GeolCarp_Vol65_No6_451

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, DECEMBER 2014, 65, 6, 451—470 doi: 10.1515/geoca-2015-0005

Oligocene—Early Miocene planktonic microbiostratigraphy

and paleoenvironments of the South Slovakian Basin

(Lučenec Depression)

SILVIA OZDÍNOVÁ

and JÁN SOTÁK

2,3

Geological Institute, Slovak Academy of Sciences, Dúbravská cesta 9, 840 05 Bratislava, Slovak Republic; geolsisa@savba.sk

Geological Institute, Slovak Academy of Sciences, Branch: Ďumbierska 1, 974 11 Banská Bystrica, Slovak Republic; sotak@savbb.sk

Department of Geography, Faculty of Education, KU Ružomberok, Hrabkovská cesta 1, 03 401 Ružomberok, Slovak Republic

(Manuscript received May 16, 2013; accepted in revised form October 7, 2014)

Abstract: Oligocene and Lower Miocene sediments of the Lučenec Depression were studied to demonstrate the plank-
tonic bioevents and climatic proxies from the Číž Formation (Rupelian) and Lučenec Formation (Chattian—Aquitanian)
on the basis of quantitative analyses of foraminifers and calcareous nannofossils. The oldest nannofossil assemblages of
the Číž Formation belonged to the NP23 Zone and were dominated by Reticulofenestra ornata known for preference of
temperate eutrophic water conditions. An increase in bioproductivity was documented by abundant large-sized plank-
tonic foraminifers (e.g. Turborotalia ampliapertura, Paragloborotalia nana, Subbotina gortanii) and epifaunal to shal-
low-infaunal benthic species. The middle part of the Číž Formation reveals a lowstand progradation of deltaic sediments
of the Rapovce Member. There, the planktonic foraminifers are impoverished in both size and diversity, containing
mostly tenuitellid and cassigerinellid species, probably as a result of decreased salinity and increased anoxia in the Tard
Clay. Contrary of this, the benthic foraminifers are rich, mainly the infaunal forms of uvigerinid species. They probably
proliferated due to a high organic flux from riverine input. Open marine conditions were restored in the upper part of the
Číž Formation above the lowest occurrence (LO) of Cyclicargolithus abisectus on the NP23—NP24 zone boundary. The
transitional interval between the Číž and Lučenec formations (O5/O6 – NP24/25) was approximated by the HOs of
Paragloborotalia opima and Sphenolithus distentus and the LOs of Globigerinoides primordius and Pontosphaera
enormis. Benthic foraminifera of the Lučenec Formation indicate a high productivity and oxygen-deplected environ-
ments. The Oligocene—Miocene boundary in the Lučenec Formation was appointed by the HOs of Helicospahera recta
and Dictyococcites bisectus. Foraminiferal markers of this boundary were established from the HO of Globigerina
ciperoensis and the LO of G. ottnangiensis. The highest nannofossil dating in the Lučenec Formation is recorded by the
LOs of Helicosphaera mediterranea (NN1 Zone) and Discoaster druggi (NN2 Zone). The uppermost part of the Lučenec
Formation contained many Paratethys benthic foraminifera, such as Uvigerina posthantkeni.

Key words: Oligocene—Lower Miocene, calcareous nannofossils, planktonic foraminifers, biozonation, climatic proxies,
paleoecology.

Introduction

The Paleogene formations of the Intra-Carpathian area belong
to two different basins – the Hungarian Paleogene Basin and
Central-Carpathian Paleogene Basin. These basins overlay the
Mesozoic basement nappe units, which were emerged during
the post-Gosau time and differ in type of sedimentation. Shal-
low-water epicontinental deposits fill the Hungarian Paleogene
Basin, while deep-water flysch is characteristic of the Central-
Carpathian Paleogene Basin (Nagymarosy 1990). The two ba-
sins also differ in their geotectonic position. The Hungarian
Paleogene Basin was probably formed as a retro-arc foredeep
basin (Tari et al. 1993), but the Central-Carpathian Paleogene
Basin is interpreted as a fore-arc basin (Soták et al. 2001).

The Hungarian Paleogene Basin extends northward into

the South Slovakian Basin (Fig. 1). Its north-western margin
occurs on the Šahy Antiform, which represents a strike-slip
elevation bordering the Buda Line (Vass 2003). Sediments
of the Hungarian Paleogene Basin occur in the Štúrovo area
and in the Ipe , Lučenec and Rimava depressions. The Paleo-
gene formations were drilled by a series of boreholes such as

Muž a-4 (Seneš 1960; Brestenská & Lehotayová 1960), Cha-
nava LR-9 (Šutovská 1987), Lučenec LC-2 (Vass et al.
2004), Rapovce LR-3 (Vass & Elečko 1992), Číž C-2 (Vass
& Elečko 1982), Muž a LKŠ-1 (Zlinská & Šutovská 1990),
Ivanice FGRK-1 (Zlinská 2009), Bátka RKZ-1 (Vass
1995a), Gemerská Párnica (Halásová et al. 1996), Gemerček
RAO-5 (Nagy et al. 2004) and others (see Vass et al. 2007).

The core of the Rapovce GTL-2 borehole drilled for the

geothermal  survey  by  Geospectrum  Ltd.  Bratislava  in  2007
provided a new opportunity to study the Oligocene and Lower
Miocene formations of the Lučenec Depression. The GTL-2
core  provided  the  reference  section  for  study  and  under-
standing  of  the  high-resolution  stratigraphy  and  paleoenvi-
ronmental  proxies  of  the  Oligocene  and  Lower  Miocene
deposits in the Lučenec Depression.

Geological setting

The Hungarian Paleogene Basin began to develop after a

long-term uplift, lateritic weathering and karst bauxite depo-

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sition  in  Bakony  and  the  Transdanubian  area  (Báldi  1986).
The Lutetian transgression gradually flooded lagoons, where
coal-bearing  layers  were  accumulated  (Dorog  Coal,  Obid
Member).  Progradation  of  a  shallow-water  carbonate  plat-
form is documented by the Szöc and Szépvölgy limestones.
Their outer shelf equivalent is represented by the Padrag and
Buda Marls (Báldi-Beke & Báldi 1985; Kázmér et al. 2003).
Late  Eocene  depocenters  were  shifted  to  the  Buda  Basin,
which  rapidly  subsided  during  the  Oligocene,  until  bathyal
conditions  were  reached.  Basin  differentiation  led  to  initial
isolation recorded by euxinic facies of the Tard Clay (Báldi
1986).  The  Rupelian-Chattian  sequences  of  the  North  Buda
Basin are formed by the Kiscell Clay, Széczény Schlier and
Eger Sandstone (Báldi 1986). The Oligocene transgression is
also  expressed  by  the  initial  flooding  of  the  basinal  area  in
Southern Slovakia (Vass 1995a).

The Oligocene sequence of the Lučenec Depression (Fig. 2)

started by the continental fluvial deposits of the Skálnik Mem-
ber, followed by transgressive sediments of the Číž Formation
represented  by  conglomerates,  breccias,  sandstones  and  silt-
stones with marine fauna. The lower members of the Číž For-
mation  consist  of  lagoonal  sediments  of  the  Blh  Member,
nearshore sediments of the Hostišovce Member and offshore
and  carbonate  peri-platform  facies  named  the    Bátka  Lime-
stone.  The  major  part  of  the  Číž  Formation  belongs  to  the
Lenártovce Member, which is characterized by deep-water fa-
cies  of  grey  claystones,  siltstones  and  sandstones  known  as
Kiscell Clay. The regressive sequence of the Číž Formation is

developed in deltaic sediments of the Rapovce Member, rep-
resented by grey sandstones and siltstones with plant rem-
nants, coal laminae and shallow water fauna (Vass 1995a).

