GeolCarp_Vol66_No1_51

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, FEBRUARY 2015, 66, 1, 51—67 doi: 10.1515/geoca-2015-0010

Biostratigraphy, sedimentology and paleoenvironments of

the northern Danube Basin: Ratkovce 1 well case study

SAMUEL RYBÁR

, EVA HALÁSOVÁ

, NATÁLIA HUDÁČKOVÁ

, MICHAL KOVÁČ

MARIANNA KOVÁČOVÁ

KATARÍNA ŠARINOVÁ

and MICHAL ŠUJAN

Department of Geology and Paleontology, Faculty of Natural Sciences, Comenius University, Mlynská dolina G, 842 15 Bratislava,

Slovak Republic; samuelrybar3@gmail.com; halasova@fns.uniba.sk; hudackova@fns.uniba.sk; kovacm@fns.uniba.sk; kovacova@fns.uniba.sk

Department of Mineralogy and Petrology, Faculty of Natural Sciences, Comenius University, Mlynská dolina G, 842 15 Bratislava,

Slovak Republic; sarinova@fns.uniba.sk

(Manuscript received April 24, 2014; accepted in revised form December 10, 2014)

Abstract: The Ratkovce 1 well, drilled in the Blatné depocenter of the northern Danube Basin penetrated the Miocene
sedimentary record with a total thickness of 2000 m. Biostratigraphically, the NN4, NN5 and NN6 Zones of calcareous
nannoplankton were documented; CPN7 and CPN8 foraminifer Zones (N9, 10, 11 of the global foraminiferal zonation;
and MMi4a; MMi5 and MMi6 of the Mediterranean foraminiferal zonation were recognized. Sedimentology was based
on description of well core material, and together with SP and RT logs, used to characterize paleoenvironmental condi-
tions of the deposition. Five sedimentary facies were reconstructed: (1) fan-delta to onshore environment which devel-
oped during the Lower Badenian; (2) followed by the Lower Badenian proximal slope gravity currents sediments;
(3) distal slope turbidites were deposited in the Lower and Upper Badenian; (4) at the very end of the Upper Badenian
and during the Sarmatian a coastal plain of normal marine to brackish environment developed; (5) sedimentation fin-
ished with the Pannonian—Pliocene shallow lacustrine to alluvial plain deposits. The provenance analysis records that
the sediment of the well-cores was derived from crystalline basement granitoides and gneisses and from the Permian to
Lower Cretaceous sedimentary cover and nappe units of the Western Carpathians and the Eastern Alps. Moreover, the
Lower Badenian volcanism was an important source of sediments in the lower part of the sequence.

Key words: Danube Basin, Blatné depression, Middle and Upper Miocene, biostratigraphy, sedimentology, sedimentary
petrology, depositional systems.

Introduction

The Danube Basin, located at the junction of the Eastern Al-
pine,  Western  Carpathian  and  Transdanubian  Range,  repre-
sents  an  important  depocenter  of  the  Pannonian  Basin
System on its north-western margin (Kováč 2000). The basin
is divided into finger like bays situated between the Western
Carpathian core mountains (Malé Karpaty, Považský Inovec,
and  Tríbeč  Mts),  and  from  W  to  E  known  as  the  Blatné,
Rišňovce  and  Komjatice  depressions  (Vass  2002).  In  the
Blatné Depression, the Ratkovce 1 well (Lat: 48° 29’4.2216”
Lon:  17° 55’48.3528”)  penetrates  the  Middle  and  Upper
Miocene  sedimentary  record  (Fig. 1).  The  studied  well,
along  with  multiple  other  wells  was  drilled  for  petroleum
prospecting in the late 1960s and 1970s, and was technically
documented  in  a  drilling  report  (Imrichová  1969).  Litho-
stratigraphy,  biostratigraphy  and  geophysical  measurements
were compiled adequate to current knowledge and methods.
Isopach maps of the basin sedimentary fill were worked out
by Adam & Dlabač (1969), and later the available well data
were summarized by Biela (1978), without revision of sedi-
mentology,  and  only  with  scarce  refining  of  existing  bio-
stratigraphy.  Reinterpretations  of  the  older  geophysical
data in the 1990s were carried out by Hrušecký et al. (1993,
1996). Complex studies of the paleogeography, geodynamic
evolution,  and  sequence  stratigraphy  of  the  Carpathian-
Pannonian  region  during  the  Miocene  were  published  by

Kováč et al. (1999), and Kováč (2000). Paleoflora, paleocli-
mate and Miocene landscape was analysed in the papers of
Kvaček et al. (2006), Kováč et al. (2006, 2011) and
Kováčová et al. (2011). Andreyeva Grigorovich et al. (2003),
Harzhauser et al. (2007), Harzhauser & Mandič (2008), and
Hohenegger et al. (2014) enriched the integrated stratigraphy
of the Central Paratethys, with possible implications for the
Danube Basin.

Revision and re-evaluation of the well-core material from

the  Ratkovce 1  borehole  after  more  than  45  years,  using  ad-
vanced  methods  of  biostratigraphy,  sedimentology  and  geo-
physics  should  contribute  not  only  to  clarify  the  models  of
basin  evolution,  but  also  the  paleogeography  and  geodyna-
mics of adjacent area (the works were carried out in the scope
of the SRDA Project 0099-11 Danube).

Geological setting

Opening of the Danube Basin was caused by Badenian

rifting  over  an  asthenospheric  upwelling,  like  in  the  whole
Danube  Basin  area  (Lankreier  et  al.  1995;  Konečný  et  al.
2002). A NW-SE orientated transtensional regime was active
during the entire Middle Miocene. In the latest Miocene ther-
mal  subsidence  set  in  and  subsequently  deltaic  and  alluvial
sediments filled the depocenter (Tari et al. 1992; Tari & Hor-
váth 1995; Kováč 2000; Horváth et al. 2006).

RYBÁR, HALÁSOVÁ, HUDÁČKOVÁ, KOVÁČ, KOVÁČOVÁ, ŠARINOVÁ and ŠUJAN

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Fig. 1. Geological maps of (A) the Danube Basin, (B) Western Slovakia and (C) the Blatné Depression and its surroundings, with the position of
the Ratkovce 1 well marked. Explanatory notes to A and B: 1 – Inner Alpine-Carpathian-Dinaride Units, 2 – Pieniny Klippen Belt, 3 – Neo-
gene volcanic fields, 4 – Alpine and Outer Carpathian Flysch Belt, 5 – Neogene basins (modified from Kováč et al. 2011).  Explanatory
notes to C: a – mostly clays, silts, sands, gravels and rare lignite seams (Late Miocene—Pliocene); b – clays, claystones, siltstones, sands,
sandstones,  gravels,  conglomerates,  subordinate  evaporites,  algal  limestones,  coal  seams  and  andesite  tuffites  and  epiclastic  volcanic  rocks
(Middle Miocene); c – claystones, siltstones, sands, sandstones, gravels, conglomerates, subordinate evaporites, organodetritic limestones,
coal seams and rhyolite tuffs and tuffites (Early Miocene); d – conglomerates, sandstones, limestones, breccias (Paleocene—Eocene); e – marls,
limestones, sandstones, conglomerates (Late Cretaceous); f – shales, marls, sandstones, conglomerates – mostly flysch (Late Cretaceous—
Eocene); f-a – klippen of Jurassic—Early Cretaceous radiolarites and limestones; g – limestones, marly limestones, marlstones, shales, sand-
stones  (Early  Cretaceous);  h  –  sandy,  crinoid,  mottled,  radiolarian  and  nodular  limestones,  cherts,  shales  (Jurassic);  i  –  limestones,
dolomites, locally shales and sandstones (Middle—Upper Triassic); j – calcareous shales, shales, sandstones and quartzites (Early Triassic);
k – variegated conglomerates, sandstones and shales, locally evaporites and volcanic rocks (Permian); l – phyllites and mica shists with
metavolcanite horizons (Proterozoic?—Early Paleozoic); m – paragneisses, mica shists and migmatitic gneisses (Proterozoic?—Early Paleozoic);
n – orthogneisses and migmatites with amphibolites and paragneiss layers (Proterozoic?—Early Paleozoic); o – granitoids, granites, grano-
diorites, tonalites (Late Devonian?); p – geological boundaries; r – faults: a – assumed, s – nappe and overthrust lines, t – areas where depth
to basement exceeds 2000 m, u – areas where depth to basement exceeds 4000 m. Modified from Biely et al. (1996) and Kováč et al. (2011).

