GeolCarp_Vol68_No5_419

GEOLOGICA CARPATHICA

, OCTOBER 2017, 68, 5, 419–444

doi: 10.1515/geoca-2017-0028

www.geologicacarpathica.com

Foraminiferal, ostracod, and calcareous nannofossil

biostratigraphy of the latest Badenian – Sarmatian interval

(Middle Miocene, Paratethys) from Poland,

Romania and the Republic of Moldova

SIMINA DUMITRIŢA DUMITRIU

, SERGIU LOGHIN

, ZOFIA DUBICKA

, MIHAELA CARMEN

MELINTE-DOBRINESCU

, JOLANTA PARUCH-KULCZYCKA

and VIOREL IONESI

Alexandru Ioan Cuza University of Iasi, Department of Geology, Carol I Blvd., 20A, RO-700505 Iaşi, Romania; siminadumitriu@gmail.com

University of Warsaw, Faculty of Geology, Al. Żwirki i Wigury 93, PL 02-089 Warsaw, Poland

National Institute of Marine Geology and Geo-Ecology (GeoEcoMar), 23–25 Dimitrie Onciul Street, RO-024053 Bucharest, Romania

Polish Geological Institute – National Research Institute, Rakowiecka 4, PL 00–975 Warsaw, Poland

(Manuscript received October 10, 2016; accepted in revised form June 9, 2017)

Abstract: This study presents detailed foraminiferal, ostracod, and calcareous nannofossil analyses of five Middle

Miocene sections located in the Central Paratethyan realm, namely in Poland, Romania and the Republic of Moldova.

Based on foraminiferal distribution, five biostratigraphically important assemblages (labelled A–E) are distinguished.

Foraminifera data combined with ostracoda and nannofossil evidence allowed correlation between the studied sections,

and a comparison with the deposits of similar age from the Transylvanian, Vienna and Pannonian basins, as well as with

the Transcarpathian regions. The micropaleontological record across the Badenian–Sarmatian boundary interval is also

presented.

Keywords: Central Paratethys, Badenian–Sarmatian boundary, Carpathian Foredeep, foraminifera, ostracoda, calcareous

nannofossils.

Introduction

During the Middle Miocene the studied areas from Poland,

Romania and the Republic of Moldova were covered by the

Paratethys Sea, which was formed in the Early Oligocene as

a result of the collision between the African–Arabian Plate and

Eurasian Plate related to the Alpine tectonics (Seneš 1988;

Steininger & Rögl 1985

;

Pisera 1996). From the Oligocene,

this gigantic inland sea was periodically connected with the

Mediterranean and the Indo–Pacific Ocean (Rögl & Steininger

1984; Paramonova 1995; Rögl 1998, 1999; Iljina 2000; Kováč

2000; Popov et al. 2004, 2005; Nevesskaja et al. 2006;

Harzhauser & Piller 2007; Harzhauser et al. 2007). The Para-

tethys intercontinental domain with its specific paleobio-

geography, hydrological regimes and sedimentation dynamics

(e.g., Báldi 1980; Popov et al. 2004) is subdivided into the

Central Paratethys (Alpine–Carpathian) and the Eastern Para-

tethys (Euxinian–Caspian). The Badenian and Sarmatian sedi-

ments of those two basins were studied separately, leading to

differences in chronostratigraphic subdivision (for a synthesis,

see Piller et al. 2007). The Sarmatian deposits of the Central

Paratethys exposed in many countries such as Austria, Czech

Republic (Moravia), Hungary, Slovakia, Romania (regions

from extra and intra Carpathian area), northern part of the

Republic of Moldova, and Poland are assigned to the Sarma-

tian sensu stricto (Suess 1866), while the Eastern Paratethys

deposits of the same age are mainly exposed in Romania

(regions from extra Carpathian area), southern Republic of

Moldova, Ukraine, Georgia and Bulgaria, and are attributed to

the Sarmatian sensu lato (Barbot de Marny 1866) (see Grad-

stein et al. 2012). The Sarmatian sensu lato was subdivided

into Volhynian, Bessarabian and Chersonian substages

(Andrusov 1899; Simionescu 1903) corresponding to the

lower, middle and upper Sarmatian respectively. Additionally,

the lower part of the Sarmatian of the Moldavian Platform (NE

Romania) is assigned to the Buglovian substage, sensu

Laskarew 1903 (Ionesi 1968, 1991; Paghida Trelea 1969;

Ionesi & Guevarra 1993; Brânzilă 1999; Ionesi 2006). The term

Buglovian derives from the “Buglovka Beds” from Ukraine,

where Laskarew (1903) remarked for the first time that the sedi-

ments are characterized by the presence of intermediare fauna,

between the Badenian normal marine fauna and the brackish

Sarmatian one. The stratigraphic position of this substage has

been discussed for a very long time and many contradictory

opinions have appeared, for example that it was part of the

latest Badenian (Vyalov & Grishkevich 1965) or a first sub-

stage of the Sarmatian (Atanasiu 1945; Ionesi 1968; Paghida

Trelea 1969; Brânzilă 1999; Ionesi et al. 2005; Ionesi 2006).

Microfossils, namely foraminifera, ostracoda, calcareous

nannoplankton, and dinoflagellates are very important strati-

graphically, hence, they are commonly studied in the whole

Paratethys. The first foraminiferal zonations were established

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GEOLOGICA CARPATHICA

, 2017, 68, 5, 419–444

by Grill (1941) and Papp (1956), for the Central Paratethys

(Vienna Basin) and by Venglinsky (1958) for the Eastern

Paratethys. The last author distinguished some foraminiferal

zones that were correlated with the mollusc zones for several

Transcarpathian areas. Numerous foraminiferal studies have

been carried out up to now, to accurately assign the sediment

age (Subbotina et al. 1960; Łuczkowska 1964; Ionesi 1968;

Jiříček 1972; Boda 1974; Brestenská 1974; Venglinsky 1975;

Darakchieva 1989; Görög 1992; Popescu 1995; Koiava 2006;

Filipescu & Silye 2008). In general, these studies have been

realized for distinct regions of the Paratethys Basin; hence,

different microfossil zonations were published, not allowing

or hampering the correlation of Middle Miocene or Sarmatian,

deposits at the scale of the whole Paratethyan basin. The fora-

miniferal zonation for the Polish part of the Carpathian

Foredeep, comprising most of the Sarmatian s.s. units, was

published by Łuczkowska (1964). This zonation was commonly

referred and/or slightly modified in further studies by

Odrzywolska-Bieńkowa (1966, 1972), Czepiec (1996),

Olszewska (1999), Szczechura (2000), Gąsiewicz et al. (2004),

Garecka & Olszewska (2011), and Paruch-Kulczycka (2015).

The foraminiferal zonation of the Moldavian Platform (strata

exposed in NE Romania and the Republic of Moldova) for the

Sarmatian s.l. sediments was defined by Ionesi (1968, 1991)

and Bobrinskaya (1981, 1986, 2014).

The ostracod biostratigraphy of the Sarmatian Paratethyan

deposits, especially from the Eastern Paratethys received con-

siderably less attention than the foraminiferal biostratigraphy.

Some papers presenting the stratigraphic utility and/or

ostracod zonation of the Middle Miocene of the Central

Paratethys were published (Jiříček 1983; Zelenka 1990; Jiříček

& Říha 1991; Ionesi & Chintăuan 1994; Gross 2006; Tóth

2008, Filipescu 1996; Filipescu et al. 1999, 2014; ter Borgh et

al. 2014; Miclăuş et al. 2015). Additionally, some published

papers about ostracods also focus on the paleoenvironment

and taxonomy (Szczechura

2000; Aiello & Szczechura 2004;

Filipescu 1996; Filipescu et al. 1999, 2005, 2014; ter Borgh et

al. 2014; Loghin 2014).

Unfortunately, apart from Ionesi and

Chintăuan (1974, 1975, 1978, 1994), who presented the ostracod

zonation of the Moldavian Platform, only a few ostracod

studies of this region are available (Radu & Stoica 2005).

Calcareous nannofossils, which are extremely important for

correlating the Paratethys with the Mediterranean realms,

were studied in Poland by Krzywiec et al. (2008), Lelek et al.

(2010), and Garecka & Olszewska (2011) and in Romania

(Moldavian Platform) by Mărunţeanu (in Brânzilă &

Mărunţeanu 2001), and Chira (in Brânzilă & Chira 2005).

The aim of this paper is to produce an integrated biostrati-

graphical work, by combining the detailed foraminiferal and

ostracod studies from five sections of Poland, Romania and

the Republic of Moldova, and nannofossil analyses of two

lower Sarmatian successions from Romania and the Republic

of Moldova. Note that the calcareous nannofossils from the

Polish sections were previously published, as mentioned

above. This kind of approach will fill in a gap of knowledge,

since so far the correlation of the Badenian and Sarmatian

strata of these regions of the Paratethys Basin has been based

only on the published data (see Ionesi 1968; Paghida Trelea

1969). A revision of the Miocene ostracod collection, mostly

the stratigraphically important species, of Ionesi & Chintăuan

(1994), from the Paleontological Collections of the Museum

of “Alexandru Ioan Cuza” University (Iaşi, Romania), was

also done.

Geological setting

The studied deposits of SE Poland and NW Romania belong

to the Carpathian Foredeep, which was developed as a typical

peripheral foreland basin related to the Carpathian frontal

movement (Oszczypko & Oszczypko-Clowes 2012), resulting

from the flexural subsidence of a craton under an orogenic belt

(DeCelles & Gilles 1996) (Fig. 1A). In turn, the investigated

sediments from the Republic of Moldova belong to the back-

bulge depozone of the foreland system basin of the Eastern

Carpathians (Grasu et al. 2002).

The Polish successions are placed in the central part of the

Polish Carpathian Foredeep Basin which is about 300 km long

and up to 100 km wide. The basin is subdivided into external

and internal parts which are situated at the front of the

Carpathians and below the Carpathians flysch nappes respec-

tively (Ney 1968; Oszczypko 1999). To the west, the Car-

pathian Foredeep of Poland links up, by the Moravian Gate,

with the Moravian part of the Carpathian Foredeep, Slovakia

and Vienna basins, whereas to the SE it continues into the

Ukrainian, Republic of Moldova and Romanian foreland

basins (Oszczypko 1999). During the Miocene, the depocentre

was moving southeastward, resulting in late sedimentation in

the southeastern area which lasted until the latest Sarmatian

(Oszczypko 1999). The Polish Carpathian Foredeep Basin is

filled up with Middle Miocene (Badenian and Sarmatian)

marine deposits, which range from a few hundred metres thick

in the northern — marginal part, up to 3000 m in the south-

eastern — more central part (Ney et al. 1974; Oszczypko &

Oszczypko-Clowes 2012). Deposits which belong to the

Machów Formation include “Pecten beds”, “Syndesmya

beds” and “Krakowiec Clays” (Alexandrowicz et al. 1982;

Oszczypko 1996). The “Pecten beds” have been dated as

upper Badenian (Kosovian) by Odrzywolska-Bieńkowa

(1966) based on microfaunal assemblages of Hanzawaia

crassiseptata (Łuczkowska 1964). The

Ar/

Ar age determi-

nation placed the Badenian/Sarmatian boundary at the base of

the “Syndesmya beds” (Śliwiński et al. 2012). Based on the

micropaleontological analyses, the Krakowiec Clays have

been assigned by Odrzywolska-Bieńkowa (1972) and

Łuczkowska (1972) to the early Sarmatian age. Additionally,

Anomalinoides dividens and Elphidium hauerinum zones were

recently confirmed (Olszewska 1999; Krzywiec et al. 2008;

Lelek et al. 2010). This age is also confirmed by more recent

studies carried out on calcareous nannofossils by Peryt (1997)

and Garecka & Olszewska (2011), which distinguished in the

“Krakowiec Clays” the upper part of the NN6 biozone (early

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, 2017, 68, 5, 419–444

100 km

Budapest

Vienna

Austria

Bratislava

Slovakia

Apuseni Mts.

