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ISSN 0869-5938, Stratigraphy and Geological Correlation, 2007, Vol. 15, No. 3, pp. 310–320. © Pleiades Publishing, Ltd., 2007. Original Russian Text © L.G. Bragina, Yu.V. Agarkov, N.Yu. Bragin, 2007, published in Stratigrafiya. Geologicheskaya Korrelyatsiya, 2007, Vol. 15, No. 3, pp. 76–86.

Radiolarians of the Upper Cenomanian and Lower Turonian from Deposits of the Ananuri Formation, the Western Caucasus (Lazarevskoe Area) L. G. Braginaa, Yu. V. Agarkovb, and N. Yu. Bragina a Geological

Institute, Russian Academy of Sciences, Moscow, Russia State University, Rostov-on-Don, Russia

b Rostov

Received May 16, 2005; in final form, September 29, 2006

Abstract—Diverse radiolarians (over 70 species) are detected in cherty rocks above the bituminous shale horizon, the marker of anoxic event OAE-2 recorded across the Cenomanian–Turonian boundary in the upper part of the Ananuri Formation of flyschoid deposits, the Lazarevskoe area of the western Caucasus. The radiolarian assemblages studied are comparable in composition with radiolarians from concurrent Cenomanian–Turonian boundary strata in other Mediterranean regions (e.g., in the Crimea and Turkey). The lower radiolarian assemblage includes index species Dactyliosphaera silviae of synonymous Cenomanian zone. Alievium superbum present in the upper assemblage is index species of the relevant Turonian zone. Within the studied flyschoid sequence, sediments indicative of the above event (bituminous shales and cherts) are confined to upper elements of flysch rhythms. DOI: 10.1134/S0869593807030069 Key words: western Caucasus, Cenomanian, Turonian, radiolarians, anoxic events, flysch.

INTRODUCTION Radiolarians of the lower Upper Cretaceous in Tethyan areas (Italy and Spain) have been studied in detail during the last two decades (Erbacher, 1994; O’Dogherty, 1994; Salvini and Marcucci Passerini, 1998). Of special importance is monograph by O’Dogherty (1994) who described dozens of new taxa and revised species originally identified by Squinabol (1903, 1904, 1914). In radiolarian zonation suggested by O’Dogherty for the Barremian–lower Turonian interval, radiolarian subdivisions in the Cenomanian– Turonian transition, where the Oceanic Anoxic Event (OAE-2) of global extent is recorded, are of particular interest (Kuhnt et al., 1986; Schlanger et al., 1987). It is confidently established that this event greatly influenced composition of biota (Vishnevskaya et al., 2006), in particular, of radiolarians (Bragina, 2001). In Italy and Spain, the event is recorded in the so-called “Bonarelli Beds” with elevated content of organic carbon, which represent a reliable regional reference horizon. The Cenomanian–Turonian boundary is defined at the Alievium superbum Zone base exactly in the “Bonarelli Beds.” As is established, termination of the OAE-2 was followed in different regions of the world by quantitative increase of radiolarian productivity, taxonomic diversification of radiolarian assemblages, and by deposition of siliceous radiolarian sediments (O’Dogherty, 1994; Bragina, 1999, 2001).

Bragina (2004) who studied Cenomanian–Turonian radiolarians in the Crimean Mountains and northern Turkey verified taxonomic composition of their assemblages and stratigraphic ranges of certain species. Having distinguished the relevant radiolarian zones in these regions, she failed to establish here subdivisions of subzone rank. It can be assumed therefore that index species of radiolarian subzones recognized in Italy and Spain are of a limited geographic range, but the assumption should be checked on radiolarian successions in other regions. Accordingly, we carried out fieldwork in the Lazarevskoe area of the western Caucasus, where the widespread Upper Cretaceous sequence of deep-water flysch contains radiolarians at different stratigraphic levels. Our attention was concentrated on the Ananuri Formation composed in its upper part of clay and chert beds with interlayers of bituminous shales, the OAE-2 markers. The overlying Kerket Formation is composed in lower interval of flaggy limestone beds with interlayers of radiolarian chert. During fieldwork, we discovered abundant and diverse radiolarian assemblages confined to chert interlayers near the Ananuri Formation top. These assemblages are very suitable for comparison with concurrent assemblages of the Crimea and other Mediterranean regions. Radiolarians of the Greater Caucasus attracted attention of geologists since the 1930s (Vyalov, 1934; Karstens, 1932). To a considerable extent, these are Cenomanian–Turonian radiolarians of the Ananuri

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chert horizon, which extends along southern flank of the Greater Caucasus from Tuapse across Abkhasia, Kutaisi region and South Osetia to Ananuri and further via Kakhetia to southeastern Azerbaijan (Vishnevskaya, et al., 1990, 2006). In the Greater Caucasus western flank, radiolarians have been studied earlier at the base of carbonate sequence exposed along the Ol’khovaya and Khosta rivers, where they are confined to cherts and bituminous marls of the Ananuri Horizon (Vishnevskaya, 2001). Radiolarians confined to topmost horizons of the Ananuri Formation in the Lazarevskoe section have not been studied until this work. We macerated radiolarians from cherts sampled here using conventional method of rocks decomposition in 5% solution of hydrofluoric acid (Nazarov and Vitukhin, 1981).

