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, JUNE 2015, 66, 3, 235—244 doi: 10.1515/geoca-2015-0022
Introduction
The territory between Africa and the European Platform doc-
uments a very complex geodynamic development during the
whole Cenozoic era (e.g. Kováč et al. 1998; Schmid et al.
2008; Ustaszewski et al. 2010; Handy et al. 2010, 2014).
Convergence between these plates led to extreme geodynamic
and paleogeographical changes associated with subduction,
collision, folding and thrusting of the meso- and neo-Alpine
complexes of accretion wedges and emersion of the paleo-
Alpine consolidated rear parts of the orogenic systems.
These processes leading to development of mountain chains
were followed by disintegration of the Alpine Tethys. In the
south, the domain of the Mediterranean—Tethys persisted,
while the rest of the Valais—Penninic—Magura oceanic realm
in the north, together with flooded margins of the European
platform and flanks of Alpine-Carpathian orogen represented
the realm of the Paratethys Sea (Laskarev 1924), continuing
toward the east in the regions of the present Black and Cas-
The correlation of the Neogene of Central and Eastern
Paratethys segments of Ukraine with the International
Stratigraphic Chart based on planktonic microfossils
PETRO GOZHYK, VLADIMIR SEMENENKO†, AIDA ANDREEVA-GRIGOROVICH and
NINEL MASLUN
Institute of Geological Sciences, National Academy of Sciences of Ukraine, O. Gonchara str. 55-b, 01601 Kiev-54, Ukraine;
aida_g@ukr.net; aida_grigorovich@mail.ru
(Manuscript received May 20, 2014; accepted in revised form March 12, 2015)
Abstract: Detailed analysis of microplankton occurrence (planktonic foraminifera, nannoplankton, dinocysts) in Neo-
gene sediments situated at the north-western and south-eastern margins of Ukraine enabled us to distinguish 10 associa-
tions of oceanic plankton which specified the relative age of lithostratigraphic units of various regions and were used as
correlation levels within the Central and Eastern Paratethys strata. Moreover, an attempt to correlate regional stages and
the International Stratigraphic Chart (ISC) is performed. The Oligocene/Miocene boundary (of ISC) represented by the
correlation level I was placed within the Central Paratethys regional stage Egerian and in the middle part of the Eastern
Paratethys regional stage Caucasian s.l. The latter regional stage is subdivided by the correlation level into two sub-
stages: Lower Caucasian (Chattian of ISC) and Upper Caucasian (Aquitanian of ISC). The correlation level II was
placed within the upper part of the Eggenburgian and lower part of the Batisifonian (Sakaraulian) regional stages and is
correlated approximately with the middle part of the Burdigalian (of ISC). The base of the Middle Miocene is marked
by level IV and was recognized only in deposits of the Eastern Paratethys belonging to the Tarkhanian regional stage.
This level corresponds to the lowermost Badenian and Langhian (of ISC) stages. Correlation level V is traced in the
Konkian sediments of the Eastern Paratethys and is compared with the Upper Badenian and Lower Serravalian (of ISC)
stages. Level VI at the Middle/Upper Miocene boundary is situated in the middle part of the Bessarabian regional sub-
stage of the Eastern Paratethys and enables its correlation with the Serravallian/Tortonian boundary (of ISC). Level VII
is recognized in the Baherovo Member (Meotian stage), while level VIII is fixed at the top of the Meotian regional stage
in the Azov and Black Seas, Crimea and adjacent region named Northern Prichornomorye. Both these levels are also
identified in the Berezhnytsya Formation of the Eastern Carpathian Foredeep. Correlation of these sediments is similar
to the correlation of sediments of Lake Pannon (Pannonian regional stage), hence with the Tortonian stage (of ISC).
Level IX was recognized in sediments of the Azov Member belonging to the Kimmerian regional stage of the Eastern
Paratethys and represents the top of the Miocene strata. Level X occurs within the Taman Member of the Black Sea shelf
and is correlated with the upper part of Kuyalnikian regional stage; corresponding to the Pliocene/Pleistocene boundary.
Key words: Neogene, Paratethys, biostratigraphy, plankton correlation levels, foraminifers, nannoplankton, dinocysts.
pian Seas, so covering areas between the Caucasus and Pon-
tides.
