993,cf.Day2), Southern Alps, providing large scalephysical layers (“Pietra Verde”) weredepositedintheentire During thesametimeinterval, acidic volcanogenic base ofslopemigrationwas considerablysmaller. where subsidencewas stillquiteactive, therateof (Figure 2.2,Day1).InthenortheasternDolomites, of very steep(upto30-40°),planarbrecciaslopes 26-05-2004, 15:21:46 P44_R_OK 9 by record thecolonizationofmargin environments Schlern Dolomit). The earlypost-volcanic platforms Dolomite, sometimesreferredtoalsoasOberer post volcanic carbonateplatforms(socalledCassian the widespreadprogradationofseveral generationsof healthier carbonateproductiondeveloped, supporting At thefading outofthemagmaticactivity, aneven (late Ladinian-earlyCarnian) Post-volcanic platforms volcanic successionlocallydiffi break makes thedistinctionbetweenpre-andpost- to keep onatany timeandthelackofany depositional eastern Dolomites)thecarbonateproductionwas able Schlern). Inareasfar away fromthevolcanoes (e.g. even closetothemajormagmaticcentres(e.g.Sciliar/ carbonate productionwas stillactive atany time, and thermometamorphism.However somekindof products andpartiallyinvolved intocaldericcollapses were buried beneath thevolcanic andvolcanoclastic placed incloseproximitytothevolcanic centres, Lucano). A few platformsofthewesternDolomites, onlapping theirslopes(Figure5.4B,Day4,Pale diSan “freezing” theformerplatformmorphologyby hyaloclastites) partiallyinfi adjacent basins. The volcanic products(pillow lavas, (Caotico Eterogeneo Auct.) accumulatedintothe while hugeheterogeneousmegabreccia bodies dykes andcarved bylarge collapsingepisodes, were cutbyagreatnumberofshoshoniticbasaltic middle Ladiniantectono-magmaticevent; they The carbonateplatformswereinvolved intothe The volcanic event phase, withintheDolomitesthemselves. which was soontodevelop animportantmagmatic volcanic deposits witness anactive tectonicscenario, outcropping insouthernareas. The terrigenousand base-of-slope migration,visibleinareasfacing major evolution ofthebasinsandoftenforcedaclimbing huge volcanoclastic input,inducedashallowing high basinalsedimentationrates,supportedbythe subsidence was stillongoingandconsiderable. The fast subsidencephase;intheeasternDolomites space was mainlyinheritedfromthepre-volcanic In thewesternDolomites,available accommodation Fm), afterbeinglackingsincetheEarly Triassic. the earliestphasesofvolcanic activity (Acquatona producing organisms. Ooidgrainsreappearedduring however always subordinated tosmallersediment- Thecosmilia -like branchingcorals,whichwere lled thedepressions, cult. TRIASSIC CARBONATEPLATFORMSOFTHEDOLOMITES PRODUCTION, RELATIVESEALEVELFLUCTUATIONSANDTHE SHAPING OFTHEDEPOSITIONALARCHITECTURE patch reefs,forthefi these platformswas matchedwiththeappearanceof di Vallandro/Dürrenstein). The very lateevolution of Platforms (e.g.LastoidiFormìn, Day3,andPicco the slopeangles,asvisibleinlatestCassian elevation; thesefactors combinedtogethertoreduce the shallowing ofthebasinreducedplatform increased, whilesomeclaywas stillavailable and carbonate mudfedontototheprogradingslopes During theearlyCarnian,amountofloose carbonate platforms The Carnian crisisoftherimmed some oftheoldestknown amber. phases, anditisalsonoteworthy foritsharbouring fl 3). These complex interval witnessimportantclimatic available accommodationspace(cf.SellaMassif, Day poorly recorded,mainlybecauseofthelack western Dolomites,thisCarnianinterval ishowever (e.g. HeiligkreutzFm/DürrensteinFm,Day5).Inthe vertically gradedintomixed andterrigenous systems carbonate sub-toperi-tidalsuccessionslaterallyand a complex palaeoenvironmental evolution. Purely Heiligkreutz Fm/DürrensteinFm,whichrecords triggered thedepositionoflow gradient even inthedeeperdepocentreareas. This evolution drop, startinganinsituactive carbonateproduction, zone, probablyalsobecauseofarelative sea-level The basineventually shallowed upintothephotic carbonate platforms. corresponds toaworldwide crisisoftherimmed buildup systemsdisappeared. This evolution probably corals (AlpediSpecie,Russoetal.,1991),whiletrue carbonate slopes. and withtheonlapofbasinalbedsontoformer progradation, matchedwitharenewed transgression Auct.) areseparatedbyatemporarystillstandofthe two platformgenerations(CassianDolomiteIandII Plateau Beds”).Inthecentral-easternDolomites, and associatedwithsometerrigenousinfl whereas inthewesternDolomitesthey werethinner Dolomites (e.g.Piccodi Vallandro-Dürrenstein), successions arerelatively thickinthesubsidingeastern Early post-volcanic aggradingplatform-top argillaceous content. being richerinmicriteandcharacterizedbysome and generallylesssteepthanthepre-volcanic ones, Clinostratifi sediment sources(e.g.westernSellaMassif,Day3). uctuations, marked bythedevelopment ofmoist cations werenow oftenconcave inshape rst timerichin“modern”colonial ux (“Schlern 9 -

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Volume n° 5 - from P37 to P54 P44 - P44 Leader: M.Stefani the uppermostCretaceous. remained underpelagicconditionuptoatleastuntil region experienced ageneralized drowning, andthen During theJurassicpassive margin evolution, the exceed 4,000minthickness. Lombardy) areastheNorian-Rhaetianinterval can 1,000 mDay5);inothersouthern-alpine(central (about 250m,Day3)and Tofane successions(about of the Val Badia,whilecomparingthevisitedSella striking thicknessvariation willshow upatthesides continental margin of Adria. Within theDolomites,a heralding theriftingstageofJurassicpassive the evolution ofthisUpper Triassic platform, of theDolomites.Differential subsidencecontrolled and Carnia),south(Bellunese)west(Lombardia) wide DolomiaPrincipaleplatform,totheeast(Friuli organic matter, developed indifferent areas of the intraplatform depressions,richincarbonatemudand and Hardie,1988).DuringtheNorian,dis-anoxic rapidly aggradingperitidalsuccessions(Bosellini bioturbated subtidalfacies, gradingupward into Principale =Hauptdolomit),normallystartedwith western Dolomites,thiscarbonatesystem(Dolomia through wideSouthern-Alpineareas.Inthecentral- following phase,alarge carbonateplatformdeveloped Day 5),witnessingasharpreturntoaridity. Duringthe environments developed (RaiblFm/Travenanzes Fm, shallow-water terrigenous,evaporite andcarbonate During themiddle-lateCarnian,avariety of a regional peritidalsuccession Upper Triassicplatform: carbonate relative sea-level drop;18:whileemergingmainlanddevelopment. f)CarnianTime. A complexsystemofshallow water emerged carbonateareas,24:tidalfl new generationofplatforms (CassianD.,15,16)startedtorapidlyprogradeover theshallowing volcanoclastic basins anoxic depressions(MoenaFm,2)andfl Ladinian. At theclimaxofmagmaticactivity, alargevolcano develloped inthePredazzoarea,eventually evolving (Cassian Dm,19)hadconqueredthemajorityofarea,leavingafew shallowed terrigenous-carbonatedepressions thick, immediatelypredatingthevolcanism onset;5:innerplatform, 6:basinalareas,7:drowned platform. c)Middle (La Valle/Wengen Fm,17);14:whileemergingmainlanddevelopment. e)EarlyCarnian.Theexpandingplatforms Figure 1.6-Schematic, nonpalinspasticsketches ofthepalaeogeographic elementsdistribution duringMiddleand carbonate andterrigenousenvironments developed acrosstheeasternDolomites (Heiligkreuz-DürrensteinFm,23: (upper S.CassianoFm:20:coarseterrigenousfacies,21).Thisdepositional systemwas eventually terminatedbya Upper Triassic timesintheDolomitesregion. Alpine deformation hasstructurallytelescopedtheregion(cf. Figure up oftheaccommodationspace.a)Late Anisian. Low reliefcarbonate platforms (ContrìnFm,1),interspacedwith area sawthedevelopment ofseveral generationsofisolatedcarbonateplatforms, untiltheeventual Carnianfi materials fi 1.3) producingasignifi volcanoclastic basinalareas,13:inferred extension ofthePredazzocaldera.d)LateLadinian.Thevolcanogenic Fm, 3).b)EarlyLadinian.Themaximumprogradationphaseofplatforms (Sciliar/Schlern Fm,4),about800m were killedandburied byvolcanic andvolcanoclastic, whereasothercarbonatesystemssurvived inmoredistal areas; 8:stressedcarbonateplatfoms; 9:mainvolcanic area,10:buried platforms, 11:drowned platform, 12: carbonate andsiliciclasticareas,27:basins.a:overthrusts, b:clinostratifi lled uptheinter-platform basinsinthesouth-western Dolomites. At thefadingoutofvolcanisms, a cant shortening,particularlysowithinthebasinalunits.Thedepositionalevolution ofthe anked bythewider, terrigenousinfl at, 25:restrictedcirculationlagoon,26:coastalalluvialplainandmixed the carbonateproductivity was solarge tobeable skeletal faunae, nearthe Anisian-Ladinian boundary & Schlager, 1999).Despitetheminorroleof Brandner etal.,1991;Russo1997;1998;Keim and abundance (Biddle,1981;Fois &Gaetani,1981; characterised byamuchgreatertaxonomicdiversity reduced lithogeniticrole,even ifthey werenow Day 6),whereastheskeletal organisms playeda induced syndepositionalcements(e.g.Marmolada, were stilldominatedbymicrobialitesand/ororganic- Cernera, Day4). The Ladinianbuildup biofacies Crinoidal calcareniteswerelocallyabundant (e.g. Gaetani, 1984;Senowbari-Daryan etal.,1993). ecc.) andbriozoans.(Gaetanietal.,1981;Fois & sphinctozoans ( biota, asmicrobialcommunities(microbialites), framework, beingdominatedbybinderandbuffl a limitedreliefandlacked any wave-resistant organic Fms). These buildups weregenerallycharacterisedby the Anisian Time (MtRite,UpperSerlaandContrìn 1.7). The oldercarbonateplatformsoccurredduring ranging from Anisian toNorian-Rhaetianinage(Fig includes many carbonateplatformgenerations, previously discussed,the Triassic oftheDolomites disappeared fora7-10Myrinterval (Flügel2002). As Triassic boundary, “reef”communitiesvirtually Following thebiologicalcrisismarkingPermian- F. Russo, A. Mastandrea. M.Stefani&C.Neri the dolomites organisms inthetriassicplatforms of Evolution offrame-building into acalderadepression.Thesurroundingplatforms uenced easternDolomitesbasin(Ambata Olangocoelia cation, c:tetrapodsfootprints.

otti , Celiphia

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Volume n° 5 - from P37 to P54 P44 - P44 Leader: M.Stefani complex scheme, seetheguide-booktext.Modifi Figure 1.7- A synthesisoftheTriassic carbonateplatform stratigraphyoftheDolomites.For furtherexplanationofthis ed fromBosellinietal.(2003b);agesGradstein(1995). 18-06-2004, 14:41:29 P44_R_OK 13 Bridge, 1995),withproductive margins mainly buildups aslarge mudmounds( These microfacies suggesttoview the Cassian locally comparatively abundant. but calcifi contribution ofmetazoansissharplysubordinated, like (Figure 1.12a)aswellbymicroproblematica, cyanobacteria, like Platforms. The faunae aredominatedbyskeletal than the10%ofentirerockvolume oftheCassian Fossilised skeletal organisms normallyrepresentless calcite, fi botryoidal aragonite),andsecondaryblocky ferroan were recognised(isopachoushighmagnesiumcalcite, the microfacies (25-30%ofprimarymarinecements quantitatively representthesecondcomponentof minor constituentofthesefacies. The cements The detritalmicrites(allomicrites)arebyfar the of automicrite(morethan50%). Cassian Platforms,thedominantcomponentconsists and allomicritecomponentstobeproposed.Inthe distinction betweentheautomicrite(microbialite) Micromorphological andfabric featuresallow afi texture (Figure1.8-10)(Russoetal.,1998a ;1998b). stromatolitic microfabric, withanaphaniticorpeloidal The micritesmayshow disorganized, thromboliticor main components:micrites,cementsandskeletons. and subordinatedbaffl platform microfacies manlyconsistofbindstones & Schlager, 2001,cf.Day3). The post-volcanic dolomitised platforms,suchasintheSella(Keim preserved facies arelocallyfoundalsowithin 1994; Mastandreaetal.,1997).Somelesswell Archelaus tothe Austriacum p.p.Zones,Mastandrea, the UpperLadiniantoLower Carnian(fromthe Valle/Wengen Formations, theiragespanningfrom or megabreccia lenseswithintheS.CassianandLa The “Cipit”facies arepreserved asisolatedblocks comparatively pristinestate(Russoetal.,1991). circulating, thuspreservingtheblockfacies ina which prevented thedolomitisingfl into low-permeability argillaceous basinalunits, Boulders”, platform-derived olistolithsresedimented be studiedindetailonlyonthesocalled“Cipit and microfacies ofthesecarbonatebuildups can Dm, e.g.Sella,Day3). The originalfabric, texture post-volcanic platforms weredeveloped (Cassian During theLateLadinianandCarnianp.p., hundred ofmetresthick(Sciliar/SchlernFm). the growth ofimpressive carbonatebuildups, many to take pacewiththestrongsubsidence,supporting Tubyphites lling uptheresidualcavity space. ed demospongesareoftenvisibleand (Figure 1.12b). The lithogenetic estones, dominatedbythree Cladogirvanella cipitensis TRIASSIC CARBONATEPLATFORMSOFTHEDOLOMITES sensu PRODUCTION, RELATIVESEALEVELFLUCTUATIONSANDTHE Bosence& ud from uid rst SHAPING OFTHEDEPOSITIONALARCHITECTURE Towards the topofJulianSubstage(Carnian),at ones (e.g.Marmolada,Day6). sharply dominatingrolerecordedinthepre-volcanic volcanic platformsthey werefar fromplaying the syndepositional lithifi cements provide evidence ofawidespreadearly amount ofskeletal remains. The primarymarine made upbymicrobialites,withsubordinate Figure 1.9-Stromatoliticpeloidalmicrobialite. Figure 1.10-Thromboliticmicrobialite. Figure 1.8-Stromatoliticmicrobialite. cation, but inthesyn-post- Punta Grohmann.X7.5. Punta Grohmann.X6. Passo Gardena.X30. 13 -

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Volume n° 5 - from P37 to P54 P44 - P44 Leader: M.Stefani volcanites oftheSouthern Alps. Iftheafternoon the thickMesozoiccarbonateplatformsandPermian fl terrigenous depositsoftheNorthern Apennines, the will provide uswithafast overlook onthe Tertiary from FlorencetotheDolomites. This transfertrip Most ofthefi p. brack,f. maurer andm.stefani general introduction totheregional geology Transfer tripfrom Florence totheDolomitesand scleractinian corals. the acquisitionofsymbionticassociationin a biologicalradiationandmostlikely relatedto between theLateCarnianandNorian-Rhaetian, reef-building communities,occuringataglobalscale These biofacies anticipatethe“modernization”of subordinated tosponges,inthesefaunal associations. the 50%ofrockvolume. Coralswerehowever still increases greatlyandtheskeletal componentexceeds and scleractinians(Figure1.12e). Taxonomic diversity sphinctozoans, chaetetids,inozoans)(Fig1.12c,d,f) by calcifi building organism framework developed, dominated 1991). For thefi and texture (MastandreaandRusso,1995;Russoetal., both skeletal microstructureandcementsmineralogy marly matrix,allowing theperfectpreservation of in limestonesbodiesembeddedwithinimpermeable “modern” faunal association,very wellpreserved (i.e. Alpe diSpecie)patch-reefsshow muchmore the baseofHeiligkreutz/DürresteinFormation facies, Valle delFontanel). margin faciesfromtheLatemarpaltform (lower cyclic Figure 1.11-Bioconstructedandstronglycemented at QuaternarylandscapeofthePoPlainBasin,and ed demosponges(stromatoporoids, rst daywillbespentthroughabus drive rst timeinthe Triassic, areal primary DAY 1 area. of Permianacidicvolcanites, dominatingtheBozen Plateau, throughawindingroadonthicksuccession the motorway, wewillrapidlyreachthe Ritten/Renòn basins, inanappropriateafternoonlight.Leaving scale geometryof Triassic carbonateplatformsand stops willoffer aspectacularview ofthelarge- and Triassic successionsoftheDolomites. These be thenmadetogetanoverview ofthePermian weather conditionsareappropriate,two stopswill proximity thanthepalaeogeographicone. brought theplatformstoamuchgreatermutual However, the Alpine tectonictelescopingofthearea basin, oftencorrespondingtothepresent-dayvalleys. Middle Triassic platform,grew betweendeepwater each present-daymassifcorrespondingtoanisolated region fromdeveloping elongatedmountainridges, architecture ofthe Western Dolomitesprevented the platform andbasinsize. The peculiarstratigraphic Catinaccio, Latemar)give quitegoodanideaofthe platforms (Geisler/Odle,Schlern/Sciliar, Rosengarten/ mountain-scale outcropsofMiddle Triassic carbonate and structuralframework ofthearea.Spectacular The landscapemorphologyreveals thestratigraphic Dolomites, from20kmtothewest(Figure2.1). This stopoffers anoutstandingview ofthewestern introduction Gasthof Himmelreich, Ritten/Renòn:general Stop 1.1: steepening upward clinoforms,andtheequivalent Laurino, whereitischaracterisedbycontinuously foreslope isexposed at Laurinswand/Torri diRe nucleus, atthe Vajolet towers. The corresponding of theplatformispreserved inasmallplatform ammonoid zones(Figure2.2). The aggradingportion Km andwithinatimeframework encompassing 4 (Buchenstein/Livinallongo Fm)over adistanceof5 the interfi and progradationalhistoryoftheplatform The Rosengartensectionrecordstheaggradational of carbonateplatformsandwillbediscussedindetail. range, isatextbook caseforprogradationgeometries portion, outcroppingintheRosengarten/Catinaccio platform evolution (Schlern/SciliarFm).Itssouthern Dolomites isawellpreserved example ofaprevolcanic The Schlern/RosengartenPlatforminthewestern Schlern/Rosengarten Platform Unterinn, Ritten/Renon:geometryofthe Stop 1.2: ngering ofslopeandbasinalsediments 26-05-2004, 15:19:05 P44_R_OK 15 at thebaseofHeiligkreuz(c-f).a-Cladogirvanellacipitensisbaffl d- Coralsolenoporaceanboundstone.Polished section, Alpe diSpecie.X0.8;f-Detailof Atrochaetetes mediuswiththe Figure 1.12- Well preserved bioconstructorfaciesfrompost-volcanic Cassianplatform (a,b)andCarnianpatch reefs b- Peloidal boundstonewithTubiphytes. Passo Gardena.X2.8;c-Colony ofPeronidella loretzi. Alpe diSpecie.X1.2; TRIASSIC CARBONATEPLATFORMSOFTHEDOLOMITES PRODUCTION, RELATIVESEALEVELFLUCTUATIONSANDTHE SHAPING OFTHEDEPOSITIONALARCHITECTURE skeleton preserved stillin aragonite. Alpe diSpecie.X2. estone. Polished section,PuntaGrohmann.X0.7; 15 -

