GEOLOGICA CARPATHICA
, AUGUST 2019, 70, 4, 311–324
doi: 10.2478/geoca-2019-0018
www.geologicacarpathica.com
Oligocene turbidite fans of the Dukla Basin: New age data
from the calcareous nannofossils and paleoenvironmental
conditions (Cergowa beds, Polish–Slovakian borderland)
JOANNA PSZONKA
1,
, KATARÍNA ŽECOVÁ
2
and MAREK WENDORFF
3
1
Mineral and Energy Economy Research Institute, Polish Academy of Sciences, Wybickiego 7a, 31261 Krakow, Poland;
joanna.pszonka@gmail.com
2
State Geological Institute of Dionýz Štúr, Jesenského 8, 040 01 Košice, Slovakia
3
Faculty of Geology, Geophysics and Environmental Protection, AGH University of Science and Technology, Mickiewicza 30,
30059 Krakow, Poland
(Manuscript received February 21, 2018; accepted in revised form May 15, 2019)
Abstract: Calcareous nannofossils found in the Cergowa beds of the Dukla and Fore-Dukla tectonic units in the Outer
Carpathians indicate a time of deposition in the range of the NP23–NP24 nannoplankton zones of the Lower Oligocene.
Nannoplankton assemblages reflect the paleoecological changes at the Eocene–Oligocene transition from: (i) a green-
house to an icehouse climate; (ii) brackish to normal salinity suggesting open sea conditions, which were controlled by
the Paratethys Basin closure followed by opening and connection with the Tethyan Ocean. The absence of nannofossils
of NP25 zone, but their presence in the tectonic windows between 40 and 80 km to the west, shows that deposition of
the Cergowa beds in the western part of the basin lasted longer than in the east. Occurrences of nannofossils indicating
zones NP16 and NP21, found in the uppermost mudstone-rich parts of studied sections, may prove the remobi lization
and redeposition of sediments of this stratigraphic age. Potentially, eroded material could be derived from some of
the following lithostratigraphic units: NP16 — the Hieroglyphic beds, Przybyszów sandstones and Upper variegated
shales; NP21 — the Globigerina marls, Mszanka sandstones and sub-Chert marls and shales and/or fine- grained
equi valent of these units. Reworked specimens derived from the older Mesozoic strata occur occasionally in various
samples.
Keywords: Flysch Carpathians, Cergowa beds, calcareous nannofossils, Lower Oligocene, Eocene–Oligocene icehouse.
Introduction
Observations on calcareous nannofossil assemblages from
the Cergowa beds in the Dukla and the Fore-Dukla tectonic
units (Fig. 1) have not been published until the most recent
work of the present authors (Pszonka et al. 2014). Therefore
the ages of these units were generally determined on the basis
of foraminiferal assemblages that occur in the overlying rocks
of the Menilite beds (Olszewska & Smagowicz 1977;
Olszewska 1983, 1984). On the other hand, several publica-
tions on the calcareous nannofossils from the strata outcrop-
ping to the west of the Dukla Tectonic Unit, in tectonic win-
dows within the Magura Tectonic Unit (Fig. 1), and considered
as correlative to the Cergowa beds, were published in the last
two decades (Oszczypko-Clowes & Oszczypko 2004, 2011;
Oszczypko- Clowes & Ślączka 2006; Oszczypko-Clowes 2008).
The analysis of the calcareous nannofossils appears most
informative for the purpose of biostratigraphical and paleo-
geographical determinations of the Cergowa beds. Therefore,
the aim of this study is to: (i) present the data on the calcareous
nannofossils providing more precise age determination of
the Cergowa beds in the Dukla and Fore-Dukla tectonic units;
(ii) discuss paleoecolgical conditions in the Dukla Basin;
(iii) compare the time frame of deposition of the Cergowa
beds on a regional scale.
Geological setting
The Cergowa beds were deposited in the basin, which has
subsequently been partitioned during the Carpathian
Orogenesis so that the Cergowa beds now occur in two tec-
tonic units of the Flysch Carpathians: in the Dukla Tectonic
Unit and in the southernmost part of the Silesian Tectonic
Unit (also called the Fore-Dukla Tectonic Unit) adjacent to
the north (Fig. 1). The Cergowa beds form a lenticular
lithosome depo sited by a variety of submarine mass gravity
flows (Ślączka 1971; Pszonka 2015). The unit consists of
two main lithofacies: (i) fine-grained sandstones in the axial
part and (ii) fine-grained sandstones interbedded with shales,
mudstones, marls and limestones in marginal zones (Ślączka
1971).
The Cergowa beds sandy lithosome, embedded within
a generally fine-grained succession of the Menilite beds,
records increased uplift and emergence of source areas related
to the advancement of the Outer Carpathian orogenic wedge
(Oszczypko 2004; Dirnerová et al. 2012). Paleocurrent pat-
terns, facies trends and sediment provenance indicators sug-
gest that a hypothetical Silesian Ridge located north-west
acted as the main source supplying the terrigenous detritus
transported by sediment gravity flows predominantly oriented
towards the south-east (Fig. 1; Ślączka & Unrug 1976; Winkler
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PSZONKA, ŽECOVÁ and WENDORFF
GEOLOGICA CARPATHICA
, 2019, 70, 4, 311–324
Fig.
1.
Schematic
tectoni
c
map
of
the
Outer
Carpathians
(simplified
from
Żytko
et
al.
1989).
GPS
coordinates
of
the
sampled
localities:
Iwla
—
49°33’06.0”
N
21°37’17.4”
E;
Lipowica
—
49°31’42.3”
N
21°40’46.0”
E;
Tylawa
—
49°27’53.2”
N
21°43’52.3”
E;
Rudawka
Rymanowska
—
49°31’15.3”
N
21°55’41.8”
E;
W
ernejówka
—
49°28’27.9”
N
21°54’19.3”
E;
Medzilaborce — 49°16’20.8” N 21°54’23.6” E; Habura — 49°19’28.3” N 21°51’05.1” E; Ruská
Volová — 48°57’15.3” N 22°22’54.8” E.
