GeolCarp_Vol63_No2_149

www.geologicacarpathica.sk

GEOLOGICA CARPATHICA

, APRIL 2012, 63, 2, 149—164 doi: 10.2478/v10096-012-0012-8

Paleoecology of the Upper Eocene—Lower Oligocene

Malcov Basin based on the calcareous nannofossils: a case

study of the Leluchów section (Krynica Zone, Magura Nappe,

Polish Outer Carpathians)

MARTA OSZCZYPKO-CLOWES

and BARTŁOMIEJ ŻYDEK

Jagiellonian University, Institute of Geological Sciences, Oleandry 2a, 30-063 Kraków, Poland; m.oszczypko-clowes@uj.edu.pl

(Manuscript received February 8, 2011; accepted in revised form September 30, 2011)

Abstract: During the period of ca. 20 Ma (Middle Eocene—Chattian) the Leluchów Succession of the Magura Basin
passed through drastic changes of sedimentary condition and paleobathymetry from well oxygened red shales with
Reticulofragmium amplectens, deposited beneath CCD, red Globigerina oozes, to oxygen depleted organic-rich menilite-
type shales and finally to flysch deposition of open marine conditions. The biostratigraphic and lithostratigraphic scheme
is well established with the Leluchów Marl Member – Zones NP19—20 to NP22 (Late Eocene—Early Oligocene), Smereczek
Shale Member, Zone NP23 (Early Oligocene) and the Malcov Formation s.s., Zone NP24 (Early—Late Oligocene). The
aim of the paper is to present the quantitative analyses as the basis for paleoecological changes in the Magura Basin
during the Late Eocene—Late Oligocene period. The changes manifest themselves through a decrease in the water tem-
perature and progressing eutrophication. Species typical of brackish water conditions and restricted to the Paratethys
region were identified from the NP23 Zone.

Key words: Late Eocene—Oligocene, Western Carpathians, Magura Nappe, Krynica Zone, Malcov Formation,
paleoecology, biostratigraphy, calcareous nannoplankton.

Introduction

The Eocene and Oligocene were periods of major change in
ocean circulation and global climate. Starting from the Mid-
dle  Eocene  through  to  the  Late  Oligocene  several  paleocli-
matic  events  have  been  identified  by  paleontological  and
geochemical data. The main episodes include:
– The Middle Eocene Climatic Optimum (MECO) warming
event at  ~ 40 Ma (Bohaty & Zachos 2003; Jovane et al. 2007);
–  Late  Eocene  warming  interval  at  ~ 36 Ma  (Bohaty  &
Zachos 2003);
– Oi-1 event at ~34 Ma (Miller et al. 1991; Wei et al. 1992;
Aubry 1992; Zachos et al. 1996; Persico & Villa 2004; Coxall
et al. 2005);
–  The  warming  episode  in  the  Late  Oligocene  at  ~26 Ma
(Miller et al. 1987; Zachos et al. 2001; Villa & Persico 2006;
Pekar et al. 2006).

According to Miller et al. (2009) the Eocene-Oligocene

transition is characterized by 3 main episodes: (1) 2 °C deep-
water  cooling  and  a  drop  in  sea  level  of  ca.  25 m  (EOT-1,
33.80 Ma);  (2)  a  deep-water  cooling  and  minor  drop  in  sea
level  (EOT-2,  33.63 Ma),  (3)  a  deep-water  cooling  of  2 °C
and  a  drop  in  sea  level  of  80 ± 25 m  (Oi-1,  33.45 Ma).  The
initiation, as well as the continuous growth of ice on Antarc-
tica could have been the result of gradual global cooling cou-
pled  with  the  uplift  of  continental  areas  even  situated  away
from Antarctica.

Understanding the relationship between the Central Car-

pathian Paleogene Basin, Pieniny Klippen Belt and the Magu-

ra Nappe is important for establishing a better understanding
of the paleogegraphy and paleotectonic evolution of the Outer
Carpathians.  The  first  steps  in  this  direction  were  made  by
Książkiewicz  &  Leško  (1959),  who  correlated  Upper
Eocene—Oligocene  deposits  in  the  Pieniny  Klippen  Belt  to
the southern part of the Magura Nappe. This study was fol-
lowed  by  Leško  &  Samuel  (1968)  who  suggested  the  exist-
ence of a Late Eocene-Oligocene seaway connection between
the Magura and Central Carpathian Paleogene Basin via the
Pieniny Klippen Belt.

Stráník & Hanzlíková (1968) described several transition-

al facies (Ujak, Kremna, Lackovce and Inovce) between the
Central  Carpathian  Paleogene,  Pieniny  Klippen  Belt  and
Magura basins. Traditionally the Oligocene Malcov Forma-
tion  has  been  regarded  as  a  typical  transitional  facies  be-
tween  the  Magura,  Pieniny  Klippen  Belt  and  Central
Carpathian  Paleogene  basins.  In  Poland  the  best  exposures
of the Malcov Formation are known from the Leluchów sec-
tion  (Birkenmajer  &  Oszczypko  1989;  Oszczypko-Clowes
2001;  Oszczypko  et  al.  2005;  Oszczypko  &  Oszczypko-
Clowes 2010). This section, located along the Polish-Slovak
boundary,  is  directly  linked  with  the  Lubotin—Plaveč—Ujak
(Udol)  –  tectonic  depression,  which  is  filled  with  Upper
Eocene—Oligocene  deposits  of  the  Pieniny  Klippen  Belt
(Nemčok 1990). The Leluchów section records the transition
from  the  Magura  Formation,  a  typical  lithofacies  of  the
Magura Basin to the Malcov Formation – a typical lithofa-
cies of the Pieniny Klippen Belt and the Central Carpathian
Paleogene Basin.

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Previous work

Exposures of variegated marls, menilite-type shales and Kros-

no-type beds in Leluchów have been studied for a long time and
are  discussed  in  several  papers  (Książkiewicz  &  Leško  1959;
Świdziński 1961; Leško & Samuel 1968; Książkiewicz 1977).
The  first  detailed  description  of  these  beds  was  provided  by
Blaicher & Sikora (1967). In 1989 Birkenmajer & Oszczypko
described the Leluchów section as transitional from the Magura
Formation (Middle Eocene) to the Malcov Formation (Upper
Eocene—Oligocene) of the Ujak Succession. Thin-bedded flysch
and  red  shales  containing  Reticulophragmium  amlectens  were
attributed  to  the  Mniszek  Shale  Member.  At  the  same  time
variegated marls and menilite-type shales were included in the
Leluchów  Marl  Member  and  Smereczek  Shale  Member,  re-
spectively. In the lower part of the Leluchów Marl the domi-
nating  arenaceous  Middle/Late  Eocene  foraminifera  were
discussed by Malata in Oszczypko et al. (1990). Towards the
top  of  the  marls  the  amount  of  planktonic  foraminifera  in-
creases and is typical for the Globigerina Marls (Late Eocene—
Oligocene,  see  Malata  in  Oszczypko  et  al.  1990).  In  the
Smereczek Shale Member foraminifera were not found. High-
er up in the section (marly mudstones with sandstone interca-
lations) the foraminiferal assemblage is dominated by poorly
preserved planktonic foraminifera with admixtures of benthic
forms  and  reworked  older foraminifera  (Malata  op.cit.).  The
litho-  and  calcareous  nannoplankton  biostratigraphy  of  the
Malcov  Formation  in  the  Leluchów  sections  A  and  B  were
studied  by  Oszczypko-Clowes  (1996,  1998,  1999,  2001,  see

also Oszczypko et al. 2005; Oszczypko & Oszczypko-Clowes
2010). As a result the Leluchów Marl Member is assigned to
Zones NP19—20, 21 and 22, the Smereczek Shale Member to
Zone NP23, and the Malcov lithofacies to Zone NP24.

