Cent. Eur. J. Geosci. • 4(1) • 2012 • 188-204 DOI: 10.2478/s13533-011-0065-8

Central European Journal of Geosciences

Middle–Upper Miocene stratigraphy of the Taman Peninsula, Eastern Paratethys

Research Article

Eleonora P. Radionova1∗, Larisa A. Golovina1, Natalia Yu. Filippova1, Valery M. Trubikhin1, Sergey V. Popov2, Irina A. Goncharova2, Yulia V. Vernigorova3, Tatiana N. Pinchuk4

1 Geological Institute RAS, Pyzhevskii 7, Moscow, Russia 2 Paleontological Institute RAS, Profsoyuznaya 123, Moscow, Russia 3 Institute of Geological Sciences NAS, O. Gonchara 55, Kiev, Ukraine 4 Kuban University, Krasnodar, Russia

Received 3 November 2011; accepted 5 March 2012

Abstract: The stratigraphy of the Taman Peninsula is defined using the sections at Zelensky Hill – Panagia, Popov Kamen, Taman and Zheleznyi Rog. The stratigraphy is constructed from distribution of mollusks, foraminifers, nannofos- sils, diatoms, and organic-walled phytoplankton, as well as incorporating paleomagnetic data. The occurrence of oceanic diatom species in the Middle-Upper Sarmatian, Maeotian and Lower Pontian makes a direct corre- lation possible between the sections studied, the Mediterranean basin and oceanic zonation. The new data on planktonic and benthic biotic groups suggests a pulsating connection of the Eastern Paratethys with the open marine basins, especially during transitional intervals within constant environments. Comprehensive studies of the Chokrakian–Kimmerian microbiota provide evidence for several levels of marine microbiotic associations that are related to short-term marine invasions. The biotic and paleomagnetic data of the Taman Peninsula sections give a more comprehensive, but sometimes a controversial picture on the Eastern Paratethys history and the nature of its relationship with the adjacent marine basins. Keywords: Euxinian basin • Neogene • biostratigraphy • magnetostratigraphy • mollusks • foraminifers • nannofossils • diatoms • organic-walled phytoplankton © Versita sp. z o.o.

1. Introduction chronization of geological events, both within the East- ern Paratethys and in the adjacent regions of the Cen- tral Paratethys, Mediterranean, and the World Ocean. N.I. Andrusov [2,3, 5, 6] has successfully developed the The Eastern Paratethys in the Neogene and Quaternary Miocene regional stratigraphy of the Eastern Paratethys was represented by a series of isolated or semi-isolated and distinguished the horizons based on changes of mol- basins. The major problem with Neogene stratigraphy lusk associations that represented different bionomic con- in this region is the correlation of deposits and the syn- ditions and hydrological regimes. To date, these re- gional horizons (currently regional stages) are recog- nized throughout the entire Eastern Paratethys. Andrusov ∗E-mail: [email protected]

188 E.P. Radionova et al.

has also revealed the cyclicity of the basin. The Neo- gene history of the Eastern Paratethys is divided into the Tarkhanian—Karaganian, Konkian—Sarmatian, and Maeotian transgressive-regressive cycles. The beginning of each cycle is marked by the accumulation of sediments bearing marine fauna, which indicates a connection with the open-marine basin, and the termination is charac- terized by deposits with endemic brackish- or marginal- marine fauna that inhabited the basin during its complete or partial isolation. At present our knowledge of the regional stages does not meet modern standards. The accumulation of strato- Figure 1. Location of the studied sections. types in a shallow-water zone with inconsistent deposition 1 – Zhelezniy Rog section; 2 – Zhelenskiy Mount – Cape and various biologic and facies influenced environments Panagia section; 3 –Popov Kamen’ section; 4 – Taman’ considerably hampers the refinement of the stratigraphic section. range and position of the boundaries. During the last decade the group led by Natalia Filippova, Yulia Ros- tovtseva, Sergey Popov and Larisa Golovina has under- Black coastal outcrops of the Taman Peninsula (Fig. 1) taken detailed studies of Neogene litho-, magneto-, and display a continuous succession of seven regional stages, biostratigraphy of sections in the Taman Peninsula (Rus- i.e. Upper Chokrakian – Karaganian – Konkian – Sar- sia) [22, 27, 53, 57, 60, 61] to gather new data on the matian – Maeotian – Pontian – Kimmerian, ranging from Neogene marine biota evolution in this part of the East- the Middle Miocene to Pliocene and forming a system ern Paratethys. of synclinal and anticlinal folds. The most complete sec- The main goals of this study are as follows: tion is the Zelensky Hill – Panagia Cape that includes an uninterrupted succession of Upper Chokrakian to Up- 1. The detailed study of benthic and planktonic as- per Maeotian sediments (Fig. 2). The Maeotian–Pontian sociations of macro- and microfauna and the de- sediments were studied in three key sections, the Taman termination of assemblages characteristic of each (Kerch Strait coast), Popov Kamen, and Zheleznyi Rog regional stage and substage; (Black Sea coast). The Taman and Popov Kamen sections are composed of relatively shallow-water deposits where 2. The selection of local and regional litho- and the Maeotian–Pontian boundary falls on a stratigraphic biomarkers that permit both a cross-correlation of gap, whereas the Zheleznyi Rog section contains a se- sections within the Taman Peninsula and inter- quence of relatively deep-water Maeotian–Pontian sedi- regional correlations; ments (Fig. 4). 3. The comprehensive study of intervals bearing the The sections were lithologically studied layer-by- most “marine” associations of macro- and micro- layer [26, 29, 58–61]. The composition of sediments is fauna and flora in order to reveal the most common shown in Figures 2 and 4. Each sample was examined microplankton taxa for straightforward correlation for foraminifers, ostracods, nannofossils, diatoms, organic- with the international stratigraphic scale. walled phytoplankton, spores and pollen. All sections were additionally sampled for malacofauna and paleomag- netic studies. 2. Materials and methods

The Middle—Late Miocene and Pliocene sediments in 3. Results the Taman Peninsula are mainly represented by clay and, rarely, by carbonate deposits accumulated on a relatively 3.1. Biotic groups and paleomagnetic record deep shelf (the Enikalskii trough) [37]. To the northwest, in the Kerchenskii Peninsula theis facies is replaced by Mollusks shallow carbonate sediments, commonly by clayey shell- The key sections of the Taman region were first described stone. A considerably variable thickness and sharp fa- by Andrusov [4], where the stratigraphy was based on mol- cies changes in the Miocene Taman Peninsula deposits lusk distribution. Subsequently, mollusks from the Maeo- resulted from their accumulation under the conditions of tian part of the Taman sections have been described by growing diapiric folds. Ilyina, Nevesskaja and Paramonova [33]. Extensive stud-

