© Author(s) 2023. CC Atribution 4.0 License Taxonomic and stratigraphic remarks on Placites urlichsi Bizzarini, Pompeckjites layeri (Hauer), Carnites floridus (Wulfen) and Sageceras haidingeri (Hauer) Taksonomija in stratigrafski razpon vrst Placites urlichsi Bizzarini, Pompeckjites layeri (Hauer), Carnites floridus (Wulfen) in Sageceras haidingeri (Hauer) Andreas SPATZENEGGER 1 & Walter POLTNIG 2 1 A-5113 St. Georgen, Wetterkreuzstraße 16, Austria, e-mail: andreas.spatzenegger@outlook.com 2 A- 8063 Eggersdorf, Feldweg 16, Austria, e-mail: walter.poltnig@gmx.at Prejeto / Received 19. 8. 2022; Sprejeto / Accepted 12. 4. 2023; Objavljeno na spletu / Published online 4. 8. 2023 Key words: ammonoids, Triassic, Carnian, Wettersteinkalk, Bleiberger Sonderfazies, Upper San Cassian Formation Ključne besede: amoniti, trias, karnij wettersteinski apnenec, pliberški facies, Zgornja San Cassianska formacija Abstract Investigations of an Lower Carnian Wettersteinkalk ammonoid fauna found in the Hochobir massif (Carinthia/ Austria) gave rise to problems in the taxonomic relationship within the Triassic ammonoid Family Pinacoceratidae. The morphological parameters of the ammonoid genus Pompeckjites are rather unclear. Morphological variation of at least two ammonoid species as Pompeckjites layeri Hauer on one end, Placites urlichsi Bizzarini on the other end have to be take into account. Numerous field surveys, studies and excavations on upper Wettersteinkalk sites within the Karavank Mountains and Hallstatt-facies sites in the Northern Calcareous Alps were implemented and compared with the reference sites in the Dolomites. As a consequence of our investigations, the Hochobir Wettersteinkalk ammonite assemblage is thought to be equivalent in time to the ammonoid fauna of the Upper San Cassian Formation. The frequent occurrence of the Julian (Lower Carnian) ammonoid Placites urlichsi Bizzarini may be a powerful tool in field investigations for a refined correlation of the upper Wettersteinkalk reef limestone to the coeval basinal facies of the Upper San Cassian Formation (Lower Carnian/upper Trachyceras aonoides Zone). As a result of this study Placites urlichsi was included in the genus Pompeckjites. This paper could be an attempt to recognize the differences in juvenile forms of Pompeckjites layeri and Placites urlichsi and other similar disciform ammonoid genera like Carnites floridus and Sageceras sp. based on suture lines, polished transversal-sections and morphological features. Izvleček Rezultati raziskave amonitne favne v spodnjekarnijskem wettersteinskem apnencu, ki se pojavlja na Obirju, na avstrijskem Koroškem, odpirajo problem v taksonomskem razlikovanju triasnih amonitov družine Pinacoceratidae. Razlikovanje na podlagi morfoloških parametrov amonitov rodu Pompeckjites je precej nejasno, pri čemer je treba upoštevati morfološke variacije najmanj dveh vrst, in sicer Pompeckjites layeri Hauer na eni ter Placites urlichsi Bizzarini na drugi strani. Številni ogledi nahajališč v zgornjem wettersteinskem apnencu Karavank in hallstattskem faciesu Severno apneniških Alp, njihova izkopavanja ter raziskave, poleg tega pa tudi primerjava z referenčnimi najdišči v Dolomitih kažejo, da je zbrana amonitna združba wettersteinskega apnenca najverjetneje časovni ekvivalent amonitni favni zgornje San Cassian formacije. Pogosto pojavljanje julijskega (spodnji karnij) amonita Placites urlichsi Bizzarini je na terenu lahko močno orodje za oceno korelacije med grebenskim zgornjim wettersteiskim apnencem ter ekvivalentnim bazalnim faciesom zgornje San Cassian formacije (spodnji karnij/zgornji del Trachyceras aonoides cone). Kot rezultat te raziskave je bil Placites urlichsi vključen v rod Pompeckjites. Pričujoči članek na podlagi suturnih linij, poliranih rezov in morfoloških značilnosti, pomaga prepoznati razliko med juvenilnimi oblikami Pompeckjites layeri in Placites urlichsi ter drugimi amoniti diskoidne oblike kot sta Carnites floridus in Sageceras sp. GEOLOGIJA 66/1, 87-105, Ljubljana 2023 https://doi.org/10.5474/geologija.2023.003 88 Andreas SPATZENEGGER & Walter POLTNIG Introduction The Julian (Lower Carnian) Trachyceras aon- oides and Austrotrachyceras austriacum ammo - noid zonation was originally established in the fossiliferous Hallstatt Limestones of the Northern Calcareous Alps (Mojsisovics 1892, 1893; Frech 1911a, 1912, subsequently better defined by Kr - ystyn 1978 and verified by Hornung et al. 2007). Later on it was compared with the biostratigraph - ic framework of the San Cassian Formation of the Southern Calcareous Alps/Dolomites (see refer - ence lists of Mietto et al. (2012) and Urlichs (2017). It was recognized that the San Cassian Formation spans more than the previously thought late Lad - inian to earliest Carnian ( Trachyceras aon Zone) age (Bizzarini 1987, 2000; Mastandrea 1995; Di Bari & Baracca 1998). Consequently, attempts were made to correlate both facies on the basis of occuring Trachyceratidae (Urlichs 1994, 2017). However, other co-occurring ammonoid genera (except Lobites, see Urlichs 2012) were never part of such studies. From the Julian part of the Wet - tersteinkalk (Bleiberger Sonderfazies of Holler 1960) such comparative ammonoid studies were not carried out until today. Current biostratigraph - ic studies in the UNESCO Geopark Karawanken/ Karavanke (A/Slo) evidence a T. aonoides Zone age of these strata that is based on the occuring Tra - chyceratidae (Poltnig & Spatzenegger 2022). The co-occuring ammonoids of the Family Pinacocer - atidae show striking similarities to the Pinacocer - atidae of the Upper San Cassian Formation East of Cortina d’ Ampezzo that were revised by Bizzarini (1987). A small disciform ammonoid fauna, found in the uppermost Wettersteinkalk (Bleiberger Son - derfazies, Holler 1960) caused severe taxonomic classification problems that hampered a clear Car - nian/Julian ammonoid subzone (see Fig. 2, middle column) identification already in the field. Because of syndiagenetic dolomitization and recrystalliza - tion during lithogenesis, only very few ammonoids showed well preserved suture lines. This fact made it complicated to distinguish between the Julian contemporaneous ammonoid genera Pompeckjites, Sageceras and Carnites. To make matters worse, some juvenile growth stages of Placites urlich- si show strong homeomorphism to Sageceras sp. and Pompeckjites layeri. To facilitate the classification on poorly pre - served ammonoids of the genera above mentioned we provide our