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საქართველოს ეროვნული მუზეუმის მაცნე, საბუნებისმეტყველო და პრეისტორიული სექცია, №5, 2013, 68-75
Proceedings of the Georgian National Museum, Natural Sciences and Prehistory Section, #5, 2013, 68-75
68
PALEOBIOLOGY
THE RESULTS OF MICROPALEONTOLOGICAL ANALYSIS OF THE LATE MEOTIAN -
EARLY PONTIAN DEPOSITS OF THE BLACK SEA REGION
Lamara Maissuradze,
1
Irina Shatilova,
2
Mzia Vekua
†
, Kakhaber Koiava,
3
Irma Kokolashvili,
4
Luara Rukhadze
5
1,2,5
Georgian National Museum, L. Davitashvili institute of Paleobiology, 0108, Tbilisi. irashatilova@yahoo.com
3
Ivane Javakhishvili State University, Alexandre Janelidze Institute of Geology, Tbilisi. koiava_ka@yahoo.com
4
Georgian Technical University, Tbilisi. irmakokolashvili@gmail.com
Abstract
. The results of microfaunistical and palynological analysis of the Late Meotian - Early Pontian
deposits of Eastern part of the Black Sea region are presented in the work. The data on the mollusks fauna
studied from the same deposits were also used.
The microfaunistical analysis
In the Black Sea region the Lower Pontian is divided into two horizons – Eupatorian and Odessian.
Eupatorian layers were established by Davitashvili (1933, 1937) on territory of Crimea, near the town Eupatoria.
They contain the impoverished assemblages of brackish mollusks of the genera Eupatoria, Dreissena, Congeria,
Prosodacna and others.
In the Eastern part of the Black Sea region the Eupatorian horizon first was established in outcrop on
river Atapi (the left tributary of r. Duabi, between the villages Chlou and Tkhina). Here are exposed deposits
of Meotian on which the whole Pontian is conformably bedded (Taktakishvili, 1985). The following
layers are
exposed beginning from the bottom of the section:
1.
Stratified, bluish-gray clays, which are changed by sandstones. The mollusks are represented mainly
by
brackish species: Congeria novorossica (Sinz.), C. panticapaea Andrus., Theodoxus stephanescui (Font.),
Caspiohydrobia starabogatovi L. I., C. tamanensis L. I., Turricaspia brusinae (Andrus.), Sphaeronassa mutabilis
andrusovi Dav. By opinion of Badzoshvili (1986) this is the impoverished part of Early Meotian
assemblage in
which the mediterranean species are mainly preserved. Most of them are widely distributed in the Meotian
deposits of Eastern Paratethys.
The Upper Meotian assemblage of foraminifers is represented by following species: Quinqueloculina
seminulum maeotica Gerke, Cycloforina gracilis Karrer, Sinuloculina ex. gr. consobrina
(d’Orb.), Miliolinella
ex. gr. circularis (Born.), Elphidium macellum maeotica Gerke, E. feodorovi Bogd., Ammonia becarii (L.). The
species, similar to mediterranean stenobiontic forms were not seen.
The assemblage of ostracods is composed from the following species: Leptocythere maeotica (Livent.),
L.
scabrida Suzin, L. sulakensis Suzin, Cyprideis littoralis (Brady), C. punctillata Brady, Loxoconcha eichwaldi
Livent., Caspiocypris candida (Livent.), Candona propria Popch., Caspiolla balkanica (Zal.).
2.
Bluish-gray sandy clays, with interlayers of yellow sandstones (40-50 cm) and lens with coquina, in
which are determined: Congeria novorossica (Sinz.), C. panticapaea Andrus., Prosodacna littoralis (Eichw.),
Lythoglyphus (?) sp. Thickness of layer 4 m.
საქართველოს ეროვნული მუზეუმის მაცნე, საბუნებისმეტყველო და პრეისტორიული სექცია, №5, 2013, 68-75
Proceedings of the Georgian National Museum, Natural Sciences and Prehistory Section, #5, 2013, 68-75
69
3.
