GeolCarp_Vol67_No6_525

GEOLOGICA CARPATHICA

, DECEMBER 2016, 67, 6, 525 – 542

doi: 10.1515/geoca-2016-0033

www.geologicacarpathica.com

Late Miocene sedimentary record of the Danube / Kisalföld

Basin: interregional correlation of depositional systems,

stratigraphy and structural evolution

ORSOLYA SZTANÓ

, MICHAL KOVÁČ

, IMRE MAGYAR

3,4

, MICHAL ŠUJAN

, LÁSZLÓ FODOR

ANDRÁS UHRIN

, SAMUEL RYBÁR

, GÁBOR CSILLAG

and LILLA TŐKÉS

Department of Physical and Applied Geology, Eötvös Loránd University, H-1117 Budapest, Pázmány Péter sétány 1/c, Hungary;

sztano.orsolya@gmail.com

Department of Geology and Palaeontology, Faculty of Natural Sciences, Comenius University, Mlynská dolina 842 15, Bratislava, Slovakia

MOL Hungarian Oil and Gas Plc., H-1117 Budapest, Október 23. u. 18, Hungary; immagyar@mol.hu

MTA-MTM-ELTE Research Group for Palaeontology, H-1431 Budapest, Pf. 137, Hungary

MTA-ELTE Geological, Geophysical and Space Science Research Group of the Hungarian Academy of Sciences, Eötvös University,

H-1117 Budapest, Pázmány Péter sétány 1/c, Hungary

Eriksfiord AS, N-4068 Stavanger, Postboks 8034, Norway

Geological and Geophysical Institute of Hungary, H-1143 Budapest, Stefánia út 14, Hungary

(Manuscript received April 27, 2016; accepted in revised form September 22, 2016)

Abstract: The Danube / Kisalföld Basin is the north-western sub-basin of the Pannonian Basin System. The lithostrati-

graphic subdivision of the several-km-thick Upper Miocene to Pliocene sedimentary succession related to Lake Pannon

has been developed independently in Slovakia and Hungary. A study of the sedimentary formations across the entire basin

led us to claim that these formations are identical or similar between the two basin parts to such an extent that their

correlation is indeed a matter of nomenclature only. Nemčiňany corresponds to the Kálla Formation, representing locally

derived coarse clastics along the basin margins (11– 9.5 Ma). The deep lacustrine sediments are collectively designated

the Ivanka Formation in Slovakia, while in Hungary they are subdivided into Szák (fine-grained transgressive deposits

above basement highs, 10.5 – 8.9 Ma), Endrőd (deep lacustrine marls, 11.6 –10 Ma), Szolnok (turbidites, 10.5 – 9.2 Ma)

and Algyő Formations (fine-grained slope deposits, 10 – 9 Ma). The Beladice Formation represents shallow lacustrine

deltaic deposits, fully corresponding to Újfalu (10.5 – 8.7 Ma). The overlying fluvial deposits are the Volkovce and

Zagyva Formations (10 – 6 Ma). The synoptic description and characterization of these sediments offer a basin-wide

insight into the development of the basin during the Late Miocene. The turbidite systems, the slope, the overlying deltaic

and fluvial systems are all genetically related and are coeval at any time slice after the regression of Lake Pannon initiated

about 10 Ma ago. All these formations get younger towards the S, SE as the progradation of the shelf-slope went on.

The basin got filled up to lake level by 8.7 Ma, since then fluvial deposition dominated.

Keywords: Late Miocene, Tortonian, Pannonian, lithostratigraphy, Pannonian Basin, turbidites, delta, alluvial.

Introduction

The main objective of this study is to establish a correlation

between the Late Miocene–Pliocene lithostratigraphic systems

of the northern, Slovakian and the southern, Hungarian parts

of the Danube / Kisalföld Basin (DKB), a sub-basin of the

Neogene Pannonian Basin System. This approximately 200 km

long and 120 km wide, NE–SW trending basin is crossed in

the middle by the Danube, which marks the international

boundary between Slovakia to the north and Hungary to the

south (Fig. 1). In Slovakia, the area is known as “Danube

Lowland” because it lies adjacent to and was formed mainly

by the activity of the Danube and its tributaries. The Hungarian

name of the region is Kisalföld (“Little Plain”), as opposed to

the Alföld (“Great Plain”), the latter referring to the central

part of the Pannonian Basin System located east of the middle

course of the Danube. To avoid confusion with other large

Miocene to Quaternary depocenters along the course of the

Danube, we prefer to name this portion of the system as

Danube / Kisalföld Basin.

Lithostratigraphic subdivision of the upper Neogene basin

fill evolved independently in Slovakia and Hungary, in spite of

the fact that the geological formations are continuous across

the political boundary. The attempt of correlation induced

re-consideration and re-definition of lithostratigraphic units in

both countries, and led to renewed description of the forma-

tions. This work was supported by mutual visits of the

Slovak-Hungarian team of authors to both parts of the DKB.

In this paper we give parallel description and characteri-

zation of each upper Neogene sedimentary formation, and

interpret the evolution of their depositional environment

within a large-scale tectonic and sedimentary framework.

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, 2016, 67, 6, 525 – 542

of the DKB were recently published by Magyar et al. (2000,

2007, 2013) and Šujan et al. (2016).

The present-day lithostratigraphic subdivision of the lacus-

trine to fluvial depositional sequence is a result of a historical

evolution in both countries. In Hungary, Jámbor (1980) elabo-

rated a lithostratigraphic system for the Pannonian deposits of

the Transdanubian Range, Gajdos et al. (1983) for the Panno-

nian of the Alföld (“Great Plain”), and Bardócz et al. (1987)

for the deep basins of western Hungary, including the DKB.

The proposal of Juhász (1994) to use a uniform lithostrati-

graphic subdivision for the basin deposits of the entire country

was accepted and implemented by the Stratigraphic Committee

of the Hungarian Academy of Sciences (Császár 1997). Recent

developments include the correlation and nomenclatural revi-

sion of the “basinal” and “marginal” formations and the con-

struction of a comprehensive lithostratigraphic model for the

entire Lake Pannon depositional system (e.g., Sztanó et al.

2013a).

In Slovakia, lithostratigraphy was based on correlation of

the regional (Central Paratethys) stages, such as the Panno-

nian, Pontian, and Dacian (e.g., Steininger et al. 1985); these

stages were defined as brackish water, brackish to freshwater,

and freshwater to terrestrial, respectively. All the three stages

were considered as distinct units bounded by transgressions

(e.g., Buday et al. 1967; Adam & Dlabač 1969; Biela 1978).

A formation system was introduced during the late 80’s, but

only the names changed: the Ivanka Fm. corresponded to the

same sequence as the previous “Pannonian”, the Beladice Fm.

to the “Pontian”, and the Volkovce Fm. to the “Dacian” (e.g.,

Priechodská & Harčár 1988; Vass et al. 1990; Vass 2002). By

definition, each formation contained several depositional sys-

tems (e.g., basinal, deltaic, alluvial) and variable lithology,

which led to difficulties in correlation. Recent efforts have

focused on establishing a genetic definition of depositional

systems in the lithostratigraphy of the northern DKB, and on

obtaining new geochronological constraints (Kováč et al.

2006, 2010, 2011; Šujan et al. 2016), which resulted in litho-

stratigraphic redefinitions included in this study.