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Volume n° 5 - from P37 to P54 P44 - P44 Leader: M.Stefani the Latemarplatform-topsuccession(Figure1.2).In the highfrequency sedimentarycyclicity recordedin attention was focusedthroughthelast20yearson As discussedintheintroduction,considerable period oftheprevolcanic platforms. records, withoutstandingaccuracy, thewholegrowth the magmatism,toppingabasinalsuccession,which reached thevisitedareabeforeeventual onsetof needle inLadin). The baseofsloperesedimentedbelt forming theOdleelongatedpicks(“odla”meaning as recordedbytheclinostratifi phase, theplatformexpanded throughprogradation, sub-vertical wall. After anearlyprogradational NE ofthevisitedarea,inSasRigais northern eroded aggradingplatformnucleusisvisibleatthe the Geisler/OdlePlatform. A smallremnantofthe a growing proximitytotheprogradingslopeof The discussedbasinalsuccessionaccumulatedinto sedimentary dynamics. magmas andtheirrelationshipwiththecoeval timing andemplacement/extrusion modeofLadinian discussed. The trip will alsobriefl on acoredrilledinthebasinalsuccessionwillbe results ofaninternational-interdisciplinaryresearch Buchenstein Fmandofthetoe-of-slopebrecciae, will beobserved. After acloseexamination ofthe basinal sediments(Buchenstein/Livinallongo Fm) Platform (Schlern/SciliarFm)andthecorresponding Seceda Massif,wheretheprevolcanic Geisler Dolomites, wherewewillstayovernight. Groeden Tal-Val Gardaina-Val Gardena,western The daytripwillendwithabus transfertothenearby directly overlain byLadinianvolcanics. Schlern massif,wherethe900mthickplatformis the Rosengarten,but ispreserved atthenorthin 2.2, sections5-10). The platformtopiserodedat because ofthefast baseofslopemigration(Figure thickness but barely intheirstratigraphicrange, SE, andbybasinalsedimentsthatincreasesin by 30-35°steepclinostratifi progradational phaseoftheplatformischaracterised the stratigraphicrange(Figure2.2,sections1-4). The basinal sedimentsshow amarked lateralincreasein The seconddaywillbespentinthefi Introduction P. Brack, F. MaurerandM.Stefani sediments atSeceda Prevolcanic platform andbasin DAY 2 cations, dippingtowards ed slopedeposits y xmn the examine y ed n the on eld of the Triassic. thus directlyaffecting thechronologicalframework Stage andaretiedtothestandardammonoidzones, because thedataarefromtypeareaofLadinian Hinnov, 1997). The debatecarriesaddedweight Triassic stratigraphy(Bracketal.,1996;Hardie& obvious andledtodifferent interpretationsofMiddle- of theLatemarsuccessionbecameimmediately Triassic timescalesandwiththeorbitalinterpretation this detailedframework, thediscrepancy withcurrent 1996) andmagnetostratigraphicdatawereaddedto from zirconsinvolcanoclastic layers(Mundiletal., plattform-basin correlation. When isotopicageresults Brack &Rieber, 1993),toeventually establisha stratigraphic pointsofview (Cros&Houel,1983; were studiedfromsedimentologic,petrographicand the meanwhile,coeval basinalBuchensteinbeds pelagic pelecypods such as signifi area, thisformationhassofar yieldedthemost hanging over avertical ContrinFmcliff). Inthis to bepaywhilevisitingthedangerousoutcrops, in asteepeastcliff oftheSecedapeak (cautionhas A fullsectionofBuchensteinFormation isexposed (Maurer &Schlager, 2003). erosion byturbiditycurrentsorcontour 30 -40kmandthereisnoevidence forsignifi Beds oftheDolomiteshave beenindeedtracedover (Brack &Muttoni,2000).LayersintheBuchenstein sets ofpelagicstratacanbetracedover longdistances laterally uniform(e.g.Brack&Rieber, 1993),since Buchenstein successionsarehowever remarkably At somedistancefromthecoeval platforms,the platforms areabundant, suchasinthevisitedarea. successions, reworked debrisfromadjacentcarbonate levels. IntheupperportionofcompleteBuchenstein detritus andashfalls, providing key correlationdatum from surroundingcarbonateplatforms;(c)volcanic carbonate detritusandfi also calcareoustestsofmicro-organisms; (b) consisting oforganic matter, siliceousandpossibly three ofthembeingactive: (a)plankticmaterial, interference ofmultiplesedimentssources,atleast The Buchensteinbedsweremadecomplex bythe the Dolomites(Figure3.1)andinadjacentareas. Fm; Viel, 1979)arefoundinawideareathroughout Successions ofbasinalBuchensteinFm(Livinallongo the drillsite general outlineandgeologyaround The Buchenstein/Livinallongo Fm: cant succession ofmacrofossils(ammonoids, ne grainedmud,exported Daonella ) ofuppermost 26-05-2004, 15:19:11 cant

P44_R_OK 17 Figure 2.1 - Outline of the geology of the Western Dolomites as seen from stop 1. stop from seen as Dolomites Western the of geology the of Outline - 2.1 Figure TRIASSIC CARBONATEPLATFORMSOFTHEDOLOMITES PRODUCTION, RELATIVESEALEVELFLUCTUATIONSANDTHE SHAPING OFTHEDEPOSITIONALARCHITECTURE 17 -

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Figure 2.2 - Correlation of platform slope (Schlern/Sciliar Fm) and basinal deposits (Buchenstein/Livinallongo Fm) at the Rosengarten. At the southern end of the ridge the basinal sediments are preserved in their whole stratigraphic range; moving in a northward direction they are progressively replaced by time-equivalent foreslope clino- forms. The slope sediments at Laurinswand (Reitzi- to Curionii zones) correspond to the aggradation phase of the platform, while southerner slope deposits were formed during progradation (Gredleri and Archelaus 26-05-2004, 15:19:16 zones). The sections 1-10 can be correlated by different basinal lithologies and tuffi tic intervals (Pietra Verde layers). The radiometric dating (in Myr; from Mundil et al. 1996) and the biostratigraphic range of the Buchenstein Fm are listed at the right of the sections. Slightly modifi ed from Maurer (2000). P44_R_OK 19 also performedintheuncasedwell,providing further with onlyminorlosses.Geophysicalwellloggingwas such asmarlsandcertainashlayers,wererecovered better than95%andeven themostfriablelithologies, succession ispreserved there. Average recovery was of metresandonlythelower halfoftheBuchenstein the westofthis Alpine fault iselevated byafew tens between SecedaPeakandPana Scharte. The areato Geisler PlatformslopeandaN-Srunningfault, section, inanarrow areabetweenthetoeof chosen asclosepossibletothereferenceoutcrop The locationofthedrillsite(Figs.3.1B,3.3)was The cored stratigraphic succession Mastlé. outcropping geometricrelationshipsvisiblenear through thissubvolcanic body, assuggestedbythe nearby basalticextrusive rockswereprobablyfed a laccolithisvisibleintheBuchensteinBeds. The the ridgesouthofcablecarstationatSeceda, in theslopesaroundSeiser Alm/Alpe diSiusi. Along to thesouthofColRaiser(2kmSESeceda)and volcanic andvolcanoclastic rockswhichispreserved Seceda belongtothelowermost partofathickpile platform growth. These lavas andsedimentlayersat to theSEofPana Scharte,recordingasynvolcanic with baseofslopecarbonatestheSchlernDolomite Formation. These basinalsiliciclasticsinterfi basalts andsiliciclasticbasinal Wengen/La Valle Cucca, thesuccessionisoverlain byLadinianpillow whereas tothesouthwest,nearKuka Sattel/Sella by thecoeval slopedepositsoftheGeislerPlatform, the east,Buchensteinbedsaregraduallyreplaced Anisian toLadinianagefoundintheDolomites. To TRIASSIC CARBONATEPLATFORMSOFTHEDOLOMITES PRODUCTION, RELATIVESEALEVELFLUCTUATIONSANDTHE nger SHAPING OFTHEDEPOSITIONALARCHITECTURE 30% intheunitC(Baenderkalke). Inthebreccia (Knollenkalke, unitD),andfurtherincreasetoover E), but they becomefrequentinthemiddlepart of theBuchensteinsuccession(Plattenkalke, unit surrounding platformsarequitescarceatthebase of calcarenitesandcalcareousrubbleshedbythe laminated intervals isclearlyvisible. The layers The alternationofbioturbatedandanoxic layers. beds, breccialayers,andthe Tc and Td andothertuff centimeter thickbeds,suchaspelagiclimestone of correspondence,even atthelevel ofindividual between thecoreandoutcropshows ahighdegree part oftheContrìnFormation. The comparison Plattenkalke” respectively. Interval Fisthetopmost “Baenderkalke”, the“Knollenkalke” andthe“Lower members oftheBuchensteinFormation, i.e.the derived carbonatebrecciae;intervals C–E,typical characterised byabundant coarse-grained,platform- unit atthebaseof Wengen Beds;interval B, distinguished: Interval A, representingatransitional From toptobottom,thefollowing mainunitswere penetrated around88mofstratigraphicthickness. Bolzano NaturalHistoryMuseum. The borehole and ispresentlystoredforreferenceattheBozen/ geochemical andmagnetostratigraphicpointsofview sedimentological, palaeontological,mineralogical, The corematerialwas carefullyexamined from for actualhydrocarbonexploration andexploitation. data forsubsurface correlation,particularlyuseful B: Geologicalsketch mapof Anisian toCarnianunitsin distribution intheDolomitesduringLadinian. Figure 3.1- A: Carbonateplatforms andbasins the Val Gardenaarea. 19 -

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Volume n° 5 - from P37 to P54 P44 - P44 Leader: M.Stefani breccia layersobserved inthecore,whencompared derived carbonateclasts. The amountofcoarse the occurrenceofthickbreccialayers,withplatform Platform. The uppercoreinterval ischaracterised by subsequent progradationofthenearbyGeisler/Odle distributionrefl 2003). This over 60%ofthesedimentvolume (Maureretal., interval (unitB),platformderived debrismake up (after Brack etal.2000). Figure 3.2-GeologicalmapoftheSecedaarea ects theupbuilding and pichleri basalts, immediatelyabove ahorizonswith the outcropsection.Itpostdateslevel ofpillow II). This importantmarker bediseasilyrecognisedin of basinallimestones,aswellbasalticvolcanics (MB 30.3 -31.45metreinterval ofthecore, containsclasts A conspicuousanduniquepolygenicbreccia,inthe Platform slope. of thedrillsitewithrespecttotoeGeisler with theoutcropsection,suggestsacloservicinity and Daonella tyrolensis , pelagicpelecypods Daonella 26-05-2004, 15:19:23 P44_R_OK 21 Figure 3.3- Aerial viewof the Secedaarea(afterBrack etal.2000).Thelocationofthewell siteandoftheexcursion TRIASSIC CARBONATEPLATFORMSOFTHEDOLOMITES PRODUCTION, RELATIVESEALEVELFLUCTUATIONSANDTHE stops areindicated.ThearrivalofSecedacablecarisclosetoSite A. SHAPING OFTHEDEPOSITIONALARCHITECTURE 21 -

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Volume n° 5 - from P37 to P54 P44 - P44 Leader: M.Stefani ages afterMundiletal.(1996).(Slightlymodifi Figure 3.4-Correlationofcoreandoutcropreference sectionandcorrespondingmagneto-stratigraphicdata.Radiometric ed afterMuttonietal.,subm.). 26-05-2004, 15:19:31 P44_R_OK 23 shallow-marine nodularlimestones andmarls(upper sandstones (RichthofenCgl);theMorbiacFormation, unconformity, covered byredconglomeratesand clastics andcarbonates;theupper Anisian erosional Triassic), consistingofshallow marinereddishtogrey detachment levels; the Werfen Formation (Lower (Sabkha evaporite cycles), locallysiteoftectonic Permian), withconspicuouswhitegypsumlayers Ridge; theBellerophonFormation (uppermost Bozen Volcanics, visibleinthenearbyRasciesa (upper Permian),depositedontopofthePermian include fl Middle Triassic formationscanbeobserved. These From thecablecar, theUpperPermianandLower- to St.Christina. lunch inthefi trip fromSecedatoColRaiser, with6stopsandpicnic from Urtajai/Ortisei/St.UlrichtoSeceda,awalking The dayitinerarywillinvolve transportbycablecar Excursion stops bearing asignifi Fm slopedeposits. Fm; ontheleftOdle,avisibleconsistingofSchlern Morbiàc, Co:ContrinFm,Lv:Buchenstein/Livinallongo the Seceda. Wf: Werfen Fm,R:Richthofen Cgm,Mb: Figure 3.5-SpectacularPermo-Triassic outcropbeneath Schlern region (e.g. Val Duròn). Wengen Formation, inthisarea,aswellthe stages ofbasalticvolcanism anddepositionofthe carbonate growth continuedatleastduringtheinitial The stratigraphicframework suggeststhatplatform SE, closetotheCislesCreek,southofColRaiser. SW (MastlèandKuka Sattle/SellaCucca),and in thestratigraphicsuccessionsoutcroppingto uvial redbeds,the Val GardenaSandstones eld, cablecardescentfromColRaiser cant biostratigraphicsignifi TRIASSIC CARBONATEPLATFORMSOFTHEDOLOMITES PRODUCTION, RELATIVESEALEVELFLUCTUATIONSANDTHE cance, SHAPING OFTHEDEPOSITIONALARCHITECTURE grassy slopesattheSecedatop. bedded basinalBuchensteinFormation, formingthe and byadrowning surface (Upper Anisian); thethin compact dolomiteinterval, cuppedbyabreccialevel Anisian); theContrinFormation, acliff-forming succession, anoxicblackshaleswillbevisible. laccolith body. Inthelower portionofthebasinal Buchenstein Fm,below intrusive basaltsanda the ContrinFormation, thelowermost 25mofthe This stopwillshow thedrowning topsurface of View from trailnorthofcablecararrival Stop 2.1: verde) ofBuchenstein Fm(‘Lower Plattenkalke’ and fossils andacidicvolcanoclastic layers(pietra basin depositionalrelationships.Sedimentology, a cliff 300mtoeast,anddetails oftheplatform- Formation, Brack &Rieber1993).outcroppingin Anisian-Ladinian basinalsuccession(Buchenstein View ofthefullyexposed referencesectionofthe Small ridgeatthenorthofSecedasummit Stop 2.3: primary palaeogeographicrelationships. has however tobetaken inmindevaluating the associated withtheBullacciaOverthrust (Figure3.1) The tectonictelescopingofthearea,forinstance of postvolcanic platformdeposits(Sella,Plattkofel). Schlern/Rosengarten Platforms)andthedistribution between coeval carbonatebuildups (Geislerand Buchenstein basins(Figure3.1),thedistance of thegeometryanddimensioninterplatform The view fromSecedasummitgives agoodidea Panorama from theSecedasummit. Stop 2.2:

23 -

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Volume n° 5 - from P37 to P54 P44 - P44 Leader: M.Stefani hydrocarbon carrierbodies. and illustratethedepositionalgeometryofpotential slope recordofaplatformprogradationalevolution the GeislerPlatform. The outcropprovides a baseof Buchenstein Fmandtransitiontoslopecarbonateof Examination ofcarbonatebrecciabodiesinupper Surroundings ofPana Scharte Stop 2.5: volcanism. in abasinalsetting,attheonsetofLadinian late historyandendingofthepre-volcanic deposition Wengen Beds. This stopwillprovide aview ofthe Bänderkalke’ andbrecciainterval) andtransitionto Close-up view oftheupperBuchensteinFm(‘Upper Trail toPana Scharte Stop 2.4: hydrocarbon systems. topic foranoutcroppinganalogoussubsurface core-outcrop correlation(Figure3.4),aninteresting ‘Knollenkalke’) willbealsodiscussed,aswellthe photograph. From Maurer(2003). on theright(E-eccentricity, T-tilt,Pprecession).Notethefairlygoodrecognitionofdifferent cyclesinthecore presumed compositeMilankovitch signal(ETP),which isthesumofgreyscalescan’s bandpassedsignalcomponents Figure 3.6-Comparisonbetween acoresectioncleanedofturbidites andcorrespondinggreyscalescanwiththe Surroundings ofMastlé Alm Stop 2.6: arrival andtransportbycablecartoSt.Christina The daytripwillendthroughawalk toColRaiserlift planktic pelecypod. preserved plantremainsand a siliciclasticsuccession(Wengen Fm),withnicely examined. The sedimentarycover ofbasaltsincludes their transitiontosubmarinepillow basaltswillbe subintrusive basaltswithpiroxene crystalsand the depositionalevolution oftheregion. Vesicular will bediscussed,sinceitdramaticallyaffected basinal recordofthevolcanism onsetinthearea Early syndepositionalbasalticmagmatism. The The Buchensteinbasinwas foundtohave been fed sedimentological analysisofthedrilledsuccession. Seceda corestudyandwas approachedinadetailed rhythm was acentraltopicofresearchinthe within theDolomites. The originofthisbedding tracing ofindividual bedsover several kilometers limestones oftheBuchensteinFm.whichallows A distinctbeddingpatternispresentinthenodular F. Maurer Buchenstein Fm Bedding rhythms inthe Daonella lommeli 26-05-2004, 15:19:37

P44_R_OK 25 made upbytheDolomia (Puez Marls,Lower Cretaceous). The upperwall if Rosso, Mid-UpperJurassic)andhemipelagicmarls showing condensedpelagiclimestones (Ammonitico occur onlyatthevery summit oftheMassif(PizBoè), pertains totheUpper Triassic; youngerthindeposits buildup (SellaPlatformproper),thesecondone (Figure 4.2). The lower cliff iscutintoaLadinian forming two steepcliffs, separatedbyadistinctledge made upbytwo superimposedcarbonateplatforms, Sella Massif(Figure4.1). The wholeoftheMassifis postvolcanic carbonateplatform,showing upinthe depositional geometryofanatoll-like, high-relief This dayisaimedatobservingthewellpreserved Introduction L. Keim &C.Neri The SellaPlatform underlying greyscale scan. Eccentricity, Tilt, Precession)fi bandpassed frequency components(ETP, standsfor next toitforcomparison. The compositecurve ofthe restored andthepresumedorbitalsignalsareplotted succession usedfortimeseriesanalysisisvisually the fi at theresidualsedimentanditsbeddingpatterns.In technique isthatonecangobacktothecoreandlook of BuchensteinFm.). The greatadvantage ofthis core interval between59and45m(“Bänderkalke” quasi-periodic signalsinthegreyscale scanofthe sedimentology oftheformation,was usedtodetect kind oftuning,whichisexclusively basedonthe of changesinsedimentationrateisminimised. This construction ofaresidualsuccession,wheretheeffect deposits fromthebackgroundsedimentallows the thickness representstime. The separationofthese because they ruleoutthesimpleapproachthatbed one ofthemajorobstaclesincyclostratigraphy, sediment. Suchchangesinsedimentationratesare rates comparedtotheofperennialbackground and weredepositedatextremely highsedimentation in thicknessandpercentagetheBuchensteinbasin Calciturbidites andvolcaniclastics changesignifi as welltestofmarinemicroorganisms andclay. surrounding carbonateplatforms,volcanic material by different sedimentsources,namelydetritusfrom Principale isoverlain bysometensofmeters here about250mthick. The peritidalDolomia consisting offl gure below a1mlonginterval oftheperennial at lyingregion-wide peritidaldeposits, DAY 3

Principale ts very welltothe TRIASSIC CARBONATEPLATFORMSOFTHEDOLOMITES – Hauptdolomit PRODUCTION, RELATIVESEALEVELFLUCTUATIONSANDTHE cantly SHAPING OFTHEDEPOSITIONALARCHITECTURE beds croppingoutatthetopofSchlern(Sciliar) Sella withtheuppermostpartofSchlernplateau based onthepossiblecorrelationofinterval atthe by Keim &Brandner(2001). This nomenclatureis evaporite, werereferredtoas“Schlernplateaubeds” red andgreenshales,whitishdolomicrites,sulphate which is Tuvalian inageandischaracterized by to theRaiblFormation intheeasternDolomites, The so-called“Raiblbeds”oftheSella,notcorrelatable proposed byMojsisovics (1879). however, thatthename“Cassian Dolomit”was fi at leastsince Assereto etal.(1977);itshouldbenoted, work) andas“CassianDolomite”byItalianauthors, (including Keim &Brandner, 2001,andL.Keim, this Schlern DolomitebyGerman-speakingauthors names: thus,theSellaPlatformisreferredtoasUpper have indicatedthesamerock-unitswithdifferent summarized inFigure4.2.Different researchgroups the rockbodiesmakingupSellaMassifis The intricatelithostratigraphicnomenclatureof lithostratigraphic terminology Remarks on Valle - Wengen Fm,Figs.4.2-5). portion ofthevolcanoclastic basinalsediments(La These brecciasareinterbeddedwithinthetopmost 200 mthick(Bosellini,1982;Bosellini&Neri,1991). megabreccia body, the“GardenaMegabreccia”, upto characterised bytheoccurrenceofaprominent Massif shows apeculiarstratigraphicsuccession, Ladinian timeinterval. The northernsideoftheSella Brandner, 2001),andispresentlyreferredtoalate Neri, 1991,Keim &Schlager, 1999,2001;Keim & Bosellini, 1982,1984,Kenter, 1990,Bosellini& of isolatedplatforms(Leonardi&Rossi,1957, in thestudyoflarge-scale depositionalgeometry This carbonatebodyattractedconsiderableattention with relatively thintopsetbeds(Figure4.3and4.4). mainly ofclinostratifi measuring 7-8kmindiameter. This unitconsists The lower platformwas probablysubroundinshape, zero. this unitdecreasesdistinctlyandislocallyreducedto Towards thecentreofmountain,thickness attributed totheSchlernplateau Formation (L.Keim). out thatthiscorrelationisincorrect,they areherein As several litho-andbiostratigraphicevidences point alternations, traditionallyreferredtoas“RaiblBeds”. consists ofwell-beddeddolomiteandmarlstone ledge inbetweenthe Triassic platformcarbonates Rhaethyan shallow water DachsteinLimestone. The ed slopedeposits,associated rstly 25 -