Yellowish-gray sandy coquina, composed mainly from
Prosodacna littoralis
(Eichw.). Except this spe-
cies are presented:
Congeria novorossica
(Sinz.),
C. panticapaea
Andrus.,
C . navicula
Andrus.,
Hydrobia
sp.,
Neritina
sp.,
Micromelania
sp. Thickness of layer is 10m.
In the layers 2 and 3 the following foraminifers were seen: Quinqueloculina seminulum maeotica Gerke,
Elphidium macellum maeotica Gerke, E. ex gr. pontica Dolgopolskaya et Pauli, Porosononion ex. gr. subgranosus
(Egger), Ammonia beccarii (L.). The assemblage of ostracods is richer than in layer 1 and is composed
from the
following forms: Caspiolla acronasuta (Livent.), Caspiolla venusta (Zal.), Caspiocypris labiata (Zal.), Candona sp.
Cypria sp., C. tocorjescui Hanganu, Pontoniella accuminata (Zal.), P. loczyi (Zal.), Cyprideis torosa Jones, C.
punctilata pliocenica Rosjeva, Leptocytere goitensis (Suz.), L. crebra (Suz.), L. ex gr. gutata Suz., L. collativa Suz.,
L. praebacuana Livent., L. pontica Suz., L. microlata ( Livent.), Loxoconcha eichwaldi Livent., L. ex gr. temperata
Olteanu.
4.
Bluish-gray sandy clay, with mollusks fauna: Dreissena sp., Pontalmyra (?)sp., Pseudocatillus pseudo-
catillus (Barb), Prosodacna littoralis (Eichw.), Parvivenus widhalmi Sinz., Abra tellinoides (Sinz.), Lythoglyphus
(?) sp. Thickness of layer is 20m.
5.
Bluish-gray clay, here and there sandy, with Paradacna abichi (R. Hoern.). In clays are also seen: Con-
geria novorossica (Sinz.), Prosodacna littoralis (Eichw.) and Hydrobia sp. Nearly on 15 m from base is located a
small (0,4-0,5 m) intercalation of sandy clay with Dreissena tenuissima Andrus., Pseudocatillus pseudocatillus
(Barb.), Prosodacna littoralis (Eichw.), Parvivenus widhalmi (Sinz.), Hydrobia sp., Neritina sp. The upper part of
layer (20-25m) contains macroremains of plants. Thickness of layer is nearly 50m.
The layers 4 and 5 contain single foraminifers: Quinqueloculina seminulum maeotica Gerke and
Ammonia beccarii (L.). Among ostracods are presented Pontoniella accuminata (Zal.), P. loczyi (Zal.), Bakunella
dorsoacuata (Zal.), Cypria tocoriesqui Hanganu, Leptocythere andrussovii Livent., L. multituberculata Livent.,
L. praebacuina Livent., L. bosqueti Livent., L. cellula Livent., Pontoleberis pontica Stanc., Loxoconcha djaffarovi
Schneid., Xestoleberis sp.
By data of fauna in Atapi outcrop the deposits of Upper Meotian (layer 1) and Lower Pontian (layers 2-5)
are presented. The layers 2 and 3 belong to Eupatorian and the layers 4, 5 to Odessian horizon.
By data of macrofauna the deposits of Eupatorian are characrerized by impoverished assemblage of
brakish
mollusks. According to the data of Ebersin (1949) in the Black Sea–Caspian region the representatives
of the genera Eupatoria, Dreissena, Prosodacna, Monodacna first appeared in Eupatorian. But more important
is the fact of origin of several Prosodacna from the group “littoralis “on one and the same stratigraphical level.
In Pliocene the expansion of brackish Cardiidae in basins of Ponto-Caspian region began by these forms.
