UDK 551.761.3/.4:56.016.3+563.96+565.33+563.12(436+437)=20 The Norian-Rhaetian boundary in the light of micropaleontological data Andrzej Gaždzicki Institute of Paleobiology of the Polish Academy of Sciences Al. Zwirki i Wigury 93, 02-089 Warszawa, Poland Heinz Kozur State Museum of Meiningen Schlofi Elisabethenburg GDR-61 Meiningen Rudolf Mock Department of Geology and Paleontology of the Faculty of Natural Sciences J. A. Comenius University Gottwaldovo nam. 19 86200 Bratislava Summary The stratigraphic ranges of Late Triassic conodonts, holothurian sclerites. ostracodes, and foraminifers are studied in representative sections of the uppermost Triassic of the Western Carpathians and Eastern Alps. The zonal subdivisions based on the above mentioned microfossils could be correlated with the ammonoid zonation and the stratigraphic scheme proposed by Kozur (1973b). The definition of the Norian-Rhaetian boundary with the base of the Choristoceras haueri zone agrees with the priority. This boundary is supported by distinct changes in animal and plant groups. The typical Kossen Beds appear to be of Rhaetian age, contemporaneous with the Zlambach Beds, and only the lowermost parts of these two units represent (Zlambach Beds) or at some places represent (Kossen Beds) the uppermost Norian (upper Sevatian). In the systematic part a new foraminifer species, »Vidalina« carpathica Gaždzicki, n. sp. is described. Project 4 Contents Introduction........................... Stratigraphical analysis of representative sections............."3 Hybe (Low Tatra, Kossen Beds)..................73 Bleskovy pramefi (Drnava, Slovak Karst)............... Mal£ MLinsky vrch (Slovak Karst, Zlambach Beds)...........77 Fischerwiese (Salzkammergut, Zlambach Beds).............78 Kendelbachgraben (Osterhorn Group, Kossen Beds)...........79 The problem of the Norian-Rhaetian boundary..............81 Stratigraphic value of microfossils at the Norian-Rhaetian boundary.....85 Conodonts...........................jjjj Holothurian sclerites.......................89 Ostracodes ..........................89 Foraminifers...................!..!!'.! 90 Some remarks to the papers of Hohenegger & Piller (1975) and Bystricky (1975) 92 Description of the new species....................96 Conclusions..........................97 References ..........................108 Introduction The paper presents the results of studies on the stratigraphic sequences of conodonts, holothurian sclerites, ostracodes, and foraminifers from Upper Norian-Rhaetian sections of the Western Carpathians (Hybe, Bleskovy pramefi, Maly Mlynsky vrch) and of the Eastern Alps (Fischerwiese, Kendelbachgraben, WeiBloferbach) developed in different facies (cf. figs, 1, 2). The Late Norian and Rhaetian conodont, ostracode, and holothurian sclerites assemblages comprise several short-living guide forms. Other fossils of steadily increasing importance for the stratigraphy, the foraminifers, were studied in thin sections. The foraminifers have yielded guide forms also in such parts of the sections where conodonts and holothurian sclerites are scarce or absent and ostracodes are hardly obtainable from the rocks. More than one hundred thin sections of samples from the above mentioned sections were available. The zonations based on the above mentioned microfaunistic elements were correlated with the orthostratigraphic ammonoid zonation in accordance with the stratigraphic subdivision of the Norian and Rhaetian sensu Kozur (1973 b), concordant with the priority Giimbel's (1861) subdivision. T \ 3 ? Y ^ Prah a "J ___ < \ V * e ^ S s^yf- V C u 6-V N 0 c Hybe• Koiice t K r.J '■^•^J-V V A 9Bleskovy pro/nefi r-J vj^ ) 9f v V J j ( Maly Mlynsky vrch f Wien^^ sp Bratislava ____' \ Salzburg !-». f ,H t. ! V,______I f\ P"-* ) • .Flscherw,e5e r--" / \.J "—r Kendelbachgraben J V, A u ^ ' V rv .-------- S T * J '-v v c T r \ f _______s—**' ^ 0 200 km Fig. 1. Locality map of the investigated Upper Triassic sections in Czechoslovakia and Austria Stratigraphical analysis of representative sections Hybe (Low Tatra, Kossen Beds) Hybe is the best known locality of Kossen Beds in the Slovak Carpathians, a classical locality on account of its rich fauna. It is situated south of the village of Hybe in the valley of the Biely Vdh river, on the northern slopes of the Low Tatra (Koutek, 1927, fig. 1: Bystricky & Biely, 1966, fig. 8; Mi-c ha lik, 1973, figs. 1,2; Michalik in: Bystricky, 1973, figs. 13,14). Its surroundings are built up of Upper Triassic of the Cho£ nappe ("Biely Vdh Facies"), transgressively overlain by Paleogene sediments. The Upper Triassic is represented here by monotonous dolomites O'Hauptdolomit") of Carnian and Norian age, bedded light-grey "Dachstein Limestones", in places very variegated ones (Norian), and Kossen beds with rich Early Rhaetian fauna (fig. 2). The tectonical structure of the surroundings of the locality is highly complicated (cf. Michalik, 1973). The highly fossiliferous beds were discovered by S t ache (1867). Goetel (1917) described the rich assemblage of brachiopods, lamellibranchiates, corals, and echinoderms from this locality (about 40 species). This Rhaetian fauna is the typical Kossen fauna with Rhaetina gregaria (Suess), R. pyriformis (Suess) Zeil-Ieria norica (Suess), Oxycolpella oxycolpos (Emmrich), Rhaetavicula contorta (Portlock), Oxytoma inaequivalvis intermedia (Emmrich), Cassianella inaequi-radiata (Schafhautl), Modiolus schajhaeutli (Stur), Retiophyllia clathrata (Emmrich) etc. Andrusov (1934) found here the ammonite Rhaetites rhaeticus (Clark). Recently, the fauna of Kossen Beds from Hybe was studied by K o-chanovž (1967) and Michalik (1973, 1975). Budurov & Pevny (1970) have reported from Hybe 4 fragments of the conodont Gondolella navicula Huckriede. This species ranges highest into the Sevatian, but not into the uppermost Sevatian. Unfortunately, it is not known from which place this sample was taken and thus this finding is open to discussion. It possibly originates from the "Dachstein Limestones". In the Kossen Beds in the layer XXXII in the profile by Michalik (1973, fig. 2) M a - KOSSEN BEDS DACHSTEIN LIMESTONE HAUPTDOLOMIT Fie 2 Section of the Upper Triassic deposits near Hybe, Slovakia (cf. Koutek, 1927, fig l 'Bystricky & Biely, 1966, fig. 8; Michalik, 1973, figs. 1, 2; Michalik in: Bystricky, 1973, figs. 13, 14); numbered are the sampling sites jerska (1973) found conodonts originally determined as Spathognathodus hernstemi Mostler. These conodonts have later been described by Kozur & Mock (1974 b) as Misikella posthemsteini Kozur & Mock, the index species of the posthemsteini assemblage zone of the Rhaetian. Foraminifers of this sequence were studied by Salaj & J e n d r e j £ k o v a (1967) and Salaj; Biely & Bystricky (1967), and their stratigraphic importance was emphasized by Salaj (1969 a, b) and Gaždzicki & Zawidzka (1973). In the years 1972—1975 the section was sampled by Gaždzicki. About 40 thin sections made of these samples yielded numerous determinable foraminifers that made possible to discriminate faunal successions. The following foraminifers were found (location of samples see fig. 2): Samples 1—3: Semiinvoluta dart Kristan, 1957, Involutina gaschei (Koehn-Zamnetti & Bronnimann, 1968), Involutina sp., and Trocholina acuta Ober-hauser, 1964. Age : Norian (Alaunian — Sevatian), clari & oberhauseri ass. zone. Samples 4—7: Trochammina alpina Kristan-Tollmann, 1964, Alpinophrag-mium ? sp., Agathammina austroalpina Kristan-Tollmann & Tollmann 1964 Nodosana ordinata Trifonova, 1965, Nodosaria sp., Miliolipora cuvillieriBronnimann & Zamnetti, 1972, Semiinvoluta clari Kristan, 1957, Involutina communis (Kristan, 1957), Involutina tenuis (Kristan, 1957), Involutina gaschei (Koehn-Zaninetti & Bronnimann, 1968), Involutina sp., Trocholina permodiscoides Ober-hauser, 1964, and Triasina oberhauseri Koehn-Zaninetti & Bronnimann, 1968. Age : Upper Norian (Sevatian), clari & oberhauseri ass. zone. Samples 8—12: Glomospira sp., Glomospirella friedli Kristan-Tollmann, 1962, ro«T°APlrena pofcorn^ 1967)> Glomospirella parallela Kristan-Tollmann, 1964, Glomospirella sp., Tolypammina sp., Trochammina alpina Kristan-Tollmann, 1964, Tetrataxis inflata Kristan, 1957, Agathammina austroalpina Kristan-Tollmann & Tollmann, 1964, Ophthalmidium sp., Miliolipora cuvillieri Bronnimann & Zaninetti, 1972, Planiinvoluta deflexa Leischner, 1961, Nodosaria ordinata Trifonova, 1965, Nodosaria sp., Lingulina aff. placklesensis Kristan-1 ollmann, 1970, Diplotremina sp., Involutina communis (Kristan, 1957) Involutina tumida (Kristan-Tollmann, 1964), Involutina sinuosa sinuosa Wey'nschenk 1956 Involutina gaschei (Koehn-Zaninetti & Bronnimann, 1968), Involutina sp, Trocholina permodiscoides Oberhauser, 1964, and Triasina oberhauseri Koehn-Zaninetti & Bronnimann, 1968 — pi. 1, fig. 9. Age: Lower Rhaetian, pokornyi & friedli ass. zone. Bleskovy pramen (Drnava, Slovak Karst) This locality is about 1.5 km southeast of the village Drnava (Derno) 12 km east of Rožfiava (Slovak Karst) on the southern spur of the Drienovec Hi'll (formerly Drienkova hora, Somhegy) near the karst spring "Bleskovy pramen" (Szornyukut, cf Mello in: Bystricky, 1973, fig. 9). Rich thanatocoenosis, composed mainly of brachiopods, lamellibranchiates and cephalopods can be found m some lenses of grey and blue-grey crinoidal to coquinoid limestones. The fauna is less frequent in the surrounding dark massive limestones that form the highest parts of the thick light "Furmanec Limestones" (Dachsteinriffkalk) Sturzenbaum, 1879 (discoverer of the locality) considered these limestones rich in fossils to be Salzburg development of the Kossen Beds. He mentioned the species Choristoceras marshi Hauer and "Terebratula" gregaria Suess. The brachiopods from this locality were studied by Bittner, 1890, who considered most of the species to be typical of the Kossen Beds of the Alps. The cephalopods from Bleskovy pramen were investigated by Mojsisovics, 1896. He put them to the Sevatian zone of Pinacoceras metternichi (the index species itself was not found here). G o e t e 1, 1917 considered the limestones of this locality to be Dachstein Limestones and he regarded the fauna as Upper Rhaetian. Suf, 1939 has demonstrated that cephalopods, brachiopods and other fossils occur together and not in a Norian and a Rhaetian horizon. Matej-ka & Andrusov, 1931, ascribing the higher stratigraphic value to the "Norian" cephalopods, considered