The Egerian cycle of deposition in the South Slovakian

Basin  is  represented  by  the  Lučenec  Formation,  reaching
thicknesses  of  more  than  1000 m  in  some  places.  The  sedi-
ments of the Lučenec Formation superposed the deep-water
sediments  of  the  Číž  Formation  or  covered  the  pre-Tertiary
basement. These transgressive deposits are formed by brec-
cias,  conglomerates  and  sandstones  of  the  Panica  Member,
bioclastic  limestones  and  calcareous  sandstones  with  Mio-
gypsina  and Lepidocyclina  of  the  Budikovany  Member  and
clastic  limestones,  breccias  and  conglomerates  with  large
pectinids  of  the  Bretka  Member.  The  Lučenec  Formation
is  mostly  composed  of  grey  calcareous  siltstones  of  the
Szecsény  Schlier,  which  documents  the  outer  shelf  up  to
upper  bathyal  environment.  Upper  Eggerian  sediments  of
the  Lučenec  Formation  belong  to  the  Opatová  Member
(Šutovská-Holcová et al. 1993), representing delta-type sedi-
ments,  such  as  channel  gravels,  prodelta  claystones,  delta-
front  sandstones  and  coal  seams,  developed  in  a  great
thickness  (150 m).  These  deltaic  deposits  represent  the  ter-
minal  sediments  of  the  North  Buda  Basin,  which  evolved
into  the  Fi akovo/Pétervására  Basin  from  the  beginning  of
the  Early  Miocene  and  then  from  the  Ottnangian  into  the
Nógrád/Novohrad Basin.

Transgressive sediments of the Fi akovo/Pétervására Basin

are represented by the Fi akovo Formation. They are shallow-

Fig. 1.

Regional geological context of area studied (A) within the Hungarian Paleogene Basin (B – scheme after Nagymarosy 1990), South

Slovakian North Hungarian units (C – sketch map after Vass 1995b) and location of the Rapovce GTL-2 borehole. Legend to sketch
map: 1 – pre-Teriary units; 2 – Hungarian Paleogene Basin; 3, 4 – Fi akovo-Pétervására Basin: 3 – Fi akovo Formation and Péter-
vására Sandstone, 4 – Upper Szécsény and Putnok Schliers; 5 – Eggenburgian rhyodacide tuffs in Gyulakeszi and Bukovina Formations;
6 – Nógrad-Novohrad Basin, Ottnangian and Karpatian sediments; 7 – Upper Karpatian—Lower Badenian ryolite formation (Tarr Tuff);
8 – Middle to Upper Miocene volcanics; 9 – Middle to Upper Miocene sediments; 10 – Upper Miocene to Pleistocene basalts.

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Fig. 2. Lithostratigraphic scheme of the North Hungarian—South Slovakian basins, providing the correlation of the Oligocene—Lower Mio-
cene formations in the Lučenec, Ipe and Rimava Depressions (Vass & Elečko 1982 adapted by Holcová 2005) and Eger area (Báldi 1986).
Abbreviations: Mb – member, CGL – conglomerates, Lms. – limestones.

water sediments deposited in high-energy shoreface and shal-
low-marine  environments  described  as  the  Čakanovce  Beds,
Lipovany Sandstone, Tachty Sandstone, Jalová Sandstone and
Pétervására  Sandstone  (e.g.  Vass  &  Elečko  1982;  Sztanó  &
Tari 1993). The Late Eggenburgian regression resulted in ter-
restrial  clay  and  sandy-gravel  deposition  of  the  Zagyvapálfa
and Bukovinka Formations, which include numerous bird and
mammal  footprints  covered  by thick  tuff  deposits  of  the
Gyulakeszi Rhyolite Tuff Formation (Márton et al. 1996).

The new subsidence is related to accommodation of the

Nógrád/Novohrad  basin  in  the  Early  Ottnangian  time.  Ma-
rine  transgression  was  preceded  by  fluvial,  swampy  and
lacustrine  sedimentation  of  the  Salgótarján  Formation,
which  contains  coal  bearing  deposits  of  the  Pôtor  Member
(Vass  et  al.  1983).  The  upper  Ottnangian—Karpatian  forma-
tions  of  marine  deposits  are  represented  by  the  Plachtince/
Mátra  Beds  and  Modrý  Kameň/Egyházasgerge  Formations.
The main part of the Modrý Kameň Formation belongs to the
Sečianky Member also named the Garáb Schlier, consisting
of  calcareous  claystones  with  full-marine  fauna  such  as
benthic  and  planktonic  foraminifers,  mollusks,  gastropods
(e.g.  Holcová  1996;  Ondrejíčková  1972;  Vass  2002).  The
Modrý  Kameň  Formation  is  superposed  by  the  Tarr  Tuff
Formation, which marks the beginning of volcanic activity at
the Karpatian-Badenian boundary. Badenian basin-fill forma-
tions are formed by shoreface sands of the Príbelce Member,
volcanoclastic  sediments  and  volcanic  intrusive  complexes
named the Vinica Formation, Halič and Šiator Andesites and
Pokoradza Formation. The Nógrád/Novohrad Basin came to
an end due to domal uplift of the South Slovakian volcanic

area, which resulted in marine regression and basin inversion
from the Middle Badenian time (Vass & Šucha 1994; Vass
1995b; Kováč et al. 2001). Upper Miocene deposits of the
Lučenec and Rimava depressions are represented by fluvial
gravels and variegated clays of the Poltár Formation and ba-
salts of the Podrečany Formation.

Material and methods

The Rapovce GTL-2 core was drilled at a site located

4.36 km  south  of  Lučenec  near  Rapovce  village
(N 48°16’39.52”, E 19°40’43.47” – Fig. 1). The borehole
reached a depth of up to 1501.5 m and caught the following
lithostratigraphic  formations  (Vass  et  al.  2008  –  Fig. 2):
Fi akovo  Formation  (5.00—45.00 m),  Lučenec  Formation
(45.00—606.00 m),  Číž  Formation  (606.00—775.00 m)  and
Mesozoic basement complex represented by the Middle- and
Upper  Triassic  carbonates  (775.00—1501.50 m).  The  sands
and sandstones of the Fi akovo Formation in the upper part
of the GTL-2 borehole belong to the Lipovany Member. The
Lučenec Formation consists of grey calcareous siltstones of
the  Széczény  Schlier  (45.00—595.00 m)  with  intercalations
of 1m thick beds of fine-grained sandstones. Sediments below
the Széczény Schlier belong to the Panica Member, consisting
of  coarse-  to  medium  grained  conglomerates  and  sandstones
(595.00—606.00 m). The Číž Formation reaches a thickness of
up to 169 m (606.00—775.00 m) and its main part is formed by
deltaic  sands  of  the  Rapovce  Member  (606.00—745.00 m),
outer shelf siltstones and claystones of the Lenártovce Mem-

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ber  (745.00—65.00 m),  lagoon  coal-bearing  sandstones  of  the
Hostišovce  Member  (795.00—770.00 m)  and  transgressive
sandstones  and  pebbly  sandstones  of  the  Blh  Member
(770.00—775.00 m).