As for microfauna in Meotian the predominate fossils are foraminifers. The ostracods are represented by
single tests. The picture is changed in Eupatorian, in which deposits the abundance and specific variety of
ostracods are increased. The assemblage has a mixed Meotian - Pontian compositon, the genera Pontoniella
and Bakunella are appeared here for the first time. The genera Leptocythere and Loxoconcha are represented
by numerous species. The number of foraminifers and their specific composition is small. The assemblage
com
posed from euryhaline species, which morphologically differ from taxa widely distributed in the Late
Meotian. So, it is possible to say, that in Eupatorian the both assemblages are of mixed Meotian-Pontian
composition.
In Odessian time (Lower Pontian) from the several basins of Paratethys into Rionian Bay, besides the
species of genera Pontoniella and Bakunella, the representatives of genera Caspiocypris, Lineocypris, some
Leptocythere, Loxoconcha djaffarovi Schneid, and Cytherura perata Schneider also penetrated. The Meotian
relicts disappeared fully, but the common assemblage of ostracods became richer (Imnadze, 1974; Djanelize et
al., 1985).
The ecological conditions of desalted Odessian Sea were fatal for foraminifers and in deposits of the
საქართველოს ეროვნული მუზეუმის მაცნე, საბუნებისმეტყველო და პრეისტორიული სექცია, №5, 2013, 68-75
Proceedings of the Georgian National Museum, Natural Sciences and Prehistory Section, #5, 2013, 68-75
70
Odessian horizon they are represented by single Quinqueloculina seminulum maeotica and Ammonia beccarii.
In Western Georgia the second outcrop of Eupatorian horizon is situated in vicinity of village Bia. The
following layers are exposed here:
1.
Gray-bluish sandy clays with Congeria subnovorossica Osaul, Hydrobia sp., Congeria panticcapaea An-
drus., Abra tellinoides Siniz., Nassa sp., Cyprideis littoralis Brady. On basis of this fauna the age of deposits is
dated as Upper Meotian (Chelidze, 1971,1974; Popkhadze , 1974).
2.
Yellowish-gray sandstone without mollusks. The foraminifers are represented by Ammonia beccarii
(L.), Porosononion sp., Elphidium ex gr. macellum (F.et M.), Nonion ex gr. bogdanowiczi Volosh. and ostracods
by Caspiolla acronasuta (Livent.), Caspiocypris labiata (Zal.), Bakunella dorsoarcuata (Zal.), Pontoniella accumi-
nata (Zal.), P. loszyi (Zal.), Hemicythera marinescui Olteanu, Urocytheris (Drobetiella) ex gr. mirabilis Olteanu,
Cyprideis littoralis (Brady). Thickness of layer 10-15m.
3.
Grey-bluish clays with badly preserved mollusks. Thickness of layer 3m.
The mixed character of microfaunistical assemblage, the presence of Upper Meotian species side by side
with species typical for Pontian and the presence of foraminifers peculiar for brackish basins of the Late Meo-
tian allows to date the layer 2 of Bia outcrop as Eupatorian (Vekua 1979).
The layer 3 contains the microfaunistical assemblage, in which the foraminifers and Meotian species of
ostracods are absent. In whole the assemblage is poor and monotonous, without forms typical for the Middle
Pontian, which are represented in uppermost part of outcrop together with mollusk fauna. Accordingly, the
age of the layer 3 is determined as Odessian.
The data about the microfauna of the Upper Meotian and Lower Pontian were used by Suladze (1984) for
ecosystemic analysis of sedimentation basin of Eupatorian deposits. In the section near town Eupatoria two
assemblages of foraminifers and ostracods of different age were established.
In lower part of outcrop foraminifers are represented by the following species: Quinqueloculina seminu-
lum maeotica Gerke, Cycloforina aff. gracilis (Karrer), Affinetrina sulacensis Gerke, A. ludwigi (Reuss), Ammonia
beccari (L.), Elphidium ex. gr. macellum (F. et M.). Among ostracods were determined: Leptocythere praebos-
queti Suz., L. collativa Suz., Loxoconcha eichwaldi Livent., Loxoconcha sp., Leptocythere sp., Cyprideis littoralis
Brady, Mediocytherideis praeapotoica Schweier, Xestoleberis sp., Cyprinotus ex gr. triangularis Kasimova. The
dominate role in this assemblage belongs to foraminifers. As for ostracods, they are represented by single
individuals of Upper Meotian age.