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OLIGOCENE TURBIDITE FANS OF THE DUKLA BASIN (POLISH–SLOVAKIAN BORDERLAND)
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& Ślączka 1992; Dirnerová & Janočko 2014). Locally obser-
ved indicators show deviations of paleoflows to the south,
suggesting the influence of local basin floor paleotopography
(Dirnerová & Janočko 2014). Subordinate opposite paleoflow
directions towards the north-west, observed in the lower part
of the succession in the north-western part of the Dukla
Tectonic Unit, were interpreted as reversals of turbidity cur-
rents caused by local paleotopography at an early stage of
deposition (Wendorff & Pszonka 2015). Alternatively, supply
from another source area was considered, namely from the
hypothetical Fore-Magura Ridge at the southern margin of
the Dukla Basin, now overthrust by the Magura Nappe
(Cieszkowski et al. 2009). A longitudinal facies gradient
within the Cergowa beds lithosome, generally parallel to the
Dukla Basin axis and extending south-eastward from the pro-
ximal zone in the north-west part of the Dukla Tectonic Unit
(Ślączka & Unrug 1976), appears to be reflected by regional
trends in the recently identified sedimentary facies associa-
tions and inferred depositional mechanisms (Dirnerová et al.
2012; Dirnerová & Janočko 2014; Pszonka et al. 2014;
Pszonka 2015); these are consolidated below.
Facies in the proximal sections of the succession, located in
the western part of the Dukla Tectonic Unit at Iwla, Lipowica
and Tylawa (Fig. 1), suggest sediment supply to the deep
marine Cergowa beds depositional system by high-density
turbidites and hyperpycnal flows as megaturbidite beds of
the Central Carpathian Paleogene Basin (Starek et al. 2013)
fed from a directly connected delta (Plink-Björklund & Steel
2004). Such a paleogeographic relationship is suggested by
complexes of beds with sedimentary features implying depo-
sition by aggrading sustained turbidity currents (Kneller &
Branney 1995) and containing exceptionally high proportions
of coalified plant detritus, including tree trunks present at
Lipowica (Plink-Björklund & Steel 2004). Successions in
the proximally located sections are characterized by very
thick- and thick-bedded massive or laminated sandstones,
absence of mudstone interbeds and are usually devoid of ver-
tical sequences. Very low spread of paleocurrent directions
measured in these sections implies deposition in confined
troughs elongated from NW to SE.
Successions in the more distally located sections document
mainly deposition from the short-lived, surge-type turbidity
currents (Pszonka et al. 2014) and are characterized by vertical
sequences and more “distally” developed facies associations
represented by medium to thin-bedded sandstones displaying
complete or incomplete sequences of Bouma divisions
(Tabcde–Tcde). These are associated with thin to thick
mudstone interbeds, deposited by turbidity currents with
densities ranging from moderate to low. Facies related to low
and very low energy turbidites and hemipelagic/pelagic depo-
sition appear in considerable proportions in distal and mar-
ginal sections. These features suggest deposition within
a classic turbidite fan system in an unconfined basin (Mutti
et al. 2009) represented, for example, by the fan-shaped pattern
of paleocurrents at Komańcza. A deep marine fan-shaped
depositional body in the SE part of the basin is also suggested
by coarse ning upwards and fining upwards sedimentary
cycles of outer- fan lobes documented by Dirnerová and
Janočko (2014).
Therefore, comparisons of the facies associations and
paleocurrent patterns throughout this part of the basin suggests
a longitudinal transition between two domains. The proximal
area in the NW part of the Dukla Tectonic Unit may be inter-
preted as partly confined, located on the slope, supplied
directly from shelf-edge delta and passing to the south-east
into a floor-fan distributary system deposited in the open part
of the Dukla Basin.
Material and methods
Study of calcareous nannofossils from the Cergowa beds
turbidite succession includes twenty-five samples from eight
sections: Iwla, Lipowica, Tylawa, Rudawka Rymanowska,
Wernejówka, Medzilaborce, Habura and Ruská Volová, repre-
senting their main lithofacies (Figs. 1, 2; Table 1). In the light
of the submarine fan model (Walker 1978) the facies associa-
tions observed in the analysed sections of the Cergowa beds
and described in the previous section can be interpreted as
follows:
• NW sections, namely Iwla, Lipowica and Tylawa, contain
successions deposited in the channelized upper part of mid-
fan/suprafan because of very thick beds, with sedimentary
features interpreted as products of sustained/hyperpycnal
flows and rapidly depositing megaturbidites, very low
spread of paleocurrent indicators reflecting transport
towards the SE in elongated troughs or channels, and
absence of vertical sequences, which suggests sedimenta-
tion by aggradation (Pszonka 2015);
• middle sections, namely Rudawka Rymanowska and
Wernejówka represent mid-fan/suprafan lobes composed of
sandstone–mudstone Bouma divisions deposited by turbi-
dity currents of concentration normal to low and forming
coarsening-upwards and fining-upwards vertical sequences
(CU and FU) that reflect lateral shifts or changing intensity
of the local sediment supply (Pszonka 2015);
• SE sections, namely Medzilaborce and Habura illustrate
deposition in the lower/outer fan part of the Cergowa depo-
sitory supplied by low and very low energy and highly
diluted turbidity currents depositing thin and very thin sand-
stone beds (Tc), only locally interlayered with isolated thick
massive sandstones interpreted as infills of small channels.
These channels were occasionally incised into outer fan sedi-
ments and supplying new suprafan lobes (Dirnerová &
Janočko 2014; Pszonka 2015) formed in the distal regions
of the depositional system. Poor quality of the Ruská Volová
outcrop does not provide ground sufficient for the interpre-
tation of submarine fan facies association with confidence.
The samples were collected from calcareous mudstones,
marls and limestones. Their positions were precisely deter-
mined within the sedimentary succession on the basis of
detailed bed-by-bed logging and are shown on generalized
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PSZONKA, ŽECOVÁ and WENDORFF
GEOLOGICA CARPATHICA
, 2019, 70, 4, 311–324
Fig. 2.