189 Middle–Upper Miocene stratigraphy of the Taman Peninsula, Eastern Paratethys

Figure 2. Upper–Middle Miocene sequence in the Zhelensky Hill –Panagia section based on different paleontological groups. The section shows an uninterrupted succession of deposits from the Upper Chokrakian to the Upper Maeotian distinguished using 190 mollusk fauna. Other biotic groups were used for recognition of units in the rank of local zones or beds and even levels based on different microfaunal and microfloral groups. The composition of sediments is shown according to [52]. The lithology legend is in Fig. 4. The zones or beds with marine microfossils are marked. E.P. Radionova et al.

Figure 3. Correlation of diatom zonal scales. The regional diatom scale of the Eastern Paratethys is used to subdivide the Upper Miocene sediments [39]. The correlation between the Miocene diatom scale of the Central Paratethys [32] and the tropical oceanic zonal diatom scale [9, 14, 15] is shown. The occurrence of oceanic diatom marker species in the Sarmatian, Maeotian, and lower Pontian permits the correlation of local units with the oceanic diatom scale. Diatom* – The age estimation of the Messinian sediments in the Capodarso stratotype section was carried out based on the same marker species [15, 23]. All siliceous deposits of the Mediterranean Lower Messinian are dated by diatoms as the upper Nitzschia miocenica Zone and Subzone A of the Thalassiosira convexa Zone [24].

ies by Popov and Zastrozhnov [52] include a description aries, facial assignment, genesis and main typical eco- of the major sections, which were later complemented by logical characters” [11]. The key sections in the Taman the work of Goncharova [27–29, 57–59, 72]. Recently Peninsula are relatively poor in foraminifers. Only the the stratigraphy of the Taman sections based on ben- Konkian–Maeotian interval in the Zelensky Hill – Pana- thic groups and mollusk composition was briefly discussed gia section and the Maeotian part of the Taman and Popov by Popov, Vernigorova, Goncharova et al. [53]. Despite Kamen sections are well characterized by foraminifers [57]. the impoverished composition of malacofauna, its pres- A thorough study of foraminiferal assemblages in the con- ence permitted the recognition of almost all regiostages tinuous section of Zelensky Hill – Panagia revealed a and substages from the Upper Chokrakian to Kimmerian, consecutive replacement of Upper Chokrakian to Upper the definition of their boundaries, and the correlation of Maeotian associations named for their typical species the sections investigated (Fig. 2). (Fig. 2). The characteristic foraminiferal assemblages were revised and their resolution for the distinction of re- Foraminifers giostages and regiosubstages in the studied sections was recognized. The new data on the occurrence of planktonic The study of foraminiferal assemblages in the Miocene foraminifers in the Konkian and Maeotian sediments in deposits of the Crimea and northern Ciscaucasia (west- the Zelensky and Kholodnaya Dolina sections were ob- ern and eastern Georgia) was undertaken by Krashenin- tained [53, 72, 73]. nikov [40–42] and Bogdanovich [11, 12]. In the western Ciscaucasia, local stratigraphic units were characterized Nannoplankton by Bogdanovich [11, 12]. All distinguished foraminiferal associations were considered in terms of “vertical distribu- Nannofossils in the Zheleznyi Rog and Panagia sections tion and suitability for definition of stratigraphic bound- of the Taman Peninsula were first studied by Lyul’yeva

191 Middle–Upper Miocene stratigraphy of the Taman Peninsula, Eastern Paratethys

Figure 4. Correlation of Maeotian–Pontian deposits in the Zheleznyi Rog, Taman and Popov Kamen sections. The Zh. Rog section contains relatively deep-water sediments, whereas Taman and P. Kamen sections are composed of relatively shallow-water deposits. The composition and correlation of the sections was taken from [56], Fig. 3 with a supplement [18, 22]. The references to Zh. Rog, Taman, P. Kamen paleomagnetic results are given in [21, 68, 70]. Each of the marker diatomites J, L, A, SP contains specific diatom and nannoplankton assemblages. This makes it possible to identify different sections. I and II are different points of view on Sarmatian- Maeotian boundary at Zh. Rog section. The border is conventionally placed.

and Semenenko [64, 65]. According to their data, “the representative nannofossil association was recorded in lower part of the Maeotian is referred to Zone NN9, the the Konkian deposits in the Zelensky Hill – Pana- upper part contains assemblage of Zone NN10, in the gia section [26, 72]. The assemblage includes Braaru- Pontian deposits zonal species have not been found, and dosphaera bigelowi, Coccolithus pelagicus, Cricolithus the Lower Kimmerian includes species typical for Zones jonesi, Reticulofenestra pseudoumbilica, Rhabdosphaera NN11 and NN12” [65]. In the Pontian sediments of the sicca, Helicosphaera carteri, Lithostromation perdurum, Zheleznyi Rog section Lyul’yeva recognized a stratotype Sphenolithus moriformis, Discoaster sp., Helicosphaera of the zone Isolithus semenenko Luljewa [44]. Subse- sp., Sphenolithus sp., and Thoracosphaera sp.; accord- quently Lyul’yeva reported the occurrence of Amaurolithus ing to Martini zonation [46], it corresponds to zones primus and Amaurolithus delicatus at the contact between NN6/NN7. A final stage of the Konkian basin was char- the Maeotian and Pontian [66]. These records were not acterized by the development of a monospecific assem- confirmed by subsequent investigation [47]. blage of Reticulofenestra pseudoumbilica. The Konkian– The nannoplankton zonal subdivision of most sections Sarmatian boundary is marked by the disappearance of in the Eastern Paratethys remains problematic because nannoplankton. The Lower Sarmatian deposits are char- the impoverished nannofossil assemblages include cos- acterized by the development of a monospecific assem- mopolitan species and lack stratigraphically significant blage with Syracosphaera sp. marked by the extremely taxa. In the sections of the Taman Peninsula the most small size of coccoliths. In the Middle and Upper Sar-

