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From Precambrian to Holocene – Biodiversity Changes Recorded in the Rocks

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From Precambrian to Holocene – Biodiversity Changes Recorded in the Rocks POLSKIE TOWARZYSTWO GEOLOGICZNE UNIWERSYTET WROCŁAWSKI ZAKŁAD GEOLOGII STRATYGRAFICZNEJ INSTYTUTU NAUK GEOLOGICZNYCH ZAKŁAD PALEOZOOLOGII INSTYTUTU BIOLOGII ŚRODOWISKOWEJ XXIV Konferencja Naukowa Sekcji Paleontologicznej Polskiego Towarzystwa Geologicznego OD PREKAMBRU DO HOLOCENU - ZMIANY BIORÓŻNORODNOŚCI ZAPISANE W SKAŁACH From Precambrian to Holocene – biodiversity changes recorded in the rocks Wrocław, Długopole Górne 11-14 września 2019 r. Materiały konferencyjne Redakcja i recenzja: Jolanta Muszer, Alina Chrząstek, Robert Niedźwiedzki Wrocław 2019 POLSKIE TOWARZYSTWO GEOLOGICZNE ZAKŁAD GEOLOGII STRATYGRAFICZNEJ INSTYTUTU NAUK GEOLOGICZNYCH UNIWERSYTETU WROCŁAWSKIEGO ZAKŁAD PALEOZOOLOGII INSTYTUTU BIOLOGII ŚRODOWISKOWEJ UNIWERSYTETU WROCŁAWSKIEGO OD PREKAMBRU DO HOLOCENU - ZMIANY BIORÓŻNORODNOŚCI ZAPISANE W SKAŁACH From Precambrian to Holocene – biodiversity changes recorded in the rocks XXIV Konferencja Naukowa Sekcji Paleontologicznej Polskiego Towarzystwa Geologicznego Wrocław, Długopole Górne 11-14 września 2019 r. Materiały konferencyjne Redakcja i recenzja: Jolanta Muszer, Alina Chrząstek, Robert Niedźwiedzki Wrocław 2019 XXIV Konferencja Naukowa Sekcji Paleontologicznej PTG, Wrocław, Długopole Górne 11-14 września 2019 PÓŹNOTRIASOWE DICYNODONTY ZE ŚLĄSKA Late Triassic dicynodonts from Silesia Tomasz Sulej1, Grzegorz Niedźwiedzki2, Tomasz Szczygielski1 1Instytut Paleobiologii PAN, ul. Twarda 51/55, 00-818 Warszawa, Polska, e-mail: [email protected]; [email protected]; 2Department of Organismal Biology, Evolutionary Biology Centre, Uppsala University, Norbyvӓgen 18A, 752 36 Uppsala, Sweden, e-mail: [email protected] Słowa kluczowe: Lisowicia, Woźniki, Lisowice, czaszka Key words: Lisowicia, Woźniki, Lisowice, skull Dicynodonty to grupa roślinożernych synapsydów (gadów ssakokształtnych), żyjących od środkowego permu do późnego triasu. Były reprezentowane zarówno przez formy wielkości borsuka, jak również przez zwierzęta o ponad dwumetrowej wysokości. Większość zamiast zębów używała rogowego dzioba do rozdrabniania pokarmu. Niedawna seria odkryć nowych stanowisk paleontologicznych górnego triasu w Polsce przyniósła również nowe dicynodonty, które są wyjątkowo rzadkie w Europie. Do ubiegłego roku wstępnie opisane były szczątki z Woźnik, Lisowic i Zawiercia-Marciszowa. W roku 2019 nazwana została Lisowicia bojani – największy i najmłodszy na świecie dicynodont. W publikacji tej przedstawiono szczątki zebrane jedynie w cegielni Lipie Śląskie w Lisowicach. Przybliżony wiek tych osadów to 210-205 milionów lat. Morfologia kości piszczelowej z Marciszowa i łokciowej z Myszkowa sugeruje jednak, że należą one do tego samego gatunku, i że stanowisk z lisowicją może być na Śląsku więcej. Jest to o tyle ważne, że wciąż nie udało się znaleźć kompletnej czaszki tego dicynodonta i wielu ważnych informacji o tym gatunku wciąż brakuje. Obecnie autorzy (T.S., T.Sz.) przygotowują opis niekompletnego szkieletu jednego osobnika z cegielni w Woźnikach. Badania są prowadzone w ramach grantu NCN 2017/27/B/NZ8/01543. Wstępne wyniki sugerują, że forma z Woźnik jest pośrednia między znanym z Rosji Rabidosaurus a amerykańskim Placerias (z którym blisko spokrewniona była z pewnością lisowicja). Istotną częścią tego projektu są także poszukiwania szczątków dicynodontów w Krasiejowie (ten sam wiek co Woźniki) oraz w środkowotriasowych osadach w Miedarach. 79 XXIV Konferencja Naukowa Sekcji Paleontologicznej PTG, Wrocław, Długopole Górne 11-14 września 2019 Morawsko-Śląskim i Żywieckim, Beskidzie Wyspowym oraz w pasie pogórzy: P. Rożnowskie, P. Strzyżowsko-Dynowskie, a także na przedpolu Beskidu Niskiego i Bieszczadów. Podczas badań zwrócono uwagę na wpływ procesów sedymentacyjnych i środowiska depozycji na rozdzielczość zapisu oraz redepozycji niektórych skamieniałości (Olsson & Liu, 1993). Uwzględniono przy tym wpływ czynników środowiskowych, tj.: cyrkulacja wód, natlenienie, dostępność pożywienia i węglanu wapnia (Alegret & Thomas, 2012) oraz wydarzeń paleogeograficznych (tektonika, wulkanizm, poziom morza) i klimatycznych, które przyczyniły się do nagłych zmian w biotopach (Keller, 2008; Keller & Abramovich, 2008; Pardo & Keller, 2008). Te relacje są szczególnie widoczne w zespołach otwornicowych polskich Karpat zewnętrznych (Olszewska, 1984), które w odróżnieniu od nanoplanktonu i dinocyst posiadają odmienny potencjał fosylizacyjny i inaczej reagowały na stres. Rozprzestrzenienie i stan zachowania wapiennych otwornic oraz fitoplanktonu, a także obecność zarodników grzybów oraz pyłków i nasion roślin wyższych i ich szczątków organicznych (fragmenty drewna, często ostrokrawędziste) wskazuje na silne związki z obszarem nerytycznym i lądowym, a także potwierdza zmiany poziomu morza i klimatu. Materiał był dostarczany w warunkach niestabilności geotektonicznej, która po okresie nasilenia w kampanie i pojawieniu się form chłodnolubnych (LMC, Jarvies et al., 2002) ustabilizowała się w mastrychcie udokumentowanym przez ciepłolubne masywne i ornamentowane otwornice planktoniczne i nanoplankton (Gasiński, 1997; Jugowiec-Nazarkiewicz, 2007). Na pograniczu z paleogenem uległy one stagnacji przy gwałtownym spadku poziomu morza i podniesieniu CCD. Zakwaszenie i niedotlenienie środowiska doprowadziło wówczas do zubożenia biotopów na dnie i powierzchni wód. Pod wpływem stresu (KTBE) plankton we wczesnym paleocenie (Jednorowska, 1975) osiągał bardzo małe rozmiary (karłowaciał) (Keller & Abramovich, 2009). Odnowienie biotopów pod koniec paleocenu (LPTE, Bains et al., 2000) przyczyniło się do wzrostu zróżnicowania planktonu (Morozovella, Accarinina) oraz bentosu (Nuttalides), który był wyznacznikiem reaktywacji wód dennych (Friedrich et al., 2006). Na badanym obszarze zapis zmian biocenoz był często niedostateczny. Depozycja turbidytowa i fluktuacje poziomu przyczyniały się nie tylko do erozji osadu, ale także zaniku środowiska, w którym ten zapis mógłby powstać. Dlatego mamy często lukę w zapisie najniższego paleocenu. Literatura Alegret, L., Thomas, E., Lohmann, K.C., 2012. End-Cretaceous marine mass extinction not caused by productivity collapse. Proceedings of the National Academy of Science, 109: 728–732. Bains, S., Norris, R.D., Corfield, R.M., Faul, K.L., 2000. Termination of global warmth at the Palaeocene/Eocene boundary through productivity feedback. Nature, 407: 171–173. Friedrich, O, Schmiedl, G., Erlenkeuser, H., 2006. Stable isotope composition of Late Cretaceous benthic foraminifera from the southern South Atlantic: Biological and environmental effects. Marine Micropaleontology, 58 (2), 135–157 Gasinski, M. A., 1997. Tethyan-Boreal connection: influence on the evolution of mid-Cretaceous planktonic foraminiferids. Cretaceous Research, 18: 505–514. Jankowski, L., 2015. Nowe spojrzenie na budowę geologiczną Karpat – ujęcie dyskusyjne. Instytut Nafty i Gazu-PIB: 1–155. Jarvis, I., Mabrouk, A., Moody, R.T.J., de Cabrera, S., 2002 Late Cretaceous (Campanian) carbon isotope events, sea - level change and correlation of the Tethyan and Boreal realms. Palaeogeography, Palaeoclimatology, Palaeoecolology, 188: 215–248. Jednorowska, A., 1975. Small Foraminifera assemblages in the Paleocene of the Polish Western Carpathians, Studia Geologica Polonica, 47: 1–149. Jugowiec-Nazarkiewicz, M., 2007. Nanoplankton wapienny górnokredowych facji pelagicznych jednostki podśląskiej Polskich Karpat fliszowych. Biuletyn PIG, 426: 53–90. Keller, G., 2008. Cretaceous climate, volcanism, impacts, and biotic effects. Cretaceous Research, 29: 754–771. Keller, G., Abramovich, S., 2009. Lilliput effect in late Maastrichtian planktic foraminifera: Response to environmental stress. Palaeogeography, Palaeoclimatology, Palaeoecology. 284: 47–62. Molina, E., Arenillas, I., Arz, J.A., 1998. Mass extinction in planktic foraminifera at the Cretaceous/Tertiary boundary in subtropical and temperate latitudes. Bulletin de la Société géologique de France, 169: 351–363. Liszkowa, J., Morgiel, J. 1985. Contribution to the knowledge of the foraminifers of the Frydek type facies in the Polish Outer Carpathians. Kwartalnik Geologiczny, 29 (1): 65–83. Olsson, R. K,. Liu, Ch., 1993. Controversies on the Placement of Cretaceous-Paleogene Boundary and the K/P Mass Extinction of Planktonic Foraminifera. Palaios, 8 (2): 127–139. Olszewska, B., 1984. Interpretacja paleoekologiczna otwornic kredy i paleogenu polskich Karpat zewnętrznych. Biuletyn Instytutu Geologicznego, 346: 7–53. 81 .
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