According to dinocyst studies, Gedl (1999, 2004) placed

the Eocene/Oligocene boundary in the upper part of the
Leluchów Marl Member.

Studied section

The Leluchów section (Krynica Zone) is situated on the

right bank of the Smereczek Stream, which is the right con-
fluence of the Poprad River (Figs. 1, 2) close to the Polish-
Slovak border (Fig. 2). The main section (A) of the Malcov
Formation is located along the creek near the tourist path,
close to the Greek-Catholic Church (Fig. 2) and the studied
section (B) is situated 500 m NE of the church (Fig. 2).

The lowest part of the Leluchów section crops out along the

Leluchów-Muszyna  road,  and  consists  of  south  dipping,  thick
bedded  (0.4—2.5 m)  muscovite  sandstones  and  conglomerates
of the Piwniczna Sandstone Member of the Magura Formation
(?Lower—Middle Eocene, see Birkenmajer & Oszczypko 1989;
Oszczypko  et  al.  1990;  Oszczypko  &  Oszczypko-Clowes
2010).  In  2001  the  uppermost  portion  of  the  Piwniczna  Sand-
stone  Member  was  drilled  in  hydrogeological  borehole  P-8,
200 m depth (Figs. 2, 3). The core material displays light grey
and dark grey, muscovite rich, thick-bedded sandstone and fine
conglomerates (Fig. 4) with layers (0.5—6 m thick) of grey, non-

Fig. 1. A – Simplified tectonic scheme of the Alpine-Carpathian orogens (based on Picha 1996). B – Geological map of the Polish
Carpathians (based on Żytko et al. 1989, modified), with location of studied areas.

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calcareous shales with intercalations of thin- to medium-bedded
sandstones. The sandstones are very hard (siliceous cement) and
fractured. The Piwniczna sandstone was also cored in 2009, in
borehole L-3 (Figs. 2, 4). In 2005, in borehole PG-1, ca. 100 m
south  of  borehole  P-8,  red  shales  were  pierced  at  a  depth  of
15.5—27.0 m,  and  more  recently  in  borehole  L-1  (Fig. 2,  see
also Nescieruk et al. 2010). The first time these red shales with
Reticulophragmium  amplectens  were  found  by  Blaicher  &
Sikora  (1967)  in  the  BS  excavation  (Fig. 2).  The  thin-bedded
flysch and red shales from Leluchów were regarded by Birken-
majer & Oszczypko (1989) and Oszczypko et al. (1990) as the
Mniszek  Shale  Member  of  the  Magura  Formation  (Middle
Eocene). The Magura Formation grades upwards into the Mal-
cov Formation. The Malcov Formation was divided by Birken-
majer & Oszczypko (1989) into three members: the Leluchów
Marl Member, Smereczek Shale Member, and Malcov lithofa-
cies. The exposures (A, B) of the Leluchów Marl Member, also
known as the Sub-Menilite Globigerina Marls, are at least 6.5 m
thick. The basal part (2.5 m thick) of the member is represented
by grey-greenish marls with numerous calcite veins, covered by
a 4 m thick unit of red and olive marls. The red marls contain
burrows  of  Planolites,  Chondrites  and  Thalassinoides  (see
Leszczyński 1997). Taking into account the results from bore-

hole  L-1  (Figs. 2,  3)  the  thickness  of  the  grey-greenish  marly
shales can be up to 45 meters. The Leluchów Marl Member is
covered  by  the  ca.  20 m  thick  Smereczek  Shale  Member,  a
dark,  bituminous,  non-calcareous,  menilite-like  shale  (see
Blaicher & Sikora 1967). The lower part of this member con-
tains thin intercalations of marly shales (sample 39/98/N), a
few  1—2 cm  thick  tuffite  intercalations,  and  a  thin  (2—5 cm)
intercalation  of  cherts  as  well  as  two  thin  intercalations  of
detrital  Bryozoa—Lithothamnium  limestones  (see  Oszczypko-
Clowes 2001; Oszczypko & Oszczypko-Clowes 2010). The
upper part of the member is developed as Menilite Shale with
black  non-calcareous,  bituminous  shales,  with  intercalations
of coarse-grained, thick-bedded sandstones. In this part of the
section,  thin  layers  of  marly  shales  were  recognized  (sample
38/98/N).  The  black  shales  are  covered  by  a  10 m  packet  of
coarse-grained, muscovite rich, thick-bedded sandstones of the
Magura type with intercalations of green marly claystones and
medium-bedded  sandstones  with  Tabc  Boumas  intervals
(Fig. 3).  The  uppermost,  flat-laying  part  of  the  section  con-
sists  of  the  Krosno-like  facies:  dark  grey  marly  shales  with
intercalations  of  thin-bedded,  cross-laminated  calcareous
sandstones  (Birkenmajer  &  Oszczypko  1989;  Oszczypko-
Clowes 2001; Oszczypko & Oszczypko-Clowes 2010).

Fig. 2. Geological map of Leluchów area (based on Oszczypko & Oszczypko-Clowes 2010, and Neścieruk et al. 2010).

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Methods

Sixteen samples were examined for calcareous nannofossil

content (Figs. 2, 3). Samples labelled as x/98/N were collected
and first published by Oszczypko-Clowes (1996, 1998,
1999, 2001), while samples labelled as x/82/N were obtained
from Ewa Malata. Additionally new samples from the Le-
luchów Marl Member (x/08/N) were collected.

All samples were prepared using standard smear slide tech-

niques for the light microscope (LM). The investigation was
carried out using Nikon – Eclipse E 600 POL, scope at a mag-
nification of 1000 using parallel and crossed nicols. Speci-
mens photographed using the LM are illustrated in Figs. 5—6.

The taxonomic frameworks of Perch-Nielsen (1985), Aubry

(1984, 1988, 1989, 1990, 1999) and Bown (1998 and refer-
ences  therein)  have  been  followed.  Quantitative  analyses
were performed by counting 300 specimens on each slide. In
order  to  analyse  and  calculate  the  percentage  abundance  of
autochthonous  and  allochthonous  assemblages  the  authors

accepted the 5 % range of error. The nominal values are pre-
sented in Table 1. The paleoecological analyses were per-
formed on autochthonous assemblages. Abundances were
calculated for individual species with an error range of 0 %
– the total amount of autochthonous species in each of the
slides is equal to 100 %. The nominal values as well as per-
centages are also presented in Table 1.

