Faciès and biostratigraphy of the Late Carboniferous/Early Permian sedimentary séquence in the Carnic Alps (Austria/ltaly)

Karl KRAINER Institute for Geology and Paleontology, University of Innsbruck, Innrain 52, A-6020 Innsbruck (Austria) Karl.Krainer® uibk.ac.at

Vladimir DAVYDOV Department of Geosciences, Boise State University, 1910 University Drive, Boise, Idaho 83725 (USA) [email protected]

In memoriam Franz Kahler (1900-1996)

Krainer K. & Davydov V. 1998. — Faciès and biostratigraphy of the Late Carboniferous/Early Permian sedimentary séquence in the Carnic Alps (Austria/ltaly), in Crasquin-Soleau S., Izart A., Vaslet D. & De Wever P. (eds), Peri-Tethys: stratigraphie cor- relations 2, Geodiversitas 20 (4) : 643-662.

ABSTRACT The Late Catbonifetous/Early Permian séquence in the Carnic Alps (Austria/ltaly) is a more than 2000 m thick succession of shallow matine clastic and carbonate sedimentaty rocks. The succession unconformably overlies rhe folded Variscan basement and is divided into Bombaso Fotmation, Auernig Group, Rartendotf Group and Trogkofel Group. Auernig Group and Rattendorf Group are charactetized by clastic-catbonate cycles related to Gondwana glacioeustatic sea level changes. Catbonates contain abundant fossils throughout the séquence, biostratigtaphy is mainly based on fusulinids. Fine-grained clastic intervais contain abundant plant fossils, allowing a close corrélation with fluvial succession of the Eastern Alps KEYWORDS (Stangnock Fotmation of the Gutktal Nappe). Fusulinids of the Carnic Alps Peri-Tethys, Late Carboniferous, show high similarity wirh those of the Russian Platfotm, Donets Basin and Early Permian, Ptedonets Trough, Southern Urals and particulatly with Central Asia. Carnic Alps, faciès, Uppermost Moscovian, Kasimovian, Gzhelian, lowermost Asselian, late biostratigraphy, Asselian, Sakmarian and Artinskian équivalents ate established and précise fusulinids, corrélation with sttatotype légions have been completed. Fusulinid, cono- conodonts, plant fossils. dont and plant fossil data well coirespond with each othet.

GEODIVERSITAS • 1998 • 20(4) 643 Krainer K. & Davydov V.

RÉSUMÉ Faciès et biostratigraphie de la séquence sédimentaire Carbonifère supérieur! Permien inférieur dans les Alpes carniques (Autriche/Italie). La séquence Carbonifère supérieur/Permien inférieur dans les Alpes carniques (Autriche/Italie) est constituée de plus de 2000 m de roches élastiques et car- bonatées marines peu profondes. La succession recouvre en discordance le socle varisque plissé et est subdivisée en la Formation Bombaso, les Groupes Auernig, Rattendorf et Trogkofel. Les Groupes Auernig et Ratendorf sont caractérisés par des cycles élastiques et carbonates produits par des variations glacio-eustatiques (Gondwana). Les carbonates contiennent des fossiles abon­ dants tout au long de la séquence, la biostratigraphie étant principalement fondée sur les fusulines. Les intervalles élastiques fins contiennent des fossiles de plantes abondants, permettant une corrélation étroite avec la succession fluviatile des Alpes orientales (Formation Stangnock de la nappe de Gurktal). Les fusulines des Alpes carniques montrent de grande similarité avec celles de MOTS CLÉS la plate-forme russe, bassins du Donetz et Predonetz, Oural du Sud et parti­ Péri-Téthys, Carbonifère supérieur, culièrement Asie centrale. Des équivalents de la partie supérieure du Permien inférieur, Moscovien, Kasimovien, Gzhélien, de la partie inférieure de l'Assélien, de Alpes carniques, l'Assélien supérieur, du Sakmarien et de l'Artinskien ont pu être établis et faciès, biostratigraphie, une corrélation précise avec les régions stratotypes a été accomplie. Les don­ fusulines, nées sur les fusulines, conodontes et plantes fossiles correspondent bien les conodontes, plantes fossiles. unes aux autres.

INTRODUCTION 1981; Kahler 1983, 1985, 1986, 1989; Fritz et al. 1990; Venturini 1990; Krainer 1992, 1993 In the Carnic Alps (southern Austria/northern and Forke 1995 for further informations and Italy) the folded Variscan basement is unconfor- références). The présent paper gives a summary mably overlain by a thick succession of shallow of the Late Carboniferous/Early Permian séquen­ marine clastic and carbonate rocks of the Late ce with spécial emphasis on the biostratigraphy Carboniferous Bombaso Formation and Auernig and corrélation with other régions. Group and the Early Permian Rattendorf and Trogkofel Group (Fig. 1). Thèse rocks were deposited in discrète basins formed by block and FACIES wrench faulting subséquent to the Variscan oro­ genic phase with its climax during the BOMBASO FORMATION Westphalian. Classic outcrops occur in the cen­ The Bombaso Formation consists of poorly sort- tral Camic Alps along the Austrian/Italian border ed immature breccias and conglomérâtes which (Fig. 2). Sedimentary rocks of ail formations, are either predominantly composed of radiola- particularly the carbonates, contain abundant rian chert and volcanic clasts (Pramollo Member) fossils providing the basis for biostratigraphic or of Silurian to Devonian carbonate clasts subdivision and corrélation. Biostratigraphy of (Malinfier Horizon). Thickness ranges from a the Late Paleozoic séquence in the Carnic Alps is few meters up to about 200 meters. The clasts mainly based on fusulinids, although plant fossils are derived from the Variscan basement of the and conodonts are of importance too. During uplifted Paleocarnic Chain. The succession of the last décades major progress has been achieved the Bombaso Formation generally shows a fining concerning sedimentology, paleontology and bio­ upward trend. Bioclasts of brachiopods, crinoids stratigraphy of this séquence (see Flugel 1980 a-b, and fusulinids are rarely présent indicating

