balini_kry 47..84 LATE CARNIAN-EARLY NORIAN AMMONOIDS FROM THE GSSP CANDIDATE SECTION PIZZO MONDELLO (SICANI MOUNTAINS, SICILY) MARCO BALINI 1, LEOPOLD KRYSTYN 2, MARCO LEVERA1 & ANGELO TRIPODO 3 This paper is dedicated to the memory of Paola De Capoa, the first paleontologist since the time of G.G.Gemmellaro to understand the great paleontologic potential of the ‘‘calcari con selce’’ of western Sicily. Received: January 9, 2012; accepted: February 27, 2012 Key words: Upper Triassic, Carnian/Norian boundary, Ammo- noids, Biostratigraphy, Sicily, Sicanian Domain, Scillato Formation. Abstract. A small collection of ammonoids from the Upper Triassic Scillato Formation at Pizzo Mondello (Agrigento, Sicily) is studied. These specimens were collected within the framework of a project intended to provide integrated high-resolution bio-chronostra- tigraphic support for the Upper Carnian-Norian magnetostratigraphic scale defined at this site, which is located in an historical area from which G.G. Gemmellaro collected and monographed Upper Triassic ammonoids at the beginning of the 20th century. The specimens, which were collected utilizing the bed-by-bed sampling method, represent the first collection of Upper Triassic ammonoids described from western Sicily since Gemmellaro’s time. Several levels of the Pizzo Mondello section yielded ammonoids, but very few beds have provided more than one specimen. This scarcity of specimens has resulted in a complex taxonomic analysis because Gemmellaro, who described 166 new spe- cies, did not explain the variability of many of his taxa. Sixteen taxa belonging to eleven genera are described. They include Placites sp. ind., Discotropites plinii (Mojsisovics), Anatropites sp. ind., Microtropites cf. paronai, Metathisbites cf. affinis, Hyattites cf. praefloridus, Projuvavites boehmi (Gemmellaro), Projuvavites inflatus (Gemmellaro), Goniono- tites cf. italicus, Gonionotites aff. recuperoi, Pregriesbachites n. gen., P. bukowskii (Gemmellaro), Dimorphites noricus n. sp., Dimorphites se- lectus Mojsisovics, Dimorphites sp. and Discophyllites insignis. Among the new taxa, Dimorphites noricus n. sp. formalizes the nomen nudum ‘‘Dimorphites n. sp. 1’’, which has been quoted in the literature for several years as the index ammonoid for the lowest subzone of the Norian stage. The small collection documents the Discotropites plinii and Go- nionotites italicus subzones of the uppermost Carnian Spinosus Zone as well as the Dimorphites noricus and D. selectus subzones of the Jandia- nus Zone, the first zone of the Lower Norian. This chronostratigraphic classification not only confidently ties the Pizzo Mondello succession to the Tethyan chronostratigraphic scale, but it is also crucial for the calibration of the Halobia and conodont bioevents identified in the section. Also discussed is the chronostratigraphic ammonoid-based correlation of the Pizzo Mondello section with Feuerkogel (Austria), Jomsom (Nepal), West Union Canyon (Nevada, USA), Black Bear Ridge (British Columbia, Canada) and the Yana Okhotskaya River (Siberia, Russia). These are the most complete ammonoid-bearing sec- tions in the world that span the Carnian/Norian boundary, and they exhibit a discrete distribution of ammonoid-bearing beds across the boundary. Ammonoids will not provide the primary marker event for the definition of the GSSP of the Norian, but they are crucial for the selection of the most significant events based on other groups. Riassunto. In questo lavoro viene studiata una piccola collezio- ne di ammonoidi proveniente dalla Formazione Scillato (Triassico su- periore) di Pizzo Mondello (Agrigento, Sicilia). Gli esemplari sono stati raccolti nel quadro di un progetto finalizzato alla taratura bio-crono- stratigrafica integrata e ad alta risoluzione della scala magnetostratigra- fica del Carnico superiore e Norico riconosciuta in questa località. Pizzo Mondello è una località fossilifera nuova, ubicata in un’area storica della Sicilia da cui G.G. Gemmellaro raccolse gli ammonoidi del Triassico superiore che descrisse in un’importante monografia al- l’inizio del XX secolo. Gli esemplari di Pizzo Mondello sono stati raccolti strato-per-strato e rappresentano la prima raccolta di ammo- noidi del Triassico superiore della Sicilia occidentale descritta in oltre un secolo dalla monografia di Gemmellaro. Gli esemplari provengono da numerosi livelli della sezione, all’interno dei quali però spesso gli ammonoidi sono molto rari. La classificazione dei nuovi esemplari è risultata complessa in quanto Gemmellaro, che nella sua monografia descrisse 166 specie nuove, non fornı̀ indicazioni chiare sulla variabilità dei suoi taxa. Vengono descritti 16 taxa, appartenenti a 11 generi: Placites sp. ind., Discotropites plinii (Mojsisovics), Anatropites sp. ind., Microtropi- tes cf. paronai, Metathisbites cf. affinis, Hyattites cf. praefloridus, Pro- juvavites boehmi (Gemmellaro), Projuvavites inflatus (Gemmellaro), Gonionotites cf. italicus, Gonionotites aff. recuperoi, Pregriesbachites Rivista Italiana di Paleontologia e Stratigrafia volume 118 no. 1 3 pls. pp. 47-84 March 2012 1 Dipartimento di Scienze della Terra ‘‘Ardito Desio’’, Via Mangiagalli 34, 20133 Milano, Italy. E-mail: Marco.balini@unimi.it 2 Department of Palaeontology, Vienna University, Althanstraße 14, 1090 Wien, Austria. 3 Dipartimento di Scienze della Terra e del Mare, Università di Palermo, Via Archirafi 22, 90123 Palermo, Italy. n. gen., P. bukowskii (Gemmellaro), Dimorphites noricus n. sp., Dimor- phites selectus Mojsisovics, Dimorphites sp. e Discophyllites insignis. Dimorphites noricus n. sp. è il più importante tra i nuovi taxa e rap- presenta la descrizione di un nomen nudum riportato nella letteratura recente come ‘‘Dimorphites n. sp. 1’’. Questa specie è indice della prima sottozona del Norico. La collezione studiata permette di riconoscere le sottozone a Discotropites plinii e a Gonionotites italicus della Zona a Spinosus del Carnico sommitale, e le sottozone a Dimorphites noricus e D. selectus della Zona a Jandianus, la prima zona del Norico inferiore. Questa classificazione cronostratigrafica data in modo chiaro la successione di Pizzo Mondello con la scala cronostratigrafica della Tetide, ed è fondamentale per la taratura dei bioeventi ad Halobia ed a conodonti individuati nella stessa sezione. Vengono discusse le correlazioni cronostratigrafiche ad ammo- noidi con le migliori sezioni stratigrafiche del mondo, per quanto ri- guarda il limite Carnico/Norico. Queste sono Feuerkogel (Austria), Jomsom (Nepal), West Union Canyon (Nevada, USA), Black Bear Ridge (British Columbia, Canada) e del fiume Yana Okhotskaya (Si- beria, Russia). Tutte queste sezioni sono caratterizzate da una distribu- zione discontinua di ammonoidi, soprattutto in corrispondenza del limite Carnico/Norico. Di conseguenza, molto probabilmente gli am- monoidi non forniranno l’evento primario per la definizione del GSSP del Norico, ma sono fondamentali nel processo di ricerca e valutazione dei bioeventi riconosciuti in altri gruppi sistematici. Introduction The ‘‘cherty limestone’’ (‘‘Calcari con selce’’ or Halobia Limestone auct., Scillato Formation: Schmidt di Friedberg et al. 1960) of western Sicily are been well known since the second half of the 19th century for its rich macrofossil record of Upper Triassic pelagic bi- valves (halobiids) and ammonoids, first described by G.G. Gemmellaro (1882 and 1904). Following Gem- mellaro’s pioneering works, the investigation of halo- biids continued and a few authors (Montanari & Renda 1976; De Wever et al. 1979; Cafiero & De Capoa Bo- nardi 1982; De Capoa Bonardi 1984) provided the first picture of the stratigraphic distribution of the various species within the ‘‘cherty limestone’’ as well as the re- finement of their taxonomy (see especially Cafiero & De Capoa Bonardi 1982 and De Capoa Bonardi 1984). Curiously, not even one specialist has chosen to follow in the ‘‘footprints’’ of Gemmellaro and continue the study of Triassic ammonoids from western Sicily, and since Gemmellaro’s 1904 monograph, the literature regarding this fossil group is restricted to just the report of a single specimen of Hoplotropites from the Monte Cammarata section by Cafiero & De Capoa Bonardi (1982: fig. 2 and pl. 6, fig 4-5). Such a lack of literature is surprising because on the one hand, the collection from western Sicily described by Gemmellaro consisted of several hundreds of specimens from several localities scattered over six different areas (Gemmellaro 1904; Tripodo 2011). On the other hand, a few new but very small collections have been made during the 20th cen- tury from localities in Sicily that did not provide near as much material as found during Gemmellaro’s time (e.g., Mufara Formation [Ladinian-Carnian] from Palermo area: Zia 1956; ‘‘cherty limestone’’ from Monte Judica, eastern Sicily: Lentini 1974). In this paper we describe and illustrate ammo- noids collected during a four-year long research pro- gram, whose purpose was to provide a high-resolution integrated bio-chronostratigraphy for the Upper Trias- sic magnetostratigraphic scale and stable isotope curve by Muttoni et al. (2001 and 2004) in the Pizzo Mondello section (Sicani Mountains, Agrigento). In just a very few years, this section has become known worldwide for its unusually thick and uniform Late Carnian to Rhaetian pelagic record as well as for the good preser- vation of its primary magnetization. Such a rare combi- nation of features lead Hounslow & Muttoni (2010) to propose this section as a standard reference for the cali- bration of the Upper Triassic GPTS (Geomagnetic Po- larity Time Scale). This extensive bio-chronostratigraphic investiga- tion, based on a very thorough bed-by-bed sampling pro- gram for ammonoids, halobiids, conodonts and radio- larians was carried out by specialists from five Italian universities in cooperation with foreign specialists with- in the framework of the activities of the Carnian-No- rian boundary Task group of the Subcommission on Triassic Stratigraphy. Due to the importance of the Piz- zo Mondello section for the definition of the GSSP (Global Stratotype Section and Point) of the Norian Stage, the investigation focused on the lower part of the Scillato Formation, which is the formal name for the ‘‘cherty limestone’’ auct., straddling the Carnian/ Norian boundary. We herein provide taxonomic de- scriptions for the ammonoids collected during the pro- ject, which complement the taxonomic descriptions for the halobiids (Levera 2012) and the conodonts (Mazza et al. 2012). Lithostratigraphy and stratigraphic section As shown in Fig. 1, the Sicani Mountains of Wes- tern Sicily are characterized by a typical Permian to Cenozoic pelagic succession (Mascle 1979) of the Sica- nian domain, which is divided into several tectonic units (Sicanian structural units: Catalano et al. 1995) that are overthrust onto a thick allochthonous complex of Neo- gene mudstones and evaporites of the Gela Nappe (Bel- lanca et al. 1993; Bellanca et al. 1995; Guaiumi et al. 2007 and references therein). The Pizzo Mondello section, located in the low- ermost Sicanian thrust sheet (Pizzo Mondello tectonic unit) that overthursts upper Tortonian-Messinian clays, consists of three Triassic units, the Mufara Formation, the Scillato Formation and the Portella Gebbia Lime- stone (Di Stefano 1990; Gullo 1996; Di Stefano & Gullo Balini M., Krystyn L., Levera M. & Tripodo A.48 1997; Guaiumi et al. 2007). The Scillato Formation (Schmidt di Friedberg et al. 1960) is the formal name accepted and codified by the ISPRA (Italian Geological Survey) for the unit known as ‘‘cherty limestone’’ or ‘‘Calcari con selce’’ or Halobia Limestone in Sicily. Relatively new, the Pizzo Mondello locality was first described in the mid 1990s (Bellanca et al. 1995 and Gullo 1996), but it is located within Gemmellaro’s ‘‘Regione ex-feudo Votano’’, one of the source areas for a large part of his collection of Halobia and ammo- noids. Within this wide area (Fig. 1) the two best known localities for the Scillato Formation are Monte Triona and Monte Cammarata, both of which were studied in the 1970s and early 1980s (Montanari & Re- nda 1976; Mascle 1979; De Wever et al. 1979; Cafiero & De Capoa Bonardi 1982; De Capoa Bonardi 1984). Monte Triona is located about 14 km northwest of Piz- zo Mondello, and Monte Cammarata is about 19 km to the east. Outcrops at Pizzo Mondello are of much better quality than at Monte Triona and Monte Cammarata, and the locality is much better suited for a high resolu- tion bed-by-bed sampling study. This observation ap- plies especially to the lower part of the 430 m thick Scillato Formation, which straddles the Carnian/Norian boundary. This part is easy accessible at Pizzo Mondello because it is exposed in an abandoned quarry that was active in the 1970s (‘‘La Cava’’ on some topographic maps). This 143 m thick interval (Fig 2), equivalent to Interval II of Muttoni et al. (2001, 2004), has been ex- tensively sampled for ammonoids along two segments A and B, which in part overlap (Fig. 3). The distance between the two segments is about 200 m, and correla- tion is achieved simply by following the beds along strike. Bed thickness does not change between the seg- ments and the thicker beds serve as excellent marker levels. Lithologically, the succession consists mostly of evenly bedded to nodular Halobia-bearing cherty calci- lutites. This particular sequence was recently described by Guaiumi et al. (2007), Nicora et al. (2007), Balini et al. (2008) and Balini et al. (2010). Sampling During the past 10 year period, the Pizzo Mon- dello section has been sampled several times by specia- lists from a wide spectrum of fields including magnetos- tratigraphy, sedimentology, micro- and macropaleontol- ogy. During this time, sampling has become more and more thorough and several types of labels and number- ing schemes have been used (for details see Balini et al. 2010). Beginning in 2006, the basis for all samplings has been an extremely detailed stratigraphic log measured by Preto and Guaiumi in the lower 143 m of the section underlying the Slump breccia (interval III of Muttoni et Carnian-Norian ammonoids from Pizzo Mondello 49 Fig. 1 - Geological and Structural map of the Monti Sicani (Sicani Mountains) showing the distribution of the Sicanian Triassic to Oligocene pelagic successions, as well as the position of Pizzo Mondello with respect to Monte Triona and Monte Cammarata (from Cacciatore et al. 2010). Balini M., Krystyn L., Levera M. & Tripodo A.50 Fig. 2 - Stratigraphic log of the Pizzo Mondello section. A) The complete development of the section, from the base of the Scillato Formation to the Portella Gebbia Limestone, with magnetostratigraphy (Muttoni et al. 2001, 2004) and position of the conodont samples studied by Nicora et al. (2007), Mazza et al. (2010), Mazza et al. (2011) and Mazza et al. (2012). The log is from Balini et al. (2010) and is partly modified from Muttoni et al. (2004). B) detail of the lower part of the Scillato Formation (143 m) sampled for ammonoids. al. 2001, 2004). All