the beds of Bleskovy pramen to belong to the Sevatian. As to age, this locality was classified in the same manner also by Bystricky, 1964, who supplemented the fossil list by the Dasycladacean algae Diplopora cf. phanerospora Pia. This species is known from the Kossen Beds of the Alps (O 11, 1974, F 1 u g e 1, 1975). Recently, brachiopods found here were restudied by s'iblik, 1967. He described 21 species. On the whole this fauna is of Rhaetian character. The presence of the Norian Halorella amphitoma (Bronn) and the absence of Rhaetina gregaria (Suess) in this rich association are interesting. The cephalopods (15 species), lamellibranchiates (56 species) and gastropods (19 species) from Bleskovy pramefi were studied monographically by Kollžrova-Andrusovova & Kochanova (1973). Complete lists of fossils and many informations about the locality are given in this monography. Budurov & Pevny (1970) mentioned 4 conodont species from the limestones of Bleskovy pramen, among others "Polygnathus" tethydis Huckriede and "Hindeodella" petraeviridis Huckriede. These conodonts are illustrated on a photographic table. An erroneous determination can be therefore excluded. This conodont association cannot be younger than Middle Carnian, because such species as Gladigondolella tethydis (Huckriede) and Metaprioniodus petraeviridis (Huckriede) have never been found higher than Middle Carnian; most probably this association has a Ladinian age. Therefore these conodonts cannot originate from the limestones of Bleskovy pramen as already pointed out by M o c k (1971,1975). For this reasons it is surprising that in the above mentioned monography on molluscan fauna of Bleskovy pramen the authors ascribed primordial significance to the cephalopods and to the conodonts in their stratigraphic interpretation of the Bleskovy pramen fauna as Sevatian and not as Rhaetian (p. 206: »die wichtigste Rolle spielten dabei die Cephalopoden und Conodonten«). Up to present no conodonts were found by the present authors from this locality inspite of the fact that relatively large rock samples were dissolved by acetic acid. Holothurian sclerites are scarce here, being mainly represented by Theelia rosetta Kristan-Tollmann. It should be also pointed out that some "decisive Norian" ammonoid species described by Mojsisovics (1896) — e. g. Chon-stoceras (Peripleurites) boeckhi, Choristoceras (Peripleurites) stuerzenbaumi and Eopsiloceras clio — have the following locus typicus and stratum typicum: Bleskovy pramen, Drnava (Derno), "Upper Norian" (in reality Rhaetian). The question of the age of the Bleskovy pramefi beds was repeatedly studied by Kozur & Mock. In their first publication (Kozur & Mock, 1972, J974a) they determined the age of these beds as highest Sevatian (uppermost Sevatian sensu Tozer = uppermost Rhabdoceras suessi zone; Kozur, 1973b has divided this Rhabdoceras suessi zone in the Sevatian Sagenites giebeli and Cochloceras suessi zones and the Lower Rhaetian Choristoceras haueri zone). Kozur (1973b, pp. 17—18) put Bleskovy pramefi to the higher part of the zone with Choristoceras haueri (= uppermost Rhabdoceras suessi zone sensu Tozer, formerly uppermost Sevatian, now Lower Rhaetian) and he drew a parallel between this fauna and the middle Kossen Beds of its type locality in Austria. Such an age is also indicated by the brachiopods: Zugmayerella koessenensis (Zugmayer), Rhaetina pyriformis (Suess), and Triadithyris gre-gariaeformis (Zugmayer). These species occur at the type locality of the Kossen Beds in the upper part of the zone of Choristoceras haueri, immediately below the strata with Choristoceras marshi Hauer.* Kozur&Mock (1974c) pointed out that the fauna of Bleskovy prameri is still Lower Rhaetian, but younger than the Lower Rhaetian (Lower Rhaetian sensu Kozur, 1973b, see above) of Hybe with Rhaetites cf. rhaeticus (Clare), Rhaetavicula contorta (Portlock) and Misikella posthernsteini Kozur & Mock. Foraminifers were previously reported from the Bleskovy prameft area by Jendrejakova (1970). During the present studies foraminifers were found in the following samples: Sample 166/2: »Vidalina« mar tana Farinacci, 1959, »Vidalina« carinata (Leischner, 1961), Diplotremina cf. subangulata Kristan-Tollmann, 1960, Involutina cf. communis (Kristan, 1957), and Involutina tenuis (Kristan, 1957). Sample 166/2: Glomospirella sp., Trochammina alpina Kristan-Tollmann, 1964, Tetrataxis cf. inflata Kristan, 1957, »Vidalina« martana Farinacci, 1959 — pi. 1, figs. 2, 3, Ophthalmidium sp. — pi. 1, fig. 4, Galeanella cf. tollmanni (Kristan, 1957) — pi. 1, fig. 6, Miliolipora cf. cuvillieri Bronnimann & Zaninetti, 1972, Diplotremina ? sp., — pi. 1, fig. 7, Variostoma ? sp., Involutina communis (Kristan, 1957), and Involutina cf. turgida Kristan, 1957. Sample 166/3-Di: Tolypammina sp., Ammobaculites sp. — pi. 1, fig. 5, Variostoma ? sp., and Involutina gaschei (Koehn-Zaninetti & Bronnimann, 1968). Sample 166/3-Dt: Tolypammina sp. Sample 166/5-D4: Tolypammina sp., Trochammina sp., »Vidalina « cf. carinata (Leischner, 1961) — pi. 1, fig. l. Sample Dr.: Tolypammina sp., Trochammina alpina Kristan-Tollmann, 1964 Agathammina austroalpina Kristan-Tollmann & Tollmann, 1964, Planiinvoluta deflexa Leischner, 1961, Involutina communis (Kristan, 1957), Trocholina per-modiscotdes Oberhauser, 1964, and Triasina hantkeni Majzon, 1954 — pi. 1, fig. 8. The majority of the listed taxa are known from the Upper Norian to the Rhaetian. Attention should be paid to the foraminifer fauna of the sample Footnote 1) r *?°me °f iheSt brachiopods may occur also in the Choristoceras marshi zone. Seemu to be rfLther a bad index sPecies for the uppermost ammo-rhnwX °f tlle Tn?sslc' b«ause this species should be expected to occur also in the Choristoceras haven zone. Therefore the haueri and marshi zones should be rather nfP£o^by the disappearence of R^doceras suessi and not by the first appearence °CZaS maIShl- F°rJhis reason some correlations of brachiopod faunas with the ammonoid zonation of the Rhaetian are rather unclear. no. 166/2 with Galeanella cf. tollmanni and Involutina cf. turgida, known from strata not older than Rhaetian or even Liassic of the Tethys (K r is t a n, 1957; Kristan-Tollmann, 1962, 1964; Bronnimann et al., 1973). Moreover, the sample Dr. yielded somewhat recrystallized specimens of Triasina hantkeni Majzon, indicative of the Rhaetian. The occurrence of these forms in the Bleskovy prameft succession indicates that these strata are younger than the Kossen Beds from Hybe, as it was previously suggested by Kozur (1973b) and Kozur&Mock (1973, 1974c). Maly Mlynsky vrch (Slovak Karst, Zlambach Beds) The Maly Mlynsky vrch hill (456,8 m) is the best locality of Zlambach Beds in the Slovak Karst (cf. Mock, 1973). This hill is situated appr. 1 km east of the village Silickd Brezovd, near to the Slovak-Hungarian boundary. Its surroundings are built up of Upper Triassic limestones of the Silica nappe. In the structure of the Maly Mlynsky vrch hill we can find light massive limestones (so-called Tisovec Limestone), overlain by the typical pink and red Norian Hall-statt Limestones. The topmost beds of this locality consist of Upper Sevatian and Rhaetian Zlambach Beds. These Zlambach Beds have developed from the underlying Hallstatt Limestones quite gradually by accession of the clay component and by change in colour from pink through yellowbrown to grey. In its lower parts the Zlambach Beds are grey micritic limestones, followed by marls or marly slates, and finally by sandy shales. The thickness of the Zlambach Beds is here up to 10 m. The conodonts, holothurian sclerites, and fora-minifers from this locality are listed by Mock (1973) and Kozur&Mock (1974a, b). The residues of the samples of Zlambach Beds with the Lower Rhaetian conodont fauna with Misikella posthernsteini Kozur & Mock and Grodella delicatula (Mosher) have yielded the following foraminifers (determined by Dr. A. Oravecz-Scheffer, Budapest): Ammobaculites rhaeticus Kristan-Tollmann, A. alaskensis Tappan, Ammovertella polygyra Kristan-Tollmann, Glomospira gordialis (Jones & Parker), Haplophragmoides subglobosus (Sars), Hyperamminoides expansus elongatus Kristan-Tollmann, and Trochammina alpina Kristan-Tollmann. The cephalopods that occur in relative abundance, have not yet been studied in detail. The genus Choristoceras is present. During the present studies foraminifers were found in the following samples: Sample MMV-1 — grey, slightly marly micrite from the lower part of the Zlambach Beds: Trochammina alpina Kristan-Tollmann, 1964 — pi. 4, fig. 10, Apathammina ? iranica Zaninetti et al., 1972 — pi. 4, figs. 8, 9, Ophthalmidium sp., and Nodosaria sp. — pi. 4, fig. 7. Associated are the following conodonts and holothurian sclerites: Misikella hernsteini (Mostler), Oncodella paucidentata (Mostler), and Theelia immisorbi-cula Mostler, T. kristanae Mostler, T. petasiformis Kristan-Tollmann, T. simoni Kozur & Mock. The conodonts and holothurian sclerites indicate the upper part of the Upper Sevatian (hernsteini assemblage zone). Sample MMV-2 — Hallstatt Limestone from a small quarry on the northern slope of the Maly Mlynsky vrch: Glomospira sp. — pi. 4, fig. 15, Glomospirella ? sp. — pi. 4, fig. 14, Tolypammina sp., Trochammina alpina Kristan-Tollmann, 1964 — pi. 4, figs. 12, 13, Agathammina austroalpina Kristan-Tollmann & Toll- 6 — Geologija 22/1 mann, 1964, »Vidalina« sp., Nodosaria ordinata Trifonova, 1965, and Nodosaria sp. Associated are the following conodonts and holothurian sclerites: Metapoly-gnathus spatulatus (Hayashi) + ramiform conodonts and Biacumina acanthica (Mostler), Canisia symmetrica (Mostler), Frangerites complexus (Kozur & Mock), Praeeuphronides multiperforatus Mostler, Theelia immisorbicula Mostler, T. planorbicula Mostler, T. zawidzkae Kozur and Mock. The conodonts and holothurian sclerites indicate a Lower to Middle Norian age (spatulatus zone). Sample MMV-3 — grey marly limestone, directly overlying the beds with Misikella hernsteini (Mostler): Glomospirella sp., Trochammina ? sp., Tetrataxis sp., Agathammina austroalpina Kristan-Tollmann & Tollmann, 1964, Ophthal-midium cf. triadicum (Kristan, 1957) — pi. 4, fig. 6, Ophthalmidium sp., and Nodosaria sp. This sample yielded also the conodont Metapolygnathus slovakensis Kozur (cf. Kozur, 1972a, p. 10) and the holothurian sclerites Theelia rosetta Kristan-Tollmann, T. variabilis Zanki, T. heptalampra (Bartenstein), and Calclamna germanica