Gutak, Ja. M.

Rodygin, S. A.

English

Tomsk State University Repository

16th International Conference EMMM-2011, Borissiak Paleontological Institute RAS, Russia, September 19-22, 2011Russian Academy of SciencesBorissiak Paleontological Institute of RASKarpinsky Russian Geological Research InstituteLomonosov Moscow State University, Geological FacultyWinogradsky Institute of Microbiology of RASRussian Academy of Natural SciencesAvalon Institute of Applied ScienceRussian Branch of International Society “Environmental Micropaleontology, Microbiology and Meiobenthology”Proceedingsof the Sixth International Conference“Environmental Micropaleontology, Microbiology  and Meiobenthology”September 19–22, 2011MoscowMoscow PIN RAS2011116 1176th International Conference EMMM-2011, Borissiak Paleontological Institute RAS, Russia, September 19-22, 20116th International Conference EMMM-2011, Borissiak Paleontological Institute RAS, Russia, September 19-22, 2011LATE FAMENNIAN SHALLOW CONODONTS OF THE KUZNETSKY BASINJa.M. Gutak1, S.A. Rodygin21 Kuzbass State Pedagogical Academypr. Pionersky, 13, Kemerovo region, Novokuznetsk 654027, Russiagutakjaroslav@yandex.ru2 Tomsk State UniversityLenin ave. 36, Tomsk 634050, Russiarodygin@ggf.tsu.ruDuring inspection of terminal deposits of the Later Devonian in Kuzbass in typical section of Topkian Sub-stage we found out original assemblage of shallow conodonts of the Late Famennian. Described site was localized along the left board of the river Bolshaya Kamyshnaya 500 m above the railway bridge at Topki Village (not town of Topky located nearby). Geographical coordinates of the site 55°21’13.0’’ N, 85°46’23.0’’ E. Conodont samples were collected from the layer of dark gray organogenic limestone containing fragments of brachiopod shutters, small colonies of bryozoans and crinoids detritus. The assemblage of conodonts received from these samples is variable in structure (the most important taxa are shown on the Plate 1). It includes the following: Polygnathus aff. parapetus Druce (Pl. 1, figs. 1, 6), Polyg-nathus inornatus Branson et Mehl (Pl. 1, figs. 3, 4), Neopolygnathus lectus Kononova (Pl. 1, figs. 2, 5), Pseu-dopolygnathus primus Branson et Mehl (Pl. 1, fig. 7), “Icriodus” costatus darbyensis Klapper, Morphotype 2 (Pl. 1, fig. 9), “Icriodus” costatus (Thomas) (Pl. 1, fig. 8). Besides there are fragments of conodonts of the worst safety, which are not possible to indentify, and backbone elements of the apparatus: Drepanodina sp., Ligonodina sp., Hindeodella sp., Acodina sp., etc. The resulted association of conodonts, especially prevalence of numerous species of Polygnathus (dominant) and representatives of Icriodus among them is typical for shallow facies o the open sea. This conclusion is proved to be true by lithologic characteristics of rocks were generated in wave-cut zone), the limestone pack of small thickness (to 50 m) lies over red-colored deposits of continental genesis and is overlapped by pyroclastic (ash) deposits. Polygnathus inornatus Branson et Mehl is traced in the range from the Famennian Lower expansa to the Tournaisian anchoralis zone: (1) Neopolygnathus lectus Kononova (former Polygnathus communis lectus) is dis-tributed in the Famennian of the Upper Devonian and the Tournaisian of the Lower Carboniferous, in praesul-cata – sulcata – duplicata zone interval; (2) Pseudopolygnathus primus Branson et Mehl is distributed within praesulcata zone in the upper part of Famennian; (3) the subspecies “Icriodus” costatus darbyensis Klapper, Morphotype 2 is traced “from level within the Lower expansa zone, presumably above the first occurrence of a morphotype 1, is definitely traced through all the Upper expansa zone and probably also through the zones of the Lower and Middle praesulcata, on basis of rare finds” (Sandberg, Dreesen, 1984); (4) “Icriodus” costatus (Thomas) is extended in shallow facies of Famennian for which some researchers allocate the zone with the cor-responding name, which correlates with standard conodont zones of Uppermost marginifera, trachytera, postera, expansa and praesulcata (Sandberg, Dreesen, 1984; Matyja, 