Advanced Search

Indexed by SCI、CA、РЖ、PA、CSA、ZR、etc .

Volume 32 Issue 3
Jun.  2021
Turn off MathJax
Article Contents

Ali Murat Kılıç. Anisian (Middle Triassic) Conodonts of the Kocaeli Triassic, Western Turkey. Journal of Earth Science, 2021, 32(3): 616-632. doi: 10.1007/s12583-020-1384-9
Citation: Ali Murat Kılıç. Anisian (Middle Triassic) Conodonts of the Kocaeli Triassic, Western Turkey. Journal of Earth Science, 2021, 32(3): 616-632. doi: 10.1007/s12583-020-1384-9

Anisian (Middle Triassic) Conodonts of the Kocaeli Triassic, Western Turkey

doi: 10.1007/s12583-020-1384-9
More Information
  • The present study of Anisian (Middle Triassic) conodonts from the Kocaeli Peninsula (western Turkey) encompasses over 10 species of the families Gondolellidae and Gladigondolellidae, providing Early and Middle Triassic time constraints, Chiosella timorensis (Nogami, 1968); Cornudina oezdemirae Gedik, 1975; Gladigondolella tethydis (Huckriede, 1958); Neostrachanognathus tahoensis Koike, 1998; Paragondolella aegaea (Bender, 1970); Paragondolella bulgarica Budurov and Stefanov, 1975; Nicoraella kockeli (Tatge, 1956); P. hanbulogi (Sudar and Budurov, 1979), and Gladigondolella sp. A. Newly established are Paragondolella hirschii n. sp. Kılıç and Budurov; P. praecornuta n. sp. Kılıç, Budurov, Petrunova and Mirăuţă; and P. ebruae n. sp. Kılıç. The Kocaeli Anisian conodonts show a faunal affinity with Bulgaria. The present Anisian fauna is characteristic of the Tethys. The strong homeomorphy that characterizes the Anisian in western North America is discussed.
  • 加载中
  • Agematsu, S., Orchard, M. J., Sashida, K., 2008. Reconstruction of an Apparatus of Neostrachanognathus tahoensis from Oritate, Japan and Species of Neostrachanognathus from Oman. Palaeontology, 51(5): 1201-1211. doi:  10.1111/j.1475-4983.2008.00804.x
    Assereto, R., 1972. Notes on the Anisian Biostratigraphy of the Gebze Area (Kocaeli Peninsula, Turkey). Zeitschrift der Deutschen Geologischen Gesellschaft, 123(2): 435-444. doi:  10.1127/zdgg/123/1972/435
    Assereto, R., 1974. Aegean and Bithynian: Proposal for Two New Anisian Substages. In: Zapfe, H., ed., The Stratigraphy of the Alpine-Mediterranean Triassic. Springer, Vienna. 23-39.
    Bender, H., 1970. Zur Gliederung der Mediterranen Trias II. Die Conodontenchronologie der Mediterranen Trias. Annales Geologiques des Pays Helleniques, 19: 465-540
    Bender, H., Stoppel, D., 1965. Perm-Conodonten. Geologisches Jahrbuch, 82: 331-364
    Budurov, K., 1960. Uber die Anwesenheit von Conodonten im Anis bei Granitovo, Bezirk Vidin. Bulg. Geol. Soc. Rev., 21: 77-80 (in Bulgarian with English Summary)
    Budurov, K., 1973. Carinella n. gen. und Revision der Gattung Gladigondolella (Conodonta). Comptes Rendus de l'Academie Bulgare des Sciences, 26: 799-802
    Budurov, K., 1975. Paragondolella foliata sp. n. [Conodonta] von der Trias des Ostbalkans. Rev. Bulg. Geol. Soc., 36(1): 79-81
    Budurov, K., 1980. Conodont Stratigraphy of the Balkanide Triassic. Rivista Italiana di Paleontologia e Stratigrafia, 85: 767-780
    Budurov, K. J., Stefanov, S., 1972. Platform-Condonten und Ihre Zonen in der Mittleren Trias Bulgariens. Mitt. Ges. Geol. Bergabaustud, 21: 829-852
    Budurov, K. J., Stefanov, S., 1975. Neue Daten über die Conodonten-Chronologie der Balkaniden Mittleren Trias. Comptes Rendus de lʼAcademia Bulgare des Sciences, 28(6): 791-794
    Budurov, K. J., Sudar, M. N., 1990. Late Triassic Conodont Stratigraphy. In: Ziegler, W., ed., 1st International Senckenberg Conference and 5th European Conodont Symposium (ECOS V) Contributions IV. Papers on Conodonts and Ordovician to Triassic Conodont Stratigraphy. Courier Forschungsinstitut Senckenberg, 118: 203-240
    Budurov, K. J., Sudar, M. N., Gupta, V. J., 1988. Kashmirella a New Early Triassic Conodont Genus. Bulletin of Indian Geologists Association, 21: 107-112
    Buryi, G. I., 1989. Triassic Conodonts and Stratigraphy of Sikhote-Alin. FEB Academy of Sciences of the USSR, Vladivostok. 136
    Chen, Y. L., Krystyn, L., Orchard, M. J., et al., 2016. A Review of the Evolution, Biostratigraphy, Provincialism and Diversity of Middle and Early Late Triassic Conodonts. Papers in Palaeontology, 2(2): 235-263. doi:  10.1002/spp2.1038
    Chen, Y. L., Scholze, F., Richoz, S., et al., 2019a. Middle Triassic Conodont Assemblages from the Germanic Basin: Implications for Multi-Element Taxonomy and Biogeography. Journal of Systematic Palaeontology, 17(5): 359-377. doi:  10.1080/14772019.2018.1424260
    Chen, Y. L., Richoz, S., Krystyn, L., et al., 2019b. Quantitative Stratigraphic Correlation of Tethyan Conodonts across the Smithian-Spathian (Early Triassic) Extinction Event. Earth-Science Reviews, 195: 37-51. doi:  10.1016/j.earscirev.2019.03.004
    Clark, D. L., Sweet, W. C., Bergstrom, S. M., et al., 1981. Conodonta. Part W, Miscellanea, Supplement 2. In: Robison, R. A., ed., Treatise on İnvertebrate Paleontology. Geological Society of America, Boulder, Colo., University of Kansas, Lawrence
    Dagys, A. S., 1987. Boreal Trias. Institute of Geology and Geophysics, Academy of Sciences of the USSR Siberian Branch. Transactions у, 689: 131
    Donoghue, P. C. J., Purnell, M. A., Aldridge, R. J., et al., 2008. The Interrelationships of 'Complex' Conodonts (Vertebrata). Journal of Systematic Palaeontology, 6(2): 119-153. doi:  10.1017/s1477201907002234
    Dzik, J., 1976. Remarks on the Evolution of Ordovician Conodonts. Acta Palaeontologica Polonica, 21(4): 395-455
    Farabegoli, E., Levanti, D., Perri, M. C., et al., 1984. M. Bivera Formation: An Atypical Middle Triassic "Rosso Ammonitico" Facies from Southern Alps (Italy). Giornale di Geologia, 46: 33-46
    Franz, M., Kaiser, S. I., Fischer, J., et al., 2015. Eustatic and Climatic Control on the Upper Muschelkalk Sea (Late Anisian/Ladinian) in the Central European Basin. Global and Planetary Change, 135: 1-27. doi:  10.1016/j.gloplacha.2015.09.014
    Gaetani, M., Jacobshagen, V., Nicora, A., et al., 1992. The Early-Middle Triassic Boundary at Chios. Rivista Italiana di Paleontologia e Stratigrafia, 98(2): 181-204
    Gedik, İ., 1975. Die Conodonten der Trias auf der Kocaeli Halbinsel[Turkei]. Palaeontographica Abteilung, [A]: 99-160
    Götz, A. E., Gast, S., 2010. Basin Evolution of the Anisian Peri-Tethys: Implications from Conodont Assemblages of Lower Muschelkalk Key Sections (Central Europe). Zeitschrift Der Deutschen Gesellschaft Für Geowissenschaften, 161(1): 39-49. doi:  10.1127/1860-1804/2010/0161-0039
    Golding, M. L., Orchard, M. J., Zonneveld, J. P., et al., 2014. An Exceptional Record of the Sedimentology and Biostratigraphy of the Montney and Doig Formations in British Columbia. Bulletin of Canadian Petroleum Geology, 62(3): 157-176
    Golding, M. L., Orchard, M. J., Zonneveld, J. P., et al., 2015. Determining the Age and Depositional Model of the Doig Phosphate Zone in Northeastern British Columbia Using Conodont Biostratigraphy. Bulletin of Canadian Petroleum Geology, 63(2): 143-170. doi:  10.2113/gscpgbull.63.2.143
    Golding, M. L., Orchard, M. J., 2018. Magnigondolella, a New Conodont Genus from the Triassic of North America. Journal of Paleontology, 92(2): 207-220. doi:  10.1017/jpa.2017.123
    Goudemand, N., Orchard, M. J., Bucher, H., et al., 2011. Is Chiosella timorensis a Good Index for the Olenekian-Anisian Boundary?. In: Håkansson, E., Trotter, J. A., eds., Programme and Abstracts: The XVII International Congress on the Carboniferous and Permian. July 2011, Perth. 61
    Goudemand, N., Orchard, M. J., Bucher, H., et al., 2012. The Elusive Origin of Chiosella timorensis (Conodont Triassic). Geobios, 45(2): 199-207. doi:  10.1016/j.geobios.2011.06.001
    Grãdinaru, E., Kozur, H., Nicora, A., et al., 2006. The Chiosella timorensis Lineage and Correlation of the Ammonoids and Conodonts around the Base of the Anisian in the GSSP Candidate at Desli Caira (North Dobrogea, Romania). Albertiana, 34: 34-38
    Hayashi, S., 1968. The Permian Conodonts in Chert of the Adayama Formation, Ashio Mountains, Central Japan. Earth Science (Chikyu Kagaku), 22(2): 63-77
    Hirsch, F., 1969. La Succession des Faunes de Conodontes dans les Couches de Passage de lʼAnisien Supérieur au Ladinien Inférieur des Alpes Orientales et Méridionales. Arch. Sc. Genève, 22(1): 83-90 (in French)
    Hirsch, F., 1975. Lower Triassic Conodonts from Israel. Bull. Geol. Surv. Israel, 66: 39-48
    Hirsch, F., 1994. Triassic Conodonts as Ecological and Eustatic Sensors. In: Embry, A. F., Beauchamp, B., Glass, D. J., eds., Pangea: Global Environments and Resources. Memoir of the Canadian Society of Petroleum Geologists, 17: 949-959
    Hirschmann, C., 1959. Uber Conodonten aus dem Oberen Muschelkalk des Thüringer Beckens. Freiberger Forschungshefte, Paläontologie, 76: 35-86
    Huang, J. Y., Hu, S. X., Zhang, Q. Y., et al., 2019a. Gondolelloid Multielement Conodont Apparatus (Nicoraella) from the Middle Triassic of Yunnan Province, Southwestern China. Palaeogeography, Palaeoclimatology, Palaeoecology, 522: 98-110. doi:  10.1016/j.palaeo.2018.07.015
    Huang, J. Y., Martínez-Pérez, C., Hu, S. X., et al., 2019b. Middle Triassic Conodont Apparatus Architecture Revealed by Synchrotron X-Ray Microtomography. Palaeoworld, 28(4): 429-440. doi:  10.1016/j.palwor.2018.08.003
    Huckriede, R., 1958. Die Conodonten der Mediterranen Trias und ihr Stratigraphischer Wert. Paläontologische Zeitschrift, 32(3/4): 141-175 doi:  10.1007/BF02989028.pdf
    Ishida, K., Hirsch, F., 2011. The Triassic Conodonts of the NW Malayan Kodiang Limestone Revisited: Taxonomy and Paleogeographic Significance. Gondwana Research, 19(1): 22-36. doi:  10.1016/
    Ishii, K., Nogami, Y., 1966. Discovery of Triassic Conodonts from the So-Called Palaeozoic Limestone in Kedah, Malaya. Osaka City University, Journal Geosciences, 9: 92-98
    Karádi, V., Dulai, A., 2016. Sándor Kovácsʼs Conodont Collection. Annales Musei Historico-Naturalis Hungarici, 108: 221-229
    Kılıç, A. M., 2004. Multielement Taxonomy of the Triassic Conodonts of the Kocaeli Region: [Dissertation]. Cumhuriyet University, Sivas, Turkey. 132 (in Turkish with English Abstract)
    Kılıç, A. M., Plasencia, P., Guex, J., et al., 2018a. Challenging Darwin: Evolution of Triassic Conodonts and Their Struggle for Life in a Changing World. Stratigraphy and Timescales, 2: 333-389. doi:  10.1016/bs.sats.2017.08.003
    Kılıç, A. M., Plasencia, P., Onder, F., 2018b. Debate on Skeletal Elements of the Triassic Conodont Cornudina Hirschmann. Acta Geologica Polonica, 68(2): 147-159
    Klapper, G., Lindström, M., Sweet, W. C., et al., 1973. In: Ziegler, W., ed., Catalogue of Conodonts. Schweizerbart Science Publishers, Stuttgart. 1: XVIII
    Koike, T., 1982. Review of Some Platform Conodonts of the Middle and Late Triassic of Japan. Science Reports of the Yokohama National University, Section 2: Biological and Geological, 2/29: 15-27
    Koike, T., 1996. Skeletal Apparatuses of Triassic Conodonts of Cornudina. In: Noda, K., Sashida, K., eds., Professor Hisayoshi Igo Commemorative Volume on Geology and Paleontology of Japan and Southeast Asia. Gakujyutsu Tosho Insatsu Co. Ltd., Tokyo. 113-120
    Koike, T., 1998. Triassic Coniform Conodont Genera Aduncodina and Neostrachanognathus. Paleontological Research, 2(2): 120-129