Both the standard Mediterranean and regional Central

Paratethys stages to the Oligocene and Early Miocene strati-
graphic  interpretation.  The  Paleogene  Time  Scale  for  the
standard  Mediterranean  stages  followed  Gradstein  et  al.
(2012)  and  the  Paratethyan  stages  were  applied  in  accor-
dance  with  their  definition  for  the  Kiscellian  (Báldi  1969,
emend.  Báldi  et  al.  1984),  Egerian  (Báldi  &  Seneš  1975,
emend.  Báldi  et  al.  1999)  and  Eggenburgian  (Steininger  &
Seneš 1971). The Paratethyan nomenclature was also used in
an  informal  sense,  as  for  designation  of  Kiscell-type  fossil
assemblages,  sedimentary  facies,  transgressive  events  (e.g.
initial flooding of the Kiscellian Sea into the South Slovakian
Basin – cf. Vass 2003).

The borehole section was sampled every 5 meters and pro-

vided  78  samples  for  foraminiferal  and  calcareous  nanno-
plankton  study.  The  samples  were  taken  mainly  from  the
calcareous-rich  claystones  and  siltstones.  Nannofossil  sam-
ples were prepared by the decantation method (Haq & Loh-
mann  1976;  Perch-Nielsen  1985).  The  smear  slides  were
inspected under the light microscope Zeiss at 1.500

× magni-

fication and nannofossils documented by digital camera. For
quantitative analysis, at least 300 specimens per sample were
counted in randomly selected fields.

The foraminiferal microfauna was washed, dried and

sieved, obtaining the size fractions > 250 µm, > 150 µm and
> 38 µm. The residues were examined under a stereomicro-
scope Olympus and picked for study using the JEOL Scan-
ning Electron microscope.

Nannoplankton age determination was carried out accord-

ing to the zonation by Martini (1971), completed by Perch-
Nielsen  (1985),  Young  (1998)  and  Wise  et  al.  (2002).
Planktonic foraminiferal biostratigraphy was applied on the ba-
sis of the Oligocene—Early Miocene zonal schemes (Berggren
&  Miller  1988;  Spezzaferri  1994;  Berggren  et  al.  1995)  and
Paratethyan  foraminiferal  data  (Sztrákos  1979;  Rögl  1985;
Cicha et al. 1998; etc.). Bioevents of nannoplankton and fora-
miniferal  biostratigraphy  were  denoted  by  the  acronyms
sensu Berggren & Pearson (2005), “LO” for the lowest occur-
rence and “HO” for the highest occurrence of the index species.

determinable, G (good) – the species are very easily identi-
fiable, etching and overgrowth is slight.

The samples were evaluated by using the following abun-

dance scale: VH (very high) – more than 20 specimens in the
1 field of view, H (high) – 10—20 specimens in the 1 field of
view, M (moderate) – 5—10 specimens in the 1 field of view,
L (low) – 1—5 specimens in the 1 field of view and VL (very
low) – less than 5 specimens in the 5 field of view.

Climatic proxies and trophic conditions were inferred

from the temperature preferences and life strategy of calcare-
ous nannofossils (Wei et al. 1992; Bralower 2002; Persico &
Villa 2004; Bartol et al. 2008) and planktonic foraminifera
(Boersma & Premoli Silva 1983, 1991; Spezzaferi 1995;
Wade et al. 2007).

Results

Calcareous nannofossils

Preservation of calcareous nannofossils was moderate, be-

cause the specimens are slightly mechanically damaged, but
most of them can still be identified easily. Abundance of cal-
careous nannofossils was low, considering < 5 specimens oc-
cur in one field of view of the microscope.

Species diversity

Nannoplankton assemblages are moderately diversified,

involving  a  total  number  of  37  nannofossil  taxa  with
30  (85 %)  autochthonous  and  7  (15 %)  reworked  species.
Their  proportion  is  rather  equal,  showing  a  slight  downwar
increase  of  reworked  species  in  the  Číž  Formation  (18 %)
and  upward  increase  of  autochthonous  species  in  the
Lučenec  Formation  (86 %)  –  Fig. 3.  The  ratio  of  the  re-
worked  species  could  have  increased  due  to  nannofosil  re-
sedimentation  in  prodeltaic/deltaic  sediments  of  the  Číž
Formation,  whereas  the  indigenous  species  dominated  dur-
ing  the  stabilization  of  full-marine  environments  in  the
Lučenec Formation (Széczény Schlier – cf. Vass 1995a).

Nannofossils of the Číž Formation from the depth

775—595 m are rich in species Coccolithus pelagicus, Cycli-

Fig. 3. Nannofossil variations in the ratio of autochthonous versus re-
worked species across the Rapovce GTL-2 section.

Nannofossil assemblages were evaluated on the basis

of  specimen  preservation  and  abundance,  nannofossil
temperature preferences and their trophic strategy. Sta-
tistical  methods  (percentage  analyses)  were  performed
by counting of 300 specimens on each sample, provid-
ing  paleoecological  data  for  evaluation  of  autochtho-
nous  nannofossil  species.  Percentage  share  of  each
nannoplankton group is expressed in diagrams.

Preservation of calcareous nannofossils was deter-

mined according to Roth & Thierstein (1972) as fol-
lows: VP (very poor) – etching and mechanical
damage to specimens is very intensive, P (poor) – frag-
mentation and/or overgrowth of the specimens makes it
difficult to identify them, M (moderate) – mechanical
damage and etching of the specimens are visible in the
minority of the nannoassemblage, specimens are easily

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cargolithus  floridanus,  Dictyococcites  bisectus  and  Zygrha-
blithus bijugatus. The common species of this nannoplankton
association  are  Helicosphaera  compacta,  Helicosphaera
euphratis,  Reticulofenestra  lockeri  and  Reticulofenestra
scrippsae.  There  is  also  a  low  abundance  of  the  species
Isthmolithus  recurvus  and  Reticulofenestra  ornata,  which
disappear at the 595 m interval.

The most abundant nannofossils in the Lučenec Formation

comprise the species Coccolithus pelagicus, Cyclicargolithus
floridanus,  Dictyococcites  bisectus  and  Zygrhablithus  biju-
gatus.  They  are  commonly  associated  with  Helicosphaera
compacta,  Helicosphaera  euphratis  and  Reticulofenestra
lockeri.  The  nannofossil  association  with  Cyclicargolithus
abisectus,  Helicosphaera  recta  and  Pontosphaera  desueta
appeared  from  the  depth  of  470—595 m.  The  association
changed  at  the  depth  of  470 m  by  disappearance  of  Heli-
cosphaera  compacta  and  Sphenolithus  distentus  and  appear-
ance of Pontosphaera enormis. Rare occurrences of Discoaster
cf.  adamanteus,  Triquetrorhabdulus  cf.  carinatus  and  Sphe-
nolithus conicus were recorded from the depth of 345—300 m.
Some important species of the association, such as  Cyclicar-
golithus  abisectus,  Helicosphaera  recta  and  Dictyococcites
bisectus,  vanished  at  the  depth  of  210 m.  New  specimens  of
nannofossils Helicosphaera carteri, Helicosphaera mediterra-
nea and Discoaster druggii appeared from the depth of 160 m.

Nannoplankton biostratigraphic interpretations

Nannofossil assemblages of the Číž and Lučenec forma-

tions consist of several stratigraphically important taxa,
which enable us to distinguish the following nannoplankton
zones (Figs. 4, 5):

The NP23 Zone was determined in the interval 775—595 m

based on the species Reticulofenestra ornata, R. lockeri and
Isthmolithus recurvus, which have their lowest common oc-
currence reported from this zone.