From the Late Chattian, the connection between the basins
of both aforementioned systems was unstable – the marine
straits developed or were destroyed depending on tectonics
and sea level changes. Partial or total isolation of individual
basins of the Paratethys Sea began to be more and more pro-
nounced in the Miocene to Quaternary times.
The Neogene Paratethys Sea was linked to the Mediterra-
nean for a shorter or longer period through the Alpine Fore-
deep (Rhone Depression), Northern Dinarides (Slovenia)
and through the Aegean and Black Sea regions – possibly
also through the territory of Iran and Afghanistan on the east.
These links depended upon tectonics of the Alpine chains as
well as the development of the Ponto—Taurides and Iranian
mountain systems, and evidently also on glacioeustatic fluctu-
ations of the World Ocean.
The changes in Paratethys Sea paleogeography were clearly
reflected in faunal evolution – therefore Seneš (1961, 1963)
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considers this region as an independent trans-European bio-
province (Seneš & Cicha 1967) which was divided into three
segments (Fig. 1) – Western (Alpine), Central (Carpathian,
Balkan) and Eastern (Crimean—Caucasian) Paratethys. The
Western Paratethys comprised the region of the Alpine Fore-
deep (Alpine Molasse Zone) in front of the French, Swiss,
German, and Austrian Alps, and the marine sedimentation
was restricted only to Early Miocene time. The Central Para-
tethys included the Carpathian Foredeep and basins of the
easternmost margin of the Alps, Carpathians, Pannonian Basin
System and basins of the Internal Dinarides and Balkans. The
marine sedimentation and short living relations between the
Mediterranean and this region existed not only during the Early
but also in the Middle Miocene. The Euxinian—Caspian region
belongs to the Eastern Paratethys. The accumulation of marine
sediments occurred longer here than in the Central Paratethys,
up to the Late Miocene—Pliocene—Quaternary times.
History, fundamentals and creation of correlation
levels
The problem of recognition of stratigraphical boundaries
in the system of Neogene sequences of the Central and East-
ern Paratethys, their position in various regions, substantia-
tion and specification of the age of regional stages, as well as
correlation with the stages of the International Stratigraphic
Chart is a subject of continuous discussion till today. First of
all, this problem is connected with the absence of continuous
marine sections with pelagic micro-organisms, different de-
velopment of semi-isolated basins of the Paratethys realm,
and also because the level of study of plankton is evidently
insufficient (in spite of the long history of investigations of
Neogene deposits, but mainly only in marginal facies).
The first, broadly accepted Neogene stratigraphic scale
for the South of Russia and Ukraine was created by Andrusov
(1965) on the basis of mollusc fauna analysis (as other
groups were not investigated at that time). He recognized a
number of cycles, each of them beginning with deposits with
rich marine fauna and ending with a monoform association.
These cycles reflected changes in the hydrological regime
and were later confirmed by geochemical research in strato-
type areas, in particular in rocks of the Kerch Peninsula
(Semenenko 1993, 2001, 2003, 2005). The “Andrusov divi-
sion of the Ponto-Caspian Neogene” was later confirmed by
study of microfauna as well (benthic foraminifers, ostracodes,
etc.). It is necessary to emphasize, that all the information
given in this research on basic sections of stratotypes (origi-
nally proved with mollusc fauna) was later confirmed. The
Lower Miocene biostratigraphy was worked out by Nosovsky
and co-workers (Nosovsky et al. 1976; Nosovsky & Bog-
danovich 1980; Nosovsky 2001) and the Upper Miocene and
Pliocene by Semenenko and Gozhyk (Semenenko 1993, 2001,
2003, 2005; Gozhyk 2006; Gozhyk & Datsenko 2007).
It is also necessary to note difficulties of correlation be-
tween the stratigraphy of the individual Ponto-Caspian ba-
sins and the Mediterranean time scale, which is far from
complete – as is proved by the recognized break between
Fig. 1. Neogene basin systems of the Mediterranean Tethys and Paratethys.
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the Tortonian and Zanclean filled with the time of the
Messinian evaporite deposition. Therefore, the plankton
scale of the Atlantic realm does not coincide with the zonal
Pliocene scale of the Mediterranean. However, in the West-
ern and Eastern Black Sea depressions the inherited charac-
ter of deep-water marine sedimentogenesis has been traced
since the Early Paleogene, and nannoplankton and foramini-
fer associations found in this most complete section enable
us to carry out direct correlations with oceanic time scales.