644 GEODIVERSITAS • 1998 • 20(4) Waidegger Hbhe 1961 + Leitenkogel 1845 +

Triassic of the Gartnerkofel-Massif

Rattendorf Group and Trogkofel Group

Bombaso Formation and Auernig Group

ON

FIG. 1. — Map showing the distribution of Late Carboniferous and Early Permian sedimentary rocks in the Carnic Alps (Austria/ltaly). Krainer K. & Davydov V.

crossbedded sandstone (shoreface), bioturbated Goggau Limestone _I (130 m) and locally fossiliferous siltstones and shales (off­

3KIA N LLÛ- z Tressdorf Limestone shore) and fossiliferous limestones containing < (10 m) ARTIN ! calcareous algae {Anthracoporella spectabilis, GRO U Trogkofel Limestone Archaeolithopbyllum missouriense, Epimastopora, s (400 m) TROGK O RIA N Eugonophyllum), fusulinids, small foraminifers, te Upper Pseudoschwagerina LU Limestone echinoderms, bryozoans, Tubiphytes, sphincto-

SAKM A (Zweikofel Formation; 170 m) 0. zoans, solitary corals and others. Massive lime­ Grenzland Formation ASSELIAN (125 m) stones represent algal mounds {Anthracoporella

Lower Pseudoschwagerina GROU P mounds; Krainer 1995), in the Meledis tn Limestone (Schulterkofel Formation; 160 m) RATTENDOR F Formation small mounds formed of auloporid GIA N corals are présent (Fliigel & Krainer 1992). In o Camizza Formation (120 m) the upper part of the Auernig Group (Corona-, CL oc Auernig- and Carnizza Formations) thèse lithofa­

ORENBU R Auernig Formation UJ (250 m)

RO U cies types form prominent clastic-carbonate LL

Corona Formation G regressive-transgressive cycles ("Auernig cyclo- (300 m) LIA N

z MI G themes") with thicknesses of 10-40 m (Fig. 3). O Pizzul Formation Within thèse cycles conglomérâtes formed

GZH E (300 m) m UER I during relative sea-level lowstands and fossilife­ a: Meledis Formation rous limestone was deposited during periods of KASIMOVIAN (120 m) < relative sea-level highstands. The formation of o UPPERMOST Bombaso Formation MOSCOVIAN thèse cycles is related to eustatic sea-level changes caused by Gondwanan glaciation (Massari & Variscan Basement Venturini 1990; Krainer 1992, 1995).

FIG. 2. — Stratigraphy of the Late Carboniferous and Early Permian strata in the Carnic Alps. RATTENDORF GROUP The Rattendorf Group comprises a succession of shallow marine sédiments of nearshore, inner déposition in a marine environment. Thèse bree- shelf and outer shelf environments. The succes­ cias and conglomérâtes are interpreted as mass sion is divided into Lower Pseudoschwagerina gravity flow deposits primarily deposited on fan Limestone (LPL), Grenzland Formation and deltas, partly subaerially, partly submarine. Upper Pseudoschwagerina Limestone (UPL) (Fig. 2). AUERNIG GROUP The LPL is composed of three depositional The Bombaso Formation is overlain by the cycles consisting of shallow marine limestones Auernig Group, which is up to 1.200 m thick and thin intervais of clastic sédiments (Fig. 4). and composed of Meledis-, Pizzul-, Corona-, Clastic intervais form the base of the depositio­ Auernig- and Carnizza Formations according to nal succession and were deposited during relative Selli (1963) (Fig. 2). The succession consists of sea-level lowstands. During transgression well cyclic clastic and carbonate rocks of a shallow bedded fossiliferous limestones and massive algal marine environment. Meledis-, Corona- and mounds accumulated. Bedded cherty limestones Carnizza Formations predominantly consist of with mari intetcalations are interpreted to have clastic sédiments, Pizzul- and Auernig been deposited during relative sea-level high­ Formations contain substantial quantities of fos- stands with water depths of some tens of meters. siliferous carbonate rocks. The main lithofacies Fusulinid-rich limestone beds are présent in dif­ types are a quartz-rich conglomerate of a near- férent stratigraphie levels, particularly at the base shore environment, frequently overlain by shale and on top of the clastic intervais. Fusulinids of containing abundant and well-preserved mega- thèse beds are considered as parautochthonous plant fossils, trough-crossbedded and hummocky assemblages, accumulated during periods of low

646 GEODIVERSITAS • 1998 • 20(4) Late Carboniferous-Early Permian of Carnic Alps

Relative Lithology Faciès Sea-levei low high

conglomerate LS T uppe r beac h

coarse-grained shorefac e sandstone fine-grained sandstone with lowe r

hummocky crossbedding shorefac e HS T siltstone, bioturbation c fossiliferous

bedded limestone she l and massive algal

mounds (ope n r> CD

siltstone, offsho i bioturbation

.S I t-

fine-grained sandstone with

hummocky crossbedding lowe r shorefac e

coarse-grained sandstone shale, plant fossils uppe r conglomerate beac h LS T shoreface ,

erosive base

FIG. 3. — Idealised "Auernig-Cyclothem" from the upper part of the Auernig Group in the Garnitzenberg-Kronalpe area, Carnic Alps.

sédiment input (see Homann 1969; Flûgel 1974, Boeckelmann 1984; Boeckelmann 1985). A 1977; Buggisch et al. 1976; Forke et al. in press). caliche unit and a red shale unit with scattered The Gtenzland Formation is a cyclic succession, angular quartz grains in the upper part of the predominantly composed of shallow marine clas­ succession indicate subaerial exposure. Fusulinids tic sédiments (quartz-rich conglomerate, sand­ were described from rhe thin carbonate inrercala- stone and siltstone) and intetcalated thin tions (Kahler & Kahler 1937; Kahler 1985; fossiliferous carbonate intervais (Buttersack & Forke 1995). Plant fossils have been described