Generalized sections of the Cer
gowa beds, documenting successions of lithofacies associations and indicating positions of samples collected for the calcareous nannoplankton analysis
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OLIGOCENE TURBIDITE FANS OF THE DUKLA BASIN (POLISH–SLOVAKIAN BORDERLAND)
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sections (Fig. 2). The samples were prepared following the
standard preparation technique according to Haq & Lohmann
(1976) and studied with the polarizing microscope Carl Zeiss
Axioskop 40 at magnification 1000×. The standard zonation
by Martini (1971) and Berggren et al. (1995) was used for
the stratigraphic interpretation. Paleoecology was developed
following: Haq & Lohmann (1976), Wei & Wise (1990), Soták
& Kováč (2002), Persico & Villa (2004), Villa et al. (2008),
Oszczypko-Clowes (2012) and Ozdínová (2013).
Results
Iwla section
Samples in the Iwla section (Fig. 2) were taken from its
stratigraphically youngest, mudstone–siltstone part. The lower-
most sample 1I mostly contains Reticulofenestra lockeri and
Pontosphaera fibula. It also comprises Helicosphaera com
pacta, H. euphratis, Lanternithus minutus, Pontosphaera
latelliptica, P. multipora and P. obliquipons. In the next sam-
ple 2I, located 5 m above the sample 1I, the most numerously
represented are: Coccolithus eopelagicus (Fig. 3.1, 3.2),
C. pelagicus, Cyclicargolithus abisectus, Reticulofenestra
bisecta, R. lockeri, Lanternithus minutus, Pontosphaera fibula
and Zygrhablithus bijugatus. Furthermore, the assemblage
contains high numbers of specimens of genera of Chias
molithus, Coccolithus, Cyclicargolithus and Reticulofenestra,
and less Helicosphaera, Isthmolithus, Lanternithus, Ponto
sphaera and Zygrhablithus, (particular species are listed in
Table 2). The two uppermost samples 3I and 4I chiefly contain
Reticulofenestra lockeri, and less common representatives of
genera Coccolithus (Fig. 3.3), Cribrocentrum, Cyclicargolithus
and Reticulofenestra (particular species are listed in Table 2).
Rare occurrences of genus Helicosphaera were noted in sam-
ples 3I and 4I, and of Isthmolithus and Pontosphaera in sam-
ple 4I (particular species are listed in Table 2).
Lipowica section
Sample 1L from the lower part of Lipowica section (Fig. 2)
contains Cyclicargolithus floridanus (Fig. 3.4), Reticulo
fenestra bisecta (Fig. 3.5), R. umbilica and less abundant
Coccolithus formosus, C. pelagicus, Helicosphaera compacta
and Sphenolithus moriformis. On the other hand, samples 3L
and 4L from the uppermost part of this section primary imply
Reticulofenestra lockeri. The presence of genera Coccolithus,
Cyclicargolithus and Reticulofenestra (particular species are
listed in Table 2) is also noted. Isthmolithus recurvus and
Lanternithus minutus in sample 4L occur in low numbers.
Sample 2L provided only poor nannofossils.
Tylawa section
Samples 1T and 2T from the Tylawa stratigraphic section
(Fig. 2) were collected from the upper part of section. Sample
T1 provided a poor nannofossil assemblage with low species
diversity, containing mostly Reticulofenestra bisecta and
R. umbilica, whilst R. lockeri, R. ornata and Pontosphaera
fibula occur scarcely. A rich and well diversified assemblage
was found in sample 2T, in which Reticulofenestra ornata,
R. reticulata and R. umbilica dominate. Specimens of genera
Helicosphaera, Isthmolithus, Lanternithus and Pontosphaera
(particular species are listed in Table 2) in sample 2T occur
in low numbers. Samples 3T and 4T provided only rare
nannofossils.
Rudawka Rymanowska section
Samples 1R and 2R, which represent the lowermost part of
the Rudawka Rymanowska section (Fig. 2) primarily provided
Reticulofenestra bisecta, R. lockeri (Fig. 3.6), Reticulofenestra
ornata (Fig. 3.7, 3.8) and Pontosphaera fibula (Fig. 3.9, 3.10).
The next sample 3R from the upper part of the section (Fig. 2)
mostly contains Reticulofenestra lockeri (Fig. 3.11) and
genera Coccolithus, Cyclicargolithus and Reticulofenestra
(particular species are listed in Table 2). The assemblage is
complemented by significant species of Helicosphaera com
pacta and Lanternithus minutus. Sample 4R did not provide
any nannofossils.
Wernejówka section
The only sample 1W from the Wernejówka section (Fig. 2)
did not provide any nannofossils.
Habura section
Samples 1H and 2H from the Habura section (Fig. 2) con-
tain rich but poorly diversified nannofossil assemblages with
Coccolithus pelagicus and Reticulofenestra bisecta, whereas
C. eopelagicus, Cyclicargolithus abisectus (Fig. 3.12), C. flori
danus, Lanternithus minutus, R. lockeri and Zygrhablithus
bijugatus occur in lower numbers. Genera Helicosphaera,
Isthmolithus, Pontosphaera and Sphenolithus (particular spe-
cies are listed in Table 2) are less abundant. Sample 3H did not
provided any nannofossils.
L.p. Locality of sections
Number of samples to be
analysed (labeled)
1.
Iwla/ Poland
4 (1I, 2I, 3I, 4I)
2.
Lipowica/ Poland
4 (1L, 2L, 3L, 4L)
3.
Tylawa/ Poland
4 (1T, 2T, 3T, 4T)
4.
Rudawka Rymanowska/ Poland
4 (1R, 2R, 3R, 4R)
5.
Wernejówka/ Poland
1 (1W)
6.
Medzilaborce/ Slovakia
4 (1M, 2M, 3M, 4M)
7.
Habura/ Slovakia
3 (1H, 2H, 3H)
8.