Moreover, the cyclicity traced in the Neogene marine sedi-
ments of the Azov-Black Sea region is precisely reflected in
complexes of various facial compositions on seismic profiles
as abiotic events (Maslun et al. 2007), and is also clearly man-
ifested in the development of the microplankton biota – that
enabled us to substantiate the recognition of some correla-
tion levels.
Using all published materials on microplankton from the
territory of Ukraine, including new, often unpublished data
we attempted to carry out biostratigraphic correlation of the
Paratethys Sea Neogene sediments. The review attempted to
specify maximally the Regional Neogene Chart/Time Scale
of the Central and Eastern Paratethys for the territory of
Ukraine and to correlate it with the International Stratigraphic
Chart/Time Scale (ISC). The papers of Piller et al. (2007),
ter Borgh et al. (2013) and Neubauer et al. (2015) were used
as etalon/standard for division of the Central Paratethys
Neogene, as well as the Mediterranean stages affirmed in
ISC (Gradstein et al. (ed.) 2012). For the Eastern Paratethys
Neogene the following regional divisions were adopted:
Caucasian, Batisifonian (Sakaraulian and Kotsakhurian),
Tarkhanian, Chokrakian, Karaganian Konkian, Sarmatian,
Meotian, Pontian, Kimmerian, Kuyalnikian (Akchagilian),
Fig. 2. Distribution of the Neogene deposits of Ukraine. Explanatory notes: Study areas of the Carpathian region – Central Paratethys:
1a – Transcarpathian Basin, 1b – Outer Carpathian nappe units, 1c – Carpathian Foredeep, 1d – Adjacent part of the Eastern European
Platform. Study areas of the Eastern Paratethys: 2 – Northern margins of the Black Sea – Northern Prichornomorye region, 3 – Crimea
and Kerch Peninsula, 4 – Azov-Black Sea area.
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and Apsheronian – modifying the division of Popov et al.
(2004), Vasiliev et al. (2011) and Stoica et al. (2013).
For the purpose of definition of correlation levels, the
most complete sections of the Central Paratethys were stud-
ied in north-western Ukraine (Transcarpathian Basin, Outer
Carpathian nappe units, Eastern Carpathian Foredeep and the
adjacent part of the Eastern European Platform). The Eastern
Paratethys sequences were studied in south-eastern Ukraine,
at natural sections and boreholes in the Northern Prichorno-
morye region adjacent to the Crimea and Kerch Peninsula and
the Azov-Black Sea area (Fig. 2). The results of integrated
techniques were used as well, including bio-, litho-, cyclo- and
magnetostratigraphic investigations for some temporal inter-
vals. The detailed analysis of the distribution of microfossils
(planktonic foraminifers, nannoplankton and dinocysts) in the
Neogene deposits enabled us to recognize 10 associations of
marine plankton (correlation levels) that gave a possibility to
specify the age and diachronous nature of lithostratigraphic
units and so contributed to division of the Neogene sedimen-
tary record. Definition of levels with similar associations of
marine plankton also enabled correlation in the framework of
the Central and Eastern Paratethys regional stages and demon-
strated their positions in relation to the ISC stages.
Definition of the correlation levels
Correlation level I represents the lower boundary of the
Neogene time interval. It is substantiated by three planktonic
groups in the Carpathian region and traced by the last ap-
pearance of the dinocysts Membranophoridium aspinatum,
Chiropteridium galea, nannoplankton assemblage with
Sphenolithus delphix and the first appearance of the plank-
tonic foraminifer Globoquadrina dehiscens. It is traced in
the middle part of the Grushevo Formation of the Transcar-
pathian Basin (eastern part of the Central Paratethys) and in
the upper part of the Krosno and Menilite formations of the
Outer Eastern Carpathians of Ukraine (Andreeva-Grigorovich
2004). In the Eastern Paratethys realm, the lower boundary
of the Miocene is substantiated by dinocysts. It is conven-
tionally traced in the rhythmic flysch-like sequence belong-
ing to the Caucasian regional stage (Karadzhalganian – see
e.g. Neubauer et al. 2015), which was recognized as an ana-
logue of the Aquitanian on the basis of benthic foraminifers,
ostracods, spores and pollen. Due to the almost complete
absence of carbonate facies, the nannoplankton and plank-
tonic foraminifers are present only in the borehole sections
of the Azov-Black Sea aquatory. The boundary is conven-
tional and is traced in the rhythmic flysch-like sequence of
the Kerleut Formation (Maslun et al. 1989, 2005, 2007;
Gozhyk et al. 2006; Gradstein et al. (ed.) 2012) accounting
for the change of complexes with Globigerina ciperoensis,
Gl. praebulloides and the biota complex without foramini-
fers but with a significant content of sponge spicules and fish
skeletons. Higher, at the level of the NN1 Zone, a mixture of
the Oligocene and Lower Miocene foraminifers is found.
