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Upper Cretaceous Deposits in the Northwest of Saratov Region, Part 2: Problems of Chronostratigraphy and Regional Geological History A

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Upper Cretaceous Deposits in the Northwest of Saratov Region, Part 2: Problems of Chronostratigraphy and Regional Geological History A ISSN 0869-5938, Stratigraphy and Geological Correlation, 2008, Vol. 16, No. 3, pp. 267–294. © Pleiades Publishing, Ltd., 2008. Original Russian Text © A.G. Olfer’ev, V.N. Beniamovski, V.S. Vishnevskaya, A.V. Ivanov, L.F. Kopaevich, M.N. Ovechkina, E.M. Pervushov, V.B. Sel’tser, E.M. Tesakova, V.M. Kharitonov, E.A. Shcherbinina, 2008, published in Stratigrafiya. Geologicheskaya Korrelyatsiya, 2008, Vol. 16, No. 3, pp. 47–74. Upper Cretaceous Deposits in the Northwest of Saratov Region, Part 2: Problems of Chronostratigraphy and Regional Geological History A. G. Olfer’eva, V. N. Beniamovskib, V. S. Vishnevskayab, A. V. Ivanovc, L. F. Kopaevichd, M. N. Ovechkinaa, E. M. Pervushovc, V. B. Sel’tserc, E. M. Tesakovad, V. M. Kharitonovc, and E. A. Shcherbininab a Paleontological Institute, Russian Academy of Sciences, Profsoyuznaya ul. 123, Moscow, 117997 Russia b Geological Institute, Russian Academy of Sciences, Pyzhevskii per. 7, Moscow, 119017 Russia c Saratov State University, Astrakhanskaya ul., 83, Saratov, 410012 Russia d Moscow State University, Vorob’evy Gory, Moscow, 119991 Russia Received November 7, 2006; in final form, March 21, 2007 Abstract—Problems of geochronological correlation are considered for the formations established in the study region with due account for data on the Mezino-Lapshinovka, Lokh and Teplovka sections studied earlier on the northwest of the Saratov region. New paleontological data are used to define more precisely stratigraphic ranges of some stratigraphic subdivisions, to consider correlation between standard and local zones established for different groups of fossils, and to suggest how the Upper Cretaceous regional scale of the East European platform can be improved. Considered in addition are paleogeographic environments in the study region during the Late Cretaceous epoch and principal stages of the regional geological evolution. DOI: 10.1134/S0869593808030040 Key words: Turonian, Coniacian, Santonian, Campanian and Maastrichtian stages; Bannovka, Mozzhevelovyi Ovrag, Mezino-Lapshinovka, Rybushka, Ardym and Lokh formations; Borisoglebsk Sequence; chronostratig- raphy, tectonic history, and paleogeography. This work is continuation of the first part (Olfer’ev northwest of the Saratov region and to get insight into et al., 2007),1 where we considered characterization of general composition of the Late Cretaceous biota. Cor- regional stratigraphic subdivisions of the Upper Creta- relation with the general scale is based on the standard ceous, the first distinguished Borisoglebsk Sequence ammonoid zonation (Olfer’ev and Alekseev, 2002). inclusive, and biostratigraphic zonations for different Geochronological dates for biostratigraphic zones are groups of fossils in the Vishnevoe section. estimated based on the work by Hardenbol et al. (1998) Lithostratigraphy of the Vishnevoe section is well and used for chronometric calibration of boundaries correlative with the local stratigraphic chart approved separating local zones of mollusks and benthic fora- for western part of the Ul’yanovsk–Saratov depression minifers in the regional scale for the East European (Stratigraphic Chart…, 2004). Characteristic features platform (Figs. 4, 5; Olfer’ev and Alekseev, 2003). The enabling identification of all subdivisions in the section Late Cretaceous paleogeographic environments in the (Melovatka, Bannovka, Mozzhevelovyi Ovrag, Mez- Volga River basin are considered, the trend and possible ino-Lapshinovka, Rybushka, Ardym and Lokh forma- factors of sea-level fluctuations are discussed, and the tions) are known from that chart. An exception is the regional geological history is elucidated. Borisoglebsk Sequence distinguished for the first time in the section and formerly known in the Tambov and Khoper monoclines only. MAIN BIOSTRATIGRAPHIC MARKERS In this work, we consider biotic events recorded not Melovatka Formation (Cenomanian) only in the Vishnevoe section, but also in the Lokh, Teplovka (Alekseev et al., 1999) and Mezino-Lapshi- The Melovatka Formation 68 to 78 m thick is unex- novka (Olfer’ev et al., 2004) sections studied earlier. posed in the currently studied section. The respective Paleontological data on these sections are used to spec- sediments have been recovered by survey boreholes (4, ify ranges of some local subdivisions known on the 7, 19 and 26) in the Petrovsk area (map sheet N-38- XXXIV). Zozyrev (2006) divided the formation into 1 See “Stratigraphy and Geological Correlation,” 15 (6), 2007. three units: the lower (Medveditsa), middle (Krasno- 267 268 OLFER’EV et al. yar), and upper (Kalininsk) subformations. Sediments penetrated