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, DECEMBER 2011, 62, 6, 519—534 doi: 10.2478/v10096-011-0037-4
Late Miocene and Pliocene history of the Danube Basin:
inferred from development of depositional systems and
timing of sedimentary facies changes
MICHAL KOVÁČ
1*
, RASTISLAV SYNAK
1
, KLEMENT FORDINÁL
2
, PETER JONIAK
1
, CSABA TÓTH
4
,
RASTISLAV VOJTKO
1
, ALEXANDER NAGY
2
, IVAN BARÁTH
2
, JURAJ MAGLAY
2
and JOZEF MINÁR
3
1
Department of Geology and Paleontology, Faculty of Natural Sciences, Comenius University, Mlynská dolina G, 842 15 Bratislava,
Slovak Republic;
*
kovacm@fns.uniba.sk
2
State Geological Institute of Dionýz Štúr, Mlynská dolina 1, 817 04 Bratislava, Slovak Republic
3
Department of Physical Geography and Geoecology, Faculty of Natural Sciences, Comenius University, Mlynská dolina B1,
842 15 Bratislava, Slovak Republic
4
Central Slovak Museum, Department of Natural History, Radvanská 27, 974 05 Banská Bystrica, Slovak Republic
(Manuscript received March 17, 2011; accepted in revised form June 9, 2011)
Abstract: The development of the northern Danube Basin (nDB) was closely related to the Late Miocene geodynamic
evolution of the Pannonian Basin System. It started with a wide rifting which led to subsidence of several basin depocenters
which were gradually filled during the Late Miocene and Early Pliocene. In the Late Pliocene the subsidence continued
only in the basin’s central part, while the northern marginal zone suffered inversion and the uplifted sedimentary fill
began to be eroded. Individual stages of the basin development are well recorded in its sedimentary succession, where
at least three great tectono-sedimentary cycles were documented. Firstly, a lacustrine cycle containing Lower, Middle
and lowermost Upper Pannonian sediments (A—F Zones; sensu Papp 1951) deposited in the time span 11.6—8.9 Ma and
is represented in the nDB in Slovakia by the Ivanka and Beladice Formations. In the Danube Basin of the southern part
in Hungary, where the formations are defined by the appearance of sedimentary facies in time and space, the equivalents
are: (1) the deep-water setting marls, clays and sandy turbidites of the Endrőd and Szolnok Formations leading to the
overlying strata deposits of the basin paleoslope or delta-slope represented by the Algyő Formation, and (2) the final
shallow-water setting deposits of marshes, lagoons and a coastal and delta plain composed of clays, sands and coal
seams, represented by the Újfalu Formation. The second tectono-sedimentary cycle was deposited in an alluvial envi-
ronment and it comprises the Upper Pannonian (G and H Zones; sensu Papp 1951) and Lower Pliocene sediments dated
8.9—4.1? Ma. The cycle is represented in the nDB, by the Volkovce Formation and in the southern part by the Zagyva
Formation in Hungary. The sedimentary environment is characterized by a wide range of facies from fluvial, deltaic and
ephemeral lake to marshes. The third tectono-sedimentary cycle comprises the Upper Pliocene sediments. In Slovakia
these are represented by the Kolárovo Formation dated 4.1—2.6 Ma. The formation contains material of weathering crust
preserved in fissures of Mesozoic carbonates, diluvial deposits and sediments of the alluvial environment.
Key words: Late Miocene, Pliocene, Lake Pannon, Danube Basin, tectono-sedimentary cycles.
Introduction
The Danube Basin is situated in the territories of Slovakia,
Hungary and Austria; it is located in the NW part of the Pan-
nonian Basin System (Fig. 1). A large part of this basin system
was covered by a Late Miocene lake which represented one of
the most extensive flooded areas in Central Europe (Harzhaus-
er & Mandič 2008; Magyar 2009).
Lake Pannon (Magyar et al. 1999), surrounded by the East
Alpine—Western Carpathian and Dinaride mountain chains,
developed due to the isolation of this part of the Central Para-
tethys Sea from the Eastern Paratethys and the Mediterranean
(Royden & Horváth 1988; Horváth 1993; Rögl 1998; Kováč
et al. 1999, 2006, 2010; Magyar et al. 1999; Konečný et al.
2002; Popov et al. 2006; Harzhauser & Mandič 2008). The
specific environmental conditions of the lake are confirmed by
an enormously diversified endemic mollusc fauna, which suf-
fered selective rapid phylogenetic radiation (Magyar et al.
1999; Harzhauser et al. 2004; Harzhauser & Mandič 2008;
Magyar 2009). From the Late Miocene to the Pliocene, Lake
Pannon was continuously filled by sediments, generally from
the W—NW to E—SE (Meulenkamp et al. 1996; Magyar et al.
1999). Gradual infilling of the individual depocenters or ba-
sins is reflected in the extent of specific sedimentary facies
and their change over time and space. Evaluation of hundreds
of seismic lines and electrical logs from boreholes penetrating
the sedimentary fill of the lake’s individual depocenters docu-
ments the presence of a great number of depositional systems
in shallow- and deep-water settings whose positions varied
over time and space (Juhász 1991; Pogácsás & Seifert 1991;
Csató 1993; Vakarcs et al. 1994; Magyar et al. 1999; Sacchi &
Horváth 2002; Kováč et al. 2006; Csató et al. 2007; Juhász et
al. 2007; Uhrin et al. 2009; Magyar 2009; Leever et al. 2011).
These individual depocenters have their own tectono-sedi-
mentary history and the main factors which influenced the de-
velopment of their depositional systems were climatic
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changes controlling humidity and evaporation and also local
tectonics which influenced uplift and subsidence, and conse-
quently the development of the river network and burial his-
tory (Kováč et al. 2006, 2010; Uhrin et al. 2009; Leever et al.
2011). The sedimentary record of individual basins normally
started with brackish to freshwater lacustrine deposits chang-
ing in the overlying strata to lagoonal, deltaic, fluvial and al-
luvial facies with a great thickness of often more than
2000—4000 m. This deposition was mostly in an alluvial envi-
ronment and it was followed by tectonic inversion of the basin
margins during the Pliocene and Quaternary era (Cloetingh
et al. 2005; Jarosinski et al. 2011).
The predominantly lacustrine to alluvial character of the
Late Miocene and Pliocene sedimentation in individual depo-
centers of Lake Pannon gave rise to many problems in correla-
tive lithostratigraphy between the Carpathian, Pannonian, and
Dinaride regions (Magyar 2009; Kováč et al. 2010). Al-
though, the thick piles of lacustrine deposits are mainly cor-
related on the basis of fossil records using endemic aquatic
fauna and flora, the biostratigraphy of alluvial sequences re-
lies on scarce results from mammalian fossils. The biostrati-
graphical data are only supported by magnetostratigraphy or
numerical dating of interbedded volcanic rocks in some places
(Vasiljev et al. 2004; Kováč et al. 2006; Magyar et al. 2007).
Therefore the correlation of sedimentary formations existing
between individual depocenters over greater distance is
sometimes difficult.
The more important second problem is the confidentiality
of data which can be acquired by the Oil and Gas Industry.
Previously, this has led to many problems in the exchange of
geological and geophysical information on the sedimentary
records of basins encompassing the territories of more than
one country. An excellent example of the different approach-
es in geological investigation can be found in the Danube
Basin which encompasses both a northern Slovak portion
and a southern Hungarian part.
A complete re-evaluation of geophysical and geological
data obtained in the northern Danube Basin (nDB), together
with new field-work and laboratory results formed the
ground-work for a new determination of particular sedimen-
tary facies and their changes in time and space. This allowed
a new model of the development of the basin’s depositional
system and an inter-regional correlation of the sedimentary
fill and formations within the northern Slovak and the south-
ern Hungarian portions of the Danube Basin.
Late Miocene and Pliocene biostratigraphy of the
northern Danube Basin
The biostratigraphy of the nDB Upper Miocene sediments
(Fig. 2), similar to that in the Vienna Basin, is predominantly
based on the following; (1) brackish to freshwater mollusc
fauna (A—F Zones, sensu Papp 1951, 1953; Fordinál 1997,
1998; Magyar et al. 1999; Harzhauser et al. 2004; Kováč et
al. 2006, 2008), (2) refined mammalian biozonation
(Harzhauser et al. 2004; Joniak 2005; Kováč et al. 2005,
2006, 2008, 2010; Vlačiky et al. 2008; Magyar 2009; Tóth
2010a,b), and (3) dinoflagellates and sporadic calcareous
nannoplankton (Hudáčková 1995; Hudáčková & Slamková
2000; Andrejeva-Grigorovich et al. 2003a,b; Kováč et al.
2006, 2008).
The shallow-water mollusc associations (Fig. 2) docu-
mented during the Early Pannonian (A, B, C Zones; sensu
Papp 1951) belong to the Mytilopsis ornithopsis and
Mytilopsis hoernesi Biozones (Harzhauser et al. 2004;
Kováč et al. 2005, 2006, 2008). In the Middle Pannonian
sediments (D, E Zones; sensu Papp 1951), in the Lymnocar-
dium conjugens Biozone associations with Congeria partschi
and Congeria subglobosa were found (Fordinál 1997; Kováč
et al. 2006, 2008). The Early and Middle Pannonian deep-
water mollusc fauna has previously only been recognized in
Fig. 1. Position of the Danube Basin within the Alpine-Carpathian-Pannonian region. The northern part of the Danube Basin (nDB) – po-
sition of basin depocenters: Blatné, Rišňovce, Komjatice, Želiezovce and Gabčíkovo Depressions.
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Hungary and it is characterized by the Congeria banatica
Biozone (Magyar et al. 1999).
The beginning of the Late Pannonian (F Zone; sensu Papp
1951) represents a time interval when the lacustrine environ-
ment of the Vienna Basin changed into an environment of
marshes and alluvial plains, and it is characterized by the
Mytilopsis neumayri—Mytilopsis zahalkai Biozone (Harzhauser
et al. 2004). A similar environment was also detected on the
western flanks of the nDB and it is documented by the
Mytilopsis neumayri Biozone in the Ivánka Formation’s up-
permost part (Fordinál 1997). In the basin center which is doc-
umented only on seismic lines and also on the basin’s SE
Hungarian margin, a lacustrine environment defined by the
Congeria czjzeki and Lymnocardium ponticum Biozone was
still present during this time (Magyar et al. 1999; Cziczer et al.