GEODIVERSITAS • 1998 • 20(4) 647 Krainer K. & Davydov V.

from a thin shale intercalation by Fritz & relative sea-level Boersma (1984). low high (shoreface) (offshore)

The Upper Pseudoschwagerina Limestone is fine-grained represenred by a cyclic succession composed pte- sandstones dominantly of dark-grey, thin bedded fossiliferous limestones and intercalated thin intervais of silt- and sandstones and fine-grained, well-rounded and well-sorted quartz rich conglomerares. mariy limestones with mari Limestones contain abundant fossils, particularly intercalations calcareous algae (Homann 1972), small foramini- fers (Fliigel 1971), fusulinids, corals, bryozoans, brachiopods, gastropods, pelecypods and echino- derm fragments. Microfacies has been described by Fliigel (1968) and Buttersack & Boeckelmann (1984). Cycles indicate repeared shifting from nearshore to offshore environments in an open marine shelf-lagoon with normal water circula­ tion (Fliigel 1981). Compared ro the LPL and Grenzland Formation the limestones are characte- rized by more diverse biota and microfacies rypes (Fliigel 1971, 1981; Fliigel et al. 1971).

TROGKOFEL GROUP The Trogkofel Group is composed of approxima- rely 400 m thick, predominantly massive, subor- dinately bedded limestones (Trogkofel limesrone, Tressdorf limestone and Goggau limesrone). The limestones were deposited in shallow, restricted and open marine shelf-lagoons with only minor bathymetrical différences. Tubiphytesl Archaeolithoporella build-ups composed of sedi- ment-binding organisms like encrusting forami- nifers, phylloid algae, Tubiphytes, Archaeo­ lithoporella and bryozoans formed at the shelf edge (Fliigel 1980a, b, 1981). Fliigel & Fliigel- Kahler (1980) described 46 species of calcareous algae, the fusulinid fauna is represented by 70 species (Kahler & Kahler 1980).

BIOSTRATIGRAPHY FIG. 4. — Stratigraphie column of the Lower Pseudoschwagerina Limestone (Rattendorf Group) from the north-western side of the FUSULINIDS Schulterkofel (type section). The first comprehensive paper on fusulinids from Lare Paleozoic limestones of the Carnic Alps was presenred by Schellwien (1898). From nas of the Bombaso Formation, Auernig, 1932-1996 F. Kahler (till 1982 with his wife Rartendorf and Trogkofel Groups. The biostrati- G. Kahler) intensively studied the fusulinid fau- graphic classification and subdivision of the Late

648 GEODIVERSITAS • 1998 • 20(4) Late Carboniferous-Early Petmian of Carnic Alps

Paleozoic séquence of the Carnic Alps is mainly Quasifusulinoides pakhrensis, Q. pulchella, based on the detailed investigation of fusulinids Protriticites ovatus. by F. Kahler & G. Kahler. Their data are publi- Carbonates from the basai Meledis Formation shed in numerous papers, summaries are given in near Zollnersee and at Cima Val di Puartis Kahler (1983, 1985, 1986, 1989). Additional contain fusulinids of the Protriticites pseudomon­ data concerning fusulinid stratigraphy have been tiparus zone in its lowermost part, and of the contributed by Pasini (1965, 1990) and recently Montiparus paramontiparus zone in the middle by Forke (1995), Forke et al. (in press) and portion of this formation. The Protriticites pseu­ Davydov (Davydov & Krainer, in press). We use domontiparus zone is characterized by Protriticites the sign * in cases of différence from original globulus, Pr. pseudomontiparus, Pr. sphaericus, authors taxonomy. Pr. rotundatus, Pr. ovoides, Pr. lamellosus and Praeobsoletes burkemensis. Thèse species are cha­ Bombaso Formation and Meledis Formation racteristic only in the Protriticites pseudomontipa­ The oldest fusulinid fauna of the Carnic Alps is rus - Obsolètes obsoletus zone of the Russian described from carbonate rocks on top of the Platform (Kreviakian Horizon) and Timan- Bombaso Formation west of Zollnersee, consis- Pechora région, in the Urals, Donets Basin, ting of Ozawainella angulata, O. kumpani and O. Central Asia, Spitsbergen and in the Cantabrian cf. mosquensis, Fusulinella colaniae rasdorica, F. Mountains (see Davydov & Krainer, in press). fluxa, Beedeina* nytvica callosa, Fusulina (s.str.) The Montiparus paramontiparus subzone is cha­ fortissima, Quasifusulinoides* mjachkovensis, racterized by the occurrence of Praeobsoletes pau- Quasifusulinoides* quasifusulinoides and Quasi­ per, P. burkemensis, Obsolètes timanicus, fusulinoides juvenatus (Kahler 1983). According O. obsoletus, Montiparus paramontiparus, to Kahler (1983), this fusulinid fauna corres­ M. umbonoplicatus, M. montiparus, M. likharevi, ponds to the Fusulinella bocki zone of the Late M. rhombiformis and M. priscus. Montiparus spe­ Myachkovian of the Russian classification. cies found in the Carnic Alps are well-known Carbonate from the lowermost Meledis from middle Kasimovian strata of the Russian Formation of the Auernig Group yielded a Platform (Khamovnicheskian), Timan-Pechora Fusulinella, Fusulina and Quasifusulinoides fauna Basin, the Urals (upper part of the Orlovskyi near Waidegger Alm indicating lowermost Horizon), Central Asia, Spitsbergen and the Cantabrian Mountains. In Central Asia and the Kasimovian C3A, (Kahler 1986) and a Protriticites-ïdMna. containing P. pseudomontiparus Southern Urals the Montiparus montiparus zone SW of Zollnersee pointing to lowermost is divided into two subzones: the M. paramonti­ Kasimovian A, (Kahler 1983). parus subzone in the lower part and the M. sub- Récent investigation yielded a small fusulinid crassulus subzone in the upper part. The assemblage from conglomérâtes of the Bombaso assemblage recognized in the Carnic Alps corres­ Formation near Straniger Alpe, composed of ponds to the M. paramontiparus subzone (see dis­ Quasifusulinoides quasifusulinoides, Q. fallax, cussion by Davydov & Krainer). Q. intermedia, Protriticites ovatus, P. cf. ovoides. It should be indicated that the représentatives of The composition of this assemblage is most simi­ the Praeobsoletes-Obsoletes lineage in the Carnic lar to that from the Protriticites ovatus - Alps appear later. In the Russian Platform, the Praeobsoletes burkemensis zone in the sttatotype Urals, Donets Basin and Central Asia Praeob­ section in the Moscow Basin and occurs only in soletes first appears in the uppermost Myach­ the Peskovskaya Formation of the Myachkovian kovian and ranges into the lowermost Kasi­ Horizon of the Moscovian (Davydov 1997; movian. Obsolètes first appears at the base of the Davydov & Krainer, in press). A similar assem­ Kasimovian and is most characteristic for the blage was found near the top of the Bombaso Early Kasimovian (Kreviakian). Only rarely Formation west of Zollnersee and includes Obsolètes ranges into the middle Kasimovian Fusiella lancetiformis, Beedyina consobrina, B. pes- (Kahmovnicheskian). In the Carnic Alps, simi- kensis, B. pseudocylindrica, Fusulinella rara, larly with the Cantabrian Mountains and