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In a railway excavation to the northwest of the Station Volkonka, there is exposed the rock succession of the Pauk, Ananuri, and Kerket formations. The upper part of the Ananuri Formation is here of the following structure (from the base upward): (1) Rhythmically alternating sandstones, siltstones, and shales. Gray to greenish gray, medium- and fine-grained sandstones with horizontal, sometimes wavy and cross stratification contain plant detritus confined to bedding planes, the basal of which are decorated with hieroglyphs (individual layers from 1 to 10 cm thick). In gray siltstones with conchoidal fracture, very fine horizontal stratification is emphasized by light-colored sandy laminae. Gray to dark greenish gray shales are calcareous sometimes. In addition, we observed rare beds of gray marl and single layers of black combustible shales foliated and ferruginate. Apparent thickness is 3.7 m, strike NW 290°, dip 30°. (2) Rhythmical interlayering of sandstones, siltstones, shales, combustible shales, and cherts. Gray to brownish gray STRATIGRAPHY AND GEOLOGICAL CORRELATION

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SECTIONS OF ANANURI FORMATION AND DISTRIBUTION OF RADIOLARIANS The thick carbonate–terrigenous flysch of the Upper Cretaceous is a remarkable sedimentary sequence in southern flank of the western Caucasus. Its Cenomanian–Turonian interval is divided here (Agarkov et al., 1992; Afanas’ev and Maslakova, 1967; Vassoevich, 1947; Keller, 1940) into the Pauk (Cenomanian sandstones, siltstones, shales and tuffites), Ananuri (Cenomanian–lower Turonian cherty limestones, cherts, marls, sandstones, siltstones and combustible shales), Kerket (lower Turonian cherty limestones and cherts), and Natukhai (upper Turonian–Coniacian limestones, marls and clays) formations. We studied two sections, one in outskirts of the settlement Lazarevskoe, the Sochi district, and the other one near the settlement Volkonka, the Mamedova Shchel Canyon (Fig. 1), which are similar to each other. Samples for micropaleontological analysis have been collected from upper elements of flyschoid rhythms, i.e., from most finegrained lithologic varieties of sediments. Depending on the rhythm thickness, we collected three to six samples per one meter of the section.

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Fig. 1. Geologic scheme of the Lazarevskoe area, southern flank of the western Caucasus: (1) Maastrichtian, (2) Campanian, (3) upper Turonian–Santonian, (4) upper Cenomanian–lower Turonian (Ananuri and Kerket formations), (5) Cenomanian and Lower Cretaceous deposits; (6) localities of the Volkonka (I) and Mamedova Shchel (II) sections.

fine-grained sandstones with thin horizontal stratification (3– 6 cm) contain small-sized plant detritus at bedding planes. Fine horizontal lamination in gray siltstones (5–15 cm) sometimes grades into vague cross and wavy lamination. Gray to dark and greenish gray laminated shales (1–5 cm) are siliceous in places. Black flaggy laminated combustible shales (2–8 cm) are ferruginate, rusty when weathered, containing fine laminae composed of sulfides and jarosite, pancake-shaped pyrite nodules and dispersed gypsum crystals and rosettes. Their bedding planes are smeared with easily inflammable bitumen. Greenish gray clayey shales (2–5 cm) commonly grade into siliceous shales. Total thickness is 1.5 m. (3) Rhythmical interlayering of siltstones, shales and cherts. Gray to yellowish gray siltstones (2–3 cm) have very fine horizontal lamination. Greenish to yellowish gray shales are foliated (laminae 0.5 cm thick). In radiolarian greenish gray, light yellowish gray and white flaggy cherts clayey sometimes (4–14 cm), fine one-mm-thick horizontal lamination is emphasized by laminae with concentrated radiolarians and dispersed pyrite frequently replacing microfossils. Radiolarians described below are found at two levels: at the level of 45 cm above the bed base (Sample L-2-3) they belong to the Dactyliosphaera silviae assemblage and at the higher level (60 cm above the base) to the Alievium superbum assemblage. Apparent thickness is 0.65 m.

Chocolate brown marls of the Kerket Formation appearing after unexposed section interval 0.5 m thick grade upward into red, pink and light yellow-gray cherty limestones and marls (Fig. 2). Vol. 15

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Fig. 2. Lithologic structure of the Cenomanian–Turonian transition in the Volkonka and Mamedova Shchel sections: (1) sandstones, siltstones and shales; (2) combustible shales; (3) cherts; (4) boundaries between beds described in the text; (5) occurrence levels of radiolarians; (6) bed numbers; (7) sample numbers.