The ostracods are represented by numerous individuals in the upper part of strata: Caspiolla acronasuta
(Livent.), Caspiocypris candida (Livent.), Cypria tocoriescui Hanganu, Cyprinotus ex. gr. triangularis Kasimova,
Pontoniella acuminata (Zal.), P. loczyi (Zal.), Leptocythere microlata (Livent.), L. praebosqueti Suz., L. goitensis
Suz., L. praebacuana Livent., L. bosqueti (Livent.), L. collativa Suz., L. pontica Suz., Loxoconcha eichwaldi Livent.,
L. valiente Stanceva, L. ponticus Agal., Leptocythere sp., Cyprideis littoralis Brady, C. punctillata (Brady), C. ex.
gr. torosa (Jones), Mediocytherideis praeapotoica Schweier. Foraminifers are represented by numerous indi-
viduals of two species: Cycloforina aff. gracilis Karrer and Elphidium ex. gr. macellum (F. et M.). These species
were passed from the Meotian, but morphologically were changed.
In rich assemblage of Ostracods the following group of species can be distinguished:
1.
The species common with those of Upper Meotian:
Leptocythere praebosqueti Suz.,
L. collativa Suz.,
Loxoconcha eichwaldi Livent.
Cyprideis littoralis Brady.
Mediocytherideis praeapotoica Schweier.
Cyprinotus ex. gr. triangularis Kasimova.
საქართველოს ეროვნული მუზეუმის მაცნე, საბუნებისმეტყველო და პრეისტორიული სექცია, №5, 2013, 68-75
Proceedings of the Georgian National Museum, Natural Sciences and Prehistory Section, #5, 2013, 68-75
71
2.
The species common with those from the Upper Meotian and Pontian deposits of Dacian basin: Caspi-
olla acronasuta (Livent.) and Caspiocypris candida (Livent.). But in the Black Sea-Caspian basins these species
are presented only in Pontian together with:
Leptocythere goitensis Suz.,
L. pontica Suz.,
Loxoconcha ponticus Agal.
3.
The species migrated from Pannonian and Dacian basins in Pontian time:
Cypria tocoriescui Hanganu.
Leptocythere microlata (Livent.)
L. praebacuana Livent.
Loxoconcha valiente Stanceva.
4.
Pontian species from Paratethys basins:
Pontoniella acuminata (Zal.)
The mixed Upper Meotian - Pontian composition of given above assemblages indicates its Eupatorian
Age.
So, judging from the composition of microfanustical assemblages of the Upper Meotian and Pontian
between these two stretches of Neogene, the succession of fauna took place in both regions, in the Western
Georgia and in Crimea. The common species for foraminifers are: Quinqueloculina seminulum maeotica, Q.
aff.pontica, Cycloforina gracilis, Elphidium macellum. The number of ostracods is much numerous: Caspiolla
acronasuta, Cypria tocorriencui, Pontoniella acuminata, P. loczyi, Leptocythere goitensis, L. collativa, L.
praebacuana,
L. pontica, L.microlata, Loxoconcha eichwaldi, Cyprideis littoralis, C. punctillata. In this list are
given both, the forms passed from Upper Meotian and properly Pointian species, which first appeared in Early
Pontian. Also the species characteristic for the Black Sea - Caspian and Pannonian - Dacian basins are given
here. This make easier the correlation of Pontian deposits of whole Eastern Paratethys.