GEODIVERSITAS • 1998 • 20(4) 649 Krainer K. & Davydov V.

Spitsbergen (Villa et al. 1992; Nilsson & Pseudofusulina multisepta originared from the Davydov 1993), the représentatives of the Carnic Alps (Schellwien 1898), but for more Praeobsoletes-Obsoletes lineage are rare. then sixty years was used in the literature as a Praeobsoletes first appears only in the lowermost Late Permian Parafusulina species, reporred from Kasimovian (Kreviakian) and Obsolètes first many Tethyan régions. Until revision and solving appears in the uppermost Kreviakian or only in of rhis taxonomical problems we use inverted the Khamovnicheskian. commas for this species. In the very rop of the Meledis Formation in rhe In Darvas and in S. Urals Schagonella in gênerai RC section (RC-12b and RC-13) the following dominated in the middle Gzhelian. Daixina fusulinids wete identified: Ferganites ferganensis admirabilis originally was described from the Miklukha-Maclay, Rauserites sp., and Rauserites Orenburgian of the Urals (Zolotova et al. 1978), rossicus (Schellwien) (Fig. 5A-E). The last species but also was reported from the late Gzhelian in the Russian Platform and the Urals characteri- (s.str.) of Darvas (Davydov 1986). Fusulinid data se lowermost Gzhelian or Rechitskyi Horizon of ftom Pizzul and Corona Formations do not the Russian Platform (Rosovskaya 1958; constrain a spécifie âge. Based on the strarigra- Makhlina et al. 1984; Davydov & Popov 1986). phic posirion of Pizzul and Corona Formations Ferganites ferganensis in Central Asia as well as in above an équivalent of the early Gzhelian (Upper S. Urals characterises also early Gzhelian, an Meledis) and below the Orenburgian Auernig équivalent of Amerevskyi Horizon of the Russian Formarion, the âge of both formarions can be Platform (Fig. 6) (Davydov & Popov 1986; estimated as late Gzhelian (s.str.) (Amerevskyi Popov et al. 1989). We suggest that the very and Pavlovoposadskyi Horizons of Russian upper portion of the Meledis Formation is early Platform). Gzhelian in âge (Fig. 6). The Auernig Formarion (Obère kalkreiche Schichtgruppe) of Garnitzenberg and Kronalpe Pizzul Formation, Corona Formation, Auernig contains Boultonia europaea; Triticites schivageri- Formation and Carnizza Formation niformis, T. perstabilis; Daixina*alpina, D.*com- According to Kahlet (1985) the Pizzul munis, D. * alpina fragilis, D. * devexa acallosa; Formarion (Untere kalkreiche Schichrgruppe) is "Pseudofusulina multiseptata", "P. paraconcinna"; characterized by the occurrence of the following Dutkevitchia dastarensis, D. "kargalensis", D. "ruz- fusulinid species: Triticites oryziformis, Rauserites* hencevi"; Quasifusulina tenuissima, Q. compacta, noinskyi plicatus; Daixina alpina vetusta, Q. karawankensis, Q. kaspiensis, Q. phaselus, D. sokensis (s.srr.*), D. naviculaeformis, D. sakma- Q. pseudoelongata, Q. pseudolonga (Kahler 1983, rensis and Quasifusulina eleganta. Récent studies 1985). of non-oriented thin-sections from rhe Pizzul The Carnizza Formation (Obère kalkarme Formation show dominance of a Schagonella and Schichrgruppe) of Garnitzenberg contains Daixina fauna. Because in Central Asia and sou­ Daixina alpina antiqua = alpina and the subspe- thern Urals représentatives of the Daixina soken­ cies fragilis, and Dutkevitchia dastarensis. sis group appear earlier than in the Russian According to Kahler (1986, 1989) Pizzul Platform, and because of the stratigraphie posi­ Formarion, Corona Formarion, Auernig tion of the Pizzul Fotmation above the early Formation and Carnizza Formation are of Gzhelian and below the Orenburgian, we believe Gzhelian âge (Gzhelian E). that the Pizzul Formation has to be an équivalent Récent studies in the southern Urals, Donets of the late Gzhelian (s.str.). Basin and in Central Asia (Darvas and southern From a thin carbonate bed of the Corona Fergana) showed that Boultonia europaea and Formation at Garnitzenberg (Mittlere kalkarme Dutkevitchia dastarensis first appear at the basai Schichtgruppe) Kahler (1983) reported Otenburgian Daixina sokensis zone (Davydov "Pseudofusulina multiseptata". Daixina alpina, D. 1984, 1992; Popov et al. 1989; Davydov et al. ex gr. admirabilis and Schagonella spp. also were 1993). Dutkevitchia ruzhenzevi and Dutkevitchia recently identified by Davydov. The species kargalensis everywhere first appear only in the