Description of Formations

Kálla Formation / Nemčiňany Formation

Lithology, facies:

Kálla Formation (Fig. 2) is made up of

coarse siliciclastics. Grain size varies from very well-sorted

fine sand to coarse gravel. Colour is usually whitish grey or

yellow-brown depending on rate of limonitic cementation. Its

type locality is in the Kál Basin, located ca. 40 km south of the

DKB, where it is matured quartz-sand or “pearl” gravel made

up of well-rounded quartzite pebbles with only a minor amount

of metamorphics and local Mesozoic constituents (Jámbor

1980). The composition of the formation, however, strongly

depends on the geology of the source area. For instance, in the

western part of the DKB (south of the Sopron Hills) the

clastics are shed from a local source; most probably from the

Rosalia Mts. (Permo-Triassic metasediments, medium-grade

metamorphics). The Kálla Formation is usually characterized

by a steep depositional dip up to 15 – 25°, as the beds comprise

clinoforms. Small-scale cross-bedding, cross-lamination and

plane lamination may occur in horizontal topset beds. Low

angle dip differences in foreset beds, shallow scours or chutes,

and backsets are rather common. The height of individual

clinoforms is variable up to 20 m, but stacking of two or three

clinoform sets is a common feature. Small-scale syn-sedimen-

tary faults, more often deformation bands are present (Schmid

& Tari 2015); they are, at least partly, due to gravity-driven

deformation along clinoforms. There are also locations where

only very well sorted sand is present without any observable

sedimentary structures other than a few vertical burrows and

limonitic or quartz cementation features.

The Nemčiňany Gravel Formation (Kutham et al. 1963), the

potential equivalent of the Kálla Formation in the northern

DKB, is also a coarse siliciclastic succession. Its type area is

the Komjatice Depression, as seen in the Nemčiňany quarry,

where the rounded to well-rounded pebbles contain mainly

quartzite and volcanites, followed by metamorphics, quartz,

and variable content of carbonates. Again, the petrographic

composition mirrors the source area, including the proximal

Central Slovakian Neovolcanic Field and the Central Western

Carpathians. Clinoform foresets are built up by 10 – 30 cm

thick tabular beds of matrix-supported gravels with normal or

reverse gradation, and have a dip of 10 – 20°. Their height may

exceed 30 m. Channels with imbricated clast-supported gravels

are incised into the foresets, and trough-cross stratified gravels

in lenticular bodies up to 12 m wide occur in the topset units.

Several-metre-thick sandy-gravelly layers interfingering with

open-water mudstones may still be part of the Nemčiňany

Formation (northern margin, well Bernolákovo-1).

In well logs, coarse clastics may appear at the base of the

Pannonian succession as low gamma ray blocky units. Resis-

tivity is usually moderate to low due to varying rate and type

of cementation (cf. Csillag et al. 2010).

Stratigraphic position, thickness:

The Kálla Formation

either directly overlies pre-Pannonian rocks or follows above

the Szák Formation. The interfingering of the Kálla and Szák

Formations was also documented (Csillag et al. 2010). The

Kálla Formation is usually overlain by shallow water deltaic

deposits of the Újfalu Formation. Its average thickness is

10 – 20 m, with a maximum of about 40 m.

The Nemčiňany Formation in the Želiezovce Depression

forms the several tens of metre thick basal part of the Panno-

nian succession (well Dubník-1). In the Komjatice Depression

it overlies a several tens of metres thick clayey-silty succes-

sion with brackish mollusc fauna, corresponding to the lower

part of the Ivanka Formation, which is an equivalent of the

Szák Formation. The overall thickness of the formation in this

part of the basin reaches 80 to 100 m, according to borehole

data.

Fossils, age: The coarse clastics of the Kálla and Nemčiňany

Formations rarely contain fossils. In the type area at the Kál

Basin, however, both molluscs and plant remains were found

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, 2016, 67, 6, 525 – 542

in the sand layers of the formation (Magyar 1988). The species

Lymnocardium schedelianum, Congeria pancici, Unio atavus,

and Melanopsis fossilis indicate the upper part of the Lymno

cardium conjungens littoral mollusc zone, which means an

age of 9.5 – 10.5 Ma (Fig. 2).

In the eastern Komjatice Depression, the Nemčiňany Gravel

was originally considered as part of the Volkovce Formation

of early Pliocene age (Priechodská & Harčár 1988; Baráth &

Kováč 1995). This assumption, however, contradicts both the

interpretation of the depositional environment and new strati-

graphic data. Biostratigraphic and magnetostratigraphic con-

straints from the ŠVM-1 Tajná borehole indicate the age of

these deposits younger than 10.0 Ma (Kováč et al. 2006,

2008), while five authigenic

Be /

Be ages point to deposition

between 9.5 and 11.0 Ma (Šujan et al. 2016).

Depositional environments:

The gravelly and gravelly to

sandy occurrences with clinoforms are interpreted as locally-fed

Gilbert-type deltas arriving into 10 – 30 m deep water along the

margin of Lake Pannon (Sztanó et al. 2010; Tóth et al. 2010).

Indications of fluvial transport and wave agitation are present

in the topsets. The steep foresets were formed by grain ava-

lanches, grain flows, and sandy debris flows with the common

occurrence of sliding. Transport of coarse clastics was limited

in the bottomsets, where decoupling of the suspended material

occurs, therefore the Gilbert-type delta deposits interfinger

with sublittoral clays (i.e. Szák Formation, Ivanka Formation)

in a very short distance. Longshore currents may have trans-

ported part of the sand into embayments along the shore,

where it was deposited on the shoreface (Budai et al. 1999;

Babinszki et al. 2003). The somewhat larger bodies along the

northern shore of Lake Pannon may have developed as

fan-deltas. In these cases a structurally active basin margin

and the lack of shallow shelf is supposed, therefore fan-deltas

may have provided some clastics into the deeper part of the

basin directly (e.g., Bernolákovo; Šujan et al. 2016).

Representative outcrops and boreholes:

The Kálla and

Nemčiňany Formations are exposed in gravel and sand pits

along the western margin of the DKB between Weppersdorf

and Lackendorf (Mostafavi 1978; Schmid & Tari 2015), near

the boundary of the Sopron-Eisenstadt basin in the upper part

of the gravel pit of Sopronkőhida-Piuszpuszta (Rosta 1993),

and in the north-eastern margin of the DKB in the gravel pits

of Volkovce, Nemčiňany, and Tajná. Important classical loca-

lities south of the DKB include Szentbékálla and Mindszent-

kálla (Magyar 1988) and Tapolca-Billege (Sztanó et al. 2010).

From boreholes within the DKB these formations were

reported either as a basal conglomerate of crystalline rocks

above the Mihályi High (e.g., well Mihályi-22; Kőrössy 1987),

or as coarse intercalations in the northern margin of the basin

from the well Bernolákovo-1 (several layers between 1050

and 820 m; Šujan et al. 2016), and the Dubník-1 well

(1250 – 1200 m) in the Želiezovce Depression.

Szák Formation / part of Ivanka Formation

Lithology, facies:

The Szák Formation (Fig. 2) is made up of

bluish grey silty clay marl. Occasionally it is laminated, but

most commonly it is structureless. Very thin, lenticular sandy

intercalations of a few mm may occur locally (Jámbor 1980).

In the bottom of the formation, a 0.2 – 2 m thick sandy gravel

occurs, with well-sorted and well-rounded pebbles, mostly

quartzite (Jámbor 1980). The grain size of the sandy, gravelly

beds rapidly decreases and they are sharply overlain by the

clay marl. Along the SE margin of the DKB (“Tata Horst”,

western Gerecse Hills) well-rounded gravel derived from local

Mesozoic carbonates also occur, some along eroded fault

Fig. 2. Litho-, bio-, magneto- and chronostratigraphy of the Late Miocene sedimentary fill of the Danube / Kisalföld Basin.

