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Popov 02.Pdf Paleontological Journal, Vol. 36, Suppl. 3, 2002, pp. S185–S259. Original Russian Text Copyright © 2002 by Popov, Akhmetiev, Bugrova, Lopatin, Amitrov, Andreyeva-Grigorovich, Zaporozhets, Zherikhin, Krasheninnikov, Nikolaeva, Sytchevskaya, Shcherba. English Translation Copyright © 2002 by MAIK “Nauka /Interperiodica” (Russia). Abstract—This is the second part of the monograph “Biogeography of the Northern Peri-Tethys from the Late Eocene to the Early Miocene.” The main section, Biogeography of the Early Oligocene, considers the stratig- raphy of the Lower Oligocene Paratethys, the biogeographic distribution of the planktonic and benthic marine biotas and the fresh-water and terrestrial fauna and flora in the Lower Oligocene, as well as the biogeographic zonation of water bodies and land areas. In the sections Latitudinal Climatic Zonation and Major Events in the Late Eocene–Early Oligocene, the climatic history of the Early Oligocene is discussed and the major Eocene– Early Oligocene tectonic, eustatic, hydrologic, and biotic events are considered. INTRODUCTION 1986; Geologicheskie i bioticheskie…, 1996); i.e., these This study is aimed at the most complete reconstruc- beds are distinguished based on the their correlation tion of the pattern of the distribution of marine and ter- with Northwest European stratotypes rather than with restrial flora and fauna over Western Eurasia from the the Mediterranean stratigraphic scale, which has been Terminal Eocene, through the Oligocene and to the used for the Priabonian. Early Miocene against the background of major geo- As a geochronological unit, the Rupelian was pro- logical events and paleogeographic and climatic posed by Dumont in 1849 based on outcrops in the changes (the objectivies of this study were discussed in Rupel cuesta (along the Rupel River), northern Bel- greater detail in the first part of this monograph). The gium. There, the major lithostratigraphic unit is the first part also covered the approaches and methods that Boom Clay. However, as a stage, the Rupelian sensu are used in the biogeographic analysis of the Recent lato also includes the underlying Upper Tongrian beds, flora and fauna. The present section is devoted to the Berg Sands, and clay beds with Nucula comta. There biogeographic distribution of planktonic and benthic are no outcrops with a complete sequence of these beds. marine biotas and freshwater and terrestrial fauna and The lowermost layers of the Rupelian Stage are flora in the Early Oligocene, as well as to the biogeo- exposed in eastern Belgium (Leuven Area), while the graphic zonation (integrated wherever possible) of outcrop of the Boom Clay lies farther to the east (Boom water bodies and land areas. At the end of this section, Area). The Upper Tongrian clays yield dinocysts of the the latitudinal-climatic zonation of the Early Oligocene Phthanoperidinium aomoenum Zone, which are typical is discussed and the major Eocene–Early Oligocene fossils of the Sannois Beds, Stampian (Cavelier and events are considered. The evolution of various floral Pomerol, 1986), whereas the sands include nanno- and faunal groups and the dynamic aspects of the evo- plankton of Zone NP22. Planktonic foraminiferal lution of biostratigraphic subdivisions will be discussed assemblages that contain no zonal species but include in the final section of this study, after the biotas of the species typical of Zones P18–P21, nannoplankton of Late Oligocene and Early Miocene are considered. Zones NP23–NP24, and rich dinocyst assemblages of The sections Lower Oligocene Stratigraphy of the the Wetzeliella gochtii Zone, including the W. symmet- Northern Peri-Tethys and Major Late Eocene–Early rica assemblage (Stover and Hardenbol, 1993), have Oligocene Events were written by S.V. Popov; the sec- been found in the Boom Clay. Rich molluskan assem- tion Paleogeography of the Paratethys, by S.V. Popov blages (Glibert and Heinzelin, 1954; Glibert, 1957) and and I.G. Shcherba; and the section Latitudinal Climatic assemblages of ostracodes, fishes, spores, and pollen Zonation of the Early Oligocene, by M.A. Akhmetiev were also recorded there. and S.V. Popov. Data on flora are presented by In deep-sea cores from the warm-water area, two M.A. Akhmetiev; on dinocysts, by M.A. Akhmetiev, planktonic foraminiferal zones, P18 and P19 (Blow, A.S. Andreyeva-Grigorovich, and N.I. Zaporozhets; on 1971), or three zones and one subzone, P18–P21a smaller benthic foraminifers, nummulitids, and disco- (Berggren et al., 1995), and three (or four) nannoplank- cyclinids, by E.M. Bugrova; on terrestrial vertebrates, ton zones, the upper part of Zones NP21, NP22, and by A.V. Lopatin; on nannoplankton, by A.S. Andreyeva- NP23 and the lower part of Zone NP24, are considered Grigorovich; on planktonic