Ruská Volová/ Slovakia
1 (1RV)
Total:
25
Table 1: Localities of sampled sections, number of samples per loca-
lity and sample labels. Interpreted samples are shown in bold font;
seven samples that have been excluded are shown in italics.
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Fig. 3. Light microscope images of calcareous nannofossils from the Cergowa beds in the Dukla and Fore-Dukla tectonic units (CN — crossed
nicols, NL — normal light): 1. Coccolithus eopelagicus, CN, sample 2I; 2. Coccolithus eopelagicus, NL, sample 2I; 3. Coccolithus pelagicus,
NL, sample 3I; 4. Cyclicargolithus floridanus, CN, sample 1L; 5. Reticulofenestra bisecta, CN, sample 1L; 6. Reticulofenestra lockeri, CN,
sample 1R; 7. Reticulofenestra ornata, CN, sample 2R; 8. Reticulofenestra ornata, CN, sample 2R; 9. Pontosphaera fibula, CN, sample 2R;
10. Pontosphaera fibula, CN, sample 2R.; 11. Reticulofenestra lockeri, CN, sample 3R; 12. Cyclicargolithus abisectus, CN, sample 1H;
13. Chiasmolithus oamaruensis, NL, sample 1M; 14. Reticulofenestra reticulata, CN, sample 1M; 15. Reticulofenestra lockeri, CN,
sample 4M; 16. Reticulofenestra lockeri, CN, sample 1M; 17. Reticulofenestra umbilica, CN, sample 4M; 18. Reticulofenestra umbilica, CN,
sample 1M; 19. Cyclicargolithus abisectus, CN, sample 1M; 20. Cyclicargolithus floridanus, CN, sample 4M; 21. Cyclicargolithus floridanus,
CN, sample 1M; 22. Cyclicargolithus floridanus, CN, sample 1M; 23. Pontosphaera fibula, CN, sample 1M; 24. Zygrhablithus bijugatus, CN,
sample 4M; 25. Helicosphaera recta, CN, sample 4M; 26. Helicosphaera recta, NL, sample 4M; 27. Helicosphaera recta, CN, sample 4M;
28. Isthmolithus recurvus, CN, sample 1M; 29. Reticulofenestra ornata, CN, sample 1M.
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Medzilaborce section
Samples 1M, 2M and 4M contain Chiasmolithus grandis,
Ch. oamaruensis (Fig. 3.13), Coccolithus eopelagicus, C. for
mosus, C. pelagicus, Reticulofenestra reticulata (Fig. 3.14),
R. bisecta, R. lockeri (Fig. 3.15, 3.16), R. umbilica (Fig. 3.17,
3.18), Cyclicargolithus abisectus (Fig. 3.19), C. floridanus
(Fig. 3.20, 3.21, 3.22), Pontosphaera fibula (Fig. 3.23) and
Zygrhablithus bijugatus (Fig. 3.24). Samples 1M and 4M
additionally contain Helicosphaera recta (Fig. 3.25, 3.26,
3.27), Isthmolithus recurvus (Fig. 3.28) and Reticulofenestra
ornata (Fig. 3.29). Lanternithus minutus was found in samples
1M and 2M and Pontosphaera latelliptica and P. multipora
were present in 4M. Sample 3M was barren of nannofossils.
Ruská Volová section
The only sample 1RV from the Ruská Volová locality
(Fig. 2) provided a low in numbers and poorly diversified nan-
nofossil assemblage of Reticulofenestra bisecta and R. umbi
lica, and with smaller numbers of Coccolithus eopelagicus,
C. formosus, C. pelagicus, Cyclicargolithus floridanus, and
Helicosphaera compacta.
Nannoplankton biostratigraphic interpretations
Nannofossils from the Cergowa beds belong to the follo-
wing groups:
• species characteristic of the Eocene standard zone NP16
(Late Lutetian/Early Bartonian; Table 3);
• species indicating the Oligocene standard zones: NP21
(Late Priabonian/Early Rupelian), NP23 (Rupelian) and
NP24 (Late Rupelian/Early Chattian, Table 3);
• reworked nannofossils from the older Mesozoic strata.
Poor preservation does not allow their more precise
identification;
• corroded and recrystallized unidentifiable nannofossils.
The Middle Eocene, zone NP16 is the oldest stratigraphic
age found in this study. It was determined in the lower part of
the Lipowica section in the sample 1L and in the Ruská Volová
section in the sample 1VR (Fig. 2). Zone NP16 was deter-
mined on the basis of species characteristic of an open water
environment: Helicosphaera compacta, Reticulofenestra
bisecta and Cyclicargolithus floridanus, all of which indicate
moderate water temperature (Perch-Nielsen 1985).
Zone NP21 was identified according to the presence of
Reticulofenestra lockeri in the upper part of three sections:
Iwla in samples 3I and 4I, Lipowica in samples 3L and 4L and
Rudawka Rymanowska in the sample 3R (Fig. 2). Assemblages
of NP21 zone were found in Iwla and Rudawka Rymanowska
localities above the strata that provide stratigraphically
younger nannofossils from zones NP23 and NP24 (Fig. 2).
On the contrary, in the Lipowica section, younger fauna (NP23
and NP24) has not been identified below zone NP21 (Fig. 2).
The presence of genera Coccolithus, Cyclicargolithus and
Reticulofenestra in these samples suggests an open-marine
environment (Perch-Nielsen 1985), whereas the occurrence
and abundance of species Helicosphaera compacta indicates
a warm marine environment and also shallow-marine (Perch-
Nielsen 1985; Nagymarosy & Voronina 1992). Open-marine
genera are mixed with by far less abundant shallow-marine
genera: Helicosphaera, Isthmolithus, Lanternithus and Ponto
sphaera (Perch-Nielsen 1985).
Zone NP23 was recorded in three sections: Iwla in the sam-
ple 1I, Tylawa in samples 1T and 2T and Rudawka Ryma-
nowska in samples 1R and 2R (Fig. 2), based on species:
Reticulofenestra lockeri, R. ornata and Pontosphaera fibula.