The biostratigraphic analyses, using the standard zonation

of Martini (1971) proved the results obtained through earlier
research (Oszczypko-Clowes 2001; Oszczypko et al. 2005),
and are summarized in Table 1. Additional samples (1/08/N—6/
08/N) from the Leluchów Marl Member were assigned to
Ericsonia subdisticha Zone (NP21). The zone assignment is
based on a continuous range of Ericsonia formosa, following
the disappearance of Discoaster saipanensis and Discoaster
barbadiensis.

The paleoecological analysis is based on quantitative results

and it takes into account three major factors (temperature, tro-
phism and salinity) controlling coccolithopores biogeography.

Fig. 3. Lithostratigraphic profile of the Leluchów Succession of the
Krynica Zone of the Magura Nappe, with samples (Oszczypko-
Clowes 2001; Oszczypko et al. 2005, supplemented).

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Each of these factors was analysed separately in the case of
nannnofossil autochthonous assemblages from Leluchów
section.

Calcareous nannofossils preservation

The most widely used method is a visual assessment of the

state of preservation of the assemblage based on the degree of
etching and/or calcite overgrowth observed during light- or
electron-microscopy (Roth & Thierstein 1972; Roth 1973;
Bown & Young 1998). For the purpose of this work the crite-
ria proposed by Roth & Thierstein (1972) were used namely:
VP – very poor, etching and mechanical damage is very inten-
sive, specimens mostly in fragments; P – poor, severe dissolu-
tion,

fragmentation

and/or

overgrowth;

the

specific

identification of specimens is difficult; M – moderate, etching
or mechanical damage is apparent but majority of specimens are
easily identifiable; G – good, little dissolution and/or over-
growth; diagnostic characteristics are preserved, the specimens
could be identified to species level without any “trouble”.

Species diversity and abundance

Estimates of the nannofossil abundance for individual sam-

ples (Table 1) was established using the following criteria: VH
– very high ( > 20 specimens per 1 field of view), H – (10—20
specimens per 1 field of view), M – moderate (5—10 speci-
mens per 1 field of view), L – low (1—5 specimens per 1 field
of view), VL – very low ( < 5 specimens per 5 fields of view).

Results

The preservation of calcareous nannofossils is moderate

(m) or predominantly moderate to good (m—g) in all investi-
gated samples (Table 1). Nannofossils show minor etching

and minor to moderate overgrowth. Good and moderate
preservation of nannofossils indicates that little carbonate
dissolution has occurred in these sediments.

During quantitative analyses of the calcareous nanno-

plankton  assemblages,  44  species  were  identified.  The  per-
centage of autochthonous and reworked species in individual
samples  was  calculated  (Fig. 7).  To  distinguish  reworked
from  in-place  nannofossil,  the  biostratigraphical  range  of
species, was used.

The most common autochthonous species are: Coccolithus

pelagicus, Cyclicargolithus floridanus, Dictyococcites bisec-
tus, Dictyococcites sp., Sphenolithus moriformis and
Zygrhablithus bijugatus.

Other autochthonous species, which occur irregularly in

the samples are: Braarudosphaera bigelowii, Discoaster de-
flandrei,  Helicosphaera  bramlettei,  Helicosphaera  compac-
ta,  Pontosphaera  multipora,  Transversopontis  pulcher,
Transversopontis  pulcheroides,  Sphenolithus  predistentus
and Sphenolithus radians (see Table 1).

The highest numbers of reworked species (13.3 %—

31.35 %; Fig. 7) were observed in samples taken from thin-
marly intercalations in the Smereczek Shale Member (39/98/N
and 38/98/N) and Malcov lithofacies (37/98/N, 42/98/N,
41/98/N and 40/98/N). Samples from the Leluchów Marl
Member are characterized by a very low level of reworking,
which does not exceed 3.80 %, (sample 3/08/N).

The percentage of reworked species is clearly associated

with lithology (Fig. 7). The lowest number (0 %—3.80 %) of
reworked species was recorded in samples from the marly fa-
cies of the Leluchów Marl Member. Turbidite facies of the
Malcov lithofacies are characterized by increased reworking,
reaching 31.35 % in sample 40/98/N, located in the upper-
most part of the studied section.

Allochthonous specimens include (samples: 40/98/N, 41/

98/N, 42/98/N, 37/98/N, 38/98/N, 39/98/N) Chiasmolithus
medius, Discoaster barbadiensis, Discoaster lodoensis, Dis-

Fig. 7. Percentage abundance of autochthonous and allochthonous (reworked)
species in samples of the Leluchów Marl Member and Malcov lithofacies,
Leluchów, section A.

coaster  saipanensis,  Dis-
coaster  sp.,  Discoaster
tani, Discoaster tani nodi-
fer,  Ericsonia  formosa,
Isthmolithus

recurvus,

Neococcolithes

dubius,

Reticulofenestra dictyoda,
Reticulofenestra

hillae,

Reticulofenestra reticula-
ta, Reticulofenestra um-
bilica

and

undivided

Cretaceous species.

The quantitative analy-

ses  of  autochthonous  as-
semblages  from  section  A
allowed the authors to ob-
serve  a  constant  decrease
in the diversity of species.
The sequence of extinction
is  as  follows:  Discoaster
barbadiensis  and  Disco-
aster  saipanensis  (Zone
NP19—20),  Ericsonia  for-

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mosa  (Zone  NP21),  Chiasmolithus  oamaruensis,  Discoaster
tanii, Discoaster tanii nodifer, Isthmolithus recurvus, Reticu-
lofenestra dictyoda, Reticulofenestra umbilica, Reticulofenes-
tra hillae, Reticulofenestra reticulata (Zone NP22), Ericsonia
fenestrata,  Ericsonia  subdisticha  and  Lanternithus  minutus
(Zone NP23). At the same time the first evolutionary appear-
ance  takes  place  in  the Zone  NP23  (Reticulofenestra ornata,
Reticulofenestra lockerii and Transversopontis fibula)  and  in
the Zone NP24 – Cyclicargolithus abisectus.

Paleoecology

Temperature. Temperature is one of the most important

factors determining the nannofossil distribution in sedimen-
tary basins. Wei & Wise (1990) grouped Paleogene calcare-
ous nannofossils according to their temperature preferences.
In addition this work takes into account more recent papers
studying Paleogene calcareous nannofossil paleoecology in
areas of the Southern Ocean (e.g. Wei et al. 1992; Bralower
2002; Persico & Villa 2004; Villa & Persico 2006; Villa et
al. 2008) and mid-latitude oceans (Agnini et al. 2006; Gibbs
et al. 2006). Taking into account the results of Wei & Wise

flandrei,  Discoaster  saipanensis,  Dicoaster  tanii,  Discoaster
tanii  nodifer,  Ericsonia  formosa,  Helicosphaera  compacta
and Sphenolithus moriformis (see Wei & Wise 1990; Villa et
al.  2008)  which  are  present,  but  never  abundant.  The  warm-
water  species  constitute  less  than  9 %  of  the  association
(Fig. 9;  Table 2).  Most  of  these  species  last  occurred  during
the latest Eocene and earliest Oligocene. The highest number
of  warm-water  species  was  observed  in  sample  1/08/N
(Figs. 3, 9; Table 2).