This situation is characteristic for the interval of “Maikop
sediments” practically of the whole Crimean-Caucasian re-
gion. On this basis the Caucasian regional stage s.l. was di-
vided into two substages: Lower Caucasian s.str (Oligocene)
and Upper Caucasian (Lower Miocene) in the interval from
23.03 Ma (lower boundary of the Aquitanian) – to ~ 20.43 Ma
was placed the lower boundary of the Sakaraulian and Burdi-
galian stages.
The Chattian/Aquitanian boundary in the Central Para-
tethys deposits of Ukraine has been placed in the Grushevo,
Krosno, and Menilite formations and ranked as the Egerian
regional stage (Fig. 3). In the Eastern Paratethys, it is traced
between the Lower Caucasian regional sub-stages (Chattian)
which include the Askania, Gornostay and a part of the Ker-
leut formations and the Upper Caucasian (Aquitanian) which
includes the Chernobaivsk, Batisifon, and Arabat formations
and the top – upper part of the Kerleut Formation (Fig. 4).
Correlation level II traced in the nannoplankton zone
NN3 contains the foraminifers Globigerinoides primordius,
Globigerinella obesa and was recognized in the upper part of
the Illichivsk Formation of the Azov and Black Sea shelf and
is considered to be an analogue of the upper part of the
“Batisifonian Formation” of Crimea and related to the Batisi-
fonian regional stage (Sakaraulian and Kotzakhurian – see
e.g. Neubauer et al. 2015). In the Central Paratethys we com-
pare these deposits with the Burkaliv Formation (Transcar-
pathian Basin) deposited in the eastern part of the Central
Paratethys and to the lower part of the Stebnik Formation
(Carpathian Foredeep) ranked approximately to the Upper
Eggenburgian and Lower Burdigalian of the ISC (Andreeva-
Grigorovich 2005).
Correlation level III is substantiated through the analy-
sis of available data on the nannoplankton and foraminifers,
which enabled us to recognize the boundary of the Lower—
Middle Miocene deposits of the Alma Depression. The com-
plex of nannoplankton from zone NN4 and the foraminifer
Globigerinoides bisphericus in turn enabled us to correlate
these deposits with the Batisifonian and the lowermost
Tarkhanian (Kamyshlak Member). Therefore, the Lower Mio-
cene deposits of the Eastern Paratethys in the territory of
Ukraine incorporate the upper part of the Caucasian s.l. and
Batisifonian regional stages and can be correlated with the
Central Paratethys regional stages: upper part of the Egerian,
Eggenburgian, Ottnangian and Karpatian and compared to the
Aquitanian and Burdigalian stages of the ISC (Figs. 3 and 4).
The position of the Lower and Middle Miocene boundary,
both in the stratotype site (Kerch Peninsula) and the whole
Eastern Paratethys is a subject of discussion. Various scien-
tists have traced it differentially. Andrusov (1965) put it at
the base of the Chokrakian regional stage, Zhizhchenko and
Merklin related it to the base of the Tarkhanian, moreover
Nosovsky and co-authors (Nosovsky et al. 1976) expanded
the volume of the Tarkhanian including into it the Kamy-
shlak Member (Lower Tarkhanian), layers with Lentipecten
denudatum (Middle Tarkhanian or Tarkhanian s. str.) and the
Yurakivka Member (Upper Tarkhanian or Spirialis clays).
They traced the Middle Miocene boundary at the bottom of
the Kamyshlak Member (Tarkhanian s.l.). Later, Nosovsky
and co-authors considered the greater part of the Spiralis
clays as the Chokrakian deposits and traced the Middle Mio-
cene boundary at the base of the Chokrakian regional stage
again (Nosovsky 2001).