previous samples taken by Muttoni et al., (2001 and 2004) that could be correlated with numbers painted on the beds, were also plotted on the log. When possible, ammonoids were labelled with the bed number from which they were collected, provided the bed had been previously sampled. Ammonoids from beds with no label have been numbered as PMAMxx. The sequence of these samples is merely chronologic and has no relation to the stratigraphic succession. The ammonoid record Six field trips to Pizzo Mondello, each averaging about one week duration, were carried out between spring 2007 and fall 2010. From the beginning, ammo- noids were found throughout the succession, but their occurrence was found to be quite rare (Fig. 4). Because of this scarcity, it was necessary to follow the beds along strike for tens of meters searching for ammonoid cross- sections on the outcrop. The resulting collection was combined with ammonoid specimens found during the thorough bed-by-bed search for Halobia that even in- cluded beds without visible macrofossils on the surface. A total number of 166 beds were sampled utilizing this approach (see Levera 2012). Overall, the final collection consists of 130 am- monoids collected from a stratigraphic interval of about 100 m. On rare occasions, two or more specimens were collected from the same bed (Fig. 4B), and even though the resulting collection is representative of the ammo- noid record of the section, it does not allow for a po- pulation analysis. Most of the ammonoids are about 1 or 2 cm in diameter (Fig. 4A) and the frequency of larger specimens decreases with increasing size. The largest specimen (Fig. 4D) is a Gonionotites of about 10 cm in diameter. Quite often, specimens are preserved with a strongly recrystallized test, but some are also pre- served as internal molds (Fig. 4C). The latter are usually very easy to extract from the rock matrix. Ammonoid taxonomy: the complex heritage of G.G. Gemmellaro As mentioned in the Introduction, our knowledge of Triassic ammonoids from western Sicily is based en- tirely on the monograph by Gaetano Giorgio Gemmel- laro (1832-1904) that was published just after his death by his collaborators G. Di Stefano, L. Schopen and A. Carapezza (Gemmellaro 1904: p. III). This monograph is based on a large collection of ammonoids from the Carnian-Norian ammonoids from Pizzo Mondello 51 Fig. 3 - General view of the lower part of the Scillato Formation at ‘‘La cava’’, showing the position of the two segments of the composite section. The beds of the upper part of the segment A can be followed along strike to the lower part of the segment B (see also Fig. 2). following areas: Palermo (‘‘Regione Giacalone’’, ‘‘Cave di Billiemi’’), Trapani (‘‘Castellammare del Golfo’’), Bi- sacquino (‘‘Regione Madonna del Balzo’’= Monte Trio- na), S. Stefano Quisquina s.l. (‘‘Regione ex-feudo Vota- no’’) and Castronuovo (‘‘Regione Modanesi’’), of which the major part is preserved in the Museo Geologico G.G. Gemmellaro of the University of Palermo. Gem- mellaro did not always provide the total number of specimens attributed to each of his taxa, but the agree- ment between the number of specimens mentioned by him and the specimens stored in the Museo is generally quite good. The registered collection includes 780 speci- mens. Gemmellaro’s monograph is devoted entirely to taxonomy, with the description of 166 new species (and 84 taxa in open nomenclature), attributed to 49 genera and subgenera. The genera Siculites, Palicites, Mojsisovicsites and Gonionotites were also erected in this monograph. However, even with this impressive and well illustrated taxonomy (30 high quality plates), two main weak points are immediately obvious. The first is the lack of detailed geographic and geological information regarding the successions from which the fossils were collected and the number and position of the fossil-bearing levels. The second major problem is the lack of a biostratigraphic analysis of the faunas. This second point is somewhat surprising because by the end of the 19th century the knowledge of ammonoid bio- chronostratigrahic scales was well developed (i.e., Moj- sisovics et al. 1895), and the common practice followed by all authors of that time was to include in every am- monoid monograph a chapter on faunal subdivision and correlation. This absence of critical information is diffi- cult to understand; it is possible that Gemmellaro did not collect the major portion of the material by himself, or maybe he was unable to complete his monograph. No matter the reason, this information was not re- ported, and this may well be one of the reasons for the relatively low scientific impact of Gemmellaro’s monograph. Balini M., Krystyn L., Levera M. & Tripodo A.52 Fig. 4 - Field pictures of ammonoids. A) Cross section of a small specimen from level PMAM12. B) Rare occurrence of two specimens from the same level, FNP317b. C) Rarely the specimens are exposed in 3D and easy to be extracted: Projuvavites inflatus MPUM 10974, level PMAM49. D) Sometimes the specimens identified on the basis of the cross section are also easy to be collected, here Gonio- notites cf. italicus MPUM 10975 from level PMAM7 (Pl. 2, fig. 1a-b). New genera described by Gemmellaro have gen- erally been accepted (e.g., Arkell et al. 1957; Tozer 1981a), but very few workers have tried to improve his taxonomy at the species level. Spath (1951) described the new genus Euisculites with Isculites bittneri Gem- mellaro as type species and Tozer (1994) included Sty- rites disciformis Gemmellaro in his new genus Discosty- rites. Some authors have not even mentioned Gemmel- laro’s monograph Diener’s (1906: 6) criticism was in some respects ‘‘extreme’’, when he wrote that Gemmel- laro’s monograph could not be used because ‘‘the types are represented in a manner which defies every attempt to realize their true shape’’. Surprisingly, for taxa with no stratigraphic posi- tion, a few of Gemmellaro’s taxa have recently been recognized as having stratigraphic significance. Gonio- notites italicus Gemmellaro was proposed by Krystyn in 1980 as an index ammonoid for the latest subzone of the Carnian Stage. Since then, the Gonionotites italicus sub- zone of the Spinosus Zone has became part of the Upper Triassic Tethyan scale (Krystyn et al. 2002; Balini et al. 2010). The genus Mojsisovicsites Gemmellaro, which is not found elsewhere in the Tethys realm, was recognized in North America by Silberling (1959), who attributed Stikinoceras kerri McLearn, 1930 to Gemmel- laro’s genus as the index taxon for the first zone of the Norian Stage. Tozer (1994) later rejected this attribu- tion, but Mojsisovicsites and Stikinoceras are still con- sidered to be very closely related forms. The lack of new discoveries and taxonomic revi- sions, especially at the species level, implies that the state of the taxonomy of ammonoids from the Scillato Formation/‘‘cherty limestone’’ remains the same as it was in 1904. This suggests that species are defined with a typologic approach, sometimes based on single speci- mens or even juveniles, or based on specimens grouped together on the basis of assumptions and not on onto- geny and population variability analyses. Last but not least, there is a lack of information about the strati- graphic position of the specimens. As so ably summar- ized by Tozer (1971), such a wide range of problems were rather normal for monographs published in the second half of the 19th century, but in the case of Gem- mellaro’s work the problem is much more severe be- cause of the much greater uncertainty about the strati- graphic position of his taxa. The interval from which his taxa were collected is not restricted to just one or two substages, but rather it encompasses much of the Upper Carnian through the entire Norian stage. Taxonomic results The classification of the present collection from Pizzo Mondello and its comparison with the type speci- mens of the Gemmellaro collection, recently re-de- scribed by Tripodo (2011), provides the opportunity to test Gemmellaro’s taxonomy with all its flaws as well as to evaluate the significance of his collection. A few points must be stressed: a) Twelve genera have been identified in the new collection: Placites, Discotropites, Anatropites, Microtro- pites, Metathisbites, Hyattites, Projuvavites, Goniono- tites, Dimorphites, Discophyllites, Rhacophyllites and Pi- nacoceras. In addition, we describe the new genus Pre- griesbachites in the Systematic paleontology. Small am- monoids are also referred to the families Sandlingitidae and Arcestidae. All genera identified herein are docu- mented in the list of taxa described by Gemmellaro. The genus Discotropites Hyatt & Smith, 1905 includes al- most all species described by Gemmellaro as Eutomo- ceras. Another Tropitidae well represented in the Gem- mellaro collection is Hoplotropites Spath, 1929, which is the new name for Margarites Mojsisovics, 1889. This genus, typical of the Discotropites plinii subzone, has not yet been found at Pizzo Mondello. A group of Juvavitidae that is well documented in the Gemmellaro collection (37 species) is Anatomites Mojsisovics, 1893. However, several species originally attributed to this genus would be better included in Projuvavites Tozer, 1971. b) The taxonomic study of ammonoids from Piz- zo Mondello provided an opportunity to describe two new taxa already outlined by Krystyn (1980, 1982) dur- ing an investigation of classic localities in the Salzkam- mergut area (Northern Alps) and a new site in the Ne- palese Himalaya. Dimorphites noricus n sp. is a new species quoted in several previous papers as Dimor- phites n. sp. 1, and the new genus Pregriesbachites is erected for the ‘‘Projuvavites n. gen. with nodes on the body chamber’’ mentioned by Krystyn (1982). Both new taxa are also documented in the Scillato Formation at Pizzo Mondello. c) Classification of our specimens to a species rank has often revealed the limits of Gemmellaro’s ty- pologic approach to taxonomy. Ammonoids are rare in the sedimentary successions, and thus far it has proven very difficult to collect more than one specimen per bed. Comparison of these newly collected single speci- mens to Gemmellaro’s species, which are often illu- strated by only one or two types, is usually quite frus- trating. Information regarding species variability is not available, and often the new specimens do not corre- spond well with one particular type specimen, but rather, they more commonly are similar to two or more type specimens of different species. For instance, this is the case for the single Microtropites specimen from level PMAM52A that in some respects resembles M. paronai (Gemmellaro), while for others it is more similar to M. brancoi (Gemmellaro). Similarly, the best preserved Go- Carnian-Norian ammonoids from Pizzo Mondello 53 nionotites from level PMAM7 does not correspond well with any of the 11 species of Gonionotites described by Gemmellaro. d) For a modern taxonomic revision of many of Gemmellaro’s groups, it would be absolutely necessary to require a definition of their variability. However, very few beds of the Scillato Formation would provide en- ough specimens for even a simplified population analy- sis. A group that may potentially benefit from this ap- proach is Gonionotites, which is relatively common in the succession. However, the main difficulty with this group is the large size of its type specimens, which con- trasts with the extreme scarcity of these larger specimens and the high frequency occurrence of small- or medium- sized specimens in the succession. Several of the eleven species attributed to this genus by Gemmellaro seem to be distinguished only by the adult body chamber. e) Overall, Gemmellaro’s studied collection is clearly representative of the ammonoid record of the Scillato Formation. A few of his genera have not been found in the field (e.g., Jovites) but it is worth noting that a number of very rare, small forms were actually collected by him or by his collaborators. Dimorphites, for instance, belongs to this group. Thus far it has been found only in five beds at Pizzo Mondello, and the specimens are of rather small size. This scarcity, not- withstanding that Dimorphites is documented by sev- eral specimens in Gemmellaro’s collection. In the next chapter, we provide descriptions for the most significant and representative taxa, but a few specimens are left in open nomenclature. This approach strictly follows the recommendations of Salvador (1994: 91) and Remane et al. (1996) concerning the publication and illustration of the fossil record documented in GSSP sections. In addition to this formal reasoning, the description of the ammonoid record is useful for calibration of the Halobia and conodont bioevents (Le- vera 2012; Mazza et al. 2012). Repository of specimens. Specimens described in this contri- bution are housed in three institutions in Italy and Austria as follows: MPUM: Museo di Paleontologia, Dipartimento di Scienze della Terra ‘‘Ardito Desio’’, Università degli Studi di Milano, Via Mangiagalli 34, 20133 Milano, Italy. MGUP: Museo Geologico G.G. Gemmellaro, Università degli Studi di Palermo, Corso Tukory 131, Palermo, Italy. GBA: Sammlungen der Geologischen Bundesanstalt, Neuling- gasse 38, A-1030 Wien, Österreich. Numbering of the specimens. Every specimen mentioned in the text is identified by both registration number (e.g., MPUM....) and collection number. The latter, in parenthesis, indicates the bed of col- lection and the individual number of the specimen (e.g., FNP144-2: 2nd specimen from bed FNP144). Dimensions. D= diameter; H= max. whorl height in D; h= min. whorl height in D; U= umbilical width in D; W= whorl width in H; SGR= (H-h)/h x 100. All measurements are in mm. SGR is in percent. Measurements in italics represent partly damaged specimens. Occurrence. In the Systematic paleontology and Chronostrati- graphy sections, the nomenclature for chronozones follows Hedberg (1976). This nomenclature is more synthetic than the one required by Salvador (1994): Jandianus Zone, instead of Guembelites jandianus chronozone. For subzones, biostratigraphic nomenclature is used be- cause there is no chronostratigraphic counterpart for such a short sub- unit. Systematic paleontology Family-group taxonomy follows that of Tozer (1981a and 1994). Order Ceratitida Hyatt, 1884 Superfamily Pinacocerataceae Mojsisovics, 1879 Family Gymnitidae Waagen, 1895 Subfamily Gymnitinae Waagen, 1895 Genus Placites Mojsisovics, 1896 Type species: Pinacoceras platyphyllum Mojsisovics, 1873 Placites sp. ind. Pl. 1, fig. 1; Fig. 5 Material: One specimen MPUM 10966 (NA49.1-1). Description. Small specimen (D= 15.3mm) pre- served as a three dimensional internal mold. Specimen is a juvenile, last 70º of coiling belongs to the body chamber. Involute platycone with nearly closed umbili- cus, compressed elliptical whorl section and very nar- row venter. Suture line (Fig. 5) is typical of Placites. Discussion. Species of Placites may reach a dia- meter of 100 mm and are distinguished (cf. Mojsisovics 1873) mainly on the basis of their whorl section and suture line at medium to large size, i.e., adult stage of growth. The specimen from Pizzo Mondello (level NA49.1) is clearly a juvenile and therefore is left in open nomenclature. Occurrence. As with most of Gymnitidae, Pla- cites is a long-ranging form; its range spans the entire Norian to Rhaetian stages. The specimen described here was collected from a bed yielding Halobia mediterranea (see Levera 2012), a species usually referred to the Paulckei Zone (Krystyn et al. 2002; Levera 2012). Balini M., Krystyn L., Levera M. & Tripodo A.54 Fig. 5 - Suture line of Placites sp. ind., specimen MPUM 10966 (NA 49.1.