The appearance of Reticulofenestra lockeri is the typical

nannofossil datum of the NP23 Zone (Nagymarosy & Voronina
1992).  This  interval  represents  a  peak  of  anoxic  conditions
and stagnant regime in Paratethyan basins (Báldi 1984). The
isolation  of  Paratethys  and  the  decline  of  salinity  within  the
NP23 Zone caused the extinction of cosmopolitan nannoflora
and expansion of the endemic species Reticulofenestra lockeri
that tolerated hyposaline waters (Nagymarosy 2000; Melinte-
Dobrinescu & Brustur 2008). The NP23/NP24 zone boundary
was  stated  on  the  basis  of  the  first  occurrence  of  Cyclicar-
golithus  abisectus  (Perch-Nielsen  1985;  Young  1998).  Some
authors reported this species already from the upper part of the
NP23  Zone  (Fornaciari  &  Rio  1996;  Kaenel  &  Villa  1996;
Maiorano  &  Monechi  2006;  Melinte-Dobrinescu  &  Brustur
2008).  In  the  borehole,  the  LO  of  C.  abisectus  was  found  at
595 m  close  to  the  boundary  of  the  Číž  and  Lučenec  forma-
tions (Fig. 5).

The NP24 Zone was delimited by the overlapping ranges

of stratigrafically important species  Cyclicargolithus abisec-
tus,  Helicosphaera  recta,  Pontosphaera  desueta  and  Reticu-
lofenestra  lockeri.  The  appearance  of  cosmopolitan  species
reflects  restored  marine  environments  and  sea-level  rise
(Krhovský  &  Djurasinovič  1992;  Švábenická  &  Stráník

2004). However, the nannoplankton diversity of the NP24
Zone is not markedly higher than that of the NP23 Zone.

The NP24—NP25 boundary is inferred from the HO of Sphe-

nolithus distentus (Berggren et al. 1995) and was recorded at
470 m.  Pontosphaera  enormis,  which  has  its  LO  within
NP24—25, can be used as a marker species (Young 1998). In
the  Rapovce  section  it  has  a  depth  of  470 m.  This  boundary
was also outlined by the species of Helicosphaera compacta,
which  has  occurrences  at  470 m  that  imply  their  HO  in  the
NP24 Zone (Maiorano & Monechi 2006; Melinte-Dobrinescu
&  Brustur  2008).  The  nannofossil  associations  of  the  NP24
and  NP25  zones  should  also  be  different  in  size  from  Cycli-
cargolithus  abisectus  (Śliwińska  et  al.  2012),  whereby  the
abundance of Cyclicargolithus abisectus >10 µm corresponds
to the lower part of the NP24 and NP23 zones and large-sized
nannofossils  of  Cyclicargolithus  abisectus  >13 µm  corre-
spond  to  the  uppermost  part  of  the  NP24  and  lower  part  of
NP25  zones.  Significant  increase  in  the  size  of  these  nanno-
fossils was not observed. The upper part of the NP 25 Zone is
marked  by  the  LOs  of  Triquetrorhabdulus  cf.  carinatus  and
Sphenolithus conicus in the interval between 345—300 m.

The Oligocene-Miocene boundary is unclear since there is

no agreement on the definition of the base of the NN1 Zone
(LO  of  Helicosphaera  recta  sensu  Martini,  1971)  and  CN1
Zone  (LO  Sphenolithus  ciperoensis  sensu  Okada  &  Bukry,
1980). Later, this boundary was redefined by the LO of Dic-
tyococcites bisectus at the base of the NN1 Zone (Berggren
et al. 1995; Fornaciari & Rio 1996) or by the FOs of Spheno-
lithus belemnos and Helicosphaera carteri in the upper part
of  the  NN1  Zone  (Young  1998).  These  nannofossil  datums
from the Mediterranean were completed by some additional
bioevents from the Paratethyan basins, where the Oligocene-
Miocene boundary can be marked by the HO of Dictyococ-
cites  bisectus  and  FADs  of  Helicosphaera  kampteri  and
Helicosphaera  scissura  (Holcová  2001;  Garecka  2012),
Reticulofenestra  pseudoumbilica  (Holcová  2005),  Spheno-
lithus  delphix  (Rögl  &  Nagymarosy  2004),  Helicosphaera
mediterranea  (Marunteanu  1999;  Chira  2004)  and  Spheno-
lithus  capricornutus  (Holcová  2005;  Melinte-Dobrinescu  &
Brustur 2008).

The Oligocene-Miocene boundary of the Rapovce section

was identified by the HOs of Helicosphaera recta and Dictyo-
coccites  bisectus  at  the  depth  of  210 m.  This  datum  is  fol-
lowed by the appearance of Helicosphaeraceae from the NN1
and NN2 zones. The LOs of Helicosphaera carteri and Heli-
cosphaera mediterranea were recorded at the depth of 135 m.
The  NN1—NN2  zone  boundary  is  constrained  by  the  LO  of
Discoaster druggii dated to 23.2 Ma chronostratigraphic scale
(Berggren et al. 1995), and in Paratethyan stages corresponds
to  the  Egerian-Eggerburgian  boundary  (Lehotayová  1982;
Marunteanu  1999;  Holcová  2002).  The  LO  of  Discoaster
druggii was recorded in the depth of 155 m. These bioevents
are too scattered to provide consistent indications of the Oli-
gocene-Miocene boundary (sensu Young 1998).

Nannofossil paleoecology

Temperature proxies: The average proportion of the

warm-water species, discoasterids, helicosphaerids and sphe-

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noliths forms  15 %  with  increased  quantity  in  the  interval  of
775—595 m  (21 %),  corresponding  to  the  NP23  Zone,  Mid-
Rupelian. The next increase of the warm-water species (17 %)
was recorded in the interval 50—150 m, which is correlated with
the NN2 Zone, Eggenburgian. The group of species preferring
temperate-water  conditions  such  as  Cyclicargolithus  florida-
nus,  Cyclicargolithus  abisectus,  Coccolithus  sp.  and  Dictyo-
coccites bisectus reaches 54 % of the assemblage (Fig. 6).

The percentage of the cold-water species, above other

reticulofenestrids is approximately 16 % of the nannofossil
assemblage. The proportion of these species varied by rhyth-
mical decreasing and inceasing with temperature fluctuation.
A slight decrease of the cold-water species to 13 % was ob-
served above 175 m.

The nannofossil distribution in the GTL-2 section suggests

water temperature differences between the Číž Formation

Fig. 4. Calcareous nannoplankton species from the Číž and Lučenec formations in the Rapovce GTL-2 section. 1 – Isthmolithus recurvus,
760 m, NP23 Zone, Číž Formation; 2 – Lanternithus minutus, 760 m, NP23 Zone, Číž Formation; 3 – Dictyococcites bisectus, 745 m,
NP23 Zone, Číž Formation; 4 – Reticulofenestra ornata, 745 m, NP23 Zone, Číž Formation; 5 – Cyclicargolithus floridanus, 725 m,
NP23 Zone, Číž Formation; 6, 7 – Cyclicargolithus abisectus, 6—560 m, 7—515 m, NP24—25 Zone, Lučenec Formation; 8 – Reticu-
lofenestra lockeri, 560 m, NP24—25 Zone, Lučenec Formation; 9 – Pontosphaera multipora, 515 m, NP24—25 Zone, Lučenec Formation;
10 – Pontosphaera desueta, 495 m, NP25 Zone, Lučenec Formation; 11, 12 – Pontosphaera enormis: 11 – 495 m, 12 – 375 m, NP24—25
Zone, Lučenec Formation; 13 – Helicosphaera euphratis, 545 m, NP24—25 Zone, Lučenec Formation; 14 – Helicosphaera mediterranea,
135 m, NN1—NN2 Zone, Lučenec Formation; 15 – Discoaster druggii, 155 m, NN2 Zone, Lučenec Formation, 16 – Helicosphaera carteri,
135 m, NN1—NN2 Zone, Lučenec Formation. Scale bars 1 µm.