2009; Magyar 2009). For the following Late Pannonian to
Pliocene predominantly alluvial sedimentary record of the
nDB, we are unable to use further correlation based on mol-
lusc assemblages. The biostratigraphy of these sediments is
therefore based only on scarce findings of mammalian fossil
associations (Figs. 3, 4).
Biostratigraphy using “small mammals” helped us to deter-
mine not only the Ruscinian MN15b Biozone, but also the
Vallesian MN9 and MN10 Biozones (sensu Harzhauser et al.
2004; Harzhauser & Tempfer 2004; Daxner-Höck et al. 2004;
Joniak 2005). The proboscideans teeth of “big mammals”, con-
stituted the main evidence used to solve the chronological suc-
cession from the Turolian to Villanyian deposition in the stud-
ied area (MN12, MN13, MN14, MN15a, MN16, and MN17;
sensu Tóth 2010a,b). The results of this research simultaneously
helped us to deduce important facts about changes in paleoecol-
ogy and paleogeography of the broader nDB area.
The oldest Late Miocene mammalian fossil associations
(MN10 and MN9 mammal Biozones) were discovered at the
Pezinok brickyard (Blatné Depression of the nDB) where
Deinotherium giganteum was found together with other fos-
sils (Holec 2005; Tóth 2010a,b). The sediments form the up-
permost part of the Ivánka Formation and the lowermost part
of the Beladice Formation. The local fauna of the Vallesian
mammalian stage document an open landscape on the Lake
Pannon shoreline (Holec 1981, 1986; Sabol & Holec 2002;
Joniak 2005). Climate can be characterized by a gradual
change from subtropical to warm temperate, with evidence
of the sporadic presence of thermophilous and evergreen
taxa (Kvaček et al. 2006).
The fossil fauna of the overlying Volkovce Formation
forms part of the MN11 to MN14 mammal Biozones and
they cover the Turolian and Lower Ruscinian mammalian
stage of the Late Miocene and Early Pliocene epochs
(Fig. 4). The fauna and characteristics of the sediments docu-
ment the change from lacustrine to prevailingly alluvial and
fluvial environments.
The Turolian shift of the Lake Pannon shoreline from the
nDB towards the southeast confirms seismic data (Magyar
Fig. 2. Biostratigraphy of the northern Danube Basin. Central Paratethys stratigraphy sensu Kováč et al. (1998), Rögl (1998), Gradstein et
al. (2004), Harzhauser et al. (2004), Vasiliev (2006), Harzhauser & Mandic (2008). Calcareous Nannoplankton sensu Martini (1971),
Marunteanu (1997), Kováč et al. (2008). Dinoflagellates sensu Sütő-Szentai (1988, 1990), Magyar et al. 1999, Szuromi-Korecz et al. 2004.
Molluscs and mammals sensu Kováč et al. 2006; Vlačiky et al. 2008; Tóth 2010a,b.
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2009) and also mammalian fossil sites at Nyárád, Tihany and
Csákvár in Hungary (Bernor et al. 1987; Kordos 1987; Nar-
golwalla et al. 2006). The associations document an increase
in species diversity during the MN11 mammal Biozone. The
findings, represented by “large” and “small” mammals are
characterized by a murid-cricetid dominated assemblage and
by an increase in carnivores, ruminants and proboscideans.
The fauna points to relatively open woodland environments
and drier conditions with seasonal climate changes – com-
pared to the Vallesian (Daxner-Höck 1996). The Turolian
MN11 Zone which is also well known from the Eichkogel
limestone in the Vienna Basin (Wenz & Edlauer 1942; Dax-
ner-Höck 1996; Harzhauser & Binder 2004; Nargolwalla et
al. 2006) can be partly correlated with the Hlavina Member
(Fordinál 1994; Fordinál & Nagy 1997) a freshwater lime-
stone described from the western foothill of the Tribeč Mts or
with the Ratnovce limestone appearing at the western foothill
of the Považský Inovec Mts. The Hlavina limestone is posi-
tioned in the Volkovce Formation basal portion (Fig. 4).
Discovery of the Deinotherium proavum (originally de-
scribed as D. gigantissimum) at the Madunice locality in the
Blatné Depression refers to the presence of the MN12 Biozone
in the nDB (Musil 1959; Tóth 2010a,b). The first occurrence of
a primitive Anancus (Anancus sp.) comes from the Topo čany-
Kalvária site. Various proboscidean taxa such as “Mammut” aff.
borsoni, Anancus sp., and Tetralophodon sp., which can be dat-
ed at MN12—13? Biozones have also been reported at the Ve ké
Bielice, Klížske Hradište, Prusy, and Horné Obdokovce locali-
ties on the basin’s northern margin, in the Bánovce and Riš-
ňovce Depressions (Figs. 1, 3). All the aforementioned Turolian
Anancus teeth have a small to extremely small size, a complex
morphology and very low hypsodonty. The remains of the Vall-
esian species Tetralophodon longirostris were also documented
at the Topo čany-Kalvária site. The taphonomy of this locality
is therefore extremely difficult and the remains of two taxa were
presumably excavated from two separate or mixed strata.
The MN12—13 Biozone mammalian fauna is also known
from the Hungarian part of the Danube Basin at Tardosbánya
(Kordos 1987; Daxner-Höck 1996; Van Dam 2006; Nargol-
walla et al. 2006), Györszentmárton (Hugeney 1999) and Bal-
tavár localities (Kordos 1987; Bernor et al. 1987; Nargolwalla
et al. 2006). The Baltavár site has the best preserved faunal as-
semblage of the “Middle Turolian” in Central Europe, with
paleoenvironments of open country woodlands in a warm,
temperate climatic zone with seasonal changes (Bernor et al.
1996; Solounias et al. 1999; Kaiser & Bernor 2006).
Fig. 3. Northern part of the Danube Basin; localization of the sites with mammal fossil occurrences and figured outcrops (see Fig. 5); local-
ization of seismic profile and boreholes (white circles: AB1 – Abrahám 1, DI1 – Diakovce 1, IV1 – Ivánka 1, KRAL1 – Králová 1,
KOL2 – Kolárovo 2, MOJ1 – Mojmírovce 1, OB1 – Obdokovce 1 and SP1 – Špačince 1, SVM1 – Tajná).
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The findings of fossil remains of large mammalians from
the Volkovce Formation at the Slepčany site in the Komjatice
Depression of the nDB (Holec 1981) belong to the MN13—14?
Biozones (Figs. 1, 3). The teeth of Anancus aff. arvernensis
have a more complex morphology and are more hypsodont
in comparison with the Anancus from previous Turolian lo-
calities (MN12—13? Biozones).
The first appearance of the “typical” Anancus arvernensis
was recognized from the Kuzmice (MN13?—14), Nitra—
Kynek and Biskupová (both MN14) localities. These find-
ings document the Early Pliocene age of the sediments. The
molars are large with a less complex morphology and low
hypsodonty. There is a progressive trend of hypsodonty,
shortening and morphological simplification of the molars
(sensu Metz-Muller 1995). This is clearly observable in the
fossil record from Slovakia from the Early Pliocene to the
Early Pleistocene; and the final appearance of the “Mammut”
aff. borsoni taxon is reported at the Kuzmice site (Fig. 3).
The Late Pliocene fauna located in the “red beds” of the
Kolárovo Formation, cover a wide area of the Považský
Inovec Mts and the uplifted margin of the nDB in the
Rišňovce and partly Komjatice Depressions, and this docu-
ments an abrupt change at the Early and Late Pliocene
boundary, which is clearly visible in the sedimentary record.
The Ruscinian mammalian stage (MN15 Zone) documents
the first occurrence of the typical “Mammut” borsoni from
the Velké Ripňany and Drahovce (Tóth 2010a) and also
from the Ceroviny sites (Holec et al. 2002) placed in the
MN15—16 Zones (the Ruscinian-Villanyian boundary). At the
Ivanovce site near Trenčín, a Late Pliocene small mammal
faunal association of the Late Ruscinian (MN15b) was docu-
mented (Fig. 3). This fauna points to humid forests with
scarce open land near rivers or local lakes in a temperate cli-
matic zone (Fejfar 1961a,b, 1970; Fejfar & Heinrich 1985).
The Early Pleistocene mammalian faunal associations
(Anancus arvernensis, “Mammut” borsoni, Mammuthus cf.
meridionalis) were found in the SE part of the nDB at Nová
Vieska and Strekov localities (Figs. 1, 3). This mammal fau-
na is represented mainly by large mammals and belongs to
the MN16—17 Zones of the Villanyian mammalian stage
(Holec 1996; Vlačiky et al. 2008). The fossil fauna points to
open woodlands in temperate climatic zone with seasonal
changes; however, the sedimentary environment and compo-
sition of fauna indicate allochthonous and probably also
heterochthonous origin of the assemblage.
The rare foraminifers identified in pelitic deposits at the
base of the Late Miocene sedimentary record of the nDB –
Miliammina subvelatina Venglinskij, Trochammina kibleri
Venglinskij (Jiříček 1974; Jámbor et al. 1985; Kováč et al.
2008) confirm an initially brackish environment. The en-
demic nannoplankton (Fig. 2) of the Praenoelaerhabdus ba-
natensis
and
Noelaerhabdus
bozinovicae
Biozones
(Andrejeva-Grigorovich et al. 2003a,b; Kováč et al. 2008)
correlated with NN9 and NN10 Zones (sensu Martini 1971;
Marunteanu 1997) partly support a brief connection with the
Eastern Paratethys, at least during the very early stage of the
Lake Pannon on the Middle/Late Miocene boundary. After
9 Ma, the nDB was almost totally isolated from the rest of
the lake.
Fig. 4. Lithostratigraphic scheme of the northern Danube Basin forma-
tions; Standard Neogene stages and Central Paratethys stratigraphy sensu
Rögl (1998), Kováč et al. (1998), Gradstein et al. (2004). Explanatory
notes: dots – coarse clastics, sand and conglomerate; lines – fine-
grained deposits, clays and silts; black rectangles – coal seams and
coalificated plant remnants; H – Hlavina Member freshwater carbon-
ates. Time span of the Late Miocene formations after Kováč et al. (2010).