Sample 6/08/N is characterized by an increase in the per-

centage  of  cold-water  taxa  (a  26.88 %  increase  when  com-
pared to sample 3/08/N), and a drop in temperate water taxa
by 23.63 %. This change is mostly due to a decrease in per-
cent  abundance  of  Coccolithus  pelagicus  (from  26 %  to
11.53 %) and Dictyococcites bisectus (from 29 % to 9.15 %)
(Fig. 9;  Table 2).  The  cooling  trend  is  apparent  in  sample
6/08/N,  which  has  an  increased  abundance  of  Lanternithus
minutus (30.85 %). Additionally sample 6/08/N is character-
ized by the lowest percentage of warm-water taxa in this sec-
tion and does not exceed 2.03 % (Fig. 9; Table 2).

The Early- and Middle Oligocene assemblages are again

dominated by temperate water species. Starting with sample

(1990 and references therein) and Villa et al.
(2008 and references therein), it is possible
to differentiate three main temperature
based, ecological groups:

1. Typical warm-water species are: all spe-

cies from the genera Discoaster, Heli-
cosphaera, Sphenolithus and Ericsonia
formosa.

2. Temperate-water species are Cyclicar-

golithus floridanus, Cyclicargolithus abisec-
tus, Dictyococcites bisectus, Dictyococcites
scrippsae and Reticulofenestra umbilica.

3. Cold-water species include Chiasmo-

lithus,  Ericsonia  fenestrata,  Ericsonia  sub-
disticha, Isthmolithus recurvus, Lanternithus
minutus,  Reticulofenestra  daviesii,  Reticu-
lofenestra  callida,  Reticulofenestra  clatrata,
Reticulofenestra  lockerii  and  Reticulofenes-
tra ornata.

And finally there is a group of nannofos-

sils,  whose  biogeography  do  not  depend  on
geographical  latitude:  all  species  belonging
to  genera  Blackites  and  Rhabdosphaera,  as
well  as  Reticulofenestra  reticulata  and
Zygrhablithus bijugatus.

In the Leluchów section the Late Eocene as-

semblages (Zones NP19—20 and NP21) (Fig. 8,
Table 1) are dominated by Coccolithus pelagi-
cus,  Dictyococcites  bisectus,  Cyclicargolithus
floridanus, Reticulofenestra umbilica and Eric-
sonia formosa. All of these species, except for
Ericsonia  formosa,  prefer  temperate-water
temperatures  (Wei  &  Wise  1990;  Villa  et  al.
2008).  The  percent  abundance  of  temperate
water  species  varies  from  82 %  up  to  88 %
(Fig. 9;  Table 2).  The  only  warm-water  taxa
are  Discoaster  barbadiensis,  Discoaster  de-

Fig. 8. Percent abundance of the four most numerous autochthonous species,
Leluchów, section A.

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54/82/N there is a constant growth in the content of temper-
ate  water  species.  A  drop  in  cold-water  species  is  always
compensated  by  an  increase  in  temperate  water  species,
which is especially clearly visible in samples 3/08/N, 5/08/N,
53/82/N  and  41/98/N  (Fig. 9;  Table 2).  The  amount  of
warm-water  taxa  is  low  and  constitutes  no  more  than  9 %
(sample  42/98/N),  though  it  does  show  a  growing  trend
(Fig. 9; Table 2). The youngest assemblage (sample 40/98/N)
is characterized by the lowest possible content of cold-water
species (0 %) and the highest content of temperate water spe-
cies (92.54 %) (Fig. 9; Table 2).

Trophic resources. Although, temperature has always

been  regarded  as  a  prime  factor  in  controlling  the  distribu-
tion  of  calcareous  nannofossils,  trophic  resources  can  also
play a major role in the distribution and abundance pattern of
Paleogene  coccolithopore  (Aubry  1992;  Krhovský  et  al.
1992; Villa et al. 2008). The fluctuation in nutrient availabil-
ity during the Paleogene was delineated through observation
of  the  relationship  between  planktonic  and  large  benthic
foraminiferal  assemblages  and  oceanic  paleochemistry
(Boresma  et  al.  1987;  Hallock  et  al.  1991).  According  to
these authors during the Early Eocene oligotrophy in euphotic
waters expanded in open oceans and marginal seas. This was
followed  by  increasing  eutrophication  and  a  loss  of  oligo-
trophic  habitats  during  the  Middle  and  Late  Eocene,  result-

Table 2:

Percent

abundance

main

paleoecological

groups.

Fig. 9. Percent abundance of taxa with different temperature prefer-
ences, Leluchów, section A.

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GEOLOGICA CARPATHICA, 2012, 63, 2, 149—164

Fig. 10. Percent abundance of taxa with different trophic prefer-
ence, Leluchów, section A.

ing in a maximum concentration of the trophic resources
continuum (TRC, Hallock 1987) in the Early Oligocene.

In the Late Eocene—Oligocene, calcareous nannoplankton

assemblages  preferring  an  eutrophic  environment  were  rep-
resented  by  Braarudosphaera  bigelowii,  Chiasmolithus
oamaruensis, Chiasmolithus sp., Cyclicargolithus abisectus,
Cyclicargolithus floridanus, Dictyococcites bisectus, Dictyo-
coccites sp., Lanternithus minutus, Pontosphaera multipora,
Reticulofenestra  ornata,  Transversopontis  fibula,  Transver-
sopontis  pulcher,  Transversopontis  pulcheroides,  Zygrha-
blithus  bijugatus  (Aubry  1992;  Krhovský  et  al.  1992;  Villa
et al. 2008).

All autochthonous species were classified either as oligo-

trophic, eutrophic or “other”. The later group is composed of
mesotrophic species or taxa whose nutrient level preferences
are not yet known. As the percent abundance of these group
is very low (on average no more than 6—7 %) it can be ex-
cluded from the analyses.

A major change in the composition of nannoplankton as-

semblages, involving a shift in dominance from oligotrophic
to eutrophic genera, occurred in the Late Eocene and Early
Oligocene (from 27.87 % in the sample 48/82/N to 70.93 %
of the sample 54/82/N) (Fig. 10; Table 2).

Fig. 11. Percentage abundance of taxa with different salinity prefer-
ence, Leluchów, section A.

Only in the case of sample 4/08/N is the amount of

eutrophic and oligotrophic species almost similar (respective-
ly 46.28 % and 47.64%) (Fig. 10; Table 2). The highest
amount of eutrophic species (81.36 %) was observed in sam-
ple 6/08/N. From this position there is a visible increase of
nearly 25 % of oligotrophic species (Fig. 10; Table 2), though
the assemblage is still dominated by eutrophic species.

Salinity. Taking into account the salinity preferences of cer-

tain species, Nagymarosy & Voronina (1992) distinguished
the endemic nannofossil assemblage, which is characterized
by the presence of Reticulofenestra ornata, Transversopontis
fibula and Transversopontis latus. The above mentioned asso-
ciation is strictly characteristic for Zone NP23 for the brack-
ish-water environments and limited to the Paratethys only.