1993). Conodonts, attributed by us to Polygnathus aff. parapetus Druce, in our opinion represent transit forms from Polygnathus paprothae Bouckaert et Groessens to P. parapetus Druce also are typical for the top part of praesulcata Zone – sulcata Zone. The most probable time of formation of the described assemblage was the Late Famennian (the upper part of praesulcata Zone). The data obtained by us correlate with data received before by Kononova (Bushmina et al., 1984), and our data on other areas of distribution of these deposits (Gutak et al., 2007). Most likely, in the end the Famennian the lowland area of northern part of the Kuznetsk bending was a part of epicontinental sea basin. ReferencesBushmina L.S., Bogush O.I., Kononova L.I. Mikrofauna i biostratigrafiya nizhnego karbona (yug Zapadnoy Sibiri) [Micro-fauna and Biostratigraphy of the Lower Carboniferous (south of West Siberia)] // Tr. IGiG SO AN SSSR, 1984. V. 599. 128 p. (In Russian).Gutak Ja.M., Rodygin S.A., Tolokonnikova Z.A. Nizhnyaya granica kamennougolnoy sistemy v zapadnoy chasti Altaye-Sayanskoy skladchatoy oblasti [The lower boundary of the Carboniferous system in the western part of Altai-Sayan folded area] // Verchniy paleozoy Rossii: Stratigrafiya i paleogeografiya / Materialy Vserossiyskoy konferencii, pos-vyaschennoy pamyaty Vyacheslava Georgiyevicha Chalyumbadjy, September 25-27, 2007, Kazan. [Upper Paleozoic Russia: stratigraphy and palaeogeography. Proceedings of the All-Russian conference dedicated to the memory of Vy-acheslav Georgievich Halymbadzha, 25-27 September 2007, Kazan] Kazan, 2007. P. 94-97. (In Russian).Conodonts from the Upper Devonian (Topkian Substage), the sample G–08–46. Conodonts are stored in the Paleontological Museum of Tomsk State University at number 68: figs. 1, 6. Polygnathus aff. parapetus Druce, P-element: 1а – top view, 1b – bottom view, 6 – top view; figs. 2, 5. Neopolygnathus lectus Kononova, P-element: 2 – top view, 5 – ventral view; figs. 3, 4. Polygnathus inornatus Branson et Mehl, P-element: 3 – bottom view, 4 – bottom view; fig. 7. Pseudopolygnathus primus Branson et Mehl, P-element, top view; fig. 8. “Icriodus” costatus (Thomas), I-element: а – top view, b – side view; fig. 9. “Icriodus” costatus darbyensis Klapper, Morphotype 2, I-element: а – top view, b – bottom view.Plate 1 116 1176th International Conference EMMM-2011, Borissiak Paleontological Institute RAS, Russia, September 19-22, 20116th International Conference EMMM-2011, Borissiak Paleontological Institute RAS, Russia, September 19-22, 2011LATE FAMENNIAN SHALLOW CONODONTS OF THE KUZNETSKY BASINJa.M. Gutak1, S.A. Rodygin21 Kuzbass State Pedagogical Academypr. Pionersky, 13, Kemerovo region, Novokuznetsk 654027, Russiagutakjaroslav@yandex.ru2 Tomsk State UniversityLenin ave. 36, Tomsk 634050, Russiarodygin@ggf.tsu.ruDuring inspection of terminal deposits of the Later Devonian in Kuzbass in typical section of Topkian Sub-stage we found out original assemblage of shallow conodonts of the Late Famennian. Described site was localized along the left board of the river Bolshaya Kamyshnaya 500 m above the railway bridge at Topki Village (not town of Topky located nearby). Geographical coordinates of the site 55°21’13.0’’ N, 85°46’23.0’’ E. Conodont samples were collected from the layer of dark gray organogenic limestone containing fragments of brachiopod shutters, small colonies of bryozoans and crinoids detritus. The assemblage of conodonts received from these samples is variable in structure (the most important taxa are shown on the Plate 1). It includes the following: Polygnathus aff. parapetus Druce (Pl. 1, figs. 1, 6), Polyg-nathus inornatus Branson et Mehl (Pl. 1, figs. 3, 4), Neopolygnathus lectus Kononova (Pl. 1, figs. 2, 5), Pseu-dopolygnathus primus Branson et Mehl (Pl. 1, fig. 7), “Icriodus” costatus darbyensis Klapper, Morphotype 2 (Pl. 1, fig. 9), “Icriodus” costatus (Thomas) (Pl. 1, fig. 8). Besides there are fragments of conodonts of the worst safety, which are not possible to indentify, and backbone elements of the apparatus: Drepanodina sp., Ligonodina sp., Hindeodella sp., Acodina sp., etc. The