The Dactyliosphaera silviae assemblage includes the following species: Acaeniotyle diaphorogona Foreman, Acanthocircus impolitus O’Dogherty, A. tympanum O’Dogherty, A. sculptus (Squinabol), Archaeocenosphaera ? mellifera O’Dogherty, Cavaspongia antelopensis Pessagno, C. californiaensis Pessagno, Crucella aster (Lipman), C. messinae Pessagno, Dactyliodiscus lenticulatus (Jud), D. longispinus (Squinabol), Halesium quadratum Pessagno, H. sexangulum Pessagno, Orbiculiforma ovoidea Bragina, Paronaella spica Bragina, Patulibracchium ingens (Lipman), Pessagnobrachia irregularis (Squinabol), Phaseliforma

inflata Bragina, Phaseliforma sp. ex gr. P. inflata Bragina, Praeconocaryomma californiaensis Pessagno, P. lipmanae Pessagno, P. universa Pessagno, Pyramispongia glascockensis Pessagno, Quinquecapsularia ombonii (Squinabol), Stylodictya insignis Campbell et Clark, Triactoma cellulosa Foreman, Amphipyndax stocki (Campbell et Clark), Diacanthocapsa antiqua (Squinabol), D. euganea Squinabol, D. fossilis Squinabol, D. ovoidea Dumitrica, D. rara Squinabol, D. sp. A, Dictyomitra montisserei (Squinabol), Distylocapsa squama O’Dogherty, D. veneta (Squinabol), Holocryptocanium astiensis Pessagno, Phalangites telum

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O’Dogherty, Pseudodictyomitra nakasekoi Taketani, P. pseudomacrocephala (Squinabol), Pseudoeucyrtis pulchra (Squinabol), Spongostichomitra elatica O’Dogherty, Stichomitra communis Squinabol, and Xitus spineus Pessagno. None of the taxa obviously prevails over others in the assemblage, and preservation degree of radiolarians is of selective character. For instance, their delicate thin-walled tests are greatly fragmented being inappropriate for precise identification. Nevertheless, these clasts suggest indirectly a much higher taxonomic diversity of radiolarian community at the lifetime. We managed to identify 45 species of the Dactyliosphaera silviae assemblage characteristic of both the upper Cenomanian and lower Turonian deposits in different Tethyan regions, e.g., in Italy, Spain, and Turkey. The assemblage includes a series of species first described by O’Dogherty (1994) from Italy and Spain (Acanthocircus impolitus, A. tympanum, Archaeocenosphaera ? mellifera, Distylocapsa squama, Phalangites telum, Spongostichomitra elatica) and by Bragina (2004) from Turkey (Paronaella spica, Phaseliforma inflata, Orbiculiforma ovoidea), and their geographic ranges can be considered wider therefore. In radiolarian zonation suggested by O’Dogherty (1994) for the Tethyan Superrealm, the Dactyliosphaera silviae Zone of the terminal lower and upper Cenomanian is divided into the lower Patellula spica and upper Guttacapsa biacuta subzones. Zonal index species Dactyliosphaera silviae is present in the studied assemblage, but index species of two subzones have not been detected like in some other Tethyan regions, e.g., in northern Turkey and Crimean Mountains (Bragina, 2004). An interesting feature of our assemblage is last occurrence of Spongostichomitra elatica, the species not recorded above the lower Cenomanian in sections of Italy and Spain (O’Dogherty, 1994), in association with Diacanthocapsa antiqua and Pseudoeucyrtis pulchra regarded to be very characteristic of the upper Cenomanian (O’Dogherty, 1994). Of particular interest is presence of Acanthocircus tympanum that appears in sections of Italy and Spain concurrently with Alievium superbum, the index taxon of the synonymous Turonian zone. Taking into account the established coexistence of Dactyliosphaera silviae, the index species of synonymous Cenomanian zone, and Acanthocircus tympanum characteristic of the Turonian, it is possible to suggest that the described assemblage corresponds in age to the terminal Cenomanian. The Alievium superbum assemblage includes many species of the Dactyliosphaera silviae assemblage being simultaneously enriched in radiolarians, which do not occur at the lower level. These are Acaeniotyle macrospina (Squinabol), Alievium superbum (Squinabol), A. cf. sp. A. superbum (Squinabol), Cavaspongia contracta O’Dogherty, Crucella cachensis Pessagno, Patellula verteroensis (Pessagno), Pessagnobrachia rara (Squinabol), Phaseliforma subcarinata Pessagno, STRATIGRAPHY AND GEOLOGICAL CORRELATION