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scarps with abrasional reworking. It is supposed that these are

also interfingering with the basal layers of the clay marl. These

coarse basal units were formerly referred to as the Kisbér and

Diás Formations, respectively (Budai et al. 1999, 2008); they

are now classified as the Kisbér Member of the Szák Forma-

tion. In well logs the Szák Formation appears as a homo-

geneous shale unit with high gamma-ray and low resistivity

response.

Stratigraphic position, thickness:

The thickness of the for-

mation varies between 10 –100 m, increasing basinward, but

the average is less than 50 m. The formation unconformably

overlies pre-Pannonian rocks. Towards the basin margins it

may interfinger with locally-sourced coarse-grained deltas of

the Kálla / Nemčiňany Formation. At the same places the Kálla

Formation may serve as its stratigraphic cover as well. In

basin ward direction it interfingers with the Endrőd Formation.

The separation of these two formations can be based on fossil

content (more profundal forms in Endrőd), and on location

within the basin. The Szák Fm. occurs above local basement

highs, therefore even cm thick sandy intercalations are rare.

Their stratigraphic position is also different: the Szák Clay

Marl is covered by the shallow-water deltaic deposits of the

Újfalu Formation, whereas the Endrőd Marl is overlain by the

Szolnok or Algyő Formations.

An enigmatic situation occurs in well ŠVM-1 on the eastern

margin of the Komjatice Depression, where a continuous

transition between Sarmatian and Pannonian marls was docu-

mented by an endemic nannoplankton. An angular unconfor-

mity of 25° appeared ca. 30 m above the Sarmatian / Pannonian

boundary. The fossils of the Pannonian marls indicate a rela-

tively shallow depositional depth similar to the Szák

Formation and are covered by the Nemčiňany Fm. (Kováč et

al. 2008).

Fossils, age:

The formation is rich in fossils. Endemic

dreissenids (most commonly Congeria czjzeki, C. ungula

caprae, C. partschi), cardiids, and deep-water pulmonate

snails (lymnaeids, planorbids) constitute the mollusc fauna.

The ostracod assemblages are dominated by Candonidae

(Bakunella, Lineocypris, Serbiella, Camptocypria, Caspio

cypris, Typhlocyprella, Zalanyiella) and Leptocytheridae

(Cziczer et al. 2009). As to fish, sciaenid otoliths and skeletal

elements of percids were reported. Trace fossils (Spiro sipho

nella, Minisiphonella, Diplocraterion) are locally abundant.

Endemic dinoflagellates, coccolithophorids and cosmopolitan

green algae also occur (Kováč et al. 2006; Cziczer et al.

2009). The formation is usually rich in spores and pollen

(Jámbor 1980; Korpás-Hódi 1983; Nagy 2005; Cziczer et al.

2009; Barna et al. 2010). In the DKB, this formation belongs

to the Congeria czjzeki or Lymnocardium soproniense

sub

littoral mollusc zone and the Spiniferites paradoxus

dinoflagellate zone (Sütő-Szentai 1991; Nagy et al. 1995;

Cziczer et al. 2009; Magyar & Geary 2012). Magneto-

stratigraphic correlations suggest that its age in the western

margin of the DKB is older than 9.7 Ma, whereas in the

eastern margin it is 9.4 – 8.9 Ma (Magyar et al. 2007; Cziczer

et al. 2009).

The calcareous nannoplankton (zones Praenoelaerhabdus

banatensis and Noelaerhabdus bozinovicae / N. jerkovici) and

magnetostratigraphic data (chrons C5r2r to C5n1n) from the

ŠVM-1 well on the eastern margin of the Komjatice Depres-

sion and from the SE edge of the Malé Karpaty Mts. Ma-1

well in Bratislava dates the shallow open lacustrine deposits in

the time span of ca. 9.9 to 11.6 Ma (Nagy et al. 1995; Kováč et

al. 2006, 2008).

Depositional environments:

The Szák Formation is an open-

water lacustrine deposit, formed in non-agitated waters below

storm wave base. Palaeoecology of sublittoral molluscs and

other considerations (Cziczer et al. 2009) point to a depth of

about 20 – 30 to 80 – 90 m. The formation marks transgression

of Lake Pannon over elevated basement blocks, either along

the shore or inside the lake, which were inundated later during

the evolution. There is no significant clastic input other than

muds from the interfingering coarse-grained deltas. The lack

of coarse clastic intercalations of mass gravity flow origin

confirms the relatively elevated position, where shelf-slope

could not develop due to restricted water depth. The gravels at

the base of the formation are of local origin, marking either the

abrasion of rocky coasts, most probably controlled by faults

(along the SE basin margin, in the western Gerecse Hills, Tata

block etc.) or winnowing of older clastic sediments forming

the substratum (i.e. Oligocene Csatka Formation; Jámbor

1980). Thus the Kisbér Member of the Szák Formation repre-

sents a transgressive lag, the large areal extension of which

reveals the continuous retreat of the shoreline.

Representative outcrops and boreholes:

Brickyard claypits

in Sopron — Balfi-út (Balázs et al. 1981; Barna et al. 2010) in

the western margin of the basin, and in Tata, Szák, Kisbér,

Pápateszér, Bakonyszentlászló, Tapolcafő, Devecser along the

eastern margin (Cziczer et al. 2009). Shallow boreholes along

the eastern margin were analysed by Korpás-Hódi (1983). In

the northern DKB, no outcrop occurrence can be correlated

with the Szák Fm. A number of wells penetrated the succession

formerly assigned to the Ivanka Fm., such as Tajná ŠVM-1,

Bernolákovo-1, Diakovce-1, as well as Trakovice together with

the Madunice well series in the Blatné Depression.

Endrőd Marl Formation / Lower part of Ivanka Formation

Lithology, facies:

The lower part of the Endrőd Formation

usually consists of calcareous marl and marl. Upwards the

carbonate content decreases, the sediment becomes dark grey

to light grey, laminated to structureless clay marl, alternating

with mm to cm-thick siltstone interbeds. In the upper part of

the formation, thin sandy intercalations may occur (Bardócz et

al. 1987; Juhász 1994). Series of thin andesitic-trachytic tuff

layers or altered tuffs are also reported in the DKB (Kőrössy

1987; e.g., in Tét-6; Fig. 3). In well logs, the upward decrea sing

carbonate content is reflected in a characteristic bell shape.

The clay marl shows a rather smooth curve of high GR,

positive SP, and low resistivity. The seismic facies of the

formation is characterized by relatively continuous, moderate

to high amplitude reflections.

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Stratigraphic position, thickness:

The formation is supposed

to develop continuously from Sarmatian marls only in the

deepest parts of the basin (Zala Member; Gyalog & Budai

2004). Elsewhere it unconformably overlies pre-Pannonian

rocks, therefore its base is commonly marked by onlaps on

seismic profiles (Fig. 4). The calcareous marls are often

mentioned as Belezna or Tótkomlós Members (Kőrössy 1987;

Juhász 1994). In the deep basins, Endrőd Formation is overlain

by turbidite sandstones of the Szolnok Formation or, above

moderate basement highs, by the Algyő Formation. The

transition towards the overlying deposits can be sharp or

gradual depending on the appearance of turbidites. Its

thickness varies between 50 – 400 m, with an average of

200 m. Over the basement highs its thickness is often below

seismic resolution.