⁰

Soroca

B l i

Chișinău

Rezina

Nistru

Răut

Racov

Ciuhur

Iași

Moldova

Siret

Suce

ava

Sir

Jijia

Bașeu

Bahlu

Jijia

Prut

Costești

Botoșani

Ukraine

Hungary

Serbia

Bulgaria

Black Sea

Bucharest

Cluj-Napoca

Rep. of

Mold a

Chișinău

Paleozoic and Mezozoic

formations

Lower Sarmatian
Badenian

Middle Sarmatian

Upper Sarmatian

Quaternary

Ukraine

Sir

50 km

Ukraine

Hungary

Serbia

Rădău i

Iaşi

Poland

Romania

Bucharest

⁰

rpa

thia

Romania

Rep.

Moldova

Dornești

Studied sections

Romania

Magura

Krakow

Lviv

Suceava

Orhei

Inner

Eastern Carpathians

Iași

Chișinău

Rep.

Mold a

Cze

Rep

ubli

Katowice

Krakow

C a r p a t h i a n s

C a r p a t h i a n F o r e d e e p

Ukraine

Holy

Cros

s Mo

untain

Vistula

The extent of Miocene deposits

Kielce

San

Przemysl

Rzeszow

50 km

Vistula

Warta

Odra

Warsaw

Slovakia

Ukraine

Czech Republic

Germany

Belarus

Lithuania

Baltic sea

San

Poland

⁰

State border

sections

tudied

Northern boundary of the

Carpathian overthrust

Jamnica M 83

Machów

Moldavian Platform

Transylvanian

Basin

Southern

Carpath.

Pannonian

Basin

Vienna

Basin

Sarmatian s.s. in age, Harzhauser & Piller

2007) and the NN7 biozone (covering the late

Sarmatian s.s.

—

early Pannonian in age,

according to Harzhauser & Piller 2007).

The studied sediments from Romania and

the Republic of Moldova (FH

Rădăuţi core,

Dorneşti and Costeşti outcrops) belong to the

Moldavian Platform (Ionesi & Ionesi 1968;

Ionesi 1968; Ionesi 1994; Ionesi et al. 2005).

These deposits, situated in the external part of

the Eastern Carpathians, are attributed to the

last marine accumulation cycle of the

Moldavian Platform (Ionesi 1994) and are

characterized by a significant increase in

thickness of the Volhynian deposits with the

approach of the Carpathian Orogen. The

thickness of these deposits is around 500

metres between the Moldova and Siret rivers

and reaches up to 800 metres in the front of the

Carpathian Orogen (Ionesi 1968; Ionesi 1994).

Ionesi & Ionesi (1968) dated these deposits

as Volhynian based on the macrofossil associa-

tion, including Inaequicostata inopinata

(Grischevich) and Obsoletiforma

lithopodolica

(Dubois), and the foraminiferal association,

with Cycloforina karreri ovata, Cycloforina

karreri karreri, Elphidiella serena and

Elphidium reginum among the foraminifers.

The Early Sarmatian age of these deposits has

also been confirmed by the other foraminiferal

studies (Ionesi 1968, 1991; Ionesi & Guevarra

1993). The studied sediments from the

Republic of Moldova section are part of the

lithostratigraphic units known as the

“Darabani–Mitoc Clays” (Ionesi & Ionesi

1981) and “Stânca Limestone” (Simionescu

1902). The Volhynian age of these sediments

was first assigned by Simionescu (1902), and

has been confirmed by more recent paleonto-

logical studies (Paghida Trelea 1969; Ionesi &

Ionesi 1981, 1982; Brânzilă 1999).

Materials and methods

The material analysed here comes from 3

outcrops and 2 drilling cores from Poland,

Romania and the Republic of Moldova. The

investigated sections from Poland are the his-

torical Machów sulphur mine (N 50°31’59.60”

E 21°39’43.47”) and Jamnica M-83 core

(N 50°36’40.18” E 21°58’15.50”) which are

situated in SE Poland (Fig. 1B) while the

Romanian sections, FH

Rădăuţi core

(N 47°49’32.34” E 25°54’27.54”) and Dorneşti

outcrop (N 47°52’52.1” E 25°52’3.4”), are

Fig. 1. Geological map of the studied areas. A — Simplified geological sketch map of

the Carpathian Foredeep and Carpathian Orogen (modified after Pawlewicz 2006;

Kováč et al. 2003); B — location of the studied Polish sections (Machów and Jamnica

M-83 core) in Poland and the extension of the Sarmatian deposits in the extra- Carpathian

area from Poland (modified after Ney et al. 1974; Paruch-Kulczycka 2015); C — loca-

tion of the studied Romanian (FH

Rădăuți and Dornești) and the Republic of

Moldova (Costești) sections and the simplified geological sketch map of the north-

eastern Romania and northern Republic of Moldova area (modified after Geological

maps of Romania and the Republic of Moldova, scale 1:200,000).

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DUMITRIU, LOGHIN, DUBICKA, MELINTE-DOBRINESCU, PARUCH-KULCZYCKA and IONESI

GEOLOGICA CARPATHICA

, 2017, 68, 5, 419–444

loca ted in NE Romania (Fig. 1C). The studied section from the

Republic of Moldova (N 47°51’27.5” E 27°14’56”) is situated

on the left side of the Prut River, near the Stânca–Costeşti

Lake (Fig. 1C).

The lower part of the Machów section is represented by

clays with intercalations of marls. Following the succession,

the sediments continue with sandstones followed by clays

with mudstone intercalations. In the Jamnica core the litho-

logy is very similar to the Machów section excluding the sand-

stones. The sediments of the FH

Rădăuţi core and Dorneşti

outcrop are mostly composed of ashy-grey clays partially

compacted and/or laminated with some fine intercalations of

sand, sandstones and coal films. Lithologically, the succession

analysed from Republic of Moldova contains ashy-grey clays

and can be compacted or laminated. Some fine intercalations

of sand may also be encountered.

In total 128 samples have been analysed for foraminiferal

and ostracod studies: 34 samples from Machów sulphur mine

(Poland), 18 from the Jamnica M-83 core (Poland), 29 from

the FH

Rădăuţi core (Romania), 26 from Dornești outcrops

(Romania) and 21 samples from the Costești outcrop (Republic

of Moldova). We also revised the Miocene ostracod collection,

mostly the stratigraphically important species, of Ionesi &

Chintăuan, from the Paleontological Collections of the

Museum of “Alexandru Ioan Cuza” University of Iaşi,

Romania; the aforementioned collection was used for the

ostracod biozonation of the Moldavian Platform (Ionesi 1991;

Ionesi & Chintăuan 1994). The calcareous nannoplankton

analyses were done on the FH

Rădăuţi core, as well as the

Dorneşti and Costeşti sections.

For the foraminiferal and ostracod analyses, the weight of

each sample was approximately 200 g. The samples were

washed using the decantation method. We analysed the entire

material. The samples were sieved through 3 sieves to produce

4 fractions. Accordingly, the material > 0.466; > 0.236; > 0.122

and < 0.122, including the material < 0.063 have been ana-

lysed. The foraminiferal specimens were handpicked using

a binocular stereo microscope Carl Zeiss Jena SM XX and

Nikon SMZ 800. SEM images of foraminifera and ostracoda

were taken using a Merlin Gemini II microscope (in the

Microcosmos laboratory of the Geological Institute of

Romania) and a Vega/Tescan SEM microscope (in the Polish

Academy of Science and Faculty of Biology of the “Alexandru

Ioan Cuza” University of Iaşi, Romania). The investigated

material from Romania (FH

Rădăuţi core and Dorneşti

outcrop) and the Republic of Moldova (Costeşti outcrop) is

depo sited in the Paleontological Collection of the Museum of

“Alexandru Ioan Cuza” University of Iași, Romania. The

mate rial from Poland (Machów sulphur mine and Jamnica

M-83 core) is hosted in the Polish Geological Institute–

National Research Institute, Warsaw, Poland.

The calcareous nannofossils were investigated in the

fraction of 2–30 μm separated by decantation method using

7 % of H

. From the obtained material, smear-slides were

mounted by Canada balsam and analysed at 1200× magnifi-

cation, using an oil-immersion objective on an Olympus

transmitting light microscope, both in transmitted and pola-

rized light.

All identified foraminifera, ostracoda, and calcareous

nanno fossil species are listed within the Appendix.

Results

In total, 131 species of foraminifera, 53 species of ostracoda,

and 16 species of calcareous nannofossils were identified in

the analysed samples. In general, the microfossils are well pre-

served and abundant (usually more than one hundred fora-

miniferal specimens per sample).

Foraminifers

In all 5 sections 108 species of calcareous benthic foramini-

fera and 13 species of plankonic foraminifera were identified.

The most abundant benthic taxa belong to Miliolida (the fol-

lowing genera are Affinetrina, Articularia, Articulina, Cyclo

forina, Miliolinella, Nodobaculariella, Pseudo

triloculina,

Varidentella, Sigmoilinita, Triloculina, Quinqueloculina);

elphidiids (Elphidium, Cribroelphidium, Porosononion),

anomalinids (Anomalinoides, Heterolepa, Hanzawaia), cibici-

dids (Cibicides, Lobatula), nonioniids (Elphidiella, Melonis,

Nonion, Pullenia), bolivinids (Bolivina, Fursenkoina), bulimi-

nids (Bulimina), uvigerinids (Uvigerina), textularinids (Semi

vulvulina), sphaeroidinds (Sphaeroidina), within Rotaliida

and Lagenida (Glandulina, Favulina, Fissurina, Hylinonetrion,

Lagena) (supra-ordinal classification follows Pawlowski et al.

2013). Some agglutinated taxa (10 species), such as Nothia,

Haplophragmoides, Reticulophragmium and Textularia spe-

cies have been also recorded.