    Koike, T., 1999. Apparatus of a Triassic Conodont Species Cratognathodus multihamatus (Huckriede). Paleontological Research, 3(4): 234-248
    Koike, T., 2016. Multielement Conodont Apparatuses of the Ellisoniidae from Japan. Paleontological Research, 20(3): 161-175. doi:  10.2517/2016pr007
    Kolar-Jurkovšek, T., Jurkovšek, B., 2010. New Paleontological Evidence of the Carnian Strata in the Mežica Area (Karavanke Mts, Slovenia): Conodont Data for the Carnian Pluvial Event. Palaeogeography, Palaeoclimatology, Palaeoecology, 290(1/2/3/4): 81-88. doi:  10.1016/j.palaeo.2009.06.015
    Kolar-Jurkovšek, T., Gaździcki, A., Jurkovšek, B., 2005. Conodonts and Foraminifera from the "Raibl Beds" (Carnian) of the Karavanke Mountains, Slovenia: Stratigraphical and Palaeobiological Implications. Geological Quarterly, 49(4): 429-438
    Kolar-Jurkovšek, T., Chen, Y. L., Jurkovšek, B., et al., 2017. Conodont Biostratigraphy of the Early Triassic in Eastern Slovenia. Paleontological Journal, 51(7): 687-703. doi:  10.1134/s003103011707005x
    Kovács, S., 2003. Pelsonian Conodonts from the Balaton Highland. Geologica Hungarica, Series Palaeontologica, 55: 159-177
    Kozur, H. W., 1968. Neue Conodonten aus dem Oberen Muschelkalk des Germanischen Binnenbeckens. Monatsber. Deutsch. Akad. Wiss. Berlin, 10(2): 130-142, Pl. 1
    Kozur, H., 1980. Revision der Conodontenzonierung der Mittel-und Obertrias des Tethyalen Faunenreichs. Geologische-Paläontologische Mitteilungen Innsbruck, 10: 79-112
    Kozur, H. W., 1989. The Taxonomy of the Gondolellids Conodonts in the Permian and Triassic. 1st International Senckenberg Conference and 5th European Conodont Symposium (ECOS V): Contributions III, Papers on Ordovician to Triassic Conodonts. 117: 409-469
    Kozur, H., 1993. Nicoraella postkockeli n. sp., a New Conodont Species from the Lower Carnian of Hungary. Neues Jahrbuch für Geologie und Paläontologie-Monatshefte, 7: 405-412. doi:  10.1127/njgpm/1993/1993/405
    Kozur, H. W., 2003. Integrated Ammonoid-, Conodont and Radiolarian Zonation of the Triassic. Hall Jahrb. Abt. Geowiss. B, 25: 49-79
    Kozur, H., Mock, R., 1991. New Middle Carnian and Rhaetian Conodonts from Hungary and the Alps. Stratigraphic Importance and Tectonic Implications for the Buda Mountains and Adjacent Areas. Jahrbuch der Geologischen Bundesanstalt, 134(2): 271-297
    Kozur, H. W., Mostler, H., 1970. Neue Conodonten aus der Trias. Ber. Nat. -Med. Verein Innsbruck, 58: 429-464
    Kozur, H. W., Mostler, H., 1971. Probleme der Conodontenforschung in der Trias. Geol. Palaont. Mitt. Innsbruck, 1(4): 1-19
    Kozur, H. W., Mostler, H., 1972. Die Bedeutung der Conodonten fur Stratigraphische und Paleogeographische Untersuchungen in der Trias. Mitt. Ges. Geot. Bergbaustud., 21: 777-810
    Kozur, H. W., Mostler, H., 1992. Erster Paläontologischer Nachweis von Meliaticum und Sud-Rudabanyaicum in den Nordlichen Kalkalpen (Osterreich) und ihre Beziehung zu den Abfolgen den Westkarpaten. Geologische-Palaontologische Mitteilungen Innsbruck, 18: 87-129
    Lambert, L. L., Wardlaw, B. R., Henderson, C. M., 2007. Mesogondolella and Jinogondolella (Conodonta): Multielement Definition of the Taxa that Bracket the Basal Guadalupian (Middle Permian Series) GSSP. Palaeoworld, 16(1-3): 208-221. doi:  10.1016/j.palwor.2007.05.017
    Lehrmann, D. J., Stepchinski, L., Altiner, D., et al., 2015. An Integrated Biostratigraphy (Conodonts and Foraminifers) and Chronostratigraphy (Paleomagnetic Reversals, Magnetic Susceptibility, Elemental Chemistry, Carbon Isotopes and Geochronology) for the Permian-Upper Triassic Strata of Guandao Section, Nanpanjiang Basin, South China. Journal of Asian Earth Sciences, 108: 117-135. doi:  10.1016/j.jseaes.2015.04.030
    Lindström, M., 1970. A Suprageneric Taxonomy of the Conodonts. Lethaia, 3(4): 427-445. doi:  10.1111/j.1502-3931.1970.tb00834.x
    Márquez-Aliaga, A., Valenzuela-Ríos, J. I., Calvet, F., et al., 2000. Middle Triassic Conodonts from Northeastern Spain: Biostratigraphic Implications. Terra Nova, 12(2): 77-83. doi:  10.1046/j.1365-3121.2000.00273.x
    Mazza, M., Rigo, M., Gullo, M., 2012. Taxonomy and Biostratigraphic Record of the Upper Triassic Conodonts of the Pizzo Mondello Section (Western Sicily, Italy), GSSP Candidate for the Base of the Norian. Rivista Italiana di Paleontologia e Stratigrafia, 8: 85-130
    Meco, S., 1999. Conodont Biostratigraphy of Triassic Pelagic Strata, Albania. Rivista Italiana di Paleontologia e Stratigrafia, 105(2): 251-266
    Mietto, P., Fratoni, R. P., Perri, M. C., 1991. Spathian and Aegean Conodonts from the Capelluzo Calcarenites of the Monte Facito Group. Memorie di Scienze Geologische, XLIII: 305-317
    Mosher, L. C., 1968. Triassic Conodonts from Western North America and Europe and Their Correlation. Journal of Paleontology, 42: 895-946
    Mosher, L. C., 1970. New Conodont Species as Triassic Guide Fossils. Journal of Paleontology, 44(4): 737-742
    Mosher, L. C., Clark, D. L., 1965. Middle Triassic Conodonts from the Prida Formation of Northwestern Nevada. Journal of Paleontology, 39: 551-565
    Müller, K. J., 1962. Zur Systematischen Einteilung der Conodontophorida. Paläontologische Zeitschrift, 36(1): 109-117. doi:  10.1007/bf02989634
    Narkiewicz, K., 1999. Conodont Biostratigraphy of the Muschelkalk (Middle Triassic) in the Central Part of the Polish Lowlands. Geological Quarterly, 43(3): 313-328
    Nicora, A., 1977. Lower Anisian Platform-Conodonts from the Tethys and Nevada: Taxonomic and Stratigraphic Revision. Palaeontographica Abteilung A, 157(1-3): 88-107
    Nogami, Y., 1968. Trias-Conodonten von Timor, Malaysien und Japan (Palaeontological Study of Portuguese Timor, 5). Memoirs of the Faculty of Science, Kyoto University, Series of Geology and Mineralogy, 34: 115-136
    Orchard, M. J., 1991a. Late Triassic Conodont Biochronology and Biostratigraphy of the Kunga Group, Queen Charlotte Islands, British Columbia. In: Woodsworth, G. W., ed., Evolution and Hydrocarbon Potential of the Queen Charlotte Basin, British Columbia. Geological Survey of Canada Paper, 1990-10: 173-193.
    Orchard, M. J., 1991b. Upper Triassic Conodont Biochronology and New Index Species from the Canadian Cordillera. In: Orchard, M. J., McCracken, A. D., eds., Ordovician to Triassic Conodont Paleontology of the Canadian Cordillera. Geological Survey of Canada, Bulletin, 417: 299-335.
    Orchard, M. J., 1994. Conodont Biochronology around the Early-Middle Triassic Boundary: New Data from North America, Oman and Timor. Memoires de Geologie (Lausanne), 22: 105-115
    Orchard, M. J., 2005. Multielement Conodont Apparatuses of Triassic Gondolelloidea. Special Papers in Palaeontology, 73(73): 73-101
    Orchard, M. J., 2007. New Conodonts and Zonation, Ladinian-Carnian Boundary Beds, British Columbia, Canada. In: Lucas, S. G., Spielmann, J. A., eds., The Global Triassic. New Mexico Museum of Natural History and Science Bulletin, 41: 321-330
    Orchard, M. J., 2013. Five New Genera of Conodonts from the Carnian-Norian Boundary Beds of Black Bear Ridge, Northeast British Columbia, Canada. In: Tanner, L. H., Spielmann, J. A., Lucas, S. G., eds., The Triassic System. New Mexico Museum of Natural History and Science Bulletin, 61: 445-437
    Orchard, M. J., 2014. Conodonts from the Carnian-Norian Boundary (Upper Triassic) of Black Bear Ridge, Northeasern British Columbia, Canada. New Mexico Museum of Natural History and Science Bulletin, 64: 139
    Orchard, M. J., Cordey, F., Rui, L., et al., 2001. Biostratigraphic and Biogeographic Constraints on the Carboniferous to Jurassic Cache Creek Terrane in Central British Columbia. Canadian Journal of Earth Sciences, 38(4): 551-578. doi:  10.1139/e00-120
    Orchard, M. J., Lehrmann, D. J., Wei, J. Y., et al., 2007a. Conodonts from the Olenekian-Anisian Boundary Beds, Guandao, Guizhou Province, China. New Mexico Museum of Natural History and Science Bulletin, 41: 347-354
    Orchard, M. J., Gradinăru, E., Nicora, A., 2007b. A Summary of the Conodont Succession around the Olenekian-Anisian Boundary at Deşli Caira, North Dobrogea, Romania. New Mexico Museum of Natural History and Science Bulletin, 41: 341-346
    Orchard, M. J., Rieber, H., 1999. Multielement Neogondolella (Conodonta, Upper Permian-Middle Triassic). In: Serpagli, E., ed., Studies on conodonts. Proceedings of the Seventh European Conodont Symposium. June 1998, Bologna Modena, Italy. Bollettino della Societa Palaeontologica Italiana, 37: 475-488
    Pander, C. H., 1856. Monographie der Fossilen Fische des Silurischen Systems der Russisch-Baltischen Gouvernements. Buchdruckerei der Kaiserlichen Akademie der Wissenschaften, St. Petersburg. 91
    Pisa, G., Perri, C., Veneri, P., 1980. Upper Anisian Conodonts from Dont and M. Bivera Formations, Southern Alps (Italy). Rivista Italiana di Paleontologia e Stratigrafia, 85: 807-828
    Rigo, M., Preto, N., Roghi, G., et al., 2007. A Rise in the Carbonate Compensation Depth of Western Tethys in the Carnian (Late Triassic): Deep-Water Evidence for the Carnian Pluvial Event. Palaeogeography, Palaeoclimatology, Palaeoecology, 246(2/3/4): 188-205. doi:  10.1016/j.palaeo.2006.09.013
    Sudar, M. N., Budurov, K., 1979. New Conodonts from the Triassic in Yugoslavia and Bulgaria. Geologica Balcanica, 9(3): 47-52
    Sun, Z. Y., Sun, Y. L., Hao, W. C., et al., 2006. Conodont Evidence for the Age of the Panxian fauna, Guizhou, China. Acta Geologica Sinica, 80(5): 621-630
    Sun, Z. Y., Hao, W. -C., Sun, Y. -L., et al., 2009. The Conodont Genus Nicoraella and a New Species from the Anisian of Guizhou, South China. Neues Jahrbuch für Geologie und Paläontologie-Abhandlungen, 252(2): 227-235. doi:  10.1127/0077-7749/2009/0252-0227
    Sweet, W. C., 1970. Uppermost Permian and Lower Triassic Conodonts of the Salt Range and Trans-İndus Ranges, West Pakistan. In: Kummel, B., Teichert, C., eds., Stratigraphic Boundary Problems: Permian and Triassic of West Pakistan. Volume Special Publication 4. University Press of Kansas, Lawrence. 207-275
    Tatge, U., 1956. Conodonten aus dem Germanischen Muschelkalk. Paläontologische Zeitschrift, 30(3/4): 129-147. doi:  10.1007/bf03041777
    Trammer, J., 1975. Stratigraphy and Facies Development of the Muschelkalk in the South-Western Holy Cross Mts. Acta Geologica Polonica, 25: 179-216
    Tüysüz, O., Aksay, A., Yiğitbaş, E., 2004. Batı Karadeniz Bolgesi Litostratigrafi Birimleri. Turkiye Stratigrafi Komitesi Litostratigrafi Birimleri Serisi-1, General Directorate of Mineral Research and Exploration Publications, Ankara, Turkey. 92 (in Turkish)
    Wang, Z. H., Dai, J. Y., 1981. Triassic Conodonts from the Jiangyou-Beichuan Area, Sichuan Province. Acta Micropalaeontologica Sinica, 20: 138-150. doi:  10.19800/j.cnki.aps.1981.02.005
    Zawidzka, K., 1975. Conodont Stratigraphy and Sedimentary Environment of the Muschelkalk in Upper Silesia. Acta Geologica Polonica, 25(2): 217-257
    Zhang, Q. Y., Zhou, C. Y., Lu, T., et al., 2009. A Conodont-Based Middle Triassic Age Assignment for the Luoping Biota of Yunnan, China. Science in China Series D: Earth Sciences, 52(10): 1673-1678. doi:  10.1007/s11430-009-0114-z
  • 加载中
通讯作者: 陈斌,
  • 1. 