Frizzell & Exline. Age: Lowermost Rhaetian or uppermost Sevatian. Sample MMV-4 — grey marly limestone and marl: Glomospira cf. perplexa Franke, 1936, Glomospira sp., Trochammina alpina Kristan-Tollmann, 1964 — pi. 4, fig. 11, »Vidalina« martana Farinacci, 1959, »Vidalina« carinata (Leischner, 1961) — pi. 4, fig. 2, »Vidalina« carpathica Gaždzicki, n. sp. — pi. 4, figs. 3—5, Ophthalmidium sp., Planiinvoluta carinata Leischner, 1961, Nodosaria sp., Austrocolomia sp., Lenticulina sp., Diplotremina sp., and Turrispirillina cf. minima Pantič, 1967. No conodonts and holothurian sclerites occur in this sample. The foramini-fers indicate an Upper Norian or Rhaetian age. Sample MMV-6 — grey limy marl: Glomospirella cf. pokornyi (Salaj, 1967) — pi. 4, fig. 1, Glomospirella sp., Agathammina austroalpina Kristan-Tollmann & Tollmann, 1964, Ophthalmidium sp., Nodosaria sp., Austrocolomia cf. rhaetica Oberhauser, 1967, and Austrocolomia sp. No conodonts and holothurian sclerites occur in this sample. The foramini-fers indicate the Lower Rhaetian pokornyi & friedli zone. Fischerwiese (Salzkammergut, Zlambach Beds) The Fischerwiese section is situated north of the village Ob. Lupitsch, appr. 6 km northwest of Bad Aussee, Salzkammergut (cf. Kristan-Tollmann, 1964, fig. 1). It is the type locality of the »coral facies« of the Zlambach Beds. These beds are denuded in the brook Korallenbach for a distance of more than 100 m. In its lower part there absolutely dominate soft, dark, clayey and marly schists, higher up there join in dm-thick beds of limestones that are calcarenites to rudites. These limestones are mainly built up of resedimented biogenetic detritus. They are massive, grey to greyviolet rocks resembling limestones from Bleskovy pramefi in the Slovak Karst. Still higher there are several beds filled up by corals and other fossil detritus. A great part of the fauna from this locality, mainly corals, derives from these places of the section. Other macro-fossils — e.g. cephalopods, brachiopods, lameliibranchiates, bryozoans are less frequent (cf. Haas, 1909; Z a p f e , 1967). Stratigraphic important faunal elements are Choristoceras marshi Hauer, Stenarcestes polysphinctus (Mojsiso-vics), Racophyllites neojurensis (Quenstedt), Fissirhynchia fissicostata (Suess), Zugmayerella koessensis (Zugmayer), Trigonia zlambachiensis Haas, Oxytoma inaequivalve (Sowerby), Amblysiphonella steinmanni (Haas), »Thecosmilia« norica Freeh, Montlivaltia norica Freeh, etc. Apart from the macrofossils there also rich microfaunas occur, see Kristan-Tollmann (1964) for foramini-fers and K o 11 m a n n (1963), B o 1 z (1971, 1974) for ostracodes. The newest list of the fauna was completed by Wiedmann (1972). By the finding of Choristoceras marshi Hauer (cf. Z a p f e , 1967) the Rhae-tian age of the Zlambach Beds from the Fischerwiese section was confirmed. B o 1 z (1971) has dated these rocks on the basis of the ostracode fauna as Upper Norian or Rhaetian. The sample 0-18 comes from the higher part of this locality, from a bed of solid grey rudite. Conodonts or holothurian sclerites have not been found in this sample. The following foraminifers could be determined in the sample 0-18: Glomospirella friedli Kristan-Tollmann, 1962 — pi. 3, fig. 1, Tolypammina sp. — pi. 3, fig. 2, Trochammina alpina Kristan-Tollmann, 1964 — pi. 3, fig. 11, Alpino-phragmium perforatum Fliigel, 1967 — pi. 3, fig. 12, Endothyra sp. — pi. 3, figs. 5, 6, Planiinvoluta deflexa Leischner, 1961, Ophthalmidium sp. — pi. 3, fig. 3, Galeanella ? sp. — pi. 3, fig. 4, Miliolipora sp., »Sigmoilina« sp. — pi. 3, figs. 9, 10, Diplotremina cf. subangulata Kristan-Tollmann, 1960 — pi. 3, fig. 7, Diplotremina sp. — pi. 3, fig. 8, Involutina communis (Kristan, 1957), Involutina sp., and Trocholina permodiscoides Oberhauser, 1964. Age: Lower Rhaetian pokornyi & friedli zone. Kendelbachgraben (Osterhorn Group, Kossen Beds) It is the famous, historical profile of Suess & Mojsisovics (1869). There arises here a thick sequence of Upper Triassic and Lower Jurassic outcropped along a distance of more than 600 m. This locality is situated southwest of Wolfgangsee in the side valley of Zinkenbachtal (cf. M o s h e r, fig. 10 and Morbey, 1975, figs. 1—3). The profile starts with a sequence of grey, accentuatedly bedded Plattenkalk with megalodonts (cf. Morbey, 1975, fig. 2). The highest part of the Plattenkalk yielded the sample 0-41 with the following foraminifers: Glomospirella friedli Kristan-Tollmann, 1962, Glomospirella sp. — pi. 2, fig. 8, Trochammina alpina Kristan-Tollmann, 1964, Alpinophragmium perforatum Fliigel, 1967 — pi. 2, fig. 3, Agathammina austroalpina Kristan-Tollmann & Tollmann, 1964 — pi. 2, fig. 4, Nodosaria ordinata Trifonova — pi. 2, fig. 6, Frondicularia xvoodwardi Hochwin, 1895, Involutina communis (Kristan, 1957) — pi. 2, figs. 10—12, Involutina cf. tumida (Kristan-Tollmann, 1964), Involutina minuta Koehn-Zaninetti, 1969, Involutina sinuosa oberhauseri (Salaj, 1967), Involutina gaschei (Koehn-Zaninetti & Bronnimann, 1968), Involutina sp., and Trocholina permodiscoides Oberhauser, 1964 — pi. 2, fig. 13. Age: Lower Rhaetian pokornyi & friedli zone. Immediately above the beds with the sample 0-41 the "classical Rhaetian" starts with thick Kossen Beds in the "Swabian development": thick and thin-bedded limestones, coquinoid limestones, calcareous shales, marls and clayey shales. There is a rich Lower Rhaetian fauna with Rhaetavicula contorta (Port-lock) and other bivalves, higher up also with the brachiopod Rhaetina gregaria (Suess). Above these beds the "Hauptlithodendronkalk" with Thecosmilia follows interbedded with layers of grey limestones with megalodonts. Still higher up are grey limestones with Rhaetina pyriformis (Suess), Oxycolpella oxycolpos (Emmrich), Zeilleria norica (Suess), etc. The highest part of the Rhaetian — the so-called Salzburg facies of Suess — itself distinguishes by the predominance of dark clayey and marly shales over the limestones. Many pyritized specimens of Choristoceras marshi Hauer occur in the black soft shales. Then there follows another short section (covered by detritus) with several beds of dark limestone separated from one another by intercalations of shales. Without a sharp litho-logical break there follow dark limestones of the Liassic with Psiloceras. From the higher part of the Rhaetian with Choristoceras marshi Hauer, M o s h e r (1968) described the conodonts Cypridodella delicatula Mosher and Neospatho-dus lanceolatus Mosher. Foraminifers, conodonts, and holothurian sclerites were found at the present studies in samples collected in the uppermost part of the section, developed in the Salzburg facies. These microfaunas were found in limestones that occur directly below and above the soft shales with Choristoceras marshi. Directly below the soft shales with Choristoceras marshi is a horizon of dark limestones, about 80 cm thick, that is divided into 5 layers ranging from 10—20 cm in thickness. The samples of these limestones have yielded the following faunas: Sample 0-34 — Basal dark limestone layer from the left bank of the brook, 15 cm thick, with Clamys cf. bavarica: Trochammina alpina Kristan-Tollmann, 1964 — pi. 2, fig. 1, Trochammina ? sp. — pi. 2, fig. 2, Cornuspira sp., Nodosaria sp. — pi. 2, fig. 7, Austrocolomia cf. rhaetica Oberhauser, 1967, Austrocolomia sp., and Diplotremina sp. No conodont and holothurian sclerites. Sample 0-35 — Third limestone layer, 10 cm thick: Nodosaria sp. and Lenti-culina sp. Beside of these stratigraphical unimportant foraminifers this sample have yielded stratigraphically significant fauna of conodonts and holothurian sclerites: Grodella delicatula (Mosher), Misikella posthernsteini Kozur & Mock, Neohindeodella dropla (Spasov & Ganev), Parvigondolella n. sp.* and Calclam-na germanica Frizzell & Exline, Fissobractites subsymmetricus Kristan-Tollmann, Theelia heptalampra (Bartenstein), T. rosetta Kristan-Tollmann, T. variabilis Zankl. Footnote 2) * This species has developed from Parvigondolella lata Kozur & Mock. It shows very strong homeomoiphy to the genus Misikella, but Misikella has never denticles behind the main denticle. Moreover, the new species is in all cases accompanied by the same ramiform elements as Parvigondolella, whereas Misikella is apparently a single element species. This new species of Parvigondolella and a new species of Misikella can be served as local guide forms in subzonal rank for the Rhaetian of the Alps to define subzones within the posthernsteini assemblage zone. But unfortunately these species are very rare and until now only present in the Alps, whereas Misikella posthernsteini has a great distribution from New Guinea through the Himalayas to Poland, Slowakia and the Alps. Therefore only Misikella posthernsteini is a suitable guide form for the Rhaetian in an useful conodont zonation. The conodonts and holothurian sclerites indicate a (Lower) Rhaetian age (posthernsteini assemblage zone). Sample 0-36 — Uppermost dark limestone layer, 22 cm thick, directly below the soft shales with Cfioristoceras marshi: Trochammina alpina Kristan-Tol-lmann, 1964, Ophthalmidium sp. — pi. 2, fig. 9, Nodosaria sp., and Frondicularia woodwardi Howchin, 1895. No conodonts and holothurian sclerites. From the dark limestones immediately above the soft shales with Choristo-ceras marshi only one sample (0-38) was investigated. This upper Rhaetian sample has only yielded foraminifers. Sample 0-38 — lowermost dark limestone bed, 20—30 cm thick, directly resting on the soft shales with Choristoceras marshi: Glomospira sp., Glomo-spirella cf. friedli Kristan-Tollmann, 1962, Trochammina alpina Kristan-Tol-lmann, 1964, Nodosaria sp., Lingulina cf. placklesensis Kristan-Tollmann, 1970 — pi 2, fig. 5, and Diplotremina sp. Age: According to the underlying soft shales with Choristoceras marshi the age must be Upper Rhaetian. The problem of the Norian-Rhaetian boundary The Rhaetian stage was introduced by Guembel (1859, 1861). In the German Basin (Franconia) he has put all beds between the top of the red and variegated marls of the Middle Keuper and the basis of the Schlotheimxa angu-lata zone of the Liassic to his Rhaetian stage (for the first time already 1856, see Kozur, 1973b). In the Alpine region he has defined the Rhaetian stage with the Kossen Beds and the zone of Rhaetavicula contort a (Guembel, 1859, 1361) Whereas the upper boundary of Guembel's Rhaetian stage lies in the German Basin within the Liassic (at the basis or in some cases within the Schlotheimia angulata zone) the Lower boundary of the Rhaetian was exactly and universally defined both in the German Basin and in the Alpine region with the basis of the Rhaetavicula contorta zone.