650 GEODIVERSITAS • 1998 • 20(4) Late Carboniferous-Early Permian of Carnic Alps

FIG. 5. — Stratigraphically significant fusulinids from the Meledis Formation (basai Auernig Group) and Lower Pseudoschwagerina Limestone (Rattendorf Group). k,Rauserites rossicus (Schellwien, 1908), tangential section, RC-13-4. B, Rausehtes sp., oblique section, RC-13-4. C-E, Ferganites aff. ferganensis (Miklukho-Maclay, 1948): C, axial section, RC-12b-9; D, tangential section, RC- 12b-12; E, paraxial section, RC-12b-2. F, G, Schellwienia bornemani (Leven ef Scherbovich, 1978): F, axial section of typical spéci­ men, SK-157-4; G, axial section of short spécimen, SK-157-2. H, Zigarella panjiensis (Leven ef Scherbovich, 1978), axial section of typical spécimen, SK-157-5. I, Likharevites inglorius (Bensh, 1962), axial section, SK-157-1. J-L, Schellwienia bornemani (Leven ef Scherbovich, 1978): J, axial section of spécimen with small axial fillings, SK-157-12; K, axial section of typical spécimen, SK-157-13; L, axial section of short spécimen, SK-157-9. Scale bar: 0,5 cm.

GEODIVERSITAS • 1998 • 20(4) 651 Krainer K. & Davydov V.

early Asselian, and we believe that their occur­ of Forke et al. lies near the base of the overlying rence in the Orenburgian Auernig Formation is Grenzland Formation. misidentified. Therefore we place inverted com- The following species were identified in récent mas with both of thèse species. The âge of studies of LPL in the Schulterkofel section: in Auernig and Carnizza Formations for now can be the very lower portion of LPL (TST of estimated as Orenburgian (équivalent of Séquence 1) we found Daixina sokensis, Nogonskian of Russian Platform) (Fig. 6). Schellwienia oblonga and Dutkevitchia bimorpha. In the HST of Séquence 1 Ultradaixina postso- Lower Pseudoschwagerina Limestone (Schulterkofel kensis and Schellwienia ulukensis and within Formation) Séquence 2, Schellwienia ulukensis and Zigarella From the uppermost part of the Lower elegans were identified. Most interesting data Pseudoschwagerina Limestone near Rudnigalm were retrieved from the top of Séquence 3, where Kahler (1985) described the following fusulinid Schwagerina versabile, Schellwienia bornemani, species: Boultonia europaea; Rugosofusulina aria- Zigarella panjiensis and Likharevites inglorius were nica, R. directa, R. latioralis, R. cf. pandae, identified (Fig. 5 F-L). R. praevia egregia, R. stabilis, R. stabilis longa; To estimate the âge of the LPL Formation we can Paraschwagerina cf. tinvenkiangi elongata, indicate the following: in Southern Fergana and Occidentoschwagerina alpina and "Eozellia miha- Darvas Ruzhenzevites ferganensis first appeats in ranoensis" (= Ultradaixina ex gr. postgallowayi). the middle portion of an équivalent of the From Schultetkofel Kahler (1983) listed Daixina sokensis zone. (Davydov 1984; Popov et Boultonia europaea; Ruzhenzevites* parasolidus; al. 1989). Ruzhenzevites parasolidus is a more Rugosofusulina cf. pandae, R. serrata, R. likana, advanced species and in Darvas it first appears in R. praevia and Rugosochusenella*pseudogregaria. the very top of the Daixina sokensis zone and In a récent paper Kahler & Krainer (1993) des­ ranges higher. In Southern and Northern cribed a fusulinid fauna composed of about Fergana this species occurs in the Schwagerina 30 species from the upper part of the LPL of the robusta-Ultradaixina bosbytauensis zone and Schulterkofel section. Species of Triticites and tanges higher into the Asselian. Schellwienia ulu­ Rugosofusulina dominate, whereas those of rare kensis in Central Asia as well as in the Southern "Daixina" {^Schellwienia), Rugosochusenella and Urals section occurs only in the Schwagerina Ruzhenzevites occur. The Carboniferous/Permian robusta-Ultradaixina bosbytauensis zone. boundary was drawn at the first appearance of Schwagerina versabile in Datvas and in the "Pseudoschwagerina" and "Occidentoschwagerina Southern Urals appears in the very top of the alpina" {- Ultradaixina) in the upper part of the Schwagerina robusta-Ultradaixina bosbytauensis section. Ftom our point of view, spécimens zone, but is characteristic of the early Asselian. named as Pseudoschwagerina could not be identi- Schellwienia bornemani, Zigarella panjiensis and fied even with genus name, because in the tan­ Likharevites inglorius in Central Asia and the gential sections reported, the juvenarium Southern Urals are known only from the Asselian structure, which is most important for taxono- (Bensh 1962 ; Leven & Scherbovich 1978; my, is not présent. Davydov 1984; Popov et al. 1989) (see corréla­ tion chart, Fig. 6). According to Forke et al. (in press) the lower part (depositional Séquence 1) of the LPL in the Based on ail this data we can suggest the follo­ Schulterkofel section, characterized by the occur­ wing. The TST (transgressive Systems tract; rence of Ruzhenzevites ferganensis and Fig. 4) of Séquence 1 of LPL can be correlated Ruzhenzevites parasolidus without species of the with the uppermost part of the Daixina sokensis genus Ultradaixina, is correlated with the zone. The HST (highstand Systems tract) of Sokensis zone. The overlying part (uppermost Séquence 1 can be correlated with the lower por­ part of depositional Séquence 1 up to the top of tion of the Schwagerina robusta-Ultradaixina bos­ depositional Séquence 3) corresponds to the bytauensis zone or with the Ultradaixina Bosbytauensis-Robusta zone. The C/P-boundary postsokensis zone of the Southern Urals and