STRATIGRAPHY, SEDIMENTOLOGY AND ENVIRONMENTS OF N DANUBE BASIN (SLOVAKIA)

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The sedimentary sequence of the Ratkovce 1 well in the

Blatné  depression  begins  with  the  earliest  Badenian  strata,
deposited unconformably above the pre Neogene basement.
After the latest Karpatian/earliest Badenian terrestrial depo-
sition, the whole area was flooded by a transgression, which
led  to  the  shallow  to  deep  marine  environment  of  the
Špačince and Báhoň formations, which persisted during the
whole  Early  and  Late  Badenian  (Vass  2002;  Kováč  et  al.
2007). During the Sarmatian, the marine environment gradu-
ally changed to brackish and the Vráble Formation was de-
posited (Vass 2002; Kováč et al. 2007). The Upper Miocene
succession  is  built  up  by  the  lacustrine  Ivánka  Formation,
which passes into the shallow water to swamp environment
of the Beladice Formation (Kováč et al. 2010). Sediments of
the  delta  to  alluvial  plain  are  represented  by  the  Volkovce
Formation (Upper Miocene to Pliocene) and in some places
are overlain by the Pliocene to Pleistocene deluvial to alluvial
Kolárovo Formation (Kováč et al. 2011).

Material and methods

Well core material was obtained from the well repository of

Nafta a.s. situated in the town of Gbely. For the micropaleon-
tological  analysis,  45  rock  samples  were  collected  and  pro-
cessed  by  standard  preparation  methods  (described  in
Kováčová & Hudáčková 2009). Calcareous nannofossils were
analysed  quantitatively  in  smear  slides  prepared  from  all
lithologies  by  the  standard  techniques  (e.g.  described  in
Švábenická  2002;  Jamrich  &  Halásová  2011).  Slides  were
studied  under  an  Olympus  BX 50  polarizing  microscope
(magnification  1250

×). For biostratigraphic interpretations

nannoplankton  and  foraminiferal  associations  were  used,  in
the sense of the standard zonation of Grill (1941) and Cicha et
al.  (1975),  the  stratigraphic  ranges  of  foraminifers  follow
Cicha  et  al.  (1998),  Wade  (2011),  Iaccarino  et  al.  (2011),
Turco et al. 2011 and Gradstein et al. (2012). Calcareous nan-
noplankton  was  compared  with  the  standard  NN  zones  after
Martini  (1971).  The  current  status  of  the  Miocene  Central
Paratethys  stratigraphy  correlation  between  the  Central  Para-
tethys  regional  stages  and  the  Mediterranean  scale  summa-
rized  by  Piller  et  al.  (2007),  Kováč  et  al.  (2007)  and
Hohenegger (2014) was used to range stratigraphically impor-
tant  taxa  found  in  the  Ratkovce 1  well  cores  (Fig. 2).  Paleo-
ecological  parameters  were  evaluated  for  samples  containing
at  least  200  individuals  of  benthic  foraminifers  on  the  pres-
ence and dominance of taxa, exhibiting special environmental
significance.  Species  with  similar  environmental  importance
were grouped to enable better interpretation of their distribu-
tional patterns. In order to identify and characterize changes in
the assemblage structures and to relate these to changing envi-
ronmental  conditions  for  general  interpretation,  the  data  was
treated statistically using the PAST software (Hammer et al.
2001).  Assemblage  structures  and  environmental  stress  of
the foraminifers were investigated through diversity indices
(Simpson,  Shannon-Wiener  –  H’  and  Evenness  –  J’).
Taphonomic analysis of the foraminiferal assemblage in the
studied  samples  was  done  and  evaluated  according  to  the
methods described by Holcová (1997, 1999).

The preparation of palynological samples followed stan-

dard laboratory methods (e.g. Erdtman 1943; Faegri & Iversen
1989; Moore et al. 1991). During the procedure 20 g of dry
sediment was treated with cold HCl (35%) and HF (70%) to
remove carbonates and silica and by using ZnCl

(heavy liq-

uid with density = 2 g/cm

); palynomorphs were extracted in

a centrifuge.

For provenance determination, coarse grained samples

were  selected  and  studied  under  a  polarization  microscope.
Heavy  mineral  analysis  was  done  using  the  0.25—0.10 mm
fraction,  which  was  studied  under  a  binocular  microscope,
and confirmed by an EDAX analysis. Garnets were analysed
by a WDS quantitative analysis, with the microprobe Camera
SX-100 at the Geological Institute of Dionýz Štúr, Bratislava,
Slovak  Republic.  Measurement  conditions:  15 keV  20 nA.
Standards:  LiF  (F K

α), albite (Na Kα), orthoclase (Si Kα),

(Al K

α), forsterite (Mg Kα), NaCl (Cl Kα), orthoclase

(K K

α), wollastonite (Ca Kα), TiO

(Ti K

α), fayalite (Fe Kα),

rodonite (Mn K

α), Cr (Cr Kα). Garnet analysis was calculated

based on 8 cations. The Fe

and Fe

charge balance was cal-

culated to ideal stechiometry. Photo-documentation of the
separated clasts was done by a trinocular stereomicroscope
(Olympus KL 1500 LCD) and the QuickPHOTO MICRO 3.0
software was used.

For the purposes of the sedimentological analysis 31 well

core  samples  were  collected,  all  available  cores  and  their
sampler  cards  were  photographed.  Then  the  samples  were
cut in half perpendicular to the bedding plane, washed, and
treated  for  preservation  with  dispersive  glue  (WURSTOL
and HERKULES), scanned, digitalized and finally the sedi-
mentary textures and structures were documented, mainly in
the  sense  of  Miall  (2010).  Further,  the  evaluation  of  a  well
was based on spontaneous potential (SP) and resistivity (RT)
core  logs.  The  curves  originally  constructed  by  Moravské
naftové  doly,  n.p.  (Imrichová  1969)  were  interpreted  based
on  Rider  (1986),  Emery  &  Myers  (1996)  and  Catuneanu  et
al. (2011).

Biostratigraphy and paleoecology of the Ratkovce 1 well
core record

The first biostratigraphical ranking of the well cores was

done by Jandová (in Imrichová 1969). Thanks to a very well
preserved  and  rich  assemblage  of  planktonic  foraminifera,
yielding  Globigerina (Zeaglobigerina) decoraperta  (Takay-
anagi  &  Saito)  and  Globigerina  (Zeaglobigerina)  druryi
(Akers) in the upper part of well core 6 – Cicha et al. (1975)
established  this  material  as  the  “holotype”  of  the  Middle
Badenian  planktonic  foraminiferal  Zone  CPN8  Globigerina
druryi—Globigerina decoraperta. This zone was correlated by
Cicha  et  al.  (1975)  with  the  NN5  nannoplankton  Zone;  al-
though  the  calcareous  nanoplankton  assemblage  was  never
studied in the well.