192 E.P. Radionova et al.

matian nannoplankton are absent. Only in the terminal (Upper Sarmatian), Thalassiosira maeotica (Lower Maeo- Upper Sarmatian clay underlying the bioherm are rare tian), Cymatosira savtchenkoi (Upper Maeotian,) and beds Coccolithus pelagicus and Reticulofenestra sp. recorded. with Actinocyclus octonarius (lower part of Pontian). The In the Maeotian and Pontian deposits zonal nannofossil base of each zone is defined by the first occurrence of an species were not found. In the Lower Maeotian Pana- index species (Fig. 3). gia and Popov Kamen sections nannoplankton is present only at discrete levels corresponding to the most marine conditions. The assemblage includes Braarudosphaera Diatom datum planes bigelowii, Calciosolenia brasiliensis, Coccolithus pelag- icus, Reticulofenestra pseudoumbilica, Helicosphaera sp., In the Middle–Upper Miocene sections of the Taman Reticulofenestra sp., Rhabdosphaera sp., Isolithus sp., Peninsula certain beds contain foraminifers, nannofossils, and numerous varieties of Lacunolithus menneri. Numer- diatoms, and dinocysts. These groups are used in the ous L. menneri occur in the upper Lower Maeotian to- zonal stratigraphy of oceanic sediments, but their appli- gether with scarce Coccolithus pelagicus and Reticulofen- cation to brackish-water Paratethian deposits is limited. estra pseudoumbilica. At the base of the Upper Maeo- Marine diatoms are the most tolerant microfossils surviv- tian in the Kholodnaya Dolina section Braarudosphaera ing a decrease of salinity down to 18–20 ppm (similar to bigelowii, Reticulofenestra pseudoumbilica, and Thora- the modern Black Sea) [54]. A preliminary overview of the cosphaera sp. were recorded [73]. In the upper part of the available material has revealed a high stratigraphic poten- Maeotian and lower part of the Pontian in the four sec- tial of diatoms for stratigraphy of the Eastern Paratethys. tions discussed, an assemblage with predominant Braaru- Most of the Upper Miocene marine invasions in the stud- dosphaera bigelowii was found. This assemblage also ied region were accompanied by incoming marine diatoms contains Coccolithus pelagicus, Discoaster sp., Lithostro- that complemented the local brackish assemblages. There mation perdurum, Reticulofenestra sp., Rhabdosphaera is a correlation between the Miocene Central Paratethys sp., Syracosphaera pulchra, Syracosphaera sp., and Tho- diatom scale [32] and the tropical oceanic diatom zona- racosphaera sp. [56]. tion [9, 14, 15] (Fig. 3).

Diatoms The occurrence of oceanic diatom marker species in the Sarmatian, Maeotian, and lower Pontian permits the cor- In the Taman Peninsula the diatom flora was first de- relation of the local diatom scale with the oceanic zonation scribed by Savchenko [63] from Maeotian sediments. scale. Neogene tropical and boreal zonal diatom scales Jousé [35] made an ecological-stratigraphical review of have been developed from the beginning of the DSDP the diatoms characteristic of the Sarmatian, Maeotian and research [14, 36]. The distribution of stratigraphically im- Pontian in the Taman and Kerch sections. She recorded portant species was revealed (Fig. 3). The stratigraphic for the first time the oceanic diatom Denticula lauta in the distribution of these species was recognized from the ma- Chokrakian of the Panagia section (V.V. Menner, personal terial of numerous oceanic sites in the Pacific, directly communication). The taxonomic composition of Sarmatian correlated to paleomagnetic data and repeatedly veri- diatoms in the Panagia section was reported by Makarova fied [8, 9, 15, 36]. Their occurrence events are synchronous and Kozyrenko [45]. in the tropical and moderate realms. Although in our ma- Diatoms are absent in the sediments of the Upper terial these species are found sporadically and are few Chokrakian-Karaganian and in most of the beds of the in number, the succession of their first occurrence events Konkian-Lower Sarmatian. In all sections discussed in is the same as that in the World Ocean. There are Tha- the paper diatoms occur in almost all the clay beds of the lassiosira burckliana (FO 8.9 Ma), Nizschia fossilis (FO Middle Sarmatian –Lower Pontian. This allows not only 8.9 Ma), N. miocenica (FO 7.1 Ma), Thalassiosira convexa the distinction of zones with characteristic Sarmatian– (FO 6.7 Ma), and others. Lower Pontian diatoms but the recognition of beds bear- ing certain ecological groups, i.e. freshwater, brackish- A remarkable peculiarity is the occurrence in certain water, brackishwater-marine, and marine diatoms. The stratigraphic intervals of oceanic marker species with a zonal subdivision is based on the Eastern Paratethys re- known stratigraphic range related to the geochronolog- gional zonal scale [38, 39]. The Middle and Upper Sar- ical scale [8, 9, 75]. This permits the straightforward matian, Maeotian, and lower Pontian sediments of the correlation of some regional zones with the units of the Taman sections were subdivided by diatoms into the fol- Mediterranean scale and with the oceanic diatom zonal lowing regional zones; Actinostephanos podolicus (upper scale as was shown for the Maeotian–Pontian Transitional Middle Sarmatian), Achnantes brevipes–Navicula zichyi strata [55, 56].