The material representing zone NP23 occurs in the uppermost
part of Tylawa and Iwla sections, and in the lower part of the
Rudawka Rymanowska succession (Fig. 2). By comparison
with all other zones, zone NP23 occupies the stratigraphically
lowermost position in these three sections (Fig. 2). In both
samples from Rudawka Rymanowska, where NP23 zone was
recognized (samples 1R and 2R), the nannofossils reflect
brackish water conditions on the basis of: Pontosphaera fibula
and Reticulofenestra ornata (Nagymarosy & Voronina 1992).
Samples 2T from Tylawa and 1I from Iwla contain genera
characteristic for coastal waters: Helicosphaera, Isthmolithus,
Lanternithus, and Pontosphaera (Perch-Nielsen 1985). Nanno-
fossils from the sample 1T from Tylawa (Table 2) represent
open shelf environment.
The youngest sediments of the Cergowa beds in the studied
region were assigned to zone NP24 on the basis of Coccolithus
eopelagicus, C. pelagicus, Cyclicargolithus abisectus, Helico
sphaera recta, Lanternithus minutus, Reticulofenestra bisecta,
R. lockeri, Pontosphaera fibula and Zygrhablithus bijugatus.
Zone NP24 was interpreted in Iwla (2I), Medzilaborce (1M,
2M and 4M) and Habura (2 H) (Fig. 2). In the Medzilaborce
and Habura sections nannofossil assemblages indicate zone
NP24 (Fig. 2). In the Iwla section, nannofossils of zone NP24
were found about 5 m above the sample representing zone
NP23 (Fig. 2). Zone NP24 in all analysed samples is charac-
terized by numerous genera typical for open waters: Cocco
lithus, Cyclicargolithus, Reticulofenestra and Chiasmolithus
(Perch-Nielsen 1985). In addition, the presence of cryophilic
species: Isthmolithus recurvus, Reticulofenestra lockeri and
R. ornata documents conditions of the cold Oligocene climate
(Wei & Weise 1990; Aubry 1992; Oszczypko-Clowes 2001;
Prothero 2003; Katz et al. 2008). Simultaneously, nannofossils
indicating near-shore and coastal waters were present in all
the above-mentioned samples. They include genera: Helico
sphaera, Isthmolithus, Lanternithus, Pontosphaera and Zygr
hablithus (Perch-Nielsen 1985).
In the lithostratigraphically continuous succession of the
Cer gowa beds at Iwla and Rudawka Rymanowska (Fig. 2) the
samples with assemblages representing the nannofossils zone
NP21 occur above younger assemblages corresponding to
zone NP23, and therefore must be redeposited. Based on
the progressively younging succession of sediments represen-
ting zone NP16 followed by zone NP21 in apparently con-
tinuous lithostratigraphic sequence at Lipowica (Fig. 2),
318
PSZONKA, ŽECOVÁ and WENDORFF
GEOLOGICA CARPATHICA
, 2019, 70, 4, 311–324
Locality
Ruská
Volová
Medzilaborce
Habura
Rudawka
Rymanowska
Tylawa
Iwla
Lipowica
Calcareous
nannoplankton
zones
(Martini 1971;
Berggren et al. 1995)
NP16 NP24 NP24 NP24 NP24 NP24 NP23 NP23 NP21 NP23 NP23 NP23 NP24 NP21 NP21 NP16 NP21 NP21
Sample number
1RV
1M
2M
4M
1H
2H
1R
2R
3R
1T
2T
1I
2I
3I
4I
1L
3L
4L
Arkhangelskiella
cymbiformis
R
R
R
R
R
R
R
R
R
R
Arkhangelskiella
maastrichtiana
R
R
R
Braarudosphaera
bigelowii
R
R
R
R
R
R
Broinsonia
parca constricta
R
R
R
Broinsonia
parca parca
R
R
R
Calculites
obscurus
R
R
R
R
R
R
R
R
Ceratolithina
hamata falcata
R
R
R
R
R
Chiasmolithus
bidens
X
X
X
Chiasmolithus
expansus
X
Chiasmolithus
grandis
X
X
X
X
X
X
X
X
Chiasmolithus
oamaruensis
X
X
X
X
Chiasmolithus
solitus
X
Coccolithus
eopelagicus
X
X
X
X
X
X
X
X
X
X
X
X
X
X
X
Coccolithus
formosus
X
X
X
X
X
X
X
X
X
X
X
X
X
X
Coccolithus
pelagicus
X
X
X
X
X
X
X
X
X
X
X
X
X
X
X
X
X
Coronocyclus
nitescens
X
X
X
X
X
X
Cribrosphaerella
ehrenbergii
R
R
R
R
R
R
R
Cruciplacolithus
tenuis
X
X
X
Cyclicargolithus
abisectus
X
X
X
X
X
X
Cyclicargolithus
floridanus
X
X
X
X
X
X
X
X
X
X
X
X
X
X
X
X
Discoaster
barbadiensis
X
X
X
X
X
X
X
Discoaster
deflandrei
X
X
X
Discoaster
distinctus
X
Discoaster
lodoensis
X
X
X
X
X
X
Discoaster
multiradiatus
X
X
X
X
X
X
X
Discoaster
saipanensis
X
X
X
X
Discoaster
sublodoensis
X
Discoaster
tanii nodifer
X
X
X
Eiffellithus
eximius
R
R
R
R
R
R
Eiffellithus
gorkae
R
Ellipsolithus
macellus
X
Ericsonia
fenestrata
X
X
X
X
Helicosphaera
bramlettei
X
Helicosphaera
compacta
X
X
X
X
X
X
X
X
X
X
X
X
X
X
X
X
Table 2: Identified calcareous nannofossils species from the Cergowa beds with their assignment to the locality of section and the sample
number. Abbreviations: X — autochthonous species, R — redeposited species.