    沈阳化工大学材料科学与工程学院 沈阳 110142

  1. 本站搜索
  2. 百度学术搜索
  3. 万方数据库搜索
  4. CNKI搜索


Article Metrics

Article views(30) PDF downloads(6) Cited by()

Proportional views

Anisian (Middle Triassic) Conodonts of the Kocaeli Triassic, Western Turkey

doi: 10.1007/s12583-020-1384-9

Abstract: The present study of Anisian (Middle Triassic) conodonts from the Kocaeli Peninsula (western Turkey) encompasses over 10 species of the families Gondolellidae and Gladigondolellidae, providing Early and Middle Triassic time constraints, Chiosella timorensis (Nogami, 1968); Cornudina oezdemirae Gedik, 1975; Gladigondolella tethydis (Huckriede, 1958); Neostrachanognathus tahoensis Koike, 1998; Paragondolella aegaea (Bender, 1970); Paragondolella bulgarica Budurov and Stefanov, 1975; Nicoraella kockeli (Tatge, 1956); P. hanbulogi (Sudar and Budurov, 1979), and Gladigondolella sp. A. Newly established are Paragondolella hirschii n. sp. Kılıç and Budurov; P. praecornuta n. sp. Kılıç, Budurov, Petrunova and Mirăuţă; and P. ebruae n. sp. Kılıç. The Kocaeli Anisian conodonts show a faunal affinity with Bulgaria. The present Anisian fauna is characteristic of the Tethys. The strong homeomorphy that characterizes the Anisian in western North America is discussed.

Ali Murat Kılıç. Anisian (Middle Triassic) Conodonts of the Kocaeli Triassic, Western Turkey. Journal of Earth Science, 2021, 32(3): 616-632. doi: 10.1007/s12583-020-1384-9
Citation: Ali Murat Kılıç. Anisian (Middle Triassic) Conodonts of the Kocaeli Triassic, Western Turkey. Journal of Earth Science, 2021, 32(3): 616-632. doi: 10.1007/s12583-020-1384-9
  • This study encompasses the Anisian conodonts of the Kocaeli Peninsula (Fig. 1). The volume of conodont taxa collected in the course of former studies in this region, as well as during our present sampling is impressive, including more than 20 form genera and 40 form species. South of Gebze, between Orta Dere and Kurt Dere (Dere=Creek in Turkish), five stratigraphic sections were measured and intensively sampled for conodonts (Figs. 1 and 2). In addition to these measured sections, some further stratigraphic sections of similar lithology were used for correlation. These sample localities are in the south of the peninsula: Eskihisar, Diliskelesi, Tepecik, and between Köseler and Gebze.

    Figure 1.  Map of the Kocaeli Peninsula in Turkey, showing the locations of measured stratigraphic sections (KTM3, KTM4, KTM4/2, KTM4/3 and KTM5) south of Gebze, on the Marmara Sea coastline; modified after Kılıç et al. (2018b).

    Figure 2.  Generalized stratigraphic columnar section of the Kocaeli Triassic (after Kılıç et al., 2018b; Gedik, 1975; Assereto, 1974) (a); and five measured co lumnar sections of Tepeköy Formation near Gebze, showing lithology and the distribution of conodont species (b). E. Early; L. late; Fm. Formation.

    This study unravels the stratigraphy of an apparently complete Anisian sequence by using conodonts. These include Chiosella timorensis (Nogami, 1968) (late Spathian–Aegean); Cornudina oezdemirae Gedik, 1975 (Spathian–Aegean); Gladigondolella tethydis (Huckriede, 1958) (Aegean–Julian); Paragondolella aegaea (Bender, 1970) (Aegean–Bithynian), differing from the North American Magnigondolella regalis (Mosher, 1970) (Spathian–Bithynian); Neostrachanognathus tahoensis Koike, 1998 (late Spathian–Aegean); Nicoraella kockeli (Tatge, 1956) (Pelsonian); Paragondolella bulgarica Budurov and Stefanov, 1975 (Bithynian–Pelsonian); P. hanbulogi (Sudar and Budurov, 1979) (Pelsonian–Illyrian); and Gladigondolella sp. A. (Fig. 2b). Several new species were established: Paragondolella hirschii n. sp. Kılıç and Budurov, P. praecornuta n. sp. Kılıç, Budurov, Petrunova and Mirăuţă, and P. ebruae n. sp. Kılıç.

    Examining Gondolellid conodont communities reveals both ontogenetic and phylogenetic features that provide an understanding of evolution throughout time. During our research, we were able to substantiate Mosher's (1968) claim of the derivation of the genus Paragondolella from a Neospathid lineage.

    The elongation of the Neospathid morph (Triassospathodus homeri) at the end of the Spathian generated a new lineage. This lineage, initiated by Chiosella timorensis, persisted until the end of the Triassic. The lineage of Paragondolella (aegaea-bulgarica- excelsa-foliata-inclinata) during the Middle Triassic consists of relatively unchanged Gondolellid morphs. Iteration, however, of Neospathid forms occurs in the higher Lower Anisian (Nicoraella).

    This study could not have been completed without the guidance, support and expertise of the late Prof. Kiril Budurov, and I wish to dedicate this paper to his memory.