Our investigations confirms the opinion of Davitashvili (1937, p. 580) about similarity of bionomical condi-
tions of Upper Meotian and Eupatorian basins. Judging from the history of development of Meotian and Early
Pontian foraminifers and ostracods (Djanelidze et al., 1985; Maissuradze, 1988) it is possible to conclude, that
gradually deterioration of bionomical conditions promoted the disappearance of foraminifers in Pliocene ba-
sins of Paratethys. Their extinction began in the Late Meotian and finished in the Middle Pontian. The decrease
of salinity was the main factor that influenced this process. The composition of brackish and freshwater mo-
llusks distributed during these epochs and also the abundance of ostracods characteristic for freshwater basins
indicates the above fact (Davitashvili, 1933, 1937; Ebersin, 1049, 1967; Taktakishvili, 1978; Suladze, 1984; Im-
nadze, 1974; Djanelidze et al., Popkhadze 1978; Nevesskaya et al., 2003; Maisuradze, Koiava, 2011). The salinity
of water in basins of the Late Meotian and Pontian is determined as 5 ‰, that was pernicious for foraminifers,
but favorable for osracods, which in Pliocene became the dominant group of fossil microorganisms.
The palynological analysis
The Lower Pontian is widely distributed on whole territory of Western Georgia, but only in three localities
(on the Atapi and Zana rivers and near village Bia) the Novorossian substage is represented by a full series of
deposits. In all other sections the Eupatorian is absent and the Lower Pontian begins with the Odessian hori-
zon (Chelidze 1974; Shengelia, 1976; Taktakishvili, 1984).
The palynological analysis samples from the Atapi and Zana deposits revealed that the changes in pollen
assemblages at the boundary of the Miocene and Pliocene were similar in both sites (Shatilova et al., 2011).
საქართველოს ეროვნული მუზეუმის მაცნე, საბუნებისმეტყველო და პრეისტორიული სექცია, №5, 2013, 68-75
Proceedings of the Georgian National Museum, Natural Sciences and Prehistory Section, #5, 2013, 68-75
72
In the beginning of the Late Meotian the territory of Western Georgia was covered with rich forest vegeta-
tion, distributed on different levels of mountain relief. Middle and lower mountain belts were covered with
polydominant forest, which were composed of subtropical and warm-temperate conifers and broad-leaved
trees: Podocarpus, Dacrydium, Cedrus, Keteleeria, Cathaya, Taxodiaceae, some species of Carya, Quercus, Fa-
gus, Castanea, Juglans, Platanus, Nyssa and the numerous genera of family Hamamelidaceae. The forest un-
derstory consisited of subtropical ferns such as Dicksonia, Gleichenia, Anemia, Polypodium, Pteris.
The beginning of the Late Meotian can be considered as the climatic optimum. The decreasing role of
dark-conifers and increase of pine forests was brought on by abrupt climatic changes in Early Pontian – Eupa-
torian time (fig.1,2).
Fig. 1. Palynological diagram of Meotian and Pontian deposits of section Atapi
Fig. 2. Palynological diagram of Meotian and Pontian deposits of section Zana
The pollen assemblages of Eupatorian show the transition from rich and diverse pollen flora of the Meo-
tian to poor assemblages with predominance of pine. The changes in composition of vegetation, probably,
were connected with decrease of humidity, phenomenon, which at the end of the Miocene embraced whole
Southern part of Russian Plain (Shchekina, 1979). In Odessian the pine was replaced by dark-conifer communi-
საქართველოს ეროვნული მუზეუმის მაცნე, საბუნებისმეტყველო და პრეისტორიული სექცია, №5, 2013, 68-75
Proceedings of the Georgian National Museum, Natural Sciences and Prehistory Section, #5, 2013, 68-75
73
ties, occupying almost all altitude. This suggest that after the Eupatorian the rise of humidity and decrease in
temperature took place.
After the Odessian the climate again became warm and humid, especially during the Middle part of
Portaferian, when the polydominant forest stabilized. It was probably during this climatic optimum that the
Kodorian flora accumulated.
The Pontian pollen assemblages we compared with those from synchronous deposits of Northern part
of
Black Sea coast. In both regions the rhythmic changes of epochs with different climates can be traced.