Machów

A total of 78 species of both benthic and planktonic

foraminifera were identified in the Machów section. In the

lowermost part of the section, comprising the interval 75–67 m

in depth, there is an abundant occurrence of the species

Sigmoilinita tenuis, Hanzawaia crassiseptata, Globigerina

bulloides which are accompanied by Globigerina praebulloi

des, G. concinna, Sphaeroidina bulloides, Pullenia bulloides,

Heterolepa dutmeplei, Bulimina aculeata, Bolivina dilatata

and Melonis pompiloides (Fig. 2). The interval 67–56.5 m in

depth is dominated by the species Anomalinoides dividens

(≈ 2000 specimens in all samples). Additionally, some miliolid

species (in relatively smaller number — 142 specimens) were

recorded at this level including Cycloforina fluviata,

Pseudotriloculina consobrina, Quinqueloculina akneriana,

Q. akneriana argunica, Varidentella rosea and V. reussi.

Following the section upwards, the interval 56–45m in depth

is marked by the disappearance of the species Anomalinoides

dividens and by the occurrence of the species Cycloforina kar

reri ovata in samples 15 and 16. Other species of miliolids,

elphidiids and lagenids progressively appear in a larger

423

THE BIOSTRATIGRAPHY OF THE LATEST BADENIAN–SARMATIAN, CENTRAL PARATETHYS

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, 2017, 68, 5, 419–444

ali

es d

ivi

den

V aridentella

reussi

V aridentella sarmatic

V aridentella

rotunda

Q. akneriana argunica

Pse

udo

tril

ocu

lin

aco

nso

brin

P . consobrina niten

Qui

nqu

elo

cul

ina

akn

eri

ana

Lobatula lobatula

Sigmoilinita tenuis

Art

icu

lar

ia a

rti

cul

ino

ide

Bolivina dilatata

Articularia karreriella

Heterolepa dutemplei

Elphidium macellum

Elphidium aculeatum

Elphidium joukovi

Elphidium hauerinum

Elphidiella serena

Nonion bogdanowiczi

V . pseudocostata

Cyc

lof

ori

na p

r ed

car

pat

ica

C. karreri karr

eri

C. karreri ovata

Bulimina aculeata

Melonis pompiloides

Fissurina cubanica

Fissurina isa

Globigerina bulloides

G. praebulloides

Globigerinaconcinna

Elphidium reginum

Q. m

ako

e ukr

ain

ica

Sphaeroidina bulloides

Pullenia bulloides

B. moldavica

Biostratigraphy

(Łuczkowsk

1964

)

1971

oraminiferal

zonatio

Ostraco

zonatio

(Jiricek

Riha

991

)

Ano

mal

ino

ide

divi

den

Cycloforina

karreri ovata

V aridentella

sarmatica

Lith

ost

rat

igr

aph

. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .

Depth (m)

Lithology

Samples

16 15 14 13

10 9 8 7

6 5 4 3 2 1

Mach

Poland

E. fitchelianum

Cribroelhidium excavatum

C. poeyanum

Elphidium crispum

Por

oso

non

ion s

ubg

ran

osu

Porosononion martkobi

C. fluviata

Bolivina sarmatica

Bolivinadir

ecta

B.nisporenica

B. elongata elongata

Dogielina sarmatica

Aurila mehesi

A notata

A merita

A sp

. 1 juvenile

Hemicytherura videns

Leptocythere foveolata

L naviculata

Leptocythere sp.

Eux

ino

cyt

her

rae

bos

que

Cal

list

ocy

the

r e c

ana

lic

ula

C egregia

C incostata

C maculata

C postvallata

C sp. 1

juvenile

C sp. 2

Cne

sto

cyt

her

e lam

elli

cos

Cytherois sarmatic

Argiloecia subtilis

Argiloecia sp.

F ab

a efo

r m

i sc

a nd

o na

p ok

o rn

y i

L ox

o co

n ch

a m ini

m a

L rhomboidea .

Loxocorniculum hastatum

Xestoleberis fuscata

X dispar

X tumida

Hen

ryh

ell

a a

spe

rim

Polycope

orbicularis

cf.

Phl

yct

ocy

the

re p

ell

uci

x x

31 30 29

Paratethys

stages

NEOGENE

SERRA V

IAN

MIOCENE

nan

no.

zon

ati

are

a &

Ols

zew

ska 2

011

)

Badenian

Sarmatian

sensu stricto

Sarmatian

sensu lato

V olhynian

Centra

Easter

Foraminiferal

Assemblages

Foraminifera

Ostracoda

H. crassiseptata/

V elapertina

indigena

Elphidium

hauerinum

P . subranosum,,

”

Bessarabian

Late

early Sarmatian

Machów Formation

sta

nda

chr

on.

rad

ste

et a

l. 2

012

)

Chronostratigraphy

Clays

. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .

udstone

Sandstone

Marls

Limestone

NO 1

C. h

ung

aric

A. m

ehe

NO 12

Neocyprideis (N.) kollmanni

Aurila notata

Hansenisca soldanii

Hanzawaia crassiseptata

Badenian

Fig. 2.

Foraminifera and ostracoda distribution in the Machów section.

424

DUMITRIU, LOGHIN, DUBICKA, MELINTE-DOBRINESCU, PARUCH-KULCZYCKA and IONESI

GEOLOGICA CARPATHICA

, 2017, 68, 5, 419–444

number and their diversity increases within the succession, for

example, Articularia articulinoides, A. karreriella, Cycloforina

predcarpatica, C. karreri karreri, Miliolinella selene, M. sub

rotunda, Varidentella sarmatica, V. rotunda, V. pseudocostata,

V. latecunata, Quinqueloculina minakovae ukrainica, Q. per

elegantissima, Affinetrina cubanica, Elphidium hauerinum,

E. aculeatum, E. macellum, E. reginum, E. joukovi, Elphidiella

serena, Porosononion subgranosus, Fissurina isa, F. cubanica

and F. toga (Fig. 2).

In the interval 43–5 metres in depth, the ribbed milliolids

are totally absent and only miliolids with a fine test are still

present (Varidentella reussi). Elphidiids and nonionids appear

in a large number and are represented by such species as

Elphidium hauerinum, E. fitchelianum, E. excavatum,

E. crispum, E. macellum, Porosononion sub granosus, P. mart

kobi, Cribroelphidium poeyanum Elphidiella serena and

Nonion bogdanowiczi.

The top of the Machów section (samples 28–34) is domi-

nated by the presence of species belonging to the genus

Bolivina, such as Bolivina directa, B. moldavica, B. nispore

nica, B. sarmatica. Ammonia beccarii and Cassidulina sp. are

also quite common here. Moreover, a small number of plank-

tonic Globigerina bulloides have been identified in most of

the samples from this interval (Fig. 2).

Jamnica M83 core

In the Jamnica M-83 core succession, 93 species of benthic

and planktonic foraminifera were recorded. The lowermost

interval, 235–225 m in depth (Fig. 3), is characterized by the

abundant occurrence of Globigerina bulloides, G. prae

bulloides, Velapertina indigena, Heterolepa dutemplei,

Bulimina elongata elongata, Favulina hexagona and

Sigmoilinita tenuis. The sample 16 yielded a large number

(50 specimens) of agglutinated species belonging to the genus

Nothia, Rhizammina, Reticulophragmium, Reophax,

Haplophragmoides, Cyclamina, Budashevaella, as well as

representatives of the genus Uvigerina; the most common spe-

cies are Uvigerina semiornata, U. brunnensis. The next inter-

val, 220–214 m deep, is characterized by the occurrence of the

species Anomalinoides dividens (at 220 metres deep) and the

common appearance of fine test miliolids such as

Pseudotriloculina consobrina, Triloculina pseudoinflata,

Affinetrina ukrainica, Quinqueloculina akneriana, Q. akne

riana argunica, Cycloforina gracilis. Lobatula lobatula is

a common and important component of this assemblage. In the

overlaying strata (the interval 202–182 m in depth) the species

Anomalinoides dividens disappears and miliolid species such

as Cycloforina karreri ovata, C. karreri karreri,

Quinqueloculina minakovae ukrainica and Articularia karre

riella clearly dominate this interval. Some of the elphidiids

species (Elphidium hauerinum, E. macellum and Elphidiella

serena) additionally occur but in smaller numbers. The upper-

most part of the Jamnica core (the interval 180–35 m in depth)

is defined by an increase in diversity of the foraminiferal

species. In sample 7, bolivinids occur in large numbers, being

strongly represented by Bolivina moldavica and B. sarmatica.

Sample 2 is represented by the species Articularia articuli

noides, which is very abundant in this part of the section.

Apart from Articularia, the most abundant foraminifera of this

interval are miliolids represented by Varidentella reussi,

V. rotunda, Quinquloculina akneriana, Miliolinella subrotunda

and M. selene, along with some representatives of the genera

Nonion, Elphidium and Porosononion (Fig. 3).

Rădăuţi FH

core

The foraminiferal assemblages of the FH

Rădăuţi core

section are composed of 29 species, of which 2 are planktonic

ones. In sample 467, from the lower part of the section

(239 metres deep), foraminifera are rare; only some specimens

of planktonic species (Globigerina bulloides and Globorotalia

miocenica) were recorded. The upper part of the section, com-

prising the interval 200–180 m, is characterized by a high

number of foraminiferal species. Sample 470 yields a very

numerous and diversified range of foraminiferal species

including Elphidium reginum, E. macellum, Elphidiella serena,

Lobatula lobatula, Cycloforina cristata, C. predcarpatica,

Varidentella pseudocostata, V. rotunda, Quinqueloculina

akneriana, Q. akneriana argunica and Q. minakovae ukrai

nica. In the middle part of the section (175–80 m in depth) the

following species Elphidium reginum, E. macellum, E. reussi

and Ammonia beccarii are presented in large numbers, while

the uppermost part of the section (77–46 m in depth) is clearly

dominated by the presence of ribbed miliolids, such as

C. karreri ovata, C. karreri karreri, C. predcarpatica and

C. fluviata (Fig. 4).

Dorneşti section

In total, 36 species of foraminifera (4 species are plank-

tonic) have been identified in the samples collected from the

Dorneşti section. The assemblages from the lower part of the

succession (samples 164, 440, 2a, 163, 108, 146, 102, 2b) are

characterized by rotaliids such as Elphidium reginum, E. haue

rinum, E. macellum, E. subumbilicatum, Elphidiella serena

and Nonion bogdanowiczi (Fig. 5). The most abundant species

are E. reginum and L. lobatula in sample 440. In the upper part

of the profile (samples 109, 4b, 98, 4a, 96, 108, 95, 93, 94) the

occurrence of a large number of the ribbed miliolids including

Articularia karreriella, Cycloforina karreri ovata, C. karreri

karreri and C. predcarpatica has been recognized (Fig. 5).

Costeşti section

In the samples from the Costeşti outcrop, 16 species of

benthic foraminifera have been identified. Planktonic fora-

minifera are totally absent. The samples collected from the

lower part of the section (samples 491/A, 491/B, 491/C,

491/D, 491/G) yielded scarce foraminiferal association; only

a few specimens of miliolid species, such as Pseudotriloculina

consobrina, P. consobrina nitens, Articulina problema,

425

THE BIOSTRATIGRAPHY OF THE LATEST BADENIAN–SARMATIAN, CENTRAL PARATETHYS

GEOLOGICA CARPATHICA

, 2017, 68, 5, 419–444

V aridentella r

eussi

V aridentella sarmatica

V aridentella r

otunda

Q. akneriana argunica

Pseudotriloculina consobrina

Quinqueloculina akneriana

Articularia articulinoides

Articulina problema

Articularia karreriella

Heterolepa dutemplei

Elphidium aculeatum

Elphidium joukovi

Elphidium hauerinum

Elphidiella serena

Nonion bogdanowiczi

Cycloforina predcarpatica

C. karreri karr

eri

C. karreri ovata

Melonis pompiloides

Fissurina cubanica

Fissurina isa

Globigerina bulloides

Globigerina praebulloides

Q.minakovae ukrainica

Anomalininoides dividens

Lobatula lobatula

Elphidium macellum

Sinuloculina mayeriana

Bolivina sarmatica

Affinetrina cubanica

Affinetrina ukrainica

Triloculina pseudoinflata

Globigerinoides bisphaerica

Porosononion subgranosus

Porosononion martkobi

Bolivina moldavica

Bolivina dilatata

Bolivina antiqua

Bulimina elongata elongata

Sigmoilinita tenuis

Globigerinoides trilobus

Aurila mehesi

Leptocythere cejcenensis

Callistocythere incostata

Callistocythere postvallata

Cnestocythere cf. truncata

Cnestocythere sp.