-1). Bar scale 2 mm. Superfamily Tropitaceae Mojsisovics, 1875 Family Tropitidae Mojsisovics, 1875 Genus Discotropites Hyatt & Smith, 1905 Type species: Ammonites sandlingensis Hauer, 1850 Discotropites plinii (Mojsisovics, 1893) Pl. 1, fig. 2a-b 1893 Eutomoceras plinii Mojsisovics, p. 289, pl. 130, fig. 4, 5, 6. 1982 Discotropites plinii – Krystyn, p. 34, pl. 7, fig. 3-4. [Cum syn.] 2000 Discotropites plinii - De Zanche et al., pl. 1, fig. 1a-b. Stratum typicum: Hällstatter Kalk, at Feuerkogel (Salzkam- mergut, Austria). Lectotype: Original of Mojsisovics 1893, pl. 130, fig. 5, GBA1893/01/264, selected by Krystyn (1982: 34). Material: One specimen MPUM 10967 (PMAM17-1). Description. Slightly elliptical, extremely crushed internal mold of large-sized specimen with diameter of about 90 mm. About 130º of the body chamber are preserved. Despite the extreme crushing, the keel is clearly visible. Ribbing consists of slightly prorsiradiate, gently sinuous-falcoid ribs. Organization of ribs is visi- ble only on the last quarter of the preserved body cham- ber. Ribs are organized in bundles, each consisting of three primary ribs (Pl. 1, Fig. 2b). Usually one interca- latory/bifurcate rib appears a few mm from the umbi- lical margin. Additional branching at a little less than ¼ of whorl height, and very rarely (once in the last half whorl) intercalatory ribs appears at 1/3 of whorl height. Near the ventral shoulder, flat ribs are 3 to 4 times wider than the narrow inter-rib intervals. Suture lines are strongly serrated, but not well preserved. Remarks. This species was revised by Krystyn (1982), who discussed the synonymy and its relation- ship with Discotropites theron (Dittmar, 1866), the most similar species. In D. theron the primary ribs start from node-like periumbilical swellings (Mojsisovics 1893: 288; Krystyn 1982: 34), that are not developed in D. plinii. The difference between D. plinii and D. theron is even greater, if we follow the interpretation of D. theron by Tozer (1994), who extended its diagnosis to forms with several spiral rows of nodes. Occurrence. The distribution of Discotropites pli- nii is widespread in the Tethys realm, from the North- ern Alps to Japan, through Sicily, Turkey, Himalaya and Timor. Its stratigraphic position is so well constrained that this species has been selected by Krystyn (1980, 1982) as the index ammonoid for the first subzone of the uppermost Carnian Spinosus Zone (see also Krystyn et al. 2002). Genus Anatropites Mojsisovics, 1893 Type species: Tropites (Anatropites) spinosus Mojsisovics, 1893 Anatropites sp. ind. Pl. 1, fig. 3, 4a-b Material: Two specimens, MPUM 10968 (FNP112-1) and MPUM 10969 (PMAM22bis). Remarks. The two specimens attributed to Ana- tropites were collected from two different levels and most probably are not conspecific. Following the stratigraphic succession, the first specimen (MPUM 10968 [FNP112-1]: Pl. 1, Fig. 4a-b) is preserved in three dimensions for one quarter of a whorl. The original diameter is about 20 mm, and the whorl cross section is typically semielliptical with lat- eral sides converging towards the rounded venter and the prominent keel. Ornamentation is also typical of the genus, consisting of prorsiradiate concave primary ribs strongly elevated/subspiny at the periumbilical border and fading towards the shoulder. The second specimen, from level PMAM22bis (Pl. 1, Fig. 3), is preserved only as a whorl cross-section that is unextractable from the rock matix. Despite its very incomplete preservation, the specimen fits perfectly with Anatropites because of its peculiar whorl section with lateral sides converging to a rounded venter, its maximum width at the umbilical margin, its elevated keel without side furrows and its weak but distinct small projections at the umbilical margin, suggesting the umbilical spines typical of Anatropites. Both specimens are left in open nomenclature, the first because of its rather small size and the second be- cause details of its ornamentation are not visible. Occurrence. The genus Anatropites occurs in the Tethys realm and North America. In both areas it is restricted to the last zone of the Carnian stage, namely the Spinosus Zone in the Tethys (Krystyn 1973, 1980; Krystyn & Gallet 2002; Krystyn et al. 2002) and the Macrolobatus Zone of central Nevada (Silberling 1959) and British Columbia (Tozer 1994). Genus Microtropites Mojsisovics, 1893 Type species: Ammonites galeolus Hauer, 1860 Preliminary remarks. The genus Microtropites Mojsisovics, 1893 includes small-sized (dwarf) Tropiti- dae that exhibit a change in coiling during growth, a weak to very weak ornamentation and an ammonitic suture line (e.g., Mojsisovics 1893: 188; Arkell et al. 1957: L169). Species attributed to this genus show some differences in their whorl section, which varies from Carnian-Norian ammonoids from Pizzo Mondello 55 slightly compressed with a nearly semi-elliptical outline (e.g., the type M. galeolus [Hauer, 1860], M. lepsiusi Mojsisovics, 1893 and M. tubercularis Mojsisovics, 1893) to slightly depressed with a broadly rounded ven- ter (e.g., Microtropites sp. ind. in Krystyn 1982). Taking into consideration the rarity of specimens from this group and the lack of pertinent literature plus the fact that their distribution is restricted to the latest Carnian (Krystyn 1980, 1982), we for now consider these differ- ences in whorl section to be part of the variability of the genus. Microtropites cf. paronai (Gemmellaro, 1904) Pl. 1, fig. 5a-c Remarks on the type series. Gemmellaro de- scribed the new species Tropites paronai based on only three specimens (Gemmellaro 1904: 96), but in the col- lection stored at Museo Gemmellaro, two groups of specimens are labelled as ‘‘Tropites paronai’’. The first group (MGUP 002.96.1-4) consists of four specimens and includes the two figured types (MGUP 002.96.1= pl. 7, fig. 27-28; MGUP 002.96.3= pl. 7, fig. 25-26). The second group includes six specimens that are referred to a different catalogue number (MGUP 002.95.1-6) than the first group. We consider the types of the species to be only the specimens of the first group (MGUP 002.96.1-4). Material: One specimen MPUM 10970 (PMAM52A-1). Description. Specimen preserved with strongly recrystallized test, but internal mold is occasionally visi- ble because test was lost in a few places during prepara- tion. Body chamber consists of 170º of the last whorl. Coiling is involute, but from approximately 4-5 mm of H it becomes evolute due to umbilical egression. Whorl cross-section is depressed with wide, rounded venter giving specimen a near cadicone shape. Ventral keel without significant bordering furrows. Specimen appears to be nearly smooth except for strong forward-projected, concave, extremely weak and fading ribs that are visible under certain light conditions on last 90º of preserved body chamber. Suture line not visible. Dimensions (mm) Discussion. The genus Microtropites was recog- nized in Sicily by Gemmellaro (1904), who classified a few specimens from his collection as M. lepsiusi Mojsi- sovics, 1893. However, certain other taxa included by Gemmallaro in Tropites may well be better referred to Microtropites; these are Tropites paronai Gemmellaro, T. brancoi Gemmallaro, T. carapezzai Gemmellaro and Tropites n.f. indet. ex aff. T. brancoi. According to the original descriptions and plates, these taxa are very si- milar with only slight differences in the degree of whorl compression, type of ribbing and whether or not umbi- lical nodes and weak furrows bordering the keel are present. An examination of Gemmellaro’s type material reveals that he emphasized these differences in his de- scriptions and also that some details of the drawings were slightly exaggerated. A revision of the whole group is beyond the scope of this paper and would require much new material to test the population varia- bility of these very small, poorly known Tropitiidae. The Pizzo Mondello specimen is closer to Micro- tropites paronai (Gemmellaro, 1904) than to M. brancoi (Gemmellaro, 1904), which is characterized by ribs (visible on Gemmellaro’s plate 25, fig. 1-4) and by a slightly more compressed whorl section. Its similarity with M. paronai includes the depressed whorl section (Gemmellaro’s plate 7 fig. 27-28) and faded ribs. The specific attribution of the Pizzo Mondello specimen is challenged by certain differences from the syntype shown in pl. 7, fig. 25-26 (MGUP 002.95.3), which shows a narrowing of the whorl section that apparently is related to umbilical egression. Our specimen is slightly smaller than this particular syntype and it ex- hibits umbilical egression, but its venter does not be- come narrower. The same syntype has weak umbilical nodes (weaker than shown in Gemmellaro’s figure) that are neither visible on the other figured syntype (pl. 7, fig. 27-28; MGUP 002.96.1), nor on the Pizzo Mondello specimen. Our specimen does not have furrows along side the keel, but this feature is often visible on Gem- mellaro’s types. We prefer not to over-emphasize this difference since it may simply be related to different types of preservation. The test of our specimen is nearly complete, whereas Gemmellaro’s types are preserved as internal molds. Occurrence. The genus Microtropites is known only from the Tethys realm, where it is regarded as a marker for the Gonionotites italicus subzone, upper part of the Spinosus Zone, uppermost Carnian (Krystyn, 1980, 1982). The stratigraphic positions of the taxa de- scribed by Gemmellaro (1904) from Sicily are un- known, but the new Pizzo Mondello specimen from level PMAM52A is herein used to mark the lower boundary of the Gonionotites italicus subzone (Fig. 6). Family Thisbitidae Spath, 1951 Genus Metathisbites Tozer, 1994 Type species: Buchites hilaris var. dawsoni McLearn, 1940 Balini M., Krystyn L., Levera M. & Tripodo A.56 Carnian-Norian ammonoids from Pizzo Mondello 57 Fig. 6 - Distribution of the Upper Carnian-Lower Norian ammonoids in the studied interval of Pizzo Mondello section. The position of all the ammonoid samples is shown, but the occurrence of small sized specimens not classified in this work is differentiated with a short dash. For the sake of completeness the position of the conodont samples of Muttoni et al. (2001 and 2004) and of the halobiids described by Levera (2012) is also shown. Metathisbites cf. affinis (Gemmellaro, 1904) Pl. 1, fig. 6a-b Material: One specimen MPUM 10971 (FNP145-1). Description. Rather small specimen (diameter about 18.5 mm) that consists of an internal mold of a body chamber and preserved only on one side with a small part of the venter exposed. Rate of coiling very low with H~U. Flank slightly convex suggesting a compressed whorl section with well developed shoulder. No keel visible on exposed part of venter. Ornamentation consists of gentle, wavy-like, pror- siradiate, slightly sinuous primary ribs. Only one bi- furcate rib occurs in about one half whorl. All ribs end on ventral shoulder with small but distinct rounded node (see Pl. 1, Fig. 6b). Suture line not visible. Discussion. The specimen is very close to This- bites Mojsisovics, 1893 and Metathisbites Tozer, 1994. Metathisbites is characterized (Tozer 1994: 232) by an ovoid whorl section, a weak keel that sometimes is lack- ing, mostly simple ribs and nodes that are weaker than in Thisbites. The available specimen does not show an ovoid section, but its cross-section seems to be more subrectangular/subquadrate. Apart from this feature, the other characters suggest attribution to Metathisbites. Ribbing is rather simple and most of the ribs are pri- mary. The ventrolateral nodes are very weak and for what is visible on the small part of the ventral side, there is no prominent keel. Thisbites includes species with more dense rib- bing, a much higher frequency of secondary ribs and usually a distinct and strong keel. As regard the species, the specimen is referred by cf. to Ceratites (Buchites) affinis Gemmellaro on the basis of ribbing and nodes. This species is characterized by weak ventrolateral nodes and a very weak keel, both features not consistent with Buchites Mojsisovics, 1893. The attribution by cf. is due to the incomplete preserva- tion of the ventral side of the specimen from Pizzo Mondello. Occurrence. According to Tozer (1994) Metathis- bites is documented in both the Tethys realm and North America. Its range is calibrated only in North America where it is restricted to the Lower Norian Kerri Zone, more precisely to the Stikinoceras kerri subzone II. The specimen from Pizzo Mondello, in open nomenclature, has been found together with Dimorphites selectus, in- dex of the 2nd subzone of the Lower Norian Jandianus Zone. This finding is consistent with the stratigraphic position of the genus in North America. Family Juvavitidae Tozer, 1971 Subfamily Juvavitinae Tozer, 1971 Genus Hyattites Mojsisovics, 1902 Type species: Pinacoceras praefloridum Mojsisovics, 1873 Preliminary remarks. Hyattites Mojsisovics, 1902, one of the poorest known ammonoid genera from the Upper Triassic of the Tethys, was established by Mojsisovics (1902) to accommodate three species with quite different stratigraphic positions that were pre- viously referred to Beyrichites Waagen, 1895 by Philippi (1901:110). Pinacoceras praefloridum Mojsisovics, 1873, Meekoceras maturum Mojsisovics, 1882 and Meeko- ceras emmerichi Mojsisovics, 1882 are of relatively med- ium size and they exhibit involute coiling and a lack of ornamentation, but Mojsisovics (1902: 306) emphasized the suture line of Hyattites with its phylloid habitus and broad median hump in the external lobe (litt. ‘‘Median- höckers im Externlobus’’) that was said to suggest a family connection with Sturia Mojsisovics, 1882. In his description of the genus, Mojsisovics selected Pina- coceras praefloridum Mojsisovics, 1873 (of Carnian age) to be representative of the development of the suture line of Hyattites, and this is probably the reason this taxon has long been considered to be the type species of the genus (Diener 1915: 154; Spath 1951: 154; Arkell et al. 1957: L182). Krystyn 1982 (p. 43) closely examined the type specimen of the species and recognized that the suture line drawing in Mojsisovics 1893 was incorrect due to excessive grinding of the test. In reality the ex- ternal suture is actually juvavitid and Hyattites is clo- sely related to Gonionotites from which it differs by the early fading of its sculpture. Spath (1951) pointed out the