GeolCarp_Vol69_No5_467

GEOLOGICA CARPATHICA

, OCTOBER 2018, 69, 5, 467–482

doi: 10.1515/geoca-2018-0027

www.geologicacarpathica.com

Miocene fan delta conglomerates in the north-western part

of the Danube Basin: provenance, paleoenvironment,

paleotransport and depositional mechanisms

TAMÁS CSIBRI



, SAMUEL RYBÁR

, KATARÍNA ŠARINOVÁ

, MICHAL JAMRICH

ĽUBOMÍR SLIVA

and MICHAL KOVÁČ

Department of Geology and Paleontology, Faculty of Natural Sciences, Comenius University in Bratislava, Mlynská dolina, Ilkovičova 6,

842 15 Bratislava, Slovakia;



tamas.csibri@gmail.com

Department of Mineralogy and Petrology, Faculty of Natural Sciences, Comenius University in Bratislava, Mlynská dolina, Ilkovičova 6,

842 15 Bratislava, Slovakia

NAFTA a.s., Plavecký Štvrtok 900, 900 68 Plavecký Štvrtok, Slovakia

(Manuscript received February 19, 2018; accepted in revised form August 8, 2018)

Abstract: The Blatné Depression located in the NW part of the Danube Basin represents the northernmost sub-basins of

the Pannonian Basin System. Its subsidence is associated with oblique collision of the Central Western Carpathians with

the European platform, followed by the back-arc basin rifting stage in the Pannonian domain. The conglomerates

recognized in the Cífer-2 well document the latest Burdigalian–early Langhian deposition in fan delta lobes situated

above the footwall and hanging wall of a WSW–ENE trending fault system, the activity of which preceded the opening

of the late Langhian–Serravallian accommodation space with a NE–SW direction. The provenance area of the “Cífer

conglomerate” was linked to the Tatric Super-unit complexes. Similar rocks crop out in the southern part of the Malé

Karpaty Mts. and are also present in the pre-Cenozoic basement of the Danube Basin. Documented extensive erosion

of the crystalline basement and its sedimentary cover lasted until the early/middle Miocene boundary. The “Cífer

conglomerate” has distinct clast composition. The basal part consists of poorly sorted conglomerate with sub-angular

clasts of metamorphic rocks. Toward the overlying strata, the clasts consist of poorly sorted conglomerates with

sub-rounded to well-rounded carbonates and granitoids. The uppermost part consists of poorly sorted conglomerates with

sub-rounded to rounded clasts of carbonate, granitoid and metamorphic rock. Within the studied samples a transition from

clast to matrix supported conglomerates was observed.

Keywords: Danube Basin, Blatné Depression, lower/middle Miocene, fan delta, conglomerates, sedimentary petrology.

Introduction

The Danube Basin, located at the junction of the Eastern Alps,

Western Carpathians and Transdanubian Range, represents

the NW part of the Pannonian Basin System. The investigated

Cífer-2 well (48°19’52.68” N, 17°28’45.44” E) is situated

in the central part of the Blatné Depression (NW Danube

Basin). It is bordered by the Malé Karpaty Mts. in NW and

by the Považský Inovec Mts. in the NE and passes into

the Gabčíkovo–Győr Depression in the south (Fig. 1).

The basin fill consists of marine to freshwater deposits

reaching up to 3000 m (Adam & Dlabač 1969; Kilényi &

Šefara 1989; Rybár et al. 2016). The early Miocene marine

sediments are situated mostly in the north. The main part of

the basin fill is represented by the middle Miocene deposits of

the Central Paratethys Sea, which are overlain by sequences of

the late Miocene Lake Pannon, and the late Miocene to

Pliocene alluvial to fluvial sediments (e.g., Kováč et al. 2011;

Sztanó et al. 2016). The prevailingly fine grained sedimentary

fill is intercalated with sandy to gravely facies, often at

the base of Transgression–Regression (T–R) cycles (e.g.,

Kováč 2000).

The Cífer-2 well (Fig. 2) was drilled to confirm natural gas

capacity at the Trnava–Sereď basement elevation located

northeast of Cífer village. The pre-Cenozoic basement rocks

are formed by crystalline complexes of the Tatric Super-unit

(Fusán et al. 1987). The original description of the well was

done by Pagáč (1959), and the data were later summarized by

Biela (1978). The deepest part of the well yielded conglome-

rates originally included in the Paleogene (1885–2031 m).