Cytherois sarmatica

Loxoconcha curiosa

Loxocorniculum hastatum

Xestoleberis dispar

Xestoleberis tumida

Xestoleberis sp.

Henryhowella asperima

Plyctocythere pellucida

Cytheropter

on vespertilio

Cytheropter

on sp.

Kirthe sp.

Eocytheropter

on inflatum

Semicytherura filicata

V erucocyther

eis sp.

x x

100

125

150

175

200

225

Depth (m)

Lithology

Samples

Jamnica

M-83 Poland

11 12

13 14

Biostratigraphy

Ostr

aco

d zon

atio

Lith

ost

rat

igr

aph

Paratethys

stages

NEOGENE

MIOCENE

nan

no.

zon

atio

are

cka

lsz

ska

201

Sarmatian

sensu stricto

Sarmatian

sensu lato

V olhynian

Centra

Easter

(Ł

ucz

kow

ska

196

)

, 197

For

ini

fer

zon

atio

ividen

ycloforina

karr

ovata

aridentell

sarmatica

Elphidium

hauerinum

Machów Formation

sta

nda

rd c

hro

rad

ste

et a

l. 2

012

)

SERRA V

IAN

Badenian

Chronostratigraphy

Foraminifera

Ostracoda

ForaminiferalAssemblages

. . . . . . . . . . . . . . . . . . . . . . . .

Clays

Sandstones

Limestones

Marls

NO 11

C. hungarica

A. mehesi

(Jir

ice

k & Rih

)

199

Bade

nian

Uvigerina brunnensis

Uvigerina semiornata

crassiseptata/

indigena

Mudstone

Sarmatian

arly

Articularia articulinoides and Quinqueloculina akneriana

have been found. In the overlying strata, an increase in diver-

sity and number of the fora-

miniferal species is noti ce able.

The assemblages of the sam-

ples 491/1, 491/2, 491/3 are

clearly dominated by the

pre sence of numerous repre-

sentatives of species A. arti

culi

noides, P. consobrina,

P. consobrina nitens and

A. problema, while the assem-

blages of the samples 491/4

and 491/5 display a decrease

in abundance in the number of

the miliolids and a bloom of

the species Porosononion

subgranosus and P. martkobi.

Additionally, some lagenids

including Fissurina cubanica,

F. isa, F. mironovi, appear in

some samples (491/1, 491/2,

491/3, 491/4, 491/5, 491/7

and 496) (Fig. 6).

Ostracods

In all the analysed sections

53 species were identified. In

general, ostracods are less

frequent than foraminifera in

all studied samples. The most

abundant taxa belong to the

family Leptocytheridae, which

includes the genera Lepto

cythere and Callisto cythere,

encountered in all the ana-

lysed sections, followed by

the species of the Aurila genus.

Additionally, the species

Cytherois sarmatica occurs in

a great number of specimens

in the analysed samples.

In the Machów section, we

identified 30 ostracod species

(Fig. 2). In the lowermost part

of the section, (samples 1, 2),

only one species, Henry

howella asperrima, occurs.

Slightly further up, within the

interval 67–55 m in depth, the

ostracod assemblages are

dominated by the presence of

the species Callistocythere

canaliculata, C. incostata,

Cytherois sarmatica and

Aurila mehesi. Beside these taxa, the species Polycope orbicu

laris and Phlyctocythere pellucida are quite abundant in this

Fig. 3.

Foraminifera and ostracoda distribution in the Jamnica M-83 section.

426

DUMITRIU, LOGHIN, DUBICKA, MELINTE-DOBRINESCU, PARUCH-KULCZYCKA and IONESI

GEOLOGICA CARPATHICA

, 2017, 68, 5, 419–444

100

125

150

175

200

225

250

Depth (m)

Samples

Lithology

Articularia karr

eriella

Elphidium aculeatum

Elphidium hauerinum

C. karr

eri karr

eri

480

469

476

Lobatula lobatula

Elphidium macellum

n s

. . . . . . . . . . . . . . .

489

488

487

486

478

468

490

482

483

484
485
479

475

477

464

463

491

473

474

470

471

481

472

467

Nonion bogdanowiczi

Elphidiella ser

ena

Elphidium r

eginum

Elphidium r

eussi

lin

Q. akneriana ar

gunica

. m

e u

Cycloforina fluviata C. pr

edcarpatica

C. kar

erri ovata

aridentella r

otunda

. pseudocostata Ps

a c

. consobrina nitens Globigerina bulloides Gl

. . . . . . . . . . . . . . .

FH P

Rădău i

Romania

Aurila mehesi Aurila notata Senesia vadaszi L

e f

Amnicyther

e tenuis

re p

Euxinocyther

e sp.

C canaliculata

C gliwicensis

C egr

egia

C incostata

Callstocyther

e sp.

e t

C hungarica

Cyprideis pannonica H

s d

Cyther

ois sarmatica

Candona cf. sagitosa Loxoconcha minima Loxoconcha impr

essa

Loxocorniculum schmidi. Xestoleberis fuscata Bosquetina carinella

x x

Foraminifera

Cycloforina karr

eri ovata, C. fluviata,

“Lobatula lobatula

”

Biostratigraphy

is p

er Foram.

onation

(Ionesi

19 )

Litho-

stratigraphy

Bădeui-Spătăreşti Member

Lespezi Formation

. 2

Paratethys

stages

NEOGENE

MIOCENE

SERRA

ALLIAN

Sarmatian

sensu stricto

Sarmatian

sensu lato

olhynian

Chronostratigraphy

Central Eastern

Foraminiferal

Assemblages

Ostracoda

. . . . . . . .

Clays Sandstones Gravel

Coal

Ostracod

zonation

(Jiricek &

Riha 1991)

NO 1

Cytheridea hungarica

Aurila mehesi

early Sarmatian

. ..

. ... ... ... ... ... ... .. ... ... .. .. ... .. ..

. . . . . . . . . . . . . . . . . . . . .

355

360

365

370

375

380

. . . . .

. . . . . . . . .

. . . . . . . .

. . . .

Alt. (m)

Lithology

Samples

. . . . . . . . . . . . . . . . . .

. ..

. ... ... ... ... ... ... .. ... ... .. .. ... .. ..

. . . . . . . . . . . . . . . . . . . . .

. . . . . . . . . . . . . . . . . . . .

. ..

. ... ... ... ... ... ... .. ... ... .. .. ... .. ..

. . . . . . . . . . . . . . . . . . . . .

. . . . . . . . . . . . . . . . . . . .

. ... ... ... ... ... ... .. ... ... .. .. ... .. ..

. . . . . . . . . . . . . . . . . . . .

. . . . . . . . . . . . . . . . . . . . .

101

102
146
163

164

103

104

105

106

107

108

110

109

. . . . . . . . . . . . . . . . . . . .

. . . . . . . . . . . . . . . . . . . . .

165

137

. . . . . . . . . . . . . . . . . . . .

. . . . . . . . . . . . . . . . . . .

. . . .

. .

144

Bolivina moldavica

Bolivina sarmatica

. . . . . . . . . . . . . . . . . . . .

. . . . . . . . . . . . . . . . . . . . .

Q akneriana

a k

Cycloforina fluviata

C. pr

edcarpatica

C. karr

eri ovata

C. karr

eri karr

eri

. pseudocostata

P consobrina

440

Lobatula lobatula

Nonion boganowiczi P

subgranosus.

Elphidiella ser

ena

E. hauerinum

E. macellum

E. r

eginum

E. r

eussi

. s

lic

na b

Dornesti

Romania

Amnicyther

e tenuis

E praebosqueti

L hastatum

H omphalodes

x x

Cycloforina karr

eri ovata, C. fluviata,

“Lobatula lobatula”

Biostratigraphy

is p

er Foram.

Zonation

Ionesi

1991

Lithostratigraphy

Bădeui-Spătăreşti Member

Lespezi Formation

t a

)

Paratethys

stages

NEOGENE MIOCENE

SERRA

ALLIAN

Sarmatian

sensu stricto

Sarmatian

sensu lato

olhynian

Chronostratigraphy

Central Eastern

Ostracod

zonation

Foraminifera

Ostracoda

. . . . . . . .

Clays

Sandstones

Jiricek &
Riha 1991

NO 1

Cytheridea hungarica

Aurila mehesi

Soil

early Sarmatian

interval. In the upper part of the section, the ostracod

assemblages are scarce. The most common species is

Cytherois sarmatica, which ranges up to 34 metres in depth

(sample 24). The presence of the species Xestoleberis

dispar throughout almost the entire section (65–55 m) is also

noticed.

Fig. 5. Foraminifera and ostracoda distribution in the Dorneşti section.

Fig. 4. Foraminifera and ostracoda distribution in the FH

Rădăuţi section.

427

THE BIOSTRATIGRAPHY OF THE LATEST BADENIAN–SARMATIAN, CENTRAL PARATETHYS

GEOLOGICA CARPATHICA

, 2017, 68, 5, 419–444

The ostracod fauna from the Jamnica section is

represented by 20 species (Fig. 3). The lower-

most part of this core (samples 16 and 19) is

characterized by the presence of the species

Cnestocythere truncata, Henryhowella asper

rima, Cytheropteron vespertilio and, Semi

cytherura filicata. Higher up in the succession,

the most abundant species is Cytherois sarmatica

(recorded in the interval between 220–175 m in

depth), followed in abundance by Callistocythere

postvallata, C. incostata and Aurila mehesi.

In the upper part of the Jamnica section, only 2

ostracod species have been encountered,

Callistocythere postvallata and Xestoleberis

tumida (sample 2).

In the Rădăuți section, 20 ostracod species

were identified (Fig. 4). In the lower part of the

section (samples 470 and 474) the most frequent

species are Aurila mehesi, A. notata, Callisto

cythere canaliculata, C. egregia, C. incostata,

Cytheridea acuminata and Xestoleberis fuscata.

The upper part of the section (samples 482, 484

and 485) is characterized by the dominance of the

species Euxinocythere praebosqueti, Cyprideis

pannonica and Xestoleberis fuscata. The com-

mon taxa in the Rădăuți section also include the

species Loxoconcha minima. Towards the top of

the studied section (samples 486 and 489),

Cytheridea hungarica dominates the ostracod assemblage.

The Dornești section yielded 6 ostracod species which were

indentified in samples 440 and 146 from the lowermost part of

the outcrop. The most abundant species are Cytheridea

hungarica and Cyprideis pannonica (Fig. 5).

In the Costești section 5 ostracod species have been

recorded. The most frequent species are Callistocythere post

vallata and Loxocorniculum spp. (L. hastatum and L. schmidi)

(samples 495/D, 491/1, 491/4 and 491/5) (Fig. 6).

Calcareous nannofossils

Several samples (440 from Dorneşti, 470, 482 and 488 from

Rădăuţi and 491/4 and 495/D from Costeşti) were ana-

lysed for their calcareous nannofossil content. The greatest

abundance of the calcareous nannofossils was recognized in

the sample 440 that contains Discoaster kugleri, D. deflandrei,

Reticulofenestra pseudoumbilicus, Triquetrorhabdulus rugo

sus, R. minuta, R. minutula, Coccolithus pelagicus, Spheno

lithus moriformis, Calcidiscus leptoporus, Pontosphaera

multipora, Helicospahera carteri. Additionally, reworked

nannofossils (around 30 %) from the older Upper Cretaceous,

Paleogene and Lower Miocene sediments were recorded.