Fossils, age:

The lowermost part of Endrőd Formation often

contains a specific mollusc fauna with “Lymnocardium”

praeponticum, “L.” cekusi, Radix croatica, and Gyraulus

praeponticus, indicating the “Lymnocardium” praeponticum

Zone (Korpás-Hódi 1992). With the deepening of the water,

a low- diversity profundal assemblage becomes dominant with

Paradacna abichi, Congeria banatica, C. partschi maorti,

Velutinopsis sp., Undulotheca sp. The age of the formation in

the DKB spans from 11.6 to ca. 9.5 Ma. The intercalated tuff

layers were related to the 11–10 Ma activity of the Pásztori

Volcano (Harangi et al. 1995, 2015; Zelenka et al. 2004),

which was an island in the middle of the basin (Fig. 5).

Depositional environments:

The clay marls were deposited

mostly in several hundred metre deep profundal waters of

Lake Pannon. Above flooded basement highs, such as the

Mihályi High, the colour of the marl is usually light grey

(cf. Magyar et al. 2004). It is supposed that the oldest/

lowermost beds were formed below wave base in sublittoral

depth, but deepening occurred rapidly, and usually it is not

possible to distinguish the sublittoral and profundal deposits in

well data.

Representative outcrops and boreholes: The

Endrőd Forma-

tion does not have a surface occurrence in the vicinity of the

DKB. Calcareous marls at the base were reported from

Vaszar-1 and Gönyü-1 (Kőrössy 1987), tuffs are common in

Tét-6. The presence of Endrőd Marl in the northern part of the

DKB is expected, but very little information about its distribu-

tion and composition is known. It was identified in well

Kolárovo-4 (Fig. 3) and in nearby wells close to the foothills

of the Transdanubian Range.

A 400 m thick succession with brackish fauna in the wells

Nová Vieska-1 and Modrany-1 (Fig. 3) was considered by

Šujan et al. (2016) as shallow water Szák-type mudstone

according to fossil dinocysts (Baranyi et al. 2014). However,

the thickness and location indicates a much deeper environ-

ment. Now it is suggested that these strata represent deep

water marls followed by shelf-slope deposits, classified as

lower and upper Ivanka Formation, equivalent to Endrőd and

Algyő Formations, respectively, with redeposited fossils.

Unequivocal interpretation of this issue is hampered by the

absence of seismic sections in this area.

Szolnok Sandstone Formation / Middle part of Ivanka

Formation

Lithology, facies:

The Szolnok Formation comprises alter-

nations of fine to very fine sandstone and siltstones/marls,

with the dominance of sandstones. Graded beds, laminated to

cross-laminated or convolute beds, as well as massive

amalgamated sandstones occur. The sand-prone strata are

interpreted mostly as turbidites. Bed thickness is highly

variable, from a few cm to metres. Coarsening and thickening

upwards series alternate with fining and thinning up ones.

Thickness of the shale units is also variable (5 – 40 m). In well

logs, the sandy character with respect to the under- and

overlying muddy formations is spectacular. A few-metre-thick

blocky and several-tens-of-metre-thick barrel-shaped units

alternate (Fig. 3, Mihályi-28 and Tét-6). The thickness of

these sand bodies is typically 10 – 50 m in the central part of

the DKB and 80 – 180 m in the north (Fig. 3). Its seismic facies

is also highly variable from low to high amplitude reflections

with moderate continuity. Short reflections with downlaps or

onlaps are common (Fig. 4). Because of the sandy compo-

sition, this formation is mentioned in old Slovak literature as

the Great Lower Pannonian Sand (Vass 2002).

Stratigraphic position, thickness:

The Szolnok Formation is

always underlain by the Endrőd Marl and is overlain by the

Algyő Clay Marl. The latter may also contain some (10 – 30 m

thick) sandstone bodies in its lower part, so the boundary of

the two formations can be gradual. Therefore, if depicted from

well log data, the thickness of the Szolnok Formation is often

overestimated. The characteristic thickness is only a few

metres in the Csapod Trough. East of the Mihályi High it

attains 300 m, and it onlaps and pinches out on the Endrőd

Formation on the flank of the Transdanubian Range in the

eastern part of the DKB (Fig. 4). In the central depression its

thickness may exceed 1000 m (area of the Dunajská Streda-1

and Kolárovo wells, Fig. 3). Further to the north, above highs

in the north-western side of the Ripňany-Galanta fault system,

it is missing or very thin, whereas in the Rišňovce Depression

it accumulated up to a thickness of almost 500 m, seemingly

without accumulation of older deepwater marls, above the

Sarmatian deltaic Ripňany Formation (Fordinál & Elečko

2000).

Fossils, age:

The formation contains a typical, low- diversity

deep-water assemblage of Lake Pannon molluscs with

thin-shelled cardiids (Paradacna abichi, Paradacna sp.,

“Pontalmyra” otiophora), dreissenids (“Dreissenomya”

digitifera, Congeria banatica), and deep-water-adapted

pulmonate snails (planorbids and lymnaeids). Deposition of

the formation is basically connected to the advance of the

shelf-margin slope, thus it spans a relatively short time period

between 10 – 9.2 Ma. Older (ca. 10.5 Ma) turbidite successions

were detected only in the northernmost Rišňovce Depression

(Šujan et al. 2016), where they form separate sandy units.

On the other hand, turbidites related to the 9.5 – 9.2 Ma old

slope probably deposited further to the south, as in the Zala

Basin (Uhrin et al. 2009).

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Depositional environment:

Szolnok Formation was formed

as part of an extensive turbidite system. Sediments arriving

through the major fluvial feeder systems were partitioned

between the deltaic lobes (Újfalu / Beladice Formation) on the

shelf and the turbidite lobes in the deep basins. Locally sourced

coarse-grained deltas (i.e. Kálla / Nemčiňany Fms.) did not

contribute to the turbidite systems. The bulk of the sand spread

in the form of large flat lobes far from the slope, indicating no

or only minor confinement, as the centre of the DKB was large

enough. The elongated troughs to the south, mostly parallel to

the transport direction (i.e. slope progradation, cf. Uhrin

2011), might have produced lateral confinement. Some of the

minor depressions, bounded by fault-related highs or volcanic

edifices in downcurrent direction also might have acted as

local sediment traps. This might have been the case of the

Rišňovce Depression, where during a very short period of time

a very thick turbidite succession was stacked in a neccesarily

confined setting. Another interesting, probably confining,

situation might have caused the deposition of ca. 800 m thick

turbidite series in the Želiezovce Depression (Kolárovo wells,

Fig. 3), where the prograding slope itself partly blocked the

“entrance” to the elongated embayment surrounded by terres-

trial to sub-lacustrine highs on three sides (i.e. 9.2 – 9.0 Ma

shelf edge, Fig. 1).

Representative outcrops and boreholes:

The Szolnok

Formation does not have a surface exposure. Characteristic

well logs include those of Mihályi-22, -28, Bősárkány-I,

Vaszar-1-2, Gönyű-1, Kolárovo well series (1 – 4), Ripňany-1,

Vráble-1 (Fig. 3, Šujan et al. 2016).