  • Within this work over 950 samples were collected. All samples were digested in acetic acid. The insoluble residue was washed and fractioned by sieving. Figured specimens are housed in the Department of Geological Engineering, Faculty of Engineering, Balikesir University, Balikesir, Turkey. Suprageneric classification follows Donoghue et al. (2008).

    Only samples taken from South of Gebze, considered stratigraphically important to this study are listed. Other marine faunas, which include foraminifers, ostracods, scolecodonts, radiolaria, fish teeth and plates, shark teeth, radulae, holothurian sclerites, crinoids, and ichthyosaur pelvic remains, are not yet fully processed. Only part of the SEM of study of conodonts, collected from the other parts of the peninsula, is complete. The most important conodont results are used (e.g., presence of late Aegean–middle Illyrian limestones in the Tepeköy Formation) and the other fossil data will be presented later.

  • The Triassic sequence of the Kocaeli Peninsula starts transgressively and closes regressively. The sequence is subdivided into six formations and six members that represent lower to late Triassic (probably Norian). We adhere to the nomenclature of the Stratigraphic Committee of Turkey (Tüysüz et al., 2004).

    The sequence starts with the barren Kapakli Formation that resembles the underlying red Permian facies. The first marine sediments are the Induan Erikli Formation. The Olenekian Demirciler Formation consists of micritic and dolomitic bioturbated clayey limestone. The Olenekian Ballikaya Formation consists of dolomite, dolomitic limestone and limestone that represent the passage to the Earliest Anisian. Above a probable unconformity follows the Tepeköy Formation that consists of four different lithologies in ascending order: (ⅰ) Kücükburun Member consisting of grey nodular limestone (Anisian); (ⅱ) Kusca Member of ammonitico rosso red nodular limestones (Ladinian-?Early Carnian); (ⅲ) the Koytepe Member consisting of shale with Halobia and grey-green marls (Carnian); (ⅳ) Bakirlikiran Member of plant bearing sandstone that laterally passes into the Cerkesli Formation, which only occurs in the Cerkesli region and consists of pebbly limestone and reef- limestone. This unit is the lateral equivalence of the upper Tepeköy Formation. The name Kazmali Formation has also been used for the two lower members by Tüysüz et al. (2004).

    The Kocaeli Triassic comprises a complete sequence of the Anisian stage, including the type section of the Lower Anisian Bithynian substage (Assereto, 1974, 1972) (Fig. 2a).

  • Class Conodonta Pander, 1856

    Order Ozarkodinida Dzik, 1976

    Superfamily Gondolelloidea Lindström, 1970

    Family Gladigondolellidae Ishida and Hirsch, 2011

    Genus Gladigondolella Müller, 1962

    Type species Polygnathus tethydis Huckriede, 1958

    Figs. 4.19, 6.1–6.11

    Figure 3.  3.1–3.7, 3.9–3.28. Paragondolella bulgarica Budurov and Stefanov. KTM3 and KTM4 sections: 3.1–3.3. KTM3-9861; 3.5–3.6. KTM3-9874; 3.10. KTM3-9883; 3.4, 3.9, 3.11, 3.13, 3.17. KTM3-9891; 3.7. KTM3-0144; 3.12, 3.14. KTM4-0150; 3.16, 3.22. KTM4-0154; 3.15, 3.18, 3.19, 3.23. KTM4-0158; 3.20, 3.21. KTM4-0160; 3.23. KTM4-0171; 3.24. KTM4-0172; 3.25. KTM4-0175; 3.26. KTM4-0177; 3.27. KTM4-0180; 3.28. KTM4-0191; 3.29. KTM4-0198; 3.8. Nicoraella kockeli (Tatge), KTM4/3-0221.

    Figure 4.  4.1–4.10. Paragondolella hirschii n. sp. Kılıç and Budurov. KTM3 and KTM4 sections: 4.1, 4.2. KTM4-0144 (holotype); 4.3, 4.6. kept in Bulgarian Academy of Sciences; 4.4, 4.5. KTM3-9891; 4.7, 4.8. KTM4-0150; 4.9, 4.10. KTM4-1054; 4.11–4.18. Paragondolella praecornuta n. sp. Kılıç, Budurov, Petrunova, Mirăuţă; 4.11, 4.15 are from Gedik (1975; pl. 1 figs. 10, 11); 4.12, 4.13, 4.17 kept in Bulgarian Academy of Sciences; 4.14, 4.16. KTM4-0154 (holotype); 4.18. KTM4-0180; 4.19. Gladigondolella sp. A, KTM4-0144; 4.20–4.21, 4.24–4.25. Cornudina oezdemirae Gedik; 4.20. KTM3-9801; 4.21. KTM3-9811; 4.24. KTM3-9824; 4.25. KTM3-9829; 4.22. Neostrachanognathus tahoensis Koike, KTM3-9841; 4.23. Cornudina cf. latidentata Kozur and Mostler, KTM3-9832. Figs. 5.20–5.25 were also used in Kılıç et al. (2018b).

    Figure 5.  5.1–5.2, 5.5–5.6. Chiosella timorensis (Nogami). KTM3 and KTM5 sections: 5.1, 5.2. KTM3-9832; 5.5. KTM3-9841; 5.6. KTM3-9857; 5.7. Neogondolella sp., KTM5-98931; 5.3–5.4, 5.8–5.9. Paragondolella hanbulogi (Budurov and Stefanov), KTM5-98893; 5.10–5.15. Paragondolella aegaea (Bender); 5.10, 5.13. KTM3-9832; 5.12. KTM3-9841; 5.11. KTM3-9861; 5.14. KTM3-9879; 5.15. KTM3-9849; 5.16, 5.19–5.21. P. ebruae n. sp.; 5.16, 5.19. KTM3-9861 (holotype); 5.20. KTM3-9878; 5.21. KTM3-9883; 5.17, 5.18. Paragondolella sp. A, KTM3-9891.

    Description: Gondolelloid platform conodont element with a basal blade and a keel, extending over the entire element. The amygdaloid basal cavity is not terminal, being a little farther away from the posterior end, with a posterior keel developed. The platform varies in width from a mid-lateral rib to a wide, flat platform, and a free blade in some species.

    Gladigondolella tethydis radiated in the Tethys area from Anisian to Julian. In the course of the Middle Triassic G. malayensis evolved from G. tethydis through expansion of the platform.

    Stratigraphic range: Gladigondolella ranges from the end of the Early Triassic to the late early Carnian; the genus consists of the Spathian G. carinata, Anisian–Julian G. tethydis and late Ladinian–early Carnian G. malayensis. The present unique specimen can only be determined as G. sp. A.

    Gladigondolella tethydis (Huckriede, 1958)

    Figs. 6.1–6.11

    Figure 6.  Gladigondolella multielement apparatus (lacking P1 element). 6.1, 6.12. Ozarkodinid P2 element; 6.2. Prioniodinid S2 element; 6.3, 6.4. Roundyid S0 element; 6.5. Anastrophognathid S0 element; 6.7, 6.8. Lonchodinid M element; 6.6, 6.9–6.11. Prioniodinid S elements; 6.1, 6.5. KTM4-0150; 6.2, 6.6, 6.9. KTM4-0158; 6.3, 6.4. KTM4-0172; 6.7. KTM4-0191; 6.8. KTM4/2-0206; 6.10. KTM4/2-0209; 6.11. KTM5-98901; 6.12. KTM5-98929.

    1958    Polygnathus tethydis n. sp.; Huckriede, pl. 12, figs. 38a, 38b; pl. 13, figs. 2–5

    1960    Polygnathus tethydis; Spasov and Ganev, p. 85, pl. 1, figs. 26, 27; pl. 2, fig. 16.

    1960    Polygnathus tethydis; Budurov, p. 117, pl. 2, figs. 28–30, 33.

    1965    Polygnathus tethydis; Mosher and Clark, p. 563, pl. 66, fig. 13.

    1966 Gladigondolella tethydis; Ishii and Nogami, pl. 1, figs. 1, 2.

    1968    Gladigondolella tethydis; Nogami, p. 123, pl. 9, figs. 1–10; pl. 11, figs. 5, 6.

    1968 Gladigondolella tethydis; Mosher, p. 937, pl. 116, figs. 1, 2, 5, 8.

    1969    Gladigondolella tethydis; Hirsch, Pl. 1, figs. 1–3.

    1970    Gladigondolella tethydis; Bender, p. 505, pl. 2, figs. 2–6.

    1973 Gladigondolella tethydis; Budurov, p. 802, pl. 1, figs. 4–7.

    1975 Gladigondolella tethydis; Gedik, p. 120, pl. 3, figs. 15–17.

    1984   Gladigondolella tethydis; Farabegoli et al., fig. 4, part e.

    1992   Gladigondolella tethydis; Kozur and Mostler, pl. 2, figs. 19, 20.

    2001   Gladigondolella tethydis; Orchard et al., pl. 1, figs. 20, 21.

    2007a    Gladigondolella tethydis; Orchard et al., fig. 6, part 35.

    2007b    Gladigondolella tethydis; Orchard et al., fig. 5, parts 29, 30.

    2015    Gladigondolella tethydis; Lehrmann et al., fig. 6, parts 26, 27.

    2016    Gladigondolella tethydis; Karádi and Dulai, fig. 2.

    2019a    Gladigondolella tethydis; Chen et al., fig. 5, parts 5a–5c.

    Remarks: In the multielement apparatus of Gladigondolella tethydis, platform and non-platform elements occur usually in a 1 : 4 ratio. But in the Kocaeli Triassic, this ratio does not apply; only ramiform elements were recovered. Among the ramiform elements found, Kılıç (2004) regarded Anastrophognathus sagittalis as S0 element in addition to Roundya (Hibbardella) magnidentata. Other elements recovered include Cratognathodus kochi, Cypridodella (Lonchodina) spp. and Prioniodina spp..

    Differing not merely in appearance at the level of P1 (platform), each element of the apparatus is morphologically distinct from its correspondent element in Gondolellidae. The multi- element widely corresponds with one of the "conodont sets" that Huckriede (1958) first observed in the Alps. In the reconstruction of an octomembrate Gladigondolellid apparatus, Hirsch (1994) regarded Cratognathodus kochi as an additional ozarkodiniform element, next to Ozarkodina saginata. In Ishida and Hirsch's (2011) view, the elements of the Gladigondolellid apparatus consist of the discrete forms Gladigondolella tethydis (P1), Ozarkodina saginata (P2a), "Cratognathodus" kochi (P2b), Lonchodina venusta (M), Roundya lautissima (S0), an enantiognathid (pars petrae-viridis sensu Koike, 1999) (S1), Lonchodina spengleri (S2), Enantiognathus petrae-viridis (S3) and Hindeodella multihamata (=H. pectiniformis) (S4).

    The position of the cratognathodiform element in the Gladigondolellid apparatus remains debatable. Koike (1999, p. 236) recalls the statement of Kozur and Mostler (1972, p. 19) that the so-called Cratognathodus pectiniform element (P1) is an immature Gladigondolella.