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Fig. 5. A – Brackish to freshwater
lacustrine deposits, Ivánka Fm, Pezi-
nok. B – Coal seams in nearshore
swamps and alluvial plain deposits,
Ivánka Fm, Pezinok. C – Shallow-
water fluvial to lacustrine deposits
with ripple marks, Beladice Fm,
Bernolákovo. D – Freshwater
limestones, Hlavina Mb, Ratnovce.
E – Coarse-grained to fine sand,
braided to meandering river depos-
its, Volkovce Fm, Hlohovec. F –
Overbank alluvial clays overlain by
deposits of small point bar, Vol-
kovce Fm, Hlohovec. G – “Hron
River” deltaic sandstones and con-
glomerates, Volkovce Fm, Nemčiňany. H – Erosional contact between grey alluvial fine-grained deposits of the Volkovce Fm and red or
variegated clays, sand and fine- to medium-grained gravel of the alluvial sediments of the Kolárovo Fm, Ve ké Ripňany.
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Lithostratigraphy of the Upper Miocene and
Pliocene northern Danube Basin fill
The Danube Basin (DB), situated in the Western Car-
pathians hinterland between the Eastern Alps on the west and
the Mid-Hungarian Range on the east, began to open at the
end of the Early Miocene (Tari et al. 1992). The initial rifting
was followed by the Middle Miocene subsidence of individual
depocenters (Lankreijer et al. 1995; Kováč et al. 1999). The
Late Miocene to Pliocene represents a separate chapter in the
basin’s history, during which more than 4500 m sediments
were deposited in the basin center (Kilényi & Šefara 1989;
Lankreijer et al. 1995; Kováč 2000).
In the nDB (Slovakia), the lower part of the Upper Miocene
basin fill (Early and Middle Pannonian A—E Zones; sensu
Papp 1951) is represented by the Ivánka Formation, originally
correlated with the time range of 11.6—7.1 Ma (Priechodská
& Harčár 1988; Vass 2002). New results from paleomagnetic
dating and biostratigraphy proved its Vallesian age and a
time range of approximately 11.6—9.7 Ma (Kováč et al.
2006, 2010; Magyar et al. 2007). The formation, with a max-
imal thickness of up to 2000 m, was deposited in a brackish
to freshwater lacustrine environment (Fig. 5A). It consists
predominantly of calcareous clays (claystones) and silts (silt-
stones) intercalated with sand bodies (sandstones). Occasion-
ally, gravels (conglomerates), coal-clays and coal seams are
present on the basin margin (Fig. 4, Fig. 5B).
The Beladice Formation (Priechodská & Harčár 1988) was
deposited towards overlying strata and this correlated with the
Late Pannonian Zone F (sensu Papp 1951) described as Pon-
tian in the time range of 7.1—5.3 Ma (Vass 2002). It is formed
by clays and silts with various sand contents attaining a thick-
ness from 30 to 500 m. The Beladice Formation was original-
ly defined as occurring only in shallow-water to alluvial
environments containing typical coal-clays and coal seams de-
posited in marshes, oxbows of meandering rivers and ephem-
eral lakes (Fig. 5C). However, it is clear from the seismic lines
crossing the basin center (Fig. 6a) that the accepted lithos-
tratigraphical definition of this formation is valid only for the
basin margins. Toward the basin center, in the southeast, the
alluvial to shallow-water facies continuously pass into deep-
water lacustrine facies. Therefore, the formation can be cor-
related with the Szák Formation located on the NE margin of
the Mid-Hungarian Range in Hungary (Cziczer et al. 2009).
The formation represents high stand deposits of the Conge-
ria czjzeki and Spiniferites paradoxus Biozones (Magyar et
al. 1999 or Zone F sensu Papp 1951), in the time span of
9.4—8.9 Ma, and therefore the upper boundary of deposition
of the Beladice Formation can be placed at approximately
8.9 Ma (Figs. 2, 4).
In the southern (Hungarian) part of the DB, Upper Miocene
sediments identical to the Ivánka and Beladice Formations can
be approximately correlated to at least four formations (sensu
Juhász 1991, 1994; Juhász et al. 2007). The Újfalu Formation
is formed of sediments deposited in a shallow-water setting as
shelf deposits, alluvial and deltaic sediments of marshes, la-
goons, coastal and delta plains. The Algyő Formation is com-
posed of fine-grained sediments, mostly clays, and marls in
the area of the basin or delta slope. The deep-water sandy tur-
bidites form the Szolnok Formation and the clays and marls of
the distant basin floor are part of the Endrőd Formation
(Fig. 6b).
The Upper Miocene to Lower Pliocene basin fill of the nDB
(G and H Zones; sensu Papp 1951) is represented by the Vol-
kovce Formation described as Dacian and correlated with the
time range of 5.3—3.6 Ma (Priechodská & Harčár 1988; Vass
2002). The formation was deposited in an alluvial environ-
ment and contains fluvial deposits and also sediments of
marshes, ephemeral lakes and small deltas (Fig. 5E,F, and G).
The formation is more than 1200 m in the central part of the
basin, and it consists predominantly of variegated clays and
silts with sand bodies, often with a lot of plant detritus. At the
basin margin, fluvial and deltaic sands and gravels are present
as well; on tectonic lines (in the case that carbonate rocks form
the pre-Neogene basement) freshwater limestone and “lake
chalk” were deposited (Fig. 5D). The freshwater limestone
bodies represent the Hlavina Member with an estimated age of
approximately 8 Ma (Fordinál & Nagy 1997; Kováč et al.
2010; Tóth 2010a,b). The base of the Volkovce Formation has
been newly dated to 8.9 Ma (Kováč et al. 2010) with its upper
part approaching the Upper Pliocene base, which is about
4.1 Ma old (sensu Gradstein et al. 2004). This new time span
of the formation is proved by findings of mammal fossils
ranging between the MN11 and MN14 Biozones (Turolian
and Early Ruscinian; 8.9—4.1 Ma).
In the southern, Hungarian part of the basin, the same pack-
age of sediments represents the Zagyva Formation with a
thickness of 1000—1200 m (Juhász 1991, 1994; Juhász et al.
2007). Its sedimentary sequence is composed of sandstones,
siltstones, clays and marls deposited in lacustrine, alluvial and
fluvial environments, similar to the northern part of the basin.
This formation contains a lot of plant remnants, coal clays,
and coal seams. Sandy bodies of 10—20 m thickness are inter-
preted as alluvial plain channel fill or deposits of point bars.
Upper Pliocene sediments in the nDB are represented by
the Kolárovo Formation (Priechodská & Harčár 1988). The
age of the formation base has conventionally been stated as
the base of the Romanian regional stage (Vass 2002) at
present dated to 4.1 Ma (Vasiliev et al. 2004). The age of the
formation upper boundary was also stated conventionally to
be at base of the Quaternary 2.6 Ma (Gradstein et al. 2004).
Findings of mammal fossils have currently proved the time
span of the MN15, 16 and 17 mammalian Zones (Ruscinian
and Villanyian; 4.1—2.6 Ma; Fejfar 1966; Vlačiky et al.
2008). The maximum thickness of 200—300 m the Kolárovo
Formation has been determined only from boreholes (Kováč
2000; Vojtko et al. 2008). The sedimentary environment of
the deposition was proluvial to alluvial; the sequence is com-
posed mostly of red or variegated clays, sand, and fine- to
medium-grained gravel (Fig. 5H). The pebble material is
represented by quartz, chert, sandstone, and crystalline
schists (Priechodská & Harčár 1988).
In the southern, Hungarian part of the basin, the Hanság
Formation (Császár et al. 1997) may be the equivalent of the
Kolárovo Formation in Slovak territory. The formation is
formed by lacustrine to fluvial variegated clays and sands
with gravel bodies, lignite layers and basalt tuffs occurring
in some places.
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Late Miocene and Pliocene depositional cycles in the
northern Danube Basin
The nDB Late Miocene and Pliocene tectono-sedimentary
evolution commenced with a phase of subsidence around the
Middle—Late Miocene boundary. The “wide-rifting” of the ba-
sin was followed by its gradual infill which lasted until the
Early Pliocene (Lankreijer et al. 1995; Kováč et al. 2010).
During the Late Pliocene a shift of subsidence in the central
Gabčíkovo Depression was documented. This occurred simul-
taneously with uplift and denudation at the basin’s northern
margins (Lankreijer et al. 1995; Kováč et al. 2006). Three pe-
riods of deposition (tectono-sedimentary cycles) have been re-
corded in the basin sedimentary fill and these are observable
in outcrops, and especially on seismic lines and well logs.
The first, Late Miocene lacustrine tectono-sedimentary cy-
cle began approximately 11.6 Ma (Magyar et al. 1999;
Kováč et al. 1999, 2006; Kováč 2000) and it can be approxi-
mately correlated with the base of the global TB3.1 cycle
(sensu Haq et al. 1988; Haq 1991), or the Ser4/Tor1 cycle
(sensu Hardenbol et al. 1998; 11.7—9.4 Ma). The coinci-
dence in timing of the depositional cycle lower boundary
with the global cycles, and more or less also with the lower
boundary of all depositional cycles in the whole Pannonian
Basin System can be related to the existence of a short period
of connection with the Eastern Paratethys during this time.
The possibility of such a connection is also supported by the
presence of marine nannoplankton in the Lower Pannonian
deposits as far as the Danube and Vienna Basins (Andrejeva-
Grigorovič et al. 2003a,b).
Fig. 6. NW—SE oriented seis-
mic profile in the central part
of the northern Danube Basin,
situation at Fig. 3: a – Seis-
mic profile with marked time
lines dividing individual tec-
tono-sedimentary cycles; 1 –
Late Miocene lacustrine tectono-
sedimentary cycle, 11.6—8.9 Ma,
Ivánka and Beladice Fms; 2 –
Late Miocene to Early Pliocene
alluvial
tectono-sedimentary
cycle, 8.9—4.2 Ma, Volkovce
Fm; 3 – Late Pliocene prolu-
vial to alluvial tectono-sedi-
mentary cycle, 4.2—2.6 Ma,
Kolárovo Fm. b – Distribution
of sedimentary facies on seismic
line (e logs of the same facies are
marked on Fig. 7). c – Paleo-
depth of Lake Pannon in the
northern Danube Basin.