These coarse-grained strata are covered by more conglomerate

layers originally ranked to the Karpatian/lower Badenian

(upper Burdigalian/Langhian) time span (1553–1885 m; Biela

1978). The conglomerates are overlapped by offshore mud-

stones and sandstones of the upper Badenian (lower

Serravallian) Báhoň Fm. (Vass 2002). The sequence ends with

the Pannonian lacustrine to alluvial sediments of the Ivanka,

Beladice and Volkovce fms. (Šujan et al. 2017).

The aim of this work is to revise the conglomerates from

the Cífer-2 well in respect to their age, petrography and

provenance. The definition of transport mechanisms and

the character of depositional paleoenvironment will be derived

from facies analysis, well-logs study, and seismic facies inter-

pretation. The acquired knowledge should contribute to

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confirmations of the geodynamic development model of the

area at the Eastern Alpine–Western Carpathian junction during

the rifting phase of the Danube Basin (Kováč et al. 2018a).

It should also contribute to paleogeographic models before

and during the maximal flooding of the Central Paratethys Sea

in the back-arc basin system (e.g., Kováč et al. 2017b; Sant et

al. 2017).

Material and methods

Well core samples were obtained from the repository of

Nafta a.s. — Oil and Gas Company (Gbely). From six well

cores twelve samples were taken (spot sampling). For the pur-

poses of provenance and facies analysis the cores were cut

in half and scanned. Individual clasts from the sampled con-

glomerates were divided into 4 grain size fractions (0.2 to 0.8

cm, from 0.8 to 1.5 cm, 1.5 to 3 cm and >3 cm) and 1 was used

for the matrix composition (0–0.2 cm). The clasts were

measured on the polished side of the well core. It needs to be

noted, that the measurements reflect the original clast size

only partially. The clast composition was confirmed by seven-

teen thin sections studied under a polarizing microscope.

Abbreviations of minerals follow Whitney & Evans (2010).

Grain size classification of clasts follows Wentworth (1922)

and the shape classification of clasts follows Powers (1953).

The sedimentary structures of the individual well cores were

evaluated in the sense of Boggs (2006) and Nichols (2009).

The conglomerates classification follows the work of Pettijohn

(1975). Carbonate classification follows the work of Flügel

(2010).

Two reflection seismic lines were used for the purposes of

seismic facies analysis: the NNE–SSW oriented 554/77 line

and the line 558/77 with a NW–SE orientation (Fig. 1). Inter-

pretations were made in the Schlumberger Petrel software using

the standard methods described by Mitchum & Vail (1977),

Brown & Fisher (1980). The well log data was eva luated

based on Rider & Kennedy (2011) and Emery & Myers (1996).

Fig. 2. Lithostratigraphic chart of the study area (time range of NN Zones according to Hohenegger et al. 2014).

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Petrography of the conglomerates of the Cífer-2 well

The conglomerate in the core 26 (1999–2005 m; Fig. 3)

represents the basal part of the sedimentary succession.

The clast supported conglomerate is poorly sorted with chaotic

orientation of clasts. This core sample consists only of meta-

morphic ?cobbles (Qz-mica schists and biotitic paragneisses;

Fig. 3). The clasts of biotitic paragneisses are sub-angular and

occasionally deformed; the Qz-mica schists are sub-rounded

to rounded. In the polarizing microscope chloritic-sericitic and

graphitic schists were observed. Segregated clasts of quartz

and lydites can also be found. The mineral composition of

the paragneisses involves: Qz, Pl, Kfs, Bt (commonly chlori-

tized) and Ms (Fig. 4; with heteroblastic texture). Accessory

minerals are represented only by Zrn and Grt. The paragneiss

clasts, together with the surrounding matrix are cut and offset

by calcite veins (Fig. 4 a, b). The clayey-sand matrix is built up

by crushed monocrystalline Qz, clasts of metamorphic rocks

(medium sand fraction), clay minerals and mica (Fig. 3).

The clast composition of core 25 (1947–1959 m) is more

variegated (Fig. 5), but the texture is still clast supported.