319
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Locality
Ruská
Volová
Medzilaborce
Habura
Rudawka
Rymanowska
Tylawa
Iwla
Lipowica
Calcareous
nannoplankton
zones
(Martini 1971;
Berggren et al. 1995)
NP16 NP24 NP24 NP24 NP24 NP24 NP23 NP23 NP21 NP23 NP23 NP23 NP24 NP21 NP21 NP16 NP21 NP21
Sample number
1RV
1M
2M
4M
1H
2H
1R
2R
3R
1T
2T
1I
2I
3I
4I
1L
3L
4L
Helicosphaera
euphratis
X
X
X
X
X
X
X
Helicosphaera
lophota
X
Helicosphaera
recta
X
X
Helicosphaera
seminulum
X
Isthmolithus
recurvus
X
X
X
X
X
X
X
X
Lanternithus
minutus
X
X
X
X
X
X
X
X
X
Lithraphidites
praequadratus
R
R
Lucianorhabdus
cayeuxii
R
R
Markalius
inversus
R
Micrantholithus
hoschulzii
R
R
R
R
R
R
R
Microrhabdulus
decoratus
R
R
R
R
R
R
Microrhabdulus
undosus
R
Micula
murus
R
R
R
R
R
Micula
staurophora
R
R
R
R
R
R
R
R
R
R
R
R
R
R
Nannoconus
steinmannii
R
R
R
R
Nannotetrina
fulgens
X
X
Neococcolithes
dubius
X
X
Neococcolithes
minutus
X
X
Pontosphaera
latelliptica
X
X
X
X
X
X
X
Pontosphaera
fibula
X
X
X
X
X
X
X
X
Pontosphaera
multipora
X
X
X
X
X
X
X
X
Pontosphaera
obliquipons
X
X
X
Pontosphaera
pulcheroides
X
X
X
X
X
Prediscosphaera
cretacea
R
R
R
R
R
R
R
R
R
R
Retecapsa
surirella
R
R
Reticulofenestra
bisecta
X
X
X
X
X
X
X
X
X
X
X
X
X
X
X
X
X
X
Reticulofenestra
coenura
X
X
X
X
X
X
Reticulofenestra
dictyoda
X
Reticulofenestra
lockeri
X
X
X
X
X
X
X
X
X
X
X
X
X
X
X
X
Reticulofenestra
oamaruensis
X
X
X
Reticulofenestra.
ornata
X
X
X
X
X
X
Reticulofenestra
reticulata
X
X
X
X
X
X
X
X
X
X
X
X
X
Reticulofenestra
umbilica
X
X
X
X
X
X
X
X
X
X
X
X
X
X
X
X
X
X
Sphenolithus
anarrhopus
X
X
Table 2 (continued): Identified calcareous nannofossils species from the Cergowa beds with their assignment to the locality of section and
the sample number. Abbreviations: X — autochthonous species, R — redeposited species.
320
PSZONKA, ŽECOVÁ and WENDORFF
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, 2019, 70, 4, 311–324
the nannofossils species that define these two zones must be
considered as reworked ones because they have been docu-
mented in the literature as autochthonous in completely diffe-
rent lithostratigraphic divisions within the Dukla Unit and
the southern part of the Silesian (Fore-Dukla) Unit. To be spe-
cific, the nannofossils defining zone NP16 are characteristic
for the uppermost part of the Hieroglyphic beds, the Przy-
byszów sandstones and the Upper variegated shales
(Oszczypko 2004), whereas zone NP21 is represented by
the Globigerina marls, Mszanka sandstones and sub-Chert
marls and shales (Ślączka 1971; Oszczypko 2004; Kotlarczyk
et al. 2006). Furthermore, the stratigraphically continuous suc-
cession in Lipowica, documented at Cergowa Góra by Ślączka
(1971), consists of the sub-Cergowa marls dated to zone NP23
(Kotlarczyk et al. 2006), which are followed by the Cergowa
beds and the overlying part of the Menilite beds.
The nannoplankton zone NP24 is recorded in whole sec-
tions in Medzilaborce and Habura, and in the uppermost part
of the Iwla suite. In Iwla nannofossils indicating zone NP23
also occur in the strata below zone NP24 (Fig. 2). Going
further, zone NP23 is present in Tylawa and Rudawka
Rymanowska (Fig. 2). Considering the above arguments, we
have concluded that the Cergowa beds in the discussed sec-
tions represent a stratigraphic succession of two nannoplank-
ton zones: NP23 and NP24.
Nannofossil paleoecology
Autochthonous calcareous nannofossils of the Cergowa
beds from the Dukla and southern Silesian (Fore-Dukla) tec-
tonic units identify the Lower Oligocene zones NP23 and
NP24. In the Tethys area, this was a time of significant cli-
matic, paleogeographical and paleoecological changes. These
were caused by the global climate cooling and eustatic sea
level fall (Haq et al. 1987, 1988), forced by the expansion of
the Antarctic ice cap. Kominz & Pekar (2001) estimate that
the eustatic sea level in the earliest Oligocene was lowered by
Locality
Ruská
Volová
Medzilaborce
Habura
Rudawka
Rymanowska
Tylawa
Iwla
Lipowica
Calcareous
nannoplankton
zones
(Martini 1971;
Berggren et al. 1995)
NP16 NP24 NP24 NP24 NP24 NP24 NP23 NP23 NP21 NP23 NP23 NP23 NP24 NP21 NP21 NP16 NP21 NP21
Sample number
1RV
1M
2M
4M
1H
2H
1R
2R
3R
1T
2T
1I
2I
3I
4I
1L
3L
4L
Sphenolithus
furcatolithoides
X
X
Sphenolithus
moriformis
X
X
X
X
X
X
X
X
X
X
X
X
X
X
X
Sphenolithus
obtusus
X
X
X
Sphenolithus
pseudoradians
X
X
Sphenolithus
radians
X
X
X
X
X
X
X
X
X
Sphenolithus
spiniger
X
X
X
Toweius
crassus
X
X
Toweius
eminens
X
Tranolithus
orionatus
R
Tribrachitaus
orthostylus
X
Uniplanarius
sissinghii
R
R
R
Watznaueria
barnesae
R
R
R
R
R
R
R
R
R
R
R
R
R
R
R
R
R
Watznaueria
biporta
R
Watznaueria
britannica
R
Watznaueria
fossacincta
Watznaueria
manivitae
R
R
R
R
R
R
R
Watznaueria
ovata
R
R
R
Zeugrhabdotus
embergeri
R
R
R
R
R
R
Zygrhablithus
bijugatus
X
X
X
X
X
X
X
X
X
X
X
X
Table 2 (continued): Identified calcareous nannofossils species from the Cergowa beds with their assignment to the locality of section and
the sample number. Abbreviations: X — autochthonous species, R — redeposited species.