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During this sedimentary cycle, the Ivánka and Beladice
Formations (Priechodská & Harčár 1988; Vass 2002) were
deposited in the nDB (Fig. 4). Reinterpretation of data from
the outcrops, boreholes, and geophysical measurements
helped in the detection of the upper boundary of this cycle,
which we placed on seismic lines to the distinct level where
a change in character of seismic reflexes appears from “a
typical lacustrine to an alluvial pattern” (Fig. 6b). This
change in seismic signal also coincides with the change in
shape of the boreholes’ electrical logs in many places
(Fig. 7). Timing of this boundary is based on the age of the
Szák Formation at 8.9 Ma (Cziczer et al. 2009). Thus, our
definition of the first Pannonian lacustrine depositional cycle
upper boundary can also be correlated with the uppermost
portion of the “Pannonian cycle PAN2” defined in the south-
ernmost part of the DB by Sacchi & Horváth (2002).
The base of the second, Late Miocene to Early Pliocene al-
luvial tectono-sedimentary cycle was confirmed on the sur-
face at the DB northern margin: in the Blatné Depression
(clay pit Hlohovec; Kováč et al. 2006) and in the Komjatice
Depression (Kováč et al. 2008), where the borehole ŠVM-1
near the town of Vráble (Fig. 3) reached below the sediments
of the Volkovce Formation on the erosion surface, lying on
the Ivánka Formation clays (E Zone, sensu Papp 1951). The
upper boundary of this depositional cycle is located at the
contact with the overlying Upper Pliocene Kolárovo Forma-
tion, which is divided from the Volkovce Formation mainly
by an angular discordance. Erosion surfaces and incised val-
leys were often present at the outcrops in the Rišňovce De-
pression (Fig. 5H).
The third, Late Pliocene proluvial to alluvial tectono-sedi-
mentary cycle is formed by the Kolárovo Formation (Fig. 3).
The age of this cycle’s lower boundary is close to the lower-
most part of the Late Ruscinian age at approximately 4.1 Ma
where the base of the Romanian stage is established accord-
ing to Vasiliev (2006). The upper boundary of the cycle is
conventionally placed at the bottom of the Quaternary at
2.6 Ma (sensu Gradstein et al. 2004). During this cycle, mas-
sive erosion of sediments of the older formations began in
the nDB marginal parts and fluvial sedimentation survived
only in the central Gabčíkovo Depression. The thickness of
the Quaternary deposits does not exceed 500 m (Janáček
1969; Scharek et al. 2000).
Correlative lithostratigraphy between the northern
and southern Danube Basin
The lithostratigraphy of the Upper Miocene and Pliocene
sediments of the DB and the consequent definition of forma-
tions in the northern Slovak and southern Hungarian portions
of the basin is totally different because various methods and
aspects of their definition have been used up to now. In the
Slovak part, the formations were defined following the verti-
cal “age” stratification of the sedimentary record (Priechodská
& Harčár 1988; Vass 2002), similar to that in the Vienna Ba-
sin (sensu Papp 1951), while in the Hungarian portion the for-
mations were defined as various depositional systems,
independent of age and characterized by their sedimentary en-
Fig. 7. Sedimentary environments and facies of the northern Danube
Basin and their response on the composite spontaneous potential (SP)
well log, correlation between the formations used in the northern
(Slovak) and southern (Hungarian) parts of the Danube Basin (sensu
Juhász 1991, 1994; Juhász et al. 2007 and Kováč et al. 2010).
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vironment which was predominantly conditioned by the pa-
leo-geomorphology of the basin. This included the shelf, basin
slope, and deep basin floor (Juhász 1991, 1994; Császár et al.
1997; Magyar et al. 1999; Juhász et al. 2007; Magyar 2009).
However, the Hungarian formations were mainly defined in
the Great Hungarian Plain basins and not in the Little Hungar-
ian Plain area of the Danube Basin.
The new reevaluation of borehole archival data and seismic
lines from the nDB in Slovak territory, together with reinter-
pretation of the electrical log patterns from the basin’s deepest
parts show that the northwestern shelf of Lake Pannon did not
exceed a paleo-depth of 20—50 m. However, the floor of the
basin depocenters in Slovak territory initially had depths of
200—300 m (Fig. 6c).
When the Hungarian definition of formations is considered,
a very approximate correlation can currently validly divide the
Upper Miocene Ivánka and Beladice Formations into sedi-
ments deposited in shallow- and deep-water settings. Shelf de-
posits such as alluvial and deltaic sediments of the marshes,
lagoons, coastal and delta plains are present in the Újfalu For-
mation. Further subdivision include the fine-grained and
mainly clay marl sediments in the basin paleo-slope or delta
slope of the Algyő Formation and the Szolnok Formation’s
deep-water sandy turbidites and the Endrőd Formation’s clays
and marls on the distant basin floor. When these facts were
considered, a partial correlation of the deep-water sedimentary
record of the nDB was performed between the still used “Papp
zones” sense and the “Hungarian” definition of formations in
the sense of depositional environments (Fig. 7).
The Upper Miocene deep-water sediments, which can be
correlated with the Endrőd Formation, correspond to the A
and B zones (sensu Papp 1951) and they reach a thickness of
50—100 m. The calcareous clays and claystones, represent
the base of the sequence and these were deposited in a basin
floor environment (Figs. 6b,c, 7). The overlying strata have a
thickness of 200 to 600 m and mainly contain fine- to medi-
um-grained massive sands and sandstone bodies separated
by layers of basin clays (C Zone; sensu Papp 1951). On the
basis of electrical log interpretations (Fig. 7) from drill holes
crossing these sediments in the central part of the basin we
can assume the presence of sandy high-density gravity cur-
rents and turbidites localized at the foot of the basin or delta
slope and on the adjacent basin floor (Figs. 6c, 7). This part
of the sedimentary sequence can be correlated with the Szol-
nok Formation.
According to the studied electrical logs, clays and silts,
100—200 m thick in the D Zone (sensu Papp 1951), capping
the sandy sediments of the “C Zone” show a distinct fining
upward trend of grain size again followed by a gradual in-
crease in sandy component towards the overlying strata
(Figs. 6c, 7). We can interpret this part of the sedimentary
record as deposits of the basin or delta slope, and also as the
facies of the lower basin or delta front in some places, and cor-
relate them with the Hungarian Algyő Formation.
Sediments of the DB marginal portion, as well as lake de-
posits above the deep-water sedimentary record were general-
ly deposited in much shallower environments (E and F Zones;
sensu Papp 1951). These sediments represent deposits of the
coastal or delta plain including marshes, lagoons and delta
front. The sedimentary record is composed of cyclic deposi-
tion of sands, silts and clays, and the presence of coal-clays
and coal seams is very common, especially in outcrops at the
basin margins. We correlate these with the Hungarian Újfalu
Formation (Figs. 6c, 7).
The Upper Miocene to Lower Pliocene basin fill (Zones G
and H; sensu Papp 1951) of the nDB is represented by the
Volkovce Formation (Priechodská & Harčár 1988; Vass
2002) which has a serrated pattern on electrical logs docu-
menting the alluvial sedimentary environment of this part of
the basin fill (Figs. 4c, 6).
Late Miocene and Pliocene geodynamics and
development of the nDB
Due to new results of multidisciplinary geological and geo-
physical research, progress in biostratigraphy, definition of
tectono-sedimentary cycles, and correlative lithostratigraphy,
we can better understand the Late Miocene and Pliocene evo-
lution of the nDB. This evolution was influenced by a geody-
namic background set up by asthenospheric mantle upheaval
in the back arc basin acting together with the overriding slab
pull – caused by the subduction retreat in front of the Eastern
Carpathians during this time (Horváth 1993; Csontos 1995;
Lankreijer et al. 1995; Bada et al. 1996, 2001; Fodor et al.
1999; Konečný et al. 2002).
The current shape of the nDB, with characteristic digit like
depocenters in a NE—SW direction: the Blatné, Rišňovce, and
Komjatice Depressions (Fig. 1) is a result of the Middle Mio-
cene structural pattern development which controlled the
opening of these depressions from west to the east during the
Badenian and Sarmatian ages.
At the Middle—Late Miocene boundary no marked change
in the basin sedimentary fill architecture was observed along
the seismic lines in the basin center. However, frequent angu-
lar discordance between the Sarmatian and Lower Pannonian
sediments on the basin margin document an accelerated sub-
sidence of the basin.
The Late Miocene “wide rifting” of the nDB (sensu
Lankreijer et al. 1995) was controlled by a fault pattern similar
to the Middle Miocene one (Marko et al. 1990, 1991, 1995;
Fodor et al. 1999; Kováč 2000). The Pannonian halfgrabens
and grabens subsided predominantly along NNE—SSW to
NE—SW trending fault zones operating in a paleostress field
with a NE—SW oriented maximal compression axis. Follow-
ing the thickness of sediments and average sedimentation
rates (m/Myr) during individual time spans at selected bore-
holes, a gradual increase in the Late Miocene deposition can
be observed from the basin margins toward its center (Fig. 8).
The Beladice Formation (9.7—8.9 Ma) gained maximum thick-
ness and an accelerated sedimentation rate during this time in
the Gabčíkovo Depression.
The following Late Miocene and Early Pliocene sedimen-
tation of the Volkovce Formation (8.9—4.1 Ma) document
a more moderate deposition. The tectonic background of
subsidence during this time span is not satisfactorily solved.
However, it is proposed that the origin of the accommoda-
tion space was initiated due to thermal subsidence of the
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back arc basin (Horváth 1993; Hrušecký et al. 1996). It ap-
pears that the mechanism of subsidence could also be mainly
controlled by the deep sub-crustal erosion above the mantle
diapir, allowing the sinking of the thinned overheated crust
of the nDB below the load of a massive sedimentary pile of
more than 4000 m at this time.
The thermal subsidence (sensu Horváth 1993), due to cool-
ing of the overheated lithosphere, may have started in the nDB
originally during the Early Pliocene (Konečný et al. 2002).