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Fig. 3. Correlation of the Neogene sediments of the Central Paratethys of Ukraine with the International Stratigraphic Chart (Gradstein et
al. 2012).
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Fig. 4. Correlation of the Neogene sediments of the Eastern Paratethys of Ukraine with the International Stratigraphic Chart (Gradstein et
al. 2012).
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In the Sambor Zone of the Eastern Carpathian Foredeep,
the Lower/Middle Miocene boundary is diachronous and is
traced in the sub-salt bearing layers with the complex of nan-
noplankton of the NN4 Zone – which is also recognized in
the upper part of the Stebnik Formation and the lower por-
tion of the Balychi Formation. In the Biltsche-Volitsa Zone
of the Eastern Carpathian Foredeep and within the sedimen-
tary cover of the Eastern European Platform, the base of the
Middle Miocene deposits (Lower Badenian regional sub-
stage) occur in the basal part of the Bogorodchany Forma-
tion, as well as at the basis of the Nagornyanski Member
containing nannoplankton of the NN4 Zone upper part
(Fig. 3). The overlying Opolie Formation on the platform
contains the NN5 and M6 zones. In the Transcarpathian
Basin the Lower Badenian sediments were deposited above
an erosional surface. They are built up by the Tereshul
Conglomerate Member of the Novoselytsya and Vodytsya
formations (NN5 Zone – Sphenolithus heteromorphus and
M6 – Orbulina suturalis).
Correlation level IV with nannoplankton of the NN5
Zone and foraminifers Praeorbulina glomerosa, Globigerina
tarchanensis was recognized in deposits of the Tarkhanian
Formation s.str. and lower part of the Spirialis Clay. To-
wards the end of accumulation of the Spirialis Clay and in
the Chokrakian time the connection to marine aquatories de-
teriorated and salinity declined. The benthos is also steadily
abundant but as early as in the Karaganian time the connection
is lost, and the plankton of the NN5 Zone is found only in the
north-western shelf together with the elfidio-nonionella fora-
miniferal complex (Maslun et al. 2007).
The above mentioned facts indicate significant differences
in the foraminiferal plankton associations of the Central and
Eastern Paratethys at the beginning of the Middle Miocene.
For the Eastern Paratethys the most characteristic is an older
complex that includes the top of zone NN4 and lower por-
tions of the NN5 Zone together with a foraminifer associa-
tion with Praeorbulina glomerosa. In the Central Paratethys,
this interval in the majority of regions is distinguished by a
sedimentation break, and the Lower Badenian is represented
by the calcareous nannoplankton zone NN5 and foraminifers
with Orbulina suturalis. The data stated above enabled us to
compare the Tarkhanian, Chokrakian and Karaganian re-
gional stages of the Eastern Paratethys with the Lower Bade-
nian in the Central Paratethys and the Langhian stage of the
ISC (Figs. 3 and 4).
At the end of the Early Badenian (NN5) and beginning of
the Late Badenian (NN6) salt accumulation took place in the
Transcarpathian Basin and Carpathian Foredeep. The estab-
lished correlation level V enables us to correlate deposits of
the Eastern Paratethys Konkian stage with the Upper Bade-
nian substage of the Central Paratethys and the Lower Ser-
ravalian of the ISC. In the Eastern Paratethys, the typical
marine sedimentation is renewed after the partial isolation
and desalination that is indicated by the appearance of the
marine nannoplankton association of the NN6 Zone and for-
aminifers Globigerina bulloides, Gl. cognata, Paragloboro-
talia mayeri and others at the base of the Konkian
(Andreeva-Grigorovich & Nosovsky 1976; Maslun et al.
2006). In the Central Paratethys, the marine sedimentation
continued during the whole Late Badenian; in sediments
nannoplankton of the lower part of the NN6 Zone was recog-
nized, as well as the planktonic foraminifera Globigerina
bulloides, Gl. concinna, Velapertina indigena etc. Only in
the latest Badenian the links to the marine aquatories became
worse, except in the Sambor zone. The marine association of
the NN6 Zone in the Teresva and Baskiv formations became
poorer, and euryhaline species with a wide stratigraphic range
prevailed (Fig. 3).
