284STRATIGRAPHICALLY IMPORTANT LOWER NORIAN CONODONTS FROM THE CS VÁRBOREHOLE (CSV-1), HUNGARY – COMPARISON WITH THE CONODONT SUCCESSION OF

THE NORIAN GSSP CANDIDATE PIZZO MONDELLO (SICILY, ITALY)

VIKTOR KARÁDI1 , HEINZ W. KOZUR2 AND ÁGNES GÖRÖG1

1 Pázmány Péter sétány 1/c, Eötvös Loránd University, Faculty of Science, Department Palaeontology, H-1117 Budapest, Hungary, email:kavik.geo@gmail.com; 2 Rézsü u. 83, H-1029 Budapest, Hungary, e-mail: kozurh@helka.iif.hu

Abstract—We investigated the lower part (360-522 m) of the cherty limestones of the Cs vár Limestone Forma-tion in the Cs vár borehole (Csv-1) for conodonts. The interval below 404 m was assigned to the upper Carnianby Góczán in Haas et al. (1997); our conodont studies indicate that this level lies in the upper Epigondolellatriangularis Zone within the upper part of the lower Norian. The Carnian-Norian boundary instead lies near thebase of the cherty limestones at 522 m. The lowermost 6 m of the cherty limestones have yielded only a fewconodonts at 520 m. These are only early juvenile Epigondolella that cannot be exactly assigned to a species, butprobably the age does not differ from the conodonts at 516 m, where primitive Epigondolella quadrata Orchard,E. rigoi Kozur and Metapolygnathus mazzai Karádi, Kozur and Görög n. sp. occur that can be assigned to thelowermost Norian. Thus, the Norian base lies more than 112 m (and probably 116 m) below the Norian baseassumed in Haas et al. (1997). The position of the Carnian-Norian boundary is discussed in detail. In the GSSPcandidate sections at Pizzo Mondello (Sicily, Italy) and Black Bear Ridge, British Columbia, Canada, this bound-ary interval lies between the youngest Carnian and the oldest Norian ammonoids. The best primary markers for theNorian base are conodonts and Halobia austriaca (Mojsisovics). Conodonts are preferred as primary marker forthe Norian base. The most suitable is the FAD of Epigondolella rigoi in the middle of the Carnian-Norian boundaryinterval. It nearly coincides with the LOD of Metapolygnathus echinatus sensu Orchard (2007). Good proxies forthe base of the Norian are the FAD of Metapolygnathus parvus Kozur, M. echinatus sensu Orchard (2007), theLOD of M. echinatus sensu Orchard (2007), the FAD of Carnepigondolella gulloae Mazza and Rigo, and the LODof Metapolygnathus communisti Hayashi and of M. parvus. Also, the general change of a Carnepigondolella (andMetapolygnathus) dominated conodont fauna with few primitive Epigondolella to a Epigondolella (andNorigondolella) dominated fauna with few remaining Metapolygnathus and Carnepigondolella is good evidence forthe position of the Carnian-Norian boundary. We describe two new species, Metapolygnathus mazzai Karádi,Kozur and Görög n. sp. and Oncodella mostleri Karádi, Kozur and Görög n. sp.

INTRODUCTION

In northern Hungary, east of the River Danube and south of theCserhát Mountains, horsts of Mesozoic basement are exposed. Thisarea is the easternmost part of the Transdanubian Range Unit. One of thebetter outcrops sections is at the Cs vár quarry (also known as Pokolvölgyquarry) near the village of Cs vár (Fig. 1). A borehole was drilled in thelate 1960s at the old quarry in the Kecskés Valley (or Pokol Valley) at thesouthern forefront of Castle Hill (Vár-hegy). Haas et al. (1997) dividedthe 1200 m deep Csv-1 core into three parts. Below 622 m there is astrongly deformed dolomitic complex. Between 622 and 522 m are dark-grey, cherty beds of the Pokolvölgy Dolomite that rest tectonically onthe underlying dolomite complex. At its upper boundary this unit gradesto the grey, cherty limestones of the Cs vár Limestone Formation thatconstitute the upper 522 m of the core. The borehole sequence continuesupward to the uppermost Rhaetian at the surface in the old quarry. Thepelagic limestones continue upward into the lowermost Hettangian abovethe quarry and up to the Sinemurian at the upper part of the Castle Hill.

The beds of the Cs vár Limestone Formation represent reef slopeand basinal environments. A similar facies occurs in the Buda Mountainsat Mátyás-hegy and surroundings southeast of the Buda Line. TheseNorian cherty dolomites and Rhaetian cherty limestones, named theMátyáshegy Formation by Haas and Kovács (1985), formed in a mar-ginal basin position while the Cs vár Limestone Formation shows char-acteristics of deep water deposition.

FIGURE 1. Location of Cs vár in Hungary and the Cs vár borehole nearthat village, modified after Korte and Kozur (2011). TR stands forTransdanubian Range.

Tanner, L.H., Spielmann, J.A. and Lucas, S.G., eds., 2013, The Triassic System. New Mexico Museum of Natural History and Science, Bulletin 61.

285Kovács (1983) claimed that all the Cs vár core material was pro-

cessed, so that none was still available for conodont research, but he wasonly partly correct. After documentation, parts of the core were sepa-rated and stored in paper bags that represent single samples or shortintervals of the borehole (mainly 2 to 3 m intervals). In one case a 6.7 m-thick interval is preserved, but it contains only two species, Epigondolellatriangularis (Budurov) and Neohindeodella summesbergerisummesbergeri Kozur and Mostler, which indicates no faunal mixing.For 10 of the samples, the exact position in the borehole is known, andfor 7 more samples placement can be made within short intervals (seeFig. 2). In the sample interval, the samples have a uniform fauna withoutfaunal mixing because of the high sedimentation rate. In one case lowerNorian conodonts occur together with lower Rhaetian conodonts, butthis appears to be caused by a fissure filling, because the lower Rhaetianconodonts occur more than 350 m higher than the lower Norian con-odonts. In the immediately underlying sample, the lower NorianNorigondolella navicula (Huckriede) occurs, and the 8 overlying samplesalso contain only lower Norian conodonts. In thin sections the matrixand the fissure filling is sharply separated. Excluding this anomalouscase, the remaining material was sufficient for our investigations. Theaim of the present study is the analysis of the lower part of the Cs várLimestone Formation between 520-368.5 m in the borehole, which con-sists of grey limestones and dolomitic limestones with common chertnodules. The investigated sequence yields rich conodont and holothuriansclerite faunas along with some sponge spicules, echinoderm spines andfish teeth.