652 GEODIVERSITAS • 1998 • 20(4) Late Carboniferous-Early Permian of Carnic Alps

Darvas. Mosr part of Séquence 2 (excepr the gerina aequalis, Ps. extensa and Sphaeroschwa­ HST) conventionally can be correlated with the gerina* confinii, from the eastern side of middle portion of the Schwagerina robusta- Schulterkofel, Pseudoschwagerina turbida and Ultradaixina bosbytauensis zone or with the Sphaeroschwagerina * carniolica. Ultradaixina bosbytauensis zone of the Southetn Based on the occurrence of Pseudoschwagerina Urals and Darvas. The HST of Séquence 2 and aequalis, Sphaeroschwagerina* confinii and LST (lowstand Systems tract) and TST of Sphaeroschwagerina* carniolica Kahler (1986) Séquence 3 should be correlared wirh the upper dated the Grenzland Formarion as middle portion of the Schwagerina robusta-Ultradaixina Asselian. bosbytauensis zone or with rhe Ultradaixina post- Forke (1995) described Sphaeroschwagerina glo- gallowayi zone of the Southern Urals and Darvas. merosa from the Grenzland Formation near The HST of Séquence 3 very probably is Early Rudnigsattel. Asselian in âge. The lasr conclusion is based on Most of the species of Grenzland Formation, rhe following: in Darvas, the Southern Urals and except Quasifusulina species, are known from the in the Donets Basin the acme-zone (maximum of middle as well as from the late Asselian. occurrences) fot Ultradaixina is in the upper por­ Sphaeroschwagerina glomerosa indicates only late tion (but not uppermost) of the Schwagerina Asselian âge. Base on this we can suggest middle- robusta-Ultradaixina bosbytauensis zone. In the late Asselian âge for the Grenzland Formation very upper portion of this zone Ultradaixina is (see Fig. 6). rare and pethaps extinct, and absolutely absent in the Asselian. Similarly in the Schulterkofel sec­ tion the acme-zone for the Ultradaixina is the Upper Pseudoschwagerina Limestone HST of Séquence 2 and the LST of Séquence 3. From the type section of the Upper In the TST of Séquence 3 Ultradaixina is extre- Pseudoschwagerina Limestone at Zottachkopf mely rare and absolutely no Ultradaixina is pré­ Kahler described the following fusulinid species: sent in the HST of Séquence 3. Schellwienia Boultonia willsi, Pseudofusulina regularis, bornemani and Zigarella panjiensis originally were McCloudia* haydeni, Darvasites contractus, described from the middle Asselian of Darvas. In Schwagerina "krtowf, Pseudoschwagerina pulchra, rhe Southetn Urals they occur in the early- Biwaella inopinata and Rugosochusenella paragre- middle Asselian. Likharevites inglorius in Darvas, garia. Northern Fergana, the Southern Urals and Red limestones at Ttoghôhe and at point 2016 Predoners Trough was found in the early-middle (according to Kahler belonging to the Trogkofel Asselian (Bensh 1962; Leven & Scherbovich Limesrone, after Forke to the Upper 1978; Davydov 1990; Davydov et al. 1993). So, Pseudoschwagerina Limestone) contain a rich occurrences of Schellwienia bornemani, Zigarella fusulinid fauna. Kahler (1983, 1985) reported panjiensis and Likharevites inglorius suggest the following species: Boultonia willsi, Asselian âge for the HST of Séquence 3 of the Quasifusulina nimia, Q. pseudoelongata, Q. Lower Pseudoschwagerina Limestone. tenuissima, Q. cf. kaspiensis, " Chusenella cheni", "Ch. chihsiaensis", "Ch. rabatei", Schwagerina* Grenzland Formation moelleri, Schw.*paraconfusa, Eoparafusulina* Ftom limestones of the Grenzland Formation at " tschernyschewi', Robustoschwagerina geyeri, Rudnigsattel Kahler (1985) reported the occur­ R. schellwieni, Paraschwagerina inflata longa, rence of Quasifusulina cf. compacta, Q. eleganta, Sphaeroschwagerina * carniolica, S. * lata, S. * pul­ Q. kaspiensis, "Darvasites contractus", Zigarella chra, Zellia heritschi, Z. galatea. pseudopointeli, Sphaeroschwagerina carniolica, According to Forke (1995) the red limestones Pseudoschwagerina extensa and Sphaeroschwage­ contain the following stratigraphically important rina sphaerica. species: Zellia heritschi, Robustoschwagerina From the type section near Rattendorfer Alm, schellwieni, R. geyeri, Paraschwagerina inflata, Kahler & Kahler (1937) described Pseudoschwa­ Schwagerina moelleri, Schwagerina cf. verneuili

GEODIVERSITAS • 1998 • 20(4) 653 Krainer K. & Davydov V.

FIG. 6. — Corrélation chart for the Late Carboniferous and Early Permian.

654 GEODIVERSITAS • 1998 • 20 Late Carboniferous-Early Permian of Carnic

GEODIVERSITAS • 1998 • 20(4) Krainer K. & Davydov V.