The re-evaluation of cores brought new data: the NN4

Zone  of  calcareous  nannoplankton  was  detected  from  the
base up to the well core 18 (1667—1670 m) based on the co-
occurrence  of  the  Sphenolithus  heteromorphus,  Heli-
cosphaera  scissura  and  rare  H.  ampliaperta.  This  zone
represents  the  Karpatian—lowermost  Badenian  stage  of  the

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Fig. 2. Passport of the Ratkovce 1 well. Biostratigraphy column shows first occurrences (FO) and last occurrences (LO) of important index
foraminifers and nannoplankton, as well as nannoplankton biozones (with black arrows) as were identified in the studied material. Correla-
tions between Central Paratethys and standard chronostratigraphy modified from (Kováč et al. 2000, 2007, 2011; Hohenegger et al. 2014).

Fig. 3.  1  – Globigerinoides quadrilobatus (d’Orbigny), Rat1/11A/1/10; 2 – Globigerinoides quadrilobatus (d’Orbigny), Rat1/2/1/30;
3 – Globigerinoides quadrilobatus (d’Orbigny), Rat1/19/2/20; 4 – Orbulina suturalis Brönnimann, Rat1/12/1/10; 5 – Globigerinoides
cf. sicanus De Stefani, Rat1/12/1/10; 6 – Catapsydrax sp. cf. parvulus Bolli, Loeblich & Tappan; 7 – Globigerina regularis d’Orbigny;
8  –  Globorotalia  partimlabiata  Ruggieri  &  Sprovieri,  Rat1/6/3/25;  9  –  Globorotalia  sp.,  Rat1/6/3/50  (not  in  WFD); 10  – Globigerina
woodi decoraperta Takayanagi & Saito, Rat1/6/3/25; 11 – Globigerina druyi Akers, Rat1/6/3/25; 12 – Turborotalita quinqueloba (Natland),
Rat1/19/2/20; 13 – Helicosphaera ampliaperta (Bramlette & Wilcoxon), Rat1/19/2/70; 14 – Sphenolithus heteromorphus (Deflandre),
Rat1/19/2/70; 15 – Helicosphaera mediterrannea (Müller), Rat1/19/2/20; 16 – Helicosphaera scissura (Miller), Rat1/19/2/20; 17 – Heli-
cosphaera scissura (Miller), Rat1/23/2/43; 18 – Sphenolithus heteromorphus (Deflandre), Rat1/23/2/43; 19 – Reticulofenestra pseudoumbi-
licus  7 µm  (Gartner)  Gartner,  Rat1/6/3/25;  20  –  Reticulofenestra  haqii  (Backman),  Rat1/6/3/25;  21  –  Calcidiscus  premacintyrei
(Theodoridis),  Rat1/6/3/25;  22  –  Umbilicosphaera  rotula  (Kamptner),  Varol,  Rat1/6/3/25;  23  –  Sphenolithus  heteromorphus  Deflandre,
Rat1/18/2/35; 24 – Discoaster variabilis (Martini & Bramlette), Rat1/6/3/25; 25 – Helicosphaera walbersdorfensis Müller, Rat1/6/6/75.

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The foraminiferal assemblage in these sediments is typical
for the CPN8 Zone, based on the FO of Globigerina druryi
(Akers) together with G. woodi decoraperta (Takayanagi &
Saito). In the sediments of core 5, the acme of Paragloboro-
talia siakensis LeRoy (?synonyme of Globorotalia partimla-
biata Ruggieri & Sprovieri) was detected.

Classical “lagenide” and “agglutinated” zones of the Lower

and  Middle  Badenian  based  on  benthic  foraminifera  were
not  identified  in  the  studied  well  profile,  in  contrast  to  the
very  well  developed  Bolivina/Bulimina  Zone  (sensu  Grill
1941;  Cicha  et  al.  1975).  These  zones  were  strongly  linked
to changes of environmental conditions and do not appear to
be  stratigraphically  significant.  In  spite  of  the  fact,  that  the
well  core6  was  formerly  assigned  to  the  Middle  Badenian
(Wieliczkian)  in  the  sense  of  our  recent  results  these  sedi-
ments represent the Upper Badenian age, associated with the
NN6 Zone (sensu Kováč et al. 2007; Hohenegger et al. 2014).

For paleoecological purposes, benthic foraminifera domi-

nance,  diversity  and  similarity  diagrams  were  constructed,
moreover  a  diversity  ratio  graph  was  added  (sensu  Murray
2006 – Fig. 4). Samples from the well cores 25, 23, 21, 18,
17 cluster in brackish marsh to normal marine environments
and confirm the deltaic to onshore position of sedimentation.
Faunal associations from the well cores 12 and 14 appear in
shelf  to  offshore  deep  marine  environments.  Nevertheless
some associations are clustered in a shallow marine environ-
ment,  mainly  in  the  samples  from  well  cores 13  and  11A,
therefore this mixture of shallow and deep marine elements
is  interpreted  as  a  re-deposition  of  foraminifera.  Moreover,
this statement is based on signs of size sorting and abrasion
of the foraminiferal tests. The majority of associations from
cores 6, 5, 4, and 2 appear to be clustered in deep marine off-
shore to shelf conditions with low energy environment. But
on the other hand a couple of associations from these cores
are scattered in-between normal marine, hypersaline lagoons
and  brackish  march  environments.  This  fact  again  confirms
re-deposition from a shallow water environment, also docu-
mented by the colour and bad preservation of tests (Fig. 3).

A palynological record from the Lower Badenian sedi-

mentary  fill  shows  rare  palynomorphs,  poor  in  quality  of
preservation, probably due to the higher oxidation rates. Ob-
tained pollen, spores and algae assemblages have been char-
acterized by rare occurrence and a high degree of corrosion.
They  include:  Ulmus,  Carya,  Pinus,  Pterocarya,  Cathaya,
Myrica,  Castanopsis,  Quercus,  Sapotaceae,  Polypodiaceae,
Dinoflagellata  and  Acritarcha.  The  samples  contain  a  high
amount  of  diverse  palyno-debris  including  reworked  ones,
pointing to dynamic transport conditions into the accumula-
tion space.

The Upper Badenian sediments contained very well pre-

served  and  diversified  palynomorph  associations.  Azonal
(coastal and swamp) vegetation was represented by  Myrici-
pites  bituides,  M.  myricoides  Sparganium,  Glyptostrobus,
Nyssa,  and  Cyperaceae.  Zonal  vegetation  was  documented
by  the  fern  spores  Polypodiaceae,  pollen  Pterocarya,  Sym-
plocos,  Cercidiphyllum,  Carya,  Carpinus,  Quercus,  Engel-
hardia,  Castanopsis,  Sapotaceae  and  a  high  amount  of
Pinus.  Extrazonal  mountain  related  vegetation  is  presented
by  Picea,  Abies,  Cathaya  and  Tsuga.  The  character  of  the

palynomorphs’ preservation, together with the high ratio of
dinoflagelates, acritarchs, foraminiferal test linings and fungi
spores confirm their fast burial without damage in the basi-
nal environment.