193 Middle–Upper Miocene stratigraphy of the Taman Peninsula, Eastern Paratethys

Organic-walled phytoplankton (dinocysts, green algae, 3.2. Synthesis of paleontological data acritarchs) The upper Middle and Upper Miocene of the Taman se- quence is recovered only in the Zelensky Hill – Pana- The modern state of the art in studies of this group gia section (Fig. 1). The section was originally described in the Eastern Paratethys can be defined as the stage by Andrusov [4]. The Zelensky section shows an unin- of material accumulation. The first data on organic- terrupted succession of deposits ranging from the Up- walled phytoplankton from the Pontian and Kimmerian per Chokrakian to Upper Maeotian. The sequence was deposits in the Kutrya section, Taman Peninsula is pub- subdivided into regiostages and substages using mollusk lished by Ananova [1]. Additionally a brief report on fauna. Other biotic groups were used for the recog- organic-walled phytoplankton presumably from the upper- nition of beds with specific faunal and floral assem- most Karaganian–Lower Sarmatian in the Zelensky Hill – blages within the sedimentary sequences (Fig. 2). In the Panagia section was published by Zaporozhets [74]. Chokrakian–Lower Sarmatian interval in addition to mol- lusks, the carbonate microfossils, i.e. foraminifers, nanno- Research on the Neogene organic-walled phytoplankton plankton and dinocysts, are of considerable importance. carried out during the last decade in the Taman Peninsula The Middle–Upper Sarmatian is stratified based on di- resulted in the elucidation of the taxonomic composition atoms and dinocysts, and the Maeotian is subdivided us- of the assemblages and their distribution, and in the dis- ing all biotic groups. tinction of the beds bearing organic-walled phytoplankton Upper Chokrakian sediments contain mollusk shells of in the sediments from the upper part of the Chokrakian to Lutetia (Davidaschvilia) intermedia, benthic agglutinated Kimmerian inclusive [17–20]. In the Maeotian–Kimmerian foraminifers Hyperammina and Trochammina, and poor interval the beds bearing organic-walled phytoplankton organic-walled phytoplankton associations of Selenopem- were correlated with paleomagnetic units. This provided phix (including S. nephroides), Lejeunecysta (including the age estimate of the beds and boundaries and their cor- L. cf. oliva, L. hyalina), ?Impagidinium/”Gonyaulax”, and relation with the geochronological scale [21, 22] (Figs. 2 Spiniferites spp. and 4). Karaganian. The base of the regiostage is defined by the occurrence of the bivalve Lutetia (Spaniodontella) and benthic foraminiferal association with Discorbis urupensis. Paleomagnetic investigations Local beds bearing ?Hystrichosphaeropsis sp. A are dis- tinguished using organic-walled phytoplankton. Upwards Paleomagnetic characteristics of the Upper Miocene sed- in the section the oppressed specimens of Spiniferites spp. iments in the Taman Peninsula were first obtained by (including S. membranaceus and S. ramosus group), ?Im- Pevzner [50, 51]. In studies of the Zelensky Hill–Panagia pagidinium/”Gonyaulax”, and others are recorded. In the section he revealed that the Pontian deposits are gener- second half of the Karaganian the association of organic- ally reversely magnetized. The upper part of the Maeo- walled phytoplankton becomes poorer. At the end of the tian shows a normal polarity and the lower part a reversed Karaganian–beginning of the Konkian the diversity and polarity. The subsequent detailed high-resolution inves- abundance of organic-walled phytoplankton slightly in- tigation confirmed as a whole this inference. In the Popov creases, it most commonly includes Spiniferites spp. and Kamen and Zheleznyi Rog sections the Lower Maeotian Cymatiosphaera. is mainly reversely magnetized and corresponds to Chrons Konkian deposits are distinguished by more diverse C3Ar and C3B. Within this interval two normally magne- foraminiferal and dinocyst associations and by the appear- tized horizons are recorded. The Upper Maeotian shows a ance of nannoplankton and mollusk assemblages with ma- normal polarity and corresponds to Chron C3An. The Pon- rine Timoclea (Parvivenus) konkensis. The sediments are tian sediments studied in the Zheleznyi Rog and Taman subdivided into three parts according to the foraminifer sections are mainly characterized by the reversed polarity and calcareous nannoplankton composition. The first and are correlated with the lower part of the Gilbert Chron part is characterized by the occurrence of rare nanno- (C3r). Only the lowermost Pontian is normally magne- plankton, planktonic foraminifers Globigerina and ben- tized and corresponds to the uppermost Chron C3An. As thic foraminifers Bolivina, Quiqueloculina, Cassidulina, for the Azovian horizon, its greater, middle part corre- Reussella, Discorbis, Articulina, and Nodobaculariella. sponds to the normal Thvera Subchron (C3n4n). These In the second part the foraminiferal species diversity records agree well with the paleomagnetic data obtained is variable depending on various factors. Some of the in synchronous sections of the Eastern Ciscaucasian sub- thinnest layers contain rich and diverse foraminiferal as- aqueous deposits [30]. semblages bearing planktonic Paragloborotalia mayeri,