* Therefor a clear priority exists for the lower boundary of the Rhaetian stage. Mojsisovics (in: Mojsisovics, Waagen & Diener, 1895) accepted this priority as he introduced the Sevatian substage of his Juvavian (now Norian) stage. According to Mojsisovics, the Sevatian substage includes the (lower) Pxnaco-ceras metternichi and the (upper) "Sirenites" argonautae zones. The age of the Arqosirenites argonautae zone was misinterpreted by Mojsisovics. lhis zone is an equivalent of the middle and upper Himavatites columbianus zone sensu Tozer (= Himavatites columbianus zone in a more restricted scope by Kozur, 1973 a) and belongs according to Kozur (1973 a) to the Lower Seva- Footnote 3> f Rhaetavicvia contorta is unknown (the same is true at many zonal index forms of the Triassic ammonoid zonation, e. g. Rhabdoceras suessi - There-lore!Rha^avicula «mtort« may begin at some places beginning of the Rhaetian. But the Rhaetavicula contorta zone is and Wiedmann (1972, 1974) agree that the Kossen Beds (the typical Rhaetian according to the intentions of Guembel) include the entire Sevatian. Krystyn (1974) even believes that the lowermost Kossen Beds belong probably to the Middle Norian! Regarding not only the ammonoid faunas from scattered incomplete and often technically disturbed sections in the Alps but also the successions and the evolution of the conodonts, holothurian sclerites and other microfossils in continuous profiles Kozur (1973 b) has arrived to a quite different opinion. Within the continuous sections of Canada (published by T o z e r , 1967) 3 horizons with different ammonoid faunas can be noticed within the Rhabdoceras suessi zone (see Tozer, 1967; Kozur, 1973b) that can be recognized also in the Alpin-Mediterranean Tnassic. The lowermost horizon was regarded by Tozer (1967) as lower subzone of the Rhabdoceras suessi zone. From this horizon T o - t z e r (1967) listed Rhabdoceras suessi together with Halorites, Sagenites, Arce-stes", Placites, and Rhacophyllites. This fauna can be correlated with the fauna of the Sagenites giebeli zone that contains beside of Rhabdoceras suessi the stratigraphically important genera Halorites, Sagenites, Hehctxtes, and Stewi-mannitesj but not Cochloceras and Metasibirites. Mojsisovics placed erroneously his Sagenites giebeli zone in the Lower Juvavian (= Lower Norian) stage because this fauna was collected from a fissure filling in older sediments By the aid of ammonoids, but also according to the conodont association (most of the Metapolygnathus bidentatus zone) the Sagenites giebeli zone can be worldwide recognized. Therefore this zone is a useful standard zone within the Sevatian stage. The second ammonoid horizon within the Rhabdoceras suessi zone is characterized by the appearence of the ammonoid genera Cochloceras (including Paracochloceras as subgenus) and Metasibirites. These genera are associated with Rhabdoceras suessi. Most characteristic is the worldwide occurrence of Cochloceras (Paracochloceras) suessi in this horizone (Cochloceras suessi zone* by Kozur, 1973b that replaces the Cladiscites ruber zone by Mojsisovics, see Kozur, 1973b). The Cochloceras suessi zone corresponds to the greatest part of Tozer's upper subzone of the Rhabdoceras su^ zone This upper subzone is characterized according to Tozer (1967) by the following ammonoids: Choristoceras suttonensis, Rhabdoceras suessi, Cochloceras (Paracochloceras) suessi, Cycloceltites cf. C. arduini, Metasibirites sp., Ar-cestes" sp "Cladiscites" sp., Megaphyllites cf. M. insectus, Placites sp., and Rhacophyllites sp. This fauna of the upper subzone of the Rhabdoceras suessi zone is a mixed fauna that derives from different places. Choristoceras suttonensis occurs only in one section in the uppermost Rhabdoceras suessi zone and Tozer (1967 p. 78) has written: "The Sutton Formation... contains an unusual fauna of the suessi zone which includes the genus Choristoceras as well as Rhabdoceras " Beside of Rhabdoceras suessi and Choristoceras suttonensis this fauna includes Megaphyllites cf. insectus and Cycloceltites cf. arduini unknown in deeper parts of the upper Rhabdoceras suessi zone of Canada but not the tvpical association with Cochloceras (Paracochloceras) and Metasibirites. Only this uppermost Rhabdoceras suessi zone sensu Tozer, 1967 (= Choristoceras haueri zone according to Kozur, 1973b) can be recognized in the Lower Rhaetian part of the Zlambach marls and of the Kossen Beds. For this fauna the concurrent occurrence of Rhabdoceras and Choristoceras (Choristoceras) as well as the species Megaphyllites insectus Mojsisovics, M. robustus Wiedemann Cycloceltites arduini (Mojsisovics), Rhaetites rhaeticus (Clark), and Phvllytoceras zlambachense Wiedmann are most characteristic. This "unusual fauna of the Rhabdoceras suessi zone" (Tozer, 1967) is the "usual" ammonoid fauna of the lower and middle part of the type Rhaetian and it belongs according to the priority to the Rhaetian stage. According to Wiedmann (1974) there Footnote 4) . ___, * Tinfortunatelv also from Cochloceras suessi the forerunner is unknown and the rather^re^ict^ occurrence of Cochloceras suessi may be facies-controlled. Therefore in the prSSrt stage 0f our knowledge no clear separation between the Sagenites oiebeU and the Cochloceras suessi zones is possible. But the conodonts and other mi-cr of ossilsfe g holothurian sclerites) indicate a clearly higher position of the Cochlo-feVassues si horizon than at least most of the Sagnttes giebeli zone. is moreover also an overlap in the stratigraphic range of Rkabdoceras suessi and Choristoceras marshi. The lower boundary of the Rhaetian lies above the uppermost Norian Pinacoceras metternichi zone, but within the upper Rkabdoceras suessi zone that is not contemporaneous with the Pinacoceras metternichi zone. By the aid of conodonts (see chapter: Stratigraphic value of microfossils at the Norian-Rhaetian boundary) it could be proved that the first appearence of Choristoceras and the disappearence of Cochloceras, Metasibirites Pinacoceras and other important fossils of the uppermost Rhaetian coincide with the first appearence of Rhaetavicula contorta in the Kossen Beds in its type locality and therefore with the lower boundary of the Rhaetian stage according to the priority (Guembel, 1859, 1861). At this basis of the Rhaetian stage many changes both in the macro- and in the microfaunas occur (see Kozur 1973b). At the ammonoids such very frequent and worldwide distributed genera as Cochloceras and Metasibirites and a lot of species of other genera disappear and Choristoceras (Choristoceras) appears. At the pelecypods a distinct change can be observed characterized e.g. by the disappearence of the worldwide distributed and very frequent Upper Norian genus Monotist by the appearence of the genus Rhaetomegalodon and the dissappearence of many species of Neomegalodon, by the appearence of Rhaetavicula contorta* and some other forms. At the gastropods many Paleozoic elements disappear before the appearence of many new forms at the base of the Jurassic system. A great change can be also observed at this level in the echinoderms (echinoids holo-thurian sclerites). At the brachiopods many Norian elements disappear and many Rhaetian elements appear at the lower boundary of the Rhaetian stage or somewhat higher. In the terrestrial, fresh water, and brackish water deposits many amphibians and reptiles as well as many ostracodes and charo-phytes disappear and some important new groups appear (see Kozur 1974) Very interesting is also the first appearence of mammals at this level The changes m the microfaunas at the Norian-Rhaetian boundary will be discussed boundary^ ^" tratigraphic value of m*crofossils at the Norian-Rhaetian fcm!!0me -f^frkS ^ ne°eSSary t0 the Problem of mixed Norian-Rhaetian faunas with Norian ammonoids and Rhaetian brachiopods and other Rhaetian fossils. This is only a virtual problem. From the plenty of Upper Norian ammonoidI species lesser than 10 Vo (e.g. Rhabdoceras suessi) straddles the Norian-Rhaetian boundary, fewer than at most other stage boundaries Some ammonoids traditionally regarded as Upper Norian elements have moreover typicum in Rhaetian beds, e.g. Choristoceras (Peripleurites) cer^lL ^T8 (PeriVleurites> ^uerzenbaumi, Choristoceras (Choristoceras) haueri. All these species were hitherto unknown from the type Rhaetian Kossen Beds- Therefore all these species were erroneously interpreted as Upper Norian guide forms with an uppermost stratigraphical range up to the uppermost Norian but not higher. On the other hand, in the type Rhaetian Sen Beds many typical Rhaetian brachiopods and pelecypods occur, but ammonoids Footnote 5) note sThe "rSt appearence 01 ^aetavicula contorta may be facies controlled (see foot- are rare or lacking. If we find the above mentioned ammonoids and the contemporaneous brachiopods and pelecypods in suitable facies together in the same layer, than seemingly Norian guide forms (in reality Norian holdovers of Lower Rhaetian age or Lower Rhaetian guide forms erroneously interpreted as Upper Norian ones) and Rhaetian brachiopods or pelecypods occur together. As mentioned above the Rhaetian ammonoid fauna does not consist almost exclusively of Upper Norian holdovers. Many seeming Norian holdovers or even Upper Norian guide forms are in reality Lower Rhaetian guide forms. For instance, the "Late Norian" species of Choristoceras (Choristoceras) have their type locality in Lower Rhaetian Zlambach marls. These species do not occur together with Cochloceras as it could seem from the faunal list for the Zlambach marls given by Mojsisovics (1893). This faunal list contains the ammonoids of Zlambach marls from different localities and of 'different ages (uppermost Norian and Rhaetian). Stratigiaphic value of microfossils at the Norian-Rhaetian boundary The studies on conodonts, holothurian sclerites, ostracodes, and foraminifers were carried out on over 2000 samples of Upper Norian and Rhaetian rocks from sections in the West Carpathians, Hungary, Austria, and the German Basin as well as on some scattered samples from various localities in Europe and Asia. These microfaunal groups comprise several important