The matrix is micritic (microsparite), and occasionally clayey–

carbonatic. The clasts of metamorphic rocks are represented

by paragneisses. Heavily weathered granitoids are also present

and are built up by Qz, altered Fs and mica. The majority of

clasts represent micritic carbonate rock fragments represented

by three types: (i) pale carbonates, (ii) dark carbonates cut by

calcite veins (Fig. 6) and (iii) laminated carbonates. Red quartz

arenites and clastic quartz were also distinguished. The round-

ness of carbonate and paragneiss clasts is generally sub-

rounded. The dark carbonates are well rounded (fraction

0.2–0.8 cm). The grain size of granitoids and red quartz

are nites varies from medium sand to granule; carbonate rocks

vary in size from medium sand to pebble/cobble; clastic quartz

vary in size from coarse sand to very coarse sand (Fig. 5).

Core 24 (1900–1905 m), was not available in the repository

but abundant carbonate clasts and rare Qz-mica schists were

described (Pagáč 1959).

The conglomerates from core 23 (1857–1882 m; Fig. 7) are

poorly sorted. They consist of pale and dark carbonate rocks,

biotitic paragneisses and chloritic-sericitic schists. Carbonates

and paragneisses are rounded to well rounded. The amount of

granitoids increases, comparing to the red quartz arenites.

The granitoid clasts are sub-rounded and formed by Qz, serici-

tized Fs and weathered mica. The size of all rock types varies

from fine sand to pebble. The texture is clast supported and

the matrix is carbonatic.

The conglomerate in core 22 (1794–1799 m; Fig. 8) has

similar grain size and roundness of clasts as in core 23, but

macroscopically only two clast types were observed: altered

granitoids to granitoids and metasandstones. The proportion

of granitoids to altered granitoids is 3:1. Carbonates were

observed only in the thin sections (Fig. 9). One packstone clast

contains thin-valued bivalves and uniserial foraminifers, other

clasts are micritic. Compared to all other conglomerates,

the main difference is that the conglomerate from core 22 is

matrix supported (clayey-carbonatic) and red in colour. In small

parts of both samples indistinct normal gradation is observed.

The conglomerates in core 21 (1746–1752 m; Figs. 10, 11)

are characterized by variegated clast composition. The texture

is matrix supported. The binding material is sparitic, and indis-

tinct normal gradation is observed. Clasts of metamorphic

rocks are still present and are accompanied by clasts of grani-

toides, red quartz arenites to minor carbonates. The clasts of

biotitic paragneisses are predominantly cut by calcite veins.

However, in contrast to the conglomerates from core 26,

the calcite veins are located only inside the clast. One piece of

a red chert was found. The carbonate rocks are represented by

(i) dark and (ii) laminated carbonates which are micritic or

recrystallized. The grain size of biotitic paragneisses, grani-

toids and carbonates clasts varies from medium sand to

pebble. Qz-mica schist clasts vary from medium sand to

granule, and red quartz arenites vary from medium sand to

coarse sand.

Interpretation of provenance, paleoenvironment,

paleotransport and depositional mechanism

The deepest part of the Cífer-2 well (Fig. 12) was previously

assumed to be of Paleogene to Karpatian age (Pagáč 1959;

Biela 1978; Fig. 13). However, this ranking was not suffi-

ciently constrained. The new data from the Trakovice-1 and

Špačince-5 wells (Rybár et al. 2016) allowed the creation of

biostratigraphicaly defined horizons, which were then corre-

lated throughout the selected seismic lines. This enabled

ran king of the studied “Cífer conglomerate” (2031–1565 m) to

the latest Burdigalian to early-middle Langhian (Karpatian/

lower Badenian) time span. This can be interpreted from

the available seismic lines 554/77 and 558/77 (Figs. 1, 13).

The early Serravallian (late Badenian) age of the overlying

mudstones (1565–1000 m) is based on the correlation with

Cífer-1 well (2 km to the south; Fig. 1). Correlations were

made by using SP and RT logs and the age data are derived

from the presence of calcareous nannofossil zone NN6

(Ozdínová 2008).

Provenance

The provenance of all processed conglomerates points to

the Central Western Carpathian source. The source of grani-

toids can be associated with biotitic granodiorites exposed in

the Modra Massif of the Malé Karpaty Mts. The described

clasts of metamorphic rocks (chloritic-sericitic schists, graphitic

schists and biotitic paragneisses) are exposed in the upper part

of the crystalline complexes of the Pezinok Group in the Malé

Karpaty Mts. The protolith of chloritic-sericitic schists was

a psammitic rock together with some rare pelitic sediment

(Cambel & Čorná 1974). The closest occurrence is situated

around the Mešťanková elevation (Modra–Harmónia area;

Polák et al. 2012). Minor occurrences of such rocks are also

found in the south-eastern part of the Tribeč Mts. (e.g., Badice;

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Kamenec — 293 m.a.s.l.). The source of quartz arenites may

be in the Lúžna Fm. (Lower Triassic) which represents a sedi-

mentary cover of the Tatric Super-unit. Similarly, dark car -

bona tes with calcite veins without fossils may belong to

the Guten stein Fm. (Middle Triassic) of the Tatric Super-unit

sedimentary cover. Nonetheless sourcing from the Fatric and

the Hronic nappe units cannot be excluded. The pale, sandy

limestones which microscopically occur in core 22 may

belong to the Paleogene sediments.