Algyő Formation / Upper part of Ivanka Formation

Lithology, facies:

Dark grey clay marl, siltstone with sandy

intercalations. Few to 10s of metres thick sandstones may

occur near its top, but usually they are common in the lower

third of the formation. The claystones are often thin bedded to

structureless. Sandy-silty intercalations can be graded, lami-

nated or cross-laminated. Convolution, soft-sediment defor-

mation structures, sedimentary folds or cm-scale en-echelon

faults may occur in cores pointing to turbidity currents, slides,

slumps. In well logs, high gamma values, positive SP and low

resistivity are typical. The log shape is smooth to finely

serrated, the sand bodies appear as sharp peaks (Fig. 3). It is

easy to identify Algyő Formation on seismic profiles (Fig. 4):

it comprises clinoforms of 200 – 400 ms height, representing

300 – 630 m decompacted thickness (Balázs et al. 2015), which

can correspond to the same water depth in the DKB. The dip

angle of the original slope surfaces might have been 2 – 5°.

The upper, steep portions of clinoforms usually show low

amplitude, poor continuity seismic facies, while high ampli-

tude, long reflections are common in their basal part.

Stratigraphic position, thickness:

The Algyő Formation

overlies the main turbidite bodies of the Szolnok Formation in

the deep basins or the Endrőd Marl above the sub-lacustrine

basement highs (e.g. Mihályi). The distinction between the

Szolnok and the Algyő-type turbidites is commonly

disputable; thickness of the sand bodies, sand/mud ratios, and

the seismic character may offer a key (cf. Sztanó et al. 2013b),

however that may depend on the rate of confinement among

many other factors. It is also difficult to mark the Endrőd /

Algyő boundary, although the appearance of thin sandstone

bodies near the base of the Algyő Formation may help.

The muddy Algyő Formation is overlain by the sandy Újfalu

Formation; their boundary is fairly well constrained both

lithologically and geometrically (Figs. 3 and 4). Although this

boundary is widely and incorrectly referred to as the “Lower /

Upper Pannonian boundary”, it get consistently younger

towards the S, SE and obviously has no chronostratigraphic

meaning. Thickness of the Algyő Formation is smaller near

the margins (150 – 250 m), and is larger (may attain 700 m)

above the deepest depocentres in the DKB.

Fossils, age:

Fossils of the formation represent low-diversity,

deep-water mollusc assemblages of Lake Pannon. Typical

forms include Paradacna abichi, Paradacna sp., Congeria cf.

czjzeki, Dreissenomya digitifera, Valenciennius sp., and

planorbid snails. The age of the formation within the DKB is

estimated as 10 – 9 Ma (Magyar et al. 2000, 2007).

Depositional environment:

This formation represents the

shelf-margin slope bridging the few tens of metres deep shelf

with the several hundred metre deep basins. Its progradation is

related to the high clastic sediment input arriving via fluvial

and deltaic feeder systems to Lake Pannon. Cyclic variations

of sediment input and lake level influence the rate of slope

progradation vs. aggradation (Uhrin & Sztanó 2012; Sztanó et

al. 2013b). On the upper part of the slope, sand bodies related

to shelf-edge deltas and sandy canyon-fills may occur.

Towards the base of the formation, where inclination of the

clinoforms is already low, simple turbidite lobes or sheets and

chaotic slump units are common. More complex channel-

levees to turbidite lobes might have developed a few tens of

km in front of the slope; these can still be correlated to slope

surfaces.

Representative outcrops and boreholes:

The Algyő Forma-

tion does not have a surface exposure. Representative bore-

holes include Bősárkány-I, Vinár-1, Celldömölk-1, Tét-3,

Tét-6, Gönyű-1, Mosonszolnok-1, Kolárovo well series,

Zelený Háj-1. SE of the Mihályi High thin packages of turbidite

sandstones deposited high on the slope (Fig. 3).

Újfalu Formation / Beladice Formation

Lithology, facies:

The formation is made up of cyclic repe-

tition of sands, silts, clays and huminitic to lignitic clays on

two scales. Well logs display a series of 20 –50 m thick coar-

sening upward units (Fig. 3), whereas in outcrops only 5 –10 m

thick coarsening upward and a few 1– 5 m thick fining upward

cycles can be observed. Mudstones contain shell beds, lenti-

cular to thin-bedded intercalations of fine, very fine sands,

small horizontal burrows and minor slump folds. Sandy beds

show symmetrical and asymmetrical cross-lamination, various

types of cross-bedding, vertical burrows, and clay-clast

conglo merates over numerous erosional surfaces. All types of

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cycles are topped by organic rich, bio/pedoturbated or varie-

gated silty beds. Higher up in the formation, the cycles become

thinner, lithological heterogeneity and abundance of thick

sandstones decreases and logs still reflect frequent alternations

of various grain size. The seismic facies of the formation is

characterized by moderate to high amplitude reflections with

fairly good continuity (Fig. 4).

Stratigraphic position, thickness:

The formation overlies

the undifferentiated Ivanka Formation, or, in the more detailed

Hungarian nomenclature, either the Algyő slope shales (above

deep basins) or the shallow open-lacustrine Szák Formation

(above sublacustrine basement highs). In the former case,

the coarsening up cycles and the overlying muddy-silty strata

are stacked up to a thickness of 300 – 500 m, whereas in the

latter case, they are usually not thicker than 200 m. These

thinner developments were formerly regarded in Hungary as

the Somló or Tihany Member / Formation (Jámbor 1980, 1989;

Sztanó et al. 2013a). The stratigraphic cover is everywhere the

Zagyva / Volkovce Formation. It is not easy to pick the upper

boundary as the upper delta plain and the alluvial plain might

show similarly heterogeneous lithology. Commonly their

boundary is assigned where the first large channel-fill sand

bodies appear or where the brackish fauna disappears. Change

in abundance of lignite layers is also indicative for this

transition. In the southern part of the DKB, however, between

the delta plain succession and the appearance of the large

sandy channel bodies there is a 250 – 600 m thick muddy, silty

interval with only subordinate thin sand beds (Fig. 3). Seismic

correlation indicates that far to the south no slope can be

related to this electrofacies. Therefore finally this interval is

assigned to the Zagyva instead of the upper Újfalu

Formation.

Fossils, age:

The formation is rich in fossils representing

diverse shallow-water and freshwater mollusc and ostracod

faunas. The most common mollusc species include Unio

atavus, Congeria spathulata, C. pancici, Lymnocardium

schedelianum, L. brunnense, L. conjungens, L. edlaueri,

“L.” desertum, Caladacna steindachneri, Melanopsis fossilis

in the western margin of the DKB (“Burgenland”), repre-

senting the Lymnocardium conjungens Zone. In the eastern

margin (Transdanubian Range), Unio mihanovici, Congeria

simulans turgida, C. ungulacaprae, Dreissena auricularis,

L. variocostatum, L. penslii, L. ponticum, Caladacna stein

dachneri, Euxinicardium schreteri, Melanopsis caryota, etc.

are the most characteristic species, representing the Lymno

cardium ponticum Zone (Magyar et al. 2000). The oldest

occurrence of the formation within our study area had

a Carpathian source area (possible palaeo-Nitra river) and,

accor ding to

Be/

Be dating, might be as old as 10.0 – 10.5 Ma

(Šujan et al. 2016). The bulk of the formation, however, was

deposited on the palaeo-Danube shelf (cf. Magyar et al. 2013)

between ca. 10 and 8.7 Ma (Magyar et al. 2000). On the foot-

hills of the Malé Karpaty Mts., mammal fauna from the

Pezinok clay pit indicates MN9 to lower MN10 biozones with

expected deposition in the age range 9.5 to 10.5 Ma (Kováč et

al. 2011; Joniak 2016; Šujan et al. 2016).