results based on polished hand specimens and morphological features. Study areas Fladung mining area on Obir massif/Austria The abandoned Fladung lead-zinc mining area is located about 8 km west of Bad Eisenkappel on the southern slope of Hochobir (see Fig. 1, A). It is easily accessible via the toll road to the Eisen- kappler Hütte. During several field excursions the majority of the ammonoids were sampled from the ravine directly east of the Fladung Berghaus (see Figs. 1, B and D with sites 1a, 1b, 1c). The western ravine wall (approximately 1200 m above sea level) crops out of a steeply dipping (55 degrees towards east-south-east) Wettersteinkalk succession that shows a slope angle parallel to the bedding. There - fore, all ammonoid locations (site 1 a-c) found in this wall originate from approximately the same stratigraphic layers. Location 2 is situated 500 m further eastwards of the Fladung Berghaus direct - ly beside the toll road near a junction with a forest road (see Fig. 1, B). It is in tectonically stressed contact (not well visible in the field) with Cardi - ta shale and Cardita limestone. Lipolt (1856:337f) mentions from the Fladung mining district light ore bearing “Hallstätter Kalk” (=Wettersteinkalk) and cited Carnian ammonoids from the locality (“ Ammonites Aon, Ammonites Joannis Austriae, Ammonites Jarbas and Ammonites Gaytani”). The “Bleiberger Schichten des Ovir (=Obir)” with Car- nites floridus, also mentioned in Lipolt (1856), correspond to the first Raibl shale horizon and should not be confused with today’s Bleiberger Sonderfazies of Holler (1960). For further infor - mation we refer to Poltnig & Spatzenegger (2022). Our newly discovered fossiliferous strata corre- spond to the Bleiberger Sonderfazies (Holler 1960) of the uppermost Wettersteinkalk and mark the area between the sediment hosted lead-zinc min - eralization (Bechstaedt 1979; Mondillo et al. 2019) and the tectonically sheared off and subsequently eroded first Raibl shale horizon. Unterpetzen mining area near Podpeca/Slovenia The former mining district Unterpetzen/Pod - peca is situated roughly 6.5 km southwest of the town Mežica/Slovenia. (see Fig. 1, A) on the south eastern slope of the Petzen massif. It should not be confused with the Helena mining district in the village Podpeca itself that is situated one kilometer eastwards. Two field campaigns were carried out in this area to verify our stratigraphic results from Hochobir. Main sampling was done alongside the forest road (sites Pod. 1-3, roughly E 46.476450, N 14.808636) to the abandoned Mariahilf mine 89 Taxonomic and stratigraphic remarks on Placites urlichsi Bizzarini, Pompeckjites layeri (Hauer), Carnites floridus (Wulfen)... Fig. 1. Overview of the Studied Areas. A, geographic situation of the Obir/Fladung area in Austria and of the Unterpetzen/Podpeca area in Slovenia. B, enlarged overview of the Fla - dung sites with mapped lithologic strata (debris and soil are not mapped). C, Unterpetzen/Podpeca mining area with sites Pod 1–3 alongside the forest road to the Mariahilf mine gallery. D, tectonically stressed contact of Wettersteinkalk (left) to Raibl shales (right) in the Fladung area. E, view from Fladung site 1a towards 1b and 1c. F, weathered in situ Wettersteinkalk ammonoid ( Joannites klipsteini), Fladung, site 1c. 90 Andreas SPATZENEGGER & Walter POLTNIG gallery (see Fig. 1, C). From Unterpetzen several ammonoid finds in Wettersteinkalk have been cit - ed in Mojsisovics (1871, 1873, 1882, 1893, 1902). Material and methods All ammonoid concentrations found at both lo - cations originate from the vicinity of algal lami - nites and do show a partial current sorting of the fossils. This suggests a deposition in the tidal to subtidal zone. Most ammonoids in this study were completely recrystallized and partially encrust - ed by a several millimeters thick dolomitic crust. Towards the surface and near mineralized layers better preservation was found. In some limestone parts the ammonoids showed calcitic shell replace - ment that was sometimes covered with a fine limo - nite crust between ammonoid shell and sediment. If this coating was missing, preparation was diffi - cult and of poor result. Another common feature of ammonoids found near the surface was the disso - lution of the ammonoid shell by humic acids. The result was an internal mold (steinkern) covered by a crumbled powder of the former ammonoid shell. The identification of ammonoids that showed steinkern preservation was also hindered by the lack of visible suture lines. Preparation was done by the authors exclusively. The best results were obtained by using coarse and fine pneumatic en - gravers. Limestone lacking preparable ammonoids was used for making polished transversal-sections (see Figs. 7, A, B, F and 9, C). Such sections gave good insights into the depositional conditions and were found to be very helpful in identification of some ammonoids. All collected fossils originate from the Blei - berger Sonderfazies (Holler, 1960) of the mining district Fladung and are stored in the administra - tion center of the UNESCO Geopark Karawanken/ Karavanke in Tichoja and in the private collection of Andreas Spatzenegger (A-5113 St. Georgen). All fossils are accessible by prior appointment. Systematics More than 300 ammonoid specimens were col - lected during fieldwork. The general preservation of the ammonoid assemblages found was moderate to poor. Sample richness in ammonoid quantity was very high and similar to the ammonoid accu - mulations within the Hallstatt limestone. For the species mentioned in the systematic part, the most important synonyms provided in the literature and the original papers describing the holotypes were carefully reviewed. The systematic paleontol - ogy below is thus based upon a careful revisitation of previous Triassic ammonoid literature (Hauer 1846, 1847; Mojsisovics 1873, 1882; Hyatt 1884; Mojsisovics 1902; Gemmellaro 1904; Arthaber 1905; Hyatt & Smith 1905; Arthaber 1911; Frech 1911a; Welter 1914; Diener 1915a, 1915b, 1916; Smith 1927, 1932; Johnston 1941; Spath 1951; Tozer Fig. 2. Simplified stratigraphic log of the Fladung area. The left column shows the Lower Carnian (Julian) sub-stages. The middle column shows the ammonoid zonation modified after Krystyn (1973) and Hornung et al. (2007). The right column shows an idealized lithologic log of the Fladung area and the stratigraphic position of the found ammonoid fauna (red star). 