The Sarmatian deposits in the Central and Eastern Para-
tethys usually contain calcareous nannoplankton of the eury-
haline species Braarudosphaera bigelowii, Reticulofenestra
pseudoumbilicus, Calcidiscus macintyrei, Sphenolithus abies
that often form monospecies complexes depending on envi-
ronmental conditions in a sedimentary basin (Andreeva-
Grigorovich 2006). Benthic foraminifers are abundant –
miliolids, elfidia, sacammines and others predominate. The
recognized marine plankton associations of the Eastern
Paratethys in sediments of the Sarmatian s.l. enabled us to
specify the time span of the Sarmatian s.str. in the Central
Paratethys (Fig. 3) and to put the correlation level VI in-
side the Bessarabian regional sub-stage (Fig. 4), as well as to
substantiate the Middle/Upper Miocene boundary.
In sediments dated as the Sarmatian and Pannonian re-
gional stages (Slovakia, Poland, Romania, and Ukraine) the
nannoplankton of zones NN6, NN7, NN8, NN9, NN10 and
NN11 have been recognized. For the Eastern Paratethys, the
nannoplankton of the NN8 Zone was found for the first time
in the Middle Sarmatian deposits of Georgia, then in the
Near-Azov region (Semenenko 2003; Semenenko et al.
2009), sections of the Azov-Black Sea shelf (Semenenko
1987; Maslun et al. 1989; Gozhyk et al. 2010) and in the Da-
cian Basin in Romania (Mărunueanu 1977, 1991, 1999;
Lulieva 1991; Semenenko & Lulieva 2006) and so together
with the NN9a in the Eastern Slovakia part of the Transcar-
pathian Basin), it represents the correlation level VI.
The Middle Miocene Langhian and Serravallian stages (of
ISC) correspond in the Central Paratethys to the Badenian and
Sarmatian s.str. regional stages, and the Middle/Upper Mio-
cene boundary is situated at the top of the Sarmatian s.str.
(Fig. 3). In the Eastern Paratethys region, the Middle Miocene
includes the Tarkhanian, Chokrakian, Karaganian, Konkian,
Lower Sarmatian s.l. – Volhynian sub-regional stage, and
the lower part of the Middle Sarmatian s.l. – Bessarabian
sub-regional stage. The Middle/Upper Miocene boundary is
traced in the middle part of the Bessarabian sub-regional
stage (Fig. 4).
Correlation level VII corresponds to the marine plank-
ton association with Discoaster hamatus, D. neohamatus, D.
neorectus and others (NN9—NN10 zones) and planktonic
foraminifers Globigerina bulloides, Gl. brevispira, Globoro-
talia scitula, Globigerinoides trilobus, Paragloborotalia
mayeri and abundant benthic foraminifers. It is traced in the
Meotian sediments of the Baherovo Member and Akmanai
Formation at the Kerch Peninsula and Azov-Black Sea re-
gion (Maslun et al. 1989, 2007; Shniukov & Grigorjef 1990;
Gozhyk et al. 2011). In the Central Paratethys, the analogous
nannoplankton associations without planktonic foraminifers
are found in the lower part of the Berezhnytsya Formation
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(marine analogue of the Lake Pannon sediments) in the Sam-
bor Zone of the Carpathian Foredeep in Ukraine, Poland and
Romania (Semenenko & Pevzner 1979; Andreeva-Grigo-
rovich 2006). This gives us a reason to compare the Kherso-
nian and Meotian stages of the Eastern Paratethys with the
Lower Pannonian deposits of the Central Paratethys and with
the Lower Tortonian of the ISC (Figs. 3 and 4).
Correlation level VIII is recognized in the boundary de-
posits of the Meotian and Pontian regional stages of the East-
ern Paratethys (Novorossiysk Member) on the basis of
planktonic foraminifers Globigerinoides extremus and rare
nannoplankton findings (Amaurolithus primus, A. delicatus,
A. tricorniculatus) at the top of the Meotian strata. It is nec-
essary to point out the presence of the endemic Isolithus
semenenko in the Pontian of the Kerch—Taman region and
Black Sea coast of the Caucasus (Lulieva 1989). It is also
widespread in the Late Pannonian sediments of Austria, Ser-
bia and Croatia (Ćorić 2004).