Both Reticulofenestra ornata and Transversopontis fibula

occur for the first time in sample 39/82/N and they constitute
9 % of the total autochthonous assemblage (Fig. 11; Table 2).
Transversopontis  fibula  is  very  rare  and  does  not  exceed
0.5 %. The occurrence of Reticulofenestra ornata varies from
8.63 % in sample 39/82/N to 3.04 % in sample 37/82/N, it is
absent from sample 40/98/N (Fig. 11; Table 2). All the other
samples  contain  nannofossil  assemblages  indicative  of  open
ocean conditions and are characterized by the presence of Dic-
tyococcites  bisectus,  Coccolithus  pelagicus,  Cyclicargolithus
floridanus,  Ponthosphaera  multipora,  Sphenolithus  morifor-
mis, Isthmolithus recurvus, Zygrhablithus bijugatus, Lanterni-
thus minutus (see also Nagymarosy & Voronina 1992).

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Discussion

During the Late Eocene through Early Oligocene, drastic

changes in paleogeography and paleoecology also took place
in  Southern  Europe.  This  was  connected  with  the  transfor-
mation  of  the  Western  Tethys  into  the  Central  Paratethys.
This  transformation  was  initiated  in  the  nannoplankton
Zones  NP21/22  and  resulted  in  long  lasting  anoxic  bottom
conditions and the deposition of black shales (see Schulz et
al.  2005).  In  the  Carpathian  sedimentary  area,  this  was  re-
corded  by  the  replacement  of  pelagic  Globigerina  Marls
with  menilite  bituminous  shales.  These  paleoenviromental
changes  took  place  mainly  in  the  northern  external  part  of
the  Carpathian  Flysch  Basin  (Skole,  Sub-Silesian/Silesian

and Dukla sub-basins) and are collectively known as the Ter-
minal Eocene Event (Van Couvering et al. 1981; Švábenická
et  al.  2007).  To  a  lesser  extent  these  changes  took  place  in
the  Transylvanian  and  Central  Carpathian  Paleogene  basins
(Soták  et  al.  2001;  Soták  2010),  and  to  a  very  small  extent
also in the Magura Basin (Oszczypko-Clowes 1998, 2001).

The Late Eocene-Oligocene assemblages of calcareous

nannoplankton from the Leluchów section are highly domi-
nated by temperate water species. The number of warm-wa-
ter taxa starts to decrease at the beginning of Zone NP21 (the
latest Eocene) and this is accompanied by an increase in
cold-water taxa (Fig. 12). The uppermost part of Zone NP21
is characterized by a maximum of cold-water taxa and this is
accompanied by the lowest content of temperate water taxa.

Fig. 12. Geological profile, paleo-
bathymetry and main paleoecological
changes, Leluchów, section A.

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The  same  sample  has  the  highest  level  of  eutrophic  species
and  the  lowest  amount  of  oligotrophic  species.  This  event
can most likely be correlated with the Oi-1 event, which in
the  Leluchów  embayment  of  the  Magura  Basin  reflects  a
progressive eutrophication rather than a cooling of sea water.
In a well-stratified water column, nannoplankton are typical-
ly  diverse  (e.g.  Hallock  1987).  In  a  less  well-mixed  water
column,  nannoplankton  diversity  is  lower,  and  mesotrophic
or more opportunist, eutrophic taxa are dominant.

Increased nutrient concentration was a prime factor con-

trolling the biogeographic distribution of calcareous nanno-
plankton (Fig. 12), and the extinction of species in the Early
Oligocene Malcov embayments in the Magura Basin (see
Oszczypko & Oszczypko-Clowes 2009).

The increase of nutrients within the uppermost part of the

Leluchów Marl Member and Smereczek Shale Member were
confirmed by Gedl (2004) on the basis of analysis of dinocysts.

The presence of Reticulofenestra ornata and Transversopon-

tis fibula in the assemblages from the Smereczek Shale Member
in the Leluchów section reflects the freshwater run-off and in-
flow  of  freshwater  carrying  a  large  amount  of  organic  matter.
However, organic material is not so prominent as what was re-
corded  in  the  Ždánice-Pouzdřany  Unit  –  Chert  Member  and
Dynów  Marl  of  the  Menilite  Formation  (Krhovský  1981a,b;
Krhovský  et  al.  1992;  Krhovský  &  Djurasinovič  1993;  Švá-
benická et al. 2007), Central Carpathian Paleogene Basin (Soták
2010) as well as in NW Transylvania – bituminous marls and
shales  of  the  Bizu a  and  Ileanda  units  and  bituminous  cherts,
marls  and  shales  of  the  Menilite  and  Lower  Dysodile  forma-
tions (Melinte 2005; Melinte-Dobrinescu & Brustur 2008).

According to Nagymarosy & Voronina (1992) Reticulofenes-

tra ornata and Transversopontis fibula are characteristic of
brackish-water environments and are limited to Paratethys only.
The presence of this assemblage is characteristic for the upper
part of Zone NP23. This event is associated with the complete
isolation of the Paratethys (Báldi 1980; Rusu 1988; Rögl 1998)
suggesting that the southern part of the Magura Basin was only
partially isolated from the Mediterranean realm at this time.

The Malcov lithofacies represents the nannofosil Zone

NP24.  This  sand-rich  deposition  of  lithofacies  was  induced
with  the  mid-Oligocene  glacio-eustatic  regression  (see  Soták
2010).  The  Malcov  lithofacies,  of  the  uppermost  part  of  the
Leluchów  section,  (sample  40/98/N)  is  characterized  by  the
disappearance  of  the  last  cold-water  taxa,  a  growth  in  abun-
dance  of  warm-water  taxa  and  an  increased  amount  of  re-
worked species. This could suggest the beginning of a warming
episode in the Late Oligocene (Chattian). This episode can be
traced  through  the  Carpathians  in  the  Czech  Republic
(Krhovský  1981a,b;  Krhovský  et  al.  1992;  Krhovský  &
Djurasinovič 1993; Švábenická et al. 2007), Poland (Oszczyp-
ko-Clowes 2001; Oszczypko & Oszczypko-Clowes 2009) and
finally  in  Romania  (Melinte  2005;  Melinte-Dobrinescu  &
Brustur  2008).  The  Malcov  lithofacies  represents  a  broader
connection in the southern part of the Magura Basin with post-
nappe Pieniny Klippen Belt and Central Carpathian Paleogene
basins (Soták et al. 2001; Soták 2010). In the Magura Basin,
as  a  result  of  the  Illyrian  vertical  movement  (see  Leško  &
Samuel  1968),  the  Malcov  lithofacies  locally  overlapped
Magura-type sandstones with an angular unconformity.

Conclusion

1. The short Leluchów section records transitional Late

Eocene-Oligocene facies between the forearc CCP Basin lo-
cated on the upper plate, the partly sub-merged Pieniny Klippen
Belt suture zone, and the Magura Basin, as the inner part of the
foreland-basin on the descending slab of the European Plate.

2. The surface-water regimes of Early Oligocene Magura

Basin is characterized by eutrophic populations preferring
high-nutrient levels and well-mixed surface waters.

3. The nannofossil assemblages are highly dominated by

temperate water and eutrophic species, which is evidence for
progressive eutrophication rather than a cooling of sea water.

4. The endemic Paratethyan species suggesting the fresh-

water inflow were observed in samples from the Smereczek
Shale Member.