Based on the clast composition the studied conglomerates

were divided into 3 groups (Table 1). The clasts of the 1

group

(core 26, 2005–1999 m) consists only of Bt-paragneiss and

Qz-mica schists which point to a different source area, then in

the overlying 2

and 3

group. They may be derived from

the southernmost part of the pre-Cenozoic basement of the

Blatné Depression, which is built up of crystalline rocks, over-

lapped by sediments of Serravallian age (late Badenian/

Sarmatian; see Biela 1978; Fusán et al. 1987).

Beside crystalline rocks, the 2

and 3

groups contain clasts

from the sedimentary cover or nappe units. The main diffe-

rence between these groups is the degree of weathering of

granitoid clasts and content of carbonate clasts. Group 2

(core 25, 1959–1947 m and core 23, 1882–1857 m) consist of

heavily weathered granitoids (17–47 %; Figs. 5, 7) and a large

proportion of carbonates (70–45 %; Figs. 5, 7). Group 3

(core 22, 1799–1794 m and core 21, 1752–1746 m) comprises

non-weathered granitoids (9–43 %; Figs. 8, 10) and a low pro-

portion of carbonates (2–8 %; Figs. 8, 10). Increase of grani-

toid clasts and decrease of their degree of weathering points to

gradual erosion of the source area. The provenance can be

linked to an area, which was similar in geological structure to

the Malé Karpaty Mts. southern part. It needs to be noted, that

in the time of denudation the eroded area was much larger and

extended further to the east up to the Kráľová stratovolcano

(Hrušecký 1999).

Transport mechanism and depositional environment

Interpretation of the transport mechanism and depositional

environment can be drawn from the 2D seismic profile 554/77

and from the SP (Spontaneous potential) and RT (Resistivity)

logs (Figs. 12, 13). The seismic facies of the “Cífer conglo-

merate” are arranged in sigmoid prograding clinoforms which

dip toward the N, NE (Fig. 13) and can be interpreted as a fan

delta body.

The reflexes are discontinuous with high amplitudes which

indicates coarse-grained deposits. The negative excursions on

the SP log and the high resistivities recorded by the RT log

also indicate coarse grained character what is additionally

confirmed by the physical well core samples. Moreover,

the high excursions point to saturation by fluids and/or gas

(cylindrical and symmetrical trends).

The conglomerate in the deepest core, interpreted as

the 1

group, contains clasts which are broken together

with their surrounding matrix. Therefore, crushing during

drilling can be excluded. The offsets (Fig. 4) indicate that

the conglomerate must have been lithified before further tec-

tonic events. So, we can deduce that group 1 was derived from

the Danube Basin crystalline basement. Based on these facts,

together with the different clast composition documented by

the 2

and 3

groups, the 1

group is interpreted as a boulder

of an older conglomerate which was incorporated into

the latest Burdi

galian–early-middle Langhian (Karpatian/

lower Bade nian) “Cífer conglomerate”. This situation can be

seen in recent deposits in the Gulf of Suez (Bosworth &

McClay 2001), where uplifted rift flanks are being eroded and

produce large boulders similar to those in the group 1 (this

study). These are transported to a recently active alluvial fan

(Fig. 14).

The conglomerates in the 2

and 3

groups are poorly

sorted with rounded to sub-rounded clasts. Moreover, indis-

tinct normal gradation is observed in all samples which indi-

cates gravity transport (Fig. 8). The conglomerates of

the 3

group are clinostratified and have higher proportions

of matrix, in some places they are even matrix supported.

Altogether, the 2

group can be interpreted as a proximal

facies of a fan delta and the 3

group as a facies of a distal fan

delta, which is supported by higher portion of carbonate matrix

(sub-aqueous deposition). The fan delta character of both

aforementioned groups can be backed up by the sigmoid

clino form visible on the seismic line 554/77 (Fig. 13).