    Koike (1999) regards the cratognathodiform element as the P1 element of the octomembrate species Cratognathodus multihamatus, whose other elements are supposedly Gladigondolellid. According to Orchard (2005), Gladigondolella and Cratognathodus are multi-element genera of Gladigondolellinae Hirsch 1994. Kolar-Jurkovšek et al. (2005) held the P1 element of the genus Cratognathodus for a cavital neospathodiform. This calls to mind a phylogenetic relationship between Cratognathodus and Gladigondolella of the kind that exists within the lineage of alternating neospathodiform and paragondolelliform taxa, sensu Hirsch (1994). In Orchard (2005), the Cratognathodus multi-element from the Spathian of Oman shows transitional features with gondolellid elements, suggesting the possible early Gladigondolellid phylogeny from a neospathodiform stock. However, Gladigondolella saginata, from the Spathian of Chios, has a cratognathodiform element.

    Koike (1999, p. 237–238, fig. 2) based his generic segregation of Cratognathodus from Gladigondolella on the apparently low correlation coefficient of their occurrence within the Taho Formation of SW Japan. Here, Cratognathodus multihamatus occurs in the early Anisian Timorensis Zone and G. tethydis covers the late Anisian (Bulgarica Zone), while they occur together in the early Carnian (Nodosus Zone). On the other hand, in the late Anisian to late Ladinian Schreyeralm Formation of the Feuerkogel Section (northern Calcareous Alps, Austria), Mosher (1968, p. 913, table 2) recorded high ratios of both Cratognathodus kochi and G. tethydis at several levels. Similar ratios occur within the samples of Nogami (1968) and Koike (1982) from Malaysia. Therefore, in our opinion, the steady distribution of ozarkodiniform P2a and cratognathodiform P2b elements in samples containing the Gladigondolella apparatus strongly suggests the coeval nature of these forms alternating in the same apparatus-position of distinct multi- element sets. In a similar case, Lambert et al. (2007) interpreted distinctive dimorphic characters in detail of the P2 element of Jinogondolella, a Middle Permian gondolellid in which an asymmetric pair or two complete pairs may represent different individuals, as indicating sexual dimorphism.

    Koike (1999) proposed an octomembrate Cratognathodus apparatus of 15 elements; the single pairs of segminate P1, angulate P2, breviform digyrate S2, extensiform digyrate S2, bipennate S3, and S3 elements, and a single unpaired alate S1 element. P1 elements characterized by relatively broad cusp with expanded basal cavity and large discrete denticles. Mosher (1968) established the genus Cratognathodus, including four form species: Prioniodina kochi Huckriede, Cratognathodus posterognathus and two unidentified species, which are both characterized by the presence of a strong broad cusp with a widely expanded basal cavity, and relatively small number of discrete denticles. Cratognathodus kochi and C. posterognathus are respectively identical with the P1 and P2 elements of the C. multihamatus apparatus. Among three specimens illustrated as C. kochi by Mosher (1968), one specimen (pl. 113, fig. 4) is not a typical P1 element of the C. multihamatus apparatus. Mosher (1968), however, regarded the form species Prioniodina kochi Huckriede as the type species of his genus Cratognathodus. Kozur and Mostler (1972) claimed that the genus Cratognathodus created by Mosher (1968) is not a valid taxon because the holotype and all other specimens previously described as the form species C. kochi are immature forms of the "gladigondolelliform" P1 elements of Gladigondolella tethydis (Huckriede). Based on Koike's (1999) observation on P1 elements of G. tethydis from the Taho Formation and other limestone formations in Japan, the immature forms of the element are characterized by a narrow platform-like anterior process and gradually increasing denticles in length toward the anterior as observed in the mature forms. The immature forms of the P1 elements of G. tethydis can be, therefore, easily distinguished from the form species Cratognathodus kochi. The P1 element of C. multihamatus represents various features in the shape and size of the cusp and denticulation on the anterior process. The holotype of the form species C. kochi (Huckriede, pl. 2, fig. 11) possessing a short broad cusp and subequal denticles is safely assigned within the range of morphologic variation of the P1 element of C. multihamatus and agrees well with the specimens illustrated in Koike (1999, figs. 3, 16, 26).

    Stratigraphic range: Aegean (Anisian)–Julian (Carnian) of Turkey, Austria, Romania, Bulgaria, Greece, China, USA and Canada.

    Gladigondolella sp. A

    Fig. 4.19

    Type locality: Kocaeli Peninsula (Turkey), between Orta Dere and Kurt Dere.

    Type stratum: Upper part of Kücükburun Member of Tepeköy Formation, sample KTM3-0144.

    Age: Early Pelsonian.

    Diagnosis: The massive platform of the P1 element is thick, flat-shaped, bilaterally convex and symmetrical. Keel is elevated and elongated with narrow amygdaloid basal pit in the posterior third of the unit. Linear carina with at least a dozen triangular, rather low denticles. Straight basal margin. Apparatus similar to that of Gladigondolella tethydis.

    Comparisons: The carina of Gladigondolella sp. A is higher and more fused than that of most other species of Gladigondolella. The platform is also wider than that of G. carinata or G. arcuata.

    Material: One single P1 element. Gladigondolellid elements are very abundant in sample KTM3-0144 and are likely to belong to this species.

    Occurrence: Limited to the Kücükburun Member of the Tepeköy Formation (Kocaeli Peninsula, NW Turkey).

    Family Gondolellidae Lindström, 1970

    Subfamily Neogondolellinae Hirsch, 1994

    Genus Neogondolella, Bender and Stoppel, 1965

    Type species Gondolella mombergensis Tatge, 1956

    Original diagnosis (Bender and Stoppel, 1965, p. 243): The holotype of the type species is unornamented segminiplanate P1 element with a strong, partly fused carina of variable height ending in a commonly pronounced (sub)terminal cusp. Neogondolella was introduced for smooth forms that had formerly been included in Gondolella Stauffer and Plummer (Bender and Stoppel, 1965, p. 243; after Orchard, 2005).

    Diagnosis: Narrow and long, slightly asymmetric platform; broadest near the middle and gradually narrowing towards both ends. A posterior platform constriction may be present. Blade with 8–16 anteriorly fused denticles, which decrease rapidly in height. The carina is lowest in the middle of the element, and rises again towards the posterior. At the posterior end, the cusp may be terminal or a posterior denticle may be present. Strongly elevated basal field occupies the lower side. Pit, surrounded by a small, rectangular loop, located below the cusp and near the posterior end. Narrow and high keel.

    Remarks: The multielement Neogondolella apparatus has been reconstructed by Orchard and Rieber (1999), and further examples are given by Orchard (2005) with modifications by Goudemand et al. (2011). In the paper by Orchard (2007), the apparatus described as "Neogondolella inclinata" is now referred to as N. liardensis. The multielement apparatus of Neogondolella is characterized by the presence of an S4 element with a bifurcated anterior process, and an S0 element whose anterior processes bifurcate either at the cusp, or several denticles to the anterior.

    Stratigraphic range and occurrence: Austria, Bulgaria, Turkey, Germany, Hungary, Japan, Nevada (USA), Slovenia, Southern Alps, Spain and Canada. Middle upper parts of the Illyrian to lower parts of the Fassanian; in terms of ammonoid zonation corresponds to the upper part of the trinodosus Zone to curionii Zone. The range extends back as far as Spathian in North America.

    Neogondolella sp.

    Fig. 5.7

    Remarks: Narrow, lanceolate platforms with weakly fused denticles that increase in size to the posterior, culminating in a large, terminal cusp are often assigned to N. cf. haslachensis (Tatge), the original stratigraphic range and occurrence of which is the Fassanian (early Ladinian) Upper Muschelkalk (Zone 4) in Germany (Franz et al., 2015). The present specimen is possibly a juvenile P1 element.

    Genus Nicoraella Kozur, 1980

    Type species Ozarkodina kockeli Tatge, 1956

    Fig. 3.8

    Remarks: A large blade, no platform, and a large gondolelloid basal groove with a large "cavital" pit characterises the Late Permian–Early Triassic Neospathid lineage, from which the Anisian Gondolelloid conodonts derive.

    The two Nicoraella species, N. germanica and N. kockeli (Kozur and Mostler, 1972; Tatge, 1956) are index fossils of the upper Bithynian and the Pelsonian.

    It is difficult to ascertain common homeomorphy in conodonts, including in the genus Neospathodus (Clark et al., 1981). It is useful to recognize the appearance of the successively distinct looking proteromorphs in its phylogeny, using distinct genera, as e.g. Neospathodus (Clark et al., 1981), Merrillina Kozur, Nicoraella Kozur, Mosherella Kozur, Neocavitella Budurov and Sudar, Misikella Kozur and Mock, all belonging in the same Darwinian anagenesis, each of them representing the successive atavistic reversals that took place over time. The rather punctuated reappearances of Neospathid morphs at certain intervals during the Middle and Late Triassic are atavistic reversals, interpretable as environmental stress-related retrogradations (Kılıç et al., 2018a).

    Partial reconstructions of Nicoraella have been attempted by Kozur and Mock (1991), Kozur (1993), Kolar-Jurkovšek et al. (2005), Sun et al. (2009), Kolar-Jurkovšek and Jurkovšek (2010) and Chen et al. (2019a). These studies differed in their identification of S4 elements, and were conflicting in their interpretation of the morphology and presence of a P2 element. The discovery of fused clusters of Nicoraella from South China has enabled the resolution of many of these issues (Huang et al., 2019a, b). The Nicoraella apparatus has been demonstrated to possess an alate S0 element, breviform digyrate S1, S2 and M elements, bipennate S3 and S4 elements, and a carminate P2 element in addition to the distinctive P1 element.

    Occurrence: Higher lower Anisian (upper Bithynian, Anagymnotoceras ismidicus Zone) to the top of the Pelsonian (top of the Balatonites balatonicus Zone).

    Nicoraella kockeli (Tatge, 1956)

    Fig. 3.8

    1956    Ozarkodina kockeli n. sp.; Tatge, p. 137, pl. V, figs. 13, 14.

    1960    Ozarkodina kockeli; Budurov, p. 16, pl. V, figs. 15–18.

    1975    Neospathodus kockeli; Gedik, p. 137, pl. IV, figs. 18, 19.

    1975    Neospathodus kockeli; Trammer, pl. XXII, figs. 1–3.

    1975    Neospathodus cf. N. kockeli; Hirsch, p. 94–96, pl. 1, figs. 1–4.

    1980    Nicoraella kockeli (Tatge); Kozur, p. 127.

    1992    Nicoraella kockeli; Kozur and Mostler, pl. 2, fig. 5.

    1999 Nicoraella cf. kockeli; Narkiewicz, pl. 1, fig. 3.

    2009    Nicoraella kockeli; Zhang et al., fig. 3, part 12.

    2010    Nicoraella kockeli; Götz and Gast, fig. 3, part 2.

    Description: The P1 elements of Nicoraella kockeli have a large blade with up to six denticles, which increase in size posteriorly to the large, sub-terminal cusp. A short posterior process bears only one or two denticles, much shorter than the cusp. In lateral view, these denticles are posteriorly inclined. Basal cavity is large and elliptical.