The Miocene—Pliocene boundary at the level of 5.322 Ma
is “fixed” between the Messinian and Zanclean stages of
SCI, and most usually between the Pontian and Kimmerian
in the Black Sea (Euxine) Basin of the Eastern Paratethys.
The position of this boundary in the Central Paratethys is un-
certain (e.g. Neubauer et al. 2015).
Correlation level IX is recognized in the sediments of
the Azov Member, which belongs to the Kimmerian regional
stage (Fig. 4). It is a nannoplankton association with Ce-
ratolithus acutus (NN12 Zone). This level is traced in
the Dacian deposits of south-western Ukraine (nearby t.
Reni – Pevzner et al. 2003). In some sections, Ceratolithus
rugosus is met together with C. acutus. The appearance of
nannofossils of the younger NN13 Zone also confirms the
Pliocene age of Kimmerian deposits above the Azov Mem-
ber. This level characterizes the Miocene/Pliocene boundary
and therefore should correspond to the Messinian and Zan-
klean of the ISC.
Correlation level X represents the last appearance of
Discoaster brouweri and Discoaster pentaradiatus (Fig. 4).
The Pliocene/Pleistocene boundary in marine sediments
(1.8 Ma) is related to the extinction of this genus. This level
is recognized in the Taman Member (Middle and Upper
Akchagylian) of Eastern Crimea and the Akchagylian sedi-
ments of the Caspian Basin (Yasamal valley, Azerbaijan –
Semenenko & Lulieva 1978, 2006).
Discussion—conclusions
The recognized correlation levels substantiated by micro-
fossils give the possibility of a more exact comparison be-
tween the Regional stages of the Central and Eastern
Paratethys and the ISC (Figs. 3, 4). The determined marine
plankton associations testify to the inherited cyclic sedimen-
tation in the Neogene basins of the Paratethys and enable us
to trace possible migration routes of the foraminiferal and
nannoplankton biota in the marine water masses of the whole
Paratethys.
The presence of the Tarkhanian plankton association (top
of NN4 Zone and the lowermost part of NN5 Zone and Prae-
orbulina glomerosa) in the deposits of the northwestern
shelf and central depression of the Black Sea in Ukraine,
Russia, and Bulgaria (Varna region), the Sea of Azov, and
Central Georgia gives a basis for supposing the existence of
one whole marine basin system that was united with the Medi-
terranean region. However, starting in the Late Tarkhanian,
the sedimentation regime in the basin changed. The shift in
depositional environment was connected with the geody-
namics of the Black Sea area, which led to changes in its
morphostructure and evidently disturbed the links to the
Mediterranean and Central Paratethys regions. Tectonic pro-
cesses in the Central Paratethys domain were followed later
by a vast marine transgression in the Early Badenian (time of
nannoplankton NN5 Zone and the first common appearance
of Orbulina suturalis (Fig. 3).
The determination of oceanic nannoplankton associations
in zones NN8 and NN9 in the Sarmatian sediments of the
Eastern Paratethys enables us to conclude that the desalina-
tion of the Sarmatian basins was not simultaneous for the
whole Paratethys and is characteristic for the marginal facies
(Figs. 3 and 4). The marine sedimentation continued till the
mean time of the ISC Tortonian stage (Middle Sarmatian
transgression in the Eastern Paratethys).
The presence of the nannoplankton complexes and plank-
tonic foraminifers in sediments of the Eastern Paratethys dur-
ing the Early Meotian, Pontian, Kimmerian and Kuyalnikian
(Taman Member, Upper Pliocene) testifies to the periodical
relations between the Eastern Paratethys and open marine
aquatories. The analysis of the available data demonstrates
that in the Kimmerian, namely at the Miocene—Pliocene
boundary, the Mediterranean, Black and Caspian Seas existed
in outlines close to their recent ones. The presence of disco-
asters in the Upper Pliocene sediments proves the connections
of both the Caspian and Black Seas to the Mediterranean Sea
till the beginning of the Pleistocene, and in deeper parts of
the aquatories the inherited sedimentogenesis is observed in
the Quaternary as well.
Acknowledgments: The authors express their thanks to col-
leagues from the Department of Geology and Paleontology,
Faculty of Natural Sciences, Comenius University in Bra-
tislava, for the technical help and fruitful discussions.
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