This fact documents the change of lithosphere elastic proper-
ties towards a more brittle condition (Lankreijer et al. 1995,
1999; Lankreijer 1998; Bada 1999; Dérerová et al. 2006). A
northward advance of crustal deformations from southern re-
gions began at the end of the Late Miocene and during the
Fig. 8. Sedimentation rates (m/million years) from boreholes in the
Blatné (Špačince 1, Abrahám 1); Rišňovce (Obdokovce 1, Diakov-
ce 1); Komjatice and Gabčíkovo Depressions (Ivánka 1, Moj-
mírovce 1 and Kolárovo 2).
Early Pliocene. This is dated by folding of the Pannonian sedi-
ments – “Sava folds”; sensu Fodor et al. (1999) and it first
reached the northern regions during the Late Pliocene (indi-
cated by the transpressive tectonic regime in the Western Car-
pathians causing their accelerated uplift; sensu Minár et al.
2011). All these tectonic events were induced by the move-
ment of the Adriatic plate northward (Sacchi & Horváth 2002;
Ruszkiczay-Rüdiger et al. 2005; Horváth et al. 2006).
In the nDB, this considerable change in tectonic regimes is
marked by angular discordance between the Upper Pliocene
sediments and underlying strata, and also by increased deposi-
tion during this time period (Fig. 8) in the central Gabčíkovo
Depression (Kolárovo Formation; 4.1—2.6 Ma).
Inversion of the DB northern margin, due to the accelerated
uplift of the Western Carpathians led to the basin inversion
which persisted into the Quaternary, and was associated with
erosion of the uplifted nDB sedimentary formations (Kováč et
al. 2006; Minár et al. 2011). This yielded sediments for sub-
siding depocenters in its central part. The following Late Qua-
ternary subsidence of the Gabčíkovo Depression along
NW—SE trending normal faults (Herrmann et al. 1998) was
possibly connected with the change of transpressive tectonic
regimes to transtensional by the NW—SE orientation of the
principal maximum paleostress axis by the final stage of the
basin’s evolution (Vojtko et al. 2008; Králiková et al. 2010).
The Pliocene to Quaternary basin inversion of the Pannon-
ian-Carpathian system is related to changes in the regional
stress field leading to differential vertical movements associ-
ated with a laterally variable folding mechanism which was
active in the entire system (sensu Cloetingh et al. 2005). The
lateral variability was a result of marked contrast in rheology
between various areas, directly related to the crustal configu-
ration, thermal properties and late-stage collision kinematics
of the Carpathians. The finite-element numerical-modelling
study by Jarosinski et al. (2011) also predicted a successive
development in surface undulations caused by crustal and/or
lithosphere folding and a change in the stress state along the
flanks of the basin, due to the development of a weak basin
lithosphere in their vicinity.
Discussion
The Late Miocene and Pliocene paleogeography of the
Western Carpathians and the northern Danube Basin (nDB),
located in the hinterland of the mountain chain (Kováč et al.
1993; Magyar et al. 1999) can also be judged from a qualita-
tive mass balance relationship viewpoint. An example of this
is the relationship between the uplifting source and the sinking
areas. The tectonically active periods of the mountain chain
uplift are recorded in the basin fill, with the deposition of
coarse-grained sedimentary bodies and the tectonically quiet
periods are characterized by predominantly fine-grained sedi-
ments deposition.
The nDB sedimentary history documents a Late Miocene
lacustrine cycle (Early and Middle Pannonian) followed after
8.9 Ma by a second cycle (Late Pannonian to Early Pliocene)
with an environment of alluvial plains. The absence of greater
amounts of coarse-grained sediments such as gravels and
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conglomerates in the majority of the sedimentary fill during
both cycles indicates the development of a moderate land-
scape in the hinterland of the basin. This agrees with the doc-
umented development of the Mid-mountain level – main
planation surfaces of the Western Carpathians (Mazúr 1963;
Minár 2003), dated between 10—6 Ma (Minár et al. 2011;
Kováč et al. 2011).
The commencement of a rapid uplift in the Western Car-
pathian mountain chain documented between 6—4 Ma (Kováč
et al. 2011) is not visible in the sedimentary record of the ba-
sin center, and no abrupt change or erosion surface is to be
found on the seismic lines crossing the basin. This tectonic
event can be supported only by the onset of coarser deltaic
sedimentation in the upper part of the Volkovce Formation
(Late Turolian MN13(14?) mammalian Biozone), when a fan
delta of the paleo-Hron river entered the basin in the Kom-
jatice Depression (Baráth & Kováč 1995; Fig. 5G).
The Late Pliocene (4.1—2.6 Ma) and Quaternary accelera-
tion of the Western Carpathian chain uplift (Minár et al.
2011), which was associated with tectonic inversion of the
nDB margins, was tectonically controlled and it led to the cur-
rent landscape and development of the river network. Eroded
material from the mountains was transported by the rivers to-
wards the lowlands (Fig. 5H); the paleo-Váh river entered the
basin and the Kolárovo Formation was deposited (Kováč et al.
2006). The Quaternary nDB was divided into uplifting hilly
lands and subsiding plains.
Conclusions
The significant results of the nDB study and its correlation
with the southern Hungarian portion can be summarized as
follows:
A new biostratigraphical and lithostratigraphical concept
of the Upper Miocene and Pliocene nDB fill:
(a) The time range of the Volkovce Formation (Priechod-
ská & Harčár 1988; Vass 2002) previously dated as the Early
Pliocene (Dacian), was shifted from 5.3—3.6 Ma to the time
span of 8.9—4.1 Ma due to new paleomagnetic and biostrati-
graphical data, and also new analysis of borehole logs and
seismic profiles;
(b) The time range of the Beladice Formation (Priechodská
& Harčár 1988; Vass 2002) previously correlated with the
Pontian regional stage, was shifted from 7.1—5.3 Ma to 9.7—
8.9 Ma due to new paleomagnetic, biostratigraphical data,
and also new analysis of borehole logs and seismic profiles;
(c) The time range of the Pannonian Ivánka Formation
(Priechodská & Harčár 1988; Vass 2002), previously dated
11.6—7.1 Ma, was shifted to 11.6—9.7 Ma due to new paleo-
magnetic, biostratigraphical data, and also new analysis of
borehole logs and seismic profiles.
Three tectono-sedimentary cycles were documented in
the Upper Miocene and Pliocene fill of the nDB (Slovakia):
(a) The first Late Miocene (Pannonian) tectono-sedimen-
tary cycle (11.6—8.9 Ma), representing a lacustrine to alluvial
depositional system, comprising the Ivánka and Beladice
Formations, was deposited on the prograding margin of the
Lake Pannon in various environments. We can define this
succession as deposits of alluvial, lagoonal, and deltaic to
basin slope and basin floor facies shifting over time and to-
wards the basin center. Just as in the southern part of the ba-
sin in Hungary, the individual depositional systems based on
sedimentary facies changes can be defined and named as
lithostratigraphic entities uniformly in the southern, as well
as in the northern DB. (1) The shallow-water setting deposits
of alluvial and delta plain (marshes, lagoons, coastal, and
delta plain) are represented by the Újfalu Formation. (2) De-
posits of the paleo-slope or delta-slope of the Lake Pannon
comprise the Algyő Formation. (3) Sandy turbidites form the
Szolnok Formation and (4) the deep-water setting marls and
clays make up the Endrőd Formation;
(b) The second Late Miocene to Early Pliocene tectono-
sedimentary cycle (8.9—4.1 Ma), representing a predomi-
nantly alluvial depositional system, began to develop after
loss of accommodation space. The alluvial package of sedi-
ments is represented by the Volkovce Formation in Slovakia,
and by the Zagyva Formation in Hungary. The depositional
environments can be characterized as alluvial – with a wide
range of facies – from fluvial, deltaic, ephemeral lake to
marshes, and dry land deposits;
(c) Third Late Pliocene tectono-sedimentary cycle (4.1—
2.6 Ma), predominantly represented by the proluvial to allu-
vial depositional system, comprises deposition at the nDB
margins and in the basin “remnant depocenters” which are
mainly situated in its central part. The third cycle comprises
the Kolárovo Formation in Slovakia.
The Late Miocene to Pliocene geodynamic development
of the nDB, with two important changes of structural pattern
(paleostress field orientation), was documented:
(a) The Late Miocene to Early Pliocene synrift stage with
paleostress field with maximal compression axis of NE—SW
orientation;
(b) The Late Pliocene and Quaternary stage of inversion
with a Quaternary paleostress field change. Here, the maxi-
mal compression axis changed orientation from NE—SW to
NW—SE.
Qualitative mass balance relations, such as relations be-
tween the uplifting source and sinking areas can be charac-
terized as follows:
(a) The Late Miocene tectonically quiet period with the
absence of a greater amount of coarse-grained sediments in
the majority of the nDB sedimentary fill (10—6 Ma) indicates
the development of a moderate topography in the hinterland
of the basin. These facts agree well with the documented de-
velopment of the main planation surfaces of the Western
Carpathians, at the Mid-mountain level;
(b) The uplift of the Western Carpathians mountain chain
documented between 6—4 Ma is not visible in the basin sedi-
mentary record, and no abrupt change or erosion surface can
be found on seismic lines crossing the basin center. This tec-
tonic event is supported only by the onset of coarser deltaic
sedimentation in the Volkovce Formation upper part, when a
fan delta of the paleo-Hron river entered the basin;
(c) Tectonically controlled Late Pliocene (4.1—2.6 Ma)
and Quaternary acceleration of the mountain chain uplift led
to the current landscape and development of the river net-
work.
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Acknowledgments: The authors wish to express gratitude to
the Geological Company EUROGEOLOGIC for providing
geophysical and geological data, and to the following review-
ers of article; M. Harzhauser, I. Magyar and P. Bosák for their
very useful suggestions which improved the scientific quality
of this paper. The work was financially supported by the Slo-
vak Research and Development Agency under the contracts
No. APVV-LPP-0120-60, APVV 0280-07, APVV 0158-06 &
ESF-EC-0006-07 and by the VEGA agency, under contracts
VEGA1/0483/10 & VEGA 1/0712/11.
References
Andrejeva-Grigorovich A.S., Kováč M., Halásová E., Hudáčková N.