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Pseudoaulophacus floresensis Pessagno, P. praefloresensis Pessagno, Triactoma compressa (Squinabol), T. fragilis Bragina, T. hexeris O’Dogherty, Vitorfus brustolensis (Squinabol), V. morini Empson-Morin, Archaeodictyomitra sliteri (Squinabol), A. sp. ex gr. A. squinaboli Pessagno, Cryptamphorella conara (Foreman), C. sphaerica (White), Diacanthocapsa elongata Bragina, Holocryptocanium barbui Dumitrica, Phalangites hastatus O’Dogherty, Pogonias ? hirsutus (Squinabol), Squinabollum fossile (Squinabol), Stichomitra insignis Squinabol, S. magna Squinabol, Thanarla sp. ex gr. T. conica (Aliev), Tubilustrium transmontanum O’Dogherty, and Xitus spicularius (Aliev). The assemblage under consideration consists of 73 species, the majority of which (60%) is known from Cenomanian and lower Turonian deposits of the Tethys. Nearly all the newcomers are also widespread in the same stratigraphic intervals. Radiolarians of the Alievium superbum assemblage are preserved rather well, as very fragile tests representing the genus Vitorfus are present among them. However, delicate thinwalled morphotypes are dilapidated and hardly identifiable. The assemblage includes species Phaseliforma inflata and Diacanthocapsa elongata described from the Cenomanian of Turkey (Bragina, 2004), Triactoma fragilis known from the Santonian–Campanian of Cyprus (Bragina and Bragin, 1996) and found also in the Cenomanian of Turkey (Bragina, 2004). Species Paronaella spica occurs in the Cenomanian of northern Turkey and in the lower Turonian of the Crimean Mountains (Bragina, 2004). The age interpretation of the Alievium superbum assemblage is based on coexistence of (1) Dactyliosphaera silviae, the index species of synonymous Cenomanian zone unknown from the Turonian of Italy and Spain, and (2) Alievium superbum, the index species of synonymous Turonian zone (Pessagno, 1976; O’Dogherty, 1994). Based on association of these two taxa, we assume that the Alievium superbum assemblage corresponds in age to earliest Turonian time, when first species Alievium superbum appeared to join still existing Dactyliosphaera silviae forms. At the Mamedova Shchel site 2.5 km upstream of the Kuapse River mouth, there are sporadic outcrops of the Aptian–Albian terrigenous deposits and overlying rocks of the Pauk Formation. The Ananuri Formation upper part and the entire Kerket Formation are observable further upstream in a continuous exposure. Transition between the last two formations is of the following structure here (from the base upward, Fig. 2): (1) Rhythmical interlayering of limestones, marls and shales. Greenish gray limestones (10–30 cm) are clay-cherty, aphanitic. Green to greenish gray layers of marl are thin (2– 15 cm). Gray to dark gray shales (2–6 cm) are foliated. Apparent thickness is 0.7 m. (2) Rhythmical interlayering of sandstones, siltstones, shales and combustible shales. Beds of gray fine-grained sandstones (2–10 cm) with hieroglyphs at the base have horizontal and more rare wavy and cross lamination. Dark gray, Vol. 15

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gray and greenish gray siltstones and shales (1–15 cm) are thin-laminated, foliated, sometimes calcareous, grading into marls. Black combustible shales (1–5 cm) are flaggy, foliated, containing jarosite at foliation planes. Thickness is 3.25 m. (3) Rhythmical interlayering of sandstones, marls, limestones and cherts. Gray fine-grained sandstones have fine horizontal stratification (0.5–1 cm). Gray to greenish gray marls (5–15 cm) contain fucoids. Greenish to yellowish gray limestones (2–15 cm) are cherty and flaggy. In greenish, yellowish and reddish gray, banded radiolarian cherts (5–15 cm) with fine horizontal lamination, radiolarians are concentrated in separate laminae. Total thickness is 1.4 m.