Tectonic context

The sedimentation of the coarse clastic facies is generally

influenced by tectonic activity (Vail et al. 1977). From

the paleo geographical point of view, the accommodation space

of the “Cífer conglomerate” was connected with the early

Miocene WSW–ENE oriented fault system, active until

the earliest-middle Miocene (Marko et al. 1991; Fodor 1995;

Marko & Kováč 1996; Hrušecký 1999; Hók et al. 2016; Kováč

et al. 2018b). This process in a transtensional/extensional

tectonic regime, associated with the lateral extrusion of

the ALCAPA lithosphere eastward (Ratschbacher et al. 1991),

which led to the opening of new depocenters situated between

the Eastern Alps and Western Carpathians (e.g., lower Miocene

terrestrial to marine deposits of the Styrian, Eisenstadt and

Danube Basin; Kováč et al. 2003, 2017a). It was partly coeval

to the basin opening of Dinaride Lake System in the south-

west (Mandić et al. 2012).

The Danube Basin pre-Cenozoic basement is built up in its

central part by crystalline complexes of the Tatric Super-unit

(Fusán et al. 1987). Gradual Oligocene–early Miocene uplift

of these complexes is documented in the Malé Karpaty Mts.

by AFT (Apatite Fission Track) cooling ages ~52 to 20 Ma

(Králiková et al. 2016). The initial rifting at the western border

of the Pannonian domain led to development of horsts and

grabens within the pre-Cenozoic basement (Hók et al. 2016;

Kováč et al. 2018b). This may have led to erosion and deposi-

tion of coarse clastics on the southern margin of the middle

Miocene Blatné Depression in the form of the “Cífer

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conglomerate” during the synrift phase of the Danube Basin

(Kováč et al. 1999, 2011; Rybár et al. 2016)

The “Cífer conglomerate” clasts composition shows erosion

of the basin’s pre-Cenozoic horsts during the latest

Burdigalian–early Langhian (Karpatian–earliest Badenian)

time. The transport direction can be deduced from dip of

the clinoforms, which seems to be prograding from S-SW to

N-NE (Fig. 13). This is in accordance with the above pre-

sented results of the provenance analyses. Latter, in the mid-

dle-late Langhian, the accommodation space was enlarged

(Kováč et al. 1999). The opening of the Blatné Depression in

its present form was a result of the oblique collision of

the Central Western Carpathians, with a spur of the Bohemian

Massif, representing the margin of the European platform

(e.g., Hók et al. 2016; Kováč et al. 2017a, b).

The stratigraphical assignment of the “Cífer

conglomerate” and correlations with

related conglomerates

The “Cífer conglomerate” (Table 1) is deposited directly on

the pre-Cenozoic basement of the Tatric Super-unit crystalline

complexes (Trnava–Sereď basement elevation, Fusán et al.

1987). This is indirectly indicated by the Trnava-1 well (7 km

to the E) which drilled the pre-Cenozoic basement to the depth

of 959.6 m (Biela 1978), as well as by the low amplitude,

discontinuous seismic facies which occur below the Cífer-2

well which can be interpreted as basement rocks (Fig. 13).

The lateral extension of the “Cífer conglomerate” may be much

larger, since synchronous conglomerates are recorded around

the Trnava–Sereď basement elevation. However, they were

Fig. 12. Lithostratigraphy of the Cífer-2 well showing interpretation of Biela (1978) and our reinterpretation.

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not studied in detail (e.g., Sereď-2, 5; Vištuk-1 wells, Biela

1978).

The Langhian age of the conglomerate upper boundary can

be deduced from the presence of the early Serravallian NN6

nanoplankton zone (sensu Martini 1971) in the fine-grained

deposits in overlying strata (Appendix 1), confirmed by

Ozdínová (2008) in the neighboring Cífer 1 well respectively.

Moreover, the southernmost part of the pre-Cenozoic base-

ment of the Blatné Depression is built up from crystalline

rocks, which are overlapped by Miocene sediments of Serra-

valian age (Late Badenian/Sarmatian; see Biela 1978; Fusán et

al. 1987). In addition, the core samples from depth interval

1405–1680 m contain calcareous nannofossils of the NN5

Zone. Further constraints come from volcanic sandstones in

core 20, bearing nannoplankton of NN5 Zone (Appendix 1

and Fig. 12), which are similar to tuffites from the Trakovice-4

well, also assigned to the NN5 Zone (Rybár et al. 2016).