    Material: 12.

    Occurrence in Kocaeli: Pelsonian; KTM4/2 and KTM4/3 measured stratigraphic sections.

    Stratigraphic Range and Occurrence: Pelsonian of Germany, Poland, Turkey, Greece, Israel, Nevada, China.

    Genus Paragondolella Mosher, 1968

    Type species Paragondolella excelsa Mosher, 1968

    Figs. 3.1–3.28; 4.1–4.18; 5.3, 5.4, 5.8, 5.9, 5.16–5.21

    Diagnosis: The species of Paragondolella have a platform that is rounded or blunt at the posterior end, while the anterior end has a short free blade measuring 1/5 to 1/3 of the total length of the unit in adult specimens. The denticles of the blade are fused to two-thirds of their height, commonly forming a curve in their lateral outline, ending in one, sometimes two, free, low, and conical to node-like denticles. Platform margins are quite thick, may be upturned or flat, and are often sculptured (Budurov and Sudar, 1990) but never bear any nodes. The lower side of the species belonging to Paragondolella is characterized by a shallow basal groove or keel that is wide open, broad or narrow, the end of which may be pointed, squared or rounded, but never bifurcated (Orchard, 2013). The basal field ends in a gently rounded loop that may also vary from rectangular-angular to even sub-triangular. The subterminal to backward shifted pit, according to the original diagnosis of Mosher (1968), is wide but shallow, with no protruding edges above the level of the basal field, or loop.

    Remarks: Mosher (1968), Orchard (2013), Golding et al. (2014) and Chen et al. (2016) emphasized the high-crested blade-carina that characterizes all growth stages of this genus as typified by its Middle Triassic type species Paragondolella excelsa. The relatively flat, oval platform is a distinctive feature of P. excelsa, that is not exhibited by some other Middle Triassic species such as P. hanbulogi. Likewise, the distinctive polygonal basal pit seen in adult specimens of Paragondolella is seen in many conodont genera throughout time and is therefore not diagnostic. Many Late Carnian species have been referred to as Paragondolella (e.g., Mazza et al., 2012; Rigo et al., 2007; Kozur, 2003), as the subterminal basal pit precludes their assignment to Metapolygnathus (contra Orchard, 1991a, b; Hayashi, 1968). However, Orchard(2014, 2013) instead referred these late Carnian species to a variety of new genera including Parapetella and Quadralella. The absence of the elements belonging to the Paragondolella multielement apparatus (Orchard, 2005) in the late Carnian is evidence that this genus was restricted to the Middle Triassic and lowest Carnian (Chen et al., 2016; Orchard, 2007).

    Comparisons: Objecting to Mosher's (1968) statement that the earliest growth stages in Paragondolella lack a platform, Kozur and Mostler (1971) claimed that this is also the case in the earliest growth stages of Neogondolella mombergensis, the type species of Neogondolella. Sweet pointed out that Paragondolella has morphologic characters indistinguishable from those of Neogondolella (Klapper et al., 1973; Sweet, 1970). Nicora (1977) considered the genus Paragondolella as a junior synonym of Neogondolella. However, Paragondolella differs from the genus Neogondolella by the tendency of developing a free blade. Additionally, it has a higher, arched carina, a deeper basal pit, and a broad basal field and a narrow loop that is commonly sub-rectangular.

    Stratigraphic range and occurrence: Anisian to lower Carnian of Austria, Hungary, Poland, Italy, Turkey, Slovenia, Croatia, Bulgaria, Greece, India, China, Japan, British Columbia (Canada), and Nevada (USA).

    Paragondolella aegaea (Bender 1970)

    Figs. 5.10–5.15

    1970    Neogondolella aegaea Bender, p. 516, pl. 3, figs. 21–26; pl. 4, fig. l.

    1975    Neogondolella aegaea Gedik, p. 31, pl. 2, figs. 1–11.

    Description: A species with a high carina and a narrow, thin platform. The first two thirds of the unit are straight, only the rear part is slightly bent down. The carina consists of high, laterally compressed and largely fused denticles, which are almost vertical at the proximal end and increase in inclination towards the back. The last or penultimate denticle is generally slightly larger than the others and should be the main denticle. It is almost straight, only towards the end can it be slightly curved to the side.

    The platform tapers to the front of the carina; it reaches its maximum width towards the end of the second third of its length. It is thin and almost straight, its edges are hardly rolled up, so that the surface of the carina and the surface of the platform are almost perpendicular to each other. On the outside it extends a little further back than on the inside, where it usually stops at the main denticle, only rarely does it go beyond the end of the carina.

    The keel, especially in juvenile specimens, is pedestal-like and is traversed by a furrow which at the end, under the main denticle, widens into a triangular and relatively large basal pit.

    Remarks: According to Bender (1970), this form is derived from Spathognathodus gondolelloides Bender, 1970, which appears to be a more recent synonym of Neospathodus timorensis (Nogami, 1968). On the other hand, it leads to Neogondolella unilobata above, with which it is connected by transitional forms. It can be easily distinguished from all other Neogondolella species by its high, fused carina.

    Kozur and Mostler (1972, p. 787), put the lower limit (First Appearance Datum, FAD) of Gondolella? aegaea in the early Anisian (Lenotropites caurus- and Anagymnotoceras varium Zone). Important conodont species in the aegaea zone are "Gondolella" timorensis that still occurs at the immediate base of the zone and Gladigondolella tethydis that appears in the upper Spathian. Since 1968 there were reprints of Benderʼs work dated 1967. The volume appeared in 1970 (Kozur and Mostler, 1972, p. 780).

    Since Kozur (1980), the taxon aegaea has been replaced by Neogondolella regale, a species that was established in North America by Mosher (1970) in the subrobustus, caurus and varium zone. Mosher (1970) also referred more evolved forms to N. regale that are thinner, have a free blade and an upturned platform that surrounds the terminal denticle. Doing so, Mosher (1970) gave a very loose definition of the species, allowing considerable morphologic latitude in topotypic specimens. Nicora (1977) noted however that some older specimens (from the subrobustus Zone) differ substantially from Anisian specimens by having a large, flat platform and a lower carina, and should be referred to as another genus (Goudemand et al., 2012). To this species, also belongs Neogondolella mombergensis, in Mosher (1968; p. 937, pl. 116, fig. 15).

    Recently, the genus Magnigondolella (Golding and Orchard, 2018) was introduced to encompass Anisian conodonts previously referred to as Neogondolella regalis (Mosher, 1970). The new genus shows a wide variety of platform morphologies, including Spathian forms within its range. The Spathian collections in North America suggest that the genus Magnigondolella does originate in the Early Triassic, with a possible ancestry in Borinella. On the other hand, the early Anisian Paragondolella aegaea, in Kocaeli, does only show resemblance to species identified in North America (Dr. Martyn Golding, personal communication, September 2020). In Nevada (USA), British Columbia (Canada), and possibly Svalbard, M. regalis extends from Spathian to Bithynian.

    Material: 66 specimens.

    Paragondolella praecornuta n. sp. (Kılıç, Budurov, Petrunova and Mirăuţă)

    Figs. 4.11–4.18

    1972   Neogondolella cornuta n. sp.; Budurov and Stefanov, p. 839–840, pl. 3, figs. 9–15, 20–22

    1975   Neogondolella cf. huckriedei Budurov and Sudar; Gedik, p. 20, pl. 1, fig. 4

    1975   Neogondolella unilobata n. sp.; Gedik, p. 20, pl. 1, figs. 10–11

    Derivation of name: Because of stratigraphic precedence and morphological resemblance with Neogondolella cornuta Budurov and Stefanov, 1972.

    Holotype: The specimen shown on Figs. 4.14 and 4.16 denoted as KTM3-0154 (kept in Department of Geological Engineering, Faculty of Engineering, Balikesir University; Figs. 4.12, 4.13, 4.17 kept in Bulgarian Academy of Sciences; Figs. 4.11 and 4.15 are from Gedik, 1975, pl. 1, figs. 10, 11).

    Type locality: Southern part of the Kocaeli Peninsula (Turkey). KTM3 measured stratigraphic section.

    Type stratum: Dolomitic limestone bed, Kocaeli Peninsula; KTM3 measured stratigraphic section, sample KTM3-0154.

    Diagnosis: Specimens referred to as Paragondolella praecornuta n. sp. are conspicuously bowed laterally and bilaterally symmetrical. The major feature of this species is its long free anterior blade. The platform is typically confined to the posterior half of the unit, and is up-curved marginally. The carina carries a series of fused denticles that increase in length and width towards the anterior end of the free blade. The cusp, which is the posterior denticle at all growth stages, is broad, separate, inclined, and circular in transverse section.

    Description: Paragondolella praecornuta n. sp. is characterized by a straight or slightly curved element and an isolated posterior cusp. The short posterior platform that completely surrounds the terminal cusp has slightly raised edges and a weak pre-terminal constriction. The carina has more than 12 denticles, the anterior 4–5 being free and massive, while the cusp is free, tall, slightly backwards inclined or upright. The basal groove widens posteriorly and the terminally located pit is small.

    Material: More than 100 specimens from the KTM3 measured stratigraphic section, Kocaeli Peninsula (Turkey, collection AMK), and from the Golobardo Section (Bulgaria, collection KB).

    Stratigraphic range and occurrence: Paragondolella praecornuta n. sp. is uncommon in the lower part of the Pelsonian (early late Anisian) to Illyrian of Turkey and Bulgaria.

    Paragondolella hanbulogi Sudar and Budurov, 1979

    Figs. 5.3, 5.4, 5.8, 5.9

    1979    Paragondolella hanbulogi n. sp.; Sudar and Budurov, p. 50, 51, pl. 1, figs. 9, 10; pl. 2, figs. 1–9; pl. 3, figs. 1–12.

    1984    Gondolella hanbulogi; Farabegoli et al., fig. 4, part e; fig. 5, part c.

    1987   Neogondolella hanbulogi; Dagys, p. 10, pl. 2, figs. 6, 7.

    1999   Paragondolella hanbulogi; Meco, pl. 1, figs. 3, 4.

    1999   Paragondolella cf. hanbulogi; Narkiewicz, pl. 1, figs. 5, 6.

    2000   Paragondolella hanbulogi; Márquez-Aliaga et al., figs. 6, 3–4.

    2003    Gondolella hanbulogi; Kovács, pl. C-4, parts 1–5; pl. C-5, part 7; pl. C-8, parts 1–4.

    2016    Paragondolella hanbulogi; Karádi and Dulai, fig. 3.

    Description: The platform is flat, broadest in the middle and with rounded posterior end. The thin to slightly thickened platform edges gently bend upwards, giving the unit its characteristic flat outline. The anterior blade rises up sharply. The carina has about 16 fused denticles, except for their free tips. The narrow basal field ends in a small, rectangular loop that meets the keel at an obtuse angle (Márquez-Aliaga et al., 2000).