relatively large age differences of the three species grouped together by Mojsisovics and therefore, reduced the composition of Hyattites. He confirmed the attribution of Anisian aged M. maturum to Beyrichites, as already suggested by Philippi (1901), and he selected Ladinian aged M. em- merichi as type species for the new genus Parasturia. Thus, Spath left only the type species in Hyattites, and until now it has remained the composition of the genus, because the only two taxa referred to this genus, Hyattites salomoni Gemmellaro, 1904 and Hyattites (?) nepalensis Jeannet, 1959 apparently are not conspecific with H. praefloridum. Gemmellaro described the new species Hyattites salomoni on the basis of two specimens from ‘‘feudo Modanesi,’’ western Sicily. However, his figured suture line (1904: pl. 27, fig. 29) contains simpler indentations than H. praefloridus. Hyattites (?) nepalensis Jeannet, 1959 from the Carnian of Nepal is referred with ques- tion to Hyattites, but apparently it is not conspecific with H. praefloridus because of its ribbed ornamenta- Balini M., Krystyn L., Levera M. & Tripodo A.58 tion. Gonionotites rarus McLearn, 1940, as figured in Tozer (1994, pl. 119), lacks ornamentation and could well be included in the genus Hyattites. Occurrence and age. Neither the occurrence nor the age of Hyattites is well defined in literature. Arkell et al. (1957), probably following Spath’s lead (1951), reported Hyattites from the Carnian of Sicily and the Northern Alps, whereas Tozer (1981a and b) provided an Early Norian age and a much wider paleogeographic distribution, from the Tethys to the East Pacific. Evi- dence in support of Tozer’s conclusions is not clear because he does not cite the genus from North America, although it may very well occur there (e.g., Gonionotites rarus). The Tethys occurrence may be supported by the distribution of Hyattites praefloridus (Mojsisovics) and H. salomoni (Gemmellaro), but there have been no re- ports of Hyattites from North America, neither before Tozer 1981a nor after (e.g., Tozer 1994). H. praefloridus is known from ‘‘Schichten mit Lobites ellipticus’’ of Röthelstein (Mojsisovics 1873: 58), a fossil site contain- ing a condensed fauna ranging in age from Carnian to Early Norian, according to Krystyn (1980). Hyattites cf. praefloridus (Mojsisovics, 1873) Pl. 1, fig. 7a-b; Fig. 7 Material: One specimen, MPUM 10972 (FNP333). Description. Specimen is preserved as an internal mold, but retains small areas of recrystallized test. Last 240º of whorl belong to the body chamber. Involute conch with very narrow umbilicus and compressed whorl section, with nearly flat flanks and rounded ven- ter. Surface of specimen is smooth on both the body chamber and portion of the last whorl that is phragmo- cone. Suture lines are strongly serrated, specimen ap- pears to be an adult. Suture is ammonitic with a gonio- notitic pattern of indentitions (Fig. 7). External lobe has a wide internal saddle. Discussion. One peculiar feature of the Pizzo Mondello specimen is the lack of ornamentation on the inner part of the last whorl at relatively small values of H. At this size, nearly all Juvavitidae have ribs and/or constrictions. The attribution of the specimen to Hyattites re- lies mainly on these features and on the gonionotitic- like suture line that is consistent with the general pat- tern of the type specimen’s suture line, re-described by Krystyn (1982: 42). However, the suture line of the type specimen of H. praefloridus is more indented, but this magnitude of difference is not fully justified by the slightly larger size of the type specimen (D about 50 mm) with respect to specimen MPUM 10972 (D about 39 mm). Because of this difference the speci- men from Pizzo Mondello is attributed to this species, with cf. Hyattites salomoni Gemmellaro from ‘‘feudo Modanesi’’ differs from Hyattites cf. praefloridus by its suture line with seven saddles on the lateral sides, very simple indentitions, and ribs developed on the ex- ternal part of the lateral side. Occurrence. Hyattites cf. praefloridus is the old- est ammonoid collected to date from the Scillato For- mation at Pizzo Mondello. It was collected from the Upper Carnian part of the section, about 9 m below the single occurrence of Discotropites plinii. Genus Projuvavites Tozer, 1971 Type species: Juvavites (Anatomites) brockensis Smith, 1927 Projuvavites boehmi (Gemmellaro, 1904) Pl. 1, fig. 8a-b; Fig. 8 v 1904 Juvavites (Anatomites) böhmi Gemmellaro, p. 207, pl. 27, fig. 9. partim Carnian-Norian ammonoids from Pizzo Mondello 59 Fig. 7 - Suture line of Hyattites cf. praefloridus, specimen MPUM 10972 (FNP333). Bar scale 5 mm. ?v 1904 Juvavites (Anatomites) böhmi Gemmellaro, p. 207, pl. 27, fig. 10. Stratum typicum and locus typicus: Light gray limestone with cherty nodules, ‘‘feudo Modanesi’’ near Castronuovo (Gemmellaro 1904:208). Type series: Gemmellaro based his description of the species on two specimens, both of which are figured. Their repository is the Mu- seo Gemmellaro under registration number MGUP 002.183.1 and.2. Specimen MGUP 002.183.1 (Gemmellaro 1904: pl. 27, fig. 9) is here designated as the lectotype. Material: One specimen MPUM 10973 (PMAM27-1). Description. Specimen consists of slightly more than half whorl, representing last part of phragmocone and beginning of body chamber (about 100º). Test on phragmocone lost during extraction. Juvavitid with involute coiling and slightly com- pressed whorl section. Whorl section of inner whorls is semioval, but then apparently becomes almost subtrian- gular on body chamber. However, since body chamber is slightly crushed, this feature may be partly secondary. Two concave, projected constrictions are visible, one on phragmocone and the second located just after last visi- ble suture line, at about 80º from first. Ornamentation consists of slightly prorsiradiate, concave ribs with Projuvavites-like organization on the phragmocone (see Krystyn 1982). At the shoulder, about 13 ribs are visible between the two constrictions. Ribbing on body chamber is much weaker, consisting of widely-spaced primary ribs and intercalatory ribs visi- ble only at the shoulder. Three intercalatory ribs are usually present between two primary ribs. Suture line ammonitic (Fig. 8) with Projuvavites- like pattern of intentations. Discussion. Relatively few species of the large group attributed by Gemmellaro to the subgenus Juva- vites (Anatomites) have a large size and relatively thick whorl section. Within this small group, the species most similar to the Pizzo Mondello specimen is J. (A.) boeh- mi Gemmellaro, which exhibits a fading of the ribs on the body chamber, especially on the inner part of the lateral side. This feature is well visible on Gemmellaro’s syntype figured in pl. 27, fig. 9 (MGUP 002-182.1), which is designated as lectotype. The second specimen, now a paralectotype (pl. 27, fig. 10, MGUP 002-183.2), is a juvenile that does not show the typical features of J.(A.) boehmi. An examination of the lectotype of J.(A.) boehmi reveals that Gemmellaro’s figure of the whorl section is not correct. The specimen is more compressed than shown in the illustration in pl. 27, fig. 9, and in this feature the lectotype is more similar to the new speci- men from Pizzo Mondello. The only difference between MPUM 10973 and the lectotype is the width of the venter, which seems to be wider on the lectotype of P. boehmi. Information regarding population variability of P. boehmi is not available, but it is well known from tens of papers on Triassic ammonoids that population variability is rather wide for several groups, and thus, the shape and width of the venter may also be affected. Given that the dif- ference in the width of the venter is rather small, and that the relatively narrow venter of MPUM 10973 may be due to a slight crushing of the body chamber, we have decided to include the new specimen in P. boehmi (Gemmellaro). Occurrence. No literature is available for Proju- vavites boehmi (Gemmellaro). This species is appar- ently restricted to Sicily, where its stratigraphic position is unknown. The new specimen from Pizzo Mondello comes from level PMAM27, just slightly above PMAM17, which yielded Discotropites plinii. P. boehmi could probably be referred to this subzone. Projuvavites inflatus (Gemmellaro, 1904) Pl. 1, fig. 9a-d v 1904 Juvavites (Anatomites) inflatus Gemmellaro, p. 211, pl. 5, fig. 19-20. ?v 1904 Juvavites (Anatomites) gelonis Gemmellaro, p. 213, pl. 17, fig. 3-4, pl. 21, fig. 10. Stratum typicum: Light gray limestone with chert nodules from ‘‘feudo Modanesi’’ near Castronuovo (Palermo) (Gemmellaro 1904:212). Type series: The description of this species is based on two specimens, both registered in the Museo Gemmellaro under number MGUP 002.185.1-2. The only figured specimen (MGUP 002.185.1) is here designated as the lectotype. Material: One specimen MPUM 10974 (PMAM49-1). Description. The specimen consists of an internal mold of phragmocone and at least 270º of body cham- ber. Juvavitid with very involute coiling (U= 9% of D) and slightly depressed whorl section (H/W from 0.86 to 0.94) with semielliptical outline that becomes subtrian- gular on last whorl. Rounded venter is crossed by con- strictions, but not by ribs, at least on phragmocone. Balini M., Krystyn L., Levera M. & Tripodo A.60 Fig. 8 - Suture line of Projuvavites boehmi (Gemmellaro, 1904), specimen MPUM 10973 (PMAM 27-1). Bar scale 5 mm. Constrictions spaced about 80º-90º apart. Ribs nearly straight, but bend forward at ventrolateral shoulder and then usually fade without crossing venter. Organization of ribs between constrictions follows the typical pattern of Projuvavites without trifurcation of ribs and about four primary ribs between constrictions. Ribbing also developed on beginning of body chamber. Suture line ammonitic, not well enough preserved for drawing. Dimensions Discussion. The Pizzo Mondello specimen is at- tributed to Juvavites (Anatomites) inflatus Gemmellaro, 1904 in part because of its involute coiling and slightly depressed whorl section, but especially for the change in its whorl section, which becomes nearly subtriangular on the outer whorl and also for the development of ribs on the body chamber. The constrictions are not well- represented on Gemmellaro’s drawings, but they are clearly mentioned in the text (p. 211) and also quite visible on the lectotype. Juvavites (Anatomites) gelonis Gemmellaro, 1904 is cogeneric with Projuvavites inflatus, and probably could be synonymized with this species. The size of the largest types (Gemmellaro 1904, pl. 17, fig. 3-4) is nearly equivalent to the inner whorl of the type speci- men of P. inflatus, and their coiling and whorl sections are also very similar. Ribbing is slightly different, but this may not be of great significance at the species level. Gemmellaro’s drawing (1904, pl. 17, fig 5) of P. gelonis appears to show a few trifurcations, but this feature is not very obvious on the original. Among the large group of ‘‘Anatomites’’ de- scribed by Gemmellaro, Projuvavites inflatus is also si- milar to J. (A.) archimedis Gemmellaro, 1904, J. (A.) mariani Gemmellaro, 1904 and J. (A.) boehmi Gemmel- laro, 1904, but all three species can be attributed to Projuvavites Tozer, 1971. Juvavites (A.) archimedis (Gemmellaro 1904: pl. 9, fig. 1-2) differs by the reduc- tion of ribbing on its body chamber and its nearly semi- elliptical whorl section. Juvavites (A.) mariani has a totally different body chamber (Gemmellaro 1904: pl. 16, fig. 1-2). Its venter becomes wider (this feature is more developed on the syntype than shown on the plate), and its ribs are much reduced and wavy-like, but they persist in strength and cross the venter. Juva- vites (A.) boehmi (Gemmellaro 1904: pl. 27, fig. 9-10) also exhibits a reduction of ribbing on the body cham- ber, especially on the inner part of the lateral side. Occurrence. No information is available regard- ing the age and stratigraphic position of Juvavites (Ana- tomites) inflatus as described by Gemmellaro from wes- tern Sicily. In this respect, the discovery of the single specimen from Pizzo Mondello provides at least a par- tial solution to its age. The new specimen was found in a level just slightly above the base of the Gonionotites italicus subzone (Spinosus Zone, Tuvalian 3, Upper Car- nian) that is marked by the occurrence of Microtropites in level PMAM52A. Genus Gonionotites Gemmellaro, 1904 Type species: Gonionotites italicus Gemmellaro, 1904 Preliminary remarks. Gonionotites Gemmellaro, 1904 has been recognized in several Tethyan localities and North America, but despite a relative abundance of literature, the taxonomy of this genus at the species level is still complex. Gemmellaro described eleven new spe- cies of Gonionotites and two indeterminate taxa from the ‘‘cherty limestone’’ of Sicily. Since then, the genus has been recognized in the Tethys Himalaya (Diener 1906 and 1908; Wang & He 1976; Krystyn 1982), Northern Alps (Diener 1921; Krystyn 1973 and 1980), Iran (Besse et al. 1998) and Turkey (Krystyn & Gallet 2002), but it is worth noting that most of the species identified from these areas are different than those from Sicily. The first report of Gonionotites from North America was by Smith (1927). Afterwards a number of species, most of which are different from the Tethyan faunas, were described from Canada by McLearn (1940, 1947 and 1960) and Tozer (1962). Then, in 1994 Tozer provided a comprehensive revision of the Canadian Go- nionotites species. No recent literature is available from the United States apart from the illustration of two spe- cimens by Kristan-Tollmann & Tollmann (1983). Tethyan Gonionotites are not as well known as the North American faunas. Krystyn (1982) described G. haugi Gemmellaro, 1904, G. gemmellaroi Diener, 1906, and G. noricus Diener, 1921 from Nepal. He also revised G. tingriensis Wang & He, 1976 and transferred this species to Malayites Welter, 1914, based on its spiral strigations (Krystyn 1982). However, no updates are available for most of the eleven species erected by Gem- mellaro, including the index species G. italicus. An examination of Gemmellaro’s species and their comparison with other species from the Tethys and North America suggests the following brief com- ments. a) As already mentioned for other ammonoid groups of Gemmellaro’s collection, several of his species appear to be morphologically very close. Surprisingly, a syntype of a given species is often more similar to a syntype of another species than to the other members of the same type-series. This is the case for Gonionotites Carnian-Norian ammonoids from Pizzo Mondello 61 mojsisovicsi in Gemmellaro’s pl. 21, fig. 1-3, which is more similar to the compressed inner whorls of the syntype of G. italicus in pl. 21 (fig. 4-6) than to the syntype of G. mojsisovicsi figured in pl. 13, fig. 1-2. b) Many of Gemmellaro’s species exhibit com- pressed to very compressed inner whorls with a sub- triangular whorl section followed by a widening venter and a thickening of the whorl width on the body cham- ber. This modification of the whorl section on the ma- ture body chamber is much less common in other Teth- yan and North American species. c) Few Sicilian species of Gonionotites exhibits a thickening of the ribs on the widest part of the flank before the shoulder, which resembles radially elongated and forward concave nodes. These bulges are shown in G. recuperoi Gemmellaro (pl. 7, fig. 43-44), G. diblasii Gemmellaro (pl. 5, fig. 1-2) and possibly G. dubius Gemmellaro (pl. 6, fig. 9-10), but they also occur in a few very compressed species that Gemmellaro attribu- ted to the subgenus Anatomites, such as Juvavites (Ana- tomites) pulcher Gemmellaro (pl. 5, fig. 3-4) and J. (A.) formosus Gemmellaro (pl. 20, fig. 6-7). A clarification of these problems would require a population analysis of many bed-by-bed collected spe- cimens, but thus far the scarcity of specimens from Piz- zo Mondello does not allow such a revision. Pending a thorough revision of the group, we can only compare our new specimens with Gemmellaro’s taxonomy. Gonionotites cf. italicus Gemmellaro, 1904 Pl. 2, fig. 1a-c v 2007 Gonionotites maurolicoi - Nicora et al., pl. 2, fig. 6a-b. Remark on the Type series: Gemmellaro (1904: 159) clearly stated that the new species was based on five well preserved specimens plus several fragments. Seven specimens are housed in the Museo Gem- mellaro collections, under registration number MGUP 002. 