194 E.P. Radionova et al.

Globigerina sp. (juv.), Globigerina sp.1, Globigerina bul- Lower Sarmatian benthic foraminifer assemblages are very loides, Globorotalia sp., Guembelina sp., Pseudohastige- impoverished with a predominance of the genera Nonion rina sp., and polyhaline benthic Discorbis kartvelicus, D. and Elphidium that also dominate in the Sarmatian sensu supinus, Asterigerina sp., Cassidulina bulbiformis, Cas- str. of the Pannonian Basin. The occurrence of Quinque- sidulina sp., Angulogerina angulosa, Uvigerina gracilis- loculina reussi reussi Bogd., Articulina sarmatica (Karrer), sima, Bolivina dilatata, Bulimina ex gr. elongate, Bulim- and Elphidium josephina (Orbigny) permits the correla- inella elegantissima, Globulina gibba, Varidentella reussi tion of these layers with the regional Miliolinella reussi sartaganica, Virgulina schreibersiana, Quinqueloculina Beds [12] of the Lower Sarmatian and with the Elphidium gracilis, Q. badenensis, Q. ex gr. consobrina, Q. konkensis, reginum – E. hauerinum Zone of the Central Paratethys. Q. minakovae ukrainica, Quinqueloculina sp.1, Sigmoilina The nannofossils are represented by a monospecific as- mediterranensis, Melonis soldanii, Nonion granosus, Flo- semblage of Syracosphaera sp., which is characterized by rilus boueanus, and Elphidium antonina. The richest cal- its extremely small size of coccoliths. The organic-walled careous nannoplankton assemblage was found in the sec- phytoplankton significantly increased in abundance in the ond part; it includes Braarudosphaera bigelowi, Coccol- mid-Lower Sarmatian. All taxa are well developed and ithus pelagicus, Cricolithus jonesi, Reticulofenestra pseu- large-sized. C. placacanthum retains a dominant role doumbilica, Rhabdosphaera sicca, Helicosphaera carteri, in the associations. The subdominant Hystrichokolpoma Lithostromation perdurum, Sphenolithus moriformis, Dis- rigaudiae, Homotryblium tenuispinosum, and Spiniferites coaster sp., Helicosphaera sp., Sphenolithus sp., and Tho- ramosus also occur. Diatoms are nearly absent in the racosphaera sp. According to Martini’s zonation [46], Lower Sarmatian. it corresponds to zones NN6/NN7 and is well corre- lated with the nannofossil associations from the Upper Middle Sarmatian. The lower part of the Middle Sar- Badenian (Kosovian) sediments. However, according to matian is represented by thick monotonous clayey “Cryp- some researchers, the occurrence of Rhabdosphaera po- tomactra Beds” with endemic Obsoletiformes, Replidacna culi and Rhabdosphaera pannonica in the assemblage and Cryptomactra pesanseris. Endemic miliolids domi- likely indicates the Zone NN7 [13]. The third part of the nate in the rich benthic foraminifer assemblages that be- Konkian is characterized by poor benthic foraminifer and long to the Middle Sarmatian Dogielina sarmatica re- nannoplankton associations. Changes in the hydrological gional Beds [12]. The assemblages include Porosononion regime of the basin and water column stratification led to subgranosus (Egger), the common species for the whole the formation of beds with a mass development of Retic- Paratethian Sarmatian basin. The lower part of the Mid- ulofenestra pseudoumbilica in this part of the section. dle Sarmatian is characterized by polydominant associ- Similar changes took place in the organic-walled phyto- ations of organic-walled phytoplankton with significant plankton assemblages; among them a relatively abundant open-marine species Impagidinium aculeatum, I. patulum, oligo-dominant association with Cleistosphaeridium pla- and forms of the Achomosphaera sagena-type. In the over- cacanthum, Cleistosphaeridium sp.A, and Polysphaerid- lying sediments Spiniferites spp. (including Spiniferites ium zoharyi. The association with C. placacanthum is of a Pannonian type) and the freshwater green algae Pe- known from the Central Paratethys. According to some diastrum spp. are recorded. Diatoms occur in the upper researchers, the C. placacanthum acme-zone corresponds half of the Middle Sarmatian. In the Panagia section to the top of the Badenian, however, others correlate this (Fig. 2) the provincial Actinostephanos podolicus Zone zone with the beginning of the Sarmatian sensu str. [7, 34]. with a semi-marine diatom assemblage is recognized. It is According to Filippova [20], the C. placacanthum beds in subdivided into the Actinostephasnos podolicus Beds with the Taman sections should be considered in full range the predominant planktonic diatoms and the Achnanthes within the Lower Sarmatian, however, she does not ex- baldjikii var. podolica Beds that are dominated by ben- clude that their lowest part can be referred to the Konkian. thic fouling algae. The Actinostephanos podolicus Beds The Upper Konkian boundary is marked by the extinc- include the index species Coscinodiscus doljiensis, Tricer- tion of nannofossils and further impoverishment of benthic atium sp. and at times Azpeitia aff. apiculata, the marine foraminifers. species with a first occurrence at 10.6 Ma ago. Among the benthic forms the most common are Grammatophora (Gr. marina, Gr. hungarica), Cocconeis scutellum var. scutel- Sarmatian sensu lato. lum + var. pulchra, C. grata, and Achnanthes baldjikii Lower Sarmatian sediments are characterized by the var. baldjikii + var. podolica. The Achnanthes bald- abundant mollusk Abra alba scythica and the occurrence jikii var. podolica Beds contain abundant benthic flora of Mactra eichwaldi, Ervilie dissita, and Obsoletiformes with scarce planktonic species. The most numerous are sp. that are typical Sarmatian genera and species. The Achnantes baldjickii + var., Cocconeis scutellum + var.,