The above beds 1–3 belong to the Ananuri Formation and are overlain by reddish, yellowish and greenish limestones and marls of the Kerket Formation. We studied radiolarians from two levels of Bed 3: 55 cm (Sample L-3-9) and 1 m (Sample L-3-12) above the bed base. The radiolarian assemblages from the Mamedova Shchel section are less representative in general than their counterparts from the Volkonka section most likely due to a worse preservation of radiolarian skeletons. The lower assemblage (Sample L-3-9) includes Archaeocenosphaera ? mellifera O’Dogherty, Crucella irwini Pessagno, Godia coronata (Tumanda), Halesium sexangulum Pessagno, Patulibracchium woodlandensis Pessagno, Phaseliforma inflata Bragina, Praeconocaryomma lipmanae Pessagno, Protoxiphotractus cf. sp. P. ventosus Pessagno, Pyramispongia glascockensis Pessagno, Cryptamphorella sphaerica (White), Diacanthocapsa antiqua (Squinabol), D. elongata Bragina, Distylocapsa squama O’Dogherty, Pseudodictyomitra pseudomacrocephala (Squinabol), Squinabollum fossile (Squinabol), Stichomitra communis Squinabol, and Xitus spicularius (Aliev). The assemblage includes 17 species, many of which are universally widespread in the Cenomanian of the Tethyan Superrealm. Diacanthocapsa elongata Bragina that is present in the assemblage and has been originally described from Cenomanian deposits of northern Turkey (Bragina, 2004) extends geographic range of this species. The assemblage is lacking index species of Cenomanian and Turonian radiolarian zones, and its stratigraphic range cannot be defined precisely. Presumable age limits are the late Cenomanian and early Turonian, because the greater part of listed species is characteristic of both time spans. The assemblage occurring 0.45 m higher in the section includes nearly all the species of previous assemblage. Species unknown below and first occurring at

this level are Acanthocircus tympanum O’Dogherty, Alievium sculptus (Squinabol), A. sp. cf. A. superbum (Squinabol), Archaeospongoprunum sp. A, Cavaspongia antelopensis Pessagno, C. californiaensis Pessagno, C. euganea (Squinabol), Crucella cachensis Pessagno, C. messinae Pessagno, C. aff. C. messinae Pessagno, Patellula verteroensis (Pessagno), Pessagnobracchia irregularis (Squinabol), Phaseliforma sp. ex gr. P. inflata Bragina, Praeconocaryomma sp. ex gr. P. lipmanae Pessagno, Pseudoacanthosphaera galeata O’Dogherty, Pseudoaulophacus praefloresensis Pessagno, P. putahensis Pessagno, Amphipyndax stocki (Campbell et Clark), Diacanthocapsa sp. ex gr. D. antiqua (Squinabol), D. brevithorax Dumitrica, D. sp. ex gr. D. elongata Bragina, D. cf. ex gr. D. fossilis (Squinabol), Dictyomitra sp. ex gr. D. densicostata Pessagno, Holocryptocanium barbui Dumitrica, and Stichomitra insignis (Squinabol). The assemblage includes 43 species in total, but well-preserved specimens of Alievium superbum have not been detected, and we managed to identify only Alievium cf. sp. A. superbum. As Acanthocircus tympanum is found in association with species widespread in the Cenomanian–Turonian transition, their host deposits span the late Cenomanian–early Turonian interval in our interpretation. Thus, the described radiolarian assemblages surely prove the upper Cenomanian–lower Turonian stratigraphic range of the Ananuri Formation upper part, and relevant combustible shales can be interpreted as sediments of the OAE-2. The last inference is important for comparative analysis of this event recorded in different sections and facies of the Mediterranean region. Sections with the OAE-2 records are comprehensively studied in Italy, where this event took place in a relatively deep basin with slow hemipelagic sedimentation in quiet environments (O’Dogherty, 1994). In upper part of the Scaglia Bianca Formation (middle Albian–lower Turonian) represented by fairly thin (65– 70 m) sequence of alternating micritic limestones and cherty rocks, there have been distinguished the socalled “Bonarelli Beds” with interlayers of bituminous shales most carefully studied in the Gorgo a Cerbara, Gola del Bottaccione, and Monte Casalini sections of the Umbria–Marche Apennines (O’Dogherty, 1994). The Bonarelli Beds are of the following structure in these sections: (1) lower interval (30–100 cm) of lightcolored siliceous shales, siltstones and radiolarites with minor admixture of organic matter; (2) middle interval (30–100 cm) of black shales enriched in organic matter and phosphorus, frequently containing fish remains;

Radiolarians of the Cenomanian–Turonian transition in the Volkonka section, southern flank of the western Caucasus (Volkonka section, plates 1, 2). P l a t e I. (1) Acanthocircus tympanum O’Dogherty, ×200; (2) Acanthocircus impolitus O’Dogherty, ×200; (3) Archaeocenosphaera ? mellifera O’Dogherty, ×150; (4, 5) Acaeniotyle macrospina (Squinabol), ×300; (6) Phaseliforma sp. ex gr. P. inflata Bragina, ×150; (7) Multastrum sp. ex gr. M. regalis Vishnevskaya, ×200; (8) Pseudoacanthosphaera sp. ex gr. P. magnifica (Squinabol), ×100; (9) Pessagnobracchia irregularis (Squinabol), ×150; (10) Crucella messinae Pessagno, ×200. Figs. (1, 4, 5, 9) – Turonian; fig. (10) – upper Cenomanian. STRATIGRAPHY AND GEOLOGICAL CORRELATION