via tracks of burrowing organisms from of the lower subformation (13–16 m) commonly rest on sands of Bed 42 of the overlying Borisoglebsk eroded surface of the Albian deposits that is evident Sequence. Accordingly, the Bannovka Formation from basal accumulations of phosphorite nodules. This should be attributed, like everywhere in the Saratov subformation is composed of fine-grained glauconite- region near Volga River, to the middle–upper Turonian quartz sands with thin aleurite and clay interlayers. that is consistent with the fact that inoceramids of the Sands recovered by Borehole 4 (Berezovka site) con- Mytiloides labiatus local zone have never been found in tain foraminifers Gavelinella cenomanica (Brotz.), Val- its basal part (Kharitonov et al., 2001, 2003). vulineria lenticula (Reuss), and Marginulina jonesi Reuss of the Gavelinella cenomanica local zone. The Nevertheless, new data on the Lokh section situated middle subformation of dark gray sandy clay grading 20 km to the east-northeast of the Vishnevoe section upward into greenish gray micaceous clayey aleurite is point to doubtable status of the above dating. Sandy 27 to 38 m thick. At the Antipovka site (Borehole 19), grumous chalk grading into calcareous sand (0.9 m) is these sediments contain, in addition to pectinacean exposed here below soil and overlies with a sharp con- bivalves Entolium orbiculare (Sow.), the foraminifers tact the glauconite-quartz sand of the Cenomanian Lingulogavelinella globosa (Brotz.) and Valvulineria Melovatka Formation. The sandy chalk yielded rostrum lenticular of the Lingulogavelinella globosa local zone. Goniocamax intermedius (Arkh.) and foraminifers The upper subformation (15–29 m) is represented by Whiteinella holzli (Hagn et Zeil), Hedbergella baltica fine-grained feldspar-quartz sandstones containing (Dougl.), Globorotalites hangensis Vass., Pseudoval- glauconite admixture and foraminifers of the L. glo- vulineria nana (Akim.), Lingulogavelinella globosa, bosa local zone. Sands of Bed 44 formerly exposed in Gavelinella vesca (Bykova) and others of the Globoro- ravine near the Vishnevoe village should be attributed talites hangensis/Pseudovalvulineria nana local zone. to this subformation. In the standard borehole logs, the According to Beniamovski (2006), this lower Turonian lower and upper subformations are easily recognizable, zone is correlative with two lower local zones of the as they are marked by distinct positive anomalies of Turonian molluscan fauna. If this correlation is correct, apparent resistance in contrast to clays of the upper then stratigraphic range of the Bannovka Formation Albian and middle (Melovatka) subformation. must be spanning the entire Turonian. According to conclusion of S.S. Dem’yankov, nannoplankton from the Lokh section is represented by species of wide Bannovka Formation (Turonian) stratigraphic ranges, but it includes Kamptnerius mag- nificus, the form that appears in the Pseudaspidoceras This stratigraphic unite of the Vishnevoe section has flexuosum Zone of the lower Turonian (Burnett, 1998). been studied only in its terminal part (0.5 m) that bears assemblages of foraminifers and calcareous nanno- plankton. Foraminifers are typical of upper part of the Borisoglebsk Sequence (middle–upper Coniacian) Turonian Gavelinella moniliformis local zone that is inferable from occurrence of Ataxoorbignyna nauti- The middle–upper Coniacian range of this strati- loides, Osangularia whitei praeceps, and Reussella graphic subdivision is confirmed by occurrence of for- kelleri, the taxa characteristic of the Coniacian and aminiferal assemblage characteristic of the middle appearing in the uppermost Turonian of the Russian Coniacian (s. str.) Gavelinella thalmanni local zone and plate (Golubtsov et al., 1978; Olfer’ev et al., 2004). On lower part of the Gavelinella infrasantonica/Stensioe- the other hand, the foraminiferal assemblage includes ina exsculpta exsculpta Zone distinguished by Beniam- species typical of the overlying Gavelinella kelleri ovski (2006) in the terminal Coniacian–lower Santo- local zone of the lower Coniacian. Koval’skii and nian. In the assemblage, Stensioeina emscherica, Gav- Ochev (1980) who studied foraminifers from chalk-like elinella costulata, G. thalmanni, abundant Osangularia marl with inoceramids in the Vishnevoe site were of the whitei whitei (Brotz.) and O. whitei praeceps are asso- same opinion. ciated with typical upper Coniacian Bolivinopsis Calcareous nannofossils suggest somewhat differ- embaensis, Gavelinella vombensis, and Santonian ent age for marls of the Bannovka Formation. In addi- Praebulimina ventricosa (Brotz.), which are identified tion to the middle–upper Turonian species Lithastrinus in Sample 31. Among these species, there is also Pal- septenarius, Lucianorhabdus maleformis Reinhardt, mula baudouiniana, the upper distribution limit of Eiffellithus eximius (Stover) Perch-Nielsen, and which is constrained
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