91 Taxonomic and stratigraphic remarks on Placites urlichsi Bizzarini, Pompeckjites layeri (Hauer), Carnites floridus (Wulfen)... 1967; Silberling & T ozer 1968; T ozer 1971; Krys - tyn 1973, 1978, 1980; Tozer 1981; Krystyn 1982; Tozer 1984; Sestini 1992; Tozer 1994; Doguzhae - va et al. 2007; Balini 2008; Konstantinov 2008; Mietto et al. 2008; Balini et al. 2010, 2012; Hy - att & Smith 2012; Konstantinov 2012; Lukeneder & Lukeneder 2014; Ritterbush e t a l . 2 0 1 4 ; J e n k s et al. 2015) and our own investigations based on morphology and transversal sections. For each ammonoid species, remarks are provided with re - spect to the original identifications and descrip- tions provided in the literature. The main subject of the systematic part is the Lower Carnian/Julian genus Pompeckjites of the Family Pinacoceratidae Mojsisovics, 1879. The additionally described ge - nus Carnites ( Carnitidae Arthaber , 1 9 1 1 ) is not a member of Pinacoceratidae but included with the latter in the Superfamily Pinacoceratoidea (Tozer, 1981). The genus Sageceras (Superfamily Sagecer - atoidea Hyatt, 1884) is shown here only for com - parison purposes to highlight some morphological similarities with the above mentioned genera in transversal sections. For the higher taxonomic no - menclature of ammonoids the work of Hoffmann et al. (2022) was used. In regards to the taxonomy of ammonite families and subfamilies we used the classification of Tozer (1971, 1981) and Krystyn (1982). For the detailed descriptions of Carnites floridus and Pompeckjites layeri, we refer to the original descriptions (Hauer 1847; Mojsisovics 1873, 1902). The description of Placites urlichsi Bizzarini, 1987 is more detailed because of its im - portance for this work. Superorder Ammonoida Haeckel 1866 Order Ceratitida Hyatt, 1884 Pinacoceratoidea Mojsisovics, 1879 Carnitidae Arthaber, 1911 Carnites Mojsisovics, 1879 Type species: Carnites floridus (Wulfen, 1793) 1793 Nautilus bisulcatus Wulfen, p. 103, fig. 10. 1793 Nautilus floridus Wulfen, p.113, fig. 16. 1793 Nautilus nodulosus Wulfen, p. 115, fig. 17. 1793 Nautilus redivivus Wulfen, p. 116, fig. 18. 1846 Ammonites floridus H a u e r , p . 2 , p l . 1 , fi g s . 5-14. 1855 Ammonites floridus Hauer, p. 150. 1873 Pinacoceras floridum Mojsisovics, p.58, pl. 22, figs. 15, 16; pl. 25, figs. 1-6. 1882 Carnites floridus, Mojsisovics, p.228, pl. 50, figs. 5-8; pl. 51, figs. 1-8. 1911b Carnites floridus, Frech, p. 19, figs. 24 a, b, non c. 1911b Carnites floridus, Frech, p. 19, figs. 25 a, b, c. non 1911b “Carnites” falcifer, Frech, p. 21, figs. 26, 27. 2007 Carnites floridus, Hornung et al., pl. 6, figs. b1-b4. Description: For the detailed morphological de - scription we refer to (Hauer, 1846) and (Mojsiso - vics, 1873, 1882). Remarks: The juvenile development of Carnites floridus (Wulfen, 1793) was first described in de - tail in Hauer (1846) and is excellently pictured in his plate. Hauer recognized the different growth stages of Carnites floridus which were assigned by Wulfen (1793) to four different Nautilus species. Hauer (1846) established on contemporary no - menclature and the “ammonitic” suture line Am- monites floridus. Mojsisovics (1873) confirmed the growth development illustrated and described by Hauer (1846) and identified it as Pinacoceras floridum. Mojsisovics (1879a) first mentioned the genus name Carnites and formally established the genus Carnites in Mojsisovics (1879b) with C. floridus as its type species. The original type spec - imen of C. floridus was found in the first Cardita shale horizon of Bad Bleiberg. Its stratum typicum in th e so call ed first Raib l shal e h o rizo n ( = first Cardita shale horizon) was clearly named and de - scribed too. The hitherto considered large stratigraphic range of C. floridus most probably has its origin in the descriptions of Hauer (1846) and Mojsisovics (1873) where both authors refer to a great mor - phologic variability in the mature growth stages of C. floridus. Alas, some subsequent authors (Leon - ardi & Polo, 1952) didn’t focus on the juvenile de - velopment of C. floridus and mis-identified speci - mens showing divergent juvenile development and mature Carnites shape as C. floridus. Carnites floridus ( see Figs. 3, E-E2 and F-F1 ) found in the Hallstatt Limestone of the Rappolt - stein hill (= historic „Mons Tuval“, located in Bavaria) show the same development in juvenile 92 Andreas SPATZENEGGER & Walter POLTNIG stage as in C. floridus from the first shale horizon of Bad Bleiberg. At Rappoltstein C. floridus was found with Austrotrachyceras sp., and Neopro- trachyceras thous (see Figs. 3, G, G1) what allows a correlation with the beginning of the A. austri- acum Zone (Hornung et al. 2007). This indicates that the first Raibl shale horizon can be correlated as well, which implies that the uppermost Wetter - steinkalk (Bleiberger Sonderfazies) occurring be - low roughly corresponds to the upper T. aonoides Zone. Frech (1911b: 19ff) established “ Carnites” falcifer as a new Carnites species from presumably Tuvalian (Upper Carnian) strata. Our own investi - gations on Rappoltstein revealed that “C.” falcifer belongs to the genus Parahauerites. It is of early Tuvalian age and was found with Pleurotropites sp. and Trachysagenites sp. Therefore, we can ex - clude an occurrence of Carnites in lower Tuvalian (Tropites dilleri Zone) strata. To illuminate the juvenile morphological devel - opment and the development of the suture line of C. floridus we have pictured the modified plate of Hauer (1846: pl. 1), (see Figs. 3, A-D) with addi - tional metric measurements. The added black cir - cles in the suture line drawings (see Figs. 3, C-C5) focus on the development of an adventitious lobe/ saddle what is a diagnostic feature for C. floridus. Fully mature specimens of C. floridus show two adventitious elements that both emerged in the same way. In the largest suture (see Fig. 3, C5), the genesis of the second adventitious element is visible in the small adventitious bulgy saddle near the venter on the right side of the black circle. The juvenile specimen illustrated in Figure 3, A shows a ventral furrow with a faint keel in the middle (not visible in Hauers drawing). According to Hau - er (1846) this is not the regular development. Most juvenile cores at this size show a normal round - ed venter. The Figure 3, B in this text, shows the subsequent development of the tricarinate venter that is also an important morphological feature of C. floridus too (see Figs. 3, E1 and 9, A1). Following this stage, the shape of C. floridus diverges considerably. There can occur equal sized Fig. 3. Carnites floridus. A, B, D, different growth stages of C. floridus with added metric measurements (modified after Hauer 1846: pl. 1, figs. 5-14). C–C5, original suture drawings in Hauer (1846). The development of an adventitious saddle is focused on the black circles. E–E1, side and venter view of Carnites floridus from Carnian Hallstatt Limestone of Rappoltstein. F, C. floridus from Rappoltstein in iridescent shell preservation. F1, en - largement of the faint growth lines on ammonoid F. G–G1, Neoprotrachyceras thous, found together with Carnites floridus on Rappoltstein. E2, sutureline of C. floridus from Rappoltstein. 