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(Rupelian)  and  Lučenec  Formation
(Chattian).  In  the  Číž  Formation,  the
highest  share  of  nannofossils  belongs
to the temperate-water species (54 %),
complemented  by  relatively  common
warm-water  taxa  (22 %)  and  a  small
number of cold-water taxa (13 %). The
assemblages of the Lučenec Formation
were also formed mostly by temperate-
water  species  (54 %),  but  they  were
complemented  by  few  specimens  of
warm-water  taxa  (13 %)  and  an  in-
creased  number  of  cold-water  species
(17 %).  Considering  the  above  men-
tioned  data,  the  sediments  of  the  Číž
Formation  were  deposited  in  warmer
water conditions than the sediments of
the Lučenec Formation.

The balanced composition of the

nannofossil  assemblages  in  the  inter-
val  from  535—770 m  of  the  Lučenec
Depression  indicates  an  increase  of
warm water conditions during the Early
Oligocene. That is related to the onset
of  the  Kiscellian  transgression  (Soták
et  al.  2002;  Soták  2010).  This  period
corresponds  to  the  NP23  and  NP24
zones. Similar conditions were reported
from  the  Novaj  section  (Báldi-Beke
1980,  1984),  the  Harshegy  Sandstone
Formation  and  the  Kiscell  Clay  For-
mation  (Báldi-Beke  1980).  Early  to
Middle  Oligocene  temperature  varia-
tions were also recorded by nannofos-
sil  proxies  in  the  Krynica  Zone  of  the
Magura  Nappe  (Oszczypko-Clowes  &
Żydek 2012).

Samples from the interval between

50—150 m show an increase of warm-
water species related to Early Miocene
climate warming in the NN2 Zone
(Soták et al. 2002; Chira 2004; Švábe-
nická et al. 2007).

Trophic resources: Calcareous

nannofossils of the Rapovce section
imply

different

trophic-preference

conditions. The first group consists of

Fig. 6. Quantitative diagram of nannofossils
expressed  as  percentage  of  species  with
warm-water  preferences  (A),  temperate-
water  preferences  (B)  and  cold-water  pref-
erences (C) plotted against the depth in the
Rapovce  GTL-2  borehole  section  (nanno-
plankton temperature preferences according
to Wei et al. 1992; Bralower 2002; Persico
& Villa 2004; Bartol et al. 2008).

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eutrophic species such as Braarudosphaera bigelowii, Cycli-
cargolithus floridanus, Cyclicargolithus abisectus, Dictyo-
coccites bisectus, Reticulofenestra ornata and Zyghrablithus
bijugatus (Aubry 1992; Krhovský et al. 1992; Villa et al.
2008).

The second group consists of oligotrophic species that are

able to survive even in the areas poorer in nutrients. Oligo-
trophic species are represented by autochthonous forms such
as Coccolithus, Discoaster, Helicosphaera, Reticulofenestra,
Sphenolithus, Thoracosphaera, Triquetrorhabdulus (Haq &
Lohman 1976; Wei & Wise 1990a,b; Aubry 1992; Bralower
2002).

The third group consists of species for which trophic strat-

egy is not exactly specified. Their quantity forms the missing
percentage in calculation of high- and low-nutrient taxa in
nannofossil assemblages.

Trophic preferences of calcareous nannofossils (Fig. 7)

show  a  slightly  higher  percentage  of  oligotrophic  species
(44 %)  over  the  high-nutrient  taxa  (42 %).  Eutrophic  species
are more present in the lower part of the section (48 %), where
they  prevail  over  oligotrophic  species  (38 %).  This  interval
corresponds to the NP23 Zone. Contrary to this, the eutrophic
species  are  less  frequent  in  the  higher  part  of  the  borehole
(39 %),  where  the  oligotrophic  species  become  dominant
(49 %). Considering that, the nannofossils of the Číž Forma-
tion  indicate  more  eutrophic  conditions  (48 %)  than  their
mostly  oligotrophic  assemblages  in  the  Lučenec  Formation
(39 %). The proliferation of eutrophic species could have been
caused by increased resources of nutrients in the basins during
the  Kiscellian  transgression  (cf.  Báldi-Beke  1980,  1984;
Švábenická  et  al.  2007).  Similar  eutrophic  conditions  have
also been identified in the Lower Oligocene formations of the
Magura basin (Oszczypko-Clowes & Żydek 2012).

Foraminifera: biostratigraphy and paleoenvironments

Planktonic foraminifera of the borehole section show a wide

species diversity and distinctive changes in frequency and dis-
tribution  (Figs. 8,  9).  Their  succession  reaches  a  great  abun-
dance  already  at  the  base  of  the  Číž  Formation  (770/750 m),
comprising large-sized forms of globigerinids, turborotaliids
and paragloborotaliids. Planktonic associations are diversified
to include the following species: Turborotalia ampliapertura,
Paragloborotalia  nana,  Subbotina  gortanii,  Globigerina
praebulloides,  Globigerina  officinalis  and  Globigerina  leroi.
These foraminiferal species enable us to determine the Mid-
dle  Rupelian  age  (O2  Zone  sensu  Berggren  &  Pearson

2005). Planktonic bioproductivity increased probably simul-
taneously with the sea-level rise during the Kiscellian trans-
gression. Transgressive conditions of the Číž Formation are
also indicated by well-aerated shelf environments of benthic
foraminifera, represented by the epifaunal species Eponides
umbonatus,  Heterolepa  dutemplei, Anomalina  cryptomphala,
Lenticulina  budensis,  Percultazonaria  fragaria.  Microfau-
nistic  assemblages  of  the  Číž  Formation  changed  in  deltaic
sediments  of  the  Rapovce  Member  in  620—750 m,  where
planktonic  foraminifers  provide  a  distinct  reduction  in  test-
size,  abundance  and  diversity.  Their  association  consists  of
minute forms of tenuitellids, cassigerinellids, globorotaloids
and  catapsydracids.  A  similar  horizon  of  small-sized  forms
of planktonic foraminifers was observed by Horváth (1998)
in the Hungarian Paleogene Basin. The taxonomic diversity
of planktonic foraminifers in the Rapovce Member decreases
to several species: Tenuitella gemma, Cassigerinella globu-
losa,  Globorotaloides  hexagonus  and  Catapsydrax  martini.
Dwarfing  of  planktonic  foraminfers  implies  stress-induced
conditions, such as the influence of hyposaline waters on the
morphogenesis  of  Cassigerinella  chipolensis  (Martinotti,
1989)  or  cool-water  preferences  of  tunuitellids  (Pipperr  &
Reichenbacher,  2010).  Stress  conditions  of  surface-water
productivity, which were also indicated by the appearance of
pyritized  frustules  of  diatoms  and  tests  of  pteropods,  were
caused probably by eutrophication, shallowing and brackish-
ing of sea-water (Šutovská 1987). The decreased planktonic
productivity  is  replaced  by  increased  benthic  productivity,
which was manifested by the abundance of uvigerinid fora-
minifers.  The  population  density  of  the  Rapovce  Member
was  increased  in  some  horizons  by  monospecific  associa-
tions of Uvigerina hantkeni corresponding to “the Uvigerina
bloom”  in  the  Kiscell  Clay  at  the  base  of  the  NP24  Zone
(Horváth 1998).