& Zlinská A. 2003a: Division of the Middle and Upper Mio-
cene (Badenian—Pannonian) sediments in the Slovakia and
Ukraine; using nannoplankton and foraminifers’ data. Theoret-
ical examples from the current biostratigraphy of the Phanero-
zoic in Ukraine. (Kiiv) UDK 551 782.1, 551, 7 (in Russian).
Andrejeva-Grigorovich A.S., Fordinál K., Kováč M. & Zlinská A.
2003b: Occurrence of calcareous nannoplankton in the Pan-
nonian sediments of Slovakian Neogene Basins. Acta Univ.
Carolinae-Geologica 47, 1—33.
Bada G. 1999: Cenozoic stress field evolution in the Pannonian Basin
and surrounding orogens: Inference from kinematic indicators
and finite element stress modelling. PhD. Thesis, Vrije Univer-
siteit, Amsterdam, 1—204.
Bada G., Fodor L., Székely B. & Timár G. 1996: Tertiary brittle
faulting and stress field evolution in the Gerecse Mountains,
northern Hungary. Tectonophysics 255, 3—4, 269—289.
Bada G., Horváth F., Cloetingh S., Conbletz D.D. & Tóth T. 2001:
Role of topography-induced gravitational stresses in basin inver-
sion. The case study of the Pannonian Basin. Tectonics 20, 3,
343—363.
Baráth I. & Kováč M. 1995: Sedimentology and paleogeography of
the Pliocene Hron river delta in the Komjatice depression
(Danube Basin). Miner. Slovaca 27, 4, 236—242.
Bernor R.L., Brunet M., Ginsburg L., Mein P., Picford M., Rögl F.,
Sen S., Steiniger F. & Thomas H. 1987: A consideration of some
major topics concerning Old World Miocene Mammalian chro-
nology, migrations and paleogeography. Geobios 20, 4, 431—439.
Bernor R.L., Solounias N., Swisher C.C. III & van Couvering J.A.
1996: The correlation of three classical “Pikermian” mammal
faunas – Maragheh, Samos, and Pikermi – with the Europe-
an MN unit system. In: Bernor R.L., Fahlbusch V. & Mittmann
H.-W. (Eds.): The evolution of Western Eurasian Neogene
Mammal Fauna. Columbia University Press, 137—154.
Cloetingh S., Matenco L., Bada G., Dinu C. & Mocanu V. 2005:
The evolution of the Carpathians—Pannonian system: Interac-
tion between neotectonics, deep structure, polyphase orogeny
and sedimentary basins in a source to sink natural laboratory.
Tectonophysics 410, 1—14.
Csató I. 1993: Neogene sequences in the Pannonian Basin, Hungary.
Tectonophysics 226, 377—400.
Csató I., Kendall Ch.G.St.C. & Moore P.D. 2007: The Messinian
problem in the Pannonian Basin, Eastern Hungary – Insights
from stratigraphic simulations. Sed. Geol. 201, 111—140.
Csontos L. 1995: Tertiary tectonic evolution of the Intra-Carpathian
area: a review. Acta Vulcanol. 7, 2, 1—13.
Czászár G. (Ed.) 1997: Basic lithostratigraphic units of Hungary.
Geol. Inst. Hung., Budapest, 1—114.
Cziczer I., Magyar I., Pipík R., Böhme M., Ćorić S., Bakrač K., Sütő-
Szentai M., Lantos M., Babinszki E. & Müller P. 2009: Life in
the sublittoral zone of long-lived Lake Pannon: paleontological
analysis of the Upper Miocene Szák Formation, Hungary. Int. J.
Earth. Sci. (Geol. Rundsch.) 98, 1741—1766.
Daxner-Höck G. 1996: Faunenwandel im Obermiozän und Korrela-
tion der MN-“Zonen” mit den Biozonen des Pannons der Zen-
tralen Paratethys. Beitr. Paläont. 21, 1—9.
Daxner-Höck G., Hír J., Joniak P., Kordos L. & Sabol M. 2004: Ro-
dent asemblages from the Central Paratethys. Stratigraphical
and Palaeoenvironmental Considerations, European Science
Foundation, EEDEN Meeting, 3—7 Nov., Irakleion, 1—3.
Dérerová J., Zeyen H., Bielik M. & Salman K. 2006: Application of
integrated geophysical modeling for determination of the conti-
nental lithospheric thermal structure in the Eastern Carpathians.
Tectonics 25, 3, s. Art. No. TC3009.
Fejfar O. 1961a: Die plio-pleistozänen Wirbeltierfaunen von Hajnáč-
ka und Ivanovce (Slowakei), ČSSR. II. Microtidae und Crice-
tidae inc. sed. Neu. Jb. Geol. Paläont., Abh. 112, 1, 48—82.
Fejfar O. 1961b: Die plio-pleistozänen Wirbeltierfaunen von Hajnáč-
ka und Ivanovce (Slowakei), ČSSR. I. Die Fundumstände und
Stratigraphie. Neu. Jb. Geol. Paläont., Abh. 111, 3, 257—273.
Fejfar O. 1966: Die plio-pleistozänen Wirbeltierfaunen von Hajnáčka
und Ivanovce (Slowakei), ČSSR. V. Allosorex stenodus n.g.
n.sp. aus Ivanovce A. Neu. Jb. Geol. Paläont., Abh. 123, 3,
221—248.
Fejfar O. 1970: Die plio-pleistozänen Wirbeltierfaunen von Hajnacka
und Ivanovce (Slowakei), ČSSR. VI. Cricetidae (Rodentia,
Mammalia). Mitt. Bayer. Staatsslg. Paläont. Hist. Geol. 10,
277—296.
Fejfar O. & Heinrich W.D. 1985: Zur Bedeutung der Wirbeltierfund-
stätten von Ivanovce und Hajnáčka für die Säugetierpaläontolo-
gie im Pliozän und frühen Pleistozän in Europa: Kenntnisstand
und Probleme. Věst. Ústř. Úst. Geol. 60, 4, 213—225.
Fodor L., Csontos L., Bada G., Györfi I. & Benkovics L. 1999: Ter-
tiary tectonic evolution of the Pannonian basin system and
neighbouring orogens: a new synthesis of paleostress data. In:
Durand B., Jolivet L., Horváth F. & Séranne M. (Eds.): The
Mediterranean Basins: Tertiary extension within the Alpine
Orogen. Geol. Soc. London, Spec. Publ. 156, 295—334.
Fordinál K. 1994: Upper Pannonian (zone H) on Eastern Edge of the
Považský Inovec Mts. Geol. Práce, Spr., 99, GÚDŠ, Bratislava,
67—75 (in Slovak).
Fordinál K. 1997: Mollusc (gastropoda, bivalvia) from the Pannonian
deposits of the western part of the Danube Basin (Pezinok-clay
pit). Slovak Geol. Mag. 3, 4, 263—283.
Fordinál K. 1998: Freshwater gastropods of Upper Pannonian age in
the northern part of the Danube basin. Slovak Geol. Mag. 4, 4,
293—300.
Fordinál K. & Nagy A. 1997: Hlavina member – marginal Upper
Pannonian sediments of the Rišňovce depression.
Miner. Slo-
vaca 29, 401—406 (in Slovak).
Gradstein F.M., Ogg J.G. & Smith A.G. (Eds.) 2004: A geologic time
scale 2004. Cambridge Univ. Press, 1—610.
Haq B.U. 1991: Sequence stratigraphy, sea level change and signifi-
cance for the deep sea. In: MacDonald D.I.M. (Ed.): Sedimen-
tation, tectonics and eustasy. SEPM Spec. Publ. 12, 3—39.
Haq B.U., Hardenbol J. & Vail P.R. 1988: Mesozoic and Cenozoic
chronostratigraphy and cycles of sea level changes. In: Wilgus
C.K., Hastings B.S., Kendall C.G.St.C., Posamentier H.W.,
Ross C.A. & Van Wagoner J.C. (Eds.): Sea level changes – an
integrated approach. SEPM Spec. Publ. 42, 71—180.
Hardenbol J., Thierry J., Farley M.B., Jacquin T., Graciansky P.C.
& Vail P.R. 1998: Mesozoic and Cenozoic sequence chrono-
stratigraphic framework of European Basins. In: Graciansky
C.P., Hardenbol J., Jacquin T. & Vail P.R. (Eds.): Mesozoic
and Cenozoic sequence stratigraphy of European Basins.
SEPM Spec. Publ. 60, 3—13.
532
KOVÁČ, SYNAK, FORDINÁL, JONIAK, TÓTH, VOJTKO, NAGY, BARÁTH, MAGLAY and MINÁR
GEOLOGICA CARPATHICA
GEOLOGICA CARPATHICA
GEOLOGICA CARPATHICA
GEOLOGICA CARPATHICA
GEOLOGICA CARPATHICA, 2011, 62, 6, 519—534
Harzhauser M. & Binder H. 2004: Synopsis of the late Miocene mol-
lusc fauna of the classical sections Richardhof and Eichkogel in
the Vienna Basin. Arch. Molluskenkunde 133, 1/2, 109—165.
Harzhauser M. & Mandic O. 2008: Neogene lake systems of Central
and South-Eastern Europe: Faunal diversity, gradients and interre-
lations. Palaeogeogr. Palaeoclimatol. Palaeoecol. 260, 417—434.
Harzhauser M. & Tempfer P.M. 2004: Late Pannonian wetland ecolo-
gy of the Vienna Basin based on molluscs and lower vertebrate
assemblages (Late Miocene, MN9, Austria). Cour. Forsch.-Inst.
Senckenberg. 246, 55—68.
Harzhauser M., Daxner-Höck G. & Piller W.E. 2004: An integrated
stratigraphy of the Pannonian (Late Miocene) in the Vienna Ba-
sin. Aust. J. Earth Sci. 95/96, 6—19.
Herrmann P., Scharek P., Kaiser M., Pristaš J. & Tkáčová H. 1998:
Map of genetic types and thickness of Quarternary sediments,
1 : 200,000. In: Scharek P. (Ed.): DANREG Danube Region En-
vironmental Research. MÁFI, GÚDŠ, GSSR, GBA.
Holec P. 1981: Occurrence of Hipparion primigenium (Meyer, H.V.
1829) (Mammalia, Equidae) remnants in the Neogene of the
Western Carpathians (Slovakia, Czechoslovakia). Geol. Zbor.