PREVIOUS WORK

The Upper Triassic succession of the Csv-1 borehole and theUpper Triassic–Lower Jurassic sections of the Cs vár quarry and CastleHill have been the subject of several studies. The Mesozoic formationsfrom Cs vár were first mentioned by Szabó (1860) who suggested anEarly Jurassic age for these rocks. It was Vadász (1908, 1910) whodescribed the cherty limestones of the area and placed them in the Carnianon the basis of fossils.

The drilling of the Cs vár borehole (in 1968-1969) led to a betterunderstanding of the geological setting of the area. Three Hungarian ge-ologists, Jámbor, Nagy and Detre took part in the description of the core.At the Cs vár quarry Detre and Nagy found ammonoids and nautiloidsidentified as Badiotites eryx (Münster), Apleuroceras sp. ex. gr. sturi(Mojsisovics), Clionitites sp. and Michelinoceras cf. politum (Klipstein).According to Detre (1969, 1970, 1971) the presence of these fossilsconfirmed an early Carnian age of the oldest beds in the section, anopinion that was supported by Krystyn on an excursion to Cs vár,though later he recognized that Clionitites occurs also in the upper Norian.Detre (1971) described specimens of Halobia styriaca (Mojsisovics),assigned at that time to the lower Carnian (now lower Norian) from theCs vár borehole, between 347.4-352.4 m. Between 403.5-406.2 m heidentified Daonella pichleri Mojsisovics and Halobia cassiana(Mojsisovics) and regarded them as indicators of the Ladinian/Carnianboundary interval.

In 1970, Detre provided one of us (Kozur) some material from theupper Halobia-bearing level for micropaleontologic research. The plat-form conodonts of this sample were erroneously identified by Kozurand Mostler (1973) as the lower Carnian Budurovignathus mostleri(Kozur) and Budurovignathus diebeli (Kozur and Mostler) at a timewhen most of the lower Norian platform conodonts were not yet de-scribed. However, the microfossils found by Kozur and Mostler (1973)in all samples collected in the Cs vár quarries had unexpected results, forsurface outcrops turned out to be Rhaetian, thought to be uppermostSevatian at that time. Later this age was supported by the Sevatianammonite Clionitites nicetae Diener found by Kozur and identified byKrystyn (Detre, 1981). Similarly, Detre (1981) mentioned contempo-rary studies that pointed out that Halobia styriaca is typical of thelowermost Norian, instead of being found in the lower Carnian.

Balogh (1981) introduced the name Cs vár Limestone Formationfor the cherty limestones that form the section of the quarry and theupper 522 m of the borehole. He used the term “Pokolvölgy dolomite”for the cherty dolomites representing the middle unit of the core (522-622 m).

After new fossil finds by Detre et al. (1988), including 6 speci-mens of Choristoceras nobile Mojsisovics, the Rhaetian (in that paperstill given as Sevatian) age of the Cs vár quarry was undoubted. Thedetailed conodont investigations of Kozur and Mock (1991) showed thepresence of all three Rhaetian conodont zones in the Cs vár LimestoneFormation at the main quarry. In addition they described Neohindeodelladetrei Kozur and Mock from this locality; this is the youngest conodontspecies in the world as it ranges up into the lowermost Jurassic. In thesame paper they suggested dividing the Cs vár Limestone Formationinto two formations on the basis of their somewhat different facies. Intheir proposed stratigraphy, the dark limestones and cherty limestonesof the borehole, as well as the dark, bituminous limestone and chertylimestone beds of the Cs vár quarry and the lowermost part of theCastle Hill, would remain the Cs vár Limestone Formation, while thelighter-colored limestones and rare cherty limestones of the main part ofthe Castle Hill (Vár-hegy) section became the Várhegy Cherty Lime-stone Formation. The former belongs to the Norian-Rhaetian and thelatter is Hettangian-Sinemurian. They also concluded that the Cs várLimestone Formation is the time and facies equivalent of the Rhaetiancherty limestones of the Buda Mountains, southeast of the Buda Line,named by Balogh (1981) as the “Mátyáshegy limestone.” Balogh sepa-rated the “Mátyáshegy limestone” from the cherty dolomites of theBuda Mountains, also southeast of the Buda Line, and named the latterthe Sashegy Dolomite Formation. Later Haas and Kovács (1985) namedthe Mátyáshegy Formation, which included both the Sashegy DolomiteFormation and the “Mátyáshegy limestone,” and placed the whole for-mation within the Carnian. Kozur and Mock (1991) documented a num-ber of misconceptions that went into this interpretation and listed thereasons why the Mátyáshegy Formation cannot be accepted.

Haas et al. (1997) made detailed investigation on the sequence ofthe borehole and the sections of the Cs vár quarry, including microfaciesanalysis and micropaleontological research. The authors proposed toincorporate the cherty dolomitic unit of the core into the Cs vár Lime-stone Formation as its lower member, applying the name PokolvölgyDolomite Member as established by Balogh (1981). The foraminiferfauna of the upper 350 m of the core was studied by Haas et al. (1997),who also made a palynological study on the lower and middle part of theCs vár Limestone Formation. On the basis of sporomorphs, they placedthe Carnian/Norian boundary at 404.0 m. It should be noted that belowthe presumed Carnian/Norian boundary there is a nearly 60 m interval inwhich no index fossils and almost no sporomorphs were found. There-fore the actual location of the boundary was totally uncertain and needsto be revised.

More emphasis was placed recently on the Triassic/Jurassic bound-ary, so the surface outcrops increasingly became the focus of investiga-tions (Haas and Tardy-Filácz, 2004; Pálfy et al., 2007; Götz et al., 2009;Korte and Kozur, 2011).

POSITION OF THE NORIAN BASE WITHINTHE INTERNATIONAL TRIASSIC SCALE

The base of the Norian is not yet officially fixed by the Interna-tional Stratigraphic Commission and it is not even yet proposed by theSubcommission on Triassic Stratigraphy. However, two GSSP candi-dates for the definition of the Norian base are under consideration, PizzoMondello in western Sicily (Italy) and Black Bear Ridge on WillistonLake in northeastern British Columbia (Canada).