Core 23 (1857–1862 m) yielded nanoplankton of the NN4

Zone, which document the age of deposition or it was redepo-

sited from older sediments (Appendix 1).

As noted in the introduction, the Blatné Depression sedi-

mentary fill contains several conglomerate bodies, generally

at the base of T–R cycles (e.g., Kováč 2000). The oldest,

Burdigalian (Eggenburgian) Dobrá Voda conglomerates

belong to the Lužice Fm. (Vass 2002) and onlap onto

the pre- Cenozoic basement in the northern part of the Malé

Karpaty Mts. In comparison to studied samples, they consist

of mono mict carbonate pebbles and cobbles (Buday et al.

1963).

The younger, pebbly mudstone of middle Burdigalian age

represents the Ottnangian Planinka Fm. (Kováč et al. 1992;

Fordinál et al. 2012) which has a polymict character, similar

to the early-middle Langhian (Karpatian–earliest Badenian)

Jablonica conglomerate.

The Jablonica conglomerate assigned to the early-middle

Langhian is mainly found on the northern slopes of the Malé

Karpaty Mts. and in the vicinity of the Dobrá Voda depression

(Vass 2002; Maglay et al. 2011). The conglomerate is matrix

supported with calcareous–sandy matrix and the depositional

environment is linked to the littoral zone or to a deltaic envi-

ronment (Kováč 1985; Kováč et al. 1989). The conglomerates

are composed of staurolite–garnet schists, Devonian meta-

morphic limestones, Wetterstein and Reifling limestones

(Mišík 1986). Based on their stratigraphic position the “Cífer

conglomerate” may be synchronous or a bit older (latest

Burdigalian to early-middle Langhian) than the Jablonica

conglomerate. Nevertheless, the Jablonica conglomerate from

the Cerová–Lieskové locality yields a much lower portion of

crystalline schists and granitoids than were documented in

the “Cífer conglomerate” (Table 2). However, the clast com-

position in conglomerates is generally of local provenance.

So, conglomerates may be very different in composition, but

still synchronous.

Devínska Nová Ves Fm. occurs on the western slopes of

the Malé Karpaty Mts. and is ranked to the Langhian (lower

Badenian; Vass et al. 1988; Fordinál et al. 2010, 2012).

The sediments were deposited in the terrestrial environment of

an alluvial fan. The clasts are represented by siliciclastics,

carbonates, and crystalline rocks which can be derived from

the Malé Karpaty Mts.; and their vertical distribution (MKZ-1

well) shows gradual erosion of the provenance area. The base

of the MKZ-1 well is mainly formed by clasts of metamorphic

rocks with rare carbonates, and granitoids, but the highest part

of the well is formed exclusively by granitoid rocks (Fordinál

et al. 2012). The terminal part of the coarse-grained formation

shows reworking by waves in the littoral zone, beyond

the frontal part of the alluvial fans. Toward the Vienna Basin,

the formation intercalates with the middle-late Langhian

(lower Badenian) Jakubov Fm. (Vass 2002; Zlinská 2015) that

contains calca reous nano plankton of the NN5 Zone. Like

the “Cífer conglomerate”, the Devínska Nová Ves Fm. is

covered by mudstones contai ning the NN6 nanoplankton zone

(sensu Martini 1971).

The younger Doľany conglomerate Mb. (Vass 2002), occurs

on the eastern slopes of the Malé Karpaty Mts. It is coarse-

grained, has poorly rounded clasts and calcareous–sandy

matrix; some breccias are present as well. The clasts are com-

posed of metamorphic and carbonate rocks. Most importantly

the Doľany Mb. was deposited around the lower/upper

Badenian boundary (Buday 1957; Cicha 1957) between

the Špačince and Báhoň fms. (Vass 2002). According to

Ogg et al. (2016) this time interval corresponds to the late

Langhian–early Serravallian. This time span can be characte-

rized by the accelerated uplift of the NE–SW orientated horst

structure of the Malé Karpaty Mts. and synrift subsidence of

the Blatné Depression (Kováč et al. 2018b).

The comparison of the Doľany and Devínska Nová Ves

conglomerates (position and petrographic composition of

clasts) may point to their origin at the edges of the uplifting

Malé Karpaty Mts. The provenance of the Planinka, “Cífer”

and Jablonica conglomerates can be additionally identified as

a source situated south of the Blatné Depression.