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(3) upper interval (10–30 cm) of radiolarian shales, siltstones and cherts. Within the last interval, concentration of organic matter declines gradually upward, while content of carbonate components increases. A similar horizon corresponding to the OAE-2 is known in sections of the southwestern Crimea (Naidin and Alekseev, 1980; Naidin et al., 1981; Naidin and Kiyashko, 1994a, 1994b), which are composed of alternating limestone and marl beds. A horizon of black bituminous marls, which contain fish remains and laterally grade into marls with elevated content of organic matter, is locally observable here at the level of the Cenomanian–Turonian boundary. In sections of the Mt. Selbukhra and Mt. Belaya, this horizon is overlain by bed (20–30 cm) of cherty and highly silicified limestones with radiolarians. Despite certain distinctions in structure and lithologic composition, sections of the Crimea and Italy reveal an important feature in common: bituminous shales grade upward into cherty sediments with radiolarians crowned by carbonate deposits. In southern flank of the western Caucasus, sections of the Ananuri Formation have been deposited in deepwater settings under conditions of intense influx of clastic material (Afanas’ev, 2004). Sedimentation rate was much higher here than in the southwestern Crimea. In the Volkonka and Mamedova Shchel sections, the OAE-2 is recorded against background of concurrent flyschoid sedimentation. As a result, we observe here not one but several horizons of combustible shales representing crowning elements D or E in typical rhythms of turbidity flysch (Bouma, 1962) that characterizes completely or partially the background sedimentation in the basin. The lower elements of rhythms (A, B, C) composed of sandstones with graded bedding and finegrained siltstones are lacking signs of the OAE-2, although it is clear that this event was concurrent to but independent of the turbidity sedimentation. In a similar manner, radiolarian cherts appearing above last horizons of combustible shales are confined to terminal elements of flyschoid rhythms. As a consequence, total thickness of sediments deposited at the OAE-2 time in southern flank of the western Caucasus is essentially greater than in Italy, for instance, and their lithologic composition is much more diverse because of deposition of siliciclastic material. Nevertheless, the general trend of sedimentogenesis first established in the Bonarelli Beds and corresponding to lithologic succession of bituminous shales, radiolarian cherts and carbonate rocks almost lacking organic matter is traceable in the studied sections as well. Accordingly, the anoxic event (OAE-2) was similarly manifested in different

settings of deep-sea basin: in a zone of hemipelagic or even pelagic sedimentation (Italy), shelf zone (Crimea), and a relatively deep flysch trough (southern flank of the western Caucasus). Data on taxonomic diversity of radiolarian assemblages from different sections of the Tethys elucidates paleogeography of these fossil organisms. There is no doubt of course that Tethyan basins have been largely populated by identical radiolarian taxa. Nevertheless, it is possible to state even now that concurrent radiolarian assemblages were dissimilar to a certain extent. For example, comprehensive study of the middle–upper Cenomanian radiolarians in northern Turkey (Bragina, 2004) showed that 32 species of their assemblages are unknown in concurrent deposits of Italy and Spain. Preliminary data on the Cenomanian–Turonian radiolarians from the Perapedhi and Moni formations of Cyprus (Bragina and Bragin, 2006) also imply that some of their species do not occur in the Crimean Mountains, Turkey (Bragina, 2004), Italy and Spain (Erbacher, 1994; O’Dogherty, 1994; Salvini and Marcucci Passerini, 1998). In this work, some radiolarian taxa from the southwestern Caucasus are identified in open nomenclature and need subsequent systematic description. Despite the taxonomic diversity of upper Cenomanian–lower Turonian radiolarians in the study objects, we failed to detect among them the index species of the Guttacapsa biacuta Subzone (established by O’Dogherty in the upper Cenomanian of Italy and Spain) in either the Volkonka or the Mamedova Shchel sections. The studied assemblages are lacking also some other species (Sciadiocapsa pertica, Diacanthocapsa matsumotoi, Dictyomitra crassispina) typical of this subzone. As Guttacapsa biacuta is unknown as well in the Crimean Mountains and northern Turkey, we suspect that the relevant subzone is of a limited geographic range. SOME CHARACTERISTIC RADIOLARIAN SPECIES Acanthocircus tympanum O’Dogherty, 1994, emend. Bragina, 2004 Plate I, fig. 1

Mesosaturnalis sp.: Erbacher, 1994, pl. 19, figs. 6, 7. Acanthocircus tympanum: O’Dogherty, 1994, p. 259, pl. 45, figs. 17–24; Salvini and Marcucci Passerini, 1998, Fig. 8.p; Bragina, 2004, pl. 34, fig. 15. Distribution: lower Turonian of Italy and Spain; lower Turonian of the Crimean Mountains; uppermost Cenomanian–basal Turonian of the western Caucasus.