147.1-4 and MGUP 002.148.1-3. Material: Two specimens, MPUM 10975 (PMAM7-1) and MPUM 10976 (PMAM36-1). Description. The two specimens attributed to Gonionotites cf. italicus are of rather large size. One is slightly less than half one whorl (about 170º) of body chamber (estimated diameter of about 100 mm) with inner whorls visible in cross section, while the second is an incomplete fragment of less than 45º of body chamber. Both specimens have a compressed, slender subtriangular whorl section with very narrowly rounded venter and a smooth surface. The most com- plete specimen (Pl. 2, Fig. 1) exhibits a gradual thicken- ing of the whorl section that is not accompanied by a widening of the venter. At the end of the preserved part of the body chamber (Pl. 2, Fig. 1b-c), the venter is still relatively narrow, and the maximum width of the whorl section is located just slightly above one- half of the whorl height. Dimensions Discussion. As emphasized in the Preliminary re- marks, the difference between some of Gemmellaro’s species is rather obscure. We do not doubt that G. ita- licus, the first species described by Gemmellaro, is a valid species, and accordingly, we place slightly more emphasis on this taxon than to the other species. Specimen MPUM 10976 is too incomplete for a fully accurate identification, while the attribution of the figured specimen (MPUM 10975; Pl. 2, Fig. 1) requires additional discussion. Comparison of this specimen with the Gonionotites of Gemmellaro’s collection leads us to conclude that only part of the body chamber of the new specimen is preserved, with about 70-90º miss- ing. A second observation resulting from the examina- tion of Gonionotites of Gemmellaro’s collection is that the thicknening of the whorl and widening of the venter usually take place on the last quarter of the whorl of the mature body chamber. Apparently, this particular part of the whorl is not preserved in specimen MPUM 10975. This specimen definitely exhibits a thickening of the whorl, but apparently its growth was not yet sufficient for the venter to become wider. Instead its venter is still rather narrow at the end of the preserved part of the body chamber (Pl. 2, Fig. 1c). In this aspect, Balini M., Krystyn L., Levera M. & Tripodo A.62 PLATE 1 Upper Carnian and Lower Norian ammonoids from Pizzo Mondello. 1) Placites sp. ind., specimen MPUM 10966 (NA49.1-1). 2) Discotro- pites plinii (Mojsisovics, 1893), specimen MPUM 10967 (PMAM17- 1): a, lateral view, b enlargement showing branching of the ribs at the umbilical margin. 3) Anatropites sp. ind., specimen MPUM 10969 (PMAM22bis). 4) Anatropites sp. ind., specimen MPUM 10968 (FNP112-1): a, lateral view, b) ventral view. 5) Microtropites cf. pa- ronai, specimen MPUM 10970 (PMAM52A-1): a, lateravl view; b, ventral view; c, apertural view. 6) Metathisbites cf. affinis, specimen MPUM 10971 (FNP145-1), a, lateral view; b, detail of the weak ven- trolateral nodes. 7) Hyattites cf. praefloridus, specimen MPUM 10972 (FNP333), a) lateral view; b, view of the cross section. 8) Projuvavites boehmi (Gemmellaro), specimen MPUM 10973 (PMAM22-1), a, lat- eral view; b, ventral view. 9) Projuvavites inflatus (Gemmellaro), spe- cimen MPUM 10974 (PMAM49-1), a, lateral view; b, lateral view after removal of the last part of body chamber; c, apertural view; d, ventral view; dots mark the constrictions. All specimens whitened with ammonium chloride except Fig. 3. Bar scale is 1 cm, that in lower right corner is for all the figures except for 2b and 6b. Asterisk marks the last septum. Carnian-Norian ammonoids from Pizzo Mondello 63 the specimen seems to differ from G. italicus, but on the other hand, none of Gemmellaro’s other type specimens appear to be close to specimen MPUM 10975. The type specimen of G. discus (see 1904: pl. 13, fig. 3-6) has a body chamber that exhibits a flattening of the venter, a trend that is opposite with respect to the venter of MPUM 10975. The type specimen of G. maurolicoi also has a narrow venter, but it is characterized by much thicker whorls, whose maximum width is very close to the umbilical margin (e.g., 1904: pl. 14, fig. 5); there- fore, the previous attribution of specimen MPUM 10975 to this species (Nicora et al. 2007) is here emended. One of the syntypes of G. mojsisovicsi shows some similarity with the new specimen, with respect for its narrow venter, but unfortunately this feature is ac- companied by a maximum whorl width very close to the umbilical margin, instead of at about 50 % of the whorl height. This syntype (MGUP 002.153.2) was not figured by Gemmellaro, and thus it cannot be consid- ered to be especially representative of G. mojsisovicsi. According to Gemmellaro (1904), the characteristic syntypes of this species include the large, much thicker specimen figured in pl. 13, fig. 1-2 with a more rounded venter than the present specimen, and the syntype in pl. 21, fig. 1-3, with a broad venter and maximum whorl width located at about ½ of whorl height. Occurrence. Both specimens were collected from levels PMAM36 and PMAM7. The first level is located about 3 m below the occurrence of Microtropites cf. paronai, which presently marks the lower boundary of the Gonionotites italicus subzone. The second speci- men was collected from the middle part of the G. itali- cus subzone. Gonionoites aff. recuperoi Gemmellaro, 1904 Pl. 2, fig. 2a-b; Fig. 9 Material: One specimen MPUM 10977 (PMAM43-1). Description. Specimen, which is preserved as an internal mold partly covered by recystallized test, con- sists of a phragmocone with about 270º of body cham- ber. Whorl section is compressed and slender for first 160º of body chamber, but then venter rapidly widens and maximum width of whorl section moves from the umbilical margin to 1/3 of whorl height. A weak con- striction is visible at beginning of the body chamber. Ribbing follows pattern typical of Gonionotites. On visible part of the phragmocone, ribbing consists of extremely weak prorsiradiate, primary ribs on the flank, and three to four secondary ribs are visible very close to the shoulder. On body chamber, ribs are barely visible and noticeable only on the outer half of the whorl. These ribs are widely spaced (about 4-5 ribs in 90º) and develop node-like elongated thickenings very close to the shoulder, which tend to follow the course of the ribs, first radially, but then bending forward and fading on the venter. Suture line is ammonitic (Fig. 9), with well-devel- oped Gonionotites-like indentations. Three sutures are visible and show a serration. Dimensions Discussion. The specimen, attributed to Gonio- notites, agrees well with Gemmellaro’s interpretation of the genus. An analysis of the taxonomic significance of the thicknening of the ribs on the outer part of the flank may be important, but would require a much lar- ger collection of specimens. At the species level, the specimen from level PMAM43 is referred by aff. to G. recuperoi Gemmel- laro, 1904 because this particular species exhibits the Balini M., Krystyn L., Levera M. & Tripodo A.64 Fig. 9 - Suture line of Gonionotites aff. recuperoi, specimen MPUM 10977 (PMAM 43- 1). Bar scale 5 mm. thickening whorl section and widening of the venter at a size that is comparable to the size of the Pizzo Mon- dello specimen. The new specimen from Pizzo Mondel- lo, however, shows the thickening of ribs on the outer part of the flank at a larger size with respect to the only figured syntype of G. recuperoi, after the weak ventral ribs have disappeared. G. diblasii Gemmellaro, 1904 reveals a ventral thickening of the whorl section that occurs at much larger size, while the ‘‘nodes’’ of G. dubius Gemmellaro, 1904 are only barely visible on the figured syntype. Occurrence. Gonionotites recuperoi Gemmellaro has not been found since Gemmellaro’s (1904) time and it is unknown outside of western Sicily, where its age might span from Late Carnian to Early Norian. The herein described specimen was collected from a level slightly above the younger of the two Anatropites sp. ind. collected thus far from the Pizzo Mondello section. The co-occurrence of Halobia radiata (cf. Levera 2012) suggests a Late Carnian age. Pregriesbachites gen. n. Type species: Juvavites (Anatomites) Bukowskii Gemmellaro, 1904 Etymology: from the suffix ‘‘pre’’ and Griesbachites. The com- pound name emphasizes the evolutionary link with the genus Griesba- chites Mojsisovics, 1896. Diagnosis: Small to middle-sized, relatively slim juvavitids with highly differing sculpture from juvenile to adult stage. Phragmocone bears prorsiradiate, paulostome constrictions and multi-branching, ex- ternally alternating or interrupted ribs. Body chamber is characterized by fading ribs and development of numerous pointed ventrolateral nodes. Suture line projuvavitid with low and medium indented saddles similar to Griesbachites. Composition of the genus: Juvavites (Anatomites) bukowskii Gemellaro, 1904 (Type), Juvavites timaei Gemmellaro, 1904, Griesba- chites auctoris Tozer, 1994, G. pinensis Tozer, 1994, G. laevis Tozer, 1994, G. humi (McLearn, 1937) and G. selwyni (McLearn, 1940). Remarks. The new genus Pregriesbachites forma- lizes a taxonomic entity that was outlined as ‘‘nov. gen. (= Projuvavites mit Wohnkammerknoten)’’ (=Projuva- vites with nodes on body chamber) by Krystyn (1982: 46, 59-60). The previous interpretation of this taxon as a descendent of Projuvavites and forerunner of Griesba- chites is here confirmed. Comparisons. Pregriesbachites has inner whorls similar to Projuvavites Tozer, 1971, but is distinguished from that genus by the presence of ventrolateral nodes on its body chamber. The shape and size of the nodes permits separation from the slightly younger but timely overlapping genus Griesbachites Mojsisovics, 1896. These nodes are rounded and pointed in Pregriesba- chites n. gen., whereas in Griesbachites, they are larger and clavate. Guembelites Mojsisovics, 1896 lacks con- strictions and bears nodes in a more external position on the phragmocone as well as on the body chamber. The inner whorls of Pregriesbachites may show similiarity with those of Anatomites. However, the type species, A. rotundus Mojsisovics, 1893, brings to mind the mor- phology of the inner whorls of Griesbachites and there- by, is suspected of representing the phragmocone stage of the latter genus (Krystyn 1982: 46). Occurrence. The new genus is documented in the Tethys realm and North America. In Canada the species herein included in Pregriesbachites n. gen. document a latest Carnian, late Tuvalian 3 Macrolobatus Zone to Early Norian Kerri Zone range. An equivalent strati- graphic distribution (G. italicus Subzone of late Tuva- lian 3 to Jandianus Zone of Lacian 1 is known for the Tethys (Krystyn 1982: 58). At Feuerkogel Pregriesba- chites n. gen. was collected from level IV of F4 section (Fig. 10). The Pizzo Mondello occurrence (see descrip- tion of species) most likely is from the Gonionotites italicus subzone, Spinosus Zone. Pregriesbachites bukowskii (Gemmellaro, 1904) Pl. 2, fig. 3a-b, 4a-b v 1904 Juvavites (Anatomites) bukowskii Gemmellaro, p. 224, pl. 11, fig. 7-8. ?v 1904 Juvavites (Anatomites) bukowskii Gemmellaro, p. 224, partim. Stratum typicum and locus typicus: Whitish limestone with cherty nodules, ‘‘feudo Modanesi’’ near Castronuovo (Gemmellaro 1904: 225). Type series: Gemmellaro (1904: 225) cited seven specimens, but eight specimens are deposited in the Museo Geologico Gemmellaro, under registration number MGUP 002.193.1-8. Gemmellaro figured only one of the type specimens (pl. 11, fig. 7-8). This specimen, which is much better preserved than the other four large sized types, is here designated as lectotype. Material: One specimen MPUM 10986 (PMAM42-1). Description. Specimen is preserved as an internal mold that retains small patches of recrystallized test. Body chamber appears to occupy about 260º of whorl from last visible suture line. Very involute coiling platicone (U/D~0.06). Whorl section, with maximum width very close to um- bilical margin, exhibits a gradual change in the degree of compression combined with a very slight modification in the outline. Whorl section at end of phragmocone is semielliptical, with convex lateral sides and H/W ratio = 1.50. Just slightly past beginning of body chamber, the H/W ratio increases to 1.59, flanks become more flatter and shoulders become much more distinct. Towards the end of the body chamber, whorl section becomes more inflated and H/W decreases to 1.48. This variation is even more evident when viewing the specimen because the appearance of two more distinctive shoulders on the body chamber makes the venter appear to be even wider. Carnian-Norian ammonoids from Pizzo Mondello 65 Two constrictions are visible, one about 35º be- fore the end of the phragmocone and the other on the body chamber about 100º after the first. Ornamentation consists of slightly concave primary and secondary ribs with a general Projuvavites-like organization between the constrictions. Ribs are developed between the um- bilical margin and the shoulder on the first part of the last whorl before the first constriction. First branching of ribs occurs very close to the umbilical margin, while the second subdivision is located near the middle of the flank. Between the two constrictions, there are four widely-spaced weak primary ribs, each followed by four to five secondary ribs that are developed only ven- trolaterally. Ventral ribs also continue on the body chamber and all ribs cross the venter. Ventrolateral rounded nodes, which appear on the body chamber at whorl height of about 28 mm are located on flank, very close to the ventral shoulder. Suture line ammonitic. Dimensions Discussion. The type series consists of eight spe- cimens (MGUP002.193.1-8) of different size. Four of them are very small, and their size does not exceed the innermost part of the last whorl of the four medium to large sized individuals (MGUP002.193.1-4). Since we have no evidence that the four small-sized specimens truly represent the juvenile growth stage of the larger individuals, these specimens are separated in the Syno- nymy. The single specimen figured by Gemmellaro, de- signated as lectotype, is much better preserved and fits quite well with the original figure. Compared to the new specimen from Pizzo Mondello, the lectotype is Balini M., Krystyn L., Levera M. & Tripodo A.66 Fig. 10 - Ammonoid and Halobia record at Feuerkogel sections F4 and F5 (determination by LK). Preliminary data for these sections were previously reported by Krystyn (1973 and 1980). PLATE 2 Upper Carnian ammonoids from Pizzo Mondello. 