Geol. Carpath. 32, 4, 427—447.
Holec P. 1986: Neueste Resultate der Untersuchung von Neogenen
und Quartären Nashörnem, Bären und Kleinsäugern in dem Be-
reich der Westkarpaten (Slowakei). Acta Univ. Carol. Geol. 2,
223—231.
Holec P. 1996: A Plio-Pleistocene large mammal fauna from Strekov
and Nová Vieska, south Slovakia. Acta Zoologica Cracoviensia
39, 219—222.
Holec P. 2005:
Deinotherium giganteum Kaup (Proboscidea, Mam-
malia) of Pezinok brickyard pit (Pannonian). Miner. Slovaca
37, 551—554 (in Slovak).
Holec P., Kováč M., Sliva ., Vojtko R. & Joniak P. 2002: Finds of
Mastodon Mammut borsoni (Hays, 1834) near Ceroviny village,
stratigraphy and lithological conditions. Miner. Slovaca 34, 5—6,
353—358 (in Slovak).
Horváth F. 1993: Towards a mechanical model for the formation of
the Pannonian basin. Tectonophysics 226, 333—357.
Horváth F., Bada G., Szafián P., Tari G., Ádám A. & Cloetingh S.
2006: Formation and deformation of the Pannonian basin: Con-
straints from observational data. In: Gee D.G. & Stephenson
R.A. (Eds.): European lithosphere dynamics. Geol. Soc. London,
Mem. 32, 191—206.
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.
Hudáčková N. 1995: Dinoflagellata from the Pannonian sediments of
the NW part of Vienna basin. Roman. J. Stratigr. 76, 7, 1.
Hudáčková N. & Slamková M. 2000: Paleoecological reconstruction
of the Pannonian sediments of the NW part of the Vienna Basin
based on palynology. Miner. Slovaca 32, 4, 1—439.
Hugueney M. 1999: 28. Family Castoridae. In: Rössner G.E. & Heis-
sig K. (Eds.): The Miocene land mammals of Europe. Verlag
Dr. Friedrich Pfeil, München, 281—300.
Janáček J. 1969: New stratigraphic information on the Pliocene fill-
ing of central part of Danube Lowland. Geol. Práce, Spr. 50,
113—131 (in Slovak).
Jarosinski M., Beekman F., Matenco L. & Cloetingh S. 2011: Me-
chanics of basin inversion: Finite element modelling of the Pan-
nonian Basin System. Tectonophysics 502, 1—2, 121—145.
Jámbor Á., Korpás-Hódi M., Széles M. & Sütő-Szentai M. 1985:
Zentrales Mittleres Donaubecken: Bohrung Lajoskomárom Lk-1,
S-Balaton. In: Papp A., Jámbor Á. & Steininger F.F. (Eds.):
Chronostratigraphie und Neostratotypen, Miozän M
6
Pannon-
ien. Akadémiai Kiadó, Budapest, 204—241.
Jiříček R. 1974: Biostratigraphy of the Pliocene sediments of the
Komjatice Depression. [Biostratigrafia pliocénu komjatickej
depresie.] MS, Archív GÚDŠ, Bratislava.
Joniak P. 2005: New rodent assemblages from the Upper Miocene
deposits of the Vienna Basin and Danube Basin. MS, PhD.
Thesis, Comenius Univ., Bratislava, 1—134.
Juhász Gy. 1991: Lithostratigraphical and sedimentological frame-
work of the Pannonian (s.l.) sedimentary sequence in the Hun-
garian Plain (Alföld), Eastern Hungary. Acta Geol. Hung. 34,
53—72.
Juhász Gy. 1994: Comparison of the sedimentary sequences in Late
Neogene subbasins in the Pannonian Basin. Földt. Közl. 124, 4,
341—365.
Juhász Gy., Pogácsás Gy., Magyar I. & Vakarcs G. 2007: Tectonic
versus climatic control on the evolution of fluvio-deltaic sys-
tems in a lake basin, Eastern Pannonian Basin. Sed. Geol. 202,
72—95.
Kaiser T.M. & Bernor R.L. 2006: The Baltavar Hippotherium: a
mixed feeding Upper Miocene hipparion (Equidae, Perissodac-
tyla) from Hungary (East-Central Europe). Beitr. Paläont. 30,
241—267.
Kilényi E. & Šefara J. (Eds.) 1989: Pre-Tertiary basement contour map
of the Carpathian Basin beneath Austria, Czechoslovakia and
Hungary. Eötvös Lóránd Geophys. Inst., Budapest, Hungary.
Konečný V., Kováč M., Lexa J. & Šefara J. 2002: Neogene evolution
of the Carpatho-Pannonian region: an interplay of subduction
and back-arc diapiric uprise in the mantle. EGS Stephan Mueller
Spec. Publ. 1, 105—123.
Kordos L. 1987: Neogene Vertebrate Biostratigraphy in Hungary.
Ann. Inst. Geol. Publ. Hung. 70, 393—396.
Kováč M. 2000: Geodynamical, paleographical and structural de-
velopment of the Carpathian-Pannonian region in Miocene.
New view on Slovak Neogene basins. [Geodynamický, paleo-
geografický a štruktúrny vývoj karpatsko-panónskeho regiónu
v miocéne: Nový poh ad na neogénne panvy Slovenska.] Veda,
Bratislava, 1—202 (in Slovak).
Kováč M., Nagymarosy A., Soták J. & Šútovská K. 1993: Late Ter-
tiary paleogeographic evolution of the Western Carpathians.
Tectonophysics 226, 401—415.
Kováč M., Baráth I., Kováčová-Slamková M., Pipík R., Hlavatý I. &
Hudáčková N. 1998: Late Miocene paleoenvironments and se-
quence stratigraphy: northern Vienna Basin. Geol. Carpathica
49, 6, 445—458.
Kováč M., Holcová K. & Nagymarosy A. 1999: Paleogeography, pa-
leobathymetry and relative sea-level changes in the Danube Ba-
sin and adjacent areas. Geol. Carpathica 50, 4, 1—13.
Kováč M., Fordinál K., Grigorovich A.S.A., Halásová E., Hudáč-
ková N., Joniak P., Pipík R., Sabol M., Kováčová M. & Sliva
. 2005: Western Carpathian fossil ecosystems and their rela-
tion to paleoenvironment in context of Euroasia Neogene de-
velopment Geol. Práce, Spr. 111, 61—121, ŠGÚDŠ, Bratislava
(in Slovak).
Kováč M., Baráth I., Fordinál K., Grigorovich A.S., Halásová E.,
Hudáčková N., Joniak P., Sabol M., Slamková M., Sliva . &
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, 32—52.
Kováč M., Andrejeva-Grigorovič A., Baráth I., Beláčková K.,
Fordinál K., Halásová E., Hók J., Hudáčková N., Chalupová B.,
Kováčová M., Pipík R., Sliva . & Šujan M. 2008: Lithology,
sedimentology and biostratigraphy of the ŠVM-1 Tajná bore-
hole. Geol. Práce, Spr. 114, 51—84 (in Slovak).
Kováč M., Synak R., Fordinál K. & Joniak P. 2010: Dominant events
in the northern Danube Basin palaeogeography – a tool for
533
LATE MIOCENE—PLIOCENE DEPOSITIONAL SYSTEMS AND SEDIMENTARY CHANGES OF THE DANUBE BASIN
GEOLOGICA CARPATHICA
GEOLOGICA CARPATHICA
GEOLOGICA CARPATHICA
GEOLOGICA CARPATHICA
GEOLOGICA CARPATHICA, 2011, 62, 6, 519—534
specification of the Upper Miocene and Pliocene stratigraphy
Acta Geol. Slovaca 2, 1, 23—35 (in Slovak).
Kováč M., Hók J., Minár J., Vojtko R., Bielik M., Pipík R., Rakús
M., Krá J., Šujan M. & Králiková S. 2011: Neogene and Qua-
ternary development of the Turiec Basin and landscape in its
catchment: a tentative mass balance model. Geol. Carpathica
62, 4, 361—379.
Králiková S., Hók J. & Vojtko R. 2010: Stress change inferred from
the morphostructures and faulting of the Pliocene sediments in
the Hronská pahorkatina highlands (Western Carpathians). Acta
Geol. Slovaca 2, 1, 17—22.
Kvaček Z., Kováč M., Kovar-Eder J., Doláková N., Jechorek H.,
Parashiv V., Kováčová M. & Sliva . 2006: Miocene evolution
of the landscape and vegetation in the Central Paratethys. Geol.
Carpathica 57, 4, 295—310.
Lankreijer A. 1998: Rheology and basement control on extensional
basin evolution in Central and Eastern Europe: Variscan and Al-
pine-Carpathian-Pannonian tectonics. NSG Publication 980101,
Vrije Universiteit.
Lankreijer A., Kováč M., Cloetingh S., Pitonák 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.
Lankreijer A., Bielik M., Cloetingh S. & Majcin D. 1999: Rheology
predictions across the Western Carpathians, Bohemian Massif
and the Pannonian Basin: implications for tectonic scenarios.
Tectonics 18, 6, 1139—1153.
Leever K.A., Matenco L., Garcia-Castellanos D. & Cloetingh
S.A.P.L. 2011: The evolution of the Danube gateway between
Central and Eastern Paratethys (SE Europe): Insight from nu-
merical modelling of the causes and effects of connectivity be-
tween basins and its expression in the sedimentary record.
Tectonophysics 502, 1—2, 175—195.
Magyar I. 2009: Pannonian Basin paleogeography and paleoenvi-
ronments during Late Miocene based on paleontology and seis-
mic interpretation. GeoLitera, Szeged, 7-134 (in Hungarian).
Magyar I., Geary D.H. & Müller P. 1999: Paleogeographic evolution
of the Late Miocene Lake Pannon in Central Europe. Palaeo-
geogr. Palaeoclimatol. Palaeoecol. 147, 151—167.
Magyar I., Lantos M., Ujszaszi K. & Kordos L. 2007: Magnetostrati-
graphic, seismic and biostratigraphic correlations of the Upper
Miocene sediments in the northwestern Pannonian Basin Sys-
tem. Geol. Carpathica 58, 3, 277—290.