and Pseudofusulinoid.es pusillus. Forke (1995) the Tressdorf limestone as early Artinskian dates rhe Upper Pseudoschwagerina Limesrone as (Fig. 6). Sakmarian (Robustoschwagerina geyeri zone and Zellia heritschi zone). The following problems for fusulinid biosrrari- graphy should be addressed immediately: Trogkofel Group - précise fusulinid biostratigraphy of Pizzul, After Kahler & Kahler (1980) the fusulinid Corona, Auernig and Carnizza Formations; fauna of the Trogkofel Group consisrs mainly of - complète charactetistic of C/P boundary beds species of the gênera Triticites, Darvasites, Pseudo- and better criteria for the C/P boundary posi­ fusulinoides, Pseudofusulina, " Praeparafusulina", tion; Pamirina and Minojapanella. They described - âge of Grenzland Formation; about seventy species. Stratigraphically impor­ - fusulinid biostratigraphy and succession of the tant index fossils are Schwagerina* moelleri, cha- Trogkofel Limestone; racteristic for the lower part (Trogkofel - restudy of the Tressdorf and Goggau Lime­ limesrone), "Parafusulina lutuginf typical for the stones. Tressdorf limestone, and the Chalaroschwa- gerina* vulgaris-gtoup togethet with Pamirina CONODONTS darvasica in the Goggau limestone. True parafu- The occurrence of conodonts in Late Paleozoic sulinids and Misellina species are lacking. carbonates of the Carnic Alps was first noted by Kahler (1986) dated the Trogkofel limestone as Fliigel et al. (1971) from the Rattendorf Group Sakmarian (Tastubian-Sterlitamakian) due to the and Boeckelmann (1983) from the Auernig occurrence of Robustoschwagerina schellwieni and Group (discoveries of individual conodonr frag­ Pseudoschwagerina lata. The Tressdorf limestone, ments, which have no stratigtaphic importance). containing "Praeparafusulina lutugini" is classi- Forke (1995) described a conodont fauna from fied as Early Artinskian (Burchev), and the red limestones of the Upper Pseudoschwagerina Goggau limestone, which contains Chalaro- Limesrone. The conodont fauna is composed of schwagerina* vulgaris and Pamirina, is dated as the following species: Aethotaxis advena, Late Attinskian (Irgin). According to Forke Hindeodus minutus, Mesogondolella cf. bisselli, (1995) the Trogkofel limestone is Late Diplognathodus expansus?, Sweetognathus inorna- Sakmarian to Eatly Attinskian in âge. tus and Sweetognathus aff. whitei. It should be noted, that Sakmarian and In central and western USA S. inornatus and Artinskian fusulinids of the Urals can not occur S. aff. whitei appear in the Late Wolfcampian. in the Tethyan section, as the Carnic Alps, S. inornatus belongs to the Sweetognathus whitei- because beginning in the early Sakmarian the Mesogondolella bisselli zone. In the Utals, Boréal province was completely isolated from the Sweetognathus inornatus appears in the Tethyan provinces. None Artinskian fusulinid Sterlitamakian (Late Sakmarian) and ranges into species of the Urals are known from Tethys sédi­ the Attinskian. Sweetognathus whitei is known ments, but those listed, we believe, are identified only in Aktastian (Early Artinskian) (Chernykh & erroneously. For this reason "Praeparafusulina Reshetkova 1987; Chernykh & Chuvashov lutugini" takes inverted commas and indicates 1993). Sweetognathus whitei in the Trogkofel taxonomical misidentification. Group is represented by incomplète atypical spé­ We cannot estimate the âge of the Trogkofel cimens (idenrified with "affinity" sign). The limesrone based only on fusulinids for now. It appearance of Sweetognathus inornatus and S. aff. could be Sakmatian as well as early Artinskian. whitei together with Robustoschwagerina and Because the Goggau Limestone contains Zellia, but without typical Attinskian fusulinid Chalaroschwagerina vulgaris and Pamirina darva­ faunas (Pamirina, Chalaroschwagerina) in the sica, which in Darvas characterises the late Carnic Alps, indicates at this time Sakmarian âge. Yakhtashian (Early Artinskian) (Leven et al. According to Forke (1995) the Uppet Pseudo­ 1992), we can conventionally estimate the âge of schwagerina Limesrone is of Sakmarian âge

656 GEODIVERSITAS • 1998 • 20(4) Late Carboniferotis-Early Permian of Catnic Alps

(based on the occurrence of Robustoschwagerina Formations. (Kahler et al. 1933; Kahler & Prey geyeri and Zellia heritschî). Forke (1995) in his 1963; Fenninger & Schonlaub 1972; Francavilla paper présents corrélation charts of the 1974). Rattendorf and Trogkofel Group with sections Fritz & Boersma (since 1980) and Fritz & from the Urals, Darvas, N-China, S-China, Krainer (since 1993) systematically investigated Japan and USA. the fossil flora of the Bombaso Formation and Auernig Group from more than 30 localities. FOSSIL FLORA Plant fossils are found in ail formations of the Plant fossils were reported from the Bombaso Auernig Group, from most localities the strati­ Formation and Auernig Group more than graphie position within the section is exactly 100 years ago. Hôfer seems to be the first who known. collected plant fossils in 1869 in the Monte From ail localities 105 taxa are described Corona/Kronalpe and Casera For/Ofenalm area. (Equisetophyta 26 taxa, Lycophyta 12 taxa, The spécimens were determined and described Filicophyta, Pteridospermae and Pteridophylla by Unger (1869), the taphoflora list contains 57 taxa, Cordaitospermae 9 taxa; Coniferae 19 taxa. 1 taxon, see Fritz et al. 1990; Ftitz & Krainer The déterminations of Unger (1869) were later 1993, 1994, 1995). revised by Reichardt (1937) and Fritz & From the Gtenzland Formation the occurrence Boersma (1982). of plant fossils (no déterminations) has been Taphoflora lists from the Monte Corona section noted by several authors (Felser et al. 1956; (Corona Formation) have been published by Felser & Kahler 1963; Kahler & Prey 1963; Stache (1874), Schellwien (1892), Frech (1894) Flùgel 197A). Herzog (1984) discovered a plant and Geyer (1897). fossil bearing interval and collected a flora which From the localities Cason di Lanza (?Meledis was determined and described by Fritz & Formation) and Monte Pizzul (type locality for Boersma (1984) and Fritz et al. (1990). So far the Pizzul Formation) plant fossils were descri­ known this locality is the only one within the bed by Tommasi (1889), Bozzi (1890) and Rattendorf Group and thus the youngest fossil Vinassa De Regny & Gortani (1905). flora of the Late Paleozoic séquence in the Carnic Later, numerous new localities of plant fossils Alps. within the Auernig Group were discovered by Kahler, Metz and others in the Auernig, Nassfeld FLORA OF THE BOMBASO FORMATION and Schulterkofel areas. The plant fossils were From the Bombaso Formation 3 localities contai­ described by Reichardt (1933) and Kielhauser ning plant fossils are known (Tomritsch 1, 2 and (1937), a first summary on the fossil flora of the 6). The lowermost locality (Tomritsch 6) is cha- Auernig Group including 25 taxa was given by racterized by the occurrence of Sphenophyllum Reichardt (1937) andjongmans (1938). oblongifolium, Linopteris neuropteroid.es, Jongmans (1938) classified the flora of the Neuropteris ovata, Neuropteris scheuchzeri and Auernig Group as Westphalian D (= Early others (Fritz & Krainer 1995). According to Stephanian) and Westphalian E (= Late Wagner (1984) N. scheuchzeri is a guideform of Stephanian). He also pointed out that within the the Cantabrian {Odontopteris cantabrica zone). Auernig Group the Schulterkofel flora represents This corrélation quite precisely corresponds with the youngest flora. fusulinid data, which suggests for Cantabrian Berger (i960) reported 30 taxa from new locali­ Uppermost Moscovian and Early Kasimovian âge ties, most of them within the Bombaso (Ginkel 1971; Rauser-Chernousova & Formation and lowermost part of the Auernig Scherbovich 1974). Group. He classified the fossil flora as Westphalian D. Plant fossils have also been des­ FLORA OF THE AUERNIG GROUP cribed from several new intervais within the From the Auernig Group plant fossils are known uppermost Corona-, Auernig- and Carnizza from many horizons within ail formations. The