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Volume n° 5 - from P37 to P54 P44 - P44 Figure 4.1-Schematic geologicalmapoftheSellaGroup,withlocalisationtripstops. Leader: M.Stefani tilting, grabenstructuresandbrecciadeposits. Extensional tectonicsledtolocalfi signifi tectonics (Keim &Brandner, 2001),resultinginthe Fm. was stronglyinfl The sedimentationpatternoftheSchlernplateau bivalve coquinas(Myophoriakefersteini kefersteini). lagoonal mixed terrigenous-carbonatesedimentsand enlarged bykarst;(b)Stevia Mb:itconsistsmainlyof Platform andlocallyinfi unconformably lyingonthetopof“Cassian”Sella a key-layer consistingofvolcanoclastic sandstones, interbedded withmarlstones;itsbaseismarked by (a) PordoiMb:itconsistsofwell-beddeddolomites, interfi Fm. was informallysubdivided intotwo laterally Mountain. IntheSellaMassif,Schlernplateau ngering members(Keim &Brandner, 2001): cant changeinthicknessshown inFigure4.2A. lling openfractures,possibly une b synsedimentary by uenced sue, block- ssures, Stop 6(CampolongoPass). stratigraphic interpretations,thatwillbediscussedat in nomenclaturerefl clearly shows that,alsointhiscase,thedifference A comparisonbetweenFigures4.2Aand4.2C the formerCassianplatformslope(Figure4.2C). body nucleatingfromthebasinfl Bosellini &Neri(1991)asanaggradingcarbonate Massif (CampolongoPass) andinterpretedby (1984), croppingoutoneasternfl so-called “DürrensteinDolomite”sensuBosellini name “Schlernplateau”hastobeextended tothe According toL.Keim (thiswork) theformational several basinalsectionsoutcroppingaroundthe The available biostratigraphicdataderive from Biostratigraphy andage ects two distinclydiffering oor andonlapping ank oftheSella 26-05-2004, 15:19:41 P44_R_OK 27 Upper Ladinianage. The faunae aredominatedby Pass andSellaPass sectionsalsoclearlyindicatean (Mastandrea etal.,1997,1998)attheGardena Conodonts formthe Wengen andS.CassianoFms (in Zapfe,1984). Platform totheUpperLadinian,accordingKrystyn Triassic Stratigraphyislacking,westillrefer theSella since any offi Manfrin, 1995a,b;BroglioLorigaetal.,1999),but, as themarker fortheCarnianStagebase(Mietto& 1983). Recently, thegenusDaxatina was proposed of the canadensis by Mietto&Manfrin(1995b)totheDaxatinacf. “Gardena Megabreccia” (ColdeFrea)was assigned The S.CassianoFmsectionoutcroppingabove the indicate anupperLadinian Age ( Mietto &Manfrin,1995;Baracca,1996)clearly sections aroundtheSellaMassif(Reithofer, 1928; The ammonoidfaunae ofthe Wengen andS.Cassiano overlying theplatformtopat Ciavaces Plateau. Sella Massifandfromthesedimentsimmediately The thickness oftheSellaPlatform isatleast500m. Platform stratigraphy, seemaintextfor discussion. Figure 4.2-Two alternative interpretationoftheSella Regoledanus Subzone (correspondingtoupperpart cial decisionbytheSubcommissionon Zone ofKrystyn,inZapfe, TRIASSIC CARBONATEPLATFORMSOFTHEDOLOMITES Regoledenus PRODUCTION, RELATIVESEALEVELFLUCTUATIONSANDTHE Zone). SHAPING OFTHEDEPOSITIONALARCHITECTURE Krystyn, 1979). Early Carnianinage(AonZone,baseofJulian1 According toUrlichs& Tichy (2000)thistaxonis (Ciavaces plateau,Keim &Brandner, 2001). of thebivalve Fm isinferredonthebasisoffrequentoccurrence Zone (UpperLadinian). The ageoftheSchlernplateau al. (1998),correspondingtothestandard Assemblage ZonesensuKrystyn(1983)andGalletet genus “ structures known as“summit-thrusts” (German: portion ofthemassifiscaracterizedbysomeklippen 1985,1992, Keim &Brandner, 2001). The uppermost nearly N-Strending,high-anglefaults (Doglioni, important overthrusting anddissectedbyseveral, is representedbytheeasternfl side ofSella,see Anticline, thesouthernfl Antonellini, 1999),orgentlefolding(i.e.thePlan recorded bysmalloffset faulting (Mollema& comparatively mildintheSellaMassif,mainly Alpine compressionaldeformationisoften Tectonics Gipfelfaltungen Budurovignathus ”; Italian:“ Myophoria kefersteini kefersteini

Figure 4.5). A marked exception ank ofwhichformtheN- and belongtothe sovrascorrimenti di ank, involved in Regoledanus diebeli 27 -

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Volume n° 5 - from P37 to P54 P44 - P44 Leader: M.Stefani beds islocallyvisible. topset layersshow even tabular bedding,0.1-1m core, however isnotoutcropping. The shallow water reaches amaximumthicknessof600m;theinner Judging bytheheightofclinoforms,platform the basinalsedimentsofS.CassianoFormation. radial progradationandinterfi The steep(30-35°)clinoformsoftheSellashow the Sellaplatform Geometry andsedimentologyof of debate. the Sellaarenotentirelysettledandstillamatter the SellaMassif,geometryateasternsideof deposits arequitewellpreserved throughoutmostof relationships betweenCassianbasinandplatform result, whiletheprimarygeometric-stratigraphic vetta portion athinlevel ofhorizontally stratifi clinostratifi – Wengen Formation; theupperwall iscutintothe within theuppermostportionofbasinalLa Valle – Frara), notethewedging outofthecarbonatetongues Megabreccia” attheGardenaPass (GroednerPass Group. Thelower wall correspondstothe“Gardena Figure 4.3- View ofthenorthernsideSella ”) andspectacularlyexposed atPizBoè. As a ed SellaPlatform slope;inthetopmost nger onallsideswith ed platform top 1991). Inaddition,thebasinswerefedwithvolcano- swarms ofmeter-size boulders(Bosellini&Neri, The apronsconsistofcalciturbidites,debritesand the “Locomotiva” (SellaPass), andin Val deMesdì. shales, asforinstancevisibleattheGardenaPass, at slope carbonatespassrapidlyintobasinalmarlsand rather narrow (afew hundredmetreswidth)andthe aprons atthetoe-of-slope;theseaprons,however, are Intensive downslope transport isrecordedbydebris an obliqueparallelgeometry(Bosellini&Neri,1991). wedge ofbasindeposits,theclinostratifi area, wheretabular progradationoccursover athin (e.g., SellaandPordoipasses).Inthe Val diMesdì of slopeischaracterizedbyaclimbingprogradation towards thebasinfl is distinctlyconcave, asthedipgraduallyfl On thelower slope,theshapeofclinostratifi although itexhibits erosionalscars(Kenter, 1990). the shapeofclinostratifi of meterswideatthemost. At upperslopesettings, top andslopedepositsisquitenarrow, afew tens in growth position. The margin betweenplatform- nice meter-size tepees. At Pisciadù,withinthetopsetbeds, being representedbyoccasionalcross-beddingand thick. Sedimentarystructuresarerarelypreserved, Thecosmilia like coralcolonieshave beenfound oor, particularlywherethebase cations isoftenplanar, cationsshow attensout 26-05-2004, 15:19:46 cations P44_R_OK 29 From theevidence deriving frombothplatformand extended inlayersandtonguesontotheupperslope. formed arigidframework attheplatformmargin that such as 1998). Automicrite, associatedwithmicro-organisms preserved olistolithsmicrofacies (Russoetal.,1997; aragonite precursors,adsuggestedbythevery well arrays ofneedle-like botryoidalcrystals,deriving from former radiaxialfi dominated byisopachouslayersofrecrystallised, clotted micrite. The widely occurringcementsare peloidal, thrombolitic-peloidalorsimplecrustsof include typicalmicrobialtextures, e.g.laminitic- & Schlager, 1999,2001). Automicrite fabrics s.s. crusts) inallthedifferent platformdomains(Keim cements, detritalcarbonatesstabilizedbymicrobial of automicrites.s.,vugsfi automicrite facies (defi most strikingsedimentaryfeatureistheoccurrenceof are consideredasderiving formmargin settings. The of-slope (Russoetal.,1997,1998). These olistoliths which areembeddedinmarly-shalydepositsatthetoe- gravitatively displacedblocks(“Cipitboulder”), depositional fabrics, however, arederived from the depositionalfabrics. The bestpreserved dolomitization, itisstilllocallypossibletorecognize Although thewholeplatformisaffected bypervasive Carbonate Production Microfacies and derived siliciclasticsandextra-basinal shales. Tubiphytes Figure 4.4.-ThestratigraphicrelationsatMuntfreit(according toKeim’s interptetation). brous calciteandbyfan-shaped , andwidespreadmarinecements ned asanintimateassociation lled byprimarymarine TRIASSIC CARBONATEPLATFORMSOFTHEDOLOMITES PRODUCTION, RELATIVESEALEVELFLUCTUATIONSANDTHE SHAPING OFTHEDEPOSITIONALARCHITECTURE 1999, 2001). the angleofrepose(Kenter, 1990,Keim &Schlager, by non-cohesive sandandrubblelayerspiledupto slope was notcontrolledbytheautomicritebut rather however, indicatethatthelarge-scale geometryofthe shape andsteepangleoftheclinostratifi was pronetogravitative resedimentation. The planar probably depositedalsointheslopesetting,whereit boundstone texture. Microbialautomicritewas m indiameter. Clastsandbouldersshow amicrobial mid-lower slopecontainabundant boulders,upto5-6 The clinostratifi the carbonateproductiondynamicsofthisplatform. cement precipitationthereforeplayedamajorrolein totally recrystallised. Automicrite andcarbonate 5% ofthewholerockand,inmostcases,they are 2001). Skeletal grainsrepresentgenerallylessthan dasycladacean, solenoporacean(Keim &Schlager, ostracods, gastropods,echinoderms,foraminifers, sphinctozoan sponge,and,occasionally, bivalves, Cayeuxia Macrotubus component, including cement-fi mainly consistedofmicrobialboundstones,withlarge olistoliths samples,themargin-upper slopedeposits massif, fromtheGardenaPass totheSellaPass and proceed inacounter-clockwise directionaroundthe The excursion startsfromtheGardena Valley andwill Excursion stops lled cavities, withasubordinateskeletal , Hedstroemia ), skeletal cyanophyta (suchas ed brecciasandmegabreccias ofthe , Girvanella problematic , Ortonella a ( Tubiphytes Rivularia cations, ), rare 29 , , -

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Volume n° 5 - from P37 to P54 P44 - P44 Leader: M.Stefani the adjacentbasinalformations, Wengen andS. 15° toSE;thesametectonicdippingaffecting also Meisules/Murfreit, however, themegabreccia dips the GardenaPass, thebedsarenearlyhorizontal;at proper. The megabreccia isdistinctly stratifi thinner fl steeply clinostratifi Cassiano Fm;(2)anupperunit,composedbythe portion ofthe Wengen Fmandoverlain by the S. (Bosellini, 1982),lyingwithintheuppermost a lower one,theso-called“GardenaMegabreccia” & Neri,1991).Two maincarbonatebodiesoccur:(1) Leonardi &Rossi,1957,Bosellini,1982,Bosellini the interpretationofdepositionalgeometries(e.g. is aquiteinterestingexample ofcontroversy in the outcropsatMeisulesdalaBisces-Murfreit, The northernfl Gardena Pass Stop 3.1: and Colfosco(Figure4.1). proceed towards Arabba, CampolongoPass, Corvara observing thestratigraphicsuccession. Then wewill Pordoi (2950m)bycablecarandwalk backdown then tothePordoiPass. HerewewillassenttoSass from theclinostratifi separates the“MegabrecciadiPasso Gardena”lower wall Cassiano Fmargillaceouscarbonatebasinaldeposits Platform attheSWofColfosco. A thinlevel ofSan Figure 4.5- View ofthenorthernslopeSella at-lying top-setbedsoftheSellaPlatform ank oftheSellaPlatform, including ed slopebrecciae. ed slopedepositsandbythe e. At ed. c . Wengen succession. An alternative interpretation all stratigraphicallylocatednearoratthetopof the basinsequencebelow Grohman Spitze,etc.), Col Rossi-Padon belt;SellaPass; thelower partof out inseveral localitiesoftheDolomites(i.e. megabreccia bodiesorolistolithswarms cropping Megabreccia maybecorrelatabletoanumberofother interpretation; moreover, hethinks thattheGardena authors ofthepresentpaper(C.Neri)stillsharesthis buildup” byBosellini&Neri(1991,p.24).Oneofthe of a“pre-existing carbonateplatform,ratherthana a channalizedbody, resultingfrommultiple collapses 1998). The “Gardena Megabreccia” was interpretedas Mastandrea, inBosellini&Neri,1991;Russoetal., packstones andcement-fi scarce metazoans(sponges,corals),peloidal-skeletal boundstones, withmicroproblematicalike The boulderslargely consistofautomicritic some dm-thickbedsofcalciturbiditesintercalations. boulders, uptoseveral metresindiameter, andof Megabreccia” consistsmainlyofbrecciatongues within thebasinsediments(Figure4.3). The “Gardena outrunner blocks(“Cipitboulders”)areclearlyvisible interfi Pass, wherethemegabreccia tongue pinchsoutby m, atMeisules/Murfreit,andzero,theGardena “Gardena Megabreccia” varies betweenabout200 Cassian platform(Figure4.5). The thicknessofthe nature, aswelltheplatform-topsedimentsof Cassiano ones,thoughttobeoriginallyhorizontalin ngering withthebasinal Wengen Formation; lled cavities (Russo& Tubiphytes 26-05-2004, 15:19:52 , P44_R_OK 31 conglomerates, skeletal andlithoclasticcalciturbidites marlstones, siltstones,volcanoclastic sandstonesand called “Locomotiva”. The sectionconsists mainlyof clinostratifi the S.CassianoFmandeventually into W-dipping Fm basinalsuccessiongradingup-sectioninto The sectionattheSellaPass shows the Wengen Sella Pass Stop 3.2: of Alpine tectonicdeformation(Plananticline). bedding (fl these depositsandtheinclinationofmegabreccia oblique erosive cutoftheproximal-distalparts (0-200 m)ofthemegabreccia bodyisrelatedtothe In thisinterpretation,thestrongthicknessvariation “Gardena Megabreccia” andthebasinalsediments. who assumedalateralinterfi back tothemodelofLeonardi&Rossi(1957), Keim (Keim &Schlager, 2001)isessentiallyastep of theNorthernSellastratigraphyproposedbyL. network ofautomicritewithpelletstructure.Noteoccasionallithoclasts,fragmentsredalgae(r),dasycladaceanthalli (d) andcementfi width ofpicture=2cm).(AfterKeim &Schlager, 1999);RIGHT-Thinsectionphotomicrographofautomicritefacies on themarginupperslope,composedofdarkcrustspeloidalclots,limpidbotryoidalcement,numerousgenerations indicating thatautomicritelithifi of fi Figure 4.6-LEFT Automicrite andskeletal detritusfromtopsetbeds.Themainpartofthepictureconsistsa brous cementaswell asinternalsediment. Automicrite forms constructionalcavitiesandgravity-defyingfabrics at-lying, SEdip)isthoughtobetheresult ed dolomitemegabreccia oftheso lling irregularvugs.Thefi ngering betweenthe ed almostimmediatelyuponformation. (Val Lasties,widthofpicture=3cm).(After TRIASSIC CARBONATEPLATFORMSOFTHEDOLOMITES PRODUCTION, RELATIVESEALEVELFLUCTUATIONSANDTHE brous cementlayeratthetepee-level (t)ispartiallydissolved. (Val deMesdì, SHAPING OFTHEDEPOSITIONALARCHITECTURE interfi and carbonatebreccias. The sectiontopshows the structureless. dipping clinoformsisrathermassive andapparently only 10-20mthick;thetransitionzonetosteeply at Sella Towers (Kenter, 1990). The topsetsarehere angle decreasesfromabout30°in Val Lastiesto20° distinctly fl Cassian Platformslope. These clinostratifi above theplatformtopcanalsobeobserved. Schlernplateau Fm(PordoiMb=Raibl Lasties. The thinningoutoftherecessively weathered interior oftheSellaPlatform,outcroppingin Val clinostratifi exposed wall ofSassPordoiwithits topsetsand This stopoffers apanoramicview ofthe WNW- Road curve (2200m)justbelow theSellaPass Stop 3.3: ngering ofbasinal bedsandclinostratifi cations andprovides someinsightsintothe attening outbasinwards, sincetheirdip Keim &Schlager, 2001). cations are cations Auctorum 31 ed ) -