195 Middle–Upper Miocene stratigraphy of the Taman Peninsula, Eastern Paratethys

Grammatophora marina, and Amphora proteus; Achnan- toplankton in these deposits possibly resulted from a hy- thes brevipes and members of Diploneis, Mastogloia, and drogen sulfide contamination and low salinity. Navicula are somewhat scarcer. An uninterrupted transition from the Sarmatian to Maeo- The Middle to Upper Sarmatian transition is represented tian occurs only in the Panagia section. In the 20-m- by the Thalassiosira aff. burckliana Beds that include thick member of grey clays (Fig. 2) the beds bearing the unusual oceanic species Th. burckliana (FO 8.9 Ma, brackish-water flora alternate with that yielding marine, LO 7.9 Ma) and Nitzschia fossilis (FO 8.9 Ma), together commonly monodominant floral remains. Among nannofos- with planktonic marine Coscinodiscus asteromphalus, ma- sils scarce Coccolithus pelagicus and Reticulofenestra sp. rine and brackish-water Actinoptychus (A. senarius, A. were recorded (Sample 43/03). Sample 36/03 contains splendens), Actinoptychus spp., and spores of Chaeto- oceanic Thalassiosira grunowii and several Hyalodiscus ceras. The benthos is represented by both marine Dim- species; in Sample 41/03 marine lithoral Endyctia ocean- merogramma minor, Grammatophora insignis, Gr. ma- ica, Coscinodiscus asteromphalus, Paralia sulcata, and rina, Lyrella abrupta, L. lyra, Nitzschia marginulata, Hyalodiscus sp. dominate. The Late Sarmatian associ- Diploneis notabilis, Mastogloia baldjikiana and brackish- ation of organic-walled phytoplankton mainly consisting water Rhopalodia (R. gibberula + R. musculus) and of few freshwater algae of Pediastrum and Zygnemataceae Nitzschia epithemioides, by the species of Entomoneis is replaced by the Early Maeotian semi-marine associa- (E. alata, etc.), Amphiprora gigantea var. sulcata, com- tion with Spiniferites spp. and others directly above the mon Navicula incomperta var. fossilis, Berkeleya scopu- bioherms. lorum, Achnanthes brevipes, as well as Navicula andrus- The Sarmatian/Maeotian boundary is defined by the oc- sowii Pant. known from the uppermost Late Sarmatian currence of the marine mollusks Skenea tenuis and Sphe- and a variety of N. zichyi Pant. The assemblage also in- nia anatina at the base of the bryozoan bioherms and cludes freshwater planktonic Aulocoseira and few valves within a reef body (Fig. 2). In the Zheleznyi Rog section of the freshwater benthic Eunotia and Pinnularia. A prob- the Sarmatian–Maeotian transition is unclear. The clay lematic genus Pliocaenicus(?) occurs for the first time. layers bearing Maeotian mollusks, fishes, phyto- and di- Upper Sarmatian sediments contain impoverished macro- atom flora overlie the Upper Sarmatian that yields ash and microfauna, i.e. rare Mactra caspia synchronously dated at 8.69±0.18 Ma [71], probably with an unconfor- redeposited from a shallow zone, and among benthic mity. foraminifers rare Ammonia ex gr. beccarii. However, Lower Maeotian clayey sediments contain rare associa- brackish diatoms belonging to the Achnantes brevipes– tions of euryhaline marine mollusks dominated by Abra Navicula zichii regional zone are abundant. Within this and Cerastoderma. Assemblages with Polititapes abichi, zone the beds bearing the predominant benthic Achnan- Dosinia maeotica, Mytilaster volhynicus, Rissoa subin- thes brevipes and species of Rhopalodia, Entomoneis, flata, Pirenella disjuncta disunctoides were found in the and Amphiprora, alternate with those yielding abundant bioherm facies. Benthic foraminifers include Quinque- planktonic, probably freshwater-brackish taxa of Actinocy- loculina consobrina maeotica Maissuradze, Q. seminu- clus (Cestodiscus), namely, Actinocyclus aff. krasskei, lum maeotica Gerke, euryhaline Ammonia ex gr. becca- Actinocyclus sp.1, Actinocyclus sp.2, numerous valves rii, Elphidium macelum maeotica (Gerke), and Elphidium of freshwater Aulacoseira and, commonly, a problematic fedorovi Bogd. that are characteristic and endemic for genus Pliocaenicus(?). Marine Actinoptychus splendens, the Maeotian [73]. Diatoms belong to the Thalassiosira A. senarius, and Coscinodiscus asteromphalus are few. maeotica Zone and include endemic Paratethian Thalas- The species diversity of the assemblage is provided by siosira and oceanic Thalassiosira grunowii and Th. an- the benthic taxa common for the Late Sarmatian, how- tiqua with the established first occurrence level in the ever, they rank below the planktonic species in abundance. ocean (see Fig. 3). These species are recorded in the Among them the most common are Rhopalodia (R. gib- lower Lower Maeotian in the Panagia and Popov Ka- berula + R. musculus), Nitzschia punctata, and Surirella men sections; in the Zheleznyi Rog section the lower- striatula; others are scarcer. most Lower Maeotian contains only few Thalassiosira The top of the Middle Sarmatian and a large part of the grunowii and Nitzschia fossilis. The upper part of the Upper Sarmatian are characterized by a uniform dinocyst Lower Maeotian yields the endemic diatom assemblage. association with predominant small-sized Spiniferites spp. Calcareous nannoplankton occurs in certain beds and in- and ?Impagidinium/"Gonyaulax". The deposits of the upper cludes the most eurybiontic forms, i.e. Coccolithus pelag- Upper Sarmatian contain rare specimens of mainly fresh- icus, Reticulofenestra pseudoumbilica, Braarudosphaera water algae (Pediastrum, Zygnemataceae) and reworked bigelowii, Calciosolenia brasiliensis, Rhabdosphaera sp., dinocyst fragments. Extremely scarce organic-walled phy- and Isolithus sp. (Fig. 4). The organic-walled phytoplank-

196 E.P. Radionova et al.

ton is dominated by ?Gelatia/Geonettia, Spiniferites spp., Bolivina ex gr. variabilis and Bolivina ex gr. moldaw- and Cymatiosphaera spp.; species of Selenopemphix and ica are dominant, with rare Discorbis sp. and Cas- Lejeunecysta are also present. sidulina sp. [73]. Calcareous nannoplankton includes abundant Braarudosphaera bigelowii, Syracosphaera pul- The Lower–Upper Maeotian transition. chra, Syracosphaera sp., and rare Coccolithus pelagicus, Discoaster sp., Lithostromation perdurum, Reticulofenes- In the Popov Kamen and Panagia sections only scarce tra sp., Rhabdosphaera sp., and Thoracosphaera sp. Both nannofossils and planktonic and benthic foraminifers are the absence of zonal species and the very small size of present, including Discorbis and Cassidulina, in the tran- coccoliths point to the restricted or out-of-strait connec- sitional interval [73] immediately below the beds bearing tion with a marine basin of normal salinity. Together the mollusk Congeria panticapaea that indicates the base with typical marine diatoms [56] Azpeitia aff. komu- of the Upper Maeotian. The mollusk assemblage includes rae, Coscinodiscus perforatus, Podosira lozcii, Actinop- the euryhaline marine species Cerastoderma mithridatis tychus undulates, Actinocyclus octonarius, Actinocyclus that occurs only up to the base of the Upper Maeotian. aff. paradoxus, Rhyzosolenia bezrukovii Jouse, and Hemi- The diatom assemblage of the Cymatosira savtchenkoi aulus, there are species considered as endemics of the Zone with the index species indicating the Lower–Upper Central Paratethys, i.e. Coscinidiscus jambori, Fragilaria Maeotian boundary, was recorded in the Popov Kamen crassa [31], and Biddulphia elegantula known from the section [73] above the dolomite bearing Congeria pantica- Sarmatian [30]. Among dinocysts an extremely numerous paea. It contains mainly planktonic endemic species and, oligo-dominant euryhaline assemblage consisting of Ba- rarely, the open-marine species Nitzschia miocenica and tiacasphaera and Operculodinium species together with Thalassiosira convexa. These are the first findings of the Lingulodinium machaerophorum, occurs and continues into zonal oceanic species Nitzschia miocenica and Thalas- the lower part of the overlying Lower Pontian sediments. siosira convexa in the Maeotian. At the Lower and Upper The Upper Maeotian corresponds to chron C3An, with a Maeotian boundary in the Popov Kamen and Taman sec- thin direct polarity zone present in the upper part. tions the dinocyst assemblage is dominated by Lingulo- dinium machaerophorum and Spiniferites spp.. The base The deposits from the Upper Maeotian to the lower part of the beds bearing this assemblage approximately corre- of the Lower Pontian are composed of thick clayey beds sponds to the major paleomagnetic excursion in the Maeo- interbedded with laminated diatomite strata, over 60 m tian (C3Ar/C3An) and is dated at ∼6.8–6.9 Ma ago [22] thick, that were named “Transitional strata” [56] (Fig. 4). (Fig.4). All biota indicates a short-term marine invasion The laminated diatomites are characterized by abundant in the transitional Lower–Upper Maeotian sediments. diatoms and calcareous nannofossils, mainly represented Upper Maeotian deposits in the Popov Kamen, Zheleznyi by monospecific associations with Actinocyclus octonarius Rog, and Taman sections contain brackish-water micro- and Braarudosphaera bigelowi. Oceanic index species be- fauna and flora. In the Popov Kamen and Zheleznyi Rog longing to the tropical Nitzschia miocenica Zone and the sections the mollusk assemblage includes brackish Conge- index species of the following Thalassiosira convexa Zone ria panticapaea, Congeria amygdaloides navicula Andrus., appear in this part of the sections. Nannofossils are rep- euryhaline marine Ervilia pusilla, rare brackish Theodoxus resented by only one taxon Braarudosphaera bigelowii, stefanescui (Font.), and eurybiontic marine Abra telli- whereas Lithostromation perdurum and Reticulofenestra noides. sp. are very rare. According to the organic-walled phy- In the Zheleznyi Rog section at 8–12 m above the olis- toplankton, the Maeotian/Pontian boundary was deter- tostrom body these deposits are represented by diatom mined by the appearance of brackish-water elements C. clay up to 30 m thick, with a brackish-water associa- rugosum and G. etrusca; this level is slightly older than tion of diatoms. In the Taman and Popov Kamen sec- the paleomagnetic reversal C3An/C3r and is estimated at tions these sediments are significantly reduced in thick- 6.1 Ma [21, 22]. In the Zheleznyi Rog section the appear- ness. Actinocyclus spp. similar to the Upper Sarmatian ance of dinocyst G. etrusca is accompanied by the typical forms dominates and Cyclotella sp. appears. Ostracode Pontian mollusk Paradacna abichi. associations are depleted. Benthic foraminifers are domi- Lower Pontian deposits are marked by the appearance of nated by extremely euryhaline and brackish forms Ammo- endemic brackish mollusks aff. Cerastoderma in the basal nia ex gr. beccarii and Elphidium macelum maeotica, with part and Paradacna abichi and Pseudocatillus sp. 1.5– scarcer Ammonia ex gr. compacta, and Elphidium fedorovi. 2.0 m above in the Zheleznyi Rog section. Ostracodes The upper Upper Maeotian again yields marine mi- are represented by abundant brackish Caspiocypris can- croplankton associations. In the Panagia section in the dida, Pontoniella acuminata, P. loczyi, Cyprideis torosa, upper part of the Maeotian the open-marine foraminifers and Bacunella aff. dorsoarcuata (I.A. Nikolaeva data).