The transitional beds between the Číž and Lučenec Forma-

tions from 600—460 m contain the Kiscellian-Egerian associ-
ations  of  foraminiferal  microfauna.  The  character  of  the
microfauna implies the restoration of full-marine conditions,
which is manifested by blooming of the planktonic foramini-
fers and recolonization of the benthic biota. The abundance
of  planktonic  foraminifera  increased  abruptly  at  the  begin-
ning  of  the  transgressive  cycle  above  the  Rapovce  Member
in 600—605 m, by the appearance of the Egerian species like
Globoturborotalita  ouachitaensis,  G.  angulisuturalis,  G.
woodi  and  G.  labiacrassata  (Holcová  in  Vass  et  al.  2004).
Those  foraminifers  are  associated  with  Paragloborotalia
opima,  P.  bella,  Globigerina  praebulloides  and  Globigeri-

Fig. 8. Foraminiferal species from the Číž and Lučenec Formations in the Rapovce GTL-2 section. 1 – Turborotalia ampliapertura, 770 m,
O2 Zone, Číž Formation; 2 – Subbotina gortanii, 770 m, O2 Zone, Číž Formation; 3, 4 – Paragloborotalia opima, 515 m, O4—O5 Zone,
Číž Formation; 5, 6 – Globigerinoides primordius, 455 m, transitional beds of the Číž and Lučenec Formations, O5 Zone; 7, 8 – Globigerina
praebulloides: 7 – 55 m, M1 Zone, Lučenec Formation, 8 – 770 m, O2 Zone, Číž Formation; 9, 10 – Glogoturborotalita ouachitaensis,
605 m, O4 Zone, Číž Formation; 11 – Globoturborotalita woodi, 605 m, O4 Zone, Číž Formation; 12 – Globoturborotalita connecta,
455 m, O5 Zone, transitional beds of the Číž and Lučenec Formations; 13 – Paragloborotalia bella, 605 m, O4 Zone, Číž Formation;
14 – Paragloborotalia pseudokugleri, 455 m, O5 Zone, transitional beds of the Číž and Lučenec Formations; 15 – Globigerina wagneri,
455 m, O5 Zone, transitional beds of the Číž and Lučenec Formations; 16 – Globigerina anguliofficinalis, 225 m, O6 Zone, Lučenec For-
mation; 17, 18 – Globigerina ciperoensis, 135 m, O6 Zone, Lučenec Formation – upper part; 19, 20 – Globigerina ottnangiensis, 55 m,
M1 Zone, Lučenec Formation – uppermost part.

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nella  obesa.  Common  occurrence  of  species  from  the  Glo-
boturborotalita – group with G. angulisuturalis (LO in O4
Zone according to Berggren & Pearson 2005) and P. opima
indicates the Early Chattian biozones (P20—21/O3—O4 Zones
sensu Berggren & Miller 1988; Berggren & Pearson 2005).
Benthic  foraminifers  are  represented  by  euryoxibiont  and
low-oxygen  tolerant  species  like  Sphaeroidina  bulloides,
Pulenia  bulloides,  Eggerella  bradyi,  Uvigerina  vickburgen-
sis,  Bulimina  cf.  altasica,  Bulimina  schischkinskayae,  Cas-
sidulinoides  tenuis,  Kareriella  quadrinoides,  Stilostomella
consobrina and Stilostomella adolphina.

The base of the Szécsény Schlier of the Lučenec Formation

at  455 m  is  marked  by  the  HO  of  Paragloborotalia  opima.
Similarly, the presence of this species in the Lučenec Forma-
tion was also noted by Holcová (2001, 2005). The extinction
of P. opima provided an important datum for the early Chat-
tian biozone (O5 Zone sensu Berggren & Pearson 2005). At
the same horizon, the LO of Globigerinoides primordius was
recorded.  This  species  appeared  together  with  other  primi-
tive specimens of the genus Globigerinoides such as transi-
tional  forms  to  G.  altiaperturus  and  G.  immaturus  (Keller
1981;  Ouda  1998).  Change  to  the  new  globigerinid  forms
with secondary appertures on the spiral side appeared in re-
sponse  to  Late  Oligocene  warming  (Jenkins  1973).  The
planktonic  foraminifers  of  the  Lučenec  Formation  also  in-
clude Globoturborotalita ouachitaensis, G. connecta, Globi-
gerina  wagneri,  Paragloborotalia  pseudokugleri  (LO  in
O6  Zone  with  estimated  age  25.9  Ma  –  Berggren  et  al.
1995),  “Dentoglobigerina”  cf.  venezuelana  and  Globigeri-
nella  obesa.  The  benthic  foraminiferal  microfauna  of  the
Lučenec  Formation  is  enriched  in  epifaunal  habitats  with
plano-convex  trochospiral,  biconvex  trochospiral,  rounded
planispiral,  spherical  and  uniserial  morphotypes  (sensu
Corliss & Chen 1988). They belong to the following species
Cibicidoides  ungerianus,  C.  lopjanicus,  Gyroidenoides  sol-
dani,  Eponides  umbonatus,  Fontbothia  wuellerstorfi,
Sphaeroidina ciperana, Lenticulina cultrata, Percultazonaria
fragaria,  Vaginulinopsis  pseudodecorata,  Anomalina  affinis,
Ceratocancris  haueri,  Pullenia  bulloides  and  Stilostomella
pauperata. The predominance of epifaunal and shallow infau-
nal  benthic  foraminifers  implies  improved  conditions  of  bot-
tom water oxygenation in the the Lučenec Formation.

The foraminiferal microfauna changes in the upper part of

the  Lučenec  Formation  from  330—320 m,  with  calcareous
species  diminishing  and  agglutinated  species  becoming
dominant.  Associations  involve  species  like  Trochammina
squamata,  T.  inflata,  T.  globigeriniformis  and  Haplophrag-
moides sp. This assemblage suggests the deep-water associa-
tion  of  agglutinated  foraminifera  with  a  reduced  amount  of
dissolved  oxygen.  Deep-water  conditions  of  the  middle
bathyal  zone  are  also  indicated  by  infaunal  benthic  species
like Bulimina coprolithoides, Pullenia bulloides and Globo-
cassidulina  depressa  (cf.  Kaiho  &  Nishimura  1992).  These
species also provide evidence of dysoxic and highly produc-
tive  conditions  (Corliss  &  Chen  1988).  The  occurrence  of
trochamminid species and bathyal benthic foraminifers in the
upper  part  of  the  Lučenec  Formation  indicates  a deepening-
upward  basin  during  the  Egerian  time.  This  is  also  evident
from  a high  concentration  of  siliceous  sponge  rhaxes  in

schlier  sediments.  Sea-level  rise  in  the  Lučenec  Formation
coincides with the global eustatic cycle TB1.4, which culmi-
nated  in  the  topmost  part  of  the  Széczeny  Schlier  with  the
appearance  of  late  Oligocene  to  early  Miocene  microfauna
(Šutovská-Holcová et al. 1993; Vass 1995a).