However in the Western Georgia the frequency and amplitudes of these changes were weaker.The main differ-
ences between the northern Black Sea coast and Western Georgia was in terms of humidity. In the north, the
Pontian was a time of declining temperatures and xerophytisation (Ananova, 1974), while in Colchis precipita-
tion increased side by side with gradually lowering of temperatures.
Conclision
On the basis of given above data it is possible to conclude, that in the history of marine microfauna the
Eupatorian was the turning-point. After Eupatorian nearly fully disappeared the foraminifers, which prevailed
in the basins of Eastern Paratethys during the whole Miocene and the predominate position was occupied by
ostracods.
Significant changes in composition of macrofauna were also connected with the beginning of Eupato-
rian.
In the Black Sea - Caspian region in this time first appeared genera: Didacna, Monodacna and Prosodacna.
On the territory of Western Georgia the Eupatorian was the turning- point also in history of climate and
vegetation, after which their dynamics was changed. During the whole Pliocene the gradually increasing of
frequency and amplitudes of climatic fluctuations was proceeded. This process received the highest degree of
development in the Pleistocene.
So, in Eastern part of the Black Sea region the Eupatorian horizon can be considered as the level, after
which the Miocene stage of development of marine and terrestrial biocenosis was changed by Pliocene one.
საქართველოს ეროვნული მუზეუმის მაცნე, საბუნებისმეტყველო და პრეისტორიული სექცია, №5, 2013, 68-75
Proceedings of the Georgian National Museum, Natural Sciences and Prehistory Section, #5, 2013, 68-75
74
paleobiologia
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mdore
,
gadas-
vliT
.
faunisturi
kompleqsebis
Semadgenloba
da
maTi
xasiaTi
calkeuli
ponturi
saxe-
obebis
meotur
winaprebTan
memkvidreobiTobas
aCvenebs
.
gvianmeotur
auzSi
ekologiuri
pirobebis
gauaresebam
(
ganmarilianeba
)
foraminife-
rebis
TandaTanobiTi
gaRaribebisa
da
Suaponturis
dasawyisisTvis
maTi
amowydomis
mTa-
vari
mizezi
gaxda
.
im
dros
rodesac
Seqmnili
bionomiuri
pirobebi
ostrakodebisaTvis
im-
denad
optimaluri
aRmoCnda
,
rom
maT
gafurCqvnas
anu
axali
gvarebisa
da
saxeobebis
gaCe-
nas
Seuwyo
xeli
.
msgavsi
procesi
grZeldeboda
mTeli
pliocenis
ganmavlobaSi
.
mikrofaunis
ganviTarebis
istoria
gvianmeoturi
da
adreponturi
saukuneebis
mijnaze
arsebul
mkveTr
gardatexas
aCvenebs
,
rac
Cveni
azriT
miocenuri
epoqis
dasasrulad
da
pliocenuris
dasawyisad
unda
miviCnioT
.
igive
iTqmis
xmeleTis
floris
istoriis
Sesaxebac
.
evpatoriulis
Semdeg
gvianmio-
cenuri
epoqis
SedarebiT
stabiluri
klimaturi
pirobebi
Seicvala
naklebad
stabiluri
pliocenuri
epoqisaTvis
damaxasiaTebeli
klimatiT
.
საქართველოს ეროვნული მუზეუმის მაცნე, საბუნებისმეტყველო და პრეისტორიული სექცია, №5, 2013, 68-75
Proceedings of the Georgian National Museum, Natural Sciences and Prehistory Section, #5, 2013, 68-75
75
References
1.
Ananova E.N. 1974.
The pollen in Neogene deposits of Southern Part of Russian Plain. Pub. H. of Leningrad
University: 196 (in Russian).
2.
Badzoshvili Ts. I. 1986.
The marine gastropod mollusks of Meotian, evolution and stratigraphic significans.
“Metsniereba” Publ.H., Tbilisi: 64 (in Russian).
3.
Chelidze G.F. 1971.
Division of Pontian. Bull. Georgian Acad.Sci., vol.64, #2: 349-352 (in Russian).