Depositional environments:

The Újfalu / Beladice Formation

was formed by the progradation of deltaic lobes on the shallow

shelf of Lake Pannon. This interpretation was first proposed

by Mucsi & Révész (1975) in the Algyő hydrocarbon field in

the central part of the Pannonian Basin. Later descriptions,

however, identified the formation with the delta-plain deposits

only (e.g., Juhász 1992; Juhász & Magyar 1993). The Somló

and Tihany Members were originally considered as local sand

bodies on coasts of islands rather than parts of a major deltaic

feeder system (Jámbor 1989). Return to the delta concept of

Mucsi and Révész (1975) was partly a consequence of

high-resolution seismic studies in Lake Balaton (Sacchi et al.

1999) and correlation of the high-resolution seismic profiles

with nearby outcrops (Sztanó & Magyar 2007). The major

coarsening up units comprise prodelta shales, delta front sands

and reflect the lithological variability of the delta plain.

The thickness of such cycles mirrors the water depth at the

place of deposition as 20 –50 m on the shelf. Their stacking

indicates repeated flooding of the shelf and recurring progra-

dation of deltas, an overall rise of lake level due to subsidence

and climatic factors. Minor units are mouth bars, interdistri-

butary bay fills or distributary channel fills. Some incised

valleys may also occur to a depth of 20 – 30 m, pointing to base

level drops below the resolution of industrial seismics (Sztanó

et al. 2013a).

Representative outcrops and boreholes:

The formation has

a general distribution in the entire DKB. Outcrops are located

along the present-day basin margins: from Pezinok (Baráth et

al. 1999) through the region of Lake Neusiedl / Fertő-tó as far

south as Stegersbach (Magyar et al. 2000) in the western

margin, and from Chlaba in the north to the Somló Hill in the

south along the eastern margin (Strausz 1942; Bartha 1963;

Szilaj et al. 1999; Magyar et al. 2000; Bartha et al. 2015). All

deep boreholes in the basin have penetrated the Újfalu / Beladice

Formation, from Bratislava (Fordinál 1995) to the Trans-

danubian Range (Korpás-Hódi 1983).

Zagyva Formation / Volkovce Formation

Lithology, facies:

Zagyva / Volkovce Formation is characte-

rized by 4 – 8 m thick cross-bedded sandstones, usually

comprising fining-upward units, which alternate with m- or

10-m scale silt and clay sections. Some of the sandstones are

amalgamated into 10 – 20 m thick bodies. The clay beds are

partly variegated, and may contain carbonatic nodules. Cm- to

dm-scale lignite seams occur subordinately. Lithology within

the formation is highly variable, because floodplain deposits

can locally dominate over several hundred metres of strati-

graphic thickness, whereas in other parts of the basin (e.g.,

southern Želiezovce Depression) the formation is composed

of up to 60 % sandy channel belt sediments. Locally, alluvial

fans were formed by rivers entering the basin, with an example

located in the northern Blatné Depression. This alluvial fan

consists of up to 100 m thick gravels gradually passing towards

the south to the dominantly clayey succession of a meandering

river. The electrofacies character is spatially heterogeneous,

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a consequence of uneven channel belt distribution. The stacking

of several upward fining and blocky 8 –15 m thick units

usually alternate with long sections of low amplitude serrated

trends (Fig. 3). Freshwater limestones of the Hlavina Member

appear on margins of the recently uplifted Považský Inovec

and Tribeč Mountains and interfinger smoothly through calca-

reous clays with the mainly floodplain fines dominated

Volkovce Fm. (Fordinál & Nagy 1997; Kováč et al. 2011).

From the western margin towards the central parts of the DKB

a series of stacked lignite seems occur, which were locally

called the Torony Member (Jámbor 1980).

Stratigraphic position, thickness:

The Zagyva / Volkovce

Formation overlies, and interfingers with, the Újfalu / Beladice

Formation. The transition is gradual, thus it is difficult to pick

the exact position of the boundary. The thickness of the forma-

tion may attain 1500 m in the area of the basin centre; it is

especially thick in the northern part of the DKB. In the central

and southern part of the basin deposition of the Zagyva /

Volkovce Formation continued through the Pliocene and is

overlain by Quaternary fluvial deposits. The stratigraphic

boundary is usually marked by the appearance of gravelly

beds (Janáček 1971; Kőrössy 1987; Gábris & Nádor 2007;

Kováč et al. 2011). In the “Little Hungarian Plain Volcanic

Field” (Martin et al. 2003), latest Miocene to Pliocene volca-

nic bodies of the Tapolca Basalt Formation occur locally above

or within the Zagyva / Volkovce Formation. In the northern part

of the basin, a significant stratigraphic gap was demonstrated

between the Zagyva / Volkovce Formation and the overlying

Pliocene Kolárovo Formation. The unconformity is not

exposed in outcrops, but the log response of the under- and

overlying formations is sometimes sharply different. At such

localities the rather fine-grained floodplain succession of the

Zagyva / Volkovce Fm. does not show pronounced grain-size

variations, whereas the alluvial suit of the Kolárovo Fm. often

appears as a lithologically variable unit with dominance of

channel fills. In the Kolárovo Fm. blocky to fining up channel

bodies alternate with less frequent serrated floodplain fines,

reflecting alternations of thin clay, silt and sand layers. Varie-

gated and reddish colours are typical for the Kolárovo Fm. and

probably resulted from erosion of the uppermost Volkovce

Fm., which was deposited during the more arid Messinian

times (Böhme et al. 2011).

Fossils, age:

The formation contains freshwater and terres-

trial molluscs, such as Margaritifera flabellatiformis, various

species of Unio, Planorbarius, Bythinia, Melanopsis,

Theodoxus, etc. (Halaváts, 1925). Mammal remnants repre-

senting MN11 to MN14 are relatively common (Gasparik

2001; Kováč et al. 2006, 2010; Tóth 2010; Pandolfi et al.

2016). Authigenic

Be /

Be ages obtained from the Volkovce

Fm. range from 10 Ma up to 6 Ma (Šujan et al. 2016). The

Hlavina Freshwater Limestone, important as a correlative

horizon in the Volkovce Fm., was dated using small mammals

to ca. 8.0 Ma (Kováč et al. 2010). The age of the lignite-

bearing Torony Member within the Zagyva Formation is

7.3 – 6.7 Ma. Note that this interval equals the age of the

lignite-bearing Bükkábrány Member of the Újfalu Formation,

which occurs in the NE part of the Pannonian Basin (foothills

of the Mátra, Bükk region and the Eastern Great Plain, Juhász

et al. 2007; Magyar 2010).

Depositional environments:

Alluvial plain with meandering

or anastomosing channels (cf. Uhrin & Sztanó 2007; Uhrin et

al. 2011), which discharged into the Újfalu / Beladice delta

system along the shore of Lake Pannon. The sandstones

represent channel fills, while thin beds of sand, silt and clay

were deposited on the floodplains. Variegated clays and

carbonate nodules are interpreted in terms of palaeosols,

suggesting sustained periods of subaerial exposure under

relatively arid conditions. The extended lignite seams have

been formed in floodplain ponds and marshes, and mark

a more humid period at about 7 Ma ago (Magyar 2010; cf.

Böhme et al. 2011). Connected lake-level rise influencing

deposition in the Drava Basin and the eastern part of the Great

Plain area did not reach directly the DKB. A rise of the

ground-water table, however, might have resulted in develop-

ment of an extended floodbasin. The “channel-poor” portion

of the Zagyva / Volkovce Formation might coincide with this

stage. The relatively fine grained composition of the formation

continues up to the youngest strata (ca. 6 Ma) in the northern

part of the DKB, what indicates no changes in sediment supply

and therefore no significant tectonic activity on basin margins.