Late Oligocene planktonic foraminifera were recovered

with  the  appearance  of  Paragloborotalia  pseudokugleri  at
225 m.  It  extended  to  the  topmost  part  of  the  P22/O6  Zone
(Spezzaferri 1991). This species is associated with Globigerina
ciperoensis,  G.  anguliofficinalis,  Globigerinoides  primordius
and  G.  praealtiaperturus,  their  common  occurrences  are
known from the O6 Zone. This evidence appears to establish
the Late Chattian age of the Lučenec Formation at 225 m.

The globigerinid foraminifers in the uppermost part of the

Lučenec  Formation  (above  225 m)  are  developed  mostly  as
five-chambered  species  belonging  to  Globigerina  ottnang-
iensis. The appearance of this species can be used as a bio-
stratigraphic  marker  of  the  Oligocene-Miocene  boundary
(Rögl 1994; Cicha et al. 1998). The abundance maximum of
G. ottnangiensis occurs at 55 m. Early Miocene associations
of  planktonic  foraminifera  are  completed  by  Cassigerinella
globulosa,  Paragloborotalia  semivera,  “Dentoglobigerina”
venezuelana and Globigerina praebulloides. Benthic associ-
ations  are  formed  mostly  by  epifaunal  forms  with  rounded
planispiral,  plano-convex  and  biconvex  trochospiral,  and
spherical morphotypes. They belong to the species: Angulo-
gerina  angulosa,  Lenticulina  arcuatostriata,  L.  cultrata,
Cibicidoides  ungerianus,  C.  lopjanicus,  Almaena  osnabru-
gensis,  Hanzawia  boueana,  Melonis  affinis,  and  Pullenia
bulloides.  Infaunal  species  are  less  frequent,  for  example
Praeglobobulimina  pupoides  and  Globocassidulina  oblonga,
but some of them already belong to the Early Miocene fora-
minifera.  The  Eggenburgian  index  species  Uvigerina  post-
hantkeni  (cf.  Cicha  et  al.  1998;  Rupp  &  Haunold-Jenke
2003; Grunert et al. 2013) appeared in the uppermost part of
the Lučenec Formation at 55 m.

Conclusions

The Oligocene and Early Miocene deposits of the Číž and

Lučenec Formations provide important data for recognition
of the planktonic bioevents and paleoenvironments of the
South Slovakian Basin (Fig. 10). The data from the Rapovce
GTL-2 section lead to the following conclusions:

1. The Kiscellian transgression at the beginning of the

NP23 Zone is marked by extinction and speciation of nanno-
fossils (e.g. LO R. lockeri and R. ornata and HO I. recurvus),
and  diversification  and  high-rate  bioproductivity  of  plank-
tonic  foraminifera  (paragloborotaliids,  turborotaliids,  globi-
gerinids). The transgressive cycle corresponds to the TB1.2
event of global eustasy (Vass 1995a), which is documented
by  well-aerated  shelf  environments  with  epifaunal  benthic
foraminifers and nannofossil proxies of warm- to temperate-
water and oligotrophic conditions.

2. A regressive phase in the Late Rupelian is documented

by the lowstand deposition of prodeltaic sediments of the
Rapovce Member. These sediments reveal stress-induced
conditions due to eutrophication and brackishing of sea-wa-

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ter, which resulted in diversity fall and blooming of endemic
nannoflora, especially Reticulofenestra ornata, and dwarfing
of planktonic foraminifera such as tenuitellids and catapsy-
dracids. Infaunal biota, mainly uvigerinid foraminifers, pro-
liferated from increased nutrients and bottom-water dysoxia.
Improvement of the open-marine conditions occurred within
the NP23—24 boundary, which is approximated by the ap-
pearance of nannofossil species Cyclicargolithus abisectus.

3. Restoration of full-marine conditions was controlled by

the  sea-level  rise  of  the  TB1.3  cycle  in  the  transitional  se-
quences  of  the  Číž  and  Lučenec  formations.  Transgressive
sediments  are  enriched  with  reworked  nannofossils  (Fig. 3).
The autochthonous species of the NP24 Zone include cosmo-
politan nannofossils such as Cyclicargolithus, Helicosphaera,
Dictyococcites and Pontosphaera (Fig. 6). The climatic prox-

Fig. 10. Integrated biostratigraphy of the Rapovce section with datum events of planktonic foraminifers (black triangles) and nannofossils
(white triangles). Biostratigraphic data are indicated by the highest occurrences (HO) and lowest occurrences (LO) of the index taxa.

ies  of  nannofossils  indicate  eutrophic  and  temperate-water
conditions.  Planktonic  foraminiferal  assemblages  with  Para-
globorotalia  opima  and  Globigerina  ciperoensis  define  the
O5 Zone.  The  abundance  of  globoturborotaliid  and  para-
globorotaliid species, which belong to mixed-layered or upper
thermocline habitats (Pearson & Wade 2009), implies warm-
to  temperate-water  water  conditions.  Oxygen  depleted  con-
ditions  are  indicated  by  deep-infaunal  benthic  species  like
Bulimina, Chilostomella and Stilostomella.

4. The Rupelian-Chattian boundary was identified by the

HO of Paragloborotalia opima and the HO of Sphenolithus
distentus at the base of the Lučenec Formation (O5 Zone,
NP24—25 Zone) (Fig. 10). New taxa of planktonic foraminifer
are represented by globigerinid forms with secondary aper-
tures (the LO of Globigerinoides primordius), which are asso-

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THICA, 2014, 65, 6, 451—470

ciated with five-chambered species (Globigerina ciperoensis)
and the first paragloborotaliid forms with arched sutures (P.
pseudokugleri). Both the appearance of primitive Globigeri-
noides and the nannofossil Sphenolithus distentus provide
evidence of the Late Oligocene climatic warming. Nannofos-
sil assemblages of the Lučenec Formation are also enriched
in content of oligotrophic and temperate-water species com-
pared to those in the Late Rupelian sediments of the Číž For-
mation. The benthic microfauna of the Lučenec Formation
consists of mostly epifaunal and in the upper part also agglu-
tinated forms, which provide evidence of better oxygenation
and deepening-upward conditions during the sea-level rising
of the TB1.4 cycle.

5. The Oligocene-Miocene boundary was identified in the

uppermost part of the Lučenec Formation at 210 m, by sev-
eral nannofossil bioevents such as the HOs of Helicosphaera
recta and Dictyococcites bisectus and LOs of Helicosphaera
carteri, H. mediterranea and Discoaster druggii in the NN1
and  NN2  zones  (Fig. 10).  Early  Miocene  planktonic  fora-
minifera  are  represented  mostly  by  five-chambered  species
belonging to Globigerina ottnangiensis. Benthic microfauna
strongly  increased  in  abundance  with  large-sized  tests  of
Lenticulina species, associated with numerous specimens of
Angulogerina  angulosa  and  Uvigerina  posthantkeni.  Benthic
life could proliferate with opening of the Eggenburgian sea-
way  connection  into  the  Lučenec  Depression.  This  became
evident  mainly  in  the  Fi akovo/Pétervására  Basin  (Sztanó
1995; Kováč et al. 2001).

Acknowledgment: The authors are grateful to S. Ćorić and
M.  Oszczypko-Clowes  for  their  constructive  comments  and
improvements  of  the  manuscript.  Our  thanks  go  to  D.  Vass
and  J.  Dzúrik  for  providing  the  opportunity  to  study  the
Rapovce  borehole  section  and  their  advice  and  assistance.
This work has been supported by the research agency VEGA
Project 2/0042/12, and by funds received through the Centre
of  Excellence  for  Integrative  Research  of  the  Earth’s  Geo-
sphere (ITMS 262201200064).