Sedimentology and depositional environments of the Rat-
kovce 1 well record

The sedimentary textures, structures and the shape of the

SP and RT logs were described from bottom to top (Figs. 2,
5 and 6). The basal part of the well sequence is composed of
conglomerates  with  intercalations  of  sandstones,  siltstone
and  claystones,  resembling  the  Jablonica  Formation  (e.g.
Kováč et al. 1989). Sediments are composed of a matrix sup-
ported conglomerate with fine to coarse grained, subangular
to  well  rounded  pebbles,  including  carbonate,  quartzite,
granitoid and volcanic pebbles (some clasts reach up to 5 cm
in  diameter).  The  matrix  is  represented  by  coarse  to  fine
grained  sand.  Some  samples  of  the  well  core  contain  indis-
tinct  5—15 cm  thick  fining  upwards  conglomerate  layers,
cross-bedding  and  clay  intraclasts  –  armoured  mud  balls
(Fig. 5).  The  lower  cores  (26—24;  Fig. 2),  in  contrast  to  the
upper cores (23—19; Fig. 2) do not contain Miocene volcanic
admixture (Jablonica Formation s.s.). Occasionally, the con-
glomerates  of  upper  cores  pass  into  coarse  grained  lithic
sandstone  and  brown  claystone.  This  fabric  points  to  high
density gravitational flows during the high order cyclicity of
relative  sea  level  changes  (parasequence  sets).  Heterolithic
sediments composed of claystone and sandstone with possi-
ble  ripple  cross  lamination  indicate  onshore  environments
(Fig. 5). In claystones abundant mica, macrofauna fragments
(echinoids)  and  carbonized  plate  fragments  were  observed.
The 70—90° dip of the bedding in rhythmically layered clay-
stone and siltstone might have been caused by syn-sedimen-
tary  tectonics  due  to  transtensional  faulting  during  opening
of the Blatné Depression (1753—1758 m); or by normal fault-
ing in the delta front environment. The SP log shape is charac-
terized by 3 funnel shape trends changing from a positive to a
negative anomaly with a sharp border at the top of cycles. We
interpret them as coarse grained deltaic facies with prograda-
tional  parasequence  sets  and  minor  deepening  in-between
(Fig. 2). The first (oldest) cycle appears at 1990—1900 m; the
second cycle at 1900—1750 m and the third at 1750—1680 m.
The  RT  log  confirms  tight  coarse  clastic  material  in  the  first
cycle, while the second and third cycles are not visible in the
shape  of  RT  curve.  This  fact  can  also  be  explained  by  the
composition of well cores, which are no longer built up pre-
dominantly from conglomerate and sandstone but also contain
claystone and siltstone (Fig. 5). The onshore sedimentary en-
vironment of the deposition of conglomerate and sandstone is
also confirmed by the foraminiferal assemblage diversity ratio
belonging  to  a  marsh—brackish  environment,  as  well  as  by
pollen analysis with pollen mean dissemination values (sensu
Dyakowska 1959) and character of preservation of their exine,
pointing out dynamic transport conditions.

The overlying sequence can by divided into two parts. The

lower part (1680—1300 m) is composed of pale brown to
grey, bioturbated claystone and siltstone which contains
mica, carbonized plant fragments, macrofauna (bivalves and

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echinoid  fragments)  and  scarce  ripples.  Layered  diamictite
(pebbly claystone) in the depth 1503—1508 m is poorly sorted
(clasts  reach  up  to  5 cm  in  diameter)  and  we  interpret  it
as  debris  flows  on  the  basin  proximal  slope  (Fig. 6).  The
overlying sediments pass into turbidite sequences with hori-
zontal – ripple cross – lamination and flame structures. On
some  lithoclasts  CaCO

encrustation growth rings (pisoide)

were observed, and this validates re-deposition of the grains
from high energy shallow water conditions into a deeper low
energy environment.

The upper (1300—670 m), predominantly mudstone se-

quence is composed of pale brown to grey claystone and silt-
stone;  rare  layers  of  fine  grained  sandstone  are  present,  as
well.  The  sedimentary  succession  contains  occasional  part-
ing  lineation  indicating  upper  flow  regime  and  distal  thin
bedded  turbidity  current  transport  in  the  offshore  environ-
ment.  Parting  lineation  could  be  confused  with  traction
marks (Fig. 6).

The SP and RT logs from 1680 to 670 m show a serrated

shape which represents alterations of thin layers of sandstone
and  claystone,  indicating  frequent  changes  of  depositional
conditions confirming interpreted turbidity current transport.
Moreover,  influence  of  strong  storm  activity  cannot  be  ex-
cluded  here  (tempestites).  The  excursion  of  the  RT  log  at
around  1500 m  correlates  well  with  the  diamictite  recog-
nized in the well core material (core 14, Fig. 6). Nevertheless
this excursion on the RT log could also by explained by satu-
ration with salt waters. Sedimentology and interpretations of
the  log’s  pattern  (1680—670 m)  correspond  well  with  fora-
minifers’ diversity ratio (Fig. 3) referring to an onshore shelf
environment with gradual passage to the offshore deep marine
environment.  The  foraminiferal  associations  display  a  reduc-
tion of the shallow water species towards the upper part of the
sequence,  which  is  confirmed  additionally  by  pollen  data
pointing to their fast burial without damage on the basin floor.

The top part of the existing well cores is built up by con-

glomerate composed of angular fragments (possibly intrafor-
mational) of laminated sandstone and siltstone in siltstone to
claystone matrix (Fig. 6); carbonized plate fragments are
abundant. These sedimentary structures may be interpreted

as  coastal  plain  or  tidal  lag  deposits  (sense  Mial  2010).  On
the  SP  log  cylindrical  and  bell  -shaped  excursions  were  re-
corded (670—400 m). The basal cylindrical excursion can be
interpreted as a channel fill. The fining upwards trend of the
curved  upper  part  refers  to  a  shoreline  –  shelf  system
(Fig. 2), and documents a change from dynamic to calm en-
vironment (sensu Emery & Myers 1996). The RT log shows
gradual increase in resistivity, possibly caused by increasing
saturation of the sediment with ground water.

The uppermost part of the well belongs to the latest Mid-

dle and Upper Miocene (without well core material) and was
interpreted only with the help of available data from the
study area, as a brackish lake depositional environment (e.g.
Kováč et al. 2006, 2011).

Sedimentary petrology and provenance of sediment in the
Ratkovce 1 well record

The Ratkovce 1 well penetrates down to the basement rocks

recognized  already  in  the  original  drilling  report  as  Triassic
rocks formed by dark grey, dolomitized limestone cut by cal-
cite veins and intercalated by dark grey graphitic shale (Gaža
in  Imrichová  1969;  Biela  1978).  Nevertheless,  our  results
from the pre Neogene basement samples determined dark grey
to black limestone (wackestone) and calcareous shale. Poorly
recrystallized  limestones  (biomicrite)  containing:  abundant
calcificated  porifera  spicules,  filaments,  ostracods,  detritic
quartz  and  pyrite  alochems,  all  together  indicating  Jurassic
age which is in contrast to the original determination.

Furthermore, petrological study of clasts from the Mio-

cene sedimentary fill show that material was derived from
the crystalline basement of the neighbouring Eastern Al-
pine—Western Carpathian complexes, covered by the Meso-
zoic and Paleogene sediments.

Granitoid lithoclasts contain quartz, plagioclase, micro-

cline,  perthitized  feldspars  and  biotite  crystals,  plagioclase
with zonal structures, as well as a lesser amount of fragments
of  mica  schist  to  gneisses  composed  of  mica  and  quartz
which  were  derived  from  crystalline  complexes  (Fig. 7).
They most closely correspond in character to the granitoids at