Tozer (1965) defined the base of the Norian by ammonoids, usingthe base of the Mojsisovicsites kerri Zone (now Stikinoceras kerri Zone),which corresponds to the base of the Guembelites jandianus Zone in theTethys (Krystyn, 1980). All later proposals with other fossil groups

286

FIGURE 2. Section of the upper half of the Cs vár borehole. Location of samples and the range of the species present are shown.

287establish a base close to this boundary. It is difficult to define the Norianbase by ammonoids within a phylogenetic cline. Moreover , both GSSPcandidates are poor in ammonoids, and therefore the base of the S. kerriZone or of the G. jandianus Zone cannot be defined precisely in thesesections or in any other section of the world. In Pizzo Mondello, theyoungest Carnian ammonoids belong to the Gonionotites italicus Subzoneof the Anatropites spinosus Zone. This subzone is the youngest am-monoid subzone of the Tuvalian. The highest level of this subzone is atthe top of the level PMAM22bis, somewhat below conodont samplePM25 studied by Muttoni et al. (2004) about 80 m above the base of thesection (Balini et al., 2012). The first Norian ammonoids from theDimorphites noricus Subzone occur in the level NA42 (somewhat belowthe conodont sample PM31 studied by Muttoni et al., 2004), about 99.5m above the base of the section.

In the Black Bear Ridge section ammonoids are documented byonly a few specimens. The uppermost Carnian Klamathites macrolobatusZone is documented by a single specimen of Anatropites cf. maclearniTozer. More than 5 m higher is the Discostyrites ireneanus-Subzone(lower Stikinoceras kerri Zone, correlative with the lower Guembelitesjandianus Zone: Balini et al., 2012). This subzone is documented byGuembelites clavatus (McLearn), which is restricted to this subzone(Balini et al., 2012). The interval between the uppermost Carnian andlowermost Norian ammonoid faunas has yielded only ammonoids thatrange through the Carnian-Norian boundary. Because there is no othersection in the world where uppermost Carnian ammonoid faunas areimmediately overlain by lowermost Norian ammonoid faunas, Balini etal. (2012, p. 47) are correct in stating, “ammonoids will not provide theprimary marker event for the definition of the GSSP of the Norian, butthey are crucial for the selection of the most significant events based onother groups.”

Thus, the Carnian-Norian boundary should be in the interval be-tween the highest Carnian and the lowermost Norian ammonoid occur-rences in Pizzo Mondello and Black Bear Ridge. This is the case for thefirst occurrence of Halobia austriaca (Mojsisovics) and for a distinctturnover in the conodont faunas that can be observed at the first appear-ance datum (FAD) and the last appearance datum (LAD) of severalconodont species. The first occurrence of H. austriaca is regarded byKrystyn (2010), Levera and McRoberts (2010) and Levera (2012) as aprimary marker for the Norian base. It can be observed both in PizzoMondello and in Black Bear Ridge. However, it is not clear whether thisspecies begins exactly at the same level in Pizzo Mondello and in BlackBear Ridge. At Pizzo Mondello it begins 11.5 m above the FAD ofMetapolygnathus parvus and 9.25 m above the FAD of Metapolygnathusechinatus sensu Orchard (2007). This latter species does not correspondto Metapolygnathus echinatus (Hayashi, 1968), but it is an independentspecies which is present both at Black Bear Ridge and at Pizzo Mondello.In the following, this species is designated Metapolygnathus “echinatus.”It is notable that the FOD of Halobia autriaca is in Pizzo Mondellodistinctly above the LOD of M. “echinatus” and close to the LOD of M.parvus. Orchard (e.g., 2007, 2010) made careful studies of the conodontranges at Black Bear Ridge, and Mazza et al. (2012a) carefully studiedthe conodont ranges of Pizzo Mondello. According to these studies, atboth Black Bear Ridge and at Pizzo Mondello M. parvus begins a littlebefore M. “echinatus” and ranges somewhat higher up than M.“echinatus.” For this reason and by comparison with the ranges of otherconodont species, the ranges of M. parvus and M. “echinatus” can beregarded as true ranges and not as facies-controlled occurrences. At BlackBear Ridge H. austriaca begins immediately above the FAD of M. parvus(Mazza et al., 2012a), close to the FAD of M. “echinatus.” This meansthat H. austriaca begins somewhat later at Pizzo Mondello than at BlackBear Ridge. At Pizzo Mondello the FAD of H. austriaca is within a longinterval with relatively high and nearly constant carbon isotope values(Nicora et al., 2007), while at Black Bear Ridge, the FOD of H. austriacaoccurs within a small negative carbon isotope perturbation. Therefore,the carbon isotope values indicate that the FOD of H. austriaca is not

exactly at the same level in the Pizzo Mondello section as it is at BlackBear Ridge. However, these differences in the carbon isotope trends mayresult from the fact that 13Ccarb was measured at Pizzo Mondello,while 13Corg was measured at Black Bear Ridge. The conodont rangesare supported by the FAD and LAD of several other conodont speciesclose to the FAD of one species. The FAD of H. austriaca can be onlydetermined by the first occurrence of this species and it is not confirmedby FAD or LAD of other halobiids. Moreover, around the Carnian-Norian boundary, conodonts are more widely distributed than halobiids.Despite the fact that Levera (2012) regarded H. austriaca as a primarymarker for the lowermost Norian, he reported several occurrences of H.austriaca within the late Carnian. Thus, the FOD of H. austriaca can beused only as a rough proxy for the Carnian-Norian boundary, which liessomewhat above the conodont boundary interval at Pizzo Mondello andwithin this interval at Black Bear Ridge. As a primary marker for theNorian base, the FAD of a conodont should be chosen that occurs both atPizzo Mondello and at Black Bear Ridge and lies at the base, top orwithin the Carnian-Norian boundary interval of Mazza et al. (2012a; seebelow). It should occur in suitable facies in the entire low latitude regionsof Tethys and Panthalassa, and also in western North America, which forthe most part was in the middle latitudes (except the low-latitude BajaCalifornia region, which has similar faunas to the low latitude Tethys andlow latitude Panthalassa regions).