1) Gonionotites cf. italicus, specimen MPUM 10975 (PMAM7-1), a, lateral view; b, ven- tral view; c, apertural view. 2) Gonionotites aff. recuperoi, specimen MPUM 10977 (PMAM43-1), a, lateral view; b, ventral view. 3) Pre- griesbachites bukowskii (Gemmellaro), specimen MPUM 10986 (PMAM42-1), a lateral view; b, ventral view. 4) Pregriesbachites bu- kowskii (Gemmellaro), lectotype MGUP 002.193.1, a lateral view; b, ventral view. All specimens whitened with ammonium chloride ex- cept Fig. 4. Bar scale is 1 cm for all specimens. Asterisk marks the last septum. Carnian-Norian ammonoids from Pizzo Mondello 67 slightly more compressed, but exhibits the same varia- tion in the whorl section, especially on the body cham- ber, with nearly flat flanks meeting the shoulder on each side of the rounded venter. The ribbing pattern is also the same, but the nodes are already obvious at the be- ginning of the body chamber. Occurrence. This is the first report of this species since Gemmellaro’s 100 plus year old description. Therefore, the stratigraphic position of Pregriesbachites bukowskii (Gemmellaro) must rely on the present spe- cimen from Pizzo Mondello. This specimen is from level PMAM42, which also yields Halobia radiata and rare H. lenticularis (Levera 2012). Since it was found slightly below the second level with Anatropites (PMAM22bis), P. bukowskii is thus referred to the Upper Carnian Gonionotites italicus subzone, Spinosus Zone. Genus Dimorphites Mojsisovics, 1893 Type species: Juvavites (Dimorphites) selectus Mojsisovics, 1893 Dimorphites noricus n. sp. Pl. 3, fig. 1-5 v 1980 Dimorphites n. sp. 1 Krystyn, p. 73. v 2002 Dimorphites n. sp. 1 Krystyn et al., p. 344, fig. 1. Derivatio nominis: From noricus, -a, -um. The name empha- sizes the stratigraphic position of the species as a marker for the basal part of the Norian Stage. Stratum typicum and locus typicus: Hallstatt Limestone, Feuerkogel (Northern Alps, Austria), section F5, bed III (Krystyn 1980, fig. 12; Fig. 10). Material: Type series composed of four specimens. Holotype GBA 2011/055/0001; paratypes GBA 2011/055/0002-0004. One addi- tional specimen from Pizzo Mondello is attributed to the new species MPUM 10978 (NA42.1). Diagnosis: Relatively compressed Dimorphites with subdiscoi- dal inner whorls and semi-circular venter on the mature body chamber. Ornamentation consists of wide, flat ribs separated by narrow, furrow- like inter-spaces. Description. Since all available specimens are pre- served with the test, the description is based on features visible on outer surface of shell. Specimen from Pizzo Mondello compares well with paratype GBA 2011/055/ 0002 that is most similar. Coiling very involute (U/D decreases with growth from 7.85 to 5.4) with medium SGR. Whorl section compressed (H/W increases during the growth from 1.47 to 2.29) with maximum width very close to the umbilical margin. Flanks slightly convex, slowly converging to narrow venter. General shape of shell is subdiscoidal until first half of adult body chamber, at which point venter begins to widen. Ornamentation consists of rather wide, flat ribs separated by narrow, furrow-like inter-spaces. At all stages of growth, ribs begin slightly above umbilical margin, which is rounded and smooth. Innermost whorls differ from medium to large sized individuals by wavy-like ribbing. At whorl height less than 7-7.5 mm (specimens GBA 2011/055/0002 and 0003; MPUM 10978: Pl. 3, Fig. 1,2 and 5), ribs are slightly round rather than flat and about 1.5 times wider than the in- ter-rib spaces. At whorl height greater than 7.5 mm, ribsgradually become flat and wider than the inter-space furrows. Ribs are sinuous (falcoid sensu Arkell et al. 1957), with a rather peculiar course. Flat primary ribs begin just above the umbilical margin and gradually become wider. Bifurcation of primary ribs occurs at the beginning of a narrow furrow in the middle of rib, which is often very weak, but after a few millimeters gradually reaches depth and width of furrows delimitat- ing primary rib. In such case, it is more common for the subdivisions to occur at the middle of the flank, the branching point of the secondary rib can be located only with some approximation. Subdivision of ribs mainly occurs at two positions on the flank. The first is between the starting point of the primary rib and about 10% of whorl height. The second position is about 40 to 60% of whorl height, but may change from one rib to the next. Occasionally, additional branching may also occur on the external part of the flank, at about 70-75% of whorl height. All ribs are projected forward slightly at the ventral shoulder, but then fade higher on the shoulder in an alternating manner such that an undulating effect is imparted to the course of the relatively narrow subtabulate venter. This feature is ty- pical of the genus Dimorphites. For medium to large- sized specimens the frequency of ribs per half whorl is rather constant at about 33-35 ribs at the ventral shoulder. Suture line not exposed on the type specimens, except for one single ammonitic 1st lateral saddle visible on one side of paratype GBA 2011/055/0002. Dimensions Remarks. The description of Dimorphites noricus n. sp. formalizes a species previously mentioned in the literature (Krystyn 1980) as Dimorphites n. sp. 1, and designated as an index ammonoid for the first Norian ammonoid subzone (cf. Krystyn et al. 2002). Discussion. With respect to its coiling and pattern of rib subdivision, Dimorphites noricus n. sp. is mor- Balini M., Krystyn L., Levera M. & Tripodo A.68 phologically so close to the stratigraphically younger D. selectus Mojsisovics, 1893 that the two species may re- present an evolutionary lineage. Despite D. selectus being slightly more compressed than D. noricus, the main difference between the two species is their ribs, which at all growth stages are much wider and flatter in D. noricus n. sp. than in D. selectus. Accordingly, the frequency of ribs per half whorl is distinctly lower in D. noricus than in D. selectus. The rib frequency on the type specimens of D. noricus n. sp. compared to that of the ype specimens of D. selectus is as follows: a) Small-sized specimens: 24/25 ribs (GBA 2011/ 055/0002: Pl. 3, Fig. 1) versus 35 (Mojsisovics 1893, pl. 127, fig. 2a, D= 14mm), b) small medium-sized specimens: 32 ribs (GBA 2011/055/0003: Pl. 3, Fig. 2) versus 53 (Mojsisovics 1893, pl. 127, fig. 5a, D= 27mm), c) medium to large-sized specimens: 33-35 ribs (GBA 2011/055/0001 and 0004: Pl. 3, Fig. 3 and 4) ver- sus 41-54 (Mojsisovics 1893, pl. 127, fig. 3a [Lectotype]: 41 at D= 30mm; fig. 4a: 46 at D= 41mm, 54 at D= 50mm). Occurrence. The species has been recognized at Feuerkogel (Hallstatt, Northern Alps), section F5, level III, and at Pizzo Mondello (Sicani Mountains, western Sicily) level NA42. With regard to its chronostrati- graphic position at Feuerkogel, this species was selected as the index ammonoid for the first subzone of the Jandianus Zone (Lacian 1: Krystyn 1980, 1982), which is the first Norian ammonoid zone of the Tethyan chronostratigraphic scale. The occurrence at Pizzo Mondello is also of earliest Norian age. Dimorphites selectus Mojsisovics, 1893 Pl. 3, fig. 6-7 1893 Juvavites (Dimorphites) selectus Mojsisovics, p. 145, pl. 127, fig. 1-9. v 1904 Juvavites (Dimorphites) mariae Gemmellaro, p. 243, pl. 17, fig. 19-20. 1921 Dimorphites selectus – Diener, p. 487. 1925 Dimorphites selectus - Diener, p. 65, pl. 16, fig. 9. ? 1940 Juvavites (Dimorphites?) pardonetiensis McLearn, p. 48, pl. 1, fig. 13. ? 1960 Dimorphites pardonetiensis – McLearn, p. 92, pl. 16, fig. 1-2. v 1982 Dimorphites selectus – Krystyn, p. 45, pl. 11, fig. 6. ? 1994 Dimorphites pardonetiensis McLearn, Tozer, p. 240, pl. 114, fig. 1-3, text-fig. 91c. v 2007 Dimorphites sp. ind. – Nicora et al., pl. 2, fig. 7. Stratum typicum: Hällstatter Kalk, at Feuerkogel (Salzkam- mergut, Austria). Lectotype: Original of Mojsisovics 1893, pl. 127, fig. 3, GBA1893/01/131, designated by Diener 1925:65). Material: Ten specimens. Three are relatively complete: MPUM 10979 (FNP145-19), MPUM 10980 (FNP145-20) and MPUM 10981 (Det-1). Seven are fragmentary: MPUM 10982 (FNP144-2); MPUM 10983 (FNP144b-1); MPUM 10984 (FNP145-2, -7, -8, -14, -21). Description. The three best preserved specimens are of medium size (~30U), an elliptical whorl section and a suture line with triphyllic symmetrical saddles clearly different with respect to the asymmetrical D. patens- like saddles figured by Mojsisovics (1896: pl. 19, fig. 6). An additional difference in the suture line of Die- Carnian-Norian ammonoids from Pizzo Mondello 71 ner’s specimen is its very deep external lobe, which dif- fers notably from the external lobe of D. patens and D. insignis. However, this particular portion of the suture line is not preserved on the type specimen figured by Mojsisovics (1896); hence a comparison is impossible. We cannot exclude that it may be possibile to synonymize D. insignis Gemmellaro, 1904 with D. eb- neri Mojsisovics, 1896 but, pending a revision of the latter, we prefer to keep D. insignis Gemmellaro, 1904 separated. Occurrence. The species occurs in Sicily (Gem- mellaro 1904), but it has also been collected from the Tuvalian 3 at Feuerkogel in the Northern Alps (Krystyn 1973: 120; Fig. 10), in the Spinosus Zone. Both new specimens from Pizzo Mondello were collected from levels PMAM52 and FNP166. Level PMAM52 most likely belongs to the Gonionotites italicus subzone, Spi- nosus Zone, Tuvalian 3 Upper Carnian because of the occurrence of Microtropites in the immediately overly- ing level, while FNP166 is located within the range of Halobia mediterranea, a species usually referred to the Paulckei Zone (Lacian 2) (see Ammonoid bio-chronos- tratigraphy and Levera 2012). Ammonoid chronostratigraphy Bio-chronostratigraphic subdivision of the Piz- zo Mondello section Ammonoids collected from the Pizzo Mondello section include short ranging age-diagnostic forms as well as long ranging taxa. Among the first group the most interesting taxa, in stratigraphical order, are Dis- cotropites plinii; Anatropites, Microtropites, Dimorphites noricus n. sp. and Dimorphites selectus. Gonionotites would also be of some interest, but only on the species level. This genus is reported in the literature from the last zone of the Carnian to the first zone of the Norian (Krystyn 1982; Tozer 1994); this long range is in part confirmed by the distribution at Pizzo Mondello, where it has been identified in levels FNP80A, PMAM36, PMAM54, PMAM7, PMAM42, PMAM43, PMAM35, PM28a and PM 28d (Fig. 6). These short-ranging taxa document all four sub- zones of the uppermost Carnian and lowermost Norian and firmly tie the Carnian/Norian boundary succession under study to the Tethyan chronostratigraphic scale. Ammonoid rarity does not allow for continuous zona- tion of the section, but the discrete intervals with am- monoid-controlled chronostratigraphic standardization are presented below (from bottom to top; Fig. 6), to- gether with pertinent comments on the intermediate intervals without age diagnostic ammonoids. – The lower 25 m of the section has thus far yielded only very small ammonoids, including one Sand- lingitidae, one Arcestidae and Hyattites cf. praefloridus. The stratigraphic significance of Hyattites has not yet been defined as the genus is rare and the literature quite inconclusive (see Systematic paleontology). Those levels yielding Sandlingitidae and H. cf. praefloridus are re- ferred to the Upper Carnian, and the single level with Hyattites may well represent Tuvalian 3 due to its close relationship with Gonionotites. Discotropites plinii subzone, Spinosus Zone (Tu- valian 3, I) The index ammonoid D. plinii was identified in level PMAM17 about 25 m above the base of the sec- tion. Projuvavites boehmi was collected from level PMAM27, just slightly above the level with D. plinii. However, the stratigrahic position of P. boehmi is not defined with respect to a particular bio-chronostrati- graphic scale, so only level PMAM17 is definitely re- ferred to the Discotropites plinii subzone. Gonionotites italicus subzone, Spinosus Zone (Tu- valian 3, II) This subzone is characterized by Microtropites and Anatropites. Microtropites occurs only in the G. italicus subzone (Krystyn 1982) while Anatropites first occurs in the underlying Discotropites spinosus subzone (Krystyn 1982). The Anatropites specimens from Pizzo Mondello were found in beds overlying level PMA- M52A, which yields Microtropites aff. paronai; hence, these levels are useful for tracing the upper boundary of the G. italicus subzone. Based on our available collec- tion, the boundaries of the Spinosus Zone are drawn at Balini M., Krystyn L., Levera M. & Tripodo A.72 PLATE 3 Upper Carnian and Lower Norian ammonoids from Pizzo Mondello and Feuerkogel (Northern Alps, Austria). 