Marko F., Kováč M., Fodor L. & Šútovská K. 1990: Deformations
and kinematics of a Miocene shear zone in the northern partof
the Little Carpathians (Buková furrow, Hrabník Formation).
Miner. Slovaca 22, 5, 399—410 (in Slovak).
Marko F., Fodor L. & Kováč M. 1991: Miocene strike-slip faulting
and block rotation in Brezovské Karpaty Mts. (Western Car-
pathians). Miner. Slovaca 23, l89—200.
Marko F., Plašienka D. & Fodor L. 1995: Meso-Cenozoic tectonic
stress fields within the Alpine-Carpathian transition zone:
A review. Geol. Carpathica 46, l, l9—27.
Martini E. 1971: Standard Tertiary and Quaternary calcareous nanno-
plankton zonation. Proceedings of 2
nd
Planktonic Conference,
Roma 1970, 739—785.
Marunteanu M. 1997: Pannonian nannoplankton zonation. Interna-
tional Symposium Geology in the Danube Gorges, Geologija
derdapa, Orszova, 263—265.
Mazúr E. 1963: Žilina depression and adjacent mountains. [Žilinská
kotlina a pri ahlé pohoria.] Vydav. SAV, Bratislava, 1—184 (in
Slovak).
Metz-Muller F. 1995: Mise en évidence d’une variation intra-spéci-
fique des caractères dentaires chez Anancus arvernensis (Pro-
boscidea, Mammalia) du gisement de Dorkovo (Pliocène ancien
de Bulgarie, biozone MN14). Geobios 28, 737—743.
Meulenkamp J.E., Kováč M. & Cicha I. 1996: On Late Oligocene to
Pliocene depocenter migrations and the evolution of the Car-
pathian-Pannonian system. Tectonophysics 266, 301—317.
Minár J. 2003: Midmountain level in the West Carpathians as tec-
toplain: outline of the work hypothesis. Geografický časopis 55,
2, 141—158 (in Slovak).
Minár J., Bielik M., Kováč M., Plašienka D., Barka I., Stankoviansky
M. & Zeyen H. 2011: New morphostructural subdivision of the
Western Carpathians: an approach integrating geodynamics
into targeted morpohometric analysis. Tectonophysics 502, 1—2,
158—174.
Mottl M. 1939: Mitteilungen und Jahrbuch Konigliche. Ungar. Geol.
Anstalt. 32, 2, 266—350.
Musil R. 1959: The first find of Deinotherium gigantissimum Stefa-
nescu, 1892 in our country. [První nález druhu Deinotherium
gigantissimum Stephanescu, 1892 na našom území.] Čas.
Moravského Musea, Vědy přírodní 44, 81—88 (in Czech).
Nagy A., Fordinál K., Brzobohatý R., Uher P. & Raková J. 1995: Up-
per Miocene from SE margin of the Malé Karpaty Mts. (well
Ma-1, Bratislava)
.
Miner. Slovaca 27, 113—132 (in Slovak).
Nargolwalla M.C., Hutchison M.P. & Begun D.R. 2006: Middle and
Late Miocene terrestrial vertebrate localities and paleoenviron-
ments in the Pannonian Basin. Beitr. Paläont. 30, 347—360.
Papp A. 1951: Das Pannon des Wiener Beckens. Mitt. Geol. Gesell.
39—41, 99—193.
Papp A. 1953: Die Molluskenfauna des Pannon im Wiener Becken.
Mitt. Geol. Gesell. 44, 85—222.
Pogácsás Gy. & Seifert P. 1991: Vergleich der neogenen Meeres-
spiegelschwankungen im Wiener und im Pannonischen Becken.
In: Lobitzer H. & Császár G. (Eds.): Jubileumsschrift 20 Jahre
Geologische Zusammenarbeit Österreich-Ungarn. Publisher
Geologisches Bundesamt, Wien—Bécs, 93—100.
Popov S.V., Scherba I.G., Ilyina L.B., Nevesskaya L.A., Paramonova
N.P., Khondkarian S.O. & Magyar I. 2006: Late Miocene to
Pliocene palaeogeography of the Paratethys and its relation to
the Mediterranean. Palaeogeogr. Palaeoclimatol. Palaeoecol.
238, 91—106.
Priechodská Z. & Harčár J. 1988: Explanation to geological map of
the north-eastern part of the Podunajská lowland. (M 1 : 50,000).
GÚDŠ, Bratislava, 1—114 (in Slovak).
Royden L.H. & Horváth F. (Eds.) 1988: The Pannonian Basin.
A study in basin evolution. AAPG Mem., Tulsa 45, 1—394.
Rögl F. 1998: Paleogeographic consideration for Mediterranean and
paratethys seaways (Oligocene to Miocene). Ann. Naturhist.
Mus. Wien 99A, 279—310.
Ruszkiczay-Rüdiger Zs., Dunai T., Bada G., Fodor L. & Horváth E.
2005: Middle to late Pleistocene uplift rate of the Hungarian
Mountain Range at the Danube Bend (Pannonian Basin), using
in situ produced 3He. Tectonophysics 410, 173—187.
Sabol M. & Holec P. 2002: Temporal and spatial distribution of
Miocene mammals in the Western Carpathians (Slovakia).
Geol. Carpathica 53, 4, 269—279.
Sacchi M. & Horváth F. 2002: Towards a new time scale for the Up-
per Miocene continental series of the Pannonian basin (Central
Paratethys). EGU Stephan Mueller, Spec. Publ. Ser. 3, 79—94.
Scharek P., Herrmann P., Kaiser M. & Pristaš J. 2000: Map of ge-
netic types and thickness of quaternary sediments. In: Császár
G. (Ed.): Danube Region Environmental Geology Programme
DANREG Explanatory Notes. Jb. Geol. B—A 4, 447—455.
Solounias N., Plavcan M., Quade J. & Witmer L. 1999: The Piker-
mian Biome and the savanna myth. In: Agusti J., Andrews P.
& Rook L. (Eds.): Evolution of the Neogene terrestrial ecosys-
tems in Europe. Cambridge Univ. Press, 427—444.
Sütő-Szentai M. 1988: Microplankton zones of organic sceleton in
the Pannonian s.l. stratum complex and in the upper part of the
Sarmatian strata. Acta Botanica Hung. 34, 339—356.
534
KOVÁČ, SYNAK, FORDINÁL, JONIAK, TÓTH, VOJTKO, NAGY, BARÁTH, MAGLAY and MINÁR
GEOLOGICA CARPATHICA
GEOLOGICA CARPATHICA
GEOLOGICA CARPATHICA
GEOLOGICA CARPATHICA
GEOLOGICA CARPATHICA, 2011, 62, 6, 519—534
Sütő-Szentai M. 1990: Mikroplanktonflora der pontischen (ober-
pannonischen) Bildungen Ungarns. In: Stevanovic P.M.,
Nevesskaya L.A., Marinescu Fl., Sokać A. & Jámbor Á.
(Eds.): Chronostratigraphie und Neostratotypen. Neogen der
Westlichen (“Zentrale”) Paratethys, VIII, Pl1 Pontien. JAZU
and SANU, Zagreb—Belgrade, 842—869.
Szuromi-Korecz A., Sütő-Szentai M. & Magyar I. 2004: Biostrati-
graphic revision of the Hód-I well: Hungary’s deepest borehole
failed to reach the base of the Upper Miocene Pannonian Stage.
Geol. Carpathica 55, 6, 475—485.
Tari G., Horváth F. & Rumpler J. 1992: Styles of extension in the
Pannonian Basin. Tectonophysics 208, 1—3, 203—219.
Tóth Cs. 2010a: Miocene and Early Pliocene proboscideans of Slova-
kia. PhD. Thesis, Comenius University, Bratislava, 1—225 (in
Slovak).
Tóth Cs. 2010b: Paleoecology and diversity of Neogene probosci-
beans (Proboscidea, Mammalia) from the Slovak part of the
Western Carpathians area depending on climatic changes and
biotic interactions. Miner. Slovaca 42, 4, 439—452.
Uhrin A., Magyar I. & Sztanó O. 2009: Control of the Late Neogene
(Pannonian s.l.) sedimentation by basement deformation in the
Zala Basin. Földt. Közl. 139, 3, 273—282 (in Hungarian with
English abstract).
Vakarcs G., Vail P.R., Tari G., Pogácsás Gy., Mattick R.E. & Szabó
A. 1994: Third-order Middle Miocene—Early Pliocene deposi-
tional sequences in the prograding delta complex of the Pannon-
ian Basin. Tectonophysics 240, 1—4, 81—106.
van Dam J.A. 2006: Geographic and temporal patterns in the late
Neogene (12—3 Ma) aridification of Europe: The use of small
mammals as paleoprecipitation proxies. Palaeogeogr. Palaeo-
climatol. Palaeoecol. 238, 1—4, 190—218.
Vasiliev I. 2006: A new chronology for the Dacian Basin (Romania).
Consequences for the kinematic and paleoenvironmental evolu-
tion of the Paratethys region. Geologica Ultraiect. 267, 1—193.
Vasiliev I., Krijgsman W., Langereis Cor G., Panaiotu C.E., Ma enco
L. & Bertotti G. 2004: Towards an astrochronological frame-
work for the Eastern Paratethys Mio-Pliocene sedimentary se-
quences of the Foc ani basin (Romania). Earth Planet. Sci. Lett.
227, 3—4, 231—247.
Vass D. 2002: Lithostratigraphy of Western Carpathians: Neogene
and Buda Paleogene. GÚDŠ, Bratislava, 1—200 (in Slovak).
Vlačiky M., Sliva ., Tóth Cs., Karol M. & Zervanová J. 2008: The
fauna and sedimentology of the locality Nová Vieska (Villafran-
chian, SR). Acta Musei Moraviae, Sci. Geol. 93, 229—244 (in
Slovak with English summary).
Vojtko R., Hók J., Kováč M., Sliva ., Joniak P. & Šujan M. 2008:
Pliocene to Quaternary stress field change in the western part of
the Central Western Carpathians (Slovakia). Geol. Quart. 52, 1,
19—30.
Wenz W. & Edlauer A. 1942: Die Molluskenfauna der oberpontis-
chen Süsswassermergel vom Eichkogel bei Mödling, Wien.
Arch. Molluskenkunde 74, 82—98.