short-living guide fossils of the Upper Norian and Rhaetian that belong to well-known evolutionary lines. The results of these studies were published by Salaj, Biely & Bystricky (1967), Salaj (1969a,b, 1974, 1977), Bunza & Kozur (1971), Kozur (1971, 1972a. b, c, 1973a, b, c, d, 1974a, b, 1975), Kozur & Mock (1972,1973, 1974a, b, c), K o z u r & M o s 11 e r (1972a, b, c), Kozur & O r a ve c z (1972), Gaždzicki & Zawidzka (1973), G a ž d -z i c k i (1974a, b, 1975), Gaždzicki & Iwanow (1976). The most important results of all these studies are briefly summarized below. Conodonts (see Plate 5) The major part of Sevatian substage (Upper Norian) belongs to the Meta-polygnathus bidentatus zone that may be subdivided in some subzones. The Himavatites columbianus zone (in the restricted scope sensu Kozur, 1973a) and the Sagenites giebeli zone belong to this conodont zone. The Cochloceras suessi horizon or zone comprises the uppermost part of the Metapolygnathus bidentatus zone as well as the Parvigondolella andrusovi and Misikella hern-steini zones. The guide forms of the Rhaetian stage are Misikella posthernsteini and new, but unfortunately very rare and geographically restricted species of Parvigondolella and Misikella that are undescribed until now. Misikella posthernsteini has its first appearence in the uppermost Sevatian, where a complete transitional series to the strongly predominant Misikella hernsteini can be observed. The latter species died out at the Norian-Rhaetian boundary. The evolutionary transition between Metapolygnathus bidentatus and Parvigondolella andrusovi can be also observed in many sections (e.g. Steinbergkogel, Hernstein — both Austria — and Bohufiovo — Slovakian Karst). The existence of evolutionary transition lines both from Metapolygnathus bidentatus to Parvi• gondolella andrusovi and from Misikella hernsteini to Misikella posthemsteini prove that the entire Rhaetian proper (with highly developed species of Parvi-gondolella, more advanced than P. andrusovi, and with Misikella posthemsteini and a further highly developed species of Misikella) is younger than the Se-vatian. The absence of Metapolygnathus bidentatus, Parvigondolella andrusovi, and Misikella hernsteini in the whole Rhaetian is therefore not caused by unsuitable facies, but by the fact that the type Rhaetian Kossen Beds* and other Rhaetian beds are younger than the Metapolygnathus bidentatus zone (that comprise the major part of the Sevatian) and even younger than the Parvigondolella andrusovi and Misikella hernsteini zones of the uppermost Sevatian. Important for the definition of the Norian-Rhaetian boundary is the Stein-bergkogel section (Austria). The uppermost parts of this section displays the evolutionary transition from Misikella hernsteini to Misikella posthemsteini. Here it may be clearly proved that Misikella hernsteini is the forerunner of Misikella posthemsteini and that the distribution of these two species is not controlled by the facies. In a kind letter to one of us (K o z u r) Prof. M o s 11 e r , Innsbruck, has given very interesting new data on the distribution of conodonts in the uppermost Norian and Rhaetian stages. He has also found the evolutionary transition from Misikella hernsteini to Misikella posthemsteini in several sections. Moreover he has sent a table showing the distribution of conodonts in the type section of the Kossen Beds (Weissloferbach, Austria). From this profil we had only two samples with Misikella posthemsteini from the middle Kossen Beds. M o s 11 e r could prove that in Weissloferbach Rhaetavicula contorta and Misikella posthemsteini appear almost contemporaneously in the higher part of the lower Swabian facies and that the range of Misikella posthemsteini extends up to the top of the Choristoceras marshi zone. The conodont datings show that the Kossen Beds from their type locality are younger than the uppermost Sevatian Misikella hernsteini zone. Therefore the view of Krystyn (1974), Tozer (1974), and Wiedmann (1974) that the lower and middle Kossen Beds are contemporaneous with the entire Sevatian (Tozer, 1974, Wiedmann, 1974) or even with the Sevatian and parts of the Middle Norian (Krystyn, 1974) must be rejected. A new species of Misikella described by Mostler (in press) is locally important for the conodont zonation within the Rhaetian Kossen Beds. This species occurs in the Choristoceras marshi zone (except of the upper third of this zone) and in the uppermost part of the Choristoceras haueri zone and it is a very distinctive guide form for this time interval. The range of this species seems to be roughly the same as of Triasina hantkeni and of Choristoceras marshi (cf. Gaždzicki, 1974, 1975, Wiedmann, 1974, and table 1—2). The conodonts are also very important for dating the Zlambach Beds. The Rofimoos section (Austria) is the most important here. Footnote 6) * In the Adnet region the Kossen Beds contain according to Mostler Metapolygnathus bidentatus and Misikella hernsteini in its lower parts. Therefore the Kossen Beds of this region begins earlier (in the same level as the Upper Sevatian part of the Zlambach Beds) than in the type region of the Kossen Beds. The occurrence of Metapolygnathus bidentatus and Misikella hernsteini (= uppermost part of the M bidentatus zone = Upper Sevatian) in the lower Kossen Beds of the Adnet region proves that the absence of these species in the Kossen Beds of the type locality cannot be facies controlled. Table 1. Distribution of conodont guide-species in the Upper Norian and Rhaetian of the Alpine-Mediterranean Triassic STAGE Subsfoge Ammonoid zone Conodont zone 1 Gondolella navioula navioula 2 Gondolella navioula eteinbergeneie 3 Prioniodina sueeti saeeti 4 Mieikella longidentata 5 Mieikella herneteini 6 Misikella posthernsteini 7 Mieikella n.ep. 8 Onoodella paueidentata $ Metapolygnathue abneptis abneptie 10 Metapolygnathue abneptis spatulatue 11 Metapolygnathue poeterus 12 Metapolygnathue tapfei 13 Metapolygnathue multidentatue 14 Metapolygnathue bidentatue 15 Metapolygnathus mosheri 16 Parvigondolella andrueovi 17 Parvigondolella lata 18 Parvigondolella n.ep. NORIAN Alaunion Cyrtopleurites biorenatu8 Metapolygnathue abneptis spatulatue Sevatian Himavatites oolumbianus Sagenitee giebeli Coohlooeras eueset RHAETIAN Lower Chorietooerae haueri Rhabdoeerae euessi Upper Chorietooerae marshi Metapolygnathue bidentatue Subzone I Subzone II Subzone 111 Parvigondolella andrueovi Mieikella herneteini Mieikella posthernsteini -frequent occurrence----rare occurrence The distances in the table 1 are not time-relate d! For instance, the Sagenites giebeli zone comprises a considerably greater part of the Sevatian than the Cochloceras suessi zone. This section displays the uppermost Sevatian (grey limestone bank) and the lowermost Rhaetian (in the facies of the Zlambach marls). Bol z (1974) listed the following ammonoids from the grey limestone bank: Arcestes giganto-galeatus, A. intuslabiatus, Cladiscites tornatus, Cochloceras sp., Megaphyllites insectus, Metasibirites sp., Paracladiscites multilobatus, Pinacoceras metternichi, Placites oxyphyllus, Rhacophyllites neojurensis, and Stenarcestes cf. stibumbilicatus. This fauna is typical of the Cochloceras suessi zone. The samples of the lower part of the section have yielded many conodonts indicative of the upper bidentatus zone. The occurrence of the hernsteini zone seems to be indicated by the concurrent occurrence of Misikella hernsteini and M. posthernsteini (transitional forms to M. hernsteini) in the uppermost grey limestone bank. Because only very few conodonts are known from this level, a somewhat older age is also possible, but the hernsteini zone is certainly present in the grey limestone bank. The overlying Zlambach marls yielded single individuals of Misikella posthernsteini only. Unfortunately conodonts are absent in the samples immediately above the top of the grey limestone bank. B o 1 z (1974) has listed the following ammonoids from the Zlambach Beds above the grey limestone bank: Arcestes ? sp., Megaphyllites robustus, Phyllytoceras zlambachense. This fauna is typical for the Phyllytoceras zlambachense zone according to Wiedmann (1974) that was correlated by Wiedmann (1972) with the Swabian facies of the lower Kossen Beds. The conodont datings probably confirm this correlation. B o 1 z (1974) assigned the grey limestone bank and the Zlambach marls of Rofimoos to the Upper Norian. According to the ammonoid and probably also the conodont datings at least a part of the Zlambach marls of RoBmoos, occurring above the grey limestone bank, belong to the Lower Rhaetian. This section is important as it shows that also very high levels within the Pinacoceras metternichi zone as well as within the more restricted Cochloceras suessi zone (such level is represented by the grey limestone bank) are older than the Rhaetian Misikella posthernsteini zone. The upper range of Pinacoceras metternichi and the genera Cochloceras and Metasibirites coincide with the upper range of Misikella hernsteini, whereas the upper range of Rhabdoceras suessi is very much higher within the Lower Rhaetian Misikella posthernsteini zone. By the aid of conodonts it can be proved therefore that the upper ranges of the Pinacoceras metternichi and Rhabdoceras suessi zones do not coincide. Sometimes the Zlambach Beds also represent the uppermost Norian. We had only one sample of a transition facies between grey Hallstatt Limestone and Zlambach marls with Cochloceras (material form old collections, designated as "Zlambach marl", from unknown locality). This sample has yielded conodonts from the Misikella hernsteini assemblage zone (Misikella hernsteini and Misikella posthernsteini) and thus it represents the uppermost Sevatian. So the stratigraphic range of the Zlambach Beds seems to be the same as that of the Kossen Beds. Kozur & Mock (1973) have demonstrated that the onset of more clastic sedimentation widely spread in the Rhaetian has followed short-lasting tectonical movements in the latest Sevatian and Rhaetian time (contemporaneous in the Alps, Slovakia, and in the German Basin). According to this view it may be expected that the sedimentation of both the Zlambach Beds and the Kossen Beds begins in many cases at the basis of the Rhaetian, but in some places already earlier, in the uppermost Sevatian, or later, within the lowermost Rhaetian. Unfortunately, up to present, no conodonts were found in the lowermost