    Remarks: Transitional features have been observed in some specimens of Paragondolella hanbulogi from Turkey. Some specimens suggest a transition from P. bulgarica, by the slight inclination of the cusp and a more angular outline of the posterior platform end; and others suggest a transition to P. excelsa, by the larger rounded loop and basal groove.

    Discussion: The narrow platform and high carina of Paragondolella suggest its possible evolutionary derivation from Chiosella, although there is a stratigraphic gap between the genera (Chen et al., 2016). The small and rectangular- shaped loop and narrow platform also resemble that of Neogondolella, whereas the high carina is similar to that of Magnigondolella; derivation of Paragondolella from either of these genera is also possible.

    Stratigraphic range and occurrence: Pelsonian to middle Illyrian (upper half of the balatonicus Zone to trinodosus Zone). Bulgaria, Turkey, Hungary, Slovenia, Albania, Austria, southern Alps and Spain (CCR).

    Paragondolella bulgarica Budurov and Stefanov, 1975

    Figs. 3.1–3.7, 3.9–3.28

    1975   Paragondolella bulgarica Budurov and Stefanov; in Budurov and Stefanov, June 1975, pl. 1, figs. 1–23.

    1975    Neogondolella unilobata Gedik; in Gedik, August 1975; pl. 1, figs. 9–25.

    1980    Paragondolella bulgarica; Budurov, p. 773, pl. 57, fig. 12.

    1980    Gondolella bulgarica; Kozur, table 2, figs. 1, 2.

    1980    Neogondolella bulgarica; Pisa et al., p. 817, pl. 61, figs. 1, 2, 3, 5, 7.

    1984    Gondolella bulgarica; Farabegoli et al., fig. 4, parts a, b.

    1992    Paragondolella bulgarica; Kozur and Mostler, pl. 1, figs. 13–15; pl. 2, figs. 4, 15.

    2000    Paragondolella bulgarica; Márquez-Aliaga et al., fig. 6, parts 1–2.

    2003    Gondolella bulgarica; Kovács, pl. C1, parts 1–6; pl. C2, parts 1–4; pl. C3, parts 1–3.

    2006    Paragondolella bulgarica; Sun et al., p. 626, pl. 1, figs. 16, 17.

    2010    Paragondolella bulgarica; Götz and Gast, fig. 3, part 3.

    2015    Paragondolella bulgarica; Lehrmann et al., fig. 6, parts 6–8.

    Original diagnosis (Budurov and Stefanov, 1975): "Platform strongly curved; high curved blade with denticles; narrow grooved keel with a small, prominent basal pit."

    Description: The medium-wide platform has slightly upturned margins and honey-comb ornamentation. The high carina bears 15–20 almost discrete denticles, with at least a third of the length of the denticles being free. The last denticle is higher, sharp and inclined toward the posterior end. The posterior and anterior ends of the element are downturned to produce the high arched shape. On the lower side, a narrow grooved keel ends at the basal pit, which is small, rounded and located posteriorly. The platform tapers posteriorly where often it is upturned and appears as a denticle in lateral view. The species always shows a free blade that is characterized by 2 to 4 elliptical, laterally compressed denticles (Marquez-Aliaga et al., 2000; Nicora, 1977; Budurov, 1975).

    Comparison: With its free blade and well-developed posterior platform, the more curved Paragondolella bulgarica differentiates itself from the straight profiled carina and more massive platform in species of Magnigondolella.

    Material: Over 300 specimens from KTM3 and KTM4 sections.

    Stratigraphic range and occurrence: P. bulgarica marks the base of the Bithynian and ranges up into the Pelsonian, disappearing before the base of the Illyrian. P. bulgarica is very abundant in the Kocaeli Peninsula. It occurs also in Bulgaria, Hungary, Slovenia, Spain, China and N. America.

    Paragondolella hirschii n. sp. Kılıç and Budurov

    Figs. 4.1–4.10

    Derivation of name: Dedicated to Prof. Dr. Francis Hirsch (Naruto, Japan) for his outstanding work on Triassic conodonts and stratigraphy.

    This species was established after intensive discussion with late Prof. Kiril Budurov.

    Holotype: The specimen shown in Figs. 4.1 and 4.2 (kept in Department of Geological Engineering, Faculty of Engineering, Balikesir University).

    Type locality: South of Gebze, between the Orta Dere and the Kurt Dere.

    Type stratum: KTM3 measured stratigraphic section. From the sample KTM3-9891 (kept in Department of Geological Engineering, Faculty of Engineering, Balikesir University).

    Diagnosis: Platform conodont; the carina bears small and thin fused denticles, the 4 to 5 anterior denticles of the carina being prominent. The main cusp is a strong and isolated denticle at the posterior-end of the platform.

    Remarks: The carina of this platform conodont bears small and thin fused denticles, the 4 to 5 anterior denticles of the carina being prominent. The main cusp is a strong and isolated denticle at the posterior-end of the platform.

    Material: 186 specimens, from Gebze (Turkey) and from the Golobardo Mountains (Bulgaria).

    Occurrence: Turkey and Bulgaria.

    Stratigraphic range and occurrence: Early Pelsonian (Anisian) of Turkey and Bulgaria.

    Paragondolella ebruae n. sp. Kılıç

    Figs. 5.16, 5.19–5.21

    Derivation of name: Dedicated to the author's wife, Geological Engineer Ebru Kılıç.

    Holotype: The specimen shown in Figs. 5.16, 5.19 (kept in Department of Geological Engineering, Faculty of Engineering, Balikesir University).

    Type locality: South of Gebze, between Orta Dere and Kurt Dere.

    Type stratum: KTM3 measured stratigraphical section, from sample KTM3-0160.

    Diagnosis: The platform element of this species has a carina that bears big and fused denticles, characteristically with 3 to 4 large, broad denticles located anterior of the two most posterior denticles. In lateral view the unit is clearly arched. The platform margins are slightly upturned, and much of the upper surface of the platform has a polygonal ornamentation.

    Comparison: The species is similar to Paragondolella bulgarica in its lateral view but differs by the irregular shape of its carina, with denticles increasing and decreasing in height along its length (personal communication of the late Dr. Heinz Kozur).

    Material: 12 specimens.

    Stratigraphic range and occurrence: Early Bithynian to late Pelsonian of Turkey.

    Genus Chiosella Kozur 1989

    Type species: Gondolella timorensis Nogami, 1968 (p. 127–128, pl. 10, figs. 17a–17c)

    Figs. 5.1, 5.2, 5.5, 5. 6

    Remarks: Chiosella is characterized by a very narrow smooth platform that develops from the central-lateral rib (Kozur, 1989, p. 416). The lower surface resembles that of Neospathodus and has an excavated or V-shaped incised keel. The terminal basal cavity is very large and funnel-shaped, flaring. The carina extends over the entire unit and consists of high, equally and moderately inclined, laterally compressed denticles. The similarity between the species C. timorensis and Neogondolella aegaea is so pronounced that several authors proposed them to be synonyms; e.g., Kozur (1989, p. 415).

    Chiosella timorensis (Nogami, 1968)

    Figs. 5.1, 5.2, 5.5, 5. 6

    1968   Gondolella timorensis n. sp.; Nogami, p. 127–128, pl. 10, figs. 17–21.

    1970   Spathognathodus gondolelloides; Bender, p. 529– 530, pl. 5, figs. 19, 20.

    1970    Neospathodus timorensis; Sweet, p. 256, pl. 2, figs. 22, 23.

    1977    Neogondolella timorensis; Nicora, p. 92–98, pl. 1–4, all figs. except fig. 3 of pl. 3.

    1988    Kashmirella timorensis; Budurov et al., 107–122, pl. 1, figs. 1–4.

    1989    Chiosella timorensis; Kozur, p. 415–416, pl. 15, figs. 1–3.

    1991    Gondolella timorensis timorensis; Mietto et al., p. 311, pl. 1, figs. 1–2.

    1992    Gondolella timorensis; Gaetani et al., p. 195, pl. 17, figs. 8–13.

    1994    Chiosella timorensis; Orchard, pl. 1, figs. 1–10, 12–14.

    2006    Chiosella timorensis; Grãdinaru et al., pl. 1, figs. 1–7.

    2007a    Chiosella timorensis; Orchard et al., figs. 5(32–34).

    2007b    Chiosella timorensis; Orchard et al., figs. 6(32–34, 36–38).

    2012    Chiosella timorensis; Goudemand et al., p. 203, figs. 2(1–14), 3(1–8).

    2015    Chiosella timorensis; Golding et al., p. 166, figs. 11(4–6).

    Original diagnosis (Nogami, 1968; p. 127): Part of Gondolella, characterized by its extremely reduced platform. Kozur (1989, p. 415–416) added that, the segminate to segminiplanate P1 element developed a very narrow or rudimentary platform, commonly asymmetrically, on each side of a high carina. The multielement apparatus of Chiosella has been reconstructed by Orchard (2005).

    Description: Elongate P1 element with 12–15 moderately fused denticles becoming increasingly reclined toward the posterior margin. In lateral view, below the base of the denticles, a lateral median ridge develops along most of the length of the unit. The aboral margin is straight, somewhat downturned towards the posterior end. The lower surface is marked by a narrow longitudinal groove that expands posteriorly into a broad basal cavity.

    Remarks: This species is very similar to C. gondolelloides, which is distinguished from the latter by its relative length and the development of lateral median ridges. Our specimens have a length/height ratio of about (3.1–3.4) : 1, which is clearly different from the holotype of C. gondolelloides with a length/height ratio of 2.5 : 1 (Bender, 1970) in being much more elongate. The common length/height ratios of C. gondolelloides are about 2.1–2.9 (see specimens by Orchard et al., 2007a, b; Grãdinaru et al., 2006). The development of lateral median ridges is one of the key characters defining this species.

    Supporting the inclusion of this species in the genus Neogondolella, Nicora (1977) cited the more or less well- developed platform at all growth-stages, the brim enclosing the posterior end of the carina, as well as width/height/length ratios. Topotypic specimens of Chiosella timorensis have a ratio ranging from 1/2.7/5.5 to 1/2.3/7, Sweet's (1970) species from Pakistan 1/2.8/7 to 1/2.3/5, Nicora's (1977) species from Nevada and Chios 1/2.9/5.8 to 1/2.3/7. These values are in agreement with the ratios calculated by Sweet (1970) for some species of the genus Neogondolella (1/1.5/4 to 1/2/8) and differ from the higher and longer values of the genus Neospathodus (mean value: 1/2/3) (Nicora, 1977).

    For Goudemand et al. (2012), the downward deflection of the posterior end varies more as suggested by Sweet: in most specimens the basal margin being straight or sub-straight over most of the unit's length and deflected downwardly posterior of the cusp, the basal margin being sometimes curved along the whole length of the element without distinctive deflection posterior of the cusp (Sweet, 1970).