93 Taxonomic and stratigraphic remarks on Placites urlichsi Bizzarini, Pompeckjites layeri (Hauer), Carnites floridus (Wulfen)... specimens with almost sharp (Fig. 3, D) or with rounded venter. Some specimens showed fold-like nodes at the mid flank, which were sometimes ac - companied by nodes on the ventro-lateral margin. This is in contrast with other totally smooth spec- imens of the same size. Between these extremes, many variations exist. The suture line is identical in all of these variations. All these different forms are based on an identical juvenile stage show- ing similar measurements in ratio of diameter to thickness. This was not really taken into account in earlier classifications of similar ammonoids to Carnites floridus, which led to an enlarged strati- graphic range of true C. floridus. The ammonoid fauna of the San Cassian Forma - tion laid a base for an extended stratigraphic range of C. floridus as well. Early a uthors (M ojsisovics, 1869, 1882, Mojsisovics et al., 1895; Zittel, 1899) assigned the San Cassian layers as a whole into the former Cordevol ( T. aon Zone). All ammonoid forms similar to Carnites, were assigned to C. f lori- dus. This opinion prevailed until the 20th century and can be seen clearly in the identifications on the ammonoid plates in Leonardi and Polo (1952), where ammonoids from the upper San Cassian Formation East of Cortina d’ Ampezzo (Boa Stao - lin, Boa Tamarin, Costalares) were compared and identified with upper Ladinian to lower Carnian ammonoid species of the classic San Cassian loca - tions (Stuores Wiesen, Pralongia). For example, the genus Sirenites that begins in the upper T. aonoides Zone, was not recognized in Boa Staolin because it does not occur in San Cassian. It was identified as (Pro)trachyceras ladinum in Leonardi and Polo (1952: pl. 2, Figs. 32-35). Bizzarini (1987, 2000) took these differences into account and attempt - ed to improve the identifications by establishing Placites urlichsi (for C. floridus in Leonardi and Polo 1952) and by enlarging the stratigraphic log of the upper San Cassian Formation to include the T. aonoides and A. austriacum ammonoid Zones. For further literature regarding to the San Cassian Formation, we refer to the reference lists of Mietto et al. (2012) and Urlichs (2017). Occurrence: Carnites floridus o c c u r s i n C a r - nian Hallstatt Limestone of Feuerkogel/Austria and Rappoltstein/Germany, in the first Raibl shale in Austria and Germany (Bavaria), in the Reingra - ben shales in Austria (Frech 1911b; Lukeneder & Lukeneder, 2022). Hungary (Frech 1911b), Slove - nia (Jurkov šek et al., 2002) and Italy. Pinacoceratidae Mojsisovics, 1879 The Family Pinacoceratidae probably has its origin in the late Anisian to lower Ladinian age with Praepinacoceras damesi (Mojsisovics). In the subsequent Carnian stage the Family Pinaco - ceratidae is subdivided into several genera whose phylogenetic relationships to each other are not very clear. A close relationship exists among the genera Pompeckjites and Eupinacoceras in the de- velopment of the suture line and in some morpho - logical parameters. Genus Pompeckjites Mojsisovics, 1902 Type species: Pompeckjites layeri, (Hauer, 1847) 1847 Ammonites layeri Hauer, pl. 9, figs. 1-3. 1873 Pinacoceras layeri, Mojsisovics, pl. 23, figs. 1-6. 1902 Pompeckjites layeri, Mojsisovics, pl. 19, figs. 3-5; pl. 20, fig. 1. Description: For detailed description see in (Hauer, 1847) and in (Mojsisovics, 1873, 1902) Remarks: In the Hallstatt Limestone, Pom- peckjites layeri (see Figs. 4, A-E) spans the entire Julian stage ( T. aon, T. aonoides and A. austria- cum a m m o n o i d Z o n e s ) . O u r o w n m e a s u r e m e n t s on P. layeri from the T. aonoides and A. austria- cum Zones show slight differences in the develop- ment of the juvenile whorls. In the A. austriacum Zone the inner whorls are thicker and do show a somewhat persisting rounded venter stage (see white arrows in Fig. 7, C) than in the T. aonoides Zone where the early juvenile whorls are thinner and more fastigated (see Fig. 7, D) at equal size. According to Krystyn (1973: 125, see in faunal list of T. aon Zone) P. philopater is synonymous with P. layeri. In contrast to this opinion Pinacoceras philopater (Laube) was assigned to Pompeckjites by Bizzarini (1987). Occurrence: According to Krystyn (1978), P. layeri occurs in the T. aon, T. aonoides and A. austriacum Zones of the Hallstatt Limestone. San Cassian Formation/Italy. “Placites” urlichsi Bizzarini, 1987 Type species: Placites urlichsi Bizzarini, 1987, pl. 1 figs. 1, 2a,b, 3a,b, 6a,b, 7, 8. Holotype: pl. 1, fig. 1, from Boa Staolin. Paratypes: pl. 1, figs. 6-8, from Boa Staolin. Depository of types (see Bizzarini, 1987: 50). 1952 Carnites floridus, Leonardi & Polo, pl. 1 figs. 26, 44, 45, 47- 49, 55, 57; pl. 2, figs. 39, 40, 41, 42, 43. 2000 Placites urlichsi Bizzarini, pl. 3, figs. 3, 4. 