Kossen Beds. Holothurian sclerites As pointed out by Kozur&Mock (1974a) the Sevatian and Rhaetian can be divided into several holothurian assemblage zones: (1) Association with Theelia zawidzkae, Theelia praeseniradiata, primitive Theelia stellijera, and Fissobractites subsymmetricus. Age: Lower Sevatian; Himavatites columbianus zone; lower Metapolygnathus bidentatus zone. (2) Association with Theelia stellijera and Fissobractites subsymetncus without Theelia zawidzkae. Age: Lower Sevatian; Sagenites giebeli zone; middle Metapolygnathus bidentatus zone. (3) Association with highly developed Theelia stellijera, Theelia norica, Theelia seniradiata, Theelia stellijera bistellata, Praeeuphronides robustus, Acanthotheelia kuepperi, Fissobractites subsymmetricus, and first primitive Theelia heptalampra. Age: Upper Sevatian; lower Cochloceras suessi zone; upper Metapolygnathus bidentatus zone. (4) Association with Theelia kristanae together with the same species as in association (3). Age: Upper Sevatian; Cochloceras suessi zone; Parvigondolella andrusovi assemblage zone. (5) Association with Theelia kristanae and Acanthocaudina exlinae. Age: Uppermost Sevatian; upper Cochloceras suessi zone; Misikella hernsteini assemblage zone. . (6) Association with Theelia rosetta, Theelia variabilis, Theelia heptalampra, and Fissobractites subsymmetricus. Age: Rhaetian; Misikella posthernsteini assemblage zone. . At the Norian-Rhaetian boundary there is found one of the greatest breaks in the development of the holothurian sclerites. From over 150 species of holothurian sclerites occurring in the Upper Norian only Fissobractites subsymmetricus, Calclamna germanica, Staurocumites bartensteini, Theelia heptalampra, Priscopedatus triassicus, Theelia rosetta, Theelia variabilis, Uncinuhnoides spicata and probably Achistrum triassicum passed into the Rhaetian. The first 4 species enter also the Liassic. Except for these long-ranging species there are known up to now only 4 other species of typical Rhaetian aspect. The holothurian sclerites that occur in fairly different marine facies are one of the best markers for the Norian-Rhaetian boundary. Ostracodes In the German Basin at the Norian-Rhaetian boundary there is a sharp break in the ostracode fauna (Kozur, 1975). The same is true in Hungary, where in the Rhaetian many ostracodes of Jurassic aspect have appeared and coexisted with some ostracodes of Triassic aspect (Kozur & Oravecz, 1972). According to B o 1 z (1974) in the Alps the Upper Norian and the Lower Rhaetian ostracode fauna is quite equal. But as pointed out above, the "Upper Norian" Zlambach marls of RoSmoos with Phyllytoceras zlambachense and Megaphyllites robustus are Lower Rhaetian and overlie the grey limestone bank of uppermost Norian. Also all other localities discussed by Bolz (1974) — Fischerwiese, Grunbachgraben, Hollgraben and at least parts of the Miihl-graben section that was not sampled by us - are of Lower Rhaetian age. As it can be expected from this fact, the ostracode faunas of all these localities are very similar and differ only slightly because of facial reasons. A new (still undescnbed) Upper Norian ostracode fauna gathered by Kozur differs from the Rhaetian ones also after the elimination of facial differences. In the Rhaetian ostracode fauna primitive members of typical Meso-Cenozoic families appear for the first time (e.g. first Trachyleberididae: Boogaardella, first Cy-therundae: Parariscus). Many genera that appear for the first time in the Khaetian have clearly Jurassic aspects, e.g. Klieana, Boogaardella, Stykella, Aparchitocythere, Parariscus (Kozur, 1973c). Many species and genera, above all holdovers from the Paleozoic or near related forms, disappear near the Norian-Rhaetian boundary and within the Rhaetian. Foraminifers In some sediments where conodonts and holothurian sclerites are rare or absent and the ostracodes cannot be separated from the rocks the foraminifers have yielded most important guide forms. Among the foraminifers the representatives of the family Involutidae Butschli, 1880 have special stratigraphic and paleogeographic importance (Gaždzicki, 1974a, Fig. 11- 1974b tab V see also Salaj, 1969a, b; 1974; 1977). Three foraminifer zones can be recognized from the Middle Norian up to the uppermost Rhaetian (tab. 2; see also G azdzicki, 1974a, 1974b; Salaj, 1974, 1977). These 3 zones are the Semimvoluta clari & Triasina oberhauseri assemblage zone (Alaunian-Sevati-an), the Glomospirella pokornyi & Glomospirella friedli assemblage zone (Lower Rhaetian) and the Triasina hantkeni range zone (? higher Lower Rhaetian, Upper Rhaetian). The Glomospirella pokornyi & Glomospirella friedli assemblage zone could be proved in the samples MMV-6 (Zlambach Beds of Maly Mlynsky vrch) 166/2 (fossiliferous limestone of Bleskov* prame*), 0-18 (Zlambach Beds of Fischer- 1 ("ppfr™st "Plattenkalk" immediately below the Kossen Beds, Kendelbachgraben), 0-38 (upper Kossen Beds, Kendelbachgraben). and in the samples 8-12 from the Kossen Beds of Hybe. Most interesting is the comparison between the faunas of the samples 166/2 (Bleskovy pramefi) and the \ 12 f?^ybe- B°th f3UnaS bel0n* t0 the Lowe7Rhaetian Glomospirella pokornyi & Glomospirella friedli zone, but the occurrence of Galeanella cf tollmanm and Involutina cf. turgida indicates that the sample 166/2 from Bleskoy pramefi (until now regarded as Upper Norian) is younger than the Lower Rhaetian of Hybe as earlier pointed out by K o z ur ^1973b) and O r (1973' T,4c); Interestln* is also the from the sample ttJjT* theFlscherwiese The foraminifer fauna indicates an Early Rhaetian age as it do the ostracode fauna from this locality. Because the Late Rhaetian Choristoceras marshi was also described from this locality, the beds with or ChoZZZ maTShi v11" rePr€Sent °nly thG Uppermost P^ of the section or Choristoceras marshi occurs also in the Lower Rhaetian (as it was inferred by Wiedmann, 1974). The same age as for the Bleskovy prame* limestone Table 2. Upper Norian-Rhaetian foraminifer zonation in the Alpine-Mediterranean Triassic stage Subs tog« Zone Glomospirella pokornyi Glomospirella friedli Semiinvoluta clari Triaeina oberhauseri Triasina hantkeni Glomospirella parallela Trochammina alpina AIpinophragmium perforatum Tetrataxi8 inflata Agathammina? iranioa "Vidalina" martana "Vidalina" oarinata "Vidalina" carpathica Galeanella tollmanni Miliolipora cuvillieri Planiinvoluta deflexa "Sigmoilina" sp. Nodosaria ordinata Turrispirillina minima Involutina communis Involutina tenuis Involutina tumida Involutina sinuosa einuoea Involutina sinuosa oberhauseri Involutina gaschei Involutina minuta Trocholina acuta Trocholina permodiscoides norian Sevatian clari & oberhauseri rhaetian Lower pokornyi S friedli Upper hantkeni For stratigraphic ranges of taxa, definition of the zones and additional comments see S a 1 a j, 1969 a, b, 1974 and G a ž d z i c k i, 1974 a, b ? questionable occurrence is indicated, but an Upper Rhaetian age cannot be ruled out (see remarks to sample 0-38). The fauna of the sample 0-38 is somewhat puzzling. This sample derives from the rocks directly overlying the marls with Choristoceras marshi. Therefore the fauna of the Upper Rhaetian Triasina hantkeni zone rather than the Lower Rhaetian fauna of the Glomospirella pokornyi & Glomospirella friedli assemblage zone should be expected in this sample. Because Glomospirella friedli markedly enters the Triasina hantkeni range zone, it is possible that the sample 0-38 represents the Triasina hantkeni range zone (Upper Rhaetian), but the index form is absent because of facial reasons. The fauna of the sample 0-41 from the uppermost part of the "Plattenkalk" immediately below the Kossen Beds of Kendelbachgraben is also very important. The sample 0-41 taken just below the base of the Kossen Beds should be of Middle Norian age, if the correlations of the lower and middle Kossen Beds with the entire Sevatian (T o z e r, 1974; W i e d m a n n , 1974) or even with the entire Sevatian and a part of the Middle Norian (Krystyn, 1974) are correct. The rich fauna of the Glomospirella pokornyi & Glomospirella friedli assemblage zone in the sample 0-41 demonstrates that the uppermost "Plattenkalk" of Kendelbachgraben is most probably of Early Rhaetian age or at least not older than latest Sevatian. This dating confirms the view of Kozur (1973b) that most of the Kossen Beds are of Rhaetian age and younger than the uppermost Sevatian as it can be proved also by conodonts and holothurian sclerites (see above). The Triasina hantkeni range zone was only indicated in the sample Dr. from the Bleskovy pramen locality. This is very interesting, because the ammonoid fauna of this locality was hitherto erroneously assigned to the Sevatian (Upper Norian) substage. It may be that Triasina hantkeni already occurs in the upper part of Lower Rhaetian, so that perhaps the range of this species comprises both the upper part of the Lower Rhaetian and the Upper Rhaetian. But on the other hand parts of the Bleskovy pramefi limestone may be already Upper Rhaetian and the never confirmed record of Choristoceras marshi (Sturzen-b a u m , 1879) may be correct. Also the fauna from the sample Dr. proves that the strata from the Bleskovy pramefi locality are of Rhaetian age and younger than the Lower Rhaetian of Hybe. Some remarks to the papers of Hohenegger & Filler (1975) and Bystricky (1975) Hohenegger & Piller (1975) have assigned Glomospirella friedli Kristan-Tollmann, 1962, G. parallela Kristan-Tollmann, 1964, and G. expansa Kristan-Tollmann, 1964 to the genus Involutina. This may be correct, but it is beyond the matter of this paper to discuss this problem. Involutina gaschei (Koehn-Zanmetti & Bronnimann, 1968) is certainly not an younger synonym of Glomospirella friedli Kristan-Tollmann, 1962, because the stratigraphic range of these two species is quite different, so that the differences between these two species are not facies-controlled as supposed by Hohenegger & P111 e r (1975), but true species differences. The stratigraphic importance of Late Triassic foraminifers was recently questioned by Bystricky (1975), which is in contradiction with the data available. It should be noted that the marked stratigraphic value of the fora- minifers and especially of the representatives of the families Ammodiscidae and Involutinidae from the uppermost Triassic is connected with their rapid evolution. A fairly good knowledge of internal