Numerous data on the Norian conodont stratigraphy and the po-sition of the Carnian-Norian conodont boundary were published fromthe Pizzo Mondello section (Muttoni et al., 2001, 2004; Nicora et al.,2007; Mazza et al., 2009, 2010, 2011, 2012a,b; Balini et al., 2010, 2012;Levera, 2012). As in the Black Bear Ridge of British Columbia, a strongfaunal turnover occurred close to the Carnian-Norian boundary in thePizzo Mondello section. The latest Carnian platform conodont fauna,dominated by Carnepigondolella and Metapolygnathus with only a fewprimitive Epigondolella, is replaced by a lower Norian fauna dominatedby Epigondolella, Norigondolella, and only rare last Metapolygnathus,and a few last Carnepigondolella. These significant changes do not occurat one specific horizon, but over a short interval of about 10 m, named byMazza et al. (2012) as the Carnian-Norian boundary interval. This inter-val lies entirely within the interval between the last Carnian ammonoidsand the first Norian ammonoids, but it is somewhat shorter than thisinterval. Immediately below the base of the boundary intervalMetapolygnathus praecommunisti Mazza, Rigo and Nicora disappears,and at the base of the boundary interval M. parvus Kozur appears. Alittle above the base of the boundary interval M. “echinatus” appears.The same succession of the FAD of the latter two species occurs also atBlack Bear Ridge (Orchard, 2010) and therefore these are probably trueFADs. Probably also the LOD of M. praecommunisti is at the same levelat both Black Bear Ridge and at Pizzo Mondello, but for a long time thisspecies was incorrectly assigned at Black Bear Ridge to M. communistiHayashi and so the exact range of M. praecommunisti at Black BearRidge cannot be recognized from the literature.

Orchard (2007, 2010) proposed the base of the M. “echinatus”Zone as the base of the Norian. This definition has some obvious advan-tages. According to Orchard (2010) the FAD of M. parvus and M.“echinatus” are close to the base of the S. kerri Zone and both speciesoccur both in the Tethys and in North America. However, there is adistinct competition between Metapolygnathus and Carnepigondolella/Epigondolella (Mazza et al., 2010). Where Carnepigondolella/Epigondolella are common, Metapolygnathus is rare and sometimes evenabsent. This is the case in the Cs vár borehole. Carnepigondolella andmainly Epigondolella are very common, but with the exception ofMetapolygnathus mazzai n. sp., Metapolygnathus is absent. WhereMetapolygnathus is common, Carnepigondolella/Epigondolella are rare,but never absent. Therefore the Norian base should be defined by aspecies of Epigondolella. Most suitable is the FAD of Epigondolellarigoi Kozur. This species begins in the middle of the boundary interval.Where both Metapolygnathus and Epigondolella/Carnepigondolella are

288present, E. rigoi begins somewhat above M. echinatus sensu Orchard(2007) and immediately after the disappearance of this species. There-fore the FAD of M. “echinatus” and of the more common M. parvus canbe regarded as good proxies for the base of the Norian. The short-rangingMetapolygnathus linguiforms Hayashi begins somewhat before E. rigoiand ends somewhat after the FAD of E. rigoi. According to Orchard(personal commun.), primitive representatives of E. rigoi occur also atBlack Bear Ridge. Similarly, at Pizzo Mondello, E. rigoi is representedby primitive forms in the boundary interval.

At the top of the boundary interval, Carnepigondolella gulloaeMazza and Rigo appears. A little later M. communisti and M. parvusdisappear. None of these events can be used to define the base of theNorian. C. gulloae is generally rare and in many sections missing, as forexample in the lower Norian of the Cs vár borehole.

In summary, we propose the FAD of Epigondolella rigoi as pri-mary marker for the base of the Norian. A good proxy is the FAD of M.parvus, M. “echinatus” and the distinct turnover of the entire conodontfauna in the Carnian-Norian boundary interval (see Mazza et al., 2012a).

SYSTEMATIC DESCRIPTIONS

All illustrated material is deposited in Eötvös Loránd University,Faculty of Science, Department Palaeontology, H-1117 Budapest, Hun-gary.

Most of the species present in the lower Norian of the Cs várborehole were well described and documented in Mazza et al. (2012a).Therefore, only two new species need to be described. We generallyagree with the other determinations, but Norigondolella trinacriae Mazza,Cau and Rigo, 2012 is, based on the development of its lower side, not aNorigondolella but instead probably a Paragondolella.

Genus Metapolygnathus Hayashi, 1968

Type species: Metapolygnathus communisti Hayashi, 1968.

Metapolygnathus mazzai Karádi, Kozur and Görög n. sp.Pl. 1, Figs. 5, 8

2010 Metapolygnathus cf. primitius - Balini et al., pl. 3, fig. 92012a Metapolygnathus cf. primitius - Mazza et al., pl. 8, fig. 12

Derivatio nominis: In honor of Dr. Michele Mazza, Milan, forhis excellent research on Upper Triassic conodonts.

Holotype: The specimen illustrated by Mazza et al., 2012a, pl. 8,fig. 12; rep.-no. MPUM 9690 residing in the Dipartimento di Scienzedella Terra "A. Desio" (Università degli Studi di Milano).

Locus typicus: Pizzo Mondello (western Sicily, Italy).Stratum typicum: Cherty limestone, sample FNP 134, upper-

most part of the Carnian-Norian boundary interval (Mazza et al., 2012a,Fig. 2).

Material: About 90 specimens.Diagnosis: The unreduced part of the platform is slender, about

half of the entire length of the entire element or insignificantly more,straight or laterally curved. The anterior platform margin bears on oneside two to four, and on the other side three to five elongated nodes toshort denticles. Posterior to the lateral nodes the platform margin isflattened and depressed and has no nodes, but the margins are thick. Thispart of the platform is moderately long. The posterior end of the plat-form is blunt, straight or somewhat oblique, partly also with a slightmiddle incision. The upper surface of the platform, including the nodes,is covered by a microreticulation. The free blade is well developed, has 5-9 denticles and has a convex upper profile. It descends onto the platform.The cusp is unexceptional in size or a little larger than the foregoingdenticles of the carina, which continues after the cusp with two to three,relatively large, widely separated nodes. The basal cavity lies in or some-what before the middle of the unreduced platform. The keel terminationis mostly irregularly bifurcated.

Occurrence: Uppermost Carnian and lower part of lower Norianof Pizzo Mondello. Lower part of lower Norian of the Cs vár borehole.

Remarks: Despite the fact that we have well preserved speci-mens from the Cs vár borehole, we have chosen the holotype fromPizzo Mondello. When a new species is present in surface outcrops andin boreholes, the holotype should be taken from the surface outcrop.

Specimens of this species were formerly assigned to Metapoly-gnathus cf. primitius (Mosher, 1970) to which they are most similar. M.primitius is distinguished by a longer and narrower posterior platformand a longer posterior carina. The forerunner of M. mazzai is M.mersinensis Kozur and Moix from the uppermost Carnian. It has stron-ger upturned platform margins, and the basal cavity lies always under themiddle of the platform.