foraminifers, by V.A. Kra- to be equivalents to the Rupelian. Three dinocyst zones, sheninnikov; on ostracodes, by I.A. Nikolaeva; on mol- Phthanoperidinium amoenum (D13), Wetzeliella sym- lusks, by O.V. Amitrov and S.V. Popov; on corrals, by metrica (D14a), and W. gochtii (D14b) correspond to E.I. Kuzmicheva; on ichthyofauna, by E.K. Sytchev- the Rupelian succession based on the sequential skaya; and on insects, by V.V. Zherikhin. appearance of zonal species in the most complete Early Oligocene outcrops (table). BIOGEOGRAPHY OF THE EARLY OLIGOCENE The stratotype of the Priabonian–Rupelian bound- ary has been established in the northeastern Apennines Lower Oligocene Stratigraphy (the Massignano Section). There, in the homogenous of the Northern Peri-Tethys sequence of pelagic marly beds, this boundary is We consider the Lower Oligocene beds as equiva- defined based on the change in the planktonic foramin- lents to the Rupelian sensu lato (Cavelier and Pomerol, iferal zones (P17/P18) and the disappearance of Hanth- S185 S186 Correlation of the Upper Eocene–Lower Miocene of the Paratethys and major events in the Eastern Paratethys (after Popov et al., 2001, modified) PLANKTON ZONE Transgres- EASTERN PARATETHYS correlation acc. to Berggren ., 1995 et al Central Shallow Main events in the sion/ Paratethys salinity Dinocysts N. Usturt/ Foraminifera Nannoplankton Foraminifera regional Regression Stage Eastern Paratethys Epoch Andr.-Grig., 1994 Georgia Blow, 1969, Martini, 1971 pre- Age(Ma) (Hungary) ‰ benthos plankton 10 20 30 Carpathians stage +– 1979 Zaporozhec, 1998 Aralian N9 Sph. hetero- Florilus CHOKRAKIAN CHOKRAKIAN CHOKRAKIAN Globigerinoides morphus NN5 BADENIAN parvus Langh. sicanis N8 Globigerina Helicopontosphera TARKHANIAN TARKHANIAN TARKHANIAN G. trilobus N7 tarchanensis Full marine conditions ampliaperta NN4 KARPATIAN Saccammina Globogerinita KOZAHURIAN KOZAHURIAN Bishtyubjanian dissimilis N6 zuramakensis Sulte 20 S. belemnos NN3 OTTNANGIAN 2-nd Paratethvs isolation Burdigal. Globoquadrina SAKARAULIAN Neobulimina SAKARAULIAN Discoaster druggi EGGENBURGIAN Kintykchenian dehiscens N5 elongata NN2 KARADJAL- Suite Upper Gl. kugleri N4 GANIAN POPOV T. carinatus NN1 Cibicides Aralian Suite Aquitan. Short vast transgression D. spinulosa PALEONTOLOGICAL JOURNAL PALEONTOLOGICAL EGERIAN omatus– Baigubekian Globigerina H. floripes Sphenolithus Elphidium Suite ciperoensis P22 et al 25 ciperoensis NP25 KALMYKIAN onerosum Rhombodi- Lower Uplistsikhe Suite Chagraian . Chattian Sp. terekensis Peak of anoxy C. partispinatum nium draco Karato- Globorotalia opi- Krosno Serie Kiscellian Virgulinella makian Turbiditic activity ma opima P21 Clay Sphenolithus Menilithic Serie Troch. florifera Corbula Beds Tamdy distentus NP24 SOLENOVIAN Globiger. am- Upper Tard Wetzeliella Suite pliapertura P20 gochtii Otskhe Beds Chilikta- Paratethys isolation, 30 Sph. praed. NP23 C. lipoldi Beds nian Lower Sp. carinata Globigerina 1-st crisis of salinity Rupelian Helicopontosphera KISKELIAN W. symmetrica Asche- sellii P19 Cherts Lower Tard oligocaenica Abastumanian reticulata NP22 PSCHEKHIAN Kutan- Clay Suite airyk Globigerina Lentic. herrmanni bulak Boreal immigrants tapuriensis P18 Coccolithus Ph. amoenum Vol. 36 Vol. T. cen.–G.g.P17 subdistihus NP21 Shesho- Buda Marl Cibic. salensis Anom. munda Regression, stagnation 35 ra Marl Bryazoan Marl Bol. antegressa Akhaltsikhe B. antegressa Lesser Caucasus orogenesis T. cocoa. P16 Sp. ps.-lst. rec. BELOGLINIAN Charlesdowniella clathrata anquiosa G. tropicalis- Suite Globig. semi- NP19–20 Eastern Paratethys separation Priabon. Nummulitic Marl Beds with P. costata Gl. corpulenta Suppl. 3 involuta P15 Cheganian EOCENE OLIGOCENECh. oamar. NP18 MIOCENE Microdinium KUMIAN Rh. perforatum Gl. turcmenica 2002 BIOGEOGRAPHY OF THE NORTHERN PERI-TETHYS IN THE EARLY OLIGOCENE S187 keninidae (Hantkenina and Cribrohantkenina), as well ary of the Kiscellian is drawn at the NP20/NP21 bound- as Turborotalia cunialensis and T. cocoaensis. Outside ary, whereas its upper boundary is the lithological the tropical zone, this boundary is difficult to determine boundary between the Kiscel Clay and the finer-grained because of the poor species composition of the Late and shallower Egerian deposits. Eocene Hanthkeninidae assemblages and dominance of globigerinids (Rögl, 1996). No major events in the evo- In Transylvania, the Eocene–Oligocene boundary is lution of nannoplankton occurred at this boundary, based on planktonic data and passes through the upper which is drawn in the lower part of Zone NP21 (after part of the Brebi Marl (Bombita and Rusu, 1981; Rusu Martini, 1971) or within Zone CP16a (after Okada and et al., 1993). However, in the Early Oligocene, shallow- Burky, 1980). The volcanic biotite from the Massig- water carbonate
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