Fig. 5. Sedimentary textures and structures: Core 27, Sampler-card 1 – Dark grey, tectonically disturbed, layered limestone cut by abun-
dant calcite veins; Core 25, Sampler-card 1 – (58—64 cm from the bottom): Brown to dark blue carbonate conglomerate, (clasts reach up
to 5 cm in diameter); Core 25, Sampler-card 1 – (30—34 cm from the bottom): Pale brown to grey pebbly claystone with armoured clay
intraclasts; Core 24, Sampler-card 2 – (30—51 cm from the bottom): Pale yellow to grey, coarse grained lithic, pebbly sandstone to con-
glomerate. Clasts reach up to 4 cm in diameter; Core 23, Sampler-card 1 – (60—65 cm from the bottom): Brown claystone, and pale yel-
low, lithic, sandstone with possible ripples (interpretation: heterolithic sediment indicating deposition in the neritic zone); Core 23,
Sampler-card 1 – (0—10 cm from the bottom): Pale grey coarse grained sandstone and fine grained conglomerate with possible cross bed-
ding (interpretation: slight change in velocity or depth of flow); Core 23, sampler-card 2 – laminated siltstone and claystone; Core 21,
sampler-card 1 – (50—62 cm from the bottom): Pale brown carbonate conglomerate (clasts up to 4 cm in diameter). The sandy matrix is
poorly sorted; Core 20, Sampler-card 2 – (25—40 cm from the bottom): Pale yellow, laminated siltstone and claystone. Layers dipping at
a 60°—70° angle (nearby fault?); Core 19, Sampler-card 4 – (0—1 cm from the bottom): Pale brown to grey claystone, abundant mica and
macrofauna fragments (echinoids) visible on the bedding planes; Core 18, sampler-card 1 – (35—37 cm from the bottom): Pale brown to
grey claystone, with ripple cross lamination and flame structures, abundant occurrence of mica; Core 17, Sampler-card 1 – (30—38 cm
from the bottom): Brown and pale yellow lithic sandstone and brown claystone with carbonized plant fragments; Core 17, Sampler-
card 1 – (40—50 cm from the bottom): Brown and pale yellow medium grained sandstone and grey claystone with carbonized plant frag-
ments, containing flame structures; Core 17, Sampler-card 1 – (50—55 cm from the bottom): Pale grey sandstone and grey claystone with
carbonized plant fragments and leniticular bedding. Used scale 1 cm.

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present outcropping in the Hlohovec block of the Považský
Inovec Mts, and in the Tríbeč Mts (Broska & Uher 1988).

The Triassic source material is documented by fragments

of poorly recrystallized mudstone with stylolites (Fig. 7), do-
lomitized  mudstone,  oolitic  grainstone,  quartzites  and  dark
partly  phylitized  silica  rich  shales  (lydite).  The  Jurassic
rocks are represented by spongolites and wackstones (Fig. 7)
with abundant porifera spicules, brachiopods, bivalves, echi-
noderm  fragments,  sparite  with  phosphatized  skeletons  of
vertebrates, a high amount of pyrite and carbonate siltstones
(composed of detritic quartz in carbonate matrix). The Lower
Cretaceous  age  of  source  material  is  proven  by  the  Berias-
sian  Calpionella  limestone  fragments  (Fig. 7).  Some  of  the
carbonate  clasts  are  sparitic.  Carbonate  breccia  clasts  and
sedimentary  cherts  with  no  internal  structure  are  also
present, but the age of such source material is unknown.

Volcanic debris is an important part of the source material

and  may  be  divided  into  several  categories:  1)  rather  rare,
significantly  altered  fragments  of  acidic  volcanic  rocks,
which  take  on  the  character  of  the  quartzite  greywacke  and
felsites (Fig. 8), and can clearly be associated with the Per-
mian  sediments  of  the  Malužiná  Formation  of  the  Ipoltica
Group  (Vozárová  &  Vozár  1988);  2)  volcanic  fragments  of
andesite  composition  are  subdivided  into:  a)  rare  highly  al-
tered volcanic clasts found from 1858 m to 1639 m depth in-
cluding  recrystallized  glassy  matter.  Phenocrysts  of  biotite
are preserved and plagioclase phenocrysts are completely re-
placed  by  calcite  (Fig. 8).  The  high  level  of  alteration  sug-
gests  that  they  originate  from  the  Permian  sediments,  but
their  affinity  to  the  Miocene  volcanic  rocks  cannot  be  ex-
cluded;  b)  volcanic  fragments  composed  of  very  well  pre-
served  phenocrysts  of  the  zonal  plagioclase  in  poorly
recrystallized glass matter (appearing from the depth of 1801
to  1353 m)  with  abundant  pseudomorphs  of  amphibole
shape, filled with secondary minerals (Fig. 8). Based on the
degree  of  glassy  matrix  recrystallization  in  lithoclasts  and
absence  of  quartz  phenocrysts,  we  believe  that  these  volca-
nic  epiclastic  fragments  (dacite/andesite  composition)  are
certainly  of  the  Miocene  age.  The  epiclastic  origin  of  this
volcanic material is supported by different stages of alteration
and  recrystallization  of  lithoclasts.  Moreover  their  rounded-
ness and absence of heavy minerals (amphibole and pyroxene)
supports this claim. The overlying strata (up from core 9) were
not used for determination of the provenance of sediments, be-
cause of the very fine grain size (clay to silt deposits).

Miocene paleogeography and geodynamic aspects

of the north-western Danube Basin’s evolution

The opening of the Danube Basin – Blatné depocenter

can  be  dated  to  the  end  of  NN4  Zone  accompanied  by  a
lowermost  Badenian  fan  delta  development  at  its  southern
margin  (LO  of  H.  ampliaperta  ~ below  14.91 Ma).  The  ba-
sin’s development followed after strong changes of tectonic
pattern and paleogeography of the Western Carpathians do-
main.  The  Early  Badenian  (Langhian)  subsidence  is  docu-
mented in the sedimentary record by gradual change from near
shore  environment  to  rapid  tectonically  controlled  deepening

of  the  basin.  The  development  of  the  distal  shore  –  slope
depositional system with gravity currents and turbidite deposi-
tion  took  place  during  the  NN5  nannoplankton  Zone  (LO  of
H.  ampliaperta  ~ abowe  14.91 Ma).  The  gradual  transition
from  onshore  –  proximal  slope  to  offshore  environment  is
marked  by  the  last  occurrence  of  coarse  grained  sediments
above the base of the Špačince Formation (Fig. 2). In these
cores the presence of  O. suturalis was detected for the first
time (core 14), and continued in the deep water deposits up
to  the  Upper  Badenian  sediments  of  the  Báhoň  Formation
(up  to  core 5).  The  Lower  Badenian  deep  water  environ-
ment’s  continuation  up  to  the  lower  part  of  the  Late  Bade-
nian  NN6  Zone  is  not  supported  by  the  presence  of
S. heteromorphus (LO 13.53 Ma – sensu Kováč et al. 2007;
Hohenegger  et  al.  2014),  because  its  last  occurrence  was
documented in the middle of the Lower Badenian sedimentary
record (in core 12). In the Upper Badenian (Early Serraval-
ian),  dated  by  the  FO  of  Globigerina  druryi,  Sphenolitus
abies  and  Helicosphaera  walbersdorfensis  (Fig. 2),  the  off-
shore deep water facies development gradually  changed  to  a
shallow  water  environment  during  the  NN6  nannoplankton
Zone  ( ~ 13.82—12.83 Ma  –  sensu  Hohenegger  et  al.  2014),
which confirms the assumed calming of tectonic activity and
filling  of  the  basin.  During  the  Sarmatian  and  Pannonian
(Upper Seravalian—Tortonian), a shallow water coastal plain,
brackish to lacustrine environments were followed by devel-
opment  of  an  alluvial  plain  ( ~ 12.8—11.6—8.9 Ma)  –  sensu
Kováč et al. (2011).

As already mentioned, the provenance analysis of the clastic

material suggests sources in granitoids and mica shists/gneis-
ses. This can be additionally confirmed by the composition of
the heavy mineral fraction, which is relatively poor and con-
sists of: Gt, St, Ap, Tur, Rt, Zr, Py, Ilm, Bt, Cl, Glt. Among
the transparent heavy minerals, garnets of almandine compo-
sition are dominant (Fig. 9, Table 1) and they contain inclu-
sions of titanite, turmaline, rutile and ilmenite. In addition the
crystallo-chemical composition corresponds to garnets occur-
ring in granitoids and schist. Nevertheless a small amount of
garnets might have been derived from the Miocene volcanic
rocks or recycled from dissolved Mesozoic carbonate rocks.

Fig. 9. Composition of garnets.