5. During the deposition of the Leluchów Marls the activity

of turbiditic currents drastically decreases. That is manifested in
an extremely low number of reworked nannoplakton species.

Acknowledgments:  The  author  wishes  to  thank  Jean  Self-
Trail for her constructive criticism and detailed review of the
manuscript.  Barbara  Olszewska,  András  Nagymarosy  and
Silvia Ozdinová are gratefully acknowledged for their valu-
able  comments  on  the  manuscript.  The  author  would  also
like  to  thank  Lilian  Švábenická  who  was  a  handling  editor
for the manuscript.

References

Agnini C., Fornaciari E., Rio D., Tateo F., Backman J. & Giusberti L.

2006: Responses of calcareous nannofossil assemblages, mineral-
ogy and geochemistry to the environmental perturbations across
the Paleocene/Eocene boundary in the Venetian Pre-Alps. Mar.
Micropaleont. 63, 19—38.

Aubry M.-P. 1984: Handbook of Cenozoic calcareous nannoplankton.

Book 1. Ortholithae (Discoasters). Micropaleontology Press,
Amer. Mus. Natur. Hist., New York, 1—265.

Aubry M.-P. 1988: Handbook of Cenozoic calcareous nannoplankton.

Book 2. Ortholithae (holochoccoliths, ceratoliths and others).
Micropaleontology Press, Amer. Mus. Natur. Hist., New York,
1—279.

Aubry M.-P. 1989: Handbook of Cenozoic calcareous nannoplankton.

Book 3. Ortholithae (pentaliths, and others) Heliolithae (fascicu-
liths, sphenoliths and others). Micropaleontology Press, Amer.
Mus. Natur. Hist., New York, 1—279.

Aubry M.-P. 1990: Handbook of Cenozoic calcareous nannoplankton.

Book 4: Heliolithae (helicoliths, cribriliths, lopadoliths and oth-
ers). Micropaleontology Press, Amer. Mus. Natur. Hist., New
York, 1—381.

Aubry M.P. 1992: Late Paleogene calcareous nannoplankton evolution:

a tale of climatic deterioration. In: Prothero D.R. & Berggren
W.A. (Eds.): Eocene-Oligocene climatic and biotic evolution.
Princeton Univ. Press, 272–309.

Aubry M.-P. 1999: Handbook of Cenozoic calcareous nannoplankton.

Book 5. Heliolithae (Zygolithus and Rhabdolithus). Micropaleon-
tology Press, Amer. Mus. Natur. Hist., New York, 1—367.

Báldi T. 1980: The early history of the Paratethys. Földt. Közl., Bull.

Hung. Geol. Soc. 110, 456—472 (in Hungarian with English re-
sume).

Birkenmajer K. & Oszczypko N. 1989: Cretaceous and Paleogene

lithostratigraphic units of the Magura Nappe, Krynica Subunit,
Carpathians. Ann. Soc. Geol. Pol. 59, 145—181.

163

UPPER EOCENE—LOWER OLIGOCENE PALEOECOLOGY OF THE CALCAREOUS NANNOFOSSILS (CARPATHIANS)

GEOLOGICA CARPATHICA

GEOLOGICA CARPATHICA, 2012, 63, 2, 149—164

Blaicher J. & Sikora W. 1967: Stratigraphy of the Richvald Unit in Le-

luchów. Kwart. Geol. 11, 4, 453—454 (in Polish).

Bohaty S.M. & Zachos J.C. 2003: A significant Southern Ocean warming

event in the late middle Eocene. Geology 31, 1017—1020.

Boresma A., Premoli-Silva I. & Shackleton N.J. 1987: Atlantic Eocene

planktonic foraminiferal paleohydrographic indicators and stable
isotope paleoceanography. Paleoceanography 2, 287—331.

Bralower T.J. 2002: Evidence of surface water oligotrophy during the

Paleocene—Eocene thermal maximum: nannofossil assemblage
data from Ocean Drilling Program Site 690, Maud Rise, Weddel
Sea. Paleoceanography 17, 13.1—13.13.

Bown P.R. (Ed.) 1999: Calcareous nannofossil biostratigraphy. British

Micropalaeontological Society Series. Kluwer Academic Publ.,
Cambridge, 1—315.

Coxall H.K., Wilson P.A., Pälike H., Lear C.H. & Backman J. 2005:

Rapid stepwise onset of Antarctic glaciation and deeper calcite
compensation in the Pacific Ocean. Nature 433, 53—57.

Gedl P. 1999: Palynological record of the Eocene-Oligocene flysch of

the Polish Carpathians – preliminary results. Przegl. Geol. 47,
4, 394—398 (in Polish).

Gedl P. 2004: Dinoflagellate cyst record of the Eocene—Oligocene

boundary succession in flysch deposits at Leluchów, Carpathian
Mountains, Poland. In: Head M.J. (Ed.): The palynology and mi-
cropalaeontology of boundaries. Geol. Soc. London, 309-325.

Gibbs S.J., Bralower T.J., Bown P.R., Zachos J.C. & Bybell L.M. 2006:

Shelf and open-ocean calcareous phytoplankton assemblages
across the Paleocene—Eocene thermal maximum: implications for
global productivity gradients. Geology 34, 233—236.

Hallock P. 1987: Fluctuation in the trophic resource continuum: A fac-

tor in global diversity cycles? Paleoceanography 2, 457—471.

Hallock P., Premoli-Silva I. & Boresma A. 1991: Similarities between

planktonic and large foraminiferal evolutionary trends through Pa-
leogene paleoceanographic changes. Palaeogeogr. Palaeoclima-
tol. Palaeoecol. 83, 49—64.

Jovane L., Florindo F., Coccioni R., Dinares-Turell J., Marsili A., Mone-

chi S., Roberts A.P. & Sprovieri M. 2007: The middle Eocene cli-
matic optimum event in the Contessa Highway section, Umbrian
Apennines, Italy. Geol. Soc. Amer. Bull. 119, 3, 413—427.

Krhovský J. 1981a: Stratigraphy and paleoecology of the Menilitic

Formation of the Ždánice Unit and the diatomites of the
Pouzdřany Unit (the Western Carpathians, Czechoslovakia).
Zemní Plyn Nafta 26, 1, 45—62 (in Czech).

Krhovský J. 1981b: Microbiostratigraphic correlations in the Outer

Flysch Units of the southern Moravia and influence of the eustasy
on their palaeogeographical development. Zemní Plyn Nafta 26, 4,
665—688, 955—975.

Krhovský J. & Djurasinović M. 1993: The nannofossil chalk layers in

the Early Oligocene Stibořice Member in Velké Němčice (the Me-
nilitic Formation, Ždánice Unit, South Moravia): orbitally forced
changes in paleoproductivity. Knihovnička ZPN 15, 3—53.

Krhovský J., Adamová J., Hladíková J. & Maslowská H. 1992: Pale-

oenviromental changes across the Eocene/Oligocene boundary in
the Ždánice and Pouzdřany Units (Western Carpathians, Tchecho-
slovakia): The long-term trend and orbitally forced changes in cal-
carous nannofossil assemblages. In: Hamršmid B. & Young J.
(Eds.): Nannoplankton research. Proc. Fourth INA Conf., Prague
1991, 2, 105—187.