structure, phylogenetic relations, ecology, and paleogeography of the foraminifers is highly advantageous here (see Gaždzicki, 1974a, b; S a 1 a j , 1974, 1977; Z a n i n e 11 i, 1976). Moreover, the succession of foraminifer faunas was reconstructed on the basis of highly complete sections of the Upper Triassic from the Alpine region. Therefore, foraminifer datings are fairly reliable. By s tricky (1975) has questioned the stratigraphic value of foraminifers for the zonation of the Upper Triassic with the reference to the foraminifer succession in the Hybe profil. However, this section is technically disturbed and the succession of layers is still the matter of controversy (see Goetel, 1917; Michalik, 1973; Bystricky, 1975). According to Bystricky (1975) also the conodonts have no value for stratigraphic subdivisions in the uppermost Norian and Rhaetian. In this connection Bystricky (1975) reconstructed "contradictions" in conodont datings comparing older and newer papers and views of conodont workers. In this respect the remarks of Bystricky (1975) are pure polemic and therefore not worthy to discuss. Bystricky (1975) has not noticed that not the conodont datings, but the stratigraphic schemes were changed and that the former Spathognathodus hernsteini Mostler was revised and subdivided by Kozur & Mock (1974a, b) into Misikella hernsteini (Mostler) and M. posthernsteini Kozur & Mock. Thus, the "contradictions" in the conodont datings reconstructed by Bystricky (1975) are in reality the result of the scientific progress in the Upper Triassic stratigraphy and conodont taxonomy. The same is true for the great number of such "contradictions" in the papers of Bystricky (compare e.g. the papers of Bystricky 1972, 1973 and appendix to the latter paper with regard to the stratigraphy of the Upper Triassic of Silicka Brezova). Some remarks are necessary to special views in the paper of Bystricky (1975) that contradict the above mentioned stratigraphic results from our micropaleontological studies at the Norian-Rhaetian boundary. (1) The so-called "conodontenfreier Bereich" (cf. Huckriede, 1958; Kozur, 1971; Kozur & Mock, 1972) was not considered as an equivalent of a biozone by these authors as assumed by Bystricky (1975). Meanwhile Misikella posthernsteini and some other conodonts were found in this stratigraphic level and the posthernsteini assemblage zone was established for this stratigraphic level and the post-hernsteini fauna by Kozur & Mock (1974c). (2) According to Bystricky (1975) there are no considerable changes in the conodont, ostracode, holothurian, brachiopod, and ammonoid faunas at the Norian-Rhaetian boundary (with references to Urlichs, 1972; Mo-sher, 1968; Sweet u.a., 1971; Pearson, 1970, Dagis, 1974, and Kozur, 1972c). Urlichs (1972) has investigated only Rhaetian ostracode faunas of the Kossen Beds at Weifiloferbach, the type locality of the Rhaetian Kossen Beds. He assigned the lower and middle part of this section to the Upper Norian (because of the occurrence of Rhabdoceras suessi). In our view, discussed above, the whole section of the Kossen Beds at Weifiloferbach is Rhaetian 7 — Geologija 22/1 (perhaps with exception of the lowermost beds, where no conodonts and ostracodes were found and Rhaetavicula contorta is still absent). The "Norian" part (sensu U r 1 i c h s) of the Kossen Beds from Weifiloferbach contains Misikella posthernsteini, and new highly developed species of Misikella and Parvigondo-lella, the typical Rhaetian conodont fauna. The conodont association of the Misikella posthernsteini assemblage zone together with Rhabdoceras suessi, Choristoceras ammonitijorme, typical Rhaetian brachiopods, and pelecypods (e.g. Rhaetavicula contorta) indicate a Lower Rhaetian age (Choristoceras haueri zone) for this part of the section. Therefore U r 1 i c h s (1972) has not compared Upper Norian and Rhaetian ostracodes, but Lower Rhaetian ostracodes with Upper Rhaetian ones. The Lower and Upper Rhaetian ostracode faunas are, of course, very similar, but clearly different from the true Upper Norian ostracode faunas. Kozur (1972c) has also still assigned the uppermost Rhabdoceras suessi zone to the Upper Norian sensu Tozer (1967). The "Upper Norian" ostracodes by Kozur (1972c) were found in the uppermost Rhabdoceras suessi zone. According to Kozur (1973b) this part of the Rhabdoceras suessi zone is contemporaneous with the Lower Rhaetian Choristoceras haueri zone. Therefore the "Upper Norian" ostracodes by Kozur (1972c) have the same Lower Rhaetian age as the "Upper Norian" ostracodes described by U r 1 i c h s (1972). It is clear that these ostracode faunas are very similar to other Rhaetian ostracode fauna, but there are great differences to the true Upper Norian ostracode faunas (see chapter: Stratigraphic value of microfossils at the Norian-Rhaetian boundary). The view of Bystricky (1975) that the very rich Upper Norian holothurian fauna had passed into the Rhaetian is nowhere confirmed (neither in published nor in unpublished material — in the contrary in all published papers the great differences between the Norian and Rhaetian holothurian faunas were emphasized) and unsubstantiated. The differences between the Upper Norian and Rhaetian ammonoid faunas are considerable (see chapter: The problem of the Norian-Rhaetian boundary), in spite of the fact that some species straddles the Norian-Rhaetian boundary (e.g. Rhabdoceras suessi). In contrary to the references by Bystricky (1975) already the papers of Mosher (1968) and Sweet et al. (1971) show very clearly the great break in the conodont faunas between the Norian and Rhaetian. Mosher (1968, fig. 12) listed 22 conodont species in the Sevatian (not all range up to the Norian-Rhaetian boundary), but only 4 in the Lower Rhaetian. This break is in reality still greater, because "Neospathodus lanceolatus" comprises two species, the Upper Norian Misikella hernsteini and the uppermost Norian to Rhaetian Misikella posthernsteini. Moreover, there are some highly developed hitherto undescribed species of Misikella and Parvigondolella in the Rhaetian that are unknown in the Norian. Dag i s (1974, tab. 3) showed that at the Norian-Rhaetian boundary 32 brachiopod genera died out and 3 genera have their first appearence at the base of the Rhaetian (the latter number may by considerably higher, if the Norian--Rhaetian boundary will be revised in all areas). Moreover, Dag is (1974, p. 272) pointed out that in all sections of northwestern Caucasus a sharp, not facies-controlled change in the brachiopod fauna occurs above the beds with Monotis caucasica and Norian brachiopods. Above these Upper Norian beds a rich brachiopod fauna occurs that is very similar to the brachiopod fauna of the Kossen Beds and to the fauna of Drnava (Bleskovy pramen). The am-monoid fauna of this region was regarded as Upper Norian, but it consists of Norian holdovers that are frequent in the Lower Rhaetian (e.g. Megaphyllites insectus, Rhacophyllites debilis, Placites polydactylus). Thus, in contrary to the view of Bystricky (1975), Dag is (1974) has shown considerable changes in the brachiopod fauna at the Norian-Rhaetian boundary. Pearson (1970) accepted the "Plattenkalk"-Kossen Beds boundary as Norian-Rhaetian boundary, but he assumed that Rhabdoceras suessi has the same upper range as the genus Cochloceras and that Rhabdoceras suessi is older than the Kossen Beds or it ranges only up to the lowermost brachiopod horizon of the Kossen Beds (below the first appearence of Rhaetavicula contorta). The newest results (U1 r i c h s , 1972) have shown however that Rhabdoceras suessi occurs together with Rhaetavicula contorta and it is absent only in the upper third of the Kossen Beds. Therefore Pearson (1970) assigned the uppermost Rhabdoceras suessi zone to the Norian, but the lower and middle Kossen Beds with Rhaetavicula contorta and Rhaetian brachiopods (contemporaneous to the uppermost Rhabdoceras suessi zone) to the Rhaetian. For this reason many Rhaetian guide forms of the brachiopods were regarded as Upper Norian by Pearson (1970), if the beds were placed in the uppermost Rhabdoceras suessi zone by ammonoids (e.g. Bleskovy pramen, post-Monotis beds of northwestern Caucasus). (3) Bystricky (1975, p. 183) has erroneously equated the post-hernsteini fauna of Kozur&Mock (1972) with the posthemsteini assemblage zone (Kozur & Mock (1974c). The post -hernsteini fauna is the conodont fauna immediately above the Misikella hernsteini assemblage zone. The Misikella posthemsteini assemblage zone comprises both the post -hernsteini fauna and the formerly recognized "conodontenfreien Bereich" of the uppermost Triassic, in which now conodonts were found (above all Misikella posthemsteini). Therefore it is not correct, if Bystricky (1975) pointed out that the "conodonten-freier Bereich" of the uppermost Triassic follows above the Misikella posthemsteini assemblage zone. In reality Jurassic beds follow above the Misikella posthemsteini assemblage zone. (4) Bystricky (1975, p. 184) pointed out that in the posthemsteini assemblage zone of Maly Mlynsky vrch Gondolella navicula, Metapolygnathus bidentatus, Misikella hernsteini, and Oncodella paucidentata occur together with Misikella posthemsteini in the same beds at the same locality. This is quite incorrect. In Maly Mlynsky vrch are some outcrops with conodonts of the spatulatus assemblage zone, the upper bidentatus range zone, the hernsteini assemblage zone, and the posthemsteini assemblage zone. Metapolygnathus bidentatus, Misikella hernsteini, Oncodella paucidentata, and Gondolella navicula were not reported from the Misikella posthemsteini assemblage zone, but from the underlying zones. In the Misikella posthemsteini zone only the index species was found. In one sample taken from the beds between the Misikella hernsteini and Misikella posthemsteini assemblage zones Metapolygnathus slova-kensis, Grodella delicatula, and Prioniodina (Cypridodella) muelleri were found, but never the species mentioned by Bystricky. (5) Bystricky (1975, p. 187) pointed out that the relation of the horizon with Misikella hernsteini and the horizon with Misikella posthernsteini at the locality Hybe, "so important for the stratigraphy", is unclear. He has not noticed that the former M. hernsteini of Hybe is in reality M. posthernsteini as pointed out by Kozur & Mock (1974c). Therefore in Hybe do not exist a fauna with "Spathognathodus" hernsteini and Misikella posthernsteini as Bystricky assumed, but only a fauna with Misikella posthernsteini. In this respect it is very interesting that Bystricky has repeatedly pointed out that the position of "Spathognathodus" hernsteini in the Hybe section is clear, but the stratigraphie position of M. posthernsteini is unclear. This seems to be only polemic, because it should be quite clear that the known stratigraphie level of "Spathognathodus" hernsteini from Hybe does not change with taxonomic revision of this species. Therefore it is surprising, if Bystricky (1975, p. 190) wrote: "Without precise data on the occurrence of the fauna, which are unconditionally necessary in stratigraphy, consequently also the indication of the occurrence of Misikella posthernsteini Kozur & Mock is not more valuable than the rejected presence of the species ? Gondolella navicula Huckriede". Description of the new species ? Family Fischerinidae Millett. 