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Checklist of taxa mentioned in the text in alphabetic order:

Appendix 1

Nannoplankton species

Arkhangelskiella cymbiformis Vekshina, 1959
Braarudosphaera bigelowii (Gran & Braarud, 1935) Deflandre,
1947
Coccolithus eopelagicus (Bramlette & Riedel, 1954) Bramlette
& Sullivan, 1961
Coccolithus formosus (Kamptner, 1963) Wise, 1973
Coccolithus pelagicus (Wallich, 1877) Schiller, 1930
Coronocyclus nitescens (Kamptner, 1963) Bramlette &
Wilcoxon, 1967
Cyclicargolithus abisectus (Müller, 1970) Wise, 1973
Cyclicargolithus floridanus (Hay et al., 1967) Bukry, 1971
Dictyococcites bisectus (Hay, Mohler & Wade, 1966) Bukry
& Percival, 1971
Discoaster adamanteus Bramlette & Wilcoxon, 1967
Discoaster deflandrei Bramlette & Riedel, 1954
Discoaster druggii Bramlette & Wilcoxon, 1967
Helicosphaera ampliaperta Bramlette & Wilcoxon, 1967
Helicosphaera bramlettei (Müller, 1970) Jafar & Martini, 1975
Helicosphaera carteri (Wallich, 1877) Kamptner, 1954
Helicosphaera compacta Bramlette & Wilcoxon, 1967
Helicosphaera euphratis Haq, 1966
Helicosphaera kampteri (Hay & Mohler in Hay et al., 1967),
Locker, 1970
Helicosphaera mediterranea Müller, 1981
Helicosphaera recta (Haq, 1966) Jafar & Martini, 1975
Helicosphaera scissura Miller, 1981
Holodiscolithus macroporus (Deflandre in Deflandre & Fert,
1954) Roth, 1970

Isthmolithus recurvus Deflandre in Deflandre & Fert, 1954
Pontosphaera desueta (Müller, 1970) Perch-Nielsen, 1984
Pontosphaera enormis (Locker, 1967) Perch-Nielsen, 1984
Pontosphaera  multipora  (Kamptner,  1948)  Roth,  1970
emend. Burns, 1973
Reticulofenestra bisecta (Hay, Mohler & Wade, 1966) Roth,
1970
Reticulofenestra lockeri Müller, 1970
Reticulofenestra minutula (Gartner, 1967) Haq & Berggren,
1978
Reticulofenestra ornata Müller, 1970
Reticulofenestra pseudoumbilica (Gartner, 1967) Gartner, 1969
Reticulofenestra  scrippsae  (Bukry  &  Percival,  1971)  Roth,
1973
Reticulofenestra  umbilica  (Levin,  1965)  Martini  &  Ritz-
kowski, 1968
Sphenolithus belemnos Bramlette & Wilcoxon, 1967
Sphenolithus capricornutus Bukry & Percival, 1971
Sphenolithus ciperoensis Bramlette & Wilcoxon, 1967
Sphenolithus conicus Bukry, 1971
Sphenolithus delphix Bukry, 1973
Sphenolithus distentus (Martini, 1965) Bramlette & Wilcoxon,
1967
Sphenolithus  moriformis  (Brönnimann  &  Stradner,  1960)
Bramlette & Wilcoxon, 1967
Transversopontis pygmaea (Locker, 1967) Perch-Nielsen, 1984
Zygrhablithus  bijugatus  (Deflandre  in  Deflandre  &  Fert,
1954) Deflandre, 1959

Appendix 2

Foraminiferal species

Almaena osnabrugensis (Roemer, 1838)
Angulogerina angulosa (Willimson, 1858)
Anomalina affinis (Hantken, 1948)
Anomalina cryptomphala (Reuss, 1850)
Bulimina cf. Altasica Cushman & Parker, 1937
Bulimina coprolithoides Andreae, 1884
Bulimina schischkinskayae Samoylova, 1947
Cassidulinoides tenuis Phleger & Parker, 1951
Cassigerinella globulosa (Egger, 1857)
Cassigerinella chipolensis (Cushman & Ponton, 1932)
Catapsydrax martini (Blow & Banner, 1962)
Ceratocancris haueri (d’Orbigny, 1839)
Cibicidoides lopjanicus (Myatlyuk, 1950)
Cibicidoides ungerianus (d’Orbigny, 1846)
“Dentoglobigerina” venezuelana (Hedberg, 1937)
Eggerella bradyi (Cushman, 1911)
Eponides umbonatus (Reuss, 1860)
Fontbothia wuellerstorfi (Schwager, 1866)
Globigerina anguliofficinalis (Blow, 1969)

Globigerina ciperoensis Bolli, 1954
Globigerinella obesa (Bolli, 1957)
Globigerina ottnangiensis Rögl, 1969
Globigerina officinalis Subbotina, 1953
Globigerina praebulloides Blow, 1959
Globigerina praebulloides leroi Blow & Banner, 1962
Globigerina wagneri Rögl, 1994
Globigerinoides altiaperturus Bolli, 1957
Globigerinoides immaturus Le Roy, 1939
Globigerinoides primordius Blow & Banner, 1962
Globocassidulina depressa (Asano & Nakamura, 1937)
Globocassidulina oblonga (Reuss, 1850)
Globorotaloides hexagonus Natland, 1938
Globoturborotalita angulisuturalis (Bolli, 1957)
Globoturborotalita brazieri (Jenkins, 1966)
Globoturborotalita connecta (Jenkins, 1964)
Globoturborotalita labiacrassata (Jenkins, 1966)
Globoturborotalita ouachitaensis (Howe & Wallace,
1932)

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Globoturborotalita woodi Jenkins, 1960
Gyroidenoides soldani d’Orbigny, 1982
Hanzawia boueana (d’Orbigny, 1846)
Heterolepa dutemplei (d’Orbigny, 1846)
Kareriella guadryinoides (Fornasini, 1885)
Lenticulina arcuatostriata (Hantken, 1875)
Lenticulina budensis (Hantken, 1875)
Lenticulina cultrata (Montfort, 1808)
Melonis affinis (Reuss, 1851)
Paragloborotalia bella (Jenkins, 1967)
Paragloborotalia nana (Bolli, 1957)
Paragloborotalia opima (Bolli, 1957)
Paragloborotalia pseudocontinuosa (Blow, 1959)
Paragloborotalia pseudokugleri (Blow, 1969)
Percultazonaria fragaria (Gümbel, 1868)
Praeglobobulimina pupoides (d’Orbigny, 1846)

Pulenia bulloides(d’Orbigny, 1826)
Sphaeroidina bulloides (d’Orbigny, 1846)
Sphaeroidina ciperana Cushman & Todd, 1949
Stilostomella adolphina (d’Orbigny, 1846)
Stilostomella consobrina (d’Orbigny, 1839)
Stilostomella pauperata (d’Orbigny, 1839)
Subbotina gortanii (Borsetti, 1959)
Tenuitella gemma Jenkins, 1966
Trochammina globigeriniformis (Parker & Jones, 1865)
Trochammina inflata (Montagu, 1808)
Trochammina squamata (Jones & Parker, 1860)
Turborotalia ampliapertura Bolli, 1957
Uvigerina hantkeni (Cushman & Edwards, 1937)
Uvigerina posthantkeni Papp, 1971
Uvigerina vickburgensis (Cushman & Ellisor, 1931)
Vaginulinopsis pseudodecorata Hagn & Holzl, 1952