Książkiewicz M. 1977: The tectonics of the Carpathians. In: Pożryski

W. (Ed.): Geology of Poland tectonics (v. IV). Wydaw. Geol.,
476—669.

Książkiewicz M. & Leško B. 1959: On the relation between the Krosno

and Magura Flysch. Bull. Acad. Pol. Sci. Sér. SC. Chim. Géol.
Géogr., Vol. 7, No. 10.

Leško B. & Samuel O. 1968: The geology of the East Slovakian Flysch.

SAV, Bratislava, 1—245 (in Slovak with English summary).

Leszczyński S. 1997: Origin of the sub-menilite Globigerina marl

(Eocene—Oligocene transition) in the Polish Outer Carpathians.
Ann. Soc. Geol. Pol. 67, 4, 367—427.

Melinte M.C. 2005: Oligocene palaeoenvironmental changes in the

Romanian Carpathians, revealed by calcareous nannofossils. In:
Tyszka J., Oliwkiewicz-Miklasinska M., Gedl P. & Kaminski M.
(Eds.): Methods and applications in micropalaeontology. Stud.
Geol. Pol. 124, 341—352.

Melinte-Dobrinescu M. & Brustur T. 2008: Oligocene—Lower Miocene

events in Romania. Acta Palaeont. Romaniae 6, 203—215.

Miller K.G., Fairbanks R.G. & Mountain G.S. 1987: Tertiary oxygen

isotope synthesis, sea-level history and continental margin ero-
sion. Paleoceanography 2, 1—19.

Miller K.G., Wright J.D. & Fairbanks R.G. 1991: Unlocking the ice

house: Oligocene—Miocene oxygen isotopes, eustasy, and margin
erosion. J. Geophys. Res. 96, 6829—6848.

Miller K.G., Wright J.D., Katz M.E., Wade B.S., Browning J.V.,

Cramer B.S. & Rosenthal Y. 2009: Climate threshold at the
Eocene-Oligocene transition: Antarctic ice sheet influence on
ocean circulation. In: Koeberl C. & Montanari A. (Eds.): The Late
Eocene Earth-hothouse, icehouse, and impacts. Geol. Soc. Amer.,
Spec. Pap., 169—178.

Nagymarosy A. & Voronina A. 1992: Calcareous nannoplankton from

the Lower Maykopian beds (early Oligocene, Union of Indepen-
dent States). In: Hamršmid B. & Young J. (Eds.): Nannoplankton
research. Proc. Fourth INA Conf., Prague 1991, 187—221.

Nemčok J. 1990: Geological Map of Pieniny, ubovnianska vrchovina

Highland and Čergov Mts. Geol. Ústav D. Štúra, Bratislava.

Nescieruk P., Oszczypko-Clowes M., Wójcik A. & Oszczypko N.

2010: On the relationship between the Paleogene Magura Basin
and Pieniny Klippen Belt sedimentary area-the Leluchów sections,
a new approches (Polish Outer Carpathians). In: Chatzipetros A.,
Melfos V., Marchev P. & Lakova I. (Eds.): XIX Congress of the
Carpathian-Balkan Geological Association, Thessaloniki, Greece,
23—26 September 2010. Geol. Balcanica 39, 1—2, 272—273.

Oszczypko (Clowes) M. 1996: Calcareous nannoplankton of the Globi-

gerina Marls (Leluchów Marls Member), Magura Nappe, West
Carpathians. Ann. Soc. Geol. Pol. 66, 1—15.

Oszczypko-Clowes M. 1998: Late Eocene—Early Oligocene calcareous

nannoplankton and stable isotopes (

O) of the Globigerina

Marls in the Magura Nappe (West Carpathians). Slovak Geol.
Mag. 4, 2, 95—107.

Oszczypko-Clowes M. 1999: The Late Eocene to Early Miocene nan-

noplankton stratigraphy of the Magura Nappe (Western Car-
pathians, Poland). Geol. Carpathica, Spec. Issue 50, 59—62.

Oszczypko-Clowes M. 2001: The nannofossil biostratigraphy of the

youngest deposits of the Magura Nappe (east of the Skawa
River, Polish Flysch Carpathians) and their palaeoenviromental
conditios. Ann. Soc. Geol. Pol. 71, 139—188.

Oszczypko N. & Oszczypko-Clowes M. 2009: Stages in the Magura

Basin: a case study of the Polish sector (Western Carpathians).
Geodinamica Acta 22, 1—3, 83—100.

Oszczypko N. & Oszczypko-Clowes M. 2010: The Paleogene and Early

Neogene stratigraphy of the Beskid Sądecki Range and

ubovnianska vrchovina (Magura Nappe, Western Carpathians).

Acta Geol. Pol. 60, 317—348.

Oszczypko N., Dudziak J. & Malata E. 1990: Stratigraphy of the Creta-

ceous through Palaeogene deposits of the Magura Nappe in the
Beskid Sądecki Range, Polish Outer Carpathians. Stud. Geol.
Pol. 97, 109—181 (in Polish).

Oszczypko N., Oszczypko-Clowes M., Golonka J. & Marko F. 2005:

Oligocene—Lower Miocene sequences of the Pieniny Klippen Belt
and adjacent Magura Nappe between Jarabina and the Poprad
River (East Slovakia and South Poland) – their tectonic position
and paleogeographic implications. Geol. Quart. 49, 4, 379—402.

Pekar S.F., DeConto R.M. & Haarwood D.M. 2006: Resolving a late

Oligocene conundrum: deep-sea warming and Antarctic glacia-
tion. Palaeogeogr. Palaeoclimatol. Palaeoecol. 231, 29—40.

Perch-Nielsen K. 1985: Cenozoic calcareous nannofossils. In: Bolli

H.M., Saunders J.B. & Perch-Nielsen K. (Eds.): Plankton stratig-
raphy. Cambridge Univ. Press, 427—554.

164

OSZCZYPKO-CLOWES and ŻYDEK

GEOLOGICA CARPATHICA

GEOLOGICA CARPATHICA, 2012, 63, 2, 149—164

Persico D. & Villa G. 2004: Eocene—Oligocene calcareous nannofossils

from Maud Rise and Kerguelen Plateau (Antarctica): paleoecolog-
ical and paleoceanographic implications. Mar. Micropaleont. 52,
153—179.

Picha F. 1996: Exploring for hydrocarbons under thrust belts – A chal-

lenging new frontier in the Carpathians and elsewhere. AAPG
Bull. 80, 10, 1547—1564.

Roth P.H. & Thierstein H. 1972: Calcareous nannoplankton: leg 14 of

the Deep Sea Drilling Project. In: Hayes D.E., Pimm A.C. et al.
(Eds.): Initials Reports DSDP. Vol. 14, 421—485.

Rögl F. 1998: Palaeogeographic consideration for Mediterranean and

Paratethys seaways (Oligocene to Miocene). Ann. Naturhist. Mus.
Wien 99A, 279—310.

Rusu A. 1988: Oligocene events in Transylvania (Romania) and the

first separation of Paratethys. D.S. Inst. Geol. Geofiz. 72—73
(1985, 1986), 5, 207—223.