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Volume n° 5 - from P37 to P54 P44 - P44 Leader: M.Stefani platform (Keim &Brandner, 2001). fractures develloped duringsubaerialexposure ofthe be interpretedaskarstdikes ordissolution-enlarged several meterstotensofmeters. These structuresmay are somedm’s wide,taperdownward toadepthof within theUpperSchlernDolomite. The fi 2001). The sandstonesoccuralsoasfi glauconite andopaqueminerals(Keim &Brandner, echinoderm fragments),scarcevolcanic glass, feldspars, minorcarbonategrains(ooids,lithoclasts, consisting ofvolcanic lithoclasts,quartz,detrital m thick,cross-beddedgreenishsandstones,mainly the Cassianplatformtopissharplyoverlain by2 crops out. At thebaseofthisunit(PiccoloPordoi) desiccation cracks,interbeddedwithminormarls, coloured dolostoneswithburrows, fenestraeand Below, amonotonousalternationoflightandgreenish Norian DolomiaPrincipalecyclic peritidalsuccession. from SassPordoitoPiccolo(2,692)crossesthe of theCassianplatform-to-basintransition. The trail Cassian Dolomitesuccessionandatacross-walking The stopisaimedattheobservation ofthepost- Pordoi Pass-Sass Pordoi-Piccolo Pordoi Stop 3.5: observed. clinoforms below PiccoloPordoi)canbewell (W-dipping clinoformsatPic Ciavaces andS-dipping dimension anditsdiverging progradationdirections From thistopographicview point,thefullplatform Rif. MontiPallidi (PianSchiaveneis; 1850m) Stop 3.4: Figure 4.7-CrosssectionattheSellaeasternside(modifi ssures-fi ssures llings matched withadip-anglereductionoftheplatform- progressive infi (Dürrenstein) Cassianplatform. This modelsuggestsa Schlager etal.(1991)forthePiccodi Vallandro L. Keim, following amodelformerlysuggestedby Keim &Brandner(2001)and is herepresentedby An alternative interpretationhasbeenproposedby a ramprepresentedbytheinheritedCassianslope. moderate thrustingoftheDürrensteinDolomiteover been modifi in evidence thattheoriginalonlapgeometryhas the interpretationofDoglioni(1992)isthatheputs Cassian platforms(Figure4.2C). The peculiarityof the residualbasinsandonlappingslopesofformer deposition ofaneven-bedded carbonatebodyinfi to asea-level drop(Bosellini,1984). The resultisthe shallowing duetosedimentaryinfi nucleating fromthebasinfl was interpretedasanaggradingsedimentarybody, interpretations, however, theDürrensteinDolomite thrust planebetweenthetwo formations.Inboth clinofroms, whereasDoglioni(1992)assumeda of the“DürrensteinDolomite”ontoCassianDolomite Bosellini andNeri(1991)suggestedanonlapgeometry 1991, Doglioni,1992;Keim &Brandner, 2001). interpretations (Mojsisovics, 1879,Bosellini&Neri, delle Dieci),hasledtomany different stratigraphic of theSella,fromCrepdeMuntto Vallon (Sasso The successionsoutcroppingontheeasternfl Campolongo Pass Stop 3.6: ed afterKeim &Brandner, 2001) ed bycompressionalstress,resultingin lling shallowing oftheCassianbasins, oor asaresponsetobasin lling and,possibly, 26-05-2004, 15:19:58 lling ank P44_R_OK 33 substantial helpduringfi go to A. GruberandH.(Innsbruck)for (Cosenza) forstimulatingdiscussions.Specialthanks P. Gianolla(Ferrara), A. MastandreaandF. Russo We gratefullyacknowledge R.Brandner(Innsbruck), Acknowledgements Mesdì, alongtheNNW-facing fl spectacularly exposed clinostratifi The laststopprovides uswithapanoramicview ofthe Road toGardenaPass Stop 3.7: of theonlaprelationshipsonaninheritedslope. & Neri(1991)thisis,onthecontrary, aclearevidence extensional tectonics.IntheinterpretationofBosellini accommodation spacerelatedtosynsedimentary of theunderlyingCassianslopeorbynewly created the gentlyeast-dipping,low-gradient palaeo-relief this reductioninthicknesscouldbeexplained by few meters.IntheopinionofL.Keim (thiswork) towards theplatformtop,whereitisreducedtoa unit. The subtidal unit(c.50-60mthick)wedgesout subdivided intoalower subtidalandanupperperitidal platform top. At CrepdeMunt,thePordoiMbcanbe volcanoclastic materialwould nothave reachedthe 7). Onasteeplyfl the formerbasintowards theplatformtop(Figs.2A, can betracedwitharatherconstantthicknessfrom by thepresenceofvolcanoclastic sandstones,which platform topandtheS.Cassianbasinissupported The postulatedfi very gentlydippingslope(Keim &Brandner, 2001). palaeo-slope surface, but was ratherdepositedona Brandner, 2001)doesnotformanonlaponasteep Dolomite ofBosellini&Neri,1991,andKeim & Based onthisassumption,thePordoiMb(Dürrenstein up attheendingofCassianDolomitedeposition. that alldeepbasinsaroundtheSellaatollwerefi angle, probably<2°.L.Keim (thiswork) concludes overlaid thesedepositswithavery low depositional (2001), thelasttonguesofCassianplatform Brandner, 2001). According toKeim &Brandner the Cassianbasin(Bosellini&Neri,1991,Keim & various authorsasaresponsetotheshallowing of and peloidalpackstone,hasbeeninterpretedby including hummocky-cross-bedded ooliticgrainstone part oftheS.CassianoFmexposed atCrepdeMunt, shallow water depositionalsystem. The uppermost homogenisation intoagentlydeeppingramp-like, slope, climaxingintoalateralpalaeogeographic lling upoftheformerreliefbetween anked platform,theinputofcoarse eldwork, andtoM.Stefani ank oftheSella. cations atthe Val de TRIASSIC CARBONATEPLATFORMSOFTHEDOLOMITES PRODUCTION, RELATIVESEALEVELFLUCTUATIONSANDTHE lled SHAPING OFTHEDEPOSITIONALARCHITECTURE (iv) A niceexample ofapotentialhydrocarbon accommodation space. basinal Fm,eventually fi pre-volcanic ones,progradedontotheSanCassiano calcarenitic slopes,signifi again duringtheCarnian Time, whenfi Nuvolau andLastoideFormìn), conquering thearea (iii) Spectacularpost-volcanic platforms(Guseladel onlapped theformerplatformslope. terrigenous andvolcanoclastic successionsthen shroud oflimestonesslowly accumulated. Thick drowning intoaphoticconditions,whereapelagic giving uptoretrogradation,deepeningandfi survival” againstfast subsidence,but eventually and earliestLadiniantimes“bravely fi evolution (CerneraPlatform),duringyounger Anisian (ii) The recordofan isolatedcarbonatepinnacle platform generationsanddepositionalsequences. (i) The goodpreservation ofthreesuperposed Anisian compression. The visitedareathereforeoffers: developed, tobevariously reactivated bythe Alpine brittle (trans)-tensive Middle Triassic structures more continuousinnature.Inthehingebelt,several and theUpper Triassic successionsarequitethickand the Ladinianvolcanism didnotdirectlyaffect thearea long-lasting terrigenouslyinfl separated bygentlyerodedboundaries,followed by various generationsof Anisian carbonateplatforms, eastern andnorthernareaisonthecontrarytypifi event; theUpper Triassic isthin and gap-prone. The (Livinallongo Fm),untiltheonsetofvolcanic and widelyprogradingover thinbasinallimestones Anisian-Ladinian platforms(SciliarFm),aggrading older units;thesecarbonateswerefollowed bythick unconformity, deeplycutintotheLower Triassic and directly lyingonasinglesequencebounding characterised byupper Anisian carbonatesalmost Figure 1.6),thelesssubsidingwesternregion is hinge belt. As discussedintheintroduction(cf. developed withintheEastern/Western Dolomites pre- andpost-volcanic carbonateplatformsystems, This daywilloffer awealthofopportunitytoexamine Introduction A. Riva,P.Gianolla, M.Stefani Nuvolau andLastoideFormin Platforms The pre-volcanic Cernera andthePost-Volcanic reviewing. (Ferrara) forscientifi DAY 4 fi c discussionand extended cantly lessinclinedthanthe lling upalltheavailable uenced basinaldeposits; n grained ne gtn for ghting es by nal 33 -

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Volume n° 5 - from P37 to P54 P44 - P44 Leader: M.Stefani Anisian sequence(An3sensuGianollaetal.,1998a), is partofthetransgressive systemtractofthethird eroded depositionalsequence. The conglomerate gap, encompassingtheaccumulationtimeofahere 1992, associatedwithasignifi 1983; Blendingeretal.,1984;DeZanche (Voltago Cg),fi turn directlyoverlain bycoarsefl regional peritidalplatform(Lower SerlaDolomite),in Lower Triassic unitwas followed byanearly Anisian scale overthrust, theSelva Line(cf.Figure1.1). The Fms, outcroppinginthehangingwall ofaregional- with theshallow marineBellerophonand Werfen The stratigraphicsuccessionofthevisitedareastarts area. fl karstifi widespread permeability-enhancinghydrothermal impregnation arelocallyvisible,aswella sourced by Anisian blackshales. Actual hydrocarbon permeability volcanic andvolcanoclastic depositsand reservoir inacarbonate pinnaclesealedbylow Figure 5.1-TheCerneraplatform-top isvery rich inoncoidalfacies,developed inhighenergysubtidalenvironments. uorite mineralizationsarealsovisiblein the visited cation. Middle Triassic leadsulphideand lling uperosive channels(Blendinger, uvial conglomerates cn chronological cant erosional surface iscovered byfl boundary between An 3and An 4sequences:the Another relative sealevel dropmarked thesequence Blendinger etal.,1984;Blendinger, 1983). Dont Fmbyprevious authors(Gaetanietal.,1981; including thereefdeposits,wereincludedin toward theslope. The wholeoftheseoutcrops, developed, ofteninvolved insynsedimentarysliding of thisprogradingplatform,patchreefslargely western sideoftheCerneraMassif. At themargins documented bytheclinostratifi Serla Fm)thenprogradedontothebasinalunits,as to aterrigenousinput. The coeval platforms(Upper basinal succession(RecoaroandDontFms),subject sequence. The thirdsequenceevolved hereintoa to thewest,beforedepositionofforth Anisian which was totallyerodedoutonlyafew kilometres through transgression,aswitnessedbythedeposition Verdàl). Marineenvironments werere-established indicates anorthward palaeofl Lower SerlaFmclasts.Pebbleimbricationlocally (Richthofen Cg),madeupmainlyby Werfen Fmand cations visibleinthe uvialconglomerates ow direction(Mt 26-05-2004, 15:20:02 P44_R_OK 35 top ofContrìnplatformisvery sharpandisnormally the Cernera,between Val diZoniaandMt.Pore. The this basinalunitarevisibleintheatwesternof al., 1995;Masetti& Trombetta, 1998).Outcropsof (Moena Fm,MasettiandNeri,1980;DeZancheet micrites andresedimentedcarbonatemegabrecciae more subsidingareas,recordedbyorganic rich development ofintraplatformanoxicbasins,inthe in thesubsidencespeedarealsorecordedby evolution. Duringthistimeinterval, spatialvariations thickness, recordingthestartingofafast subsidence carbonate platformisquitethick,reaching150min of MorbiàcandContrìnFms.Inthisarea,the Figure 5.2-TOP -Geometric scheme ofthestratigraphicrelationshipsbetween theCerneraPlatform andtheadjacent TRIASSIC CARBONATEPLATFORMSOFTHEDOLOMITES PRODUCTION, RELATIVESEALEVELFLUCTUATIONSANDTHE units. BOTTOM -Chronostratigraphicscheme oftheCernerasuccessions. SHAPING OFTHEDEPOSITIONALARCHITECTURE probably forerunningthemagmatismonset. The within atectonicallyactive geodynamicframework, 2003). This evolution recordsavery fast subsidence, geochronometric datafromtheLatemar(Mundiletal. as suggestedbythecorrelationwithmostrecent span, probablyintheorderofonemillionyears, huge thicknessaccumulatedinavery shorttime is recordedbymorethan600mofsuccession,a The fast aggradationalevolution oftheSciliarFm redeposited calcarenites(basalLivinallongo Fm). separated byafew metresofbasinalmicritesand the two platformgenerationsarehowever sometimes directly overlain bytheSciliarFm platform;totheN, 35 -

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Volume n° 5 - from P37 to P54 P44 - P44 Leader: M.Stefani hyloclastites, interbeddedwithvolcanoclastic et al.1977)depositedhereabout100mofsubmarine volcanic activity withfi Lower Triassic. fi the After is bearingolistolithsrippedupfromasdown asthe erosive andoftendeeplychanalisedbase. This unit deposits (CaoticoEterogeneo),associatedwithan catastrophic gravitational driven megabreccia by theappearingofbasicvolcanoclastics andby sedimentation (AcquatonaFm),suddenlyinterrupted gave placetoatemporaryreturnhemipelagic through hydrocarbonexploration. These sandstones buried underthePoand Venetian Plain.Butknown (Viel, 1979;Bruscaetal.1981),now deeply by theerosionofanemerged crystallinebasement fl turbiditic fl side ofthedrowned platform,facing theincoming sedimentation was particularlyfast intheeastern onlapped andfossilisedthelower partoftheslope; Thick terrigenousturbiditesinthemeanwhile platform, throughLadiniantimes. rich limestones,slowly accumulatingontothedead giving uptoammonoidandpelagicpelecypods platform, encriniticshoalsaccumulated,eventually 1995a). Duringthedeepeninglastphaseof during theCrassusSbz(sensuMietto&Manfrin space eventually forcedtheplatformtodie,probably production andthefast creationofaccommodation factory potential. The imbalancebetweencarbonate area was shrinking,furtherreducingthecarbonate dramatically lengthening,theeuphoticplatformtop evolution oftheplatform,whilefl enclosed basinswestward. Duringtheaggradational between open-marineareas(eastward) andsemi- Blendinger 1989);(iii)nutrientsupplydifference (ii) windward versus leeward effect (Blendinger& between two margins, associated toaplatformtilting; could beconnectedto:(i)differential subsidence sharp difference betweenthetwo sidesoftheplatform breccia slope,retrogradingonlyatalaterstage. The whereas thewesternsidedeveloped anaggrading area wheretheplatformexportation was negligible, of themargin, withvery thinslopedeposits,inan the easternfl Cernera Platformisquitedifferent initsvarious sides: The platform-margin andslopegeometryofthe hydrodynamic energy subtidaleuphoticconditions. dasycladaceans andgastropods,depositedinhigh calcrudites andcalcarenites,associatedwithabundant Cernera platform-topismademainlyofoncoidal ank. These turbidites(ZoppèSandstones)werefed uxes, slower intheshelteredwestern ank recordsabacksteppingevolution ssural eruptions(Castellarin rst explosive phase,quiet ak were anks carbonates, duetoCO palaeokarstic systemswithintheCerneraPlatform hydrothermal circulationinducedhypogenic turbidites (Viel, 1979).Duringvolcanism, strong Dolomite, shows herslopedepositsclearly prograding the GuseladelNuvolau platform,madeupofCassian succession, bothCarnianinage. Toward the north, late CassianPlatformandofathinDuerrensteinFm the LastoideFormìn are visible,madeupofathick Lastoi deFormìn Platforms. BehindtheColPiombìn, volcanoclastic deposits,separatingtheCerneraand 1950s. Duringthistop,ourfeetwillstayonthe hydrothermal mineralisation,exploited untilthe in Italian),relatedtolateLadiniansulphides derives itsnameformtheleadmines(=piombo probably becauseof Triassic collapses. This area are directlyvisible,sincedepositshearlacking, south, theplatformtopsuccessionofCernera as agiganticolitstolith(CaoticoEterogeneo). At the probably involved intoachaoticsynvolcanic complex a hugeblockofMiddle Triassic platformcarbonates, Col Piombìniswellvisible,quitelikely toconsistof stage. Toward thesoutheast,incloserproximity, the carbonate platform,drowned atanearlyevolutionary (Figure 5.3),consistingofathicklate Anisian Mount Cernerashows upatthesouthofthissite landscape form Forcella Zonia Carbonate platforms showing upinthegeological Stop 4.1: Excursion stops renewed Upper Triassic subsidence. available accommodationspaceofthearea,upto successions, thetwo factors combiningtofi matched withashallowing upevolution ofthebasinal during afast progradationalevolution ofplatforms, The slopesprogressively reducedtheirinclination, basin fl clinostratifi platform-to-basin relationships:comparatively steep provide excellent outcropsfortheobservation ofthe (Bosellini ,1984;DeZancheetal.,1993)mountains times. The LastoideFormìn andGuseladelNuvolau generation developed hereonlyduringearlyCarnian sin- andearlypost-volcanic buildups, anew platform Fm Livinallongo, etc.) The Cerneraarealacking proximity ofvertical hydraulicbarriers(FmDont, Piombìn andapalaeokarstnetworks, particularlyin developed theimportantleadmineralisationofCol (Hill 1995,Palmer 1995). The sulphur-rich circulation oor totheplatform-topcarbonatesuccession. cations linktheterrigenouslyinfl 2 andH 2 S richcorrosive fl ll upany 26-05-2004, 15:20:08 uenced uids P44_R_OK 37 up bybasinalmaterials. The wholeofthedrowned producing detachmentnichesthatweretobefi suffered smallscallopingduring andafterdrowning, sediments (FernazzaandLa Valle Fms).TheCernera of terrigenous(ZoppèSandstones)andvolcanoclastic Cernera Platformisonlappedbyathicksuccession the drowned platformtop. The easternslopeofthe pink colouredsedimentarydikes, cuttingthrough biozonation. Ammonoids alsooccurinyellowish- Sbz, accordingtotheMietto&Manfrin(1995a) ranging fromtheCrassustoRecubariensis by ammonoidrichfacies, showing associations succession oftheplatformisvisible,covered platform. Along thewalked throughtrailthedrowning of the“post-mortem”evolution ofthedrowned The stopwillbemainlyfocusedonthediscussion onlapping theCernera Platform Val Cernera: drowning andbasinalresediments Stop 4.2: onto thebasinalCassianFormation. Lucia. located outsidethemap,near Villagrande diColleSanta Fig 5.3Thedayexcursionitinerarywithstops.Stop6is TRIASSIC CARBONATEPLATFORMSOFTHEDOLOMITES PRODUCTION, RELATIVESEALEVELFLUCTUATIONSANDTHE lled SHAPING OFTHEDEPOSITIONALARCHITECTURE cover. cover. were probablyerodedfromtheCerneraPlatform deposits (CaoticoEterogeneoFm);thesefragments limestone blocksredepositedintosynvolcanic chaotic Triassic facies have beenfoundalsoasreworked area (Cros&Houel,1983). Ammonoid-rich Middle Fm (Knollenkalke Mb),asintheForcella Vallazza they laterallygradeintothenodularLivinallongo rich facies arewidespreadontheeasternslopeand Zanche etal.,1993). Ammonoid andpelecypod (Blendinger etal.,1984;Brack&Rieber1993;De thin level ofHallstadt-typerednodularlimestones Cernera Platformwas tobeslowly covered bya edifi Alpine deformation. The sharptopofthecarbonate Platform isvisible,involved intominorbrittletectonic On theleft(South),thickupper Anisian Cernera illustrates the Triassic evolution area(Figure1.1,5.4). The geologicallandscapevisiblefromthepassclearly Lastoi deFormìn prograding platform Flank ofCernera Platform andthepost-volcanic Forcella GiauandLagodelleBaste:theeastern Stop 4.3: ce isadrowning unconformity, associatedwith 37 -

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Volume n° 5 - from P37 to P54 P44 - P44 Leader: M.Stefani 26-05-2004, 15:20:13 Figure 5.4 - A: The northward dipping, clinostratifi cation of a Cassian platform, forming the Lastoi de Formìn. The slope dolomite body is affected by several minor Alpine strike slip faults. Figure 5.4 - B: Onlap of basinal resedimented beds (Zoppè Sandstones, Caotico Eterogeneo and Fernazza Fms) onto the eastern slope of the drowned Cernera Platform. The platform is tilted toward the east (right) of about 20°, the contact is slightly reactivated by Alpine tectonics. P44_R_OK 39 intervals, differing inboththenatureandamountof demise. The successioncanbesubdivide into four condensation aftertheeventual CerneraPlatform evolution SciliarFm,followed byaneven stronger of theContrìnFmandaggrading-retrograding of theaccumulationrates,duringgrowth time The successionrecordsaprogressive reduction a dramaticlateralchangeinthesedimentationrate. about 800m,asharpstratigraphiccontrastrecording the coeval CerneraPlatform,showing athicknessof 10 mthicksuccessionisplacedincloseproximityto Rieber (1993),andDeZancheetal.(1993,1995). This then analysedindetailby Vrielynck (1984),Brack& the fi Contrìn andSciliarplatforms. The outcropwas for 5.5) accumulatedinnearbaseofslopesettingsthe The PuntaZoniacondensedcarbonatesection(Figure of Anisian -Ladinianage Punta Zonia:condensedbaseofslopesuccession Stop 4.4: excursion. (Passo Falzarego-Tofane area). visible, whichwillbevisitedduringthefi the northUpper Triassic carbonateplatformsare tectonic tilting(GuseladelNuvolau, Figure5.9). At the primaryclinostratifi slope isvisible,dippingnorthwards, becauseofboth At thenorthofGiauPass, adifferent platform 5.4). top units(cf.LastoidelFormìn sectioninFigure emersion surfaces separatesseveral peritidalplatform the slopeunits.Inuppermostportionofcliff, bedded platform-topdolomitesthenprogradedonto cut alongtheiractualstratigraphicdip.Horizontally however reduced,sincetheclinostratifi The apparentanglevisibleinthesub-vertical oneis in thislategenerationofpost-volcanic platform. since micriticfacies andslumpedbedsarecommon were now muchsmallerthanthepre-volcanic one, these deposits(LastoideFormìn). The slopeangles toward theSEthenprogressively expanded onto (S. CassianoFm). A carbonateslopeprograding a terrigenous-carbonateshallowing upsuccession the volcanoclastic unit(La Valle Fm)incontactwith faults apparentlylower theleft(eastern)side,putting environments. A subvertical Neogenestrike-slip deep volcanoclastic-fed basintoperitidalcarbonate record ashallowing upevolution, fromarelatively The following stratigraphicsuccession(Figure5.6) Platform was gentlyreactivated bythealpinetectonics. The onlapofthevolcanoclastics ontothedrowned the shallow water depositionalsystemtermination. rst timeexamined byCros&Houel(1983)and cation immersionandagentle

TRIASSIC CARBONATEPLATFORMSOFTHEDOLOMITES cation arenot PRODUCTION, RELATIVESEALEVELFLUCTUATIONSANDTHE fth dayof SHAPING OFTHEDEPOSITIONALARCHITECTURE for bothisotopicdatingandphysicalcorrelation. intercalated intothesuccession,providing key levels on theoutcrop. A few tuffi the destructive illegal fossilcollectiontoimpact fl these faunae have beenspectacularlyfossilisedas Anisian-Ladinian boundary(Figure5.5).Someof Recubariensis subzones,developed aroundthe through thesection,rangingfromReitzito factory. Ammonoids werefoundinseveral levels the drowning terminationoftheCerneracarbonate in ammonoidandpelagicpelecypods, documents pelagic condensedsedimentation,withlevels rich the calciturbiditesandestablishmentofpurely (iv) intheuppermostunit,rapiddisappearingof early aggradationalhistoryoftheCerneraPlatform, fi wedge, (iii)thethirdinterval ischaracterisedby carbonates, drapingandsuturingtheprevious chaotic interval consistsinacentimetrelevel ofdarklaminated collapsed Contrìnplatformmargin; (ii)thefollowing forming aresedimentedwedgeatthesideof in skeletal calcarenites,coquinasandmegabrecciae, the carbonateimportation;(i)lower unitisrich Brandner, with taxasuchas rich inmicroproblematicaandcalcareoussponges, These facies aredominatedbymicrobialboundstones (“ to thosedescribedthenorth,inBraiesarea (Figure 5.7). These patchreefsarevery similar involved intogravitational syndepositionalsliding marginal area, bothpreserved insituor, moreoften, mainly consistsofsmallpatchreefs,developed ina Verdàl), thelower portionoftheUpperSerlaFm In thewesternpartofCerneraMassif(Mt moving toward olderunits. the successioninareverse stratigraphicway, i.e. Zonia Valley, walking down thetrail,weshallobserve second onebeinglackinghere.Inlower partofthe fi platform andthesequenceboundaryseparating depositional geometryofthe Anisian UpperSerla This shortwalk willbefocusedonthelarge relative sealevel fl Zonia Valley: Anisian depositionalsequencesand Stop 4.5: beds. This margin unitmakes transitioneastward to suggested bythedeformationofunderlyingDontFm are gravitationaly displacedtoward theeast,asalso al. 1981). These patchreefs,onlyfew metreswide, uorite molds,afeaturethatunfortunatelyprompted ne-grained resedimentedcalcarenites,recordingthe rst andthird Anisian depositionalsequences,the Rutschblocke Celyphia ”, Bechstädt&Brandner, 1970). uctuations sp.and Olangocoelia otti tes (“Pietra Verde”) are Tubiphytes Bechstädt& (Gaetaniet 39 -