    Stratigraphic range and occurrence: The First Appearance Datum (FAD) of Chiosella timorensis is proposed as the index for the base of the Anisian GSSP (Orchard et al., 2007b). However, Goudemand et al. (2012) found C. timorensis in the late Spathian Haugi Zone of Nevada. The range of this species appears to be late Spathian to Aegean.

    Family Incertae Sedis: Taxa that are limited to small numbers (three or four) elements of Ozarkodinid derivation, such as Neostrachanognathus, are difficult to classify within the Family Gondolellidae. The genus Cornudina has had several different multielement reconstructions, and it is not clear which elements may belong to this genus and which do not; it is therefore not possible to place this genus within a known family at this time.

    Genus Cornudina Hirschmann, 1959

    Type species Ozarkodina breviramulis Tatge, 1956

    Figs. 4.20, 4.21, 4.23, 4.24, 4.25

    Remarks: Cornudina was described as a form-genus by Hirschmann (1959), and has been reported from Lower to Upper Triassic strata in the Tethyan region. The small-sized ramiform element is characterized by a relatively long cusp, a short anterior process and a posterior process with a small number of denticles. There have been several conflicting multielement reconstructions of this genus. Orchard (2005) considered Cornudina to possess bipennate S3 and S4 elements and a breviform digyrate M element based on his reconstruction of C.? igoi, and referred the genus to the Family Gondolellidae. In contrast, Koike (2016) reconstructed the apparatus of C. breviramulis with extensiform digyrate S1 and S2 elements and placed Cornudina in the Family Ellisonidae. Previously, Koike (1996) had regarded Cornudina as possessing a bimembrate apparatus, prior to his 2016 revision. Kılıç et al. (2018b) pointed out that several elements in the Orchard (2005) reconstruction can be assigned to the form-genera Ketinella and Kamuellerella, which rarely occur with Cornudina. Therefore, the multielement apparatus of Cornudina is still unknown, and as this taxon is limited to a maximum of three elements of Ozarkodinid derivation, it is difficult to classify within the family of Gondolellidae and may well belong to a Family Incertae Cedis.

    Cornudina oezdemirae Gedik, 1975

    Figs. 4.20, 4.21, 4.24, 4.25

    1968    Cornudina breviramulis breviramulis (Tatge); Kozur, pl. 3, fig. 29.

    1970    Cornudina?latidentata Kozur and Mostler; Kozur and Mostler, pl. 1, fig. 21.

    1975    Cornudina oezdemirae Gedik; Gedik, pl. 7, figs. 15, 24 (holotype), 29.

    1982    Cornudina breviramulis minor Kozur and Mostler; Koike, pl. 7, fig. 4.

    1996    Cornudina igoi Koike; Koike, figs. 4.1–4.20.

    2005    Cornudina igoi; Orchard, Text-fig. 1, P1 element.

    2018b   Cornudina oezdemirae; Kılıç et al., p. 2, figs. 1.1–1.4, 1.7–1.9.

    Diagnosis: Unit composed of a long cusp and an anterior process. The length of anterior processes changes depends on the number of the anterior denticles. Cusp inclined posteriorly 40°–50°. Basal margin of unit ranges in length from 150 to 220 μm and cusp ranges in length from 240 to 340 μm (Koike, 1996). Anterior process possesses 1 to 4 denticles. In some specimens one minute denticle present just behind cusp. Anterior denticles increase in length and inclination toward posterior. These anterior denticles can be fused or separated. Basal cavity laterally expanded and elongated as for the number of the anterior denticles. Basal cavity shows drop shape in cross-section.

    Comparisons: Cornudina oezdemirae is distinguished from C. breviramulis in having no distinctive denticle behind the cusp.

    Remarks: Cornudina oezdemirae is a unimembrate type composed of the P1 element. C. breviramulis ranges from the Early to Late Triassic but the occurrence of C. oezdemirae is restricted in the Early to Middle Triassic. The denticles on the anterior process of the element of this species vary in number as observed in the P1 element of C. breviramulis.

    For reasons of priority, Cornudina oezdemirae Gedik (1975), with one anterior denticle, may include C. igoi Koike (1996), although the latter's anterior process possesses up to 3 discrete denticles. Koike's (2006) comment about up to 4 discrete denticles instead of 1 to 3, modifies the multi-element description of Cornudina in Orchard (2005; text-fig. 1A). Cornudina oezdemirae Gedik shows an evolutionary trend of decreasing total length of the anterior processes and number of discrete denticles, ranging from 3 to 1 minute denticle just behind the cusp. Koike (1999) suggested that C. oezdemirae resembled the S0 element in his reconstruction of Neostrachanognathus tahoensis and therefore would be the senior synonym of N. tahoensis. However, C. oezdemirae commonly occurs separately from other elements of N. tahoensis, and so they are retained as separate species here.

    Material: 19 species.

    Stratigraphic range and occurrence: Early Spathian– Anisian. C. oezdemirae occurs from the basal part of the Neospathodus triangularis-N. homeri Zone and indicates the early Spathian in the Taho Formation of Japan, whereas in Turkey it indicates the Anisian.

    Cornudina cf. latidentata Kozur and Mostler 1970

    Fig. 4.23

    1956    Ozarkodina breviramulis; Tatge (pars.), p. 126, pl. 5, fig. 12.

    1959    Cornudina breviramulis; Hirschmann, p. 90, pl. 4, figs. 3, 4.

    1968    Cornudina breviramulis minor; Kozur, p. 943, pl. 3, figs. 27, 30.

    1970    Cornudina latidentata sp. nov.; Kozur and Mostler, p. 457, pl. 1, figs. 11–13, 19.

    1972    Cornudina latidentata; Kozur and Mostler, p. 37, pl. 1, figs. 18–23, 26, 27.

    1972    Cornudina cf. breviramulis minor; Kozur and Mostler, p. 53, pl. 15, figs. 19, 22, 24, 25.

    1972    Cornudina cf. breviramulis breviramulis; Kozur and Mostler, p. 53, pl. 15, fig. 23.

    1975    Cornudina latidentata; Trammer, pl. 25, fig. 3.

    1975    Cornudina latidentata; Zawidzka, p. 246, pl. 35, figs. 7, 9.

    1981    Cornudina?latidentata; Wang and Dai, p. 141, pl. 2, fig. 29.

    1992    Cornudina latidentata; Kozur and Mostler, pl. 2, figs. 16, 17.

    1999    Cornudina?latidentata; Narkiewicz, pl. 1, fig. 4.

    2010    Cornudina latidentata; Götz and Gast, fig. 3, part 6.

    2018b Cornudina cf. latidentata, Kılıç et al., figs. 1.5, 1.6, 1.10, 1.11.

    2019a    Cornudina latidentata; Chen et al., pl. 14, figs. 5A–5D.

    Remarks: The single specimen referred to as Cornudina cf. latidentata shares the relatively long anterior denticulated process of this species; however, the fragmentary nature of the specimen and uncertainty about the possible synonymy of C. latidentata with C. oezdemirae (Kılıç et al., 2018b) precludes unambiguous assignment to this species.

    Stratigraphic range and occurrence: Anisian of Austria, Poland, Turkey and China.

    Genus Neostrachanognathus Koike, 1998

    Type species Neostrachanognathus tahoensis Koike, 1998

    Fig. 4.22

    Original diagnosis: The diagnosis of Neostrachanognathus proposed is based on N. tahoensis by Koike (1998). Neostrachanognathus is characterized by a quadrimembrate apparatus composed of a non-denticulated and three denticulated nongeniculate coniform elements. The base of the element is relatively small and short and the basal cavity shallow. Cusp is proclined and tapered. Denticles of denticulated elements are situated at anterobasal portion (figs. 7 and 9 of Koike, 1998). Coniform elements were referred to as M, S1, S2, and S3 positions by Koike (1998). M element bilaterally subsymmetric adenticulated coniform. S1 element bilaterally subsymmetric denticulated coniform and carries one small proclined anterobasal denticle. S2 element has inwardly bending one or two small to large anterobasal denticles. S3 element possesses long upper basal margin and carries inwardly flexing one or two small to large anterobasal denticles. One posterior denticle may be present on the base. An alternative multielement reconstruction for Neostrachanognathus was proposed by Agematsu et al. (2008) based on natural assemblages of N. tahoensis from Japan, and of isolated specimens of N. sp. from Oman. Agematsu et al. (2008) demonstrated the occurrence of ramiform elements (which could not be differentiated due to poor preservation of the natural assemblages, and thus were all referred to as S elements) with the coniform elements of Neostrachanognathus. These reconstructions lack elements corresponding to S0 and M positions, as occur in typical 15 elements ozarkodinid apparatuses.

    Neostrachanognathus tahoensis Koike, 1998

    Fig. 4.22

    1989    Cratognathodus sp.; Buryi, pl. 2, fig. 6.

    1998    Neostrachanognathus tahoensis sp. nov.; Koike, p. 127, 128, figs. 4, 9(1–19, 22).

    2008    Neostrachanognathus tahoensis; Agematsu et al., p. 1210, figs. 3A–3C, 4A–4C, 5A–5C, 6A–6B, 6D, 6F.

    2017    Neostrachanognathus tahoensis; Kolar-Jurkovšek et al., p. 695, fig. 7.

    2019b    Neostrachanognathus tahoensis; Chen et al., fig. 6, part 5.

    Description: Four elements of this apparatus exhibit common characteristics such as thick wall, relatively small and short base, and proclined and tapered cusp (Agematsu et al., 2008). The element illustrated in Fig. 4.22 is a P2 element in the reconstruction of Agematsu et al. (2008), or an M element in the reconstruction of Koike (1998).

    Material: 14 specimens.

    Stratigraphic range and occurrence: Lower Spathian?- Aegean of China, Japan, Russia, Turkey, Slovenia and Oman.

  • New species of conodonts, Paragondolella praecornuta, P. ebruae, and P. hirschii allow the Anisian of Kocaeli to be characterized in more detail. The Anisian conodont fauna of the Kocaeli Peninsula shows strong similarities with that of Golobardo in Bulgaria (Budurov, 1980), the dominant taxa in both provinces being P. bulgarica, P. ebruae n. sp., P. praecornuta n. sp., P. hirschii n. sp. and P. hanbulogi.

    Evolutionary patterns of Anisian conodonts can be observed in the collections from Kocaeli. The elongation of the Neospathid morph (Triassospathodus homeri) at the end of the Spathian is at the origin of the lineage initiated by Chiosella timorensis that persisted until the end of the Middle Triassic, consisting of the lineage of Paragondolella (aegaea-bulgarica-excelsa-foliata- inclinata), including the iteration of Neospathid forms such as the late Anisian Nicoraella. Another important Bithynian–early Pelsonian event is the appearance of the Kamuellerella-Ketinella- Gedikella conodont genera, apparently restricted to the Kocaeli Triassic. The cause of this event is yet unexplained; however, it may be attributable to changes in local paleoclimate, which will require geochemical data to be confirmed.

Reference (104)



    DownLoad:  Full-Size Img  PowerPoint