Schulz H.M., Bechtel A. & Sachsendorfer R.F. 2005: The birth of the

Paratethys during the Early Oligocene: From Tethys to an ancient
Black Sea analogue? Glob. Planet. Change 49, 163—176.

Soták J. 2010: Paleoenvironmental changes across the Eocene-Oli-

gocene boundary: insights from the Central-Carpathian Paleogene
Basin. Geol. Carpathica 61, 5, 393—418.

Soták J., Pereszlényi M., Marschalko R., Milička J. & Starek D. 2001:

Sedimentology and hydrocarbon habitat of the submarine fan de-
posits of the Central Carpathian Paleogene Basin (NE Slovakia).
Mar. Petrol. Geol. 18, 87—114.

Stráník Z. & Hanzlíková E. 1968: Stratigraphy of the Magura Group of

nappes. In: Mahe M. & Buday T. (Eds.): Regional geology of
Czechoslovakia. Part II. The West Carpathians. Academia, Praha,
446—480.

Švábenická L., Bubík M. & Stráník Z. 2007: Biostratigraphy and paleo-

environmental changes on the transition from the Menilite to
Krosno lithofacies (Western Carpathians, Czech Republic). Geol.
Carpathica 58, 3, 237—262.

Świdziński H. 1961: Observations géologiques faites dans les enirons

de Leluchów, de Plaveč sur le Poprad et d’Ujak (Karpates polono-
slovaques). Bull. Acad. Pol. Sci. 9, 2.

Van Couvering J.A., Aubry M.-P., Berggren W.A., Bujak C.W.,

Naeser C.W. & Wieser T. 1981: The terminal Eocene event and
the Polish connection. Palaeogeogr. Palaeoclimatol. Palaeoecol.
36, 321—362.

Villa G. & Persico D. 2006: Late Oligocene climatic changes: evidence

from calcareous nannofossils at Kerguelen Plateau Site 748
(Southern Ocean). Palaeogeogr. Palaeoclimatol. Palaeoecol. 231,
110—119.

Villa G., Fioroni C., Pea L., Bohaty S. & Persico D. 2008: Middle

Eocene—late Oligocene climate variability: Calcareous nannofossil
response at Kerguelen Plateau, Site 748. Mar. Micropaleont. 69,
173—192.

Wei W. & Wise S.W. Jr. 1990: Biogeographic gradients of Middle

Eocene-Oligocene calcareous nannoplankton in the South Atlantic
Ocean. Palaeogeogr. Palaeoclimatol. Palaeoecol. 79, 29—61.

Wei W., Villa G. & Wise S.W. Jr. 1992: Paleoceanographic implica-

tions of Eocene—Oligocene calcareous nannofossils from Sites 711
and 748 in the Indian Ocean. In: Wise S.W. Jr. & Schlich R.
(Eds.): Proc. ODP. Sci. Results, 979—999.

Zachos J.C., Quinn T.M. & Salamy K.A. 1996: High-resolution (104

years) deep sea foraminiferal stable isotope records of the Eocene—
Oligocene climate transition. Paleoceanography 11, 251—256.

Zachos J.C., Pagani M., Sloan L., Thomas E. & Billups K. 2001:

Trends, rhythms, and aberrations in global climate 65 Ma to
Present. Science 292, 686—693.

Żytko K., Gucik S., Ryłko W., Oszczypko N., Zając R., Garlicka I.,

Nemčok J., Eliás M., Menčík E. & Stráník Z. 1989: Map of the
tectonic elements of the Western Outer Carpathians and their
Foreland. In: Poprawa D. & Nemčok J. (Eds.): Geological Atlas of
the Western Outer Carpathians and their Foreland. PIG, Warszawa,
GÚDŠ, Bratislava, ÚÚG, Praha.

Isthmolithus recurvus Deflandre in Deflandre & Fert, (1954)
Lanternithus minutus Stradner, (1962)
Neococcolithes dubius (Deflandre in Deflandre & Fert, 1954) Black,

(1967)

Pontosphaera multipora (Kamptner, 1948) Roth, (1970)
Reticulofenestra callida (Perch-Nielsen, 1971) Bybell, (1975)
Reticulofenestra dictyoda (Deflandre in Deflandre & Fert, 1954)

Stradner in Stradner & Edwards, (1968)

Reticulofenestra hillae Bukry & Percival, (1971)
Reticulofenestra lockerii Müller, (1970)
Reticulofenestra ornata Müller, (1970)
Reticulofenestra reticulata (Gartner & Smith, 1967) Roth & Thierstein,

(1972)

Reticulofenestra umbilica (Levin, 1965) Martini & Ritzkowski,

(1968b)

Sphenolithus moriformis (Brönnimann & Stradner, 1960) Bramlette &

Wilcoxon, (1967)

Sphenolithus predistentus Bramlette & Wilcoxon, (1967)
Sphenolithus radians Deflandre in Grassé, (1952)
Sphenolithus spiniger Bukry, (1971)
Transversopontis fibula Gheta,
Transversopontis pulcher (Deflandre in Deflandre & Fert, 1954) Perch-

Nielsen, (1967)

Transversopontis pulcheroides (Sullivan, 1964) Báldi-Beke, (1971)
Tribrachiatus orthostylus Shamrai, (1963)
Zygrhablithus bijugatus (Deflandre in Deflandre & Fert, 1954)

Deflandre, (1959)

Braarudosphaera bigelowii (Gran & Braarud, 1935) Deflandre, (1947)
Chiasmolithus grandis (Bramlette & Riedel, 1954) Radomski, (1968)
Chiasmolithus medius Perch-Nielsen, (1971)
Chiasmolithus oamaroensis (Deflandre in Deflandre & Fert, 1954)

Hay, Mohler & Wade, (1966)

Coccolithus pelagicus (Wallich, 1877) Schiller, (1930)
Coronocyclus nitescens (Kamptner, 1963) Bramlette & Wilcoxon,

(1967)

Cyclicargolithus abisectus (Müller, 1970) Wise, (1973)
Cyclicargolithus floridanus (Roth & Hay in Hay et al., 1967) Bukry,

(1971)

Dictyococcites bisectus (Hay, Mohler & Wade, 1966) Bukry &

Percival, (1971)

Discoaster barbadiensis Tan, (1927)
Discoaster deflandrei Bramlette & Riedel, (1954)
Discoaster lodoensis Bramlette & Riedel, (1954)
Discoaster multiradiatus Bramlette & Reidel, (1954)
Discoaster saipanensis Bramlette & Riedel, (1954)
Discoaster tanii Bramlette & Riedel, (1954)
Discoaster tanii nodifer (Bramlette & Riedel, 1954) Bukry, (1973b)
Ericsonia fenestrata (Deflandre & Fert, 1954) Stradner in Stradner &

Edwards, (1968)

Ericsonia formosa (Kamptner, 1963) Haq, (1971)
Ericsonia subdisticha (Roth & Hay in Hay et al., 1967) Roth in

Baumann & Roth, (1969)

Helicosphaera bramlettei Müller, (1970)
Helicosphaera compacta Bramlette & Wilcoxon, (1967)

APPENDIX

Nannofossil taxa mentioned in the text, in alphabetical order of genus names