Well Cífer-2

Nomenclature

Core

Texture

Composition

Source

Structure

Matrix

Paleo-environment

Group

Para-conglomerate

Polymict

Extraformational

matrix supported

sparitic

distal part of fan delta

Ortho-conglomerate

Polymict

Extraformational

matrix to clast supported

clayey-micritic

distal part of fan delta

Ortho-conglomerate

Polymict

Extraformational

clast supported

micritic

proximal part of fan delta

Ortho-conglomerate

Polymict

Extraformational

clast supported

microsparit/clay

proximal part of fan delta

Ortho-conglomerate

Polymict

Extraformational

clast supported

clayey-sandy

alluvial fan

Table 1: Sampled cores with interpreted paleoenvironment and nomenclature.

480

CSIBRI, RYBÁR, ŠARINOVÁ, JAMRICH, SLIVA and KOVÁČ

GEOLOGICA CARPATHICA

, 2018, 69, 5, 467–482

• The stratigraphic assignment of the “Cífer conglomerate” is

based on the seismo–stratigraphic correlation (line 554/77,

558/77) and nannofossil zonation in the Cífer-2 well with

additionally support from the Trakovice-1, Špačince-5 and

Cífer-1 wells. The conglomerate upper boundary was set

within the NN5 nannoplankton zone. Considering the pro-

ve nance, transport direction and petrological composition

of clasts the conglomerates are considered to be synchro-

nous or a bit older than the Jablonica Fm. However, the esti-

mated latest Burdigalian to lower-middle Langhian age,

inside of the uppermost part of the NN4 and NN5 nanno-

plankton zone (sensu Martini 1971) was not sufficiently

proved.

• The provenance area of the “Cífer conglomerate” was

linked to similar rock complexes to those outcropping in

the southern part of the Malé Karpaty Mts. and vicinity

(Tatric Super-unit — crystalline basement plus sedimentary

cover or nappe units).

• The latest Burdigalian to lower-middle Langhian conglo-

merates represent deposition in fan delta lobes situated

above the footwall and hanging wall of WSW–ENE tren-

ding fault system. The fault system activity preceded opening

of the middle-late Langhian to Serravallian Blatné Depression

with a NE–SW direction. Basin subsidence is associated

with oblique collision of the Central Western Carpathians

with the European platform and the back-arc basin synrift

stage in the Pannonian domain.

Acknowledgements: Our appreciation go to Nafta a.s. — Oil

and Gas Company management for allowing access to their

well core repositories. This work was supported by APVV

agency under the contract No. APVV-16-0121, APVV-15-

0575, APVV-14-0118 and by UK Grant 9/2018. Special thank

go to Š. Pramuková and M. Hronkovič for processing of

the well core material and for thin section assembly.

We express gratitude to our editor and reviewers for insightful

comments which significantly improved the manuscript.

References

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

zur lithofaziellen Entwicklung der Donau–Niederung. Západné

Karpaty, 11, 156–171.

Biela A. 1978: Deep structural boreholes in covered areas of the Inner

Western Carpathians, 1

part-Danube Lowland. Geologický

Ústav Dionýza Štúra, Bratislava, 1–224 (in Slovak with English

summary).

Boggs S. 2006: Principles of sedimentology and stratigraphy. Upper

Saddle River, New Jersey, 1–655.

Bosworth W. & McClay K. 2001: Structural and stratigraphic evolu-

tion of the Gulf of Suez rift, Egypt: a synthesis. In: Ziegler P.A.,

Cavazza W., Robertson A.H.F. & Crasquin-Soleau S. (Eds.):

Peri-Tethys Memoir 6: Peri-Tethyan Rift/Wrench Basins and

Passive Margins. Mémoires du Muséum national d’histoire

naturelle, 186, 567–606.

Brown L.F. Jr. & Fisher W.L. 1980: Seismic-Stratigraphic Interpreta-

tion of Depositional Systems and its Role in Petroleum Explora-

tion (Part 1). AAPG Continuing Education Course Note, 16,

Tulsa, 1–65.

Buday T. 1957: Report on the Neogene outline research for the

General map of Czechoslovakia. Sheets: Žilina, Bratislava,

Česká Třebová. Open file report – archive D. Štúr Inst. geol.

Bratislava, 1–106. (in Czech).