94 Andreas SPATZENEGGER & Walter POLTNIG Description: The early juvenile stage shows an open umbilicus and a rounded venter (Figs. 5, A1, B and C). Then the wide umbilicus narrows quickly, leaving a deep narrow navel. During fur - ther growth stages the venter is at first sub to high-trapezoidal rounded and finally develops a broad tabulate venter stage (see Figs. 7, A2, B1 and F1). At this growth stage Placites urlichsi resem - bles Sageceras sp. in form and cross-section (see Fig. 9, E1) but shows a totally different suture line. The suture line of P. urlichsi s h o wn in B izzarini, (1987: 51) is comparable with the suture lines of equal sized specimens from Fladung, site 2 in the Hochobir massif. Well preserved flanks of bigger specimens of P. urlichsi from the same site show faint growth lines with a distinct bend towards the aperture in the middle of the flank. Remarks: Our specimens from Fladung, site 2 reach 25 mm in diameter (see Figs. 5, D and 6, D) and show a body chamber of about a half to three quarters of the coiling. Visible sutures were found on a few specimens only. In the Hochobir mas - sif, two morphotypes of Placites urlichsi can be recognized. Both variants show the same tabulate venter in sub-mature growth stages. Morphotype 1 (see Figs. 5, A1, A2 and C) is somewhat thinner and shows a sharp high-trapezoidal venter devel- opment in juvenile stage at roughly 15 mm in di - ameter. At this stage, specimens of morphotype 1 (see Fig. 5, A2; Figs. 6, E and 7, E2) are difficult to distinguish with the naked eye from Pompeckjites layeri (see Fig. 6, A). In its juvenile stage morpho - type 2 develops a thicker, more rounded sub-trap - ezoidal venter. Placites urlichsi in Bizzarini (1987: figs. 3a, b) is identical to the same sized specimens of the mor - photype 2 from Fladung, site 2. The Figures 2a, b in Bizzarini (1987) are identical to morphotype 1 from Fladung, site 1 a-c. The suture line is iden - tical in both morphotypes. The steinkern of Pom- peckjites philopater p i c t u r e d i n B i z z a r i n i ( 2 0 0 0 : pl. 2, fig. 6) from Boa Tamarin is surmised to be a Placites urlichsi because on the steinkern the dis- tinct ventro-lateral margins (compare to Fig. 5, A2) of P. urlichsi morphotype 1 are visible. From a stratigraphic point of view, the ammonoid fauna of Fig. 4. Pompeckjites layeri. A-A2, Pompeckjites layeri (Mojsisovics, 1902: pl. 20, fig. 1), side and venter view. B, Pompeckjites layeri from Hallstatt Limestone ( T. aon- oides Zone) of Rappoltstein. B1, enlarged detail of the preserved wrinkle layer. D, suture of P. layeri (Hauer, 1847: pl. 9, fig. 3). E, suture of P. layeri (Diener, 1915: pl. 2, figs. 14 a, b). C-C1, P. layeri (Mojsisovics, 1873: pl. 23, fig. 3) side and venter view. 95 Taxonomic and stratigraphic remarks on Placites urlichsi Bizzarini, Pompeckjites layeri (Hauer), Carnites floridus (Wulfen)... Boa Tamarin in Bizzarini (2000: 22), is thought to be slightly older than the ammonoid fauna of Boa Staolin whence Placites urlichsi morphotype 2 oc - curs. Similar minor age and shape (from slender to thicker specimens) differences are also recogniza - ble at the Hochobir sites. In P. layeri a similar de - velopment from slender to thicker specimens was observed from the T. aonoides Zone towards the A. austriacum Zone (see Figs. 7, C and D). Occurrence: Morphotype 2 (see in Figs. 5, B and D) from Hochobir/Fladung exclusively at site 2 but is very common there. Morphotype 1 (see in Figs. 5, A1, A2 and C) occurs at Fladung, sites 1a, b and c. Unterpetzen/Podpeca and San Cassian Formation. Arguments to replace Placites urlichsi Bizzarini to the genus Pompeckjites The genus Placites, (Superfamily Pinacocer - atoidea Mojsisovics, 1879, Family Gymnitidae Waagen, 1895) is characterized by its platycone cross-section and its rounded venter. According to (Mojsisovics, 1873) all species of Placites are dis- tinguished mainly on their whorl sections and su - ture lines. Furthermore, all species descriptions of Placites in Mojsisovics (1873) were based on sub mature and mature stages of growth. The type species Placites platyphyllus (Moj - sisovics, 1873) as the closely related species Plac- ites polydactylus, P. oxyphyllus and P. myopho- rus s h o w a l l a c l o s e d u m b i l i c u s a n d a n e x t e r n a l saddle with one strong side branch on the ventral side. Their confirmed age is middle to late Norian. According to Diener (1915b) no real adventitious lobes/saddles occur. The same feature was noted by Spath (1951) who described in Placites platy- phyllus a simple suture line as in Gymnites with an individualized outer branch of the external saddle. Subsequently this similarity to Gymnites led to a ranking of Placites within the Family Gymnitidae. Paragymnites (Hyatt, 1900), whose generic type is Placites sakuntala (M o jsisovics, 1 896 ) was es - tablished for those species of Placites which do not show this strong side branch on the external saddle. Placites placodes and Placites perauctus, described in Mojsisovics (1873) are, according to Fig. 5. Placites urlichsi from Obir. A, ammonoid fauna from Fladung site 1c. A1, enlarged juvenile internal mold/steinkern of P. urlichsi, (morphotype 1). A2, enlarged venter (steinkern) of P. urlichsi, (morphotype 1). B, early juvenile growth stages of Placites urlichsi (morphotype 2). C, Placites urlichsi (morpho - type 1) showing partial shell preservation. D, Placites urlichsi (morphotype 2) showing partial shell preservation. 96 Andreas SPATZENEGGER & Walter POLTNIG Krystyn and Siblik (1983), of late Carnian (Tu - valian 3) and early Norian (Lacian 1) age. They both differ from other Placites sp. and from Par- agymnites sp. by a highly individualized external saddle and additionally in P. placodes by a small open umbilicus. Based on the above mentioned differences, Placites urlichsi has to be compared to the type species Placites platyphyllus exclusively. Already Bizzarini (1987: 45), mentioned the close relationship of his newly established species Placites urlichsi to the genus Pompeckjites and stated: “The two species described here present characteristics of the external saddle and the sus - pensory lobe that seem intermediate between the genera Placites and Pompeckjites”. The above men - tioned suture line characteristics were well recog- nized by Bizzarini (1987) in his own findings from the Upper San Cassian formation of Boa Staolin (horizon B, in Bizzarini, 1987) and in the pictured and classified specimens of “ Carnites floridus” in Leonardi and Polo (1952). Unfortunately, Bizza - rini (1987) recognized more analogies to the genus Placites than to Pompeckjites. The main reason for his supposed similarity to Placites was the use of exclusively juvenile specimens showing not fully developed suture lines. As mentioned above, Placites platyphyllus is restricted to the upper Norian stage. This makes a comparison of juvenile suture lines of early Car - nian Placites urlichsi with sub-mature suture lines of late Norian Placites platyphyllus not very real- istic. P. urlichsi differs from P. platyphyllus in its strongly dissolved external saddle, its persistent open umbilicus and its sub-mature tabulate ven - tral stage. Based on these differences Placites urlichsi is hereby transferred to the genus Pompeckjites. Fig 6. Comparison of Pompeckjites urlichsi from Wettersteinkalk to P. urlichsi from the upper San