In sample 482, 80% of the assemblage represents reworked

specimens from the Upper Cretaceous and Paleogene depo-

sits; nevertheless, species that have a long distribution range,

including the Middle Miocene, such as Reticulofenestra

pseudoumbilicus, R. minuta, R. minutula, Coccolithus

pelagicus, Sphenolithus morifomis and Calcidiscus leptoporus

were identified. Sample 488 commonly contains taxa of the

genus Reticulofenestra, namely R. pseudoumbilicus, R. minuta,

R. minutula, along with C. pelagicus, S. moriformis,

Calcidiscus leptoporus, C. macintyrei, Discoaster musicus

and D. deflandrei. The samples FH

No. 470 and Costeşti

491/4 provided only reworked nannofossil specimens from the

Upper Cretaceous and Paleogene strata, while the sample

Costeşti 495/D was barren of nannofossils.

Biostratigraphy

Rich foraminiferal associations from the studied areas

(Poland, Romania and the Republic of Moldova), showing

similar trends of successive foraminiferal assemblages,

enabled the identification of five foraminiferal assemblages

(named A–E), which are stratigraphically important (Fig. 7).

Based on these assemblages we correlate the investigated sec-

tions and relate them to different local zonations distinguished

in different Paratethyan regions (Fig. 8). Morover, beside the

foraminiferal assemblages we also identified several strati-

graphically important ostracods. The selected foraminifera,

ostracoda as well as calcareous nannofossils are presented in

Figs. 9–14.

Assemblage A is characterized by the abundant occurrence

of Sigmoilinita tenuis (Fig. 9A), Globigerina bulloides

(Fig. 9B,C), G. praebulloides, G. concinna, Globigerinoides

491/10

491/11

491/9

491/8

491/7

491/6

491/5

491/4

491/3

491/2

496

495/G

495/F

495/E 495/D

495/C 495/B

lin

a c

491/1

P. c

a n

a s

a a

a p

a c

a i

495/A

Samples

ife

tra

tig

ito

ân

Darabani-Mitoc Clays

. . . .

. . .

132

130

125

120

115

Alt

(m)

Costeşti

Rep. Moldova

. r

eussi

Articulina sarmatica

rugosum?

consobrina
,

beccarii

standard c

hron.

(Gradstein et

. 2012)

Paratethys

stages

NEOGENE MIOCENE

SERRA

ALLIAN

Sarmatian

sensu stricto

Sarmatian

sensu lato

olhynian

Chronostratigraphy

tra

Foraminifera Ostracoda

a a

n m

m h

m s

lis

e p

e d

Clays

Silt

oil

Micritic

limestones

Serpulid

limestones

. . .

Sarmatian

arly

str

tio

Jir

NO 1

Cytheridea hungarica

Aurila mehesi

491/12

491/13

Fig. 6. Foraminifera and ostracoda distribution in the Costeşti section.

428

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early

Sarmatian

- the Assemblage is characterized by the common occurrence

of the

Velapertina indigena, Globigerina bulloides, G.

preabulloides, G. concinna, Globigerinoides triloba, G.

bisphaerica, Sigmoilinita tenuis, Bulimina elongata, elongata,

B. aculeata, Bolivina dilatata, Heterolepa dutemplei,

accompaniedby other species as

Sphaeroidina bulloides,

Pullenia bulloides, Melonis pompiloides, Hansenisca soldanii,

Uvigerina brunnesis, U. semiornata

Textularia

and

spp.

- the Assemblage is characterized by the first occurrence

and by the great abundance of the species

Anomalinoides

dividens,

Varidentella reussi, V. rosea,

species as

Pseudotriloculina consobrina, Triloculina pseudoinflata,

T. inflata, Affinetrina ukrainica, Elphidium macellum,

Bolivina dilatata, B. sarmatica also occur.

oraminiferal

ssemblages

Paratethys

stages

Central

Eastern

late Badenian

- theAssemblage is characterized by the presence in a large number

of the ribbed miliolids, species as

Cycloforina karreri ovata, C.

karreri karreri, C. predcarpatica, C. fluviata, Articularia karreriella,

Varidentella pseudocostata,Quinqueloculina minakove ukrainica

accompanied by keeled elphidiids as

and

Elphidium reginum

aculeatum,

A. articulinoides, V. reussi, V. rotunda,

species as

Miliolinella selene,M. subrotunda, Pseudotriloculina consobrina,

E. macellum, Elphidiella serena, Porosononion subgranosus and

Lobatula lobatula also occur.

the Assemblage is characterized by the otall absence of the

ribbed miliolids, species as

Elphidium hauerinum, E.

macellum, E. excavatum, Elphidiella serena, Porosononion
subgranosus, P. martkobi, Nonion bogdanowiczi, Varidentella
reussi,V. rotunda, Articularia articulinoides, Articulina
problema, Pseudotriloculina consobrina are present in a large
number.

. m

. n

, C

e i

. p

, L

m h

. s

, X

r, X

. t

C. vespertilio,

S filicata

Sarmatian

olhynian

Bessarabian

- the Assemblage is characterized by the presence in a large
number of the small specimens belonging to the genus
Bolivina B. sarmatica B. moldavica, B. antiqua

(

) and

common occurrence of

Elphidum macellum E joukovi

subgranosus

E. crispum E. hauerinum Porosononion

martkobi,

species.

Noni n bogdanowiczi

Kossovian

late Badenian

Konkian

trilobus, G. bisphaerica, Velapertina indigena (Fig. 9D, E, F),

Sphaeroidina bulloides, Pullenia bulloides (Fig. 9G, H),

Hetrolepa dutemplei (Fig. 9I, J), Hansenisca soldanii

(Fig. 9K), Bulimina elongata elongata (Fig. 9L), B. aculeata

(Fig. 9M), Bolivina dilatata, Fursenkoina acuta (Fig. 9N).

The assemblage is recognized in the Machów section within

the interval 75–67 metres in depth and in the Jamnica M-83

core 235–225 metres in depth. Between the ostracods, the spe-

cies Kirthe sp. (Fig. 9O), Semicytherura filicata (Fig. 9P) and

Cytheropteron vespertilio (Fig. 10A, B), were encountered in

the Assemblage A. The assemblage is characteristic for the

late Badenian interval.

Assemblage B is defined by the abundance of Anomalinoides

dividens (Fig. 10C, D), though some other foraminifer species

such as Varidentella reussi (Fig. 10E, F), V. rosea,

Pseudotriloculina consobrina (Fig. G, H, I), Quinqueloculina

akneriana (Fig. 10J, K, L), Affinetrina ukrainica and Elphidium

macellum appear in a small number in this assemblage.

It occurs in the Machów section, in the interval 67–56.5 m and

in the Jamnica core section, in the interval 222–214 m

and indicates the lowermost Sarmatian (lowermost

Volhynian).

Assemblage C is defined by the abundance of the

ribbed miliolid species, such as Cycloforina karreri

ovata (Fig. 10M, N, O), C. karreri karreri (Fig. 10P,

Q,R), C. predcarpatica (Fig. 11A, B), C. fluviata

(Fig. 11C, D), Articularia karreriella (Fig. 11E, F),

A. articulinoides (Fig. 11G), Varidentella pseudo

costata (Fig. 11H, I), V. reussi, V. sarmatica (Fig. 11J),

V. rotunda (Fig. 11K, L) and Quinqueloculina mina

kovae ukrainica (Fig. 11M, N), accompanied by

elphi diids namely Elphidium reginum (Fig. 11O, P),

E. aculeatum (Fig. 11Q, R), Elphidiella serena

(Fig. 12A), Porosononion subgranosus (Fig. 12B, C)

and the species Lobatula lobatula (Fig. 12D, E, F).

Some other miliolid species, such as V. rosea, Milio

linella subrotunda, M. selene, and Pseudotriloculina

consobrina are also present in the assemblage. This

assemblage was found in all samples from the

Romanian sections (FH

Rădăuţi core and Dorneşti

outcrop) and in the Machów section comprising the

interval 56–45 m, as well as in the Jamnica core, from

the interval 202–182 m. Assemblage C indicates

early Volhynian age.

Assemblage D, recorded in the Machów section

comprising the interval 45–13, in Jamnica, the inter-

val 180–35 m, and in all samples from the Republic

of Moldova section, is characterized by the total

absence of the ribbed miliolids. The most common

species of this assemblage are Elphidium hauerinum

(Fig. 12G, H), E. excavatum (Fig. 12I), E. macellum

(Fig. 12J), E. tumidulus, Elphidiella

serena, Poro

sononion subgranosus, P. martkobi (Fig. 12K) and

Nonion bogdanowiczi (Fig. 12L), accompanied by

specimens of V. reussi, V. rotunda and Articularia

articulinoides, Articulina problema (Fig. 12M),

Pseudotriloculina consobrina and Pseudo triloculina nitens

indicating middle to late Volhynian age.

The early Sarmatian age is also confirmed by the

ostracod assemblages, which comprise Cytherois sarmatica

(Fig. 12 N, O), Aurila mehesi (Fig. 12P), A. notata (Fig. 12Q),

Callistocythere incostata (Fig. 12R, Fig. 13A), A. merita

(Fig. 13B), C. postvallata (Fig. 13C, D), C. egregia (Fig. 13E),

C. maculata (Fig. 13F), Xestoleberis dispar (Fig. 13G),

X. tumida, X. fuscata (Fig. 13H), Loxocorniculum hastatum

(Fig. 13I, J) and L. schmidi (Fig. 13K, L), Cytheridea hunga

rica (Fig. 13M, N)

Assemblage E, recorded in the top of the Machów section,

is characterized by the abundant presence of the bolivinids

with small tests, species such as Bolivina directa, B. molda

vica (Fig. 13O), B. nisporenica, B. sarmatica (Fig. 13P) and

by the common presence of elphidiids such as Elphidum

macellum, E joukovi, E. crispum, E. hauerinum, Porosononion

subgranosus, P. martkobi as well as Nonion bogdanowiczi and

possibily indicates lowermost Bessarabian age.

Fig. 7. Stratigraphically important foraminiferal assemblages (A–E) and

ostracoda identified in the analysed sections.

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Discussion

The lowermost sediments of the studied Machów and

Jamnica sections display the foraminiferal Assemblage A.