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OLIGOCENE TURBIDITE FANS OF THE DUKLA BASIN (POLISH–SLOVAKIAN BORDERLAND)
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~55 m, while Katz et al. (2008) report the amount of ~67 m.
This resulted in isolation of the Paratethys Basin in the nor-
thern part of the Tethyan Ocean (Piller et al. 2007) and
impacted on the Carpathian Basin, which was the central part
of Paratethys. Climatic cooling, sea-level fall and the isolation
of Paratethys from the Carpathian basins during the Early
Oligocene have been documented in several publications,
including Soták (2010).
Important climatic changes resulted in disappearance of
many genera, such as Discoaster, Helicosphaera, and Sphe
nolithus (Melinte 2005), which is noticeable in the analysed
material. Distinct impoverishment of calcareous nannofossils
in zones NP23–24 in the Carpathian successions was earlier
observed by Oszczypko-Clowes (2001) and others. The dec-
line and reduced diversity of nannofossil species defining
zones NP23 and NP24 in the Cergowa beds can be related
to the Lower Oligocene icehouse (Haq et al. 1987, 1988;
Prothero 2003; Katz et al. 2008).
The presence of species in the samples 1I, 1T, 2T, 1R and
2R that are characteristic for brackish sea water environments
during the NP23 zone, namely Pontosphaera fibula,
Braarudosphaera bigelowii and Reticulofenestra ornata indi-
cates a decrease of salinity as a consequence of increased
intensity of freshwater supply (Nagymarosy & Voronina 1992;
Melinte 2005). This may suggest that, due to the global sea
level fall, the Dukla Basin became isolated from the Magura
Basin to the south and from the Silesian Basin to the north at
that stage of the Carpathian basins’ development. This infe-
rence corresponds to an earlier opinion, based upon the distri-
bution of the paleocurrent directions in the sandstone facies
(Ślączka 1959), that the Carpathian basins became isolated
from the Tethys and from each other at the turn of Eocene and
Oligocene.
On the other hand, calcareous nannofossils belonging to
zone NP24 prove the open sea conditions supported by simul-
taneous disappearance of brackish species and further cooling
of climate, documented by the occurrence of cryophilic species
such as Isthmolithus recurvus, Reticulofenestra lockeri and
R. ornata. Thus, the autochthonous nannofossils from the
Cergowa beds in the Dukla Basin document considerable
paleogeographical changes in the Tethyan Ocean at the end of
zone NP23. In particular, the previously isolated Paratethys
Basin became connected with Tethys, which resulted in the
open sea environment that was continuing through the Lower
Oligocene icehouse (Melinte 2005).
The Eocene (NP16), Eocene/Oligocene (NP21) and Meso-
zoic species of calcareous nannofossils recognized in the
Cergowa beds are redeposited, as indicated by their relative
position above the autochthonous fossils in the analysed pro-
files (Fig. 2). The species representing zone NP16 document
moderate temperature of sea water in the Late Lutetian and
Early Bartonian, while species representing zone NP21 show
higher temperature at the turn of the Late Priabonian and Early
Rupelian in the time of Eocene-Oligocene transition from
the high-diversity greenhouse to the glacial icehouse condi-
tions (Prothero 2003).
Discussion
Climatically controlled eustatic global sea-level fall resulted
in separation of the Carpathian basins from Paratethys in
the Early Oligocene (Haq et al. 1987, 1988; Kominz &
Pekar 2001; Piller et al. 2007; Katz et al. 2008). The direct
effect of that is recorded in the NP23 zone by the appearance
of brackish water nannofossils that are absent in the NP21
zone containing open marine assemblage (however recycled).
In the analysed samples, transformation from greenhouse to
icehouse during the Oligocene is reflected by a significant
transition from the nannofossil assemblage typical for a warm
climate in NP21 to the fossils characteristic for cold condi-
tions during NP24. This change may also be reflected by
EPOCH
ST
ANDARD
MEDITERRANEAN ST
AGES
CENTRAL
P
ARA
TETHYS
ST
AGES
ZONE
(Martini 1971)
OLIGOCENE
LA
TE
CHA
TTIAN
EGERIAN
NP25
KISCELLIAN
NP24
EARL
Y
RUPELIAN
NP23
NP22
NP21
EOCENE
LA
TE
PRIABONIAN
PRIABONIAN
NP19-20
NP18
MIDDLE
BAR
TONIAN
BAR
TONIAN
NP17
NP16
LUTETIAN
Table 3: Correlation of international (Mediterranean) and regional
(Central Paratethys) stages with standard nannoplankton NP zones
(Martini 1971).
322
PSZONKA, ŽECOVÁ and WENDORFF
GEOLOGICA CARPATHICA
, 2019, 70, 4, 311–324
the occurrences of brackish nannofauna, which is present in
the samples assigned to NP23, but absent from the overlying
strata belonging to NP24. In this respect, it is suggested that
the evolution of climate from warm to cold resulted in reduced
precipitation and consequently fresh water runoff into the
basin, which in turn reduced the volume and extent of
the brackish water environment during the time represented by
the nannofossil zone NP24.
Regionally autochthonous calcareous nannoplankton zones
NP23 (Rupelian) and NP24 (Late Rupelian/Early Chattian)
recognized here in the main area of the Cergowa beds occur-
rences, namely the Dukla and southern Silesian tectonic units,
correlate with nannoplankton zones recognized in the western
region of occurrences of this lithostratigraphic unit (Fig. 1).