Genus Oncodella Mosher, 1967

Type species: Hindeodella paucidentata Mostler, 1967.

Oncodella mostleri Karádi, Kozur and Görög n. sp.Pl. 1, Fig. 14

Derivatio nominis: In honor of Prof. Dr. Helfried Mostler,Innsbruck, for his excellent micropaleontological research.

Holotype: The specimen shown in Pl. 1, Fig. 14; rep.-no. 477-44.Locus typicus: Cs vár borehole.Stratum typicum: Cherty limestone of the Cs vár Limestone

Formation at 477 m, lower Norian.Material: One specimen.Diagnosis: Anterior bar with a very large, backward-curved den-

ticle, followed by three to four backward-inclined small denticles andimmediately in front of the cusp by a very large, backward-curved den-ticle. The cusp is broader, but not longer than the largest denticles on theanterior bar, strongly backward-curved. The posterior bar is shorter thanthe anterior bar and has no denticles. The lower side has an elongatedbasal cavity below the cusp and posterior bar. The basal furrow is broadunder the posterior half of the anterior bar, becomes narrower against theanterior end of the anterior bar and is very narrow and disappears towardthe anterior end of the bar under the large terminal anterior denticle.

Occurrence: So far only known from the stratum typicum (lowerNorian).

Remarks: Oncodella paucidentata (Mostler, 1967) has only onevery large terminal denticle on the anterior bar, and the posterior bar hastwo denticles.

POSITION OF THE NORIAN BASE IN THE CS VÁR (CSV-1)BOREHOLE: CORRELATION WITH THE LOWER NORIAN

CONODONT SUCCESSION OF THE NORIAN GSSP CANDI-DATE PIZZO MONDELLO

Haas et al. (1997) presented the first biostratigraphic subdivisionof the entire cherty limestone interval of the Cs vár Limestone Forma-tion in the upper 522 m of the Cs vár (Csv-1) borehole. Only foramini-fers and sporomorphs were used despite the fact that the borehole isvery rich in conodonts, holothurian sclerites and partly in radiolarians,all very important for Norian and Rhaetian stratigraphy. The first fora-minifers appear at 411.3 m, and stratigraphically important foraminifersoccur only from the level above 354 m. Therefore, foraminifers could beused neither for biostratigraphic investigations within the lower Noriannor for the definition of the Carnian-Norian boundary. Diverse associa-tions of sporomorphs occur in some levels of the cherty limestone asso-ciations and are also present between 461 m and 474 m in the lower partof the cherty limestone. However, between 404 m and 461 m there is aninterval about 57 m thick that is barren of sporomorphs or contains onlya very few, stratigraphically unimportant species. At 404 m a diverseNorian sporomorph association occurs. As the samples below this levelare mainly barren of sporomorphs, it is hard to understand why Haas et

289al. (1997) placed the base of the Norian at this level. Even the diversesporomorph association from the interval of 461 m to 474 m, below thisbarren interval, consists only of species that occur both in the upperTuvalian and in the lower Norian without any species restricted to theupper Tuvalian. Below 474 m down to the base of the cherty limestoneat 522 m, the basal cherty limestones are again barren of sporomorphs.

The Norian base designated by Haas et al. (1997) is, according toour conodont data, in the upper (but not uppermost) part of theEpigondolella triangularis Zone, well above the base of the upperTuvalian. Here we found a lower Norian conodont fauna withEpigondolella quadrata Orchard, Epigondolella rigoi Kozur,Epigondolella vialovi Burij, Metapolygnathus mazzai n. sp. andNeohindeodella summesbergeri summesbergeri Kozur and Mostler. Evenour second oldest conodont fauna at 516 m, 6 m above the base of thecherty limestone, has a lower Norian fauna with E. quadrata, E. rigoi, E.vialovi Burij and Metapolygnathus mazzai n. sp. Our oldest conodontfauna at 520 m has probably the same age. This fauna is very close to thebase of the Norian, so the base of the Norian probably lies close to thebase of the cherty limestones at 522 m. At this horizon (close to the baseof the Norian) a distinct transgression can be observed in many sectionsof the northern Tethys.

Our conodont studies show that the base of the Norian in theborehole Cs vár (Csv-1) lies at least 112 m, and probably 116 m, deeperthan determined (by Góczán) in Haas et al. (1997). Our new age determi-nations were possible only due to the excellent work by Mazza et al.(2012a) on the conodont distribution in the Norian GSSP candidatesection at Pizzo Mondello, which has a very dense sampling intervalacross the upper Tuvalian and lower Norian and provides a comprehen-sive revision of the conodont taxonomy in this interval. The lower Norianconodont ranges in our borehole are very similar to the conodont rangesin the lower Norian of the Norian GSSP candidate section at PizzoMondello. Even such details as the occurrence of “Norigondolella”trinacriae Mazza, Cau and Rigo in the lowermost range of E. triangu-laris (Budurov) and E. uniformis Orchard can be found both at PizzoMondello and in our borehole. Thus, the Norian GSSP candidate PizzoMondello is very suitable for detailed correlation with other sections,even when they are far away and represent a different facies, such as theblack, bituminous cherty limestones in the case of the Cs vár borehole.

CONCLUSIONS

In the Cs vár (Csv-1) borehole we investigated the conodontsuccession in the lower cherty limestone of the Cs vár Limestone For-mation in the interval from 378 m to 522 m. There was a very richconodont and holothurian sclerite succession in this interval, of whichwe studied only the conodonts. In future papers we will describe the

conodonts from 0 to 360 m (uppermost lower Norian to Rhaetian), theholothurian sclerites of the entire borehole, and the excellently preservedRhaetian radiolarians. The lower Norian conodont fauna shows the sameranges found in the Norian GSSP candidate section at Pizzo Mondello.By this we could show that the Norian base is not at 404 m as assumedin Haas et al. (1997), but much deeper, at 516 m, where the lowest richconodont fauna of surely early Norian age occurs, or possibly somewhatdeeper, as at 520 m, where there is a poor fauna of probably early Norianage. Seemingly, the Norian base nearly coincides with the base of thecherty limestone at 522 m, at a level where a transgression is indicated inthe northern Tethys. The conodont succession of the Cs vár (Csv-1)borehole will be important in the future for the exact correlation of lowerNorian sporomorph associations with the conodont zonation.