P l a t e II. (1) Pseudoaulophacus praefloresensis Pessagno, ×200; (2) Alievium cf. sp. A. superbum (Squinabol), ×200; (2) Cavaspongia californiaensis Pessagno, ×200; (3) Crucella messinae Pessagno, ×250; (5, 6) Dictyomitra cf. sp. D. multicostata Zittel, ×120 (both); (7) Pseudodictyomitra pseudomacrocephala (Squinabol), ×150; (8) Diacanthocapsa euganea Squinabol, ×200; (9) Diacanthocapsa sp. A, ×200; (10) Diacanthocapsa brevithorax Dumitrica, ×250; (11, 12) Diacanthocapsa antiqua (Squinabol), ×200 (both); (13) Squinabollum fossile (Squinabol), ×250; (14) Distylocapsa squama O’Dogherty, ×200. Figs. (1–9,13)—Turonian; figs. (10–12,14) – Cenomanian. STRATIGRAPHY AND GEOLOGICAL CORRELATION

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4 7

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Material: over 10 specimens.

Phaseliforma sp. ex gr. P. inflata Bragina, 2004

Alievium sp. cf. A. superbum (Squinabol, 1914) Plate II, fig. 2

Remark. This form lacking spines is incompletely preserved. Nevertheless, the outer structure of shell and basal tubercles of lost spines are typical of the indicated species. Distribution: lower Turonian of the western Caucasus. Material: 2 specimens. Multastrum sp. ex gr. M. regalis Vishnevskaya, 2001 Plate I, fig. 7

Hagiastridae gen. et sp. indet: Taketani, 1982, p. 50, pl. 10, fig. 3. Multastrum sp.: Kurilov, 2005, Plate 32, fig. 19.; Vishnevskaya et al., 2005, Plate 13. fig. 5. Material: 3 specimens. Crucella messinae Pessagno, 1971 Plate II, fig. 4

Crucella messinae: Pessagno, 1971, p. 56, pl. 6, figs. 1–3; 1976, p. 32, pl. 1, fig. 4 (= holotype refigured); Pessagno, 1977, p. 27, pl. 1, figs. 3, 4, 13; O’Dogherty, 1994, p. 368, pl. 70, figs. 21–24; Bragina, 2004, pl. 23, figs. 1, 2; pl. 38, fig. 5. Non Crucella messinae: Taketani, 1982, p. 50, pl. 9, fig. 17 (= C. irwini Pessagno, 1971) Distribution: lower Cenomanian of California; Albian–Cenomanian of Italy, Spain, and Atlantic Ocean; middle–upper Cenomanian of northern Turkey; upper Cenomanian–lower Turonian of the Crimean Mountains; uppermost Cenomanian–lower Turonian of the western Caucasus; undivided Coniacian–Campanian of the Russian plate. Material: over 5 specimens. Archaeocenosphaera ? mellifera O’Dogherty, 1994 Plate I, fig. 3

Hemicryptocapsa sp. A: Marcucci and Gardin, 1992, text-fig. 3. 1. Archaeocenosphaera ? mellifera: O’Dogherty, 1994, p. 375, pl. 74, figs. 1–5; Salvini and Marcucci Passerini, 1998, Fig. 7.o; Bragina, 2004, pl. 14, fig. 3; pl. 36, fig. 14. Distribution: Cenomanian–Campanian worldwide; middle Albian–lower Turonian of Italy and Spain; middle–upper Cenomanian of northern Turkey; upper Cenomanian–lower Turonian of the Crimean Mountains; upper Cenomanian–lower Turonian of the western Caucasus; upper Cenomanian–lower Turonian, undivided Coniacian–Campanian of the Russian plate. Material: less than 10 specimens.

Plate I, fig. 6

Remarks. In shape and shell size, this form is similar to Phaseliforma inflata but has in distinction the quadrangle to heptagon knobs or relief projections. Material: over 6 specimens. Diacanthocapsa antiqua (Squinabol, 1903), emend. Bragina, 2004 Plate II, fig. 11,12

Theocorys antiqua: Squinabol, 1903, p. 135, pl. 8, fig. 25. Diacanthocapsa antiqua: O’Dogherty, 1994, p. 220, pl. 36, figs. 25–28; Bragina, 2004, pl. 10, figs. 3, 7; pl. 31, figs. 11, 12; pl. 32, fig. 2. Distribution: upper Albian–lower Turonian of Italy and Spain; upper Cenomanian of northern Turkey; upper Cenomanian–lower Turonian of the western Caucasus, lower Turonian of the Crimean Mountains. Material: over 6 specimens. Squinabollum fossile (Squinabol, 1903), emend. Bragina, 2004 Plate II, fig. 13