Hlavina Freshwater Limestone was formed along marginal

faults of the mountains, suggesting enhanced spring activity

connected to Mesozoic karstic aquifers.

Representative outcrops and boreholes:

The formation has

a large number of outcrops, especially in the northern part of

the basin. This is a result of denudation connected with basin

inversion. Outcrops are mostly artificial sandpits, representing

channel fills, whereas floodplains are exposed less frequently.

Important outcrops include Hlohovec, Bernolákovo (Blatné

Depression), Veľké Ripňany (Rišňovce Depression),

Semerovo, Veľké Lovce and Bátorove Kosihy (Želiezovce

Depression) in the northern part of the basin. It also crops out

at the elevated Pannonhalma area and a few locations along

the SE margin of the DKB (i.e. Hosszúpereszteg; Balázs et al.

1981). Typical borehole sections include, for instance,

Abrahám-1, Diakovce-1, Kolárovo-2, Mosonmagyaróvár

K-136, Abda K-12, Bősárkány-I, Bük-1, Csapod-1, Gönyü-1,

Tét-6. The alluvial fan in the northern Blatné Depression is

penetrated by the counterflush well series Piešťany and Bučany.

Basin evolution

Structural background

The onset of Late Miocene sedimentation might have been

preceded by latest Sarmatian basin inversion, an idea long

thought to be supported by the lack or very thin development

of Sarmatian sediments in the southern part of the DKB

(Kőrössy 1987; Horváth 1995). However, there are examples

along the western (Rosta 1993) and northern basin margin

(Kováč et al. 2008) that the Sarmatian and Pannonian

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sequences are continuous. Locally Sarmatian strata reach

a thickness of up to 300 – 400 m (Adam & Dlabač 1961; Vass

et al. 1990; Kováč et al. 2011). Continuous Sarmatian to

Pannonian sequences were also observed in the southernmost

DKB and Zala Basin (Fodor et al. 2013b).

The origin of the Late Miocene subsidence and basin forma-

tion is still a matter of debate. In one view the major subsi-

dence of the basin can be attributed to a crustal-scale process

and not mainly to basin-margin faulting. This interpretation is

confirmed by the relatively uniform thickness of several

formations, and by the fact that the Late Miocene basin

evolution followed crustal faulting of the syn-rift phase of ca.

19 –11.6 Ma and largely represents a post-rift thermal cooling

episode (Royden et al. 1983; Vass et al. 1990; Lankreijer et al.

1995; Kováč & Baráth, 1996; Kováč et al. 2010, 2011;

Horváth et al. 2015; Majcin et al. 2015; Hók et al. 2016). Other

processes, like magmatic underplating could also play a role

(Konečný et al. 2002). Localized (flexural) subsidence due to

sediment loading contributed to the deepening of the central

zone of the basin as well (Lankreijer et al. 1995).

Middle Miocene basin subsidence occurred in a simple

shear regime in the upper crust (Györfi 1992; Tari et al. 1992;

Lankreijer et al. 1995; Hók et al. 2016). Re-evaluation of

biostratigraphy, palaeoecology and sedimentology of deep

borehole cores in the northern part of the DKB suggest that

accommodation was filled up in the Sarmatian in most places

(Rybár et al. 2015; Kováč et al. in review). This may imply

that the rapid deepening of several depressions (e.g., Komja-

tice and Gabčíkovo - Győr Depressions) at the beginning of the

Pannonian can represent a new rifting phase acting in a pure

shear regime — an idea that is supported also by the results of

thermal modelling (Majcin et al. 2015). In the interpretation of

Tari (1994) it was probably a “wide rift stage”, when earlier

distri buted syn-rift faulting concentrated into a few fault zones

in the northern and southern parts. An increasing number of

documented Late Miocene faults support the idea that faults

also contributed to basin subsidence, although their dis-

placement remained modest, not reaching 500 m separation.

Such faults influenced sedimentation and deposition pattern

(see below).

Fault kinematics varied from normal to transtensional

strike-slip (mostly sinistral oblique-slip) although it can

mostly be deduced from outcrop-scale fault-slip data (e.g.,

Fodor 1991; Vojtko et al. 2011; Sipos-Benkő et al. 2014;

Klučiar et al. 2016). Stress calculations would suggest E –W to

SE – NW tension although it is not clear if the different values

indicate spatial or temporal variations (see Marko et al. 1995;

Fodor et al. 1999; Hók et al. 1999; Marko 2012; Sipos-Benkő

et al. 2014, Kovács et al. 2015). The Late Miocene extensional

tectonic regime with NW–SE directed Sh

min

persisted in the

northern part of the basin up to the Middle Pleistocene.

Basin-fill history

During deposition of the earliest Late Miocene sediments

(i.e. Endrőd / Lower Ivanka Formation in the basin centres)

continued subsidence was “inherited” from the syn-rift phase

(or renewed subsidence in case of Sarmatian inversion) at

about 11.6 to 10.5 Ma ago. In the Gabčikovo-Győr Depression

a notable displacement and tilting was documented along the

Ripňany-Galanta fault system (e.g., Hrušecký 1999; Bielik et

al. 2002; Kováč et al. 2011; Synak 2013; Kronome et al.

2014). Continuing fault control at Mihályi High is probable

(see Fig. 5). The subsidence history in the northernmost area,

namely the Rišňovce Depression, is surprisingly long (Figs. 2

and 5). It seems to be continuous with deep water clays and

with the occurrence of the oldest turbidites, which, however,

might have been confined by the mid-Miocene Kráľová

volcano and the southern tip of the Tribeč block, as local

highs. In the same way the oldest deltas of the Beladice

Formation fed by northerly rivers are recorded. Synak (2013)

recognized significant activity of the Ripňany-Galanta fault

(Bielik 2002) during deposition of lowermost Pannonian strata

using seismic stratigraphy. This fault probably contri buted to

subsidence of the Rišňovce Depression. The angular uncon-

formity within Ivanka Fm. (Tajná ŠVM-1 well) pro bably

represent an early Pannonian fault activity (Kováč et al. 2008)

which resulted in diversified lake bottom morphology.

Development of the Szák and Kálla / Nemčiňany Formations

was a consequence of a lacustrine base-level rise. Flooding of

the northern – north-eastern margin about 11 Ma ago and

inundation of the western basin margin ca. 10.5 Ma ago was

probably the joint effect of a climatically induced lake-level

rise and overall subsidence. In addition, the Kálla/Nemčiňany

Formation clearly indicates the existence of a fault-related

lake margin relief, however small the fault offset might have

been. Such faults were detected near the Sopron Hills in the

west (Vendel 1973; Fodor et al. 1989; Fodor 1995), and based

on other evidence along the Gerecse Hills in the east (Fodor et

al. 2013a). In contrast to the overall deepening and trans-

gression, the locally sourced Gilbert-type deltas led to normal

regression of the shoreline within a short time (cf. Sztanó et al.

2010), while deposition of the Endrőd Formation continued in

the deep basin centres (Fig. 5).