The position of the Norian base cannot be defined by ammonoids,but in the Norian GSSP candidate sections at Pizzo Mondello and BlackBear Ridge it can be constrained to an interval between the uppermostoccurrence of latest Tuvalian ammonoids and earliest Norian ammonoids.Within this interval it has been suggested that the Norian base should bedefined by a primary marker, either Halobia austriaca or conodonts.Halobia austriaca cannot be used as primary marker, however, becauseits first appearance occurs at slightly different levels in Pizzo Mondelloand Black Bear Ridge (somewhat later FO at Pizzo Mondello). Even so,the FAD of Halobia austriaca is a reasonable proxy for the base of theNorian. We prefer the FAD of Epigondolella rigoi as the primary markerof the Norian base. The FAD of either Metapolygnathus parvus or M.“echinatus” would be a good primary marker, but there is a competitionbetween Carnepigondolella/Epigondolella and Metapolygnathus. WhereCarnepigondolella or Epigondolella are very common Metapolygnathusis rare or sometimes missing, even in very rich samples. WhereMetapolygnathus is very common, Carnepigondolella/Epigondolella arerare, but never missing in rich samples. Therefore it seems to be better todefine the Norian base by the FAD of an Epigondolella species and notwith a Metapolygnathus species. Nevertheless, where the FADs of M.parvus or M. “echinatus” are present, they are very good proxies for thebase of the Norian, and are readily recognizable both in the Pizzo Mondelloand Black Bear Ridge GSSP candidate sections.

ACKNOWLEDGMENTS

We thank very much Dr. Michele Mazza, Milano, for importantdiscussions about Upper Triassic conodont taxonomy, ranges of theconodonts in the uppermost Carnian and lower Norian and a carefulreview of the paper. We thank also very much Dr. Manuel Rigo, Univer-sity fo Padova, Italy, for his careful review of the paper and to Dr. RobertE. Weems, U.S. Geological Survey, Reston, Va. , USA for improving theEnglish.

REFERENCES

Balini, M., Bertinelli, A., Di Stefano, P., Guaiumi, C., Levera, M., Mazza,M., Muttoni, G., Nicora, A., Preto, N. and Rigo, M., 2010, The lateCarnian-Rhaetian succession at Pizzo Mondello (Sicani Mountains):Albertiana, v. 39, p. 36-57.

Balini, M., Krystyn, L., Levera, M. and Tripodo, A., 2012, Late Carnian-Early Norian ammonoids from the GSSP candidate section PizzoMondello (Sicani Mountains, Sicily): Rivista Italiana di Paleontologia eStratigrafia, v. 118, p. 47-84.

Balogh, K., 1981, Correlation of the Hungarian Triassic: Acta GeologicaAcademiae Scientiarum Hungaricae, v. 24, p. 3-48.

Detre, Cs., 1969, A csovár-nézsai triászrögök slénytani vizsgálatánaklegújabb eredményei: slénytani Viták, v. 11, p. 9-17.

Detre, Cs., 1970, slénytani és üledékföldtani vizsgálatok a Cs vár, Nézsaés Keszeg környéki triász rögökön: Földtani Közlöny, v. 100, p. 173-184.

Detre, Cs., 1971, Néhány új smaradvány a cs vári alsókarni rétegekbol:MÁFI Évi Jelentése az 1969. Évr l, p. 447-451.

Detre, Cs., 1981, A Duna-balparti triász rögök rétegtani helyzete: MÁFIÉvi Jelentése az 1979. Évr l, p. 81-95.

Detre, Cs., Dosztály, L. and Hermann, V., 1988, A cs vári felso-nóri, sevatifauna: MÁFI Évi Jelentése az 1986. Évr l, p. 53-67.

Götz, A. E., Ruckwied, K., Pálfy, J. and Haas, J., 2009, Palynological evi-dence of synchronous changes within the terrestrial and marine realm atthe Triassic/Jurassic boundary (Cs vár section, Hungary): Review ofPalaeobotany and Palynology, v. 156,p. 401-409.

Haas, J. and Kovács, S., 1985, Lithostratigraphical subdivision of the Hun-garian Triassic: Albertiana, v. 4, p. 5-15.

Haas, J. and Tardy-Filácz, E., 2004, Facies changes in the Triassic–Jurassicboundary interval in an intraplatform basin succession at Cs vár(Transdanubian Range, Hungary): Sedimentary Geology, v. 168, p. 19-48.

290Haas, J., Tardi-Filácz, E., Oravecz-Scheffer, A., Góczán, F. and Dosztály, L.,

1997, Stratigraphy and sedimentology of an Upper Triassic toe-of-slope and basin succession at Cs vár, North Hungary: Acta GeologicaHungarica, v. 40/2, p. 111-177.

Hayashi, S., 1968, The Permian conodonts in chert of the Adoyama For-mation, Ashio Mountains, central Japan: Chikyu Kagaku (Earth Sci-ence), v. 22, p. 63-77.

Korte, C. and Kozur, H., 2011, Bio- and chemostratigraphic assessment ofcarbon isotope records across the Triassic–Jurassic boundary at Cs várquarry (Hungary) and Kendlbachgraben (Austria) and implications forglobal correlations: Bulletin of the Geological Society of Denmark, v.59, p. 101-115.

Kovács, S., 1983, A magyarországi conodonta-vizsgálatok eddigi eredményei(a bükki triász kivételével): slénytani Viták, v. 30, p. 73-111.

Kozur, H. and Mock, R., 1991, New Middle Carnian and Rhaetian con-odonts from Hungary and the Alps. Stratigraphic importance and tec-tonic implications for the Buda Mountains and adjacent areas: Jahrbuchder Geologischen Bundesanstalt, v. 134/2, p. 271-297.

Kozur, H. and Mostler, H., 1973, Mikrofaunistische Untersuchungen derTriasschollen im Raume Cs vár, Ungarn: Verhandlungen der Geo-logischen Bundesanstalt, v. 1973(2), p. 291-325.

Krystyn, L., 1980, Stratigraphy of the Hallstatt region; in Schönlaub, H.P.,ed., Second European Conodont Symposium (ECOS II), Guidebook, Ab-stracts: Abh. Geol. Bundesanstalt, v. 35, 69-98.

Krystyn, L., 2010, Long distance marine biotic correlation events aroundthe Carnian-Norian boundary. New Developments on Triassic Inte-grated Stratigraphy, Program and Abstracts, p. 30-31.