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Volume n° 5 - from P37 to P54 P44 - P44 Leader: M.Stefani area) andassociatedwithpalaeokarsticcavities. cutting down intothebasinal Dont Fm(Mt Verdàl overlain byasubaerialerosive sequenceboundary, platform-top unit. The UpperSerlaFmisdirectly algae boundstonesandrepresentingaback-margin limestones anddolostones,consistingofsponge/ shoals arefollowed upward byhorizontally bedded the slopedepositsandmargin patchreefsand platform recordsaprogradationevolution, since The middle-upperportionoftheUpperSerla syndepositional structure(LoschiesuoiFault). a sinistralstrike slipfaults, probablyreactivating a slope andbasinaldeposits,asvisibleattheeastof Figure 5.5-PuntaZoniaSection,modifi described inthetext. ed fromDeZanche etal.,1995;Numbers(1-4)correspondtotheunits birdseyes, arranged intoperitidalcycles. The Lower microcrystalline dolostones,withstromatolitesand The Lower SerlaFmconsistsof whitish-gray absent inthearea(DeZancheetal.,1992,1993). boundaries iswellvisible,thesecondsequencebeing sharp boundarybetweenthe An 1and An 3sequence Valley, animportant sectionisoutcropping,wherethe toward thenorth. At thelower endoftheZonia structures indicatealocalpalaeocurrentdirection to theUpperSerlaFms;laminationandimbrication unit includinglithoclastsrangingfromthe Werfen the baseforRichthofenConglomerate,offl The boundarybetweensequence3and4provides 26-05-2004, 15:20:19 uvial P44_R_OK 41 TRIASSIC CARBONATEPLATFORMSOFTHEDOLOMITES PRODUCTION, RELATIVESEALEVELFLUCTUATIONSANDTHE SHAPING OFTHEDEPOSITIONALARCHITECTURE the region (Fodom, fromtheLatinfodere=mining). so importantintheareatogenerateLadinnameof activity ofthenearby Triassic ores,which was indeed during thestopwererelatedtoancientmining The gothicchurchandrenaissancebuildings visible dolomites composetheplatform-topsuccession. of themountain,wellbeddedsubtidallimestonesand together inphysicalcontinuity. Ontheeasternfl where theContrìnandSciliarplatformsarebound unit isclearlypinching-outunderthepeaktop, the Livinallongo Fmwas accumulating. The basinal inclined atabout30øtoward thebasinfl clearly shows Northwest-dippingclinostratifi Sciliar FmCerneraPlatformattheMount Verdàl terrigenous depositsandtothebasinalunits. The by grassyledges,correspondingtothetransgressive platform generationformsteepwalls, interspaced speeding upofthesubsidencespeed. The different increase oftheaccommodationspace,inducedbya Sciliar Fm As awholethesectionrecordsdramatic this site:Lower Serla,UpperContrìnand platform generationscanbeclearlyobserved from depositional sequencesisvisible.Four carbonate (Figure 5.8),wherethewholeofMiddle Triassic view ofthewesternfl This dayexcursion willendwithaspectacular Cernera Platform and Anisian sequences Villagrande diColleSantaLucia:viewofthe Stop 4.6: TST ofthissequence. transgressive evolutionary trends,belongingtothe (Zonia Section). The unitrecordaglobally stratifi wave infl from coarserfl transition isvisible,alongaN-Sstretchingsection, and Werfen Fms.Inthisterrigenousunit,alateral pebbles, derived fromtheerosionofLower Serla the Voltago Cgisonthecontrarymadeupbycoarse plant remains.OnthesouthernsideofCernera, lands conditionsarealsodocumentedbyterrestrial deposited incoastalenvironments. The emerging dispersed aslensesintoaprevailing sandstonematrix, Cg, hereformedbyfi boundary, followed byaterrigenousunit,the Voltago Serla Fmtopiscutbyasubaerialerosive sequence Platform base ofslope.CourtesyC.Neri,unpublished. volcanoclastic conglomeratestotheLastoideFormìn Figure 5.6-Stratigraphicsectionstretching fromthe cation, tomoreopenmarineenvironments uenced siliciclastics,withhummocky cross uvial conglomeratestoshallow storm ank oftheCerneraMassif ne grainedconglomerates oor, where oor, cations, ank 41 -

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Volume n° 5 - from P37 to P54 P44 - P44 Leader: M.Stefani platforms andthepalaeo-topography fl The demiseoftheUpper Triassic (Cassian) intraplatform basin(MoenaFm)totheleft.TheSciliarFmhereconsistsofslope brecciae. Figure 5.8-Thewestern wall oftheMountCernera.TheContrìnFmrecordsstratigraphictransitiontoasmall sequence boundaries. of thedifferent Anisian-Ladinian carbonateplatform generationsanddepositionalsequences,punctuatedbysubaerial Figure 5.7- View ofCerneraand Verdàl Mountainsfrom Villagrande, spectacularlyshowing thevertical succession and palaeogeographicevolution ofUpper Triassic This dayexcursion isfocusedonthestratigraphic Introduction P. Gianolla,N.Preto,M.StefaniandC.Neri DAY 5 attening peritidal DolomiaPrincipaleplatform. Attention members, theargillaceous RaiblFmandthethick shallow marineformation,subdivided intoseveral Cassiano Fm),theHeiligkreuz(Duerrenstein) platforms andthecoeval basinalsuccessions(San area aremadeupbyUpper Triassic units:theCassian (Figure 5.1). The successionsoutcroppinginthis carbonate platformsaroundthePasso Falzarego 26-05-2004, 15:20:24 P44_R_OK 43 al., 1997;Gianollaet1998;Keim etal.,2001). 1974, 1994;Mastrandrea,1995;Mastrandreaet the uppermostLadinian–lower Carnian(Ulrichs, by ammonoids,conodontsandpalynomorphsto overthrust. The ageoftheseunitsisconstrained area beinglargely telescopedbyamajor Alpine et al.,1982),theoriginallyinterspacedbasinal ones, arevisibleincloseproximity(Bosellini two different platforms,theNuvolau andLagazuoi carbonate platformsandbasins.Intheexcursion area, These unitsrecordacomplex framework ofrimmed San CassianoFormation Cassian Dolomiteand be alsodiscussed. up ofthewidespreadDolomiaPrincipaletidalfl of thepalaeogeography(HeiligkreuzFm)andstart way toterrigenous-carbonateramps,thefl basins. The demiseoftherimmedplatforms,giving spatial relationsbetweenplatform-top,slopesand reconstruction ofthefacies stackingpatternandthe around Falzarego Pass (2,105m)allows thedetailed Cassian platforms. The seismicscaleoutcrops and thesequencestratigraphicorganisation ofthe will beparticularlyaddressedtotheclimaticforcing Figure 6.1-ThedayexcursionitineraryandstopsonanaerialphotoofthePasso Falzarego area TRIASSIC CARBONATEPLATFORMSOFTHEDOLOMITES PRODUCTION, RELATIVESEALEVELFLUCTUATIONSANDTHE attening out at will SHAPING OFTHEDEPOSITIONALARCHITECTURE 15-10°, duringtheshallowing evolution ofthebasin. The slopeanglechangedthroughtimefrom35-30°to slope breccia,interfi are characterisedbythickbedded,clinostratifi water environments ortidalfl and pisoids,indicatingdepositioninvery shallow dolostones, withbirdseye structures,stromatolites by tensofmetreswellbedded,fi here thicker thanintheSellaareaandischaracterised or massive bedding. The platformtopsuccessionis coloured crystallinedolomites,showing anindistinct et al.,1998a). The CassianDmconsistsofalight & Gaetani,1982;DeZancheetal.,1993,Gianolla recording athirdorderdepositionalcyclicity (Fois and basinalshaleonlappingontotheslopes,probably separated byaninterval ofnocarbonateexportation two superimposedaggradation/progradationphases, Lagazuoi Platform. These rimmedplatformsrecord was onthecontraryfoundinnorthernisolated know, noevidence ofcontinentaltetrapodsfootprints interior succession(Avanzini etal.,2000);upto ichnofauna, documentedinthestratifi presence ofadiversifi considered asanattachedplatform,becauseofthe The southernblock(Nuvolau Platform)mustbe ngering with basinalsediments. ed andwidespreadtetrapod ats. The slopedeposits nely crystalline nely e platform ed 43 ed -

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Volume n° 5 - from P37 to P54 P44 - P44 Leader: M.Stefani overlain bythesabkhaandparalicfacies oftheRaibl the SanCassianoFm,anditisinturnunconformably Dolomite oronthebasinalshalesandlimestonesof The HeiligkreuzFmliesbothontotheCassian areas andzonessubjecttostrongterrigenousinput. successions, recordinglarge shallow-water carbonate This formationconsistsofmixed clastic-carbonate a periodofparticularlymoistclimaticconditions. 2003; Preto&Hinnov, 2003). This interval records et al.,1993;Neri&Stefani, 1998;Bosellinietal,. abundant coarsesiliciclasticsupply(DeZanche complex topographyandaperiodofanomalously This unitrecordsthefl (Dürrenstein) Formation Santa Croce -Heiligkreuz Sella excursion. but they arequitesimilartothoseseenduringthe exposed, becauseofthewidespreadvegetation cover, excursion area,theoutcropsofthisunitarepoorly present, withinmuchfi slope, large olistoliths andisolatedbouldersareoften micrites, andsiliciclasticsandstones. At thetoeof turbidites, resedimentedbioclasticwackstones and of brown toyellowish marls,alternatedwithcarbonate The basinalSanCassianoFmpredominantlyconsists terrigenous successionforming thelower portionoftheHeiligkreuzsuccession. Passo Falzarego, showing themassive development ofintersupratidalstructuresandemersionbrecciae. At theleft, Figure 6.2-Topmost portionoftheCarnianperitidalsuccessionoutcroppingalong themainroadatsouthof attening ofthelower Carnian ner graineddeposits.Inthe limestones withplantroots,andclaystonesrichin characterised bystromatoliticdolostones,marly in peritidalcycles (Ltz interval isfollowed byadistinctlithozoneorganised rich incorals(Member A inRussoetal.,1991). This can befound,withspectacularlypreserved faunae, lower portionofthemember, metrescalepatchreefs packstone/grainstone andhybridarenites.Inthe skeletal grainscalcarenites,oolitic-bioclastic of amixed carbonate-terrigenousunit,comprising onlaps theformerCassianplatformslopes.Itconsists portion oftheSanCassianoFm;thisaggradingunit and conformablyliesontheuppermostshallowed Borca member members. the formationcanbesubdivided intoseveral informal framework ofGianollaetal.(1998b).Inthestudyare, named Car3,accordingtothesequencestratigraphic Gianolla etal.,1998a,b;Preto&Hinnov, 2003),here sequence (Russoetal.,1991;DeZanche1993; representing acomplete3rdorderdepositional The HeiligkreuzFmisaroughlyisochronousunit, (Gianolla etal.,1998b;DeZanche2000). (Carnian), byammonoidandpalynomorphsfi interval, closetotheJulian-Tuvalian boundary Fm Itsageisconstrainedtoanarrow stratigraphic

is confi ned totheformerbasinalareas D ), several metrethick, 26-05-2004, 15:20:31 ndings P44_R_OK 45 1978), showing as laterally replacedbyamoreterrigenousunit,named (Bosellini etal.,1982). The Lagazuoimemberis carbonate equivalent ofthe“Arenarie delFalzarego” be tracedforseveral kilometres,correspondingtothe forms awellrecognisablecarbonateunit,thatcan calcareous sandstonesandmassive dolostones.It consists ofdolostoneswithherringbonecrossbedding, fl abundant pelagicfossils,condensedonthemaximum water carbonates,named Fm ismainlymadeupbywellstratifi areas unreachedbysiliciclastics,theHeiligkreuz and tidalcurrentstructures.Inthenorthernshelf In thevisitedarea,thisformationisdominated Raibl Formation (Travenanzes fm) marly limestones,with (2003). This unitendswithnodular, bioturbated lithofacies databaseisdiscussedinPreto&Hinnov siliciclastics andbyadeepeningtrend. A detailed characterised byaprogressive upward decreasein consists ofamixed siliciclastic-carbonatelithozone, 2003). be tracedforseveral kilometres(Preto&Hinnov, is toppedbyawelldefi former Cassianplatforms on topoftheBorcamemberthatabove thetopof plant debrisandambers. This unitisdeveloped both abundant initslower portion. and varicoloured argillaceous layers,particularly peloidal andstromatoliticdolostones,raremarly organised inmetrescaleperitidalcycles, with odn srae h following The surface. ooding Falzarego sandstonemember, Figure 6.3-Pisoidsarewidespreadinthevisitedperitidalplatform-top succession.Photoandfi Dibona member

spectacular tractionarylamination Chondrites sp ( ned palaeosoil,whichcan

(Figure 6.8). This lithozone cf . Bosellinietal.,1982) Vallandro member

TRIASSIC CARBONATEPLATFORMSOFTHEDOLOMITES Lagazuoi member (Bosellini etal., . andsometimes PRODUCTION, RELATIVESEALEVELFLUCTUATIONSANDTHE e shallow ed ,

SHAPING OFTHEDEPOSITIONALARCHITECTURE fl Falzarego Pass mayrecordthefringingoutofsucha The thincoarsesiliciclasticdocumentedasnorth merging into coastal sabkha-lagoonenvironment. indicates afl tetrapod foot-prints. This facies associationclearly turn characterisedbymud-cracksandoccasional erosionally cuttingreddishandgrayclaystones,in sandstone bodies,withevidence oflateralaccretion, facies associationsshow metrethickcross-bedded southern borderoftheDolomites. This terrigenous the south,toprevail onallotherlithofacies atthe siliciclastics increaseinthicknessandfrequency to sandstone mayoccur(i.e.,Falzarego Pass). The coarse base oftheunit,metre-thickquartz-conglomerateand of thevisitedsections,inCortinavalley. At thevery evaporates, welldeveloped afew kilometreseastward the occurrenceofcalcretepalaeosoilandsulphate arid climaticconditionsareinferredonthebasisof into widecoastalmudfl intercalations. These facies probablyaccumulated and shales,withminor, decimetre-thicksandstone coloured dolostonesandred,greengraymarls by monotonousalternationsoffi the EandNEofDolomites(Bosellini&Hardie,1985; a rimmedplatform,whichhave themargins locatedat formation recordingthegiganticcarbonatetidalfl the DolomiaPrincipale,awidespreadLate Triassic shallowing upward peritidalcycles, pertainingto mainly madeupbythevertical stackingupof characterising thelandscapeofDolomitesare The impressive wellstratifi Dolomia Principale uvial system. uvial depositionalsetting,gradually ats andlagoons. Arid tosemi- ed cliffs spectacularly nger: M.Morsilli. ne grained,light- at of 45 -

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Volume n° 5 - from P37 to P54 P44 - P44 Leader: M.Stefani steep Alpine landscape. steep Alpine still witnessingtheviolenceoffi opportunity toobserve First World War fortifi geometry andfacies, theexcursion will offer the order. Besideshowing somespectaculardepositional will proceedinasomewhat reverse stratigraphic The excursion willstart fromPass Falzarego and Excursion Stops in theorderofonekilometre. Tofane mountains,showing astratigraphicthickness In thevisitedarea,thisunitformshighwall ofthe record fast but laterallystronglyvariable subsidence. huge thickness,rangingbetween250and2,000m, De Zancheetal.,2000;Gianolla2003). The subordinated sandstonesanddolomites(RaiblFm).Modifi subaerial karsticsequenceboundarytoppingplatform-top peritidal dolomitesandisfollowed byredclaystoneswith (Dibona mb)andanuppermainlyarenaceoushigh-energyunit(Falzarego sandstones).Theformation restsonthe Figure 6.4-TheHeiligkreuzFmsuccessionatPasso Falzarego, subdividedintoalower argillaceous-carbonateunit tting inthisvery cation, ed afterBosellinietal.(1978). in thequantityandmaturityofpalaeosoils,indicates cycles thickness,matched withtheupward increase 6.3 pisoids arealsocommonthroughthesection(Figure with tepeestructuresandcalichepalaeosoils.Marine capped bysubaerialexposure surfaces, associated is characterisedbyperitidalsedimentarycycles, al., 1986,Bosellini,1991etc.). The platforminterior is oftenquotedas“DürrensteinDolomite”(Hardieet the mainroad;ingeologicalliteraturethisoutcrop Cassian Dolomiteisparticularlywellexposed, along Slightly SWofPass Falzarego, theplatformtopof Heiligkreuz siliciclasticsat Passo Falzarego. The Cassianplatform interiorandthe Stop 5.1: ). A thinning-upward trendinthesedimentary 18-06-2004, 14:43:33 P44_R_OK 47 The HeiligkreuzFmfeaturesarehereonthecontrary the platformtopsuccessionisheremorepronounced. however, thekarsticerosive surface markingthetopof are herequitesimilartothoseseenatPasso Falzarego; rimmed carbonateplatform. The platformtopfacies slope andplatform-topfacies ofalower Carnian The LagazuoiMountainischiefl surroundings on thestratigraphy and structuralgeologyofthe siliciclastics atRif. Lagazuoi;panoramicview Cassian platform interiorandcarbonate- Stop 5.2: tractionary structures(Figure shoreface depositionalenvironment, withspectacular sedimentary structures,recordingahighenergy succession (Falzarego member)spectacularly shows Falzarego Pass, theupperportionofsiliciclastic Figure terrigenous-carbonate succession(Dibonamember; started againwiththedepositionofshallow water 6.2 developed onthetopofperitidalsuccession(Figure end throughemersionandapalaeokarsticbreccia space. Platformsedimentationcameabruptlytoan progressive decreaseintheavailable accommodation a shallowing evolution oftheplatformanda ). Above thisdiscordancesurface, sedimentation 6.4 ), herenotwellexposed. At thenearby Figure 6.5-Highenergytractionarylaminationsformed undertidal currentinfl 6.5) TRIASSIC CARBONATEPLATFORMSOFTHEDOLOMITES . y madeupbythe PRODUCTION, RELATIVESEALEVELFLUCTUATIONSANDTHE the upperportionofFalzarego sandstonesatthehomonymouspass. SHAPING OFTHEDEPOSITIONALARCHITECTURE accumulated asmassfl of theHeiligkreuzFmwillbeshown. They probably In thewalk tostop5.3,large brecciabodiesatthetop as theSellaandMarmoladaones. Other wellknown Triassic platformsarealso visible, Col Gallina,Nuvolau, Averau, and LastoidiFormin. east, theSettssas–RichthofenReef,SassdeStria, system ofattachedplatformsincluding,fromwestto The lower CarnianCassianDm records anarticulate pinched alongathrustingplainbifurcation. at somedistanceformany carbonateplatform,isnow of aCarnianbasinalsuccession,originallydeposited (Sasso diStria,ColGallina,Nuvolau) andalarge fl (Lagazuoi-Tofane) thrustedover thesouthernone et al.,1982).Here,thenortherncarbonateblock south-vergent Falzarego Pass overthrust (Bosellini also visiblefromabove, inthefootwall ofthemajor Falzarego Pass andtheoutcropsofstop5.1willbe on themain Alpine tectonicstructuresofthearea. the 360°panoramaonCarnianplatformsand structures. FromRifugioLagazuoi,wewillobserve tidal currentinfl part recordsashoalenvironment, subjecttostrong 2003). This formation ishererelatively thin;itsupper deposited inarampenvironment (PretoandHinnov, formed bymixed carbonate-siliciclasticsediments, sharply different fromthosepreviously seen,being uence, recordedbyniceherringbone ows andrepresentthelocal uence in ake 47 -