1) Dimorphites noricus n. sp., paratype GBA 2011/055/0002, lateral view. 2) Dimorphites no- ricus n. sp., paratype GBA 2011/055/0003, lateral view. 3) Dimorphites noricus n. sp., holotype GBA 2011/055/0001, a, lateral view; b, aper- tural view. 4) Dimorphites noricus n. sp., paratype GBA 2011/055/ 0004, a, lateral view; b, apertural view. 5) Dimorphites noricus n. sp., specimen MPUM 10978 (NA42.1), lateral view. 6) Dimorphites selec- tus Mojsisovics, specimen MPUM 10981 (det-1), lateral view. 7) Di- morphites selectus Mojsisovics, specimen MPUM 10979 (FNP145-19), lateral view. 8) Dimorphites sp., specimen MPUM 10985 (PM36.1), lateral view. 9) Discophyllites insignis Gemmellaro, specimen MPUM 10987 (PMAM52-1), lateral view. All specimens whitened with ammonium chloride except Fig. 5. Bar scale is always 1 cm, that in the lower right corner is for all the figures except for 1, 5 and 8. Asterisk marks the last septum. Carnian-Norian ammonoids from Pizzo Mondello 73 the base of level PMAM52A and at the top of level PMAM22bis. The fauna includes frequent Gonionotites sp., as well as Gonionotites cf. italicus, Discophyllites insignis (Gemmellaro), Projuvavites inflatus (Gemmellaro), Pi- nacoceras sp. and Pregriesbachites n. gen. bukowskii (Gemmellaro). – The interval between level PMAM22bis and NA42.1 yielded very few ammonoids, especially from the lower and very uppermost parts. Gonionotites cf. recuperoi was collected less than 1 m above the last occurrence of Anatropites and a small Tropiceltites spe- cimen was collected one-half meter below the level yielding Dimorphites noricus n. sp. No stratigraphic in- formation is available for G. recuperoi Gemmellaro and the bio-chronostratigraphic significance of Tropiceltites is not fully clear. In North America Tozer (1994) re- ported the genus from the Macrolobatus to Kerri Zones (Upper Carnian-Lower Norian). Very little information is available from the Tethyan successions apart from the report by Krystyn (1973) concerning the Lacian 1 Jan- dianus Zone at Feuerkogel and a new identification from the top of Spinosus Zone at F4 (Fig. 10). Because of the lack of reports in the literature, we do not con- sider Tropiceltites to be a marker genus. Dimorphites noricus n. sp. subzone, Jandianus Zone (Lacian 1 I) The index species occurs only in level NA42, at about 99.5 m above the base of the section. Dimorphites selectus subzone, Jandianus Zone (Lacian 1 II) Dimorphites selectus, index species of the sub- zone, was recorded from levels FNP144, FNP144b and FNP145, which range from about 99.5 to about 102 m above the base of the section, in direct strati- graphic succession with respect to the Dimorphites no- ricus n. sp. subzone. This subzone also includes Me- tathisbites cf. affinis Gemmellaro. – Level NA43, located about 2 m above the last occurrence of Dimorphites selectus yielded one cross section that could possibly be referred to Tropiceltites. This occurrence may indicate a Lacian age since the genus has not been recorded from younger beds. Paulckei Zone (Lacian 2) Dimorphites sp. ind., Discophyllites insignis (Gemmellaro) and Placites sp. ind. occur in levels FNP166 and NA49.1. These taxa are not bio-chronos- tratigraphically significant, but they occurr with Halo- bia mediterranea (see Levera 2012), which is considered as a good marker for the Paulckei Zone (Krystyn 1980; Krystyn et al. 2002). Chronostratigraphic correlations of the Pizzo Mondello section based on ammonoids Ammonoid-bearing successions documenting the latest Carnian through the earliest Norian are very rare in the world and only a few have been studied utilizing the bed-by-bed sampling method. In the Tethys realm, Pizzo Mondello can be compared and correlated with a small number of localities in the Salzkammergut area, above all with Feuerkogel, and with Jomsom in the Tethys Himalaya. In North America the most impor- tant localities are West Union Canyon (Shoshone Range, Central Nevada) and Black Bear Ridge on Will- iston Lake (British Columbia, Canada). There are a few localities in northeastern Russia that are of interest for comparison with the Boreal realm, especially in the Yana Okhotskaya River basin. With respect to such a global approach to correlation, it is obvious that the faunal composition of the different sites will be strongly influ- enced by provincialism (see Tozer 1981b, 1994; Dagys 1988; Zakharov 1997; Konstantinov 2008), but minor changes are also the result of paleoecologic control. Tethys realm Tethyan successions have provided huge collec- tions of Upper Carnian to Lower Norian ammonoids, especially from the Hallstatt red limestone facies of the Northern Alps and Timor, which were first documented in the literature in the mid 19th century. Upper Triassic successions from the Himalayas have also contributed significantly to advance the knowledge of ammonoid taxonomy, notwithstanding the fact that very few sites have been subjected to the bed-by-bed sampling ap- proach. The best site in the Northern Alps is Feuerko- gel, in the Salzkammergut area (Krystyn 1973 and 1980; Fig. 10), and in the Himalayas it is Jomsom in the Kali Gandaki (Nepal; Krystyn 1982). A limited quantity of ammonoid data are available from sections encompass- ing the Carnian/Norian boundary in Antalya, Turkey (Kavaalani: Gallet et al. 2000; Erenkolu Mezarlik 2: Krystyn & Gallet 2002). Other localities have recently provided stratigraphically controlled collections, but these are only Upper Carnian (eastern Southern Alps: De Zanche et al. 2000; Gianolla et al. 2003) or Lower Norian (Alborz, Iran: Seyed-Emami et al. 2009). Inter- esting Upper Carnian faunas have also been described in the 1970s from Okinawa, Japan (Ishibashi 1970, 1973 and 1975). Correlation of the Pizzo Mondello ammonoid re- cord with the record documented at Feuerkogel F5 and Jomsom is illustrated in Fig. 12. At both Pizzo Mon- dello and Jomsom, the successions are expanded, whereas at Feuerkogel the Hallstatt Limestone is con- densed. This notwithstanding, the Discotropites plinii, Gonionotites italicus, Dimorphites noricus n. sp. and Di- morphites selectus subzones are easily correlated by the Balini M., Krystyn L., Levera M. & Tripodo A.74 Carnian-Norian ammonoids from Pizzo Mondello 75 F ig . 1 2 - A m m o n o id re co rd o f P iz z o M o n d el lo se ct io n co m p ar ed to th e re co rd o f F eu er k o g el F 5 se ct io n (H al ls ta tt L im es to n e, N o rt h er n A lp s, A u st ri a; K ry st y n 1 9 8 0 ) an d Jo m so m (T h in ig ao n F o rm at io n , N ep al ; K ry st y n 1 9 8 2 ). Jo m so m lo g is b as ed o n th e ra n g e ch ar t o f K ry st y n ’s fi g . 4 , b u t th e sc al e is ad d ed h er e. F eu er k o g el F 5 se ct io n is d es cr ib ed in K ry st y n (1 9 8 0 ) an d it h as b ee n in cl u d ed in th is co rr el at io n s ch ar t b ec au se it is th e ty p e lo ca li ty o f D im o rp h it es n o ri cu s n . sp . F eu er k o g el F 4 re co rd is m o re co m p le te an d sh o w n in F ig . 1 0 . T h e m o st si g n if ic an t ag e- d ia g n o st ic ta x a ar e em p h as iz ed in b o ld . S ee te x t fo r d is cu ss io n . L ab el s T 1 , T 2 an d T 3 re fe r to co n o d o n t fa u n al tu rn o v er s d es cr ib ed b y M az z a et al . (2 0 1 0 ). occurrence of nominal species, or by the occurrence of genera (e.g., Microtropites), whose range is limited to a single subzone. When documenting the wide paleogeo- graphic distribution and correlation of certain ammo- noid groups such as Discotropites, Anatropites, Micro- tropites and Dimorphites over large distances, it is not surprising that some other groups show some differ- ences. The Pizzo Mondello fauna lacks certain genera, such as Griesbachites and Guembelites, that are well documented not only at Feuerkogel and Jomsom, but also in other Tethyan successions of the Himalayas (Bordet et al. 1971), Tibet (Wang & He 1976), Timor (Welter 1914) and Alborz (Seyed-Emami et al. 2009). Even though faunal distribution is quite wide from a paleogeographic point of view, the frequency of bios- tratigraphically complete successions is rather low. Not even one of the three sections illustrated in Fig. 12 in- cludes a direct superposition of lowermost Norian am- monoids on uppermost Carnian faunas. At Pizzo Mon- dello, the uppermost Carnian G. italicus and the lower- most Norian D. noricus n. sp. subzones are documen- ted, but the actual Carnian/Norian boundary falls within an interval of about 18 meters without age diag- nostic ammonoids. At Feuerkogel F5, level III is the stratum typicum of Dimorphites noricus n. sp., but G. italicus occurs only in the underlying level IV(Fig. 10 and 12), thereby demonstrating the high rate of sedi- mentary condensation. At Jomsom the unfossiliferous interval between the latest Carnian level 63 (G. italicus subzone) and earliest Norian level 78 (Jandianus Zone, Dimorphites selectus subzone) is more than 55 m thick and unfortunately lacks documentation of the D. no- ricus n. sp. subzone. West Union Canyon (central Nevada, U.S.A.) The most important ammonoid locality in North America for the Carnian/Norian boundary is West Un- ion Canyon in the Shoshone Range (central Nevada). This is the type locality of both the Schucherti and Macrolobatus Zones, the two latest Carnian ammonoid zones of the North American Triassic standard scale (Silberling 1959; Silberling & Tozer 1968). At this lo- cality there is also a good record of the earliest Norian Kerri Zone, which was actually defined at Brown Hill (Peace River Valley, British Columbia; Tozer 1965, 1967). Ammonoid faunas from West Union Canyon were described by Silberling (1959), who also provided a good description of the sedimentary succession (Lun- ing Formation). Silberling collected ammonoids and carefully documented the faunal changes from bed to bed (at least for the Macrolobatus Zone), but unfortu- nately he did not include in his paper the log with the bed-by-bed distribution of the faunas. This log pro- vided the basis for a preliminary sampling of the site carried out in 2010 (Balini et al. 2011), which resulted in the collection of the same faunas reported by Silberling in 1959. The ammonoid record of the Luning Formation is not continuous and fossil rich intervals are separated by shaly intervals without macrofossils, at least on the basis of surface sampling. Ammonoid faunas of the Schucher- ti and Macrolobatus Zones are dominated by Tropitidae (Tropites and Anatropites), but they lack Juvavitinae. At Pizzo Mondello section, the faunal composition of this particular part of the Carnian is reversed, with Juvavi- tinae (Projuvavites, Gonionotites, Pregriesbachites) dominant over Tropitidae (Hoplotropites [from litera- ture], Discotropites, Anatropites, Microtropites). Ammo- noids of the Kerri Zone include of Guembelites and Stikinoceras, but Dimorphites apparently is not present. As previously emphasized in the discussion regarding correlation with Tethyan localities, Guembelites has not been reported from the Scillato Formation, and Gonio- notites has not been found at West Union Canyon, neither by Silberling (1959) nor by Balini et al. (2011). Thus, direct correlation between West Union Canyon and Pizzo Mondello is possible for the Upper Carnian, but not for the Lower Norian, at least on the basis of the available ammonoid data. Black Bear Ridge (British Columbia, Canada) The Peace River Valley (British Columbia, Cana- da) is an important area for Middle to Upper Triassic ammonoids. Several localities were found and first de- scribed by McLearn from the 1940s through the early 1960s, and then Tozer spent the next 40 years or so expanding the ammonoid collections, improving their taxonomy and revising the biostratigraphy of the area. Although construction of the WAC Bennet dam (1968) and the subsequent flooding of the valley (1970s) de- stroyed several of McLearn and Tozer’s paleontologic sites, the new shorelines of this vast lake have provided the opportunity to collect from new and perfectly washed Triassic exposures, often of tens of kilometers in lenght. Black Bear Ridge, on the northern shore of the Lake, is the best locality for study of the Carnian/ Norian boundary because it is the only site in the Will- iston Lake area, where the succession encompassing the boundary is not affected by a lithologic change (Zonne- veld et al. 2010; cf. McRoberts 2011: fig. 3). At the well- known Pardonet Hill site on the southern lake shore, just in front of Black Bear Ridge, the Carnian-Norian boundary nearly coincides with the lithologic boundary between the Baldonel Formation and the Pardonet For- mation (Zonneveld & Orchard 2002). A similar setting is documented at Brown Hill, on the northern shore of the lake, East of Black Bear Ridge (Zonneveld & Orch- ard 2002). Balini M., Krystyn L., Levera M. & Tripodo A.76 Carnian-Norian ammonoids from Pizzo Mondello 77 F ig . 1 3 - A m m o n o id re co rd o f th e C ar n ia n /N o ri an b o u n d ar y in te rv al at P iz z o M o n d el lo co m p ar ed to th e re co rd at B la ck B ea r R id g e (W il li st o n L ak e, B ri ti sh C o lu m b ia , C an ad a) . B ed d in g o f th e tw o se ct io n s is to sc al e. B la ck B ea r R id g e se ct io n is fr o m M cR o b er ts (2 0 1 1 : fi g . 9 ). T h e B B R le v el n u m b er s re fe r to in te rv al s o f b ed s. E v er y in te rv al is fu rt h er su b d iv id ed in to b ed s, ea ch o f w h ic h is id en ti fi ed b y a le tt er . T h e fi el d p ic tu re (r ig h t) sh o w s th e b ed s o f th e C ar n ia n /N o ri an b o u n d ar y in te rv al . M cR o b er ts & K ry st y n (2 0 1 1 ) p ro p o se d to d ef in e th e b as e o f th e N o ri an at th e b as e o f le v el 1 8 F , w h er e th e F O o f th e su g g es te d p ri m ar y m ar k er H a lo b ia a u st ri a ca is re co rd ed . A m m o n o id d et er m in at io n s fr o m B B R se ct io n b y L K . In b o th se ct io n s, am m o n o id s o cc u r in d is cr et e le v el s. A t P iz z o M o n d el lo , an in te rv al o f ab o u t 1 8 m et er s w it h o u t ag e- d ia g n o st ic am m o n o id s ex is ts b et w ee n th e la st o cc u rr en ce o f la te C ar n ia n A n a tr o p it es an d th e fi rs t o cc u rr en ce o f N o ri an D im o rp h it es n o ri cu s n . sp . A t B la ck B ea r R id g e an in te rv al o f ab o u t 4 .5 m et er s ex is ts b et w ee n th e le v el y ie ld in g d ef in it e la te C ar n ia n A n a tr o p it es cf . m a cl ea rn i an d th e le v el p ro v id in g d ef in it e ea rl y N o ri an G u em b el it es cl a v a tu s. N o g o o d ag e- d ia g n o st ic ta x a ar e d o cu m en te d w it h in th is in te rv al ; se e te x t fo r d is cu ss io n o f th e si g n if ic an ce o f P te ro si re n it es . Ammonoids from Black Bear Ridge (GSC collec- tion, Vancouver and a new, small collection 2010, herein classified by LK) are rather meager, documented by only few specimens. However, their stratigraphic posi- tion permits an accurate correlation (Fig. 13). Two am- monoids from levels 16A and 22B tie the succession to the North American chronostratigraphic scale and at the same time, allow for correlation with the Tethyan scale. From the lower level (16A) a single specimen of Anatropites cf. maclearni documents the uppermost Carnian Macrolobatus Zone. Level 22B is referred to the Discostyrites ireneanus subzone, Kerri Zone (corre- lative with the lower Jandianus Zone of the Tethys) based on the occurrence of Guembelites clavatus, a spe- cies which, according to Tozer, is restricted to this sub- zone. The interval between these two levels is not bar- ren of ammonoids, but thus far, it has only yielded Gonionotites and Tropiceltites, both of which range through the Carnian/Norian boundary and Pterosire- nites, the only Boreal element in the Black Bear Ridge ammonoid fauna (Fig. 13). This genus, introduced by Tozer in 1980 from the Kerri Zone of northeastern Brit- ish Columbia, has been recognized since 1981 as a ty- pical component of the Norian Boreal assemblage (To- zer 1981b; Dagys 1988; see below). At Black Bear ridge Pterosirenites has been iden- tified both below and above (18D and 18G) the FO of H. austriaca (McRoberts 2011; McRoberts & Krystyn 2011; level 18F: Fig. 13). However, the chronostrati- graphic position of Pterosirenites is not yet fully defined. In the Boreal realm (see below) ammonoid faunal com- position is very different with respect to that of British Columbia, and the C/N boundary is based on an ammo- noid faunal change that is different with respect to the