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Defining the precise provenance area of the basal conglom-

erates  (Jablonica  Formation)  in  the  Ratkovce 1  well,  we  as-
sume  sources  in  a  part  of  the  pre-Neogene  basement  of  the
Danube  Basin  central  zone,  which  were  uplifted  during  the
Oligocene—Early  Miocene.  In  the  early  Lower  Badenian,  the
pebbles were transported from here toward the north. The up-
lifted  mountain  chains  around  the  basin  not  only  contained
crystalline  complexes  (similar  to  the  granitoids  in  the  Hlo-
hovec  block)  and  the  Mesozoic  nappe-stack,  but  were  also
covered  by  younger  sediments,  which  were  completely  ex-
humed,  eroded  and  transported  by  river  systems  toward  the
Blatné  Depression.  The  presence  of  strata  which  formed  the
paleo-surface  of  the  provenance  area  up  to  the  beginning  of
the Middle Miocene is documented by redeposits of the Upper
Cretaceous to Paleogene microfossils in the well core samples.

Extensional rifting of the basin (Blatné Depression) led to

deposition of a sedimentary sequence about 300 m thick de-
rived from volcanic epiclastic material (Figs. 2, 8 and 10).
A marine sedimentary environment is confirmed by the pres-
ence of framboidal pyrite, glauconite, pisoides and bioclasts
(Fig. 10). Nevertheless individual volcanoes must have
reached above sea level and are today buried below the sedi-
mentary fill of the northern Danube Basin. Their existence is
supported by the interpretation of seismic lines (line: 558—86
and MXS2-93 – Hrušecký 1999), as well as by the lithology
of cores in surrounding wells (Biela 1978).

Conclusions

! Re-evaluation of the Ratkovce 1 well core using ad-

vanced methods of biostratigraphy, paleoecology, sedimen-
tology and geophysics helped us to understand the
development of depositional systems in the northern Danube
Basin, as well as bringing important data affecting “state of
art” models of Central Paratethys paleogeography;

! In contrast to previous studies, the biostratigraphical

results confirmed the presence of the NN4, NN5 and NN6
calcareous nannoplankton Zones and local CPN7 a CPN8

Table 1: Chemical composition of garnet calculated on the 8 cations base. Fe

was calculated to ideal stoichiometry.

Ratkovce

1 1 2 3 4 5 6 7 8 9 10

SiO

37.31

36.85

37.74

37.82

37.57

38.34

37.13

37.21

38.49

37.25

20.88

20.71

21.42

20.92

20.81

21.63

20.84

20.69

21.22

20.64

0.01

0.04

0.00

0.01

0.00

0.03

0.02

0.00

TiO

0.18

0.03

0.04

0.38

0.30

0.08

0.35

0.10

0.36

0.37

MgO

0.82

1.50

2.76

3.74

3.84

3.90

3.45

0.81

6.64

3.51

FeO

27.47

31.47

29.99

31.18

29.76

24.25

31.27

30.96

26.72

31.46

MnO

4.52

2.54

1.31

1.62

3.42

0.55

1.74

3.42

2.00

1.67

CaO

9.31

6.51

7.60

5.68

5.08

11.44

5.52

7.37

5.20

5.50

Total

100.50

99.65

100.85

101.34

100.78

100.18

100.29

100.60

100.66

100.41

2.983 2.978 2.976 2.970 2.968 2.987 2.952 2.989 2.980 2.959

0.017 0.022 0.024 0.030 0.032 0.013 0.048 0.011 0.020 0.041

1.951 1.951 1.967 1.906 1.905 1.972 1.905 1.948 1.917 1.891

0.011 0.002 0.002 0.023 0.018 0.004 0.021 0.006 0.021 0.022

0.001 0.003 0.000 0.000 0.000 0.000 0.000 0.002 0.001 0.000

0.038 0.045 0.031 0.071 0.077 0.023 0.075 0.044 0.060 0.086

1.799 2.082 1.946 1.977 1.889 1.556 2.004 2.036 1.670 2.003

0.098 0.181 0.324 0.438 0.452 0.452 0.409 0.097 0.767 0.416

0.306 0.174 0.087 0.108 0.229 0.036 0.117 0.233 0.131 0.113

0.797 0.564 0.642 0.478 0.430 0.955 0.470 0.634 0.431 0.468

Zones of planktonic foraminifera correlated with N9, 10, 11
of  the  global  foraminiferal  zonation;  MMi4a,  MMi5  and
MMi6  of  Mediterranean  foraminiferal  zonation.  The  Medi-
terranean  Langhian  Stage  (Lower  Badenian  of  the  Central
Paratethys) is dated by the NN4 Zone, which is dated by the
presence  and  LO  of  H.  ampliaperta  and  H  scissura.  The
NN5  Zone  was  detected  by  the  FO  of  the  planktonic  fora-
minifera  Globigerinoides  quadrilobatulus  (d’Orbigny)  and
Globigerina regularis (d’Orbigny), later by the FO of Orbu-
lina  suturalis  (Brönnimann)  of  CPN7.  The  Early  Serraval-
lian (Upper Badenian) is dated by the NN6 Zone and by the
FO  of  Globigerina  druryi  (Akers)  together  with  G.  woodi
decoraperta (Takayanagi & Saito) correlated with the CPN8
biozone;

! The obtained palynomorph assemblages confirm sub-

tropical and humid climatic conditions during the Middle
Miocene time span. Mountain vegetation taxa indicate altitu-
dinal zonation;

! A fandelta proximal to the distal basin slope and off-

shore deep water basin environment was documented in the
Lower  Badenian.  The  Upper  Badenian  deep  water  dysoxic
environment  changed  gradually  to  the  Sarmatian  and  Pan-
nonian  coastal  to  alluvial  plain  depositional  systems  in  the
northern Danube Basin. Sedimentary analysis of revised core
material  led  to  recognition  of  the  various  gravity  transport
mechanisms, including debris-flows and turbibity currents;

! Sedimentary facies described from the base to the top of

the 2000 m deep well together with the results of paleoecology
helped with a more precise determination of the depositional
environments  of  formations:  1) The  Jablonica  Formation
conglomerates deposited in fandelta to onshore shallow ma-
rine  environment  during  the  earliest  Badenian  (formerly
included  in  the  Karpatian  stage);  2) Lower  Badenian  sedi-
ments  of  the  gravitational  currents  in  a  proximal  slope  set-
ting  belong  to  the  Špačince  Formation  lower  part;  3) The
upper  part  of  the  Špačince  Formation  is  represented  by  the
Lower  Badenian  distal  slope  gravitational  deposits  namely
turbidites;  4) The  Upper  Badenian  Báhoň  Formation  is  rep-
resented  by  the  deep  water  basinal  dysoxic  mudstones;

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Acknowledgments: This work was supported by the Slovak
Research  and  Development  Agency  under  the  contracts
APVV-0099-11,  APVV-0625-11  and  Grant  UK/325/2014.
We also express gratitude to APVV LPP 0120-06, ESF-EC-
0006-07, ESF-EC-0009-07 and VEGA 2/0042/12. Addition-
ally  our  acknowledgments  go  to  ….  Sliva  (Nafta  a.s.)  for
granting  access  to  the  well  repositories  and  to  I.  Broska
(Geological  Institute  at  Slovak  Academy  of  Sciences)  for
consulting on the issue of granitoid rocks. Special thanks go
to Mr. Hronkovič (Comenius University, Bratislava) for help
with well core material and thin section assembly. Above all
we  greatly  appreciate  all  questions  and  comments  from  our
reviewers O. Sztanó and K. Holcová which significantly en-
riched and improved the manuscript.

References

Adam Z. & Dlabač M. 1969: Erklärungen zur Mächtigkeitskarte

und zur lithofaziellen Entwicklung der Donau—Niederung. Zá-
pad. Karpaty 11, 156—171.

Akers W.H. 1955: Some planktonic foraminifers of the American

gulf coast and suggested correlations with the Caribbean Ter-
tiary. J. Paleontology 29, 4, 647—664.