197 Middle–Upper Miocene stratigraphy of the Taman Peninsula, Eastern Paratethys

Among dinocysts the properly Paratethyan brackish el- plements the known record of the stratigraphy and envi- ements appear, namely, rare specimens of Caspidinium ronmental evolution in the Euxinian Paratethys (Fig. 5) rugosum, Galeacysta etrusca, Millioudodinuim spp., and and permits a partial revision of previous studies [37, 48]. others, which become predominant in the upper part of the The transitional Middle–Upper Sarmatian beds are char- Lower Pontian [20]. The sediments of the interval from the acterized only by dinocysts and pollen and contain the base of the Pontian to the Azov Beds of the Kimmerian in- diatom assemblage of marine and brackish Paratethyan clude the Caspidinium rugosum–Galeacysta etrusca Beds species with stratigraphically important oceanic Thalas- and correspond to the uppermost part of C3An, C3r and to siosira burckliana (FO 8.9 Ma, LO 7.9 Ma) and Nitzschia the lower part of C3n (C3n4n, C3n3r) (Fig. 4). In the over- fossilis (FO 8.9 Ma). This suggests a short marine inva- lying diatomite beds the dominant species Actinocyclus sion at that time and the age estimation of the uppermost octonarius is replaced by brackish-water Stephanodiscus Upper Sarmatian is no earlier than 8.9 Ma. This age is hantzschii and S. digitatus. Nannofossils are mainly rep- significantly younger than believed by most of researchers resented by rare Braarudosphaera bigelowii [56]. (10.2 Ma according to [67] and 10.5 Ma [49]). At the same time is agrees well with the paleomagnetic data interpre- Upper Pontian–Lower Kimmerian. tation [22]. The base of the Upper Pontian substage, the Portaferian horizon, is separated from the underlying Lower Pontian Upper Sarmatian–Lower Maeotian deposits by an erosional unconformity. The Portaferian In the Panagia section the Upper Sarmatian variegated deposits contain numerous brackish mollusks including the clay bearing diatoms of the Navicula zichii Beds grades characteristic Pontian endemics Congeria subrhomboidea into the calcareous clay member that together with the Andrus., Plagiodacna carinata, Phyllocardium planum, typical Upper Sarmatian flora contains a thin strata of ma- and others. The Upper Pontian dinocyst association is al- rine diatoms including oceanic Thalassiosira burckliana most entirely comprised of the typical Paratethyan brack- (LO 7.9 Ma), Th. grounowii (LO 7.9 Ma), Th. antiqua (FO ish taxa C. rugosum, Millioudodinuim spp., G. etrusca. 7.7 Ma), and Nitzschia fossilis, also encountered in the The new taxa Spiniferites cruciformis, Achomosphaera an- lowermost Maeotian. The presumable age of this bound- dalousiense, and ?Komewuia also occur. The Late Pon- ary inferred from these data is also younger than that tian and Azovian dinocyst associations from the Euxinian assumed nowadays and contradicts the 40 Ar/39Ar age of Basin were similar to the Lago Mare assemblage (p-ev2) 8.69±0.18 Ma (or 8.54±0.02 Ma with other constants) ob- in the Mediterranean [10, 22]. tained for the uppermost Sarmatian in the Zheleznyi Rog The Pontian–Kimmerian boundary is erosional in the re- section [71] and the K-Ar age of 8.87±0.27 Ma received gion and is mainly defined by the occurrence of specific the at the same section [25]. bivalve endemics Paradacna deformis, P. stratonis, Pon- talmyra occidentalis, and Arcicardium subacardo in the Maeotian Azov Beds. The Lower Kimmerian dinocyst association is According to all researchers, in relatively complete Maeo- depleted and scarce and is mainly represented by Caspi- tian sections two thick magnetozones of reversed and nor- dinium rugosum and Millioudodinuim spp. The lowermost mal polarity subdividing the Maeotian approximately in part of the Azovian Horizon corresponds to the upper- half, with two or three minor excursions, are recorded [21, most part of Zone C3r; according to Trubikhin, the middle 22, 50, 51, 69–71]. They are correlated [21, 22, 68, 69] part of C3n4n (Thvera Subchron) is normally magnetized with Chrons C3An and C3Ar; in some sections zone C3B and the upper part of C3n3r is reversely magnetized again. is recognized in the lowermost Maeotian–uppermost Sar- The next unconformity is recorded at the base of the matian in the clay enclosing bioherms and slightly below Kamyshburun Beds (Middle Kimmerian), where new mol- it. With this interpretation the age of the top and the lusk endemics Pteradacna edentula (Desh.), Arcicardium base of the Maeotian is 6.1 Ma and ∼7.6 Ma, respec- acardo (Desh.), A. kubanicum Andr., and Tauricardium tively [21, 22, 69, 70], and its duration is about 1.5 Myr. squamullosum appeared. The Kamyshburun Beds corre- Consequently, the knowledge of the age inferred from the spond to the upper part of Zone C3n (Fig. 4). diatom records agrees well with the paleomagnetic inter- pretation [21, 22, 68, 69], whereas according to [71], the base of the Maeotian is dated as 8.2–8.6 Ma and its du- 4. Discussion ration is 2.2–2.6 Ma. With the latter interpretation of paleomagnetic records we should assume that the Maeo- The new data on the composition of phytoplankton, espe- tian interval contains numerous hiatuses with a duration cially diatoms, in the Taman sections considerably sup- of up to nearly a million years. In our opinion neither