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Volume n° 5 - from P37 to P54 P44 - P44 Leader: M.Stefani this pointonward, thedepositsarefullycarbonatein at thedisappearanceofargillaceous input:from and DolomiaPrincipaleformationsmaybeplaced exposure features. The boundarybetween theRaibl stromatolite horizons,oftenshowing subaerial by yielding poorlydiversifi their basebybioturbatedlagoondeposits,frequently & Hardie,1985). These cycles arecharacterisedat metre-size shallowing-up peritidalcycles (Bosellini depositional styleintheirbeingorganised into shales intercalation,heraldingtheDolomiaPrincipale characterised bywellstratifi part oftheRaiblFm(Forcella Travenanzes) is sabkha andfl or stromatoliticdolostones,depositedintotidalfl consisting ofpolychromeshales,marls,aphanitic The upperCarnianRaiblFmisherevisible,mainly fl Forcella Travenanzes.Upper Triassic The tidal Stop 5.3: Formin andfurther. S.Croce/Heiligkreuz (Badia Valley) toLastoidel position, wereobserved throughalarge area,from Similar brecciabodies,inthesamestratigraphic SB ofDeZancheetal.,1993;Gianolla1998a). expression ofanimportantsequenceboundary(Car4 by theUpperTriassic carbonateoftheCrodadaLagoandPelmo. platform oftheLastoidiFormìn isvisible,tectonicallyinclinedtowards theleft(East),whereasskylineisdominated of theCassianplatform followed bytheterrigenous-carbonate HeilgkreuzFm;inthebackground thelateCassian Figure 6.6-ThespectacularsceneryvisiblelookingsouthwhiledescendingfromtheLagazuoi,witherosionaltop ats: RaiblandDolomiaPrincipaleFms Megalodon ood plain environments.plain ood uppermost The ssp . , followed upward byplanar ed bivalve faunae, dominated ed dolomites,withminor at, thick. Sass Pordoi(Day3),wherethisunitisonly250m this DolomiaPrincipaleoutcropwiththoseseenat cliff ofthe Tofana diRotzes.Itisworthy tocompare visible, spectacularlyexposed inthenearlyvertical 900 m)oftheUpper Triassic peritidaldepositsis From theexcursion trail,thehugethickness(about smooth ledgesgeneratedbytheRaiblbeds(Fig nature andformsteepcliffs, insharpcontrastwiththe and sedimentarystructuresareoftenpoorlyvisible strongly dolomitisedunit,wheretherocktextures current megaripples; (3)Lagazuoimb,amassive facies show fl micritic limestonesandgraymarls;thegranular grainstones, regular alternations ofbioturbated comprising arenites,ooliticandbioclasticpackstone- and palaeosoils;(2)Dibonamb,acomplex unit with colouredshaleandareniteintercalations lithozone D,consistingofwhiteperitidaldolostones, unit canbeheresubdivided intothreeintervals: (1) (Rif. Dibona,at3.7kmtotheeast,Figure further thicknessincreaseisvisiblemoving eastward much thicker thanattheRif.Lagazuoi(stop5.3);a At ColdeiBos(OxHillinLadin),thisformationis Heiligkreuz Fm facies. Col deiBos:acloserviewofthe Stop 5.4: aser bedding,wave ripplesandwave- 6.9 26-05-2004, 15:20:42 ). This 6.7 ).

P44_R_OK 49 along theroad,toeofslopecalcarenitesandcarbonate cut alongtheiractualstratigraphicdip. Walking down than therealone,sinceclinostratifi angle visibleinthesub-vertical cliff ismuchlower mudstone oftheSanCassianoFm. The apparentdip interbedded withthebasinalshaleandmicritic consist ofcarbonatebrecciaandcalcarenites, be thereforeavailable. The clinostratifi progradational phaseoftheCassianplatformwill of thecarbonateslopedepositsyounger we willmove toward olderunits. A closerview along aFirst World War Italianmilitaryroad, Moving downward fromtheForcella ColdeiBos, indentation withthebasinalSanCassianoFm Cassian platform slopefaciesandtheir Stop 5.5: Col deiBossummit. tidal fl top oftheCassianDmwillbevisible,aswell and palaeokarststructuresmarkingthediscordance bedding arepreserved. Duringthisstop,thebreccias the visitedoutcrop,herringboneanddm-scalecross because ofthediageneticoverprinting; however, in Figure 6.7-Theimpressive easternwall oftheTofane Massif, formed bytheUpperTriassic peritidalcyclicsuccession of theDolomiaPrincipaleFm,recordingaperiodsubstantialsubsidence,heraldingJurassic evolution ofthe atfacies ofthelower RaiblFm,exposed atthe TRIASSIC CARBONATEPLATFORMSOFTHEDOLOMITES cation arenot ct deposits cate PRODUCTION, RELATIVESEALEVELFLUCTUATIONSANDTHE SHAPING OFTHEDEPOSITIONALARCHITECTURE clinostratifi the lowermost partofthetrail,consistingroughly lower CarnianCassianplatformwillbevisiblealong Car 2depositionalsequence. The slopefacies ofthe relationship recordsthetransgressive phaseofthe Dm. According toGianollaetal.(1998),thisonlap relationship withabaseofslopetonguetheCassian San CassianoFmareexposed, showing anonlap mudstones andvery fi camp kitchen,usedduring World War I,wellbedded with basinalshales. At thesiteofanItalianarmy olistoliths (Cipitboulders)willbevisible,interbedded top andsteepslopes,withatypicalrimmedplatform Carnian Time. The lower Carnianbuildups show afl changing indepositionalstyleoccurredduringthe under anafternoonlight,showing thedramatic panoramic view ofthefi From thesouthernsideofFalzarego valley, a geometry oftheupperCarnian sediments. the lower Carnian platforms versus theramp Scoiattoli: therimmedplatform geometryof Panorama ofthefi Stop 5.6: ed massive dolostonesandbrecciae. eld triparea from Rif. future passive continentalmargin. ne-grained calcareniteofthe eld tripareawillbevisible 49 at -

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Volume n° 5 - from P37 to P54 P44 - P44 Leader: M.Stefani in theSchilfsandsteindeposits(Germany), Raibler chronostratigraphic interval, amberwas foundalso to thelateJulian-early Tuvalian. Inthesame Heiligkreutz/Dürrenstein Formation, corresponding Amber was foundinthelower andmiddle partofthe 1998b; Roghietal.,2002,2003;Ragazzi2003). chemical featuresofthisfossilresin(Gianollaetal., extensively studiedthepalaeobotanicalandphysico- research groupofthePadua andFerraraUniversities and Wendt &Fürsich(1980).Morerecently, a Koken (1913)andlaterdescribedbyZardini(1973) amber depositsoftheworld, fi some ofthemostancientandquantitatively substantial The Heiligkreuz/DürrensteinFormation provides G. RoghiandE.Ragazzi Dürrenstein Formation Amber from theHeiligkreuz/ (Preto andHinnov, 2003). terrigenous-carbonate rampdepositionalsystem the very reducedtopographicgradientsofamixed a wedgeofcarbonate-clasticsediments,recording upper CarnianHeiligkreuzFmisinsteadformedby recognised throughouttheDolomites. The (mostly) can beidentifi geometry. Two generationsofcarbonateplatforms terrigenouscarbonate HeiligkreuzFm,atColdelBos. by asubaerialsequenceboundary, followed bythe Figure 6.8-TheCassianplatform-top successioncapped ed (CassianDm.1and2),apattern rstly indicatedby pristine state,isinprogress. The wholeofthesedata in theamber, stillpreserved atanastonishingly examined. Studyonthefossilmicrorganisms included near 437°C,was thehighestamongfossilresins the mainexothermal peak of Triassic amber, located sites oftheworld (Ragazzietal.,2003). The value of of amberandcopaldifferent agesandfrom many corresponding tothemaximalrateofweightloss, and thecomparisonwithmainexothermal peak, permitted thefi Palaeogenic burial. Thermogravimetry analysis in theembeddingsediment,duringMesozoicand an oldage,andahistoryofhighpressureexposure peaks. Also theNMRspectrumiscompatiblewith is confi unique patterns. A strongdegree ofresinmaturation “fi The diagnosticregion ofthespectrum,so-called amber (Figure6.12)isatypicaloneoffossilresins. world sites.Theinfra-redspectrumofthe Triassic with youngerambersandresins(copals)fromother from theDolomites,enablingcomparisonwithit physico-chemical characterizationofthefossilresin automated elementalanalysisproducedawhole (TG), differential thermogravimetry (DTG),and magnetic resonance(NMR),thermogravimetry with infraredspectrophotometry(FTIR),nuclear resin (Ragazzietal.,2003).Laboratoryanalysis physico-chemical characterisationofthisfossil The abundance ofsmallamberdropsallowed the Cretaceous (Roghietal.,2002). group ofconiferspresentfromUpper Triassic to producing speciestotheCheirolepidiaceaeFamily, a preserved leaves allowed thecorrelationofamber- In apalaeosoil,considerableabundance ofcuticle- transported andredeposited. and plantdebris,suggestingthattheamberwere and fromhybridsandstoneswithmarinepelecypods plants remains,indicatingautochthonousfi Formation werefoundinpalaeosoils,associatedwith desiccation.The amberoftheHeiligkreuzDürrenstein characteristic reticularstructures,suggestingafast 2-3 millimetres.Sometimes,outerdropsurface shows (Figure 6.11)withalittlestemandmaindiameterof Fossil resindropsshow typicalglobe-shapedforms palaeoclimatic fl could beinfl suggests thatresinexudation fromtheancienttrees resin throughawideareaindepositsofthesameage Chinle Formation (Arizona).Discovery ofthisfossil Schicten andLunzerschicten(Austria)inthe ngerprint region” between8and10mm,shows rmed bythelackoflabilefunctionalgroups uenced bybothevolutionary factors and nding ofmainthermalevent peaks uctuations. 26-05-2004, 15:20:47 nding, P44_R_OK 51 distances. Between the LastoideFormìn andTorri delFalzarego amajor Alpine overthrust makes theevaluationof Figure 6.9-Thestronglateralvariationoftheshallow-water, terrigenous-carbonateHeilgkreuzFmover short primary distancediffi TRIASSIC CARBONATEPLATFORMSOFTHEDOLOMITES PRODUCTION, RELATIVESEALEVELFLUCTUATIONSANDTHE cult. Lithofaciessubdivisions(A-H)asinPreto&Hinnov (2003). SHAPING OFTHEDEPOSITIONALARCHITECTURE 51 -

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Figure 6.10 - Panoramic view of the southern cliff of the Falzarego-Tofane massif, spectacularly showing the depositional geometry and the depositional sequence 26-05-2004, 15:20:52 architecture. The Col del Bos was photographed from the west (cf. Figure 6.6, 6.8). P44_R_OK 53 Zone, Brack&Rieber, 1993;1994). The profi fauna suggestsanuppermost Anisian age(Secedensis the MarmoladaPlatform(Figure7.1). The ammonoid and upperslopesettingsinthenortheasternsideof transect, stretchingfromplatform-toptothemargin The stopregards anisochronouspalaeogeographic on thecontrary, largely dominatesthemassif. preserved in comparatively smallareas. The margin facies are The well-beddedplatform-topsuccessionoutcrops kilometre ishowever likely (Stefani &Caputo,1998). of 200m;anoriginalthicknessintheorderone of theplatform-topsuccessionisapproximately the “CalcaredelLatemar”. The outcroppingthickness whereas theplatform-topsuccessionsareascribedto to the“CalcaredellaMarmolada”(Leonardi,1967); tectonics (Figure7.7,7.8) The slopesedimentsbelong were involved intoimportantpolyphase Alpine scattered withinadeepwater basin. The platforms part ofanarchipelagosmallcarbonateislands, The MarmoladaPlatform(Schlern/SciliarFm)was Introduction F. Russo, A. Mastandrea,M.Stefani,C.Neri. dominated bysyndepositionalcements The MarmoladaMassif:acarbonateplatform also asapaleoenvironmental indicator. unique kindoffossilresinwithinterestingpotentials suggest thatthe Triassic amberoftheDolomitesisa Falzarego-Lagazuoi area. Figure 6.11- Amber dropsform theHeiligkreuzFmin in situ asvery narrow belt. The slopefacies, DAY 6 TRIASSIC CARBONATEPLATFORMSOFTHEDOLOMITES PRODUCTION, RELATIVESEALEVELFLUCTUATIONSANDTHE l is le SHAPING OFTHEDEPOSITIONALARCHITECTURE genus structures asencrustingspongesandcreatedanew western Southern Alps. The author interpretedthese were alreadyrecognizedbyStoppani(1858),inthe These peculiarcementsinthe Triassic buildups facies (Figure7.8). cement crustswhichcharacterizetheupperslope Marmolada istheabundance ofstrikingconcentric easy tosample. The mostimpressive featureofthe can bestudiedingoodoutcrops,whicharereasonably The Marmoladaunderwentweakdolomitizationand analyses ofsedimentaryandearlydiageneticfeatures. by afacies-destroying dolomitizationoftenpreventing ≠ retreat oftheglacier. excellent outcropwas onlyrecentlyexposed bythe 7.1) exhibits nofaults breakingitscontinuity. The between Q2650and2750). The transect(Figure at theMarmoladaGlacierfront(PiandeiFiacconi, located inthenorthernslopeofMarmolada,and several recentstudies(Mastandreaetal.,1991;Russo in theplatformsofDolomitesisemphasized The roleoforganically-induced carbonatecementation of thestructures. and primarymineralogy(Mgcalciteversus aragonite) but drew nofi authors, recognizedalow-Mg calcite composition, Middle Triassic ofthe Western Southern Alps. The et al.(1989)performedacomprehensive studyinthe Resch, 1981;Henrich&Zankl,1986).FrisiaBruni modifi recently interpretedasearlydiageneticprecipitates, (Leuchs, 1928;Schmidegg, 1928),weremore known as sponges (Stoppani,ibidem). These structures,also that theMiddle Triassic was actuallytherealmof importance ofthe“evinospongiae”, makingthepoint The majorityoftheDolomitesplatformswas affected ed byfreshwater diagenesis(Brandner& Evinospongia “Großoolith” nal conclusionwithregard totheorigin . Heunderlinedthelithogenetic Figure 6.12-Infra-redspectrumof inthe Austroalpine Triassic similar Carnianamber. 53 -

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Volume n° 5 - from P37 to P54 P44 - P44 Leader: M.Stefani et al.1999).Several surfaces areassociatedwith as wellinthecoeval LatemarPlatform(Egenhoff they areparticularly commoninnear-margin settings, diagenesis arevisiblethroughouttheplatform,but marking thecycle topsandrecordingasubaerial in meter-scale shallowing upward cycles. Surfaces bioturbation. The platform-topfacies areorganized with rarecurrentlaminationsdespitethewidespread storm layersandwave structuresarevisible,together was winnowed inothersubtidalenvironments. Graded within syndepositionallylithifi almost absent.Micriteiscommonlypreserved only 7.4). Packstones arerare,mudstonesandwackestones Figure 7.3).Coarsegrainstonesarecommon(Figure degree ofpeloidalboundstones(Figure7.2A-B; clastic calcarenitesandcalciruditestoaminor The platform-topsuccessionconsistsofintra-bio- Platform topfacies cement crustsoftheMarmoladaMassif. (2000) proposedasimilaroriginforthespectacular et al.,1997;1998a;1998b);inparticularRussoal. the frontofMarmoladaglacier. and nicelyoutcropping;outcropsoftheplatform-top arelimitedtothenorthbyan Alpine overthrust andatthesouthby della Marmolada),togetherwiththelocationoftransect(A).Thewestern marginoftheplatform iswell preserved sketch-map illustrates therelationshipsbetween theplatform-top (CalcaredelLatemar)andtheslopedeposits Figure 7.1-Locationmapofthestudyarea,innorthernslopeMarmolada, Western Dolomites.Thegeological

ed boundstones,but inter-supratidal cementation. decimeter tometer-scale teepees,recordingamassive are alsocommonandincludeindecreasingorder by welllithifi The grainstonesfacies (Figure7.3)isdominated gastropods, echinoids,andpelecypods. algae, withasmallamountofforaminifers, cyanobacteria (porostromata) anddasycladacean are notparticularlyfrequentandconsistofskeletal lined byisopachousfi laminae. This facies isvery richinprimarycavities, thrombolitic clotsor, morerarely, inthinstromatolitic by earlylithifi The boundstonesfacies (Figure7.3)ismadeup yield abundant pelecypods pelagicandammonoids. corals andspongesarerare.Sometransgressive levels and crinoids.Greenalgaearealsocommon;solitary benthic pelecypods, articulatebrachiopods,echinoids and diversifi The macrofossilcontentofthesubtidalunitsisrich Microfacies andBiota ed. Particularly abundant aregastropods, ed boundstonesintraclasts.Bioclasts ed peloidalmicrites,organized in brous cements.Microbiota 26-05-2004, 15:20:59 P44_R_OK 55 were foundasisolatedspecimens.Someformsare Plexoramea cerebriformis Maslov rare. They arerepresentedby 1991a; 1991b;Russoetal.,1997),arerelatively in thepost-volcanic platforms(Brandneretal., Calcareous microproblematica,whicharecommon Rieber, 1993;1994;DeZancheetal.,1995). is ingoodagreementwithammonoiddating(Brack& indicates anupper Anisian-lower Ladinianage,which (Gümbel) and nodosa alpina Dasycladacean algaearerecordedby occur asmicritizedandcoatedghostsstructures. Hedstroemia are common.Mosttaxabelongtothegenera microproblematica, andafew sponges.Porostromata gastropods, pelecypods, foraminifers,echinoderms, of frequency, porostromata,dasycladaceanalgae, grainstones oftheplatform-top were onlyaffected bymarine-phreaticdiagenesis.(C)Massive precipitationofabundant concentric crustsconsistingofradiaxialfi Figure 7.2-Schematic drawing(nottoscale)ofthefaciesandgeometric relationshipsbetween platform-top, margin, margin inducedthevadosediagenesisofpeloidal-porostromataboundstonesandgrainstones.(B)Boundstones slope andbasinduringtheearlyaggradingphaseofMarmoladaPlatform. (A) Frequent emersionsoftheinner Pia, Schafhautl, on theupperslope.(D)Theslopesedimentswere predominantlyformed bycement-rich blocks derived fromthe Tubiphytes carinthiacus Diplopora annulata , Bevocastria Oligoporella Gyroporella syndepositional erosionofthenarrow platform marginbelt.Notethedifferent scaleof A andB and Mello.Spongesonly sp. This association Schafhautl, Cayeuxia Tubiphytes obscurus TRIASSIC CARBONATEPLATFORMSOFTHEDOLOMITES cf. (Flügel)and Macroporella brous marinecements(“evinospongiae”)took placeattheoutermarginand PRODUCTION, RELATIVESEALEVELFLUCTUATIONSANDTHE . Many thalli ampleforata Diplopora Ortonella ,

SHAPING OFTHEDEPOSITIONALARCHITECTURE were observed. ( Foraminifers arerepresentedbyagglutinatedforms frequent is can beattribuited tothegenus decapod coprolites,belongingtothegenus compared withagglutinatedforaminifers.Some and miliolids. These groupsarelessfrequentas grains insituasshown byconformgeopetal infi shallowing upward cycles. Pendentcementsbind developed insupratidallevels, marking thetopof and pendentcements(Figure7.3,7.4)arewell calcite (2-4mol%Mg). Vadose subaerialmeniscus to organic matterinclusionsandconsistoflow-Mg cements have a“cloudy”appearance probably, due cements (Figure7.3,7.4). The isopachousfi impressive isopachousrimsformedbymarine Both grainstonesandboundstonesfacies show Cements Endothyranella Olangocoelia otti sp.; Earlandinita Bechstädt&Brandner. versus CandDdrawings. sp.);duostominids Deningeria Favreina . More llings. brous 55 , -