The assemblage is similar in foraminiferal composition, which

means the occurrence of Globigerina bulloides, G. praebul

loides, Velapertina indigena, Sphaeroidina bulloides, Bulimina

elongata elongata, B. aculeata, Sigmoilinita tenuis, Hanzawaia

crassiseptata and agglutinated forms such as Textularia, to the

upper Badenian Hanzawaia crassiseptata Zone, distinguished

by Łuczkowska (1964, 1974) from the Tarnobrzeg–Chmielnik

area, and also recorded in other parts of the Polish Carpathian

Foredeep (Odrzywolska-Bieńkowa 1975; Gonera 1997;

Szczechura 1982, 2000; Paruch-Kulczycka 2015). Many

foraminiferal species characteristic of Assemblage A were

additionally identified in similar stratigraphic position in other

regions of the Paratethys. The co-occurrence of Globigerina

bulloides, G. praebulloides, G. concinna, Globigerinoides

trilobus, B. elongata elongata, Uvigerina brunnensis, U. semi

ornata and Velapertina indigena was also recorded in the

upper Badenian deposits of the Vienna Basin (Kováčová &

Hudáčková 2009; Kováčová et al. 2009; Paulissen et al. 2011;

Zlinská et al. 2013), Transcarpathians (western Ukraine)

and the Republic of Moldova (Bobrinskaya 1967, 1970;

Bobrinskaya et al. 1998; Peryt et al. 2014). The other taxa

which occur in Assemblage A (see Fig. 7) were commonly

described in the Upper Badenian deposits of the Vienna basin

(Papp et al. 1978), Transylvanian Basin (Popescu 1979, 1995;

Ionesi & Enache-Bouau 1987; Filipescu 1996), and Polish

Carpathians (Szczechura 1982, 2000). Accordingly, based on

the similarity in taxonomic composition of foraminiferal com-

munities (Fig. 7.) and on the presence of the index species

Velapertina indigena, in these distinct basins of the Paratethys,

Assemblage A as described here can be correlated with the

Velapertina indigena Zone, originally described by Łucz-

kowska (1971) for the area of the inner and outer Carpathians

from Poland, Romania, the Czech Republic and Slovakia,

with the Velapertina Zone described by Popescu (1975) for the

deposits from Romania, as well as with the upper Badenian

Bulimina–Bolivina Zone and Zone with agglutinated fora-

minifera of the Vienna Basin (Cicha 1960, 1998) and with the

Ammonia galiciana Zone from Western Ukraine (Venglinsky

1962; Bobrinskaya et al. 1998). Additionally, we did not observe

the abundant presence of the Tenuitellinata and Tenuitella

taxa, as mentioned by Filipescu & Silye (2008) in the latest

Badenian deposits of the Transylvanian Basin. Possibly, this

lack is due to a different paleobiogeographic setting.

The upper Badenian age is also supported by the observed

ostracod assemblages that contain significant biostratigraphic

taxa Henryhowella asperrima (samples 1, 2 in the Machów

section) and Cytheropteron vespertilio, Semicytherura filicata,

Cnestocythere truncata (samples 19, 16 in the Jamnica bore-

hole); the aforementioned species were described as proxies

for the upper Badenian deposits of the Vienna Basin, while

their last occurrences marked the Badenian–Sarmatian boun-

dary (Gross 2006). However, in the studied area the last occur-

rence of some of the species previously assigned as being

exclusively Badenian (see Gross 2006), such as Henryhowella

asperrima and Cnestocythere lamellicosta, are placed in the

Anomalinoides dividens Zone, thus above the Badenian–

Standard

chron.

Gradstein

et al. 2012

NEOGENE

MIOCENE

Standard

nannof.

zones

Martini

1971

Paratethys

stages

Polish Basin

Luczkowska

1 64

9 , 1971

Eastern

TOR

ONIAN

NN7

NN8

NN9

NN10

NN11

Sarmatian sensu stricto

Pannonian

olhynian

A. dividens

C. k.ovata

V. sarmatica

E. hauerinum

Bessarabian

Khersonian

Studied

sections

Maeotian

Jamnica

this

paper

Dorn

şe

Central Paratethys

Vienna Basin

Grill 1941, Harzhauser

& Piller 2004

E. hauerinum

P. granosum

western Ukraine

Boborinskaya

et. al. 1998

C. badenensis

E. reginum

V. pseudocostata

V. reussi

E. hauerinum

A. dividens

E. reginum

Porosononion

“subgranosum”

Foraminiferal eco bio zon

Moldavian Platform

Ionesi 1991

Cycloforina fluviata

C. karreri ovata

“Lobatula lobatula”

V. reussi,A. sarmatica

A. beccarii

Porosononion

subgranosus

Elphidium macellum

Nonion

bogdanowiczi

Machow

Coste

tiş

P. consobrina

E. rugosum

Ostracoda

Jiricek &

Riha 1991

NO 10

P. farkasi

C. carinata

NO 11

C. hungarica

A. mehesi

NO 12

N. (N)

kollmani

A. notata

A. galiciana

Velapertina

indigena

Bulimina-Bolivina

NO 13

N. (M)

janoscheky

vindobonensis

11a

with

one

agglutinated

foraminifera

Transylvanian Basin

Popescu 1995,

Filipescu & Silye 2008

Velapertina Zone

Tenuitellinata Zone

Anomalinoides

dividens

E.reginum
V. reussi

Dogielina sarmatica

A.
sarmatica

P.aragviensis/Streptochilus

Zone

Fig. 8. Regional biostratigraphic subdivision of the Badenian and Sarmatian Paratethys.

435

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Sarmatian boundary, indicated by the foraminiferal assem-

blages. Jiříček & Říha (1991) assigned the uppermost

Badenian sediments (Bulimina–Bolivina foraminiferal Zone,

sensu Grill 1941) of the Central Paratethys to the NO 10 Zone,

which is defined by the authors as the occurrence interval of

Phlyctenophora farkasi

and Carinocythereis carinata species.

However, we did not identify these species in the studied sedi-

ments. A few ostracod species mentioned by Gross (2006) as

having their last occurrence in the Badenian deposits of the

Vienna Basin, such as Bosquetina carinella, Callistocythere

canaliculata, Cytheridea acuminata, Henryhowella asperrima,

were found in the Sarmatian deposits studied by us.

The Sarmatian foraminiferal assemblages of the Paratethys

are dominated by benthic forms, whereas planktonic foramini-

fera are scattered and taxonomically much more depleted

compared with Mediterranean assemblages of the same age.

They are mainly represented by Globigerina, Tenuitella,

Tenuitellinata and Streptochilus (Venglinsky 1975; Czepiec

1996; Filipescu & Silye 2008; Koubová & Hudáčková 2010).

Some recent studies (Filipescu & Silye 2008) provide new

biozonations for the Sarmatian interval, based on the plank-

tonic foraminifera. The aforementioned biozonation is still

very difficult to apply since the planktonic foraminifera

encountered in the Sarmatian deposits are still considered by

many authors as reworked from the Badenian deposits (i.e.

Łuczkowska 1964; Ionesi 1968; Paghida Trelea 1969;

Odrzywolska-Bieńkowa 1974; Brânzilă & Chira 2005; Ionesi

2006). Consequently, the standard planktonic foraminiferal

zonation (Gradstein et al. 2012), based mainly on Medi-

terranean species, cannot always be succesfully applied in the

Sarmatian of the Paratethys. By contrast, the Paratethyan

benthic foraminiferal zonations (e.g., Grill 1941; Ionesi 1991;

Popescu 1995; Cicha 1998) are most appropriate for biostrati-

graphical purposes.

The foraminiferal Assemblage B, recognized in the lower

part of the Machów and Jamnica sections, is marked by the

extinction of the following species (e.g., Velapertina indigena,

Heterolepa dutemplei, Melonis pomiloides, Sphaeroidina

bulloides) and by the mass occurrence of the species

Anomalinoides dividens, accompanied by miliolid species

(e.g., Varidentella reussi, Quinqueloculina akneriana, Pseudo

triloculina consobrina, Articularia karreriella) and may be

correlated with Łuczkowska’s (1964, 1974) Anomalinoides

dividens Zone. The author located the Badenian–Sarmatian

boundary at the base of this biozone, which is defined by the

bloom of Anomalinoides dividens that is still commonly

accepted as the informal definition of this boundary in Poland

(Odrzywolska-Bienkowa 1966; Garecka & Olszewska 2011;

Paruch-Kulczycka 2015), and was also applied by us to locate

the Badenian–Sarmatian boundary in the studied sections.

The bloom of Anomalinoides dividens is often associated with

the base of the Sarmatian in other areas of the Central

Paratethys as well (Filipescu 2004; Piller et al. 2007).

Additionally, the Anomalinoides dividens Zone was deter-

mined in the Vienna (Papp 1974; Harzhauser & Piller 2004)

and Transylvanian basins (Popescu 1995).

While the definition of the base of the Anomalinoides divi

dens Zone in these basins is rather the same as in Poland, its

upper boundary is defined entirely differently. In Poland, the

top of the Zone (correlated with the base of Assemblage C) is

placed at the FO and mass occurrence of the species

Cycloforina karreri ovata (Łuczkowska 1964, 1974), whereas

in the Vienna Basin it is placed at the level of the abundant

occurrence of the large elphidiids such as Elphidium reginum

(Papp 1974; Cicha 1998) and in the Transylvanian Basin

at the first occurrence of the species Varidentella reussi

(Popescu 1995). Accordingly, the correlation of the upper part

of the Anomalinoides dividens Zone of these distinct regions is

very difficult. In the lowermost part of the Sarmatian of

Western Ukraine, Bobrinskaya et al. (1998) distinguished the

“Cibicides badenensis” Zone, which is marked by the com-

mon appearance of the index species accompanied by milio-

lids. This Zone, described by Bobrinskaya et al. (1998) may

approximately correspond to the Anomalinoides dividens

Zone identified by us, since the species “Cibicides badenensis”

was treated by the authors as synonymous with Anomalinoides

dividens, in agreement with Brestenská (1974) and Popescu

(1995). Moreover, the zone includes taxa (Varidentella reussi,

Psedotriloculina consobrina, Articularia karreriella) which

commonly occur in the Anomalinoides dividens Zone (sensu

Łuczkowska 1964, 1974). We note that Anomalinoides divi

dens was also presented by Szczechura (1982, 2000) as

an ecophenotype of the species Lobatula lobatula (Walker &

Jacob 1798).

Assemblage C, identified in all the studied sections from

Poland and Romania, apparently corresponds to the

Cycloforina karreri ovata and Varidentella sarmatica zones of

the Polish Basin established by Łuczkowska (1964, 1974) and

with the Cycloforina karreri ovata, Cycloforina fluviata and

“Lobatula lobatula” Zone from the Moldavian Platform,

which we assume indicates early Volhynian age.

In this Assemblage C, numerous specimens of the taxa

Cycloforina karreri ovata occur, along with abundant miliolid

species such as C. predcarpatica, C. fluviata, Articularia

karreriella, A. articulinoides, Varidentella reussi, V. rotunda,

V. rosea, Miliolinella subrotunda and Miliolinella selene

accompanied by Elphidium reginum and Lobatula lobatula.

In previous studies (Ionesi 1968, 1991; Paghida Trelea 1969;

Brânzilă 1999; Ionesi 2006) the Cycloforina karreri ovata,

Cycloforina fluviata and “Lobatula lobatula” Zone was

attributed to the Buglovian age sensu Laskarew (1903).

Łuczkowska (1964, 1974) defined the Cycloforina karreri

ovata Zone mostly based on the numerous occurrence of the

index taxon, whereas Varidentella sarmatica was defined by

the mass presence of the species V. sarmatica. Since in the

studied sections both species occur together and do not display

any significant blooms, these two zones seem to be more sub-

jective and we treat them as being a single zone. Another spe-

cies occurring in large numbers in Assemblage C is Elphidium

reginum, which is also commonly used in dating the

Paratethyan sediments. This species is an index taxon of the

Zone defined in the Vienna Basin (Grill 1941; Papp 1956, 1963;

436

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Harzhauser & Piller 2004b; Schütz et al. 2007), the Tran-

sylvanian Basin (Popescu 1995; Filipescu et al. 1999) and the

Zsámbék basin, included in the Pannonian Basin of Hungary

(Görog 1992). It is considered a proxy for the early Sarmatian

interval also called the Elphidium reginum Zone of the above

mentioned regions and for the Moldavian Platform as well

(Ionesi 1968, 1991; Ionesi 2006). On the basis of its foramini-

feral composition, Assemblage C can be correlated with the

Elphidium reginum Zone of the Vienna and Zsámbék basins

and with the Varidentella pseudocostata and Elphidium

reginum Zone of Western Ukraine (Bobrinskaya et al. 1998).