198 E.P. Radionova et al.

Figure 5. Changes of salinity regime and major plankton invasions based on the biota distribution in the Taman sections. 199 Middle–Upper Miocene stratigraphy of the Taman Peninsula, Eastern Paratethys

paleomagnetic nor paleobiological and lithological char- atoms as the upper part of Nitzschia miocenica Zone and acters of the Zeleznyi Rog section give any reason for this subzone A of Thalassiosira convexa Zone [24]. inference. For instance, if Chron C3Ar with a duration of up to nearly half a million years is missing in the Maeo- tian part of the Zeleznyi Rog section, we should see its 5. Conclusions absence in other Maeotian sections from Turkmenistan to Romania. It is unlikely that such a prolonged hiatus with The new data on planktonic and benthic groups suggests an interregional characterwould have been overlooked by a pulsating connection of the Eastern Paratethys with ad- researchers. jacent open marine basins. A comprehensive study of the Chokrakian–Kimmerian microbiota reveals the presence of Lower–Upper Maeotian boundary several beds bearing marine associations that are related to short-term marine invasions. The biotic and paleomag- The boundary is historically defined by a sharp change netic data obtained at the Taman Peninsula sections give from marine benthic assemblages to brackish ones with a more comprehensive, but sometimes a controversial pic- Congeria panticapaea, is considerably well characterized ture of the history of the Eastern Paratethys and the na- by mollusks, foraminifers, and ostracodes and is clearly ture of its relationship with the adjacent marine basins. recorded in all four key sections (Figures 4 and 5). At the same time the paleomagnetic characteristics of the Popov Kamen and Zheleznyi Rog sections near this boundary considerably differ. In the Popov Kamen section the Acknowledgments paleomagnetic excursion interpreted as C3An/C3Ar [22] is recognized 12–14 m below this boundary. In the This research started within the framework of the projects Zheleznyi Rog section the same polarity change was de- of the Russian Foundation for Basic Research (grants 01- fined above the olistostrome body where congerias were 05-64424; 07-05-00795). The studies were also sup- found, namely, after [21, 22, 68, 69], precisely above it, ported by grants 09-05-00307 and 10-05-01102 of the and according to the more detailed data [71], above the Russian Foundation for Basic Research. We are grateful olistostrome there is a 5-m-thick interval of reversely mag- to anonymous reviewers who looked through this paper netized rocks. Thus, we should either admit a significant and made valuable suggestions and comments, which sig- diachroneity of the transition of the basin to a brackish- nificantly improved the quality of the manuscript. We also water regime probably associated with the drop in height appreciate the improvements suggested by Marina Bylin- and progradation of river channels during a marginal- skaya for English language. marine regime, or explain this discrepancy by the incom- pleteness of the sections and the erroneous interpreta- tion of paleomagnetic data. It was suggested to define References this boundary not by benthic fauna but conditionally by a paleomagnetic excursion [22], slightly below the base of [1] Ananova E., Volkova N., Zubakov V., Pavlovskaya V., the dinocyst Lingulodinium machaerophorum–Spiniferites Remizovsky V., New data on the Taman reference sec- spp. beds (Fig. 5). But in this case, in the Popov Kamen tion of the Mio-Pliocene in Black Sea region. Dok- section the Upper Maeotian will include a 12-14-m-thick lady Akademy nauk SSSR, 1985, 284, 4, 925–928 (In clay bed bearing fauna that was considered as charac- Russian). teristic of the Lower Maeotian [59]. In the Popov Kamen, [2] Andrusov N., Kerch limestone and its fauna. Za- Panagia, and Taman sections the traces of marine invasion piski Imperatorskogo s.-pereburgskogo mineralogich- in the uppermost Lower Maeotian with an accepted event eskogo obshchestva, 1890, 2, 26, 193-345 (In Rus- boundary, or near the Lower–Upper Maeotian boundary sian). are recognized by the occurrence of Nitzschia miocenica [3] Andrusov N., Die südrussische Ablagerungen. Theil (FO 7.1 Ma) and Thalassiosira convexa (FO 6.7 Ma) (after 3. Sarmatische Stufe. Verhandlungen der Russisch- Barron) [8]. kaiserlichen mineralogischen Gesellschaft zu St. Pe- The Messinian sediments age determination at the stra- tersburg, 1902, 2, 39, 338-495. totype section was carried out on the grounds of the same [4] Andrusov N., Geological researches at the Tam marker species [16, 23]. The correlation of the Capodarso Peninsula, Materialy dlya geologii Rossii, 1903, 21, section with a paleomagnetic scale was initially done indi- 2, 257-383 (In Russian). rectly through diatom zonation [62]. All siliceous deposits [5] Andrusov N., The horizon of Konkian, Proceedings of the Mediterranean Lower Messinian are dated by di- of the Geologicheskij i mineralogicheskij muzej imeni

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