resulted association of conodonts, especially prevalence of numerous species of Polygnathus (dominant) and representatives of Icriodus among them is typical for shallow facies o the open sea. This conclusion is proved to be true by lithologic characteristics of rocks were generated in wave-cut zone), the limestone pack of small thickness (to 50 m) lies over red-colored deposits of continental genesis and is overlapped by pyroclastic (ash) deposits. Polygnathus inornatus Branson et Mehl is traced in the range from the Famennian Lower expansa to the Tournaisian anchoralis zone: (1) Neopolygnathus lectus Kononova (former Polygnathus communis lectus) is dis-tributed in the Famennian of the Upper Devonian and the Tournaisian of the Lower Carboniferous, in praesul-cata – sulcata – duplicata zone interval; (2) Pseudopolygnathus primus Branson et Mehl is distributed within praesulcata zone in the upper part of Famennian; (3) the subspecies “Icriodus” costatus darbyensis Klapper, Morphotype 2 is traced “from level within the Lower expansa zone, presumably above the first occurrence of a morphotype 1, is definitely traced through all the Upper expansa zone and probably also through the zones of the Lower and Middle praesulcata, on basis of rare finds” (Sandberg, Dreesen, 1984); (4) “Icriodus” costatus (Thomas) is extended in shallow facies of Famennian for which some researchers allocate the zone with the cor-responding name, which correlates with standard conodont zones of Uppermost marginifera, trachytera, postera, expansa and praesulcata (Sandberg, Dreesen, 1984; Matyja, 1993). Conodonts, attributed by us to Polygnathus aff. parapetus Druce, in our opinion represent transit forms from Polygnathus paprothae Bouckaert et Groessens to P. parapetus Druce also are typical for the top part of praesulcata Zone – sulcata Zone. The most probable time of formation of the described assemblage was the Late Famennian (the upper part of praesulcata Zone). The data obtained by us correlate with data received before by Kononova (Bushmina et al., 1984), and our data on other areas of distribution of these deposits (Gutak et al., 2007). Most likely, in the end the Famennian the lowland area of northern part of the Kuznetsk bending was a part of epicontinental sea basin. ReferencesBushmina L.S., Bogush O.I., Kononova L.I. Mikrofauna i biostratigrafiya nizhnego karbona (yug Zapadnoy Sibiri) [Micro-fauna and Biostratigraphy of the Lower Carboniferous (south of West Siberia)] // Tr. IGiG SO AN SSSR, 1984. V. 599. 128 p. (In Russian).Gutak Ja.M., Rodygin S.A., Tolokonnikova Z.A. Nizhnyaya granica kamennougolnoy sistemy v zapadnoy chasti Altaye-Sayanskoy skladchatoy oblasti [The lower boundary of the Carboniferous system in the western part of Altai-Sayan folded area] // Verchniy paleozoy Rossii: Stratigrafiya i paleogeografiya / Materialy Vserossiyskoy konferencii, pos-vyaschennoy pamyaty Vyacheslava Georgiyevicha Chalyumbadjy, September 25-27, 2007, Kazan. [Upper Paleozoic Russia: stratigraphy and palaeogeography. Proceedings of the All-Russian conference dedicated to the memory of Vy-acheslav Georgievich Halymbadzha, 25-27 September 2007, Kazan] Kazan, 2007. P. 94-97. (In Russian).Conodonts from the Upper Devonian (Topkian Substage), the sample G–08–46. Conodonts are stored in the Paleontological Museum of Tomsk State University at number 68: figs. 1, 6. Polygnathus aff. parapetus Druce, P-element: 1а – top view, 1b – bottom view, 6 – top view; figs. 2, 5. Neopolygnathus lectus Kononova, P-element: 2 – top view, 5 – ventral view; figs. 3, 4. Polygnathus inornatus Branson et Mehl, P-element: 3 – bottom view, 4 – bottom view; fig. 7. Pseudopolygnathus primus Branson et Mehl, P-element, top view; fig. 8. “Icriodus” costatus (Thomas), I-element: а – top view, b – side view; fig. 9. “Icriodus” costatus darbyensis Klapper, Morphotype 2, I-element: а – top view, b – bottom view.Plate 1 

Late famennian shallow conodonts of the Kuznetsky basin

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Late famennian shallow conodonts of the Kuznetsky basin

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