Andreyeva-Grigorovich A.S., Kováč M., Halásová E. & Hudáčková

N. 2001: Litho- and biostratigraphy of the Lower and Middle
Miocene sediments of the Vienna basin (NE part) on the basis
of calcareous nannoplankton and foraminifers. Scr. Fac. Sci.
Natur. Univ. Masaryk. Brun., Geol. 30, 27—40.

Andreyeva-Grigorovich A.S., Kováč M., Halásová E., Hudáčková N.

& Zlinská A. 2003: Middle, Upper Miocene zonation of Ukraine
and  Slovak  sediments  based  on  calcareous  nannoplankton  and
foraminifera.  Theoretical  and  practical  aspects  of  modern  bio-
stratigraphy of Ukraine Phanerozoic. [Rasclenenie srede-verch-
nemiocenovych  (Badenij—Panon)  otlozenij  Ukrajiny  i  Slovakii
po  Nannoplanktonu  i  Foraminiferam.  Teoreticny  ta  prikladni
aspekti sucasnoi biostratigrafii Fanerozoja ukrainy.] UDK, Kiiv,
1—7 (in Russian).

Biela A. 1978: Deep wells in Western Carpathians: Vienna basin,

Danube basin. [Hlboké vrty v zakrytých oblastiach Západných
Karpát: Záhorská nížina, Podunajská nížina.] Regionálna Geol.
Západ. Karpát 10, 1—224 (in Slovak).

Biely A. (Ed.), Bezák V., Elečko M., Gross P., Kaličiak M.,

Konečný V., Lexa J., Mello J., Nemčok J., Potfaj M., Rakús
M., Vass D., Vozár J. & Vozárová A. 1996: Geological map of
Slovak Republic, 1 : 500,000. Ministry of Environment, Slovak
Geological Survey, ( in Slovak).

Broska I. & Uher P. 1988: Accessory minerals of granitoid rocks of

Bojná and Hlohovec blocks, The Považský Inovec Mts. Geol.
Zbor., Geol. Carpath. 39, 4, 505—520.

Catuneanu O., Galloway W.E., Kendall C.G. St .C., Miall A.D.,

Posamentier H.W., Strasser A. & Tucker M.E. 2011: Sequence
stratigraphy: Methodology and nomenclature. Newsllett. Stratigr.
44, 3, 173—245.

Cicha I., Čtyroká J., Jiříček R. & Zapletalová I. 1975: Principal bio-

zones  of  the  Late  Tertiary  in  Eastern  Alps  and  West  Car-
pathians.  In:  Cicha  I.  (Ed.):  Biozonal  division  of  the  Upper
Tertiary  Basins  of  the  Eastern  Alps  and  West-Carpathians.
IUGS, Proc. of the VI. Congress, Bratislava, 19—34.

Cicha I., Roegl F., Rupp Ch. & Čtyroká J. 1998: Oligocene-Mio-

cene Foraminifera of the Central Paratethys. Abh. Sencken-
berg. Naturforsch. Gessell. 549, 1—325.

Doláková N., Holcová K., Hladilová Š., Brzobohatý R., Zágoršek

K., Hrabovský J., Seko M. & Utescher T. 2014: The Badenian

parastratotype at Židlochovice from the perspective of the mul-
tiproxy study. Neu. Jb. Geol. Paläont., Abh. 271, 2, 169—201.

Dyakowska J. 1959: Palynological manual; methods and problems.

[Podrecznik Palynologii; Metody i Problemy.] Wydaw. Geol.,
Warsawa, 1—325 (in Polish).

Emery D. & Myers K.J. 1996: Sequence stratigraphy. Blackwell,

Oxford, UK, 1—297.

Erdtman G. 1943: An introduction to pollen analysis. Chronica Bo-

tanica, Waltham, Mass., 1—238.

Faegri K. & Iversen J. 1989: Textbook of pollen analysis. IV edi-

tion. The Blackburn Press., 1—328.

Gradstein F.M., Ogg J.G., Schmitz M.D. & Ogg G.M. (Eds.) 2012:

The Geologic Time Scale 2012. Elsevier, Boston, USA, 1—1144.

Grill R. 1941: Stratigraphische Untersuchungen mit Hilfe von Mikro-

faunen im Wiener Becken und den benachbarten Molasse—An-
teilen. Oel u. Kohle, Berlin 37, 595—602.

Hammer Ř., Harper D.A.T. & Ryan P.D. 2001: PAST: Paleontolog-

ical statistics software package for education and data analysis.
Palaeont. Eletronica 4, 1—9.

Harzhauser M. & Mandic O. 2008: Neogene lake systems of Cen-

tral and South-Eastern Europe: Faunal diversity, gradients and
interrelations. Palaeogeogr. Palaeoclimatol. Palaeoecol. 260,
417—434.

Harzhauser M. & Piller W.E. 2007: Benchmark data of a changing

sea – palaeogeography, palaeobiogeography and events in the
central Paratethys during the Miocene. Palaeogeogr. Palaeo-
climatol. Palaeoecol. 253, 8—31.

Hohenegger J., Ćorić S. & Wagreich M. 2014: Timing of the Mid-

dle Miocene Badenian Stage of the Central Paratethys. Geol.
Carpathica 65, 1, 55–66.

Holcová K. 1997: Can detailed sampling and taphonomical analysis

of foraminiferal assemblages offer new data for paleoecologi-
cal interpretations? Rev. Micropaleont. 40, 4, 313—329.

Holcová K. 1999: Postmortem transport and resedimentation of for-

aminiferal tests: relations to cyclical changes of foraminiferal
assemblages. Palaeogeogr. Palaeoclimatol. Palaeoecol. 145, 1,
157—182.

Horváth F., Bada G., Szafián P., Tari G., Ádám A. & Cloetingh S.

2006: Formation and deformation of the Pannnian basin: con-
straints from observational data. In: Gee D.G. & Stephenson R.
(Eds.): Europian lithosphere dynamics. Geol. Soc. London,
Mem. 32, 191—206.

Hrušecký 1999: Central part of the Danube Basin in Slovakia: Geo-

physical and geological model in regard to hydrocarbon
prospection. EGRSE, Spec. Issue 6, 1, 2—55.

Hrušecký I., Šefara J., Masaryk P. & Lintnerová O. 1996: The struc-

tural and facies development and exploration potential of the
Slovak part of the Danube Basin. In: Wessely G. & Liebl W.
(Eds.): Oil and gas in Alpidic Thrustbelts and Basins of Central
and Eastern Europe. EAGE, Spec. Publ. 5, 417—429.

Hrušecký I., Pereslényi M., Hók J., Šefara J. & Vass D. 1993: The

Danube Basin geological pattern in the light of new and rein-
terpretation of old geophysical data. In: Rakús M. & Vozár J.
(Eds.): Geodynamical model and deep structure of the Western
Carpathians. GÚDŠ, Bratislava, 291—296 (in Slovak).

Iaccarino S.M., Di Stefano A., Foresi L.M., Turco E., Baldassini N.,

Cascella A., Da Prato S., Ferraro L., Gennari R., Hilgen F.J.,
Lirer  F.,  Maniscalco  R.,  Mazzei  R.,  Riforgiato  F.,  Russo  B.,
Sagnotti L., Salvatorini G., Speranza F. & Verducci M. 2011:
High-resolution  integrated  stratigraphy  of  the  upper  Burdiga-
lian—lower  Langhian  in  the  Mediterranean:  the  Langhian  his-
torical  stratotype  and  new  candidate  section  for  defining  its
GSSP. Stratigraphy 8, 199—215.

Imrichová E. 1969: Drilling report form the Ratkovce 1 well site.

[Složka pionýrské vrtby Ratkovce-1.] MND, MS, Hodonín,
1—113 (in Czech).