The latter successions were assigned to the Fore-Magura group
of units (Oszczypko-Clowes & Oszczypko 2004, 2011;
Oszczypko- Clowes & Ślączka 2006; Oszczypko-Clowes 2008)
outcropping in the tectonic windows (Fig. 1) listed below and
dated as follows:
• the Mszana Tectonic Window — zones NP23–25,
• the Szczawa Tectonic Window — zone NP24,
• the Grybów Tectonic Window — zones NP24–25 and
• the Ropa Tectonic Window — zone NP25.
The calcareous nannoplankton zone NP25 has not been
identified in the analysed samples of the Cergowa beds.
However,the fact that it was recorded by the previous authors
in the lithostratigraphically equivalent strata out cropping in
the above-mentioned tectonic windows to the west of the
Dukla Tectonic Unit suggests that deposition of the Cergowa
beds in the western part of the basin lasted longer than in its
eastern part. Such stratigraphic relations, coupled with
regional direction of sediment supply towards the SE, indi-
cates that (i) the Cergowa beds become younger towards
the SE, with facies progradation from the onset of deposition
during NP23 in the NW and middle sections to NP24 in the SE
sections, and (ii) the final stage of deposition of the Cergowa
beds was characterized by retrogradation from NP24 in the SE
part of the Dukla Basin to NP25 in what is now the Mszana
area in the NW.
Conclusions
• The assemblages of autochthonous calcareous nannofossils
recognized in the Lower Oligocene-age Cergowa beds of
the Dukla Tectonic Unit indicate zones NP23 (Rupelian) for
the suprafan of the Cergowa depository represented by NW
and middle sections and NP24 (Late Rupelian/Early
Chattian) for the outer fan parts in SE sections.
• Nannoplankton zones younger than NP23 and older than
NP24 were not found in the Cergowa beds of this part of
the Flysch Carpathians.
• The documented nannofossil species reflect the Lower
Oligocene climate, paleogeographical and paleoecological
changes. They document the Eocene-Oligocene transition
from greenhouse to icehouse, closure and subsequent
opening of the Parathetys Basin and its partial connection to
the Mediterranean and the related salinity fluctuations.
• A relatively high number of reworked specimens derived
from strata containing nannofossil assemblages older than
the NP23 zone and redeposited into the uppermost, mud-
stone-rich parts of the analysed sections, may be related to
remobilization and redeposition of the older, mostly fine-
grained deposits affected by the orogenic tectonic move-
ments at the margin of the basin: (i) the uppermost part of
the Hieroglyphic beds, the Przybyszów sandstones and
the Upper variegated shales representing zone NP16, and
(ii) the Globigerina marls, Mszanka sandstones and sub-
Chert marls and shales associated with zone NP21.
• Absence of nannofossils indicative of zone NP23 in the sec-
tions Habura and Medzilaborce suggests migration of the
Cergowa beds depositional area to SE sections.
• Absence of calcareous nannofossils indicating the NP25
zone in the studied area in contrast to their presence in
the tectonic windows further to the west reflect a longer
deposition time of the Cergowa beds in the western part of
the Dukla Tectonic Basin.
Acknowledgements: Professor Andrzej Ślączka is thanked
for helpful discussion of various age aspects of the Cergowa
beds. The Management of the Przedsiębiorstwo Materiałów
Drogowych w Rzeszowie sp. z o.o. kindly allowed us to con-
duct field work and collect samples in their Lipowica Mining
Licence area; we are grateful for this permission. RNDr. Lilian
Švábenická, two anonymous reviewers and the handling editor
Prof. Ján Soták are sincerely thanked for constructive recom-
mendations, which enabled us to considerably improve an ear-
lier version of the manuscript. Dr. Zoltán Németh is thanked
for help with the English grammar, and MSc. Paweł Godlewski
is thanked for help in drafting Figures 1 and 2. A part of this
work was carried out by MW as the AGH Statutory Research
No. 11.11.140.626.
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Appendix
Braarudosphaera bigelowii (Gran & Braarud, 1935) Deflandre,
1947
Chiasmolithus grandis (Bramlette & Riedel, 1954) Radomski, 1968
Chiasmolithus oamaruensis (Deflandre & Fert, 1954) Hay, Mohler
& Wade, 1966
Coccolithus eopelagicus (Bramlette & Riedel, 1954) Bramlette &
Sullivan, 1961
Coccolithus formosus (Kamptner, 1963) Wise, 1973
Coccolithus pelagicus (Wallich, 1877) Schiller, 1930
Cyclicargolithus abisectus (Müller, 1970) Wise, 1973
Cyclicargolithus floridanus (Roth & Hay, in Hay et al., 1967) Bukry,
1971
Helicosphaera compacta Bramlette & Wilcoxon, 1967
Helicosphaera euphratis Haq, 1966
Helicosphaera recta (Haq, 1966) Jafar & Martini, 1975
Isthmolithus recurvus Deflandre & Fert, 1954
Lanternithus minutus Stradner, 1962
Pontosphaera fibula Gheta, 1976
Pontosphaera latelliptica (Báldi-Beke & Baldi, 1974) Perch-Nielsen,
1984
Pontosphaera multipora (Kamptner, 1948 ex Deflandre in Deflandre
& Fert, 1954) Roth, 1970
Pontosphaera obliquipons (Deflandre, 1954) Romein, 1979
Reticulofenestra bisecta (Hay, Mohler & Wade, 1966) Roth, 1970
Reticulofenestra lockeri Müller, 1970
Reticulofenestra ornata Müller, 1970
Reticulofenstra reticulata (Gartner & Smith, 1967) Roth &
Thierstein, 1972
Reticulofenestra umbilica (Levin, 1965) Martini & Ritzkowski, 1968
Zygrhablithus bijugatus (Deflandre & Fert, 1954) Deflandre, 1959