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Volume n° 5 - from P37 to P54 P44 - P44 Leader: M.Stefani rich inboundstonesandearlymarinecements;c)an bioclastic belt;b)arelatively narrow massive margin, facies beltsarevisible:a)apoorlybeddedcoarseintra- Moving fromthe platform-topdown theslope,three water platform-topandthesteeplydeepeningslope. developed withinanarrow beltbetweentheshallow- patchwork ofdepositionalsub-environments, The platformmargin ischaracterizedbyacomplex Margin andupperslopefacies amount ofsyndepositionalcements,asignifi intraclasts (Figure7.4).Despitetheimpressive Tilted pendentcementsarecommonwithinreworked the margin and upperslopecarbonates. Similar latediageneticcalcitesanddolomitesoccurin by quasi-stoichiometricdolomite(Figure7.3). calcite. This late calcitehasbeenpartiallysubstituted porosity was lefttobefi and theconspicuousvadosecements(M=meniscuscements).X7. orientation oftheclast,largeamountisopachous marinecements, cyanobacteria, bivalve, andgastropodbioclasts.Notetherandom Figure 7.4-Grainstonesconsistingofboundstoneintraclasts,skeletal lled atalaterstagebysparry cant structures (Figure7.8).Broken andoverturned vivid greenepifl partially infi the foraminifer (c),againrich inmicrodispersedorganic micro-inclusions, lookinglesstransparentintransmitted light; thisexcitedlightemissionislikely tobeassociated and d),observed underidenticalobservationconditions. precipitation. Latediageneticcementsinfi High hydrodynamicenergyplatform-top calcarenites(c the contrarynotfl radiaxial fi Note thevividfl crusts (evinospongia);(b)isopachous marinecements marine cements,particularlysointhelevels richer in played asignifi with microdispersedorganicmatter, which probably observation ofstronglycementedmarginfacies;(a) Figure 7.5-Transmitted andepifl matter. MarmoladaPlatform atPiandeiFiacconi. lling aprimarycavity. In bothfacies,notethe brous cementsfromalargesyndepositional spheroidal ormorelessseparated size. These crusts formlaterallylinked millimeters toseveral centimetersin cements formthickcrusts,fromafew concentric bands(Figure7.5). These uorescence displayedbytheearlyphreatic peloidal boundstones,similartothose The narrow margin isdominatedby auct.) (Figure7.2C;Figure7.8). fi characterized byimpressive radiaxial outer-margin andupper-slope area, radiaxial fi interconnected bylarge amounts of sized boundstonesnuclei,coatedand facies arecharacterizedbydecimeter- The outermargin and upperslope abundant. lined byisopachouscementsare Millimeter- orcentimeter-scale cavities (Russo etal.,1997),arenearlyabsent. the post-volcanic carbonateplatforms micrite whicharemostabundant in the boundstonesvolume. Aphanitic remains compriselessthen5%of metazoans islacking;theskeletal primary framework formedbysessile found intheplatform-topsuccession. A X 7 = latedolomitesubstitutingsparrycalcite. cement, I=marineisopachous cements;D late sparrycalcite,P=vadosependent isopachous marinecementsandfi (porostromata). Thecavitiesarelinedby boundstones withskeletal cyanobacteria Figure 7.3-Cavity-rich peloidal brous cementcrusts(“evinospongiae” uorescence ofthecoatedgrain(d)and cant rolealsointhecarbonatecrystal ourescent underthesameconditions. brous cements,arranged in uorescence light gure bareon lled with 26-05-2004, 15:21:03 P44_R_OK 57 TRIASSIC CARBONATEPLATFORMSOFTHEDOLOMITES PRODUCTION, RELATIVESEALEVELFLUCTUATIONSANDTHE SHAPING OFTHEDEPOSITIONALARCHITECTURE 57 -

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Volume n° 5 - from P37 to P54 P44 - P44 slope depositsoftheGran Vernèl Platform (From Caputo&Stefani,2003). early pinnacleshows up,downlapped bythenorthward progradingclinostratifi Figure 7.6-IntheRodadelMulòn,tilteddepositionalgeometryofadrowned Leader: M.Stefani checked forepifl thin-sections ofthedifferent microfacies were the presenceofdispersedorganic matter, uncovered pervasive recrystallization. However, inordertodetect primary precipitationmechanismsislimitedbythe In theMarmoladaMassif,understandingof et al.,1996). (Reitner, 1993;ReitnerandNeuweiler, 1995;Reitner acidic macromoleculeswithinorganic compounds mineralization relatedtotheinteractionoforganic cavities have underlinedtheimportanceoforgano- Accurate analyticalstudiesonmodernreef trapping ofdissolved Ca alternating thechemicalmicroenvironments orby either bybiochemicalprocesses,orindirectly, by 1999; Castanieretal.,Reitner1999), Buczynski, 1992;Neumeier, 1998;Folk andChavetz, inclusions, producedavivid green fl phreatic cements,richinfi cements exhibit intensive epifl as thepeloidalboundstones. The isopachousmarine characterizes thedifferent kindsofbioclastsaswell clinostratifi slip deformation. Diverging lines indicatetheradial compression andthenaffected byNeogenestrike and overthrusted oneuponeach otherbythe Alpine three independentcarbonateplatforms, telescoped Figure 7.7-TheMarmoladaMassifismadeupby cation dip(From Caputo etal.,1999). ed uorescence. Brightepifl (Chafetz, 1986;Chafetzand induce carbonateprecipitation particularly microbes,can 1998; 2000).Many organisms, growth (Russoetal.1997; Dolomites thanthemetazoan of carbonatebuildups ofthe important fortheformation precipitation canbemore Bio-induced carbonate cementation syndepositional Organic matterand volume. then 50%oftheplatformrock slope depositsformingmore but arealsoabundant inthe margin andupperslopefacies, major constituentoftheouter These cementsrepresentthe slope deposits(Figure7.2D). widely distributed inadjacent fragments ofthesecrustsare +2 onorganic templates. uorescence too. These too. uorescence n-rie brownish ne-grained uorescence. uorescence 26-05-2004, 15:17:58 P44_R_OK 59 Fe limit. Even late sparry calciteslackany detectable Fe andSrcontentsarealways beneaththedetection common Mgcontentintherangeof2-4mol%. The marine cements,pendentvadose cements, sharea micrites, bioclasts,thickradiaxialcrusts,isopachous independently fromtheoriginalcomposition.Peloidal margin andupperslopefacies issurprisinglyuniform The Mgcontentofthecalciteonplatform-top, Minor elementsincarbonates whole oftheplatformvolumes. upper slopefacies and,asredepositedfragments,the the cementcrusts,dominating syndepositional cementationduringthefast growth of signifi Organic matrix templatescouldhave playeda show anintensegreenfl bright beltsdonotfl bands, withabundant fi wide brightbeltsalternatingwithnarrow darkbrown In trasmittedlight,thecrustsarecharacterizedby crusts (“evinospongiae”) oftheupperslopefacies. The mostconspicuousfl 1989). in thelimestones(CerconeandPedone,1987;Klotz, fl intensity variation aremostprobablyrelatedto the dolomiteshow nofl On thecontrary, thelatediagenetic calcitesand re-opened byrecentkarstifi correspond toprimaryvoids inthewave-resistant outermargin,andprobably dei Fiacconi ataboutQ2750mthepresentdayglacierfront).Thecavities facies largelydominatestheoutermarginandupperslopesettings(Pan Figure 7.8-Field viewofacementcrustnetwork (“evinospongiae”).This uctuations of theresidualorganic matterpreserved +2 content. cant roleinsupportingthewidespread uoresce, whilethedarkbands uorescence (Figure7.5). uorescence occursincement cation. n-rie icuin. The inclusions. ne-grained ursec. Fluorescence uorescence. in situ TRIASSIC CARBONATEPLATFORMSOFTHEDOLOMITES themargin and PRODUCTION, RELATIVESEALEVELFLUCTUATIONSANDTHE SHAPING OFTHEDEPOSITIONALARCHITECTURE 2002045173), CoordinatoreNazionaleediUnità collo MM04093739),andCOFIN2002(protocollo by MIUR,throughtheprojectCOFIN2000(proto- by theUniversità degli StudidiFerrara(Ex60%)and introduction andintheDay4,5,6weresupported The stratigraphicresearchesillustratedinthegeneral Dolomites. vived signifi The Parco NaturaledelleDolomiti Ampezzane pro- Seceda coring. museum Suedtirolprovided substantialhelpforthe Museo diScienzeNaturalidell’Alto Adige –Natur- The Provincia Autonoma diBolzano/Bozeneil molada, Provincia Autonoma di Trento). Provinz Bozen;Cortina,Regione Veneto; andMar- Project CARRG(F. Dobiaco-Toblach, Autonome framework oftheNationalGeologicalMapping The fi through fi The editorwife(Daniela)supportedtheguideeffort (even atlateevening working hours). many thanksalsoforhiskindnessandfriendship Dottor Stefano Furìn(FerraraUniversity), deserving paging upoftheguide-bookwas vastly improved by editing andcommunicationhelp. The art-work and Dr EdoardoPerri(CalabriaUniversity) forfi for scientifi Hinnov (JohnsHopkinsUniversity) and forproviding several photographs;DrLinda eld researchwerepartiallycarriedoutinthe eld work help,love andunderstanding. c discussion; cant helpforthestudyofEastern for support,scientifi We thankProf. Alfonso Bosellini Acknowledgements burial cementation. taking placesubsequenttoadeep a slow but long-lastingfl phase was possiblyassociatedwith diagenetic late Dolomites. This with theNeogeneupliftingof oxidizing conditions,associated stage, andundercomparatively occurring atarelatively recent ion mobilizationphase,probably sparry calcitemayindicatean and thepresenceofMginlate homogenization. The lackofFe a widespreadchemical recrystallization, causing suggest adiffuse fi microscopic observations, These data,togetherwiththe c discussion c ne-grained uid fl uid gure ux, 59 +2

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Volume n° 5 - from P37 to P54 P44 - P44 Leader: M.Stefani B B 272 Bologna. orientale -S.G.I.GuideGeologicheregionali, 267- (eds.) GuidaallaGeologiadelSudalpinoCentro- il GruppodelSella B Stratigr., 86,779-794. margins, Dolomite Alps, Italy indicators ofMiddletoUpper Triassic buildup Dolomites, NorthernItaly. carbonate platforms:example from the Triassic ofthe Falzarego (Dolomiti centrali) - B Milano. (Dolomites) and tectonicsoftheM.Pore -M.Cernera area B Modena, 21,11-14. piattaforme carbonatiche. Acc. Naz.Sci.Lett. Arti di biologiche, radiazioniadattative edinamichadelle Sudalpino nelle piattaformecarbonatiche mesozoiche del - Russo RBAU01SBEY_004) CoordinatoreNazionaleFranco Operativa Alfonso BoselliniandFIRB(protocollo A References B Ladinian area (Dolomites,Italy)duringtheupper Anisian and Paleogeography oftheM.Cernera-Piz delCorvo B Roma. Rend. Cl.Sc.Fis.Mat.Nat.ser. 8vol. 9n.1,3 33 Dolomiti centro settentrionali. G A genetica. delle Dolomiti.Quadro geologico edinterpretazione (1977) - A and related breccias. origin andclassifi cation ofperitidaltepeestructures B Geology, 64,143-166. facies oftheDolomites,northernItaly leeward effects on Triassic carbonatebankmargin Aspetti stratigrafici relaivi allapresenza ditetrapodi VANZINI OSELLINI OSELLINI LENDINGER LENDINGER LENDINGER IDDLE OSELLINI OSELLINI IANNOLLA SSERETO SSERETO Depositi litorali raibliani nellazonadiPasso K.T. (1981)- M.,D . GeologicaRomana,21,217-234Roma. L’Industria Mineraria,28,367-402. R.,K R.,B A. (1982)- A. (1968)- A., D A., A. (1984)- . InCherchi A. &CorradiniC.(eds),Crisi Le mineralizzazioni Pb-Znnel Triassico P., M W.,P W.B & W. (1983)- . Riv. Ital.Paleont. Stratigr., 89,175-208 ENDALL RUSCA ALLA AL IETTO C AROW . In: A. CastellarinandG.B. Vai LENDINGER Sedimentology, 24,153-210. V P., P IN C.,G Paleogeologia pre anisica delle Geologia deiPassi circostanti C.G.S ECCHIA R.&G The basinalCipitBoulders: Progradation geometries of A., K A., Sedimentology, 32,1-24. RETO AETANI Anisian sedimentation Atti Acc. Naz. Lincei, Naz. AttiAcc. E.(1989)- , F.M., D . Ann. Univ.Ferrara . Ann. N.&R T . Riv. Ital.Paleont. RADENIGO C. (1977)- EPLER M.&J F. (1984)- OGHI . Sedimentary E Z A. (1978) A. Windward- G.(2000) ANCHE ADOUL Nature, V., F. F. B Albertiana, 13,25-36. boundary: Retrospective andnew constraints Dolomieu ConferenceonCarbonatePlatformsand Sciliar-Rosengarten/Catinaccio platform (1991a) - B Paleoclimatology, Paleoecology, 161,361-380. from theDolomites(northernItaly) correlations inMiddle Triassic pelagic carbonates magnetostratigraphic andlithostratigraphic K B 86(2), 415-527. sections from theSouthern Alps stratigraphic dataandcorrelations ofboundary defi nition ofthe Anisian/Ladinian boundary:New B Soc. Geol.It.,30,245-266. della DolomiaPrincipaledelle Alpi Venete. B Ortisei. Dolomitization, GuidebookExcursionvol. B,pg.30, Dolomieu ConferenceonCarbonatePlatformand Platform (Upper Triassic, Dolomites,Italy) B (N.S.), sez.IX,vol.V, 13,223-238. B 375. Latemàr (Southern Alps, Italy) data questiontheMilankovitch characteristics ofhe H. (1996)- B Milano. report Dolomites, NorthernItaly)aprogress Triassic Buchenstein beds(LivinallongoFormation, B 23, 3-9. Pratt Eds.)SpecialPublicationInt. Ass. Sediment., (C.L.V. Monty, D.W.J. Bosence,P.H. Bridge&B.R. “Carbonate Mud-Mounds. Their originandevolution” the originandevolution ofcarbonatemud-mounds B Soc. Geol.It.,273-278. A., Vai G.B.eds.).Guidegeologiche regionali della Geologia delSudalpinocentro-orientale(Castellarin geologia delpassoFalzarego B 20, 5-27. theme ofamarginal marineevaporite RACK OSENCE OSELLINI OSELLINI OSELLINI OSELLINI RANDNER RACK RACK RACK RACK ENTER . Riv. Ital.Paleont. Stratigr., 106,283-292 P. &M P. &R P. &R P., S P., M J.(2000)- D.W.J. &B A. & N & A. M A., H & A. H & A. R.,F The northernmargin oftheSchlern/ UNDIL CHLAGER Biostratigraphic andradiometric age IEBER IEBER UTTONI ASETTI LÜGEL R.,O ARDIE ARDIE The SecedadrillholeintheMiddle H.(1994)- H.(1993)- W.,S RIDGE ERI E.,K D.&N G.(2000). L. A. (1988)- L. A. (1973)- BERLI C.(1991)- P.H. (1995)- TEFANI F., M OCH . Eclog.Geol.Helvet., The Anisian/Ladinian . Geology, 24,371- ERI R.& Y M.,M EIER Towards abetter . Paleogeography, C.(1982)- . inGuidaalla . Sedimentology, High-resolution M.,&R Facies ecicli Depositional A review of AURER The Sella OSE 26-05-2004, 15:18:07 Mem. L.A. IEBER F.& . In La . . .

P44_R_OK 61 P B Westlichen Dolomiten C Geol., 51(1),63-77. Jadoul, M.SellaeM.I.Spallaeds.).Mem.Scienze Volume Alpine GeologicalStudies”(G.Gosso,F. Marmolada Group (Dolomites,Italy) C Alpi Meridionaliorientali. (1998) - B 279-296. Mahlknecht Cliff, Western Dolomites) indicator ofthesource area (Middle Triassic: (1991b) - B Ortisei. Dolomitization, GuidebookExcursionvol. A, pg.61, C Triassic oftheDolomites palinspastic restoration: examples from theMiddle polynucleated carbonateplatformsthrough C Geodynamics,30, 251-274. evolution oftheSouthernEastern Alps. B Riv. It.Paleont. Strat.,105(1),37-78Milano. Section andPoint forthebaseofCarnianstage (Dolomites Italy):acandidateGlobalStratotype (1999) - E. &D C Berlin. E. Riding&S.M Awramik Eds.),32-39Springer, carbonate minerals J.P. (1999)- C Subalpino. - S., M D., G C 165-187. sul GruppodelBuffaure B 30, 203-231 Tulsa. Toomey Ed.)Soc.Econ.Paleont. Min.Spec.Publ., Austria of theNorthernLimestones Alps nearInnsbruck, in theMiddle Triassic (LadinianandCordevolian) OSENATO ASTELLARIN ASTELLARIN ASTELLARIN ASTANIER APUTO ontractional andtrascurrent tectonicsinthe APUTO RUSCA ROGLIO RANDNER RANDNER RANDNER Paleogeografi a ladino-carnicaemetallogenesi del ASTRADREA IANOLLA E . In“EuropeanFossil ReefsModels”(D.F. R.&S R.,S C.,G L L La tettonicadelleDolomitinelquadro delle The Prati diStuores/Stuores Wiesen Section R.,R UCA R.,F R. R.&R S.,L ORIGA Microfacies ofcarbonateslopeboulders: Mem.Soc.Geol.It.,22,65-82Padova. A., S A., R A., A. &C ET P., L A. (1977)- AETANI Bacterial roles intheprecipitation of TEFANI

EICHICHI C.,C A., M A., AL E LÜGEL M TEFANI ESCH . (inprep.)- ELLI OSSI AGHI . In“Microbialsediments”(R. M.,J ETAYER M.&D ANTELLI IRILLI (1:25.000). L.,P P.L., S E.&S W. (1981)- IETTO M.,R G.F., L M.(2003) . Mem.ScienzeGeol., Dati geologici epetrografici . Miner. Petrogr. Acta, 21, ADOUL S.,D Mem.Soc.Geol.It.,53, -L P., M L.(2000) ICOTTI EVREL ETTORI IMBOLI Geologische Karteder AL ENOWBARI F. & V E TRIASSIC CARBONATEPLATFORMSOFTHEDOLOMITES OWRIE Z P UTTONI V.C & G.&P Reef development ANCHE R.,&R G.,S IAZ Understanding in“Special W.,M -Neo-Alpine G.B.(1999) . Facies, 25, IEL PRODUCTION, RELATIVESEALEVELFLUCTUATIONSANDTHE G.,N -D V.,D OMMAVILLA Journal of G.(1981) ANTELLI ARYAN ERTHUISOT OGHI ERI ANFRIN I B G., C., B. L. ARI .

SHAPING OFTHEDEPOSITIONALARCHITECTURE D the Dolomites(Italy). D 85(1), 105-126Basel. inversion intheSouthern Alps. extensional tectonics,stratigraphy and Alpine & R D Dolomites. A reappraisal ofthe Anisian stratigraphy inthe section (Valdaora-Olang, Pusteria Valley, Italy). C 133-143 Padova. D 331-347 Basel. area (Julian Alps, Italy). Carnian stratigraphy intheRaibl/Cave delPredil C Petrol., 56,812-817. bacterially inducedprecipitation ofcalcite V P. P. D 11, 415-452Innsbruck. (Italian Dolomites) and pelagic sedimentsoftheLivinallongoFormation paleogeographical interpretation ofvolcanoclastic C Petrol., 57,780-782. and analyticalsource ofobservationerror (photoluminescence) ofcarbonaterocks: Instrumental mesoalpine tectonicsintheSouthern Alps. D Ann. Univ. Ferrara,Sci. Terra, 5(suppl.),41-48. al limiteLadinico-Carnico(Sudalpinoorientale). C rocks stratigrafi c repetition ofchemical andsiliciclastic D Geology, 9,181-193. Italy) (Southern Alps-Northern D 78(2), 335-350Basel. Dolomites: ramp-fl at systems C 277-293. induced lithifi cation ofmicrobial mats D Mem. Soc.Geol.It.,47,135-155Padova. Sequence Stratigraphy andBiochronostratigraphy. Carbonate PlatformintheDolomites(Italy): AIL ROS HAFETZ HAFETZ ERCONE ECIL E OGLIONI OGLIONI OGLIONI OGLIONI E E E E Z Z Z Z Z AND OGHI P. R.(1993)- ANCHE P. &H ANCHE . Geology, 18,533-536. ANCHE C.B.(1990)- ANCHE ANCHE S H.S.&B H.S.(1986)- K.R.&P G.(1995)- C.&B C.(1992)- C.(1987)- C.(1985)- IORPAES Ecl.Geol.Helv., 85(1),127-143, Basel. V.G & V.,G V.,G V.,G V.,F OUEL IANOLLA C.(1992)- IANOLLA OSELLINI IANOLLA IANOLLA RANZIN EDONE . Geol.Palaont. Mitt.Innsbruck, Triassic sequencestratigraphy in UCZYNSKI P. (1983)- Relationships betweenMesozoic Mem.Sc.Geol.,5,XLV, 1-27. A Middle Triassic Back stepping Marine peloids:aproduct of Tectonics oftheDolomites P., M V.A. (1987)- A., G A., P., M A. (1987)- Eclog.Geol.Helvet., 93, P. &R Paleoclimate controls on P. (1995)- The overthrusts inthe C.(1992)- . Eclog.Geol.Helvet., IETTO . JournalofStructural Eclog.Geol.Helvet., ANFRIN IANOLLA The PizdaPeres OGHI P., S Repartition and Litostratigrafi a S.,M Eoalpine and G.(2000)- Fluorescence . Palaios, 7, P., M IORPAES Bacterially . J.Sed. . J.Sed. IETTO Geol. IETTO C.& 61 P. P.