About 10 Ma ago, or shortly before, the palaeogeography

significantly changed: the main fluvial feeder system (i.e. the

palaeo-Danube and its major distributaries) entered the DKB

from the W-NW, and the sediments accumulated partly in

large delta systems. Where water depth was less than 100 m

(i.e. areas where formerly the Szák Formation was deposited)

prograding deltas filled accommodation rapidly, while towards

the area of the deep basin centres a shallow shelf was

constructed (Magyar et al. 2007, 2013). Progradation of the

shelf-margin slope resulted in the formation of the Algyő /

Upper Ivanka Formation, and deposition of turbidite sand-

stones (Szolnok/Middle Ivanka Formation) at the toe-of-slope

and in the basin proper (Fig. 5). Meanwhile the confined

northern Rišňovce Depression was filled up as well, therefore

turbidity currents may have “escaped” to the deepest parts of

the basin to the south (Dunajská Streda area). Finally, deltas of

the north dumped their sediments into the central depression

as well approximately 9 Ma ago (Šujan et al. 2016).

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, 2016, 67, 6, 525 – 542

The shelf-slope generally prograded towards the SE

until the elevated block of the Transdanubian Range

deviated the transport to the south. The blocking and

ultimate confinement is also indicated by the thick

accumulation of turbidite sands in the Kolarovo area.

The later development of the slope and transport direc-

tion of turbidites was turned towards the local depo-

centres often controlled by minor fault activity (Uhrin

et al. 2009; Törő et al. 2012). For example, modest dis-

placement and tilting along the Mihályi High clearly

diverted slope progradation parallel to the elongated

high (Uhrin 2011; Fodor et al. 2013a). Flexural subsi-

dence due to sediment loading continuously contri-

buted to deepening in front of the prograding shelf-slope

system, thus created ample space for the accumulation

of turbidites. Eventually the same flexural subsidence

resulted in the progressive (and gradual) flooding of

the south-eastern, Transdanubian Range basin margin

ca. 9.2 Ma ago. Limited faulting locally contributed to

subsidence (e.g. western Gerecse margin). Faulting was

maintained even during delta sedimentation a few 100 ka

later; tilted and raised fault blocks locally deflected

sediment transport to N-NE, thus delta channels and

lobes got around the block of Gerecse instead of passing

straight though it (Bartha et al. 2015).

Progradation of the fluvial to delta to shelf-slope

system led to a long term normal regression (Sztanó et

al. 2013b), as the shelf edge and delta fronts gradually

shifted to the south. Regardless of the original topo-

graphic differences, basin floor morphology, structural

evolution etc. the DKB got filled up by ca. 9 Ma within

the Congeria czjzeki and L. ponticum biochrons

(Magyar 2010). Afterwards only fluvial sedimentation

occurred, most likely influenced by compactional

subsidence and potential prolonged fault activity. By

8.6 Ma the feeder system overcame the mostly flooded

Transdanubian Range and the shelf margin was located

far to the south (Magyar et al. 2013).

The Late Miocene sedimentary fill of the DKB is

similar to that in other parts of the Pannonian Basin

System. It hosts one of the thickest successions in the

basin centre with all five lacustrine formations repre-

senting deep-water marls, turbidites, slope shales,

deltas to fluvial deposits. There are also internal highs

and large marginal areas with less complete succes-

sions, reflecting later flooding or filling up of only

shallow water depth in Lake Pannon. As the basin mar-

gins got uplifted during the Pliocene to Quaternary

inversion these latter types can be studied at several

locations. The DKB was large enough to develop good

examples of different rates of turbidite confinement or

to demonstrate how basin floor morphology influenced

slope progradation. The basin-fill succession, however,

is unique in a sense that it is the first major basin along

the NW feeder system to be filled in the history of Lake

Pannon, thus all the formations, which developed

Fig.

5. Concept

ual

model of basin

fill

successions. It

reflects

the

initial

basin

floor

topography

, gradual

flooding of the mar

gins and the progradational

character

of the fluvia

l-deltaic-slope-to-turbidite

systems. Complete

series of formations are only found in the deep basin interiors. Small structurally

influenced

depressions

may

have

accommodated

slightly

dif

ferent

successions. On sublacustrine

basement highs turbidites are missing and open-water mudstones are condensed. On basin mar

gins

the oldest part of the successions including slope deposits are also missing.

538

SZTANÓ, KOVÁČ, MAGYAR, ŠUJAN, FODOR, UHRIN, RYBÁR, CSILLAG and TŐKÉS

GEOLOGICA CARPATHICA

, 2016, 67, 6, 525 – 542

everywhere else later in the Pannonian Basin are the oldest in

the DKB. Part of the fluvial feeder system is also special as

alluvial fans occur along the northern basin margin. Except for

the rapidly subsiding basin centre, overall water depth might

have been less than 100 m over vast NW areas and only a few

hundreds of metres in the southern parts, therefore slope

progradation and overall regressive filling up of the large

DKB occurred rapidly, during less than two millions year

(Magyar et al. 2013).

Conclusions

In spite of the significant local differences in the structural

background of the individual depressions and basement highs,

the overall basin fill history and thus the sedimentary succes-

sions are uniform across the Danube / Kisalföld Basin, allowing

a robust correlation of the formation from S to N or W to E.

The Hungarian lithostratigraphic system is more detailed,

closely reflecting the depositional systems, therefore it can be

easily integrated into the Slovak system which, in turn, does

not discriminate between various deep-water deposits.

The most important aspect of correlation is that all formations

are time-transgressive, which means that their boundaries

cannot be characterized with a single precise datum even

within the DKB (Fig. 2).

Late Miocene lacustrine sedimentation started where the

basin deposits are deepest today with deposition of the Endrőd

Marls, corresponding to the lower Ivanka Formation. At about

10.5 Ma ago several marginal highs were flooded, and the

shallow offshore Szák Formation and the coarse-grained

deltas of the Kálla/Nemčiňany Formations were deposited.

These small volume, locally derived clastics were soon over-

lain by the enormous fluvial input from the N-NW, indicating

the commencement of long term normal regression. Turbidite

systems (Szolnok / middle Ivanka Fm.) and shelf-margin slope

(Algyő / upper Ivanka Fm.) formed in the several hundred

metre deep basin, while deltas (Újfalu / Beladice Fm.) deve-

loped on the few tens of metre deep shelf, being fed by

diffe rent fluvial systems (Zagyva/Volkovce Formations).

The turbidite systems rapidly spread all over the deep basin

floor with different rates of confinement. Except for the

northern most, oldest occurrences there is not much age diffe-

rence within the turbidites (10.5 – 9.5 Ma). With the gradual

progradation of the shelf-margin slope towards the S and SE

between 10 and 9 Ma, each formation became increasingly

younger in the same direction. After 9 Ma only the alluvial

Zagyva / Volkovce Formation was deposited in the DKB. In the

northern part of the basin a major unconformity is recorded at

about 6 Ma, marking a significant change in the style of alluvial

deposition. In the central part of the basin (Győr-Gabčíkovo

Depression), however, deposition was uninterrupted until the

Quaternary as a consequence of continued subsidence. These

long lasting fluvial systems acted as sediment conduits and

recorded climatic and structural events until the entire

Pannonian Basin was filled up with sediments.

Although confined in space and time, the lacustrine to

fluvial sedimentary fill of the Danube / Kisalföld Basin offers

a model of depositional system development and formation

distribution for the entire Late Miocene to Pliocene Pannonian

Basin system.

Acknowledgements: The joint project (TÉT-12-SK- HU-

2013-0020) was supported by the National Research, Deve-

lopment and Innovation Office of Hungary and the Slovak

Research and Development Agency with M. Kováč and

O. Sztanó as principal investigators. The research itself is

related to APVV-14-0118, APVV-15-0575, APVV 0099-11,

APVV-0625-11 &

APVV SK-FR-2015-0017

. Structural

results were partly achieved by the support of OTKA grant

No 81530. This is MTA-MTM-ELTE Palaeo contribution

No. 232.

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