GEODIVERSITAS • 1998 • 20(4) 657 Krainer K. & Davydov V.

lowermost horizon containing plant fossils is Typical guideforms of the Lobatopteris lamuriana from perhaps the basai part of the Meledis zone (Barruelian) and Alethopteris zeilleri zone Formation (localities Tomritsch 3, Zollnersee (Stephanian B) have not been discovered till and Straniger Alm). The fossil assemblages of now. rhese localiries are characterized by the abundan- According to the plant fossils the Bombaso ce of Linopteris neuropteroid.es. The présence of Formation is of Cantabtian âge, the Auernig Sphenophyllum angustifolium, S. oblongifolium, Group contains rypical guideforms of Srephanian Callipteridium pteridium, Odontopteris brardii C, and rhe Grenzland Formation is characterized and Pecopteris species of the group P. arborescence by a flora of Early Permian âge (see Table Carnic -P. schlotheimii indicates Stephanian âge (early to Alps, this volume). Based on Donets Basin data middle Stephanian C according to the megaflora (Davydov 1990) Stephanian A corresponds to zonation of Wagner 1984). However, there is a the middle and perhaps part of late Kasimovian, contradiction berween fusulinid and floral dating Stephanian B corresponds to the late Kasimovian of the lower Meledis Formation. Based on fusuli­ and Stephanian C to the most parr of Gzhelian. nids the lower Meledis Formation is Early to Aurunian begins from the Schwagerina robusta- Middle Kasimovian in âge and should corres­ Ultradaixina bosbytauensis zone of the pond at least with the upper portion of the Orenburgian and also cotresponds to the whole Cantabrian, Stephanian A and perhaps Asselian (Fig. 6). Stephanian B (Wagner & Winkler-Prins 1985; The flora of rhe Bombaso Formation, Auetnig Davydov 1990). Only rhe uppermosr Meledis Group, and Grenzland Formarion is well dared Formarion, which contains early Gzhelian fusuli­ by fusulinids. Fluvial séquences of the Eastetn nids, could correspond with Stephanian C. The Alps (Stangnock Formation, Gutktal Nappe), âge of the Meledis Formation in the Tomritsch 3, which contain a similar assemblage of plant fos­ Zollnersee and Straniger Alm localiries should sils ranging ffom rhe Odontopteris cantabrica also be dated by fusulinids. zone ro the Callipteris conferta zone, can be well The uppermost portion of the Auetnig Gtoup correlated with the marine séquence of the containing plant fossils lies within the uppet part Cainic Alps (Bombaso Fotmation-Grenzland of the Carnizza Formation (locality Formation). Schulterkofel). From this locality Fritz & Boersma (1981, 1983) Fritz et al. (1990) descri­ Acknowledgements bed a flora composed of 30 taxa, characterized by K. K. wishes to thank the Austrian Academy of the occurrence of Callipteridium gigas, C. pteri­ Sciences (Commission for Strarigraphy) for dium, Odontopteris alpina, O. brardii, Pecopteris financial support of field work in rhe Carnic feminaeformis and index fossils for Late Alps. Both authots thank Dora Gallegos from Srephanian âge: Aphlebia elongata, Pseudomario- Boise State University for correction of the pteris busquetii and Sphenophyllum alatifolium English. The Permian Research Institute at Boise [Sphenophyllum angustifolium zone, Stephanian C State University provided support for thin-sec- according to Wagner 1984). tion préparation and study of fusulinid biostrati­ graphy. We are very grateful to Alain Izart

FLORA OF THE GRENZLAND FORMATION (Nancy) and Daniel Vachard (Lille) for reviewing The flora of the Grenzland Formation contains rhe manuscripr and making helpful comments 16 species including Annularia sphenophylloides, and suggestions. A. stellata, Sphenophyllum cf. angustifolium, Callipteris conferta, Odontopteris brardii, Pecopteris feminaeformis and P. schlotheimii. The REFERENCES occurrence of Callipteris conferta and Spheno­ Alekseeva I. A., Glushenko N. V., Ivanov V. K., phyllum cf. angustifolium indicates Early Permian Inosova K. L, Kalmykova M. A., Kashik D. S., âge {Callipteris conferta zone according to Kozitskaya R. I., Ktuzina A. Kh., Movshovich Wagner 1984). E. V., Redichkin N. A. & Schvattsman E. G.

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Submitted for publication on 1 January 1997; accepted on 15 December 1997.

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