The lower Sarmatian age is also supported by the nanno-

fossil assemblage identified by us (Fig. 14). Two index species

have been identified in sample 440 from the Dorneşti section

(Discoaster kulgeri) and in sample 448 from FH

Rădăuţi

(Discoaster deflandrei). The LO (lowermost occurrence) of

Discoaster kugleri is globally placed in the Serravallian

(Young 1998), at the base of the NN7 zone of Martini (1971),

while its LCO (lowest common occurrence) is situated in the

Mediterranean at 11.9 Ma and the HCO (highest common

occurrence) of this nannofossil is at 11.596 Ma (Raffi et al.

2006). As within the upper part of the global stage Seravallian,

situated on the boundary between the Badenian and Sarmatian

Paratethyan stages (Piller & Harzhauser 2005), the presence of

Discoaster kugleri in the studied sediments is indicative for

the presence of lower Sarmatian (= Volhynian) sediments.

The HO (highest occurrence) of the species Discoaster deflan

drei, and the HO of Discoaster kugleri (Young 1998), nanno-

fossil events are also situated in the NN7 zone of Martini

(1971). Based on the aforementioned data, we attribute the

deposits from Romania (FH

Rădăuţi core and Dorneşti

outcrop) to the NN7 calcareous nannoplankton zone, which is

lower Sarmatian. Our results are supported by previous studies

of Peryt (1997) and Garecka & Olszewska (2011) who dated

the Krakowiec Clays as belonging to the NN7 Zone.

Assemblage D, identified in the upper parts of the Machów

and Jamnica sections as well as in the entire Costeşti section,

seems to correspond to the Elphidium hauerinum Zone sensu

Łuczkowska (1964, 1974) and to the Varidentella reussi and

Articulina sarmatica Zone and the Elphidium rugosum,

Pseudotriloculina consobrina, Ammonia beccarii Zone estab-

lished by Ionesi (1991) for the Moldavian Platform indicating

the upper part of the early Sarmatian interval, based on the

common appearance of the foraminiferal species Elphidium

hauerinum, E. joukovi, E. fitchelianum, E. excavatum,

Elphidiella serena, Nonion bogdanowiczi, Porosononion

subgranosus, P. martkobi, and the subordinate number of

miliolids. Moreover, Assemblage D could be correlated with

the E. hauerinum Zone from the Vienna Basin (Grill 1941;

Cicha 1998) and E. hauerinum and V. reussi Zone from

western Ukraine (Venglinsky 1953, 1959; Didkowski 1961),

and the Elphidium hauerinum Zone from Zsámbék Basin

(Görög 1992), based on similar foraminiferal content (namely

common occurrence of Elphidium hauerinum, E. macellum,

Porosononion subgranosus, Varidentella reussi, Articularia

articulinoides) which occur in all these zones. All of the

above-mentioned zones identified in distinct Paratethyan

basins are placed in the middle to upper parts of the early

Sarmatian.

Assemblage E recorded in the top of the Machów section

(samples 28–34) is characterized by the abundance of compa-

ratively small and thin tested bolivinids and common elphidiid

Fig. 14. All microphotographs at LM (light microscope); N+ crossed nicols; NII transmitted light; scale bar in microns. 1 — Discoaster kugleri

Martini and Bramlette, 1963, NII, Dorneşti section. 2 — Discoaster musicus Stradner, 1959; NII, Dorneşti section. 3 — Discoaster deflandrei

Bramlette and Riedel, 1954, NII, Dorneşti section. 4 — Discoaster deflandrei Bramlette and Riedel, 1954, NII, Dorneşti section.

5 — Reticulofenestra pseudoumbilicus (Gartner, 1967) Garten, 1969, N+, Dorneşti section. 6 — Triquetrorhabdulus rugosus (Bramlette et

Wilcoxon, 1967), NII, Dorneşti section. 7, 8 — Calcidiscus macintyrei (Bukry et Bramlette, 1969) Loeblich et Tappan, 1978, 7 – NII, 8 – N+,

Dorneşti section.

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THE BIOSTRATIGRAPHY OF THE LATEST BADENIAN–SARMATIAN, CENTRAL PARATETHYS

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presence. The assemblage resembles the foraminiferal associa-

tion with the Porosononion “subgranosum” Zone from

western Ukraine (Venglinsky 1975) and Slovakia (Fordinál et

al. 2006; Fordinál & Zlinská 1998). Moreover, a similar asso-

ciation with small bolivinids accompanied by planktonic spe-

cies belonging to the planktonic genus Streptochilus has been

described recently in the Transylvanian Basin in upper

Sarmatian deposits (Filipescu & Silye 2008). Accordingly, we

do not exclude the possibility that the top of the Machów sec-

tion represents the lowermost part of the upper Sarmatian s.s.

which corresponds to the lowermost Bessarabian, albeit

an increase in the number of bolivinid species was also noticed

in the lower Sarmatian deposits of the Vienna Basin and

Zsámbék Basin (Jiříček 1972; Görög 1992; Tóth et al. 2010),

as well as in the eastern part of the Moldavian Platform

(Paghida Trelea 1969).

In the Sarmatian parts of the analysed sections

(Anomalinoides dividens, Cycloforina karreri ovata +

Vari dentella sarmatica and Elphidium hauerinum forami-

niferal zones) we have found straigraphically important

ostracod species, such as Aurila mehesi, A. merita, Senesia

vadaszi, Cytheridea hungarica, Callistocythere canaliculata,

C. incostata, C. postvallata, Loxocorniculum hastatum,

L. schmidi, Xestoleberis dispar and X. tumida. In general, they

are characteristic for the early Sarmatian (Gross 2006; Tóth

2008) and support the early Sarmatian age established on the

basis of foraminifera. The ostracod assemblages from the

lower part of the Machów (the interval from 66–57 m) and

Jamnica sections (sample 12, 202 m), as well as from Rădăuți

(175–30 m in depth) and Dornești sections (samples 440, 146

respectively 356, 358m in altitude) may be attributed to the

NO 11 Cytheridea hungarica–Aurila mehesi Zone defined by

Jiříček (1983) and Jiříček & Říha (1991) for the Lower

Sarmatian of the Central Paratethys and Lower Volhynian of

the Eastern Paratethys. In the studied area, the NO 11 Zone

approximately corresponds to the depth interval which is cor-

related with the Anomalinoides dividens and Elphidium regi

num foraminiferal zones (see discussion above) of Grill (1941)

and Harzhauzer & Piller (2004b). Our correlation agrees with

the correlation made by Jiříček & Říha (1991) and Gross

(2006).

The next species, traditionally regarded as stratigraphically

very important, is Aurila notata. The species has been found in

the Machów section (sample 13, 58 m depth), within the

Anomalinoides dividens Zone, in the lower part of the lower

Sarmatian deposits. This species also co-occurs with abundant

Aurila mehesi, defining NO 11 Zone. The species A. notata

characterizes the NO 12 Neocyprideis (N.) kollmanni–Aurila

notata Zone, as defined by Jiříček & Říha (1991). According

to them, the Zone NO 12 corresponds to foraminiferal

Elphidium hauerinum Zone as well as to the Aurila notata

Total Range Zone (Zelenka 1990) and to the foraminiferal

Elphidium hauerinum and Porosononion “subgranosum”

zones in the meaning of Grill (1941) and Harzhauzer & Piller

(2004b), indicating early to middle Sarmatian age. Similarly,

Aurila notata was mentioned by Kollmann (1960) as part of

the characteristic ostracod fauna of the Elphidium reginum

Zone. Additionally, Gross (2006) marked its stratigraphic

range from the Badenian–Sarmatian boundary in the

Pannonian of the Vienna Basin, therefore, we do not consider

this species as a reliable taxon indicating either the Elphidium

hauerinum Zone (upper part of the early Sarmatian) or the

middle Sarmatian. The early Sarmatian age is supported by

other ostracod taxa recorded in these deposits namely

Callistocythere postvallata, C. incostata, Cytheridea hunga

rica, A. mehesi, A. merita and Senesia vadaszi. These species

were identified by Tóth (2008) in the E. reginum Zone from

Zsámbék Basin (part of the Pannonian Basin, Hungary).

Additionally, Gross (2006) determined the last occurrence of

the following taxa: A. merita, C. postvallata, L. hastatum,

L. schmidi, Senesia vadaszi, Xestoleberis dispar and X. tumida

in the lower Sarmatian deposits of the Central Paratethys.

Accordingly, they are important markers for the Lower

Sarmatian across Central Paratethys. The occurrences of

C. postvallata, L. hastatum and L. schmidi (Gross 2006) in the

samples of Costești section (Republic of Moldova) confirm

the appartence of these deposits to the early Sarmatian.

It should be mentioned that Ionesi & Chintăuan (1994)

established an ostracod biozonation for the Moldavian

Platform. Within the lower Sarmatian deposits, the authors

distinguished the Cytheridea acuminata Zone and Leptocythere

mironovi Zone, the latter of which was subdivided into two

subzones Xestoleberis lutrae–Leptocythere bosqueti and

Xestoleberis elongata. Unfortunately, we could not apply this

biozonation because of the lack of most of the important taxa

defining this zonation in our material. Moreover, the collec-

tion of Ionesi & Chintăuan (1994) was restudied during the

research for this work and it was found out that a large part of

the collection is either very poorly preserved, making the

proper designation impossible, or incorrectly determined, for

example, in the case of Aurila mehesi, the species described as

typical taxa for the lower Bessarabian. We found that all of the

Aurila mehesi specimens of the collection were incorrectly

determined, so the above mentioned zonation is not reliable

and is not supported by adequate material.

Conclusions

Integrated micropaleontological studies were carried out in

detail on five Middle Miocene sections of the Central

Paratethys (Poland, Romania and Republic of Moldova), to

assess their biostratigraphic utility. In addition, nannofossil

analyses were done for the Romanian and Republic of

Moldova sections and correlated with the already published

data from the Polish sections.

Five foraminiferal assemblages, one Badenian (Assemblage

A) and four Sarmatian (Assemblages B–E), were identified,

corresponding to Łuczkowska’s (1964, 1974) division. These

assemblages display stratigraphic potential, being therefore

useful for correlation of upper Badenian–lower Sarmatian

deposits from the Central Paratethyan domain. The Badenian

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, 2017, 68, 5, 419–444

Assemblage A corresponds to Hanzawaia crassispetata Zone

(sensu Łuczkowska 1964, 1974), as well as to the Bulimina–

Bolivina Zone and Zone with agglutinated foraminifera from

the Vienna Basin and to the Ammonia galiciana Zone from

western Ukraine. Based on the planktonic foraminiferal spe-

cies, Assemblage A can be additionally correlated with the

Velapertina indigena planktonic foraminiferal zone of

Łuczkowska (1971) and with the Velapertina Zone of Popescu

(1975).