Levera, M., 2012, The halobiids from the Norian GSSP candidate section ofPizzo Mondello (western Sicily, Italy): Systematics and correlations:Rivista Italiana di Paleontologia e Stratigrafia, v. 118(1), p. 3-45.

Levera, M. and McRoberts, C., 2010, Halobiid bivalves as a tool for highresolution correlation between Carnian-Norian succession in Tethys andPanthalassa: A potential datum for a base-Norian GSSP: New Develop-ments on Triassic integrated Stratigraphy, Program and Abstracts, p.34-35.

Mazza, M., Cau, A. and Rigo, M., 2012b, Application of numerical cladisticanalyses to the Carnian-Norian conodonts: A new approach for phylo-genetic interpretations: Journal of Systematic Palaeontology, doi10.1080/14772019.2011.573584 + 7 pages Online SupplementaryMaterial.

Mazza, M., Furin, S., Spötl, C. and Rigo, M., 2010, Generic turnovers of theCarnian/Norian conodonts: Climatic control or competition?: Palaeogeo-graphy, Palaeoclimatology, Palaeoecology, v. 290, p. 120-137.

Mazza, M., Rigo, M. and Cau, A., 2009, Evolutionary patterns and phylog-eny of the Carnian/Norian conodonts from the Pizzo Mondello section,GSSP candidate for the base of the Norian: Permophiles, v. 53, suppl. 1,p. 30-31.

Mazza, M., Rigo, M. and Gullo, M., 2012a, Taxonomy and biostratigraphicrecord of the Upper Triassic conodonts of the Pizzo Mondello section(western Sicily, Italy), GSSP candidate for the base of the Norian; inProceedings of the Palermo Workshop "New developments on TriassicIntegrated Stratigraphy" Palermo, September 12-16, 2010, RivistaItaliana di Paleontologia e Stratigrafia, v. 118, p. 85-130.

Mazza, M., Rigo, M. and Nicora, A., 2011, A new Metapolygnathus plat-form conodont species and its implications for Upper Carnian globalcorrelations: Acta Palaeont. Pol., v. 56, p. 121-131.

Mosher, L.C., 1968, Triassic conodonts from western North America andEurope and their correlation: Journal of Paleontology, v. 42, p. 895-946.

Mosher, L.C., 1970, New conodont species as Triassic guide fossils: Journalof Paleontology, v. 44, p. 737-742.

Mostler, H., 1967, Conodonten und Holothuriensklerite aus aus den norischenHallstätter Kalken von Hernstein (Nierösterreich): Verh. Geol. B.-A.Wien 1967(1/2), p. 54-64.

Muttoni, G., Kent, D.V., Di Stefano, P., Gullo, M., Nicora, A., Tait, J. andLowrie, W., 2001, Magnetostratigraphy and biostratigraphy of theCarnian/Norian boundary interval from Pizzo Mondello section (SicaniMountains, Sicily): Palaeogeography, Palaeoclimatology, Palaeoecology,v. 166, p. 383-399.

Muttoni, G., Kent, D.V., Olsen, P.E., Di Stefano, P., Lowrie, W., Bernasconi,S.M. and Hernández, F.M., 2004, Tethyan magnetostratigraphy fromPizzo Mondello (Sicily) and correlation to the Late Triassic Newarkastrochronological polarity time scale: Geological Society of AmericaBulletin, v. 116, p. 1043-1058.

Nicora, A., Balini, M., Bellanca, A., Bertinelli, A., Bowring, S.A., Di Stefano,P., DumitricA, P., Guaiumi, C., Gullo, M., Hungerbuehler, A., Levera,M., Mazza, M., McRoberts, C.A., Muttoni, G., Preto, N. and Rigo, M.,2007, The Carnian-Norian boundary interval at Pizzo Mondello (SicaniMountains, Sicily) and its bearing for the definition of the GSSP of theNorian Stage: Albertiana, v. 36, p. 102-129.

Orchard, M.J., 2007, A proposed Carnian-Norian boundary GSSP at BlackBear Ridge, northeast British Columbia, and a new conodont frameworkfor the boundary interval: Albertiana, v. 36, 130-141.

Orchard, M.J., 2010, Triassic conodonts and their role in stage boundarydefinition; in Lucas, S.G., ed., The Triassic Timescale: Geological Soci-ety, London, Special Publication, v. 334, p. 139-161.

Pálfy, J., Demény, A., Haas, J., Carter, E. S., Görög, Á., Halász, D., Oravecz-Scheffer, A., Hetényi, M., Márton, E., Orchard M. J., Ozsvárt, P., Veto,I. and Zajzon, N., 2007, Triassic–Jurassic boundary events inferred fromintegrated stratigraphy of the Cs vár section, Hungary: Palaeogeo-graphy, Palaeoclimatology, Palaeoecology, v. 244, p. 11-33.

Szabó, J., 1860, Geologische Detailkonte des Grenzgebietes des Nograderund Pesther Comitates: Jahrbuch des Kaiserlich-Königlichen GeologischenReichanstalt, Sitzungberichte (Sitzung am 10. Jänner 1860), p. 41–44.

Tozer, E.T., 1965, Upper Triassic ammonoid zones of the Peace Riverfoothills, British Columbia, and their bearing on the classification of theNorian stage: Canadian Journal of Earth Science, v. 2, p. 216-226.

Vadász, E., 1908, A Cserhát DNY-i triász- és óharmadkori rögeiben eszközöltföldtani vizsgálatok eredménye: Földtani Közlöny, v. 38, p. 368.

Vadász, E., 1910, A Duna-balparti id sebb rögök slénytani és földtaniviszonyai: Magyar Királyi Földtani Intézet Évkönyve, v. 18/2, p. 103-171.

291PLATE CAPTIONS

PLATE 1

FIGURES 1,7. Epigondolella quadrata Orchard, 1991, upper view, lower Norian; Fig. 1: juvenile form, sample516 m, rep.-no. 516-8; Fig. 7: sample 505 m, rep.-no. 505-26.

FIGURES 2, 6, 11, 12. Epigondolella rigoi Kozur, 2007, upper view, lower Norian; Fig. 2: juvenile form,sample 516 m, rep.-no. 516-9; Fig. 6: primitive form, sample 505 m, rep.-no. 505-24; Fig. 11: sample 487-490 m,rep.-no. 487-490-43; Fig. 12: juvenile form, sample 477 m, rep.-no. 477-49.