Cassian Formation. A, direct comparison of Pompeckjites layeri in red Hallstatt Limestone from Rappoltstein to white specimens of Pompeckjites urlichsi (mor- photype 1, from Fladung, site 1c). B, phragmocone (showing partial shell) of Pompeckjites urlichsi from the upper San Cassian Formation of Boa Staolin. B1 and B2, venter views of ammonoid B, B3 and B4, enlarged details of the trapezoidal venter development. C, backside of ammonoid B with marked suture lines. D, Pompeckjites urlichsi showing preserved shell on the body chamber and with parts of shell on the phragmocone. D1 - venter view of ammonoid D. D2 and D3, enlarged venter details (without shell) of ammonoid D. E - small specimen of P. urlichsi (morphotype 1, Fladung, site 1c) that is difficult to distinguish from same sized specimens of P. layeri. E1, enlarged trapezoidal venter detail of E. 97 Taxonomic and stratigraphic remarks on Placites urlichsi Bizzarini, Pompeckjites layeri (Hauer), Carnites floridus (Wulfen)... Pompeckjites urlichsi (Bizzarini, 1987) Type species: The designated holotype and the paratypes of Placites urlichsi i n B i z z a r i n i , 1 9 8 7 are hereby accepted as holotype and as paratypes of Pompeckjites urlichsi (Bizzarini, 1987). 1987 Placites urlichsi Bizzarini, p. 50-52, pl. 1, figs. 1, 2a, b, 3a,b, 6a,b, 7, 8; text figs. 2b, 3; tab. p. 52. 1952 Carnites floridus (Wulfen), Leonardi & Polo, pl. 1 figs. 26, 44, 45, 47-49, 55, 57; pl. 2, figs. 39, 40, 41, 42, 43. 2000 Placites urlichsi Bizzarini, pl. 3, figs. 3, 4. We propose the following characteristics to differentiate Pompeckjites layeri (Hauer) from Pompeckjites urlichsi (Bizzarini). Note that the early juvenile stage (up to 5 mm in diameter) in both species is identical in showing a round ven- ter and an open umbilicus. In further growth both species show an eccentric umbilical ingression to - wards to a closed or nearly closed umbilicus. After the umbilicus is closed or nearly closed an eccen - tric umbilical egression evolves in both species. Pompeckjites layeri (Hauer 1847): Persist- ing sharp acute venter up to more than 30 mm di - ameter. Mature sculpture on body chamber is very variable but never showing a tabulate venter. The deeply incised external saddle shows four stems already in juvenile specimens. Large mature size up to 15 cm. Pompeckjites urlichsi (Bizzarini 1987): A rounded sub to high-trapezoidal ventral stage that persists to roughly 15 mm diameter. In morpho - type 1 a distinct tabulate middle keel occurs at this size on steinkerns (Fig. 7, A1; Figs. 8, D, D2). Sometimes this tabulate part of the trapezoidal Fig. 7. Differences of P. urlichsi to P. layeri in transversal and cross-sections. A, polished hand specimen showing frequent transversal-sections of Pompeckjites urlichsi, (morphotype 1, Fladung, site 1c). A1, enlarged trapezoidal venter detail of the internal mold/steinkern. A2, enlarged tabulate venter detail with preserved shell, B, transversal-sections of P. urlichsi (morphotype 2) from Fladung, site 2. B1 and B2, enlarged tabulate venter details. C, cross section of Pompeckjites layeri from the A. austriacum Zone (Hallstatt Limestone of Feuerkogel). D, cross section of P. layeri from the T. aonoides Zone of Rappoltstein. E, trans - versal-section with frequent juvenile specimens of P. layeri (T. aonoides Zone) of Rappoltstein. E1, the white arrow shows the two different venter preservation modes in P. layeri. Blunt triangular without shell (preserved in white calcite on the internal side) compared to the acute venter with shell (preserved in darker calcite). E2, shows a comparable venter development on a steinkern of P. urlichsi morphotype 1. 98 Andreas SPATZENEGGER & Walter POLTNIG venter is very small (Fig. 7, E2). It is more rounded trapezoidal in morphotype 2 steinkerns (Fig. 7, B2) and in specimens of morphotype 1 preserved with shell. After that stage the sub-mature tabu - late venter starts to evolve (Figs. 7, A2, B1). The incised external saddle shows three stems in juve - nile morphs. The mature size of P. urlichsi remains unknown. Specimen found at Hochobir reached a size of 25-30 mm showing a body chamber length of roughly a half to three quarters of a whorl. Species differentiation of Pompeckjites urlichsi, Pompeckjites layeri, Sageceras haidingeri and Carnites floridus based on morphology and polished transversal-sections Morphological similarities between Pompeckjites urlichsi (Bizzarini, 1987), Pinacoceras philopater (Laube, 1869) and Pompeckjites layeri (Hauer, 1847) The second species treated by Bizzarini (1987), was Pinacoceras philopater (Laube, 1869). Bizza- rini (1987) tried to examine the type of P. philopa- ter ( L a u b e , 1 8 6 9 ) , t o g e t h e r w i t h M o j s i s o v i c s ’ (1882) samples, stored in the GBA (Geologische Bundesanstalt Austria). Unfortunately, the origi - nal specimens have not been found. Therefore, we compared our specimens of P. urlichsi morphotype 1 from Fladung/Obir exclusively with the speci - mens of P. philopater and P. urlichsi pictured in Bizzarini (1987: pl. 1) in regards to their form and suture line. Diener (1915b: 189) does not comment on Pinacoceras philopater as to whether it is syn- onymous to Pompeckjites layeri. He just stated that the small specimens are impossible to com - pare with other Pinacoceratidae at generic level. The same conclusion was reached by Mojsisovics (1882). According to Krystyn (1973: 125, see in faunal list of T. aon Zone) Pinacoceras philopater is synonymous with Pompeckjites layeri. Contra - ry to this opinion Bizzarini (1987) established Pompeckjites philopater as a separate species in Pompeckjites. Our own found specimens from Un - terpetzen are well comparable to the specimens shown in Bizzarini (1987: pl. 1, figs. 4a, 4b, 5a, 5b). They mainly differ from P. layeri in less acute venter development. Typical for both species are the similar adven - titious saddle elements that according to Diener (1915b) evolved from a broadly developed exter - nal saddle. In further growth stages these adven - titious saddle stems show a bifid ending in both species. The redrawn original suture line of Pina- coceras philopater (1869: pl. 4 1, fig. 1 0 ) pictured in Figure 8, C4, does not clearly show the position of the lateral saddle. It is not clear if there are three or four adventitious stems in the external saddle. The amount of suture line elements shown in Laube (1869) is similar to Pompeckjites layeri. In contrast the suture line of Pinacoceras philopater