Clistosphaera fossilis: Squinabol, 1903, p. 130, pl. 10, fig. 11. Squinabollum fossilis: Dumitrica, 1970, p. 83, pl. 19, figs. 118a–118c, 119a–119c; Teraoka and Kurimoto, 1986, pl. 4, fig. 4; Salvini and Marcucci Passerini, 1998, Fig. 6.s; Kazintsova, 1993, p. 66, pl. XV, fig. 7. Non Squinabollum fossilis: Vishnevskaya, 2001, pl. 22, figs. 7–11 (Sethocapsa?). Squinabollum fossile: O’Dogherty, 1994, p. 203, pl. 32, figs. 4–10; Bragina, 2004, pl. 12, figs. 1–4. Remark. Three or more sizeable spines in distal part of abdomen are oriented backward from cephalis. Distribution: Albian–Santonian worldwide; upper Cenomanian of northern Turkey; lower Turonian of the Crimean Mountains; uppermost Cenomanian–lower Turonian of the western Caucasus; upper Santonian of the southwestern Sakhalin (Bragina, 2001). Material: 6 specimens Pseudodictyomitra pseudomacrocephala (Squinabol, 1903) Plate II, fig. 7

Dictyomitra pseudomacrocephala: Squinabol, 1903, p. 139, pl. 10, fig. 2; Petrushevskaya and Kozlova, 1972, p. 550, pl. 2, fig. 5. Pseudodictyomitra pseudomacrocephala: Pessagno, 1977, p. 51, pl. 8, figs. 10, 11 (= specimens of Pessagno, 1976, pl. 3, figs. 2, 3); Teraoka, Kurimoto, 1986, pl. 4, figs. 10, 11; O’Dogherty, 1994, p. 108, pl. 8, figs. 5–8; Salvini and Marcucci Passerini, 1998,


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Fig. 8.h; Vishnevskaya, 2001, pl. 129, figs. 5, 9; Bragina, 2004, pl. 7, fig. 4; pl. 32, figs. 9, 14–16. Distribution: upper Albian–lower Turonian worldwide; middle–upper Cenomanian of northern Turkey; upper Cenomanian–lower Turonian of the Crimean Mountains; uppermost Cenomanian–lower Turonian of the western Caucasus. Material: over 10 specimens.

10.

11.

Distylocapsa squama O’Dogherty, 1994, emend. Bragina, 2004

12.

Plate II, fig. 14

13.

Distylocapsa squama: O’Dogherty, 1994, p. 188, pl. 28, figs. 16–21; Salvini and Marcucci Passerini, 1998, Fig. 9.s; Bragina, 2004, pl. 4, fig. 6. Distribution: upper Albian–lower Turonian of Italy and Spain; upper Cenomanian of northern Turkey; uppermost Cenomanian–lower Turonian of the western Caucasus; lower Turonian of the Crimean Mountains. ACKNOWLEDGMENTS The work was supported by the Russian Foundation for Basic Research, project no. 03-05-64964. Reviewers A.S. Alekseev and V.A. Zakharov REFERENCES 1. S. L. Afanas’ev, Geology of the Western Caucasus (Voentekhizdat, Moscow, 2004) [in Russian]. 2. S. L. Afanas’ev and N. I. Maslakova, “Upper Cretaceous Deposits in the Northwestern Caucasus,” Tr. Vsesoyuzn. Zaochn. Politekh. Inst., Ser. Gidrogeol. Eng. Geol. 37, 106–136 (1967). 3. Yu. V. Agarkov, N. I. Boiko, and V. I. Sedletskii, Cherty Rocks of the Northern Caucasus and Potential Practical Use (Rostov. Gos. Univ., Rostov-on-Don, 1992) [in Russian]. 4. A. H. Bouma, Sedimentology of Some Flysch Deposits. A Graphic Approach to Facies Interpretation (Elsevier, Amsterdam, 1962). 5. L. G. Bragina, “Cenomanian and Turonian Radiolarians from the Crimean Mountains,” Byull. Mosk. O–va Ispyt. Prir., Otd. Geol. 74 (3), 43–50 (1999). 6. L. G. Bragina, Extended Abstract of Candidate’s Dissertation in Geology and Mineralogy (GIN RAN, Moscow, 2001). 7. L. G. Bragina, “Cenomanian–Turonian Radiolarians of Northern Turkey and the Crimean Mountains,” Paleontol. J. 38 (Suppl. 4), 325–456 (2004). 8. L. G. Bragina and N. Yu. Bragin, “Stratigraphy and Radiolarians from the Type Section of Perapedhi Formation (Upper Cretaceous of Cyprus),” Stratigr. Geol. Korrelyatsiya 4 (3), 38–45 (1996) [Stratigr. Geol. Correlation 4 (3), 246–253 (1996)]. 9. L. G. Bragina and N. Yu. Bragin, “Stratigraphy and Radiolarians of Upper Cretaceous Sedimentary Cover of the Arakapas Ophiolite Massif (Cyprus),” Stratigr. Geol. STRATIGRAPHY AND GEOLOGICAL CORRELATION

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