FIGURES 3, 4. Epigondolella vialovi (Burij, 1989), juvenile forms, lower Norian, sample 516 m; Fig. 3: upperview, rep.-no. 516-10; Fig. 4: rep.-no. 516-11, a) upper view, b) oblique lateral view.

FIGURES 5, 8. Metapolygnathus mazzai Karádi, Kozur and Görög n. sp., Lower Norian, sample 505 m; Fig.5: rep.-no. 505-23; Fig. 8: rep.-no. 505-25, a) lower view, b) oblique lateral view.

FIGURES 9, 10, 16. Neohindeodella summesbergeri summesbergeri Kozur and Mostler, 1970, lateral view,lower Norian, sample 487-490 m; Fig. 9: rep.-no. 487-490-35; Fig. 10: rep.-no. 487-490-42; Fig. 16: rep.-no. 487-490-33.

FIGURES 13, 17. Epigondolella praetriangularis Kozur and Moix, 2007, lower Norian, sample 477 m; Fig.13: upper view, rep.-no. 477-47; Fig. 17: oblique upper-lateral view, rep.-no. 477-46.

FIGURE 14. Oncodella mostleri n. sp. Karádi, Kozur and Görög n. sp., holotype, lower Norian, sample 477m, rep.-no. 477-44, a) lateral view, b) oblique lateral-lower view.

FIGURE 15. Misikella longidentata Kozur and Mock, 1974, lateral view, lower Norian, sample 487-490 m,rep.-no. 487-490-31.

Scale = 200 µm

PLATE 2

FIGURES 1. (E. cf. rigoi), 2, 5, 8, 20, Epigondolella rigoi Kozur, 2007, upper view, lower Norian; Fig. 1:sample 473 m, rep.-no. 473-53; Fig. 2: sample 473 m, rep.-no. 473-54; FIGURE 5. Sample 468 m, rep.-no. 468-71; Fig. 8: sample 457-459, rep.-no. 457-459-78; Fig. 20: sample 435.6-439.2 m, rep.-no. 435.6-439.2-111.

FIGURES 3, 6. Morphologically transitional form between Misikella longidentata Kozur and Mock, 1974 andMisikella hernsteini (Mostler, 1967), lateral view, lower Norian; Fig. 3: sample 473 m, rep.-no. 473-50; Fig. 6:sample 457-459 m, rep.-no. 457-459-79.

FIGURES 4, 12. Misikella longidentata Kozur and Mock, 1974, lateral view, lower Norian; Fig. 4: sample468 m, rep.-no. 468-57; Fig. 12: sample 452.5-454.7 m, rep.-no. 452.5-454.7-88.

FIGURE 7. Norigondolella navicula (Huckriede, 1958), juvenile form, lateral view, lower Norian, sample457-459 m, rep.-no. 457-459-75.

FIGURES 9, 18, 19. Epigondolella quadrata Orchard, 1991, lower Norian; Fig. 9: upper view, sample 452.5-454.7 m, rep.-no. 452.5-454.7-90; Fig. 18: upper view, sample 444 m, rep.-no. 444-103; Fig. 19: oblique upper-lateral view, sample 444 m, rep.-no. 444-102.

FIGURES 10, 11. Oncodella paucidentata (Mostler, 1967), lateral view, lower Rhaetian fissure filling, sample452.5-454.7 m; Fig. 10: rep.-no. 452.5-454.7-11; Fig. 11: rep.-no. 452.5-454.7-82.

FIGURES 13, 14. Misikella hernsteini (Mostler, 1967), lower Rhaetian fissure filling, sample 452.5-454.7 m;Fig. 13: lateral view, rep.-no. 452.5-454.7-91; Fig. 14: rep.-no. 452.5-454.7-89, a) lateral view, b) oblique lateral-lower view.

FIGURES 15, 16. Misikella posthernsteini Kozur and Mock, 1974, lower Rhaetian fissure filling, sample452.5-454.7 m; Fig. 15: slightly oblique lateral-lower view, rep.-no. 452.5-454.7-93; Fig. 16: lateral view, rep.-no.452.5-454.7-87.

FIGURE 17. Epigondolella triangularis (Budurov, 1972), upper view, late juvenile form, lower Norian, sample444-447.5 m, rep.-no. 444-447.5-99.

Scale = 200 µm

292PLATE 3

FIGURE 1. “Norigondolella” trinacriae Mazza, Cau and Rigo, 2012, upper view, lower N o r i a n , s a m p l e433.5 m, rep.-no. 433.5-120.

FIGURE 2. Epigondolella quadrata Orchard, 1991, upper view, lower Norian, sample 433.5 m, rep.-no.433.5-121.

FIGURES 3, 5. Epigondolella rigoi Kozur, 2007, upper view, lower Norian; Fig. 3: sample 433.5 m, rep.-no.433.5-122; Fig. 5: sample 412 m, rep.-no. 412-126-127.

FIGURES 4, 6-8. Norigondolella hallstattensis (Mosher, 1968), lower Norian, sample 412 m; Fig. 4: juve-nile form, rep.-no. 412-125, a) lateral view, b) upper view; Fig. 6: upper view, juvenile form, rep.-no. 412-128; Fig.7: upper view, late juvenile form, rep.-no. 412-129; Fig. 8: lower view, early juvenile form, rep.-no. 412-136.

FIGURES 9, 10. Epigondolella uniformis Orchard, 1991, upper view, lower Norian, sample 410 m; Fig. 9:juvenile form, rep.-no. 410-149; Fig. 10: rep.-no. 410-147.

FIGURES 11, 15-17. Epigondolella triangularis (Budurov, 1972), upper view, lower Norian; Fig. 11: sample410 m, rep.-no. 410-148; Fig. 15: late juvenile form, sample 385.3-392, rep.-no. 385.3-392-158; Fig. 16: sample385.3-392 m, rep.-no. 385.3-392-159; Fig. 17: posterior margin slightly damaged, sample 376-378.3 m, rep.-no.376-378.3-160.

FIGURE 12. Epigondolella cf. triangularis (Budurov, 1972), upper view, lower Norian, sample 410 m, rep.-no. 410-150.

FIGURES 13, 14. Neohindeodella summesbergeri summesbergeri Kozur and Mostler, 1970, lateral view,lower Norian, sample 385.3-392 m; Fig. 13: rep.-no. 385.3-392-151; Fig. 14: rep.-no. 385.3-392-1.

Scale = 200 µm

293PLATE 1

294PLATE 2

295PLATE 3