1898 ? Subfamily Cyclogyrinae Loeblich & Tappan, 1961 ? Genus Vidalina Schlumberger, 1900 "Vidalina" carpathica Gaždzicki, sp. n. PI. 4, figs. 3—5 H o 1 o t y p e : The specimen presented in pi. 4, fig. 4. Type horizon: Zlambach Beds (Upper Norian-Rhaetian). Type locality: Maly Mlynsky vrch (Slovak Karst), Czechoslovakia. Derivation of the name: carpathica — after the Carpathians. Diagnosis: Test discoidal, somewhat flattened, with distinct central swell and always with keel. Wall calcareous, imperforate. Coiling planispiral, involute, probably nonseptate; 3—4 whorls in the spire. The last whorl separated from central part by deep constrictons. Material: 10 well-preserved individuals. Association: With Glomospira cf. perplexa, Glomospirella sp., Trochammina alpina, Agathammina austroalpina, "Vidalina" carinata, Nodosaria ordinata, Austrocolomia sp., and Diplotremina sp. Description: Test calcareous, imperforate, elongate, consisting of relatively large, spherical proloculus and tubular second chamber with well-marked keel. Whorls 3—4 in number; coiling planispiral, involute, bilaterally symmetrical. Axial section displaying the central part (proloculus and first 2—3 whorls) with characteristic central swell, separated from the last whorl by marked constrictions (pi. 4, fig. 4—5). Deuteroloculus circular in outline (pi. 4, fig 5). Sharp keel especially well-developed along the last whorl (pi. 4, fig. 3—5). Dimensions of the test: diameter: 280—320^, thickness: 60 jum, diameter of the proloculus: about 30 /mi. Remarks : The new species "Vidalina" carpathica Gaždzicki, sp. n. differs from all other Late Triassic and Liassic "Vidalina" in the last whorl separated from the central part with deep constrictions, especially well-displayed by axial sections (pi. 4, figs. 4—5). The small number of individuals precluded an accurate identification of the forms "A" and "B". The size of the proloculus and the number of the whorls appear almost identical in all the forms available; it is assumed that they all represent the form "B". It is highly probable that these individuals could loose their last whorl at the deep constrictions. The remaining central part appears to be very similar to the form "A" of the species "Vidalina" carinata (Leischner) — Neoangrulodiscus carinatus (Leischner) = Jnvolutina carinata Leischner (cf. pi. 1, fig. 1 herein, and Leischner, 1961, pi. 2, figs. 15 a—d) recorded from the Norian-Rhaetian and primarily from the Lower Liassic of the Tethyan areas (Leischner, 1961; Kristan-Tol-lmann, 1962; Bronnimann, Poisson & Zaninetti, 1970). Occurrence : Known from the type locality only. Conclusions The entire Kossen Beds of their type locality (perhaps with exception of the lowermost part where Rhaetavicula contorta and conodonts are absent) are Rhaetian in age and younger than the Sevatian substage of the Upper-Norian stage. The Zlambach Beds are contemporaneous with the Kossen Beds and begin at some places within the uppermost Sevatian (? upper Metapolygnathus Indebitatus zone, Misikella hernsteini assemblage zone in the conodont zonation; Cochloceras suessi zone in the ammonoid zonation by Kozur, 1973 b). The major part of the Rhabdoceras suessi zone is older than the Kossen Beds. Rhabdoceras suessi straddles the Norian-Rhaetian boundary and occurs also in the lower and middle parts of the Rhaetian, here together with the genus Choristoceras. The Rhabdoceras suessi zone is inconvenient as standard zone. The upper range of the index species R. suessi exceeds the upper range of Pinacoceras metternichi, the index species of the metternichi zone, and therefore it straddles the Norian-Rhaetian boundary. Therefore the Rhabdoceras suessi zone should be rejected and replaced by the Sagenites giebeli zone (corresponding to the lower subzone of the Rhabdoceras suessi zone by Tozer, 1967), the Cochloceras suessi zone (Upper Sevatian corresponding to great parts of Tozer's upper subzone of Rhabdoceras suessi zone), and the Choristoceras haueri zone (Lower Rhaetian corresponding to the uppermost part of the Rhabdoceras suessi zone by Tozer, 1967). The Norian-Rhaetian boundary between the Cochloceras suessi and Choristoceras haueri zones agrees with the priority and is characterized by an important faunal change both in the macro- and micro-faunas. The dating of the Glomospirella pokornyi & GlomospirelZa friedli assemblage zone as Lower Rhaetian (Gaždzicki, 1974) is confirmed. Also by the aid of foraminifers could be proved that the »Sevatian« of Bleskovy pramen is younger than the Lower Rhaetian of Hybe as it was previously suggested by Kozur & Mock (1973, 1974c). The uppermost "Plattenkalk" of Kendelgraben belongs to the Glomospirella pokornyi & Glomospirella friedly assemblage zone and therefore it probably represents the basal Rhaetian, being certainly not older than uppermost Sevatian. This disagrees with the views of Krystyn (1974), Tozer (1974), and W i e d m a n n (1974) that the Kossen Beds include the entire Sevatian or even parts of the Middle Norian (Krystyn, 1974) and confirms the view of K o -z u r (1973 b) that the typical Kossen Beds (not the lower Kossen Beds of the Adnet region) are younger than the uppermost Sevatian. Only the lowermost parts of the typical Kossen Beds (without Rhaetavicula contorta and conodonts) may locally represent the uppermost Sevatian. Plate 1 Samples from Bleskovy pramefi (fig. 1-5) and Hybe (fig. 9), Czechoslovakia 1 »Vidalina« cf. carinata (Leischner); sample 166/5-D<, x 300. 2—3 »Vidalina« martana Farinacci; 166/2, X 150. 4 Ophthalmidium sp.; 166/2, x 70. 5 Ammobaculites sp.; 166/3-Dx, X 60. 6 Galeanella cf. tollmanni (Kristan); 166/2, x 100. 7 Diplotremina ? sp.; 166/2, x 100. 8 Triasina hantkeni Majzon; Dr., X 60. 9 Triasina oberhauseri Koehn-Zaninetti & Bronnimann; sample Hybe 12, X 130. All photos taken by Dr. A. Gaždzicki Plate 2 Samples from Kendelbachgraben, Austria 1 Trochammina alpina Kristan-Tollmann; 0-34, X 250. 2 Trochammina ? sp.; 0-34, X 250. 3 Alpinophragmium perforatum Fliigel; 0-41, X 40. 4 Agathammina austroalpina Kristan-Tollmann & Tollmann; 0-41, X 100. 5 Lingulina cf. placklesensis Kristan-Tollmann; 0-38, X 150. 6 Nodosaria ordinata Trifonova; 0-41, X 150. 7 Nodosaria sp.; 0-34, X 250. 8 Glomospirella sp.; 0-41, X 150. 9 Ophthalmidium sp.; 0-36, X 250. 10—12 Involutina communis Kristan; 0-41, 10, 12 — X 90, 11 — X 70. 13 Trocholina permodiscoides Oberhauser; 0-41, X 90. Plate 3 All specimens from sample 0-18 (Fischerwiese, Austria) I Glomospirella friedli Kristan-Tollmann, X 130. 2 Tolypammina sp., X 60. 3 Ophthalmidium sp., X 150. 4 Galeanella ? sp., x 150. 5—6 Endothyra sp., X 60. 7 Diplotremina cf. subangulata Kristan-Tollmann, x 8 Diplotremina sp., X 60. 9—10 >►Sigmoilina« sp., X 150. 11 Trochammina alpina Kristan-Tollmann, X 150. 12 Alpinophragmium perforatum Fliigel, X 40. Plate 4 AU samples from Maly Mlynsky vrch (Slovakian Karst) 1 Glomospirella cf. pokornyi (Salaj), MMV-6, X 200. 2 »Vidalina« carinata (Leischner); MMV-4, X 150. 3—5 »Vidalina« carpathica Gaždzicki sp. n. (fig. 4: holotype); MMV-4, x 150. 6 Ophthalmidium cf. triadicum (Kristan); MMV-3, X 200. 7 Nodosaria sp.; MMV-1, X 200. S—9 Agathammina ? iranica Zaninetti, Bronnimann, Bozorgnia & Huber- MMV-1 X 300. 20—13 Trochammina alpina Kristan-Tollmann: 10 — MMV-1, X 250, 11 — MMV-4, X 250; 12, 13 — MMV-2, X 200. 14 Glomospirella ? sp.; MMV-2, X 300. J5 Glomospira sp.; MMV-2, X 200. Plate 5 1, 2 Misikella posthernsteini Kozur & Mock, fig. 1: posterior view; fig. 2: lateral view; Lower Rhaetian (pokornyi & friedli foraminifer zone, Misikella posthernsteini conodont zone), Choč nappe, Chocholowska Valley at the foot of Siwiaft-skie Turnie (western part of the Tatra Mts., Poland). 200 X. 3—7 Misikella hernsteini (Mostler), figs. 3 a, 4—6: lateral view; figs. 3 b, 7: upper view; all from the uppermost Sevatian of Hernstein, Austria (Bed C 1 according to Mostler, Oberhauser & Plochinger, 1987), Misikella hernsteini conodont assemblage zone. 83 X. 8, 9 Parvigondolella andrusovi Kozur & Mock, lateral view, Upper Sevatian, Parvi-gondolella andrusovi conodont assemblage zone; fig. 8: Bohuiiovo (Silica nappe, Slovakian Karst), 100 X; fig. 9: Silicka Brezova (Silica nappe, Slovakian Karst), 60 X. 10—12 Metapolygnathus bidentatus (Mosher); figs. 10 a, 12: lateral view; figs. 10 b, 12: upper view; all from the upper Metapolygnathus bidentatus conodont zone (Middle Sevatian) of Silickž Brezovš (Silica nappe, Slovakian Karst); fig. 10: platform quite reduced, only lateral denticles are present, sample S 1, 60 X; figs. 11, 12: platform still well developed, sample S 19, 100 x. 13 Metapolygnathus mosheri (Kozur & Mostler), a) lateral view, b) upper view; upper Metapolygnathus bidentatus conodont zone (Middle Sevatian), Silicka Brezova (Silica nappe, Slovakian Karst), sample S 17, 60 X. 14 Metapolygnathus posterus (Kozur & Mostler), a) lateral view, b) upper view, middle Metapolygnathus bidentatus zone (Lower Sevatian), Silickž Brezova (Silica nappe, Slovakian nappe, Slovakian Karst), sample S 30, 60 X. 25 Metapolygnathus zapfei Kozur. a) lateral view, b) upper view, Sommeraukogel (Austria), »Hangen'drotkalk«, lower Metapolygnathus bidentatus conodont zone (Lower Sevatian), 60 x. 16 Metapolygnathus abneptis spatulatus (Hayashi), upper view of an aberrant specimen, near to the holotype of this subspecies, lower Metapolygnathus bidentatus conodont zone (Lower Sevatian), Silicka Brezovd (Silica nappe, Slovakian Karst), sample S 16, 60 x. 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