The mass occurrence of the species Anomalinoides dividens

(the base of Assemblage B) allowed the establishment of the

Badenian–Sarmatian boundary. Assemblage C seems to corre-

spond to the Cycloforina karreri ovata and Varidentella sar

matica zones from the Polish Basin (sensu Łuczkowska 1964,

1974) and Cycloforina karreri ovata, Cycloforina fluviata,

”Lobatula lobatula” Zone from the Moldavian Platform

(Ionesi 1991). The foraminiferal distributions recorded in the

studied sections do not reflect a clear separation between the

Cycloforina karreri ovata and Varidentella sarmatica Zones

(sensu Łuczkowska 1964, 1974) and thus they should be

applied as one biostratigraphic division. Moreover, based on

the presence of other indicator species such as Elphidium regi

num we correlated this assemblage with the Elphidium regi

num Zone from the Vienna Basin (sensu Grill 1941) and

Zsámbék Basin (Görög 1992) and with the Varidentella

pseudo costata and Elphidium reginum zones (Bobrinskaya et

al. 1998) from Western Ukraine.

Assemblage D approximately corresponds to the Elphidium

hauerinum Zone (sensu Łuczkowska 1964, 1974), the

Elphidium hauerinum Zone (sensu Grill 1941) from the

Vienna Basin, and the Elphidium hauerinum and Varidentella

reussi Zone from western Ukraine, as well as to the Varidentella

reussi and Articulina sarmatica Zone and Elphidium rugosum,

Pseudotriloculina consobrina, Ammonia beccarii Zone from

the Moldavian Platform (Ionesi 1991), and the Elphidium

hauerinum Zone from Zsámbék Basin, Hungary (Görög

1992). Assemblage E, characterized mainly by smaller and

thin tested bolivinids, possibly corresponds to the

Porosononion “subgranosum” Zone from western Ukraine

(Venglinsky 1975) and Slovakia (Fordinál et al. 2006; Fordinál

& Zlinská 1998) of the lowermost Bessarabian, lowermost

part of the upper Sarmatian s.s.

The studied ostracod content allowed us to recognize the

NO 10 and NO 11 zones originally described in the Vienna

Basin (Jiříček & Říha 1991). We identified 11 ostracod species

which are stratigraphically significant (Aurila mehesi,

A. merita, Senesia vadaszi, Cytheridea hungarica,

Callistocythere canaliculata, C. incostata, C. postvallata,

Loxocorniculum hastatum, L. schmidi, Xestoleberis dispar

and X. tumida) and may allow correlation between the

Badenian and Sarmatian deposits in the Central Paratethys.

The Badenian–Sarmatian boundary based on foraminifers,

located at the base of the Assemblage B (Anomalinoides divi

dens Zone), is placed close to the ostracod faunal turnover,

which means the disappearance of the typical Badenian spe-

cies (Henryhowella asperrima, Cytheropteron vespertilio,

Semicytherura filicata, Eucytheropteron inflatum, Cnesto

cythere truncata) and the appearance of new forms (Aurila

mehesi, A. merita, Senesia vadaszi, Cytheridea hungarica,

Callistocythere canaliculata, C. incostata, C. postvallata,

Loxocorniculum hastatum, L. schmidi, Xestoleberis dispar

and X. tumida) specific for the Lower Sarmatian in the entire

Central Paratethys. Some of the ostracod species, traditionally

believed to be exclusively Badenian, such as Henryhowella

asperrima, Cnestocythere truncata and Hemicytherura videns,

became extinct slightly higher, in the Anomalinoides dividens

foraminiferal Zone, which is earliest Sarmatian in age. Aurilla

notata, the index taxon of the NO 12 Zone, commonly treated

as a proxy for the upper part of the lower Sarmatian and mid-

dle Sarmatian as well, was identified in the Anomalinoides

dividens Zone. This finding casts doubt on its utility as

a biostratigraphic marker for the NO 12 Zone.

Based on our integrated data we managed to correlate the

studied Polish, Romanian and Republic of Moldova sections

from the Central Paratethys. Furthermore, we demonstrate that

the Sarmatian microfossil associations, regarded as rather

stratigraphically useless mostly based on paleoenvironmental

changes, can be applied not only for regional correlations,

but also for interregional ones between the Paratethyan

basins.

Acknowledgements: This work was funded by grant number

UMO-2013/09/D/ST10/04059 from the Polish National

Science Centre (NCN). The SEM photography was partly sup-

ported by the project “Microcosmos — Laboratory of Elec-

tronic Microscopy” funded by European Regional Develop-

ment Fund no. 650/25.04.2014 implemented by the Geological

Institute of Romania. The authors wish to express their grati-

tude to Dr. Igor Nicoară from the Institute of Geology and

Seismology of Republic of Moldova for providing the geolo-

gical maps and to Daniel Bîrgăoanu for the help in realizing

the SEM photos. The comments of Lilian Švábenická and two

anonymous reviewers are gratefully acknowledged.

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Appendix

Index of listed foraminifera taxa:

Affinetrina cubanica (Bogdanowicz, 1947)

Affinetrina ukrainica (Serova, 1952)

Ammonia beccarii (Linné, 1758)

Anomalinoides dividens Łuczkowska, 1967

Articularia articulinoides (Gerke & Issaeva, 1952)

Articularia karreriella (Venglinsky, 1958)

Articulina problema (Bogdanowicz, 1952)

Articulina sarmatica (Karrer, 1877)

Asterigerinata planorbis (d’Orbigny, 1846)

Aubignyna perlucida (Herron-Allen & Earland, 1913)

Bolivina antiqua d’Orbigny, 1846

Bolivina dilatata Reuss, 1850

Bolivina directa Cushman, 1936

Bolivina moldavica Didkowski, 1959

Bolivina nisporenica Maissuradze, 1988

Bolivina sarmatica Didkowski, 1959

Bolivina subdilatata Reuss, 1850

Budashevaella laevigata (Voloshinova, 1961)

Bulimina aculeata d’Orbigny, 1826

Bulimina elongata elongata d’Orbigny, 1826

Bulimina insignis Łuczkowska, 1960

Cibicides boueanus (d’Orbigny, 1846)

Lobatula lobatula (Walker & Jacob, 1798)

Cibicidoides austriacus (d’Orbigny, 1846)

Cribroelphidium poeyanum (d’Orbigny, 1826)

Cursina porocostata Popescu & Crihan, 2004

Cyclammina cancellata Brady, 1879

Cycloforina cristata (Millett, 1898)

Cycloforina fluviata (Venglinsky, 1958)

Cycloforina gracilis (Karrer, 1867)

Cycloforina predcarpatica (Serova, 1955)

Cycloforina karreri ovata (Serova, 1955)

Cycloforina karreri karreri (Reuss, 1869)

Cycloforina suturalis (Reuss, 1869)

Dogielina sarmatica (Bogdanowicz & Didkowski, 1951)

Elphidiella serena (Venglinsky, 1958)

Elphidium aculeatum (d’Orbigny, 1846)

Elphidium crispum (Linné, 1758)

Elphidium excavatum (Terquem, 1875)

Elphidium fichtelianum (d’Orbigny, 1846)

Elphidium hauerinum (d’Orbigny, 1846)

Elphidium incertum Williamson, 1858

Elphidium josephinum (d’Orbigny, 1846)

Elphiudium joukovi Serova, 1955

Elphidium macellum (Fitchel & Moll, 1803)

Elphidium macellum tumidocamerale Bogdanowicz, 1932

Elphdium reginum d’Orbigny, 1846

Elphidium reussi Marks, 1951

Elphidium rugosum (d’Orbigny, 1846)

Elphidium subumbilicatum Czjzek, 1848

Elphidium ungeri (Reuss, 1850)

Favulina hexagona (Williamson, 1848)

Fissurina cubanica (Bogdanowicz, 1947)

Fissurina isa (Venglinsky, 1958)

Fissurina mironovi (Bogdanowicz, 1947)

Fissurina toga Popescu, 1983

Fursenkoina acuta d’Orbigny, 1846

Glandulina ovula d’Orbigny, 1846

Globigerina bulloides d’Orbigny, 1826

Globigerina concinna Reuss, 1850

Globigerina dubia Egger, 1857

Globigerina praebulloides Blow, 1959

Globigerina triloba Reuss, 1850

Globigerinoides bisphaericus Todd, 1954

Globigerinita uvula Ehrenberg, 1861

Globorotalia mayeri Cushman & Ellisor, 1939

Globorotalia miocenica Palmer, 1945

Hansenisca soldanii (d’Orbigny, 1826)

Hanzawaia crassiseptata Łuczkowska, 1955

Heterolepa dutemplei (d’Orbigny, 1846)

Hyalinonetrion clavatum (d’Orbigny, 1846)

Lagena gracilis Wiliamson, 1848

Lagena striata (d’Orbigny, 1839)

Melonis pompiloides (Fichtel & Moll, 1798)

Miliolinella selene (Karrer, 1868)

Miliolinella subrotunda (Montagu, 1803)

Neoeponides schreibersi

(d’Orbigny, 1846)

Nodobaculariella ovalis Venglinsky, 1958

Nodobaculariella sulcata (Reuss, 1850)

Nonion bogdanowiczi Voloshinova, 1952

Nonion commune (d’Orbigny, 1846)

Nonion tumidulus Pishvanova, 1959

Nothia excelsa (Grzybowski, 1898)

Orbulina bilobata d’Orbigny, 1846

Orbulina suturalis (Brönnimann, 1951)

Ortomorphina dina Venglinsky, 1958

Pappina parkeri Karrer, 1877

Parafissurina subovata Parr, 1950

Porosolenia tibiscens Popescu, 1983

Porosononion subgranosus (Egger, 1857)

Porosononion martkobi (Bogdanowicz, 1947)

Praeglobulimina pyrula d’Orbigny, 1846

Protobotellina vermicula Łuczkowska, 1990

Pseudotriloculina consobrina (d’Orbigny, 1846)

Pseudotriloculina consobrina nitens (Reuss, 1850)

Pullenia bulloides (d’Orbigny, 1846)

Reophax globosus Sliter, 1968

Reticulophragmium rotundidorsatum Hantken, 1875

Rhabdammina abyssorum Carpenter, 1869

Quinqueloculina alexandri Łuczkowska, 1974

Quinqueloculina akneriana d’Orbigny, 1846

Quinqueloculina akneriana argunica Gerke, 1938

Quinqueloculina akneriana longa Gerke, 1938

Quinqueloculina bogdanowicz (Serova, 1955)

Quinqueloculina minakovae ukrainica Didkowski, 1961

Quinqueloculina perelegantissima Didkowski, 1961

Schackoinella imperatoria (d’Orbigny, 1846)

Semivulvulina pectinata (Reuss, 1850)

Sigmoilinita tenuis (Czjzek, 1848)

Sphaeroidina bulloides d’Orbigny, 1826

Textularia beregoviensis Venglinsky, 1958

Textularia concava (Terquem & Berthelin, 1875)

Triloculina circularis Bornemann, 1855

Triloculina gibba d’Orbigny, 1826

Triloculina gibba latodentata Didkowski, 1961

Triloculina inflata d’Orbigny, 1846

Triloculina inflata konkia (Didkowski, 1961)

Triloculina trigonula (Lamarl, 1804)

Uvigerina brunensis Karrer, 1877

Uvigerina grilli Schmid, 1971

Uvigerina liesingensis Toula, 1914

Uvigerina peregrina Cushman, 1923

Uvigerina rutila Cushman & Todd, 1941

Uvigerina semiornata d’Orbigny, 1846

Varidentella latecunata (Venglinsky, 1958)