in Mojsisovics (1882: pl. 52, fig. 12a) show three stems (redrawn in Fig. 8, C2). The pictured su - ture line of P. philopater in Bizzarini (1 987 : p.49, Fig. 2, A) shows three stems in its external saddle also (redrawn in Fig. 8, C3). In Pompeckjites urlichsi morphotype 1 from Fladung, site 1a-c, the suture line is nearly iden - tical to the suture line of P. philopater in Bizzarini (1987: 49). Morphotype 1 of P. urlichsi shows a sub to high-trapezoidal juvenile venter and a tabulate sub-mature to mature ventral stage that isn’t de - scribed in P. philopater. In fact, some juvenile spec - imens of P. urlichsi morphotype 1 (see figs. 6, E-E1) can show a very acute venter. Such specimens can - not be distinguished from Pompeckjites layeri or Pinacoceras philopater w i t h t h e n a k e d e y e . T h i s can mislead to a classification as Pompeckjites lay- eri when the tabulate venter is not evolved, broken off or not visible in the matrix. Under enlargement the venter on the steinkern of Pompeckjites urlich- si morphotype 1 is always trapezoidal, though the tabulate part of the trapezoidal venter is sometimes very small (see Fig. 5, A2; Figs. 6, B4, E, E1 and F 7 E2). In Pompeckjites layeri the venter is juve- nile or sub-mature always acute. The most acute venter in P. layeri can be s ee n in s pecim e ns wi th well-preserved shell (see Fig. 7, E1). The Figure 8, A shows a fully chambered steink - ern of P. urlichsi from Boa Staolin, which was in - correctly classified as Carnites floridus. The clear - ly visible suture line is comparable to P. urlichsi morphotype 1 from Fladung/Obir. Figure 8, A1 show remains (white arrows) of an eccentric um - bilicus in further growth like in Pompeckjites lay- eri. Here, P. urlichsi shows a body chamber length from a half to three quarters of a whorl which is similar to P. layeri. D and D1, (with small part of shell) in figure 8, show the ventral development in Pompeckjites urlichsi, morphotype 1 that differs clearly from Pompeckjites layeri. The wavy band (distinctly visible on the steinkern, less distinctly visible in shell preservation) on both sides of the venter show reminiscence to the sculpture of large mature specimens of P. layeri from the Hallstatt Limestone where a similar, broader wavy sculp - ture occurs on the ventral flanks (see Fig. 4, A). The enlarged cross-section of P. layeri in Fig. 7, E1 shows a blunt triangular internal venter develop- ment preserved in white calcite (see white arrow). This feature can create distinct ventro-lateral mar - gins on steinkerns. Since similar ventro-lateral 99 Taxonomic and stratigraphic remarks on Placites urlichsi Bizzarini, Pompeckjites layeri (Hauer), Carnites floridus (Wulfen)... margins occur on steinkerns of P. urlichsi morpho - type 1 too (see Figs. 5, A2 and 7, E2) this also may point at a common ancestor of P. urlichsi and P. layeri. Morphological similarities between Pompeckjites urlichsi (Bizzarini, 1987), Carnites floridus (Wulfen, 1793) and Sageceras sp. Diener (1915b) described in Carnites floridus a development of the adventitious elements from the external lobe, precisely from the ascending part of the external lobe to the median saddle (see black circles in Figs. 3, C-C5). Pompeckjites shows, ac- cording to Diener (1915b) no real adventitious el - ements. It shows a broadly created, deeply incised external saddle instead. The fundamental differ - ences in Carnites and Pompeckjites are that the adventitious elements evolves in Carnites on the ventral side of the external lobus and in Pompeck- jites on the ventral side of the external saddle. Species differentiation of P. urlichsi from C. floridus and Sageceras sp. The bifid stem endings in the adventitious ex - ternal saddle elements of Pompeckjites urlich- si originate from a stronger growth of one side branch of former juvenile pyramidal stems. In C. floridus this bifid split of the saddle elements does not exist. In very small specimens of P. ur- lichsi, before this bifid growth feature takes place, the suture line of P. urlichsi is similar to the suture line of Carnites floridus. That may hint at a com - mon ancestor of Carnites and Pompeckjites. The trapezoidal venter development in P. urlichsi may point in this direction too. But these similarities may be just homeomorphic features too. Therefore, it is not surprising that subsequent authors (Leon - ardi & Polo, 1952,) often assigned small specimens of P. urlichsi to C. floridus. Both morphotypes of Pompeckjites urlichsi show in the sub-mature growth stage a tabulate venter which makes them look homeomorphic Fig. 8. Pompeckjites urlichsi from the San Cassian Formation. A, interal mold/steinkern of Pompeckjites urlichsi from Boa Staolin (coll. Alberto Rubini). A1, reminiscence of an eccentric umbilicus (white arrows) in further growth of P. urlichsi. B-B1, venter views of ammonoid A. C-C1, suture of “ Placites” urlichsi in Bizzarini (1987: p. 51, fig. 3, D and E). C2, redrawn suture of “ Pinacoceras” philopater (Laube), in Mojsisovics (1882: pl. 52, fig. 12a). C3, suture of Pompeckjites philopater (Laube) in Bizzarini (1987: p. 49, fig. 2, A). C4, redrawn suture of “ Ammonites” philopater Laube, 1869: pl. 41, fig. 10. D, enlarged detail of the wavy bands beside the small tabulate keel. D1, small part of shell that indicates a more rounded trapezoidal venter in specimens preserved with shell. 100 Andreas SPATZENEGGER & Walter POLTNIG to Sageceras s p . ( s e e F i g s . 7 , A 2 ; 9 C 1 , E 1 ) . I n cross-sections, P. urlichsi can be distinguished from Sageceras sp. by the different developments of the juvenile whorls (see Fig. 7, A1 compared to Fig. 9, D1). The height of the shell aperture is a helpful distinguishing feature in cross-sections too. Sageceras sp. shows roughly a proportion of 1:1 in the ratio of aperture height to the rest of the whorl (see Fig. 9 D). In Carnites floridus and P. urlichsi the ratio of aperture height to the rest of the whorl is closer to 1:2. Juvenile whorls of Sageceras sp. and Carnites floridus a r e v e r y s i m i l a r i n p o l i s h e d t r a n s v e r - sal-sections. The flatter angle of the flank is in Sageceras sp. (see in Fig. 9, D,) during growth rel - atively constant at 8-10°, whereas in C. floridus (see Fig. 9, A) the angle increases up to 30°. Both in figures. 