4.
Chelidze G.F 1974.
The marine Pontian of Georgia. “Metsniereba” Publ. H., Tbilisi: 216 (in Russian).
5.
Davitashvili L.Sh. 1933.
The review of mollusks of Tertiary and Post- Tertiary deposits of Crimea-Caucasus
oil province. “Gosnefttekhisdat” Publ.H., Moskow: 167 (in Russian).
6.
Davitashvili L.Sh. 1937.
To history and ecology of mollusks fauna of Lower Pliocene (Meotian-Pontian)
marin basins. The Problems of paleontology, vol. II-III, M.: 565-585 (in Russian).
7.
Djanelidze O.I., Vekua M.L., Maissuradze L.S 1985.
The development of foraminifers and ostracods
fauna from the Late Neogene of the Black Sea-Caspian basins. “Metsniereba” Publ.H., Tbilisi: 88 (in Russian).
8.
Ebersin A.G 1949.
About the origin of Pliocene Cardiidae in Euksinian basin. Transact. of Paleontological
Inst., vol. XX: 128 (in Russian).
9.
Ebersin A.G 1967.
The Pliocene Brackish Cardiidae of USSR . Transact. of Institute of Paleontology
Academy Sci. of USSR, vol.112, M.: 112 (in Russian).
10.
Imnadze Z.A. 1974.
The stages of development of ostracods in Pliocene deposits of Western Georgia. The
Materials on Geology and Gas-Oil- bearing of Georgia, vol.152, “Metsniereba”: 126-132 (in Russian).
11.
Maissuradze L.S. 1988.
Foraminifers of the Meotian deposits of Western Georgia. “Metsniereba” Publ. H.,
Tbilisi: 107 (in Russian).
12.
Maissuradze L., Koiava K. 2011.
Biodiversity of Sarmatian foraminifers of the Eastern Paratethys. Bulletin
Georgian National Academy of Sciences, vol.5 №1. P.143-150 (in Russian).
13.
Nevesskaya L.A., Goncharova I.A., Ilijna L.B., Paramonova N.P., Khondkarian S.O. 2003.
The
stratigraphical scheme of the Neogene of Eastern Paratethys.In Stratigraphy. Geological correlation, Vol.
11,
#2, Moscow: 3-26 (in Russian).
14.
Popkhadze L. I. 1978.
The microfacies of Meotian deposits of Western Georgia (foraminifers and
ostracods).
The theses of dissertation. Tbilisi: 26 (in Russian).
15.
Shatilova I.,Mchedlishvili N., Rukhadze L., Kvavadze E. 2011.
The history of flora and vegetation of
Georgia.Tbilisi: 199.
16.
Shchekina N.A. 1979.
The history of flora and vegetation of south of European part of USSR. “Naukova
Dumka” Pub. H. Kiev: 197 (in Russian).
17.
Shengelia F.K. 1976.
About the new locality of deposits of Eupatorian horizon in Western Georgia. Report
of Georgian Acad. Sci., vol.81, #3, Tbilisi: 733-736 (in Russian).
18.
Suladze A. 1984.
The Eupatorian horizon and the ecosystemic analysis of the basin of sedimentation
(after
materials from the Western Crimea). “Metsniereba” Publ.H., Tbilisi: 97 (in Russian).
19.
Taktakishvili I.G.
On the Eupatotian horizon of the Black Sea-Caspian Basin.” Metsniereba” Publ. H., Tbilisi:
135 (in Russian).
20.
Taktakishvili I.G. 1984.
The biostratigraphy of the Pliocene of the Western Georgia. Metsniereba” Publ.
H., Tbilisi: 50 (in Russian).
21.
Vekua M.L. 1979.
On the fauna of ostracods from the Eupatorian horizon. Abstracts of XXII Conference
of the Institute of Paleobiology Georgian Academy of Sciences. “Metsniereba” Publ. H., Tbilisi: 9-11 (in
Russian).