STRATIGRAPHY, SEDIMENTOLOGY AND ENVIRONMENTS OF N DANUBE BASIN (SLOVAKIA)

GEOL

EOL

EOLOGICA CARPA

OGICA CARPA

OGICA CARPATHICA

THICA

THICA, 2015, 66, 1, 51—67

Jamrich M. & Halásová E. 2010: The evolution of the Late

Badenian calcareous  nannofossil  assemblages  as  a  reflexion
of  the palaeoenvironmental  changes  of  the  Vienna  Basin
(Devínska Nová Ves clay pit). Acta Geol. Slovaca 2, 2,  123—140
(in Slovak, with English summary).

Konečný V., Kováč M., Lexa J. & Šefara J. 2002: Neogene evolu-

tion of the Carpatho-Pannonian Region: an interplay of sub-
duction and back-arc diapiric uprise in the mantle. EGS
Stephan Mueller Spec. Publ., Ser. 1, 105—123.

Kováč M. 2000: Geodynamics, paleogeography and structureal evo-

lution  of  the  Karpato-Pannonian  region  in  the  Miocene:  New
view  at  the  Neogene.  [Geodynamický,  paleogeografický
a štruktúrny  vývoj  karpatsko-panónskeho  regiónu  v miocéne:
Nový pohŽad na neogénne panvy Slovenska.] VEDA, Bratislava,
1—202 (in Slovak).

Kováč M., Holcová K. & Nagymarosy A. 1999: Paleogeography,

paleobathymetry and relative sea-level changes in the Danube
Basin and adjacent areas. Geol. Carpathica 50, 4, 325—338.

Kováč M., Synak R., Fordinál K. & Joniak P. 2010: Dominant

events in the northern Danube Basin palaeogeography – a tool
for specification of the Upper Miocene and Pliocene stratigraphy.
Acta Geol. Slovaca 2, 1, 23—36.

Kováč M., Baráth I., Holický I., Marko F. & Túnyi I. 1989: Basin

opening in the Lower Miocene strike-slip zone in the SW part of
the Western Carpathians. Geol. Carpathica 40, 1, 37—62.

Kováč M., Synak R., Fordinál K., Joniak P., Tóth C., Vojtko R.,

Nagy A., Baráth I., Maglay J. & Minár J. 2011: Late Miocene
and Pliocene history of the Danube Basin: inferred from devel-
opment of depositional systems and timing of sedimentary fa-
cies changes. Geol. Carpathica 62, 6, 519—534.

Kováč M., Baráth I., Fordinál K., Grigorovich A.S., Halásová E.,

Hudáčková  N.,  Joniak  P.,  Sabol  M.,  Slamková  M.,  Sliva  ….,
Töröková I. & Vojtko R. 2006: Late Miocene to Early Pliocene
sedimentary environments and climatic changes in the Alpine-
Carpathian-Pannonian  junction  area:  a case  study  from  the
Danube  Basin  northern  margin  (Slovakia).  Palaeogeogr.
Palaeoclimatol. Palaeoecol. 238, 1—4, 29, 32—52.

Kováč M., Andreyeva-Grigorovich A., Bajraktarević Z., Brzobo-

hatý  R.,  Filipescu  S.,  Fodor  L.,  Harzhauser  M.,  Nagymarosy
A.,  Oszczypko  N.,  Pavelić  D.,  Rögl  F.,  Saftić  B.,  Sliva  ….  &
Studencka  B.  2007:  Badenian  evolution  of  the  Central  Para-
tethys  Sea:  paleogeography,  climate  and  eustatic  sea-level
changes. Geol. Carpathica 58, 6, 579—606.

Kováčová P. & Hudáčková N. 2009: Late Badenian foraminifers

from the Vienna Basin (Central Paratethys): Stable isotope study
and paleoecological implications. Geol. Carpathica 60, 1, 59—70.

Kováčová M., Doláková N. & Kováč M. 2011: Miocene vegetation

pattern and climate change in the northwestern Central Para-
tethys domain (Czech and Slovak Republic). Geol. Carpathica
62, 3, 251—266.

Kvaček Z., Kováč M., Kovar-Eder J., Doláková N., Jechorek H.,

Parashiv V., Kováčová M. & Sliva …. 2006: Miocene evolution

of landscape and vegetation in the Central Paratethys. Geol.
Carpathica 57, 4, 295—310.

Lankreijer A., Kováč M., Cloetingh S., Pitoňák P., Hlôška M. &

Biermann C. 1995: Quantitative subsidence analysis and for-
ward modelling of the Vienna and Danube Basins: thin skinned
versus thick skinned extension. Tectonophysics 252, 433—451.

Martini E. 1971: Standard Tertiary and Quaternary calcareous nan-

noplankton zonation. Proc. of 2nd Planktonic Conference, Roma
1970, 739—785.

Márton E., Vass D. & Túnyi I. 1995: Early Tertiary rotations of the

Pelso megaunit and neighbouring Central West Carpathians.
In: Hamršníd E. (Ed.): New results in Tertiary of West Car-
pathians. II. MND, KZPN, Hodonín 16, 97—108.

Miall A.D. 2010: The geology of stratigraphic sequences. 1st Edi-

tion. Springer, Heidelberg, 1—544.

Moore P.D., Webb J.A. & Collinson M.E. 1991: Pollen analysis.

Blackwell Sci., 1—216.

Murray J.W. 2006: Ecology and applications of benthic foramin-

ifera. Cambridge University Press, New York, 1—426.

Piller W.E., Harzhauser M. & Mandic O. 2007: Miocene Central

Paratethys stratigraphy: Current status and future directions of
stratigraphy. Stratigraphy 4, 2/3, 151—168.

Rider M. 1986: Geological interpretation of Well Logs. Rider

French Consulting Ltd., Aberdeen and Sutherland, 1—288.

Švábenická L. 2002: Calcareous nannofossils of the Upper Karpa-

tian and Lower Badenian deposits in the Carpathian Foredeep,
Moravia (Czech Republic). Geol. Carpathica 53, 197—210.

Takayanagi Y. & Saito T. 1962: Planktonic foraminifers from the

Nobori Formation, Shikoku, Japan. Sci. Rep. Tohoku Univ.,
Ser. 2 (Geol.), Spec. V. 5, 67—106.

Tari G. & Horváth F. 1995: Middle Miocene extensional collapse in

the Alpine-Pannonian transitional zone. In: Horváth F., Tari G.
& Bokor K. (Eds.): Extensional collapse of the Alpine orogene
and hydrocarbon prospects in the basement and fill of the west-
ern Pannonian Basin. AAPG Inter. Conf. Exhib., Nice, France,
Guidebook to fieldtrip No. 6, 75—105.

Tari G., Horváth F. & Rumpler J. 1992: Styles of extension in the

Pannonian Basin. Tectonophysics 208, 203—219.

Turco E., Iaccarino S.M., Foresi L.M., Salvatorini G., Riforgiato F.

& Verducci M. 2011: Revisiting the taxonomy of the interme-
diate stages in Globigerinoides—Praeorbulina lineage. Strati-
graphy 8, 163—187.

Vass D. 2002: Lithostratigraphy of Western Carpathians: Neogene

and Buda Paleogene. [Litostratigrafia Západných Karpát:
neogén a budínsky paleogén.] ŠGÚDŠ, Bratislava, 2—202 (in
Slovak).

Vozárová A. & Vozár J. 1988: Late Paleozoic in West Carpathians.

GÚDŠ, Bratislava, 1—314.

Wade B.S., Pearson P.N., Berggren W.A. & Pälike H. 2011: Re-

view and revision of Cenozoic tropical planktonic foraminiferal
biostratigraphy and calibration to the geomagnetic polarity and
astronomical time scale. Earth Sci. Rev. 104, 111—142.