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Volume n° 5 - from P37 to P54 P44 - P44 Leader: M.Stefani F Tulsa. and J.GolonkaEds.)SEPMSpecialPublication,72 “Phanerozoic reefpatterns”(W. Kiessling,E.Flügel F 542. and theCarnian of theCivettabuildup. EvolutionduringtheLadinian F and hydrology American Bullettin,102,535-562. Triassic platformcarbonates of stratigraphic forcing: Examplesfrom the Alpine changes, cyclestacking patternsand thehierarchy (1990) - F Americana, 54,191-200. (Anisian) intheItalianDolomites in carbonatesequencesoftheMiddle Triassic building communities andtherole ofcnidarians G 685-699. and latediagenetic overprint (Southern Alps): documentationofearlylithifi cation - E Rund., 76,735-754Stuttgart. G Amsterdam. buildups intheDolomites(Italy) - G Special Publication,60,723-751. Sequence StratigraphyofEuropeanBasinsSEPM and D.Ulmer-Scholle (Eds.):Mesozoic-Cenozoic de Gracianscky, J.Hardenbol, T. Jacquin,P.R. Vail Defi nition ofsequencesandbasinevolution Triassic SequenceStratigraphy intheSouthern Alps. F Sedimentology, 46,893-912. of theLatemar(Middle Triassic, northernItaly) of anisolatedcarbonateplatform:tracing thecycles Z G 104 (3),381-390. paleoclimatic indicator? Triassic amberfrom theDolomites(NorthernItaly). A F and S.M Awramik Eds.),40-49Springer, Berlin. precipitates induced microscale andnanoscalecarbonate ORD OLK OIS OIS RISIA LÜGEL UHLKE GENHOFF Nature andevolution ofMiddle Triassic carbonate OLDHAMMER IANOLLA IANOLLA AETANI Evinosponges inthe Triassic EsinoLimestone E.&G E.&G R.L.&C D.& W -B E.(2002)- R.&G M.,F RUNI S.O.,P P., R P., D Depositional cycles,compositesealevel . In“Microbialsediments”(R.E.Riding AETANI AETANI S.,J ILLIAMS R.K.,D . UnwinHyman,London,601pp. OIS AGAZZI ROTSCH E . Riv. Ital.Paleont. Stratigr., 86,469- Z E.,J HAVETZ M.(1984)- M.(1981)- ADOUL ANCHE P. (1989)- ETERHÄNSEL E.&R J.(1999)- ADOUL UNN H.S.(1999)- Triassic reef patterns Riv. Ital.Paleont. Stratigr., F. & W V. &M P.A. &H F. &N . GeologicalSocietyof OGHI . Sedimentology, 36, Karst geomorphology A., B A., The recovery ofreef- The northernmargin , 44n.1-2,25-57 . Palaeontographica G.(1998)- Facies architecture EISSERT IETTO ICORA ECHSTADT P. (1998)- ARDIE H.(1989) Bacterially A. (1981) A. . In:P.C. L.A. Upper . In T., . di Fassa (DolomitiOccidentali):sedimentologia e K Carbonate Strata, AAPG Memoir, 63,301-306 Tulsa. Harris P.M. (1995)UnconformitiesandPorosityin Acid Oil-Field Karst G K Paleont. Teil I,897-904. Muschelkalks (Trias) inHessen Untersuchungen ankalkdunnschliffen desUnteren K 777-794 Oxford. slope angleandsedimentfabric M Beilage Bd.,59B,357-408. kalkalpiner Sedimente H Eds), 245-268SpringerBerlin. “Reef Diagenesis”(J.H.SchroederandB.Purser Triassic Wetterstein ReefsoftheBavarian Alps L Erdwissenschaftliche Schriftenreihe.,4,37-75. Wissenschaften,der Oesterreichische Akademie (ed.) BeiträgezurBiostratigraphieder Tethys-Trias. im alpin-mediterranen Unterkarn K 41, 15-26. on SteepSlopes(Triassic, Dolomites,Italy). K Earth Sciences(Geol.Rundsch.),90,813-830. Carnian carbonateplatforms(Dolomites,Italy). and synsedimentarytectonicsonlateLadinian-early L Univ. Ferrara,Sci. Terra, 3,1-26. coralligena delSella nelleDolomitiOccidentali L Rovereto. H 471. (Southern Alps, Italy)-Comment the Milankovitch characteristics oftheLatemarcycles Biostratigraphic andradiometric age dataquestion H 99, 24051-24074. Mesozoic timeScale monti tra Isarco ePiave J., K 261-283. platform (Southern Alps, Italy). compositional analysisofa Triassic carbonate EUCHS EONARDI EONARDI EIM EIM ENTER EIM ILL ENRICH ARDIE RADSTEIN RYSTYN LOTZ ASETTI VAN C.A.(1995)- L.&S L.&B L.&S W. (1998)- V , L.A.,&H K.(1928)- J.A.M.(1990)- D.&N H.&Z L.(1979)- EEN P. & R & P. P. (Ed.)(1967)- F.M., A P., T RANDNER CHLAGER CHLAGER ANKL ERI HIERRY GTERBERG H OSSI . JournalofGeophysicalresearch, C.(1980)- H.(1986)- R.(2001)- 2 W. (1999)- in:BuddD.A.,Saller A.H. & S-Related Porosity andSulfuric . N.Jb. Min.Geol.Paleont., D.(1957)- W. (2001)- .(Edizioni Manfrini)1019pp. Eine neueZonengliederung J. Beitrage zurLithogenesis Carbonate platformfl INNOV Fluoreszenzmikroskopische Le Dolomiti:Geologia dei F.P., O AND , L.A.,(1997)- Sediment.Geol.,139, H . Sedimentology, 37, Facies interfi Diagenesis ofUpper . ZentrablattGeol. , L’Anisico della Val UANG GG Automicrite Facies Geology . In:Zapfe,H. J.G.,H Z.(1994)- La scogliera Quantitative , 25,470- ARDENBOL ngering 26-05-2004, 15:18:12 Facies, anks: Int.J. . Ann. . In A

P44_R_OK 63 M Ortisei. on CarbonatePlatformsandDolomitizationabs.163 Triassic, Dolomite Alps, Italy) boulders from S.CassianoFormation (Upper (1991) - M France, 166(5),539-563. Tethys Realm. A preliminary report. Middle Triassic ammonoidstandard scaleinthe M Italy) Southern Alps, Triassic interplatformbasins(Buchenstein Formation, in sedimentcompositionandbeddingMiddle M Journal Paleont., 69,416-431. Upper Triassic Northeastern Dolomites(Italy) and diagenesis ofcalcifi M Carnia (Italy) marine UpperPermian successionofDolomitesand supradetachment (?)basin:thecontinentaltoshallow- M 7, 1-19. paleogeografi M Earth Sci.,92,593-609. succession (Seceda,Dolomites,Southern Alps) of calciturbiditesinaMiddle Triassic basinal Quantifi M 132 pp. of theSouthern Alps M Italy). (Southern Alps, carbonate platformsinthe Western Dolomites M Stratigr., 103,39-52. the Triassic oftheSouthern Alps) implications forsequencestratigraphic modelsof sourrounding theSellaMassif(Dolomites,Italy): biostratigraphy oftheSanCassiano Formation delle faunead Ammonoidi allimiteLadinico/Carnico M Stratigr., 100,493-510. Cassiano Fm.,Dolomites,Italy). Upper Triassic strata of Tamarin section(San M Sc. Geol.,50,213-237,Padova. medio-triassiche delleDolomitiOccidentali. anisica nellanascitaedevoluzione dellepiattaforme ASTANDREA ASSARI ASETTI IETTO IETTO AURER AURER AURER AURER ASTANDREA ASTANDREA ASTANDREA P. & M & P. M & P. cation ofinputandcompositionalvariations , F., R F. & S & F. F. (2003)- F. (2000)- D.& T F. & N & F. Microfacies andgeochemistry oftheCipit A. &R N A., N A., A. (1994)- a. . SedimentaryGeology, 110,181-221. EIJMER CHLAGER Ann. Univ. Ferrara (N.S.),sez.IX, ANFRIN ANFRIN ROMBETTA ERI ERI Bedding rhythmsin Triassic basins ERI J.J.G.&S , Sedimentology, 50,1-22. Growth modeofMiddle Triassic C.&R USSO C.(1997)- . PhD-thesisUniv. Amsterdam, Sed.Geol.,134,275-286. S.(1995a)- C.,R S.(1995b)- W. (2003)- ed Demosponges from the F. (1995)- G.L.(1998)- Carnian conodontsfrom USSO USSO . DolomieuConference CHLAGER F. (1997)- TRIASSIC CARBONATEPLATFORMSOFTHEDOLOMITES Riv. Ital.Paleont. . Riv. Ital.Paleont. F. & L & F. Lateral variations A highresolution Bull.Soc.Geol. The infi La successione Microstructure , W. (2003)- PRODUCTION, RELATIVESEALEVELFLUCTUATIONSANDTHE AGHI Conodont L’eredità ll ofa Mem. . Int.J. G.F. .

SHAPING OFTHEDEPOSITIONALARCHITECTURE M Alpen und Venetien. Beiträge zurBildungsgeschichte der P 1-183. (sédiments intertidaux) dans lacimentationprécoce desbeachrocks (2003) - N (submitted). chronology (2003) - E M 5 (suppl.),37-40. Carnico nelSudalpinoorientale (eds.): Verso unadefi (Sudalpino, Italia).In:C.Broglio Loriga&C.Neri P AAPG Memoir, 63,77-101 Tulsa. Unconformities andPorosityinCarbonateStrata Rocks Origin ofMacroscopic SolutionPorosity inCarbonate M clock. Carbonates: synchronizing radio-isotopic andorbital M sedimentation verifi Triassic volcaniclastics:timescalecalibration and F. (1996)- R Mineralogica Italiana,1,21-22. (2003) - R (Dolomites, Italy) in theshallow-marineLatemarcarbonatebuildup V. (2001)- N Soc. Geol.It.,53,417-463. permiana superiore etriassicadelleDolomiti cronostratigrafi R 3-40. Reef, Australia): formationandconcepts metazoan faciesfrom Lizard Island(Great Barrir M Northern Italy. of strike-slip faultsinthedolomitesofSellaGroup, R analysis. ALMER RETO GENHOFF IEBER EITNER AGAZZI AGAZZI EUMEIER ERI UTTONI UNDIL UNDIL OLLEMA OJSISOVICS cation oftuningparameters forcarbonate C.&S 552pp.Hölder, Wien. Terra Nova, 15(2),81-87. N.,H in: BuddD.A.,Saller A.H., HarrisP.M. (1995) H.(2003)- A.N. (1995)- R.,Z R.,B J.(1993)- E.,R E.,F G.N Thermochimica 43-54. 404(1-2), Acta, P.N. & A S.,M U.(1998)- L’Ambra TriassicaDolomiti. delle Classifi . Palaeogeogr. Palaeoclimatol. Palaeoecol., Middle Triassic orbitalsignature recorded E.(1879)- Integratedboundary Anisian/Ladinian INNOV High resolution U-PbdatingofMiddle RACK . EarthPlanet.Sci.Lett.,141,137-151. J.Struct.Geol.,21,273-292. OGHI ca esequenzialedell’evoluzione ÜHLKE EDELE ICORA EIER cation ofamberbasedonthermal . Geology, 29(12),1123-1126. L. A., H NTONELLINI P., M TEFANI G.,G M.,O P., G R.,B Cyclicities in Triassic Platform A., B A., Le role del’activitémicrobienne nizione delLimiteLadinico- Modern crypticmicrobialite/ . Terre &Environnement, 12, Geochemical Modelsforthe Die Dolomitriffe vonSüdtirol EIER M.(1998)- IARETTA ARDIE BERLI IANOLLA M.,R ECHSTADT M.(1999)- RACK F., P . Ann. Univ.Ferrara, . Ann. L. A. &D A. & G & A. P. & K & P. IEBER P. & R & P. T., B T., ETERHÄNSEL H.&O Development . Facies, 29, IANOLLA ENT E RACK Z OGHI Rivista . Mem. Sintesi D.V. ANCHE BERLI A., G. P., 63 P. P.

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Volume n° 5 - from P37 to P54 P44 - P44 Leader: M.Stefani R 327 pp.Gotha. Cassian undderSeisseralpen inSüdtirol Beschreibung derUmgebung vonPredazzo, Sanct R 235-236. book, (Greece) Abstract 2002, Athens Palynology Conference, August 29-September2, the Southern Alps (Italy) Paleobotanical features ofUpper Triassic amberin R 89 Göttingen. F. Gunkel Eds.)Göttinger. Arb. Geol.Paläont., 2,85- Evolution. Res.Report” (J.Reitner, F. Neuweilerand Regional ControlsonBiogenicSedimentation.I.Reef (Cervantes Western,Australia) framework ofcalcifi (1996) - R Northeastern Dolomites) the Alpe diSpecie(Seelandalpe)fauna(Carnian, (1991) - R R Awramik, Eds.),149-160Springer, Berlin. In “Microbialsediments”(R.E.RidingandS.M biogeochemical patternsincrypticmicrobialites W R maggio 2003 Abstract book,45. Giornate diPaleontologia 2003, Alessandria 22-25 delle Dolomiti - R Coordinators.) Facies, 32,4-17. Carbonate Buildups”(J.ReitnerandF. Neuweiler, Mounds: aPolygeneticSpectrumofFine-grained controlling factors ofrigidmicritebuildups R (Dolomites, Italy) Triassic platforms. The Marmoladacasehistory syndepositional cements:akey componentofMiddle C. (2000)- piattaforme triassiche delleDolomiti(Italia) - R Soc. Geol.It.,53,479-488. R Giornale diGeologia,60(spec.Issue),108-115. ECOS VII” (M.C.Perri andC.SpalettaEds.). Massif. -In“Southern Alps Field Trip Guidebook Cipit boulders from thesurroundings oftheSella EITNER USSO USSO USSO OGHI OGHI ICHTHOFEN EITNER EITNER USSO USSO Microrganismi fossiliinclusinell’ambra triassica ORHEIDE Evoluzione degli organismi costruttori nelle G.,G G.,C F., M M F., M F., F., N F., N F., J., T J.,P J.&N Lake Thetis domal microbialites -acomplex G. Depositional anddiagenetic historyof

ASTRANDREA ERI ERI OPPELLOTTI ASTRANDREA AUL AND ASTRANDREA IANOLLA VON EUWEILER :SocietàPaleontologica Italiana- C.,M HIEL C.,M Carbonate faciesdominatedby . Facies, 42,211-226. J., A G F. (1860)- V.,Z e biofi ed AUTRET P. & R & P. ASTRANDREA F. (1995)- A. & N & A. ASTRANDREA RP O.&R . Facies, 25,187-210. . 6thEuropeanPaleobotany- A., S A., A. &N G.&H ANKL P. (1999)- ls n organomicrites and lms H.M AGAZZI ERI TEFANI . In“Globaland Supposed principal A. &L AGAZZI C.(1998a)- A. & B & A. AUSE ERI E.(2002)- Geognostische M.&N C.(1998b) . PerthesEd., Organic and ICHAELIS -R E.(2003) EITNER . In“Mud AGHI . Mem. ARACCA G.F. W. W. D. The ERI :

S Wachstumsgefuge. S 28, 181-256. comunities afterthePermian/Triassic crisis. of theNorthernDolomites(Italy): The recovery ofreef F V Beiträge zurNaturkundeSerieB,97,1-10. Schlernplateau Schichten amSchlern. U Akademie Wissenschaften, 2,207-222. Erdwissenschaftlichen Kommissionen, Österreichische Cassian (Dolomiten/Italien) Ammonitenfauna derCassianerSchichten von R Massif, NorthernItaly). the CipitBoulders from PuntaGrohman (SassoPiatto platform margins oftheDolomites. A casehistory: A. (1997)- U Naturkunde, SerieB,217,1-55. der Dolomiten(Italien) (Ammonoidea) ausdemUnterkarn(Obertrias) S (Dolomiti centrali) e tettonicaalpinanelGruppoMarmolada–Costabella Z du Nord). Alpes CarniquesOccidentalesetdesDolomites(Italie conodontes del’AnisiensuperieuretduLadiniendes U Paleont. Lombarde,1,360pp.Milan. superieur desenvirons d’EsinoenLombardie. ou descriptiondesfossilesappartenantsaudepot the TethysRealm Schrift. Erdwiss.Komm. Österr. Ak. Wiss., 7-17 S Italiana, 53,479-488. delle Dolomiti comunità costruttricidellepiattaformetriassiche V 297-352. Meridionali). IIParte. paleostrutturale dell’area Dolomitico-Cadorina(Alpi una revisione. Ricostruzionepaleogeografi V 85-125. Meridionali). IParte. paleostrutturale dell’area Dolomitico-Cadorina(Alpi una revisione. Ricostruzionepaleogeografi TOPPANI TEFANI LÜGEL ENOWBARI CHMIDEGG APFE IEL IEL USSO RLICHS RIELYNCK RLICHS RLICHS G.(1979b)- G.(1979a)- H.(1983)- F., N E.(1993)- M.&C , M.(1974)- M.& T , M.(1994)- A. (1858)- Geobios,17(2),177-199Lyon. B.(1984)- -D O.(1928)- ERI The mud-moundnature oftheCassian ARYAN . MemoriedellaSocietàGeologica C.&M APUTO

(IGCP Proj. 4) Das Forschungsprojekt Triassic of Jb. Geol.Bundesanstalt,78,1-52. ICHY . Mem.Soc.Geol.It.,53,263-293. Anisian (Middle Triassic) buildups B.,Z R.(1998)- Riv. Ital.Paleont. Strat.,85(1), Riv. Ital.Paleont. Strat.,85(2), G.(2000)- Facies, 36,25-36. ASTRANDREA , StuttgarterBeiträgefür Les petrifi ÜHLKE Revision desgisements a Trachyceras Laube1896 Litostratigrafi Litostratigrafi Zur Stratigraphie und R.,B . Abschlussbericht. , Schriftenreihe Stratigrafi Uber geregelte ctos d’Esino cations A. (1998)- Zum Alter der Zum Alter ECHSTÄDT a ladinica: a a ladinica: a Stuttgarter a triassica 26-05-2004, 15:18:17 Facies, c e ca c e ca T. & & T. . Le Chronostratigraphic scheme of the Permo-Triassic of the Dolomites. For discussion see the guide introduction. 1) Continental red beds; 2) Coastalmarine; locally tidal fl at and coastal plain facies; 3) Low relief carbonate platforms; 4) High relief carbonate platforms; 5) Terrigenous- carbonate basinal facies; 6) Dis-anoxic basinal facies; 7) Cherty basinal limestone; 8) Basic volcanites, mainly subacqueous; 9) Basinal volcanoclastites; 10) Evaporites.

AVG Arenarie di Val Gardena; Be Bellerophon Fm (evaporitic carbonate); Bc Bellerophon Fm (marine carbonate); W Werfen Fm; DSei Lower Serla Dm; CgPP Piz da Peres Cg; G Gracilis Fm; DR M.te Rite Fm; CgV Voltago Cg; A Agordo Fm; DSes Upper Serla Dm; D Dont Fm; CgR Richthofen Cg; Am Ambata Fm; Mb Morbiac Fm; C Contrin Fm; M Moena Fm; Lvp Livinallongo/Buchenstein Fm Plattenkalke Mb; Lvk-b Livinallongo Fm Knollenkalke -Bänderkalke Mbs; DS Sciliar/Schlern Fm (including Marmolada and Latemar Lm); AZ Zoppè Sand.; Aq Acquatona Fm; V: Volcanites and Caotico; Eterogeneo Fm; F Fernazza Fm; Wg La Valle/Wengen Fm; MG Megabreccia di Passo Gardena; SC San Cassiano Fm; DC Dolomia Cassiana; Hk Heiligkreuz-Dürrenstein Fm; R Raibl Fm; DP Dolomia Principale/Hauptdolomite; CD Dachstein Lm.

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