faunal changes recorded in North America and the Tethys realm. If the problem is approached from the opposite side of the Panthalassa Ocean, Pterosirenites occurs in four localities in northeastern British Colum- bia, including the Williston Lake shorelines (eastern British Columbia) and Mount McLearn (Toad River area, northern British Columbia), but even here its range is not well defined. According to its documented record, Pterosirenites is not abundant and at the few Lower Nor- ian sites (e.g. Brown Hill, type locality of the Kerri Zone) from which it has been reported. These occur- rences are somewhat scattered (Fig. 14), but more im- portantly, there is no record of uppermost Carnian am- monoids underlying Pterosirenites at these four local- ities. Apparently the ammonoid record at these four sites has been influenced by the facies change that occurred at the boundary of the Baldonel-Pardonet formations. Boreal realm Ammonoid correlation of the Tethyan succes- sions with those of the Boreal realm are very difficult because of their significantly different faunal composi- tion, but it is possible to directly link the Boreal succes- sions to northeastern British Columbia by the common occurrence of Pterosirenites. The Carnian/Norian successions of northeastern Russia are dominated by Sirenitinae, with the minor contribution of a few additional genera from different families (Dagys 1988; Bychkov 1995; Zakharov 1997; Konstantinov 2008). Carnian faunas are composed of Yakutosirenites, Neosirenites, ‘‘Striatosirenites’’, Sire- nites, Proarcestes, Arctophyllites, Arctoarpadites and Obruchevites, while Norian ammonoids include ‘‘Stria- tosirenites’’, Pterosirenites, Norosirenites, Wangoceras, Yanotrachyceras, Arctophyllites, Arcestes and Pinaco- ceras. Based on this very general summary, the Car- nian/Norian boundary is marked (Konstantinov 2008) by the disappearance of Sirenites, Neosirenites, Yakuto- sirenites and Proarcestes, and by the first occurrence of Pterosirenites, Arcestes and Pinacoceras. The best successions are located in the Primorye region (summary in Zakharov 1997) and the Yana Okhotskaya River area (Bychkov 1995). While the for- mer is characterized by a few Tethyan elements (Za- kharov et al. 1996; Zakharov 1997), Boreal faunas are best developed in the latter, which also has the highest sedimentation rate. The uppermost Carnian of the Yana Okhotskaya River, well described by Bychkov (1995), is represented by the 290 m thick Yakutensis Zone (index ammonoid Sirenites yakutensis Kiparisova) and the lowermost Norian is documented by the 300 m thick Verchojani- cum Zone. Pinacoceras verchojanicum Archipov is the index taxon of the Verchojanicum Zone, but the most common taxa of this zone are Pterosirenites and Noro- sirenites. Pterosirenites, which predates the FO of Noro- sirenites, in particular is documented in the Trans-Bai- kal, Amur, Khabarovsk areas (see Zakharov 1997) as well as in Yana Okhotskaya River basin (Bychkov 1995), and is therefore of great potential as guide fossil for the base of the Norian in the Boreal realm. How- ever, the FO of its range, at least on the basis of ammo- noids, has not yet been calibrated. Pterosirenites is part of the evolutionary lineage within the subfamily Sireni- tinae, but a stratigraphic interval with no ammonoid record exists (e.g., Bychkov 1995) between the last oc- currence of Carnian Sirenitinae and the FO of Pterosi- renites. In addition to the FO of Pterosirenites, Kon- stantinov (2008) emphasized that the base of the Norian in the Boreal realm is also characterized by the FO of Arcestes and of Pinacoceras. These two genera are com- mon in the Tethys realm and they also occur in North America, but they are long ranging and their FO in the Boreal realm is clearly younger than in the Tethys and North America. Balini M., Krystyn L., Levera M. & Tripodo A.78 Data herein summarized suggest the need for an intergrated approach to the correlation of the various localities of the Boreal realm because ammonoids alone will not facilitate a final solution. Conodont, halobiid and integrated ammonoid data may provide this solu- tion, and the key area is probably southern Primorye, where the ammonoid record shows a Tethyan influence, according to literature (Zakharov et al. 1996; Zakharov 1997). Unfortunately, the occurrence of Pterosirenites in the southern Primorye successions, first mentioned by Zakharov (1997), has been refuted by Markevitch & Zakharov (2008). They have modified the generic attri- bution of the two species previously recognized in the area, Pterosirenites kiparisovae (Zharnikova) and P. evo- lutus Zakharov & Zharnikova, to the genus Norosire- nites Tozer. Conclusions: towards the definition of a world standard Even now, one centrury after Gemmellaro’s monograph on Upper Triassic ammonoids from wes- tern Sicily, the ‘‘cherty limestone’’ (Scillato Formation) still provides a huge amount of paleontologic informa- tion, including not only ammonoids and halobiids first discovered by Gemmellaro, but also conodonts, radi- olarians and nannofossils. The results of the extensive investigations conducted during the last four years (Pre- to et al. 2012; Levera 2012; Mazza et al. 2012) demon- strate the significance of the pelagic successions of wes- tern Sicily as a world reference for the understanding of the Late Carnian to Norian transition, in terms of both time and changes in marine biofacies. New ammonoid data improve the understanding of the faunal changes across the Carnian/Norian bound- ary, and are significant in perspective for the definition of the GSSP of the base of the Norian stage. Recogni- tion of the Discotropites plinii, Gonionotites italicus, Di- morphites noricus n. sp. and Dimorphites selectus sub- zones links without question certain parts of the Pizzo Mondello section to the Upper Carnian-Lower Norian standard scale and facilitates the chronostratigraphic ca- libration of conodont and Halobia bioevents. Conodont bioevents Several conodont bioevents have been identified at Pizzo Mondello during the last few years (Mazza et al. 2010; Mazza et al. 2011; Mazza et al. 2012). Mazza et al. (2010) identified three main faunal turnovers (Fig. 12) and selected two possible conodont biovents for the definition of the GSSP of the Norian stage as fol- lows: Turnover 1, at level FNP 88A (64.76 m above the base), where Epigondolella replaces Carniepigondolella; Turnover 2, between AM23 and NA35 (80 m above the base), with a decreasing of Epigondolella and increasing of Metapolygnathus; and Turnover 3, between samples NA41 and PM30A, characterized by the disappearance of Metapolygnathus and replacement with advanced specimens of Epigondolella. Mazza et al. (2010: 123) identified the FAD of Epigondolella quadrata at level FNP88A as the most suitable bioevent for the definition of the GSSP of the Norian stage, while the FAD of Metapolygnathus communisti at level NA35 was con- sidered an alternative solution. Taxonomic studies of the conodont populations has lead Mazza et al. 2012 to reconsider the position and significance of the most significant bioevents. The revision of E. quadrata and the separation of the primi- tive specimens of this group into the new species E. miettoi has resulted in the placement of the FAD of E. quadrata from FNP88A up to FNP112. Furthermore, the study of conodont populations around the FO of the bivalve Halobia austriaca, recently proposed as mar- ker event for the GSSP (McRoberts & Krystyn 2011), has lead Mazza et al. to identify three new possible conodont bioevents as follows: the FO of Metapolyg- nathus parvus at sample AM24; the FO of Metapolyg- nathus echinatus at sample NA36; and the FAD of Car- nepigondolella gulloae at sample FNP134. New ammonoid data presented in this paper al- low the dating of these bioevents. The FAD of E. quad- rata, in both of its possible locations, and the conodont turnover T1 definitely occur together with Carnian am- monoids of the Spinosus Zone, Gonionotites italicus subzone. The FADs of M. communisti, M. parvus and M. echinatus, as well as the conodont turnover T2 are located within the interval between the last record of the Spinosus Zone and the first record of the Dimor- phites noricus n. sp. subzone of the Jandianus Zone, but they are very close to the uppermost levels yielding ammonoids of the Spinosus Zone; hence, they are prob- ably latest Carnian in age, as also suggested by halobiids (see Levera 2012). The FAD of C. gulloae and conodont turnover T3 occur very close to the FO of Halobia austriaca in level FNP135A, and are likely earliest Nor- ian in age. Halobia bioevents At the present stage of the discussion within the Carnian/Norian boundary Task Group of the Subcom- mission on Triassic Stratigraphy, the most interesting bioevent for the definition of the base of the Norian stage appears to be the First Occurrence of the bivalve Halobia austriaca, as discussed during the Palermo Workshop (September 2010) and proposed by McRo- berts & Krystyn (2011). At Pizzo Mondello this bioe- vent is located within the 18 m thick interval with a very poor ammonoid record between the Spinosus and the Jandianus zones (Fig. 12). More precisely the FO of Carnian-Norian ammonoids from Pizzo Mondello 79 H. austriaca is located 4 m below the level NA42, that marks the top of the Dimorphites noricus n. sp. sub- zone, the 1st subzone of the Norian stage. For the pur- pose of a pure speculation, we assume that level FNP135A can not be far from the Carnian/Norian am- monoid boundary. The (weak) elements in support of this speculation are derived from the comparison of the range of certain species that suggests a reduction of the sedimentation rate from the Tuvalian 3 to the Lacian 1. The Spinosus Zone (Tuvalian 3) is at least 55 m thick (Fig. 6), whereas the interval between the FO of Dimor- phites selectus and the FO of Halobia mediterranea, which is equivalent to the D. selectus subzone (Lacian 1 II, sensu Krystyn et al. 2002), is only 6-7 m thick. In this respect, the position of FNP135A at four meters below the boundary between the D. noricus n. sp. and D. selectus subzones most likely corresponds to an ear- liest Norian age. Future steps At this point in time, comparison of the Pizzo Mondello ammonoid record to that from Black Bear Ridge does not solve the problem of the definition of the Carnian/Norian boundary. Both sections are rela- tively expanded and ammonoids are rather scarce; thus, it seems clear that the GSSP of the Norian stage cannot be defined on an ammonoid bioevent alone. However, due to their very high power of resolution, ammonoids are the unrivaled tool for calibration of bioevents of fossil groups with a lower power of resolution, such as conodonts and in part halobiids. The two GSSP candidate sections can be accu- rately correlated with ammonoids (Fig. 13), but not the interval around the FO of Halobia austriaca. At Pizzo Mondello, ammonoids have not been collected from level FNP135A, which records the FO of Halobia austriaca. Thus, it is necessary to conduct a new ammo- noid sampling program for the interval NA41-NA42 (i.e., from the FAD of Carniepigondolella gulloae to the FO of Dimorphites noricus n. sp.). With regard to ammonoid data at Black Bear Ridge, the FO of H. aus- triaca at level 18F, as suggested by McRoberts & Krys- tyn (2011), falls within the range of the Pterosirenites Norian element according to Tozer (1994), whose FO is recorded in bed 18B, slightly below 18F (Fig. 13). How- ever, it is conceptually wrong to use data from scattered localities, such as isolated outcrops sampled by McLearn and Tozer in northern and eastern British Co- lumbia (Fig. 14), to calibrate the cm-by-cm sampled section Black Bear Ridge. The correct approach is to Balini M., Krystyn L., Levera M. & Tripodo A.80 Fig. 14 - Stratigraphic distribution of Pterosirenites Tozer, 1980 from eastern and northern British Columbia, based upon data from Tozer (1994). All sites yielding Pterosirenites are included, but the genus has not been found in a few other Lower Norian sites (e.g., Brown Hill, type locality of the Kerri Zone). Note (*): Position of GSC locality 98880 was described by Tozer (1994:347) as ‘‘probably stratigraphically between GSC loc. 64628 (Macrolobatus Zone) and GSC loc. 64607 (Kerri subzone II)’’. Only site GSC 98880 was used for this figure because the exact position of the three sites was not fully clear to Tozer, who sampled GSC 64628 and GSC 64607 in 1964 (Tozer 1967, 1994), and GSC 98880 in 1982. Pterosirenites was not found in the samples taken in 1964. resample the relevant portion of the Black Bear Ridge section such that the first occurrence of H. austriaca can be better constrained. Acknowledgements. Ammonoids described in this paper were collected during several field excursions carried out at Pizzo Mondello from 2007 to 2010 (MB and ML, with contribution of LK and AT). We would like to warmly thank A. Nicora and M. Mazza (both UNIMI), M. Rigo and C. Guaiumi (both UNIPD) who were with us in the field and occasionally helped with the sampling. M. Balini and M. Levera are deeply indebted to C. D’Arpa (UNIPA), Curator of the collections of the Museo Geologico ‘‘G.G. Gemmellaro’’, for her very kind assistance during several visits to examine the collections, and for stimulating discussions regarding the history of the Gemmellaro collections. Spe- cial thanks also extended to P. Di Stefano (UNIPA), who was always convinced of the great potential of the sicanian facies and warmly en- couraged us to look for new localities. He was right! Last but not least we would like to express our gratitude to G. Muttoni (UNIMI), who was the first stratigrapher of Milano University who invested weeks in sampling of Pizzo Mondello section. Our work is complemental to his accurate investigations. Our knowledge of Carnian/Norian ammonoids was notably improved by a visit to the collections housed at the Geological Survey of Canada facilities in Vancouver, which occurred in 2010 with the crucial help and support of M. Orchard (GSC, Vancouver). We are also very grateful to J.P. Zonneveld (University of Edmonton, Alberta) who provided us the opportunity to visit the most important sites in the Williston Lake area in May 2010 within the framework of the activities of the Carnian/Norian boundary Task Group of the Subcommission on the Triassic Stratigraphy. John-Paul did a great job organizing the filed trip and also covered most of the cost of the logistics. We had an enjoyable time together on the Lake. Technical support by G. Chiodi (UNIMI). Special thanks to reviewers S. Lucas (Albuquerque, USA), Paolo Mietto (Padova, Italy) and Y. Zakharov (Vladivostok, Russia) for the many fruitful sugges- tions that improved the manuscript. A special warm thank to J. Jenks (Salt Lake City, USA) who very carefully reviewed the final version of the manuscript. He spent quite a lot of time on it and his suggestions improved not only the style, but also some rather complex parts of Systematic paleontology and Chronostratigraphy chapters. 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