9, A-A2 and B-B1, shown C. floridus originate from Hallstatt Limestone of Rappoltstein (Hornung et. al 2007) and were found together with a sparse A. austriacum Zone ammonoid fau - na with Neoprotrachyceras thous and Austrotra- chyceras sp. If the suture lines can be checked, a confusion of Sageceras sp. with Carnites floridus or Pom- peckjites sp. can be excluded. Stratigraphic conclusions Our data suggest that Carnites floridus Hauer is restricted to the first strong pulse of the CPE (Carnian Pluvial Episode) at the border T. aonoides Zone to A. austriacum Zone (for further literature regarding to the CPE we refer to the reference lists of Dal Corso et al. 2018; Hornung et al. 2007; Mu - eller et al. 2016 and Preto et al. 2019). An early Ju - lian T. aon Zone age or an early Tuvalian Tropites dilleri Zone age of true C. floridus can be exclud - ed. Based on true Carnites floridus the first Raibl shale horizon on Hochobir can be correlated with the beginning of the A. austriacum Zone. This is Fig. 9. Species differentiation of P. urlichsi from C. floridus and Sageceras sp. A, polished cross-section of Carnites floridus from Hallstatt Limestone of Rappoltstein. A1 and A2, enlarged development of the tricari - nate venter. B, C. floridus from Rappoltstein. B1, view of the tricarinate venter. B2, suture line of C. floridus in Mojsisovics (1873: pl. 25, fig. 4). C, transversal-sections of numerous Pompeckjites urlichsi (morphotype 1) from Fladung/Obir. C1 and C2, enlarged tabulate venter development of P. urlichsi. E, Sageceras haidingeri from the T. aonoides Zone of Rappoltstein. E1, venter of Sageceras sp., E2, suture line of Sageceras. D, cross-section of Sageceras sp. from Hallstatt Limestone of Rappoltstein with outlined flank angle and ratio of aperture height to the rest of the winding. D1, enlarged detail of the juvenile venter. 101 Taxonomic and stratigraphic remarks on Placites urlichsi Bizzarini, Pompeckjites layeri (Hauer), Carnites floridus (Wulfen)... evidenced in the Hallstatt Limestone of Rappolt - stein where Carnites floridus, Neoprotrachyceras thous and Austrotrachyceras sp. were found (Hor - nung et al. 2007) and in the Reingraben shales of Austria where Carnites floridus was referred to the A. austriacum Zone in Lukeneder & Lukened- er (2022). Therefore, the underlying Bleiberger Sonderfazies (Holler 1960) with Pompeckjites ur- lichsi can indirectly be correlated with the upper T. aonoides Z o n e . A c o r r e c t s p e c i e s r e c o g n i t i o n of P. urlichsi, allows a direct correlation of some parts/layers of the Upper San Cassian Formation with layers of the Bleiberger Sonderfazies (upper Wettersteinkalk). Minor morphologic differences in juvenile whorls of P. urlichsi further allow for a differentiation in a morphotype 1 and a slightly younger morphotype 2. Furthermore, the onset of the A. austriacum Zone can be fixed with true C. floridus in strata where Austrotrachyceras sp., was not found. Pom- peckjites urlichsi in contrast allows for a fixing of the upper T. aonoides Zone in strata where Trach- yceras s. str. was not found or is missing. Discussion A transitional ammonoid fauna spanning the period from the T. aonoides to the A. austriacum ammonoid Zones is not adequately described at present. From an evolutionary view such a fau - na should exist. Pompeckjites urlichsi (Bizzarini) seems to be an appropriate ammonoid species showing a close stratigraphic range that may fit as an index ammonoid to close this gap. It may be of future importance for a finer stratigraphic correlation between the basinal facies of the up- per San Cassian Formation and the coeval algal rhytmites of the upper Wettersteinkalk. Within the condensed pelagic deposits of the Hallstatt Limestone P. urlichsi h a s n o t b e e n f o u n d s o f a r . This might have its origin in a collecting hiatus, in a confusion with small specimens of Pompeckjites layeri or Carnites floridus or in the possibility of a habitat restriction to the reef fronts and their directly adjacent basins. The above mentioned close morphologic similarity of P. urlichsi to small Carnites floridus raises some doubts on Carnites floridus classifications from the upper T. aonoides Zone of the Rio del Lago Formation (Preto et al. 2005). Such small C. floridus are surmised to be Pompeckjites urlichsi ( B i z z a r i n i ) a n d t h u s m a y need further revision. According to Krystyn (1978) Pompeckjites lay- eri spans the entire Julian stage and Pinacoceras philopater is thought to be synonymous (Krystyn 1973: 125, see in faunal list of T. aon Zone). Con - trary to that opinion, Bizzarini (1987) established Pompeckjites philopater as a separate Pompeck- jites species. Here we classify all Pompeckjites species that show a sub-mature tabulate venter as Pompeckjites urlichsi. The transfer from Placites to Pompeckjites in P. urlichsi is based on the simi - lar sutureline, the similar juvenile venter develop - ment and the similar eccentric umbilical egression compared with Pompeckjites layeri. Especially juvenile specimens of Pompeckjites urlichsi mor- photype 1 show a close similarity to Pompeckjites layeri. Pompeckjites philopater as pictured in Biz - zarini (1987) is intermediate in shape between P. layeri and juvenile P. urlichsi morphotype 1 before evolving the tabulate venter. Juvenile specimens of P. urlichsi morphotype 2 do show some similarity in shape and suture line to Pinacoplacites Diener, 1916. A presumed evolutionary connection of Ju - lian Pompeckjites urlichsi to upper Tuvalian Pina- coplacites sp. may exist via “Placites” placodes but it is not confirmed at present. Further research to this assumption was hindered by lacking data. Acknowledgements We sincerely thank the UNESCO Geopark Kar - awanken/Karavanke (A/Slo) for the permission to car - ry out fieldwork and research in its area, Matija Križ- nar (Slovenian Museum of Natural History, Ljubljana) and Ivan Ocepek (Me žica), for the possibility to visit the historical mining area Unterpetzen/Podpeca (Slo - venia), Peter Englmaier, ECONSULT expert consultan - cy, Vienna and University of Vienna, for the help in the fieldwork, writing and literature search, Alberto Rubini (Italy) for the pictures of the ammonoid from Boa Stao - lin on Figures. 6 B-C, 8 A-D, Roger Furze (Germany), Heidi Henderson and Karen Lund (Vancouver/Canada) for their help to improve our English. References Arthaber, G. 1905: Die alpine Trias des Mediter - ran-Gebietes. In: Frech, F. (ed.): Lethaea geog - nostica, pt. II, Das Mesozoicum, Trias: 223– 391, 417–472. Arthaber, G. 1911: Die Trias von Albanien – Beiträge zur Paläontologie von Österreich. 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