10%

20%

30%

40%

50%

60%

70%

80%

90%

100%

Crystalline slates

Granitoids

Clastic quartz

Silicities

Quartz arenite

Cr, Pg clasts

Carbonates

Crystalline

slates

Granitoids

Clastic

quartz

Silicities

Quartz

arenite

Cr, Pg clasts Carbonates

Cífer-2 conglomerate

51.40%

21.90%

0.30%

0.10%

3.60%

22.70%

Jablonica conglomerate (loc.: Cerová-Lieskové)

75%

Table 2: Comparison of overall clast composition in the Cífer-2 conglomerates and in the Jablonica conglomerate from the Cerová-Lieskové

section.

481

MIOCENE FAN DELTA CONGLOMERATES IN THE NORTH-WESTERN PART OF THE DANUBE BASIN

GEOLOGICA CARPATHICA

, 2018, 69, 5, 467–482

Buday T., Benešová E., Březina J., Cicha I., Čtyroký P., Dornič J.,

Dvořák J., Eliáš M., Hanzlíková E., Jendrejáková O., Kačura G.,

Kamenický J., Kheil J., Köhler E., Kullmanová A., Maheľ M.,

Matějka A., Paulí, J., Salaj J., Scheibner E., Scheibnerová V.,

Stehlík O., Urbánek L., Vavřínová M. & Zelman J. 1963:

Ex planatory notes to geological map of Czechoslovakia in scale

1:200,000, sheet Gottwaldov. Ústř. úst. geol. Praha, 1–238 (in

Czech).

Cambel B. & Čorná O. 1974: Stratigraphy of the crystalline basement

of the Malé Karpaty Mts. in the light of the palynological inves-

tigation. Geol. Zbor. Geol. Carpth., Bratislava, 25, 231–234 (in

Russian with English abstract).

Cicha I. 1957: Microbiostratigraphic research of Neogene sediments

in western and easter part of the Malé Karpaty Mts. In: Buday T.:

Report on the Neogene outline research for the General map of

Czechoslovakia. Sheets: Žilina, Bratislava, Česká Třebová. Open

file report — archive D. Štúr, Inst. geol. Bratislava, 1–106 (in Czech).

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

Oxford, 1–297.

Fodor L. 1995: From transpression to transtension: Oligocene –

Miocene structural evolution of the Vienna basin and the East

Alpine–Western Carpathian junction. Tectonophysics 242,

151–182.

Flügel E. 2010: Microfacies of Carbonate Rocks: Analysis, Interpre-

tation and Application. Springer, Berlin, 1–929.

Fordinál K., Baráth I., Šimon L., Kohút M., Nagy A. & Kučerová J.

2010: New data on the Devínska Nová Ves Formation (Vienna

Basin, Slovakia). 16

Conference on Upper Tertiary Brno. Geol.

Výzk. Mor. Slez., Brno, 32–34.

Fordinál K., Maglay J., Elečko M., Nagy A., Moravcová M., Vlačiky

M., Kohút M., Németh Z., Bezák V., Polák M., Plašienka D.,

Olšavský M., Buček S., Havrila M., Hók J., Pešková I., Kucharič

Ľ., Kubeš P., Malík P., Baláž P., Liščák P., Madarás J., Šefčík P.,

Baráth I., Boorová D., Uher P., Zlinská A. & Žecová K. 2012:

Explanatory notes to the Geological map of Záhorská nížina

at a scale 1:50,000. Štátny Geologický Ústav Dionýza Štúra,

Bratislava, 1–232.

Fusán O., Biely A., Ibrmajer J., Plančár J. & Rozložník L. 1987: Base-

ment of the Tertiary of the Inner West Carpathians. Štátny geo

logický ústav Dionýza Štúra, Bratislava, 1–123.

Geological map of Slovakia at scale 1:50,000 [online]. Štátny geolo

gický ústav Dionýza Štúra, Bratislava, 2013. http://mapserver.

geology.sk/gm50js.

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

Miocene Badenian Stage of the Central Paratethys. Geol. Carpath.

65, 1, 55–66.

Hók J., Kováč M., Pelech O., Pešková I., Vojtko R. & Králiková S.

2016: The Alpine tectonic evolution of the Danube Basin and its

northern periphery (southwestern Slovakia). Geol. Carpath. 67,

5, 495 – 505.

Horváth F. Musitz B., Balázs A., Végh A., Uhrin A., Nádor A.,

Koroknai B., Pap N., Tóth T. & Wórum G. 2015: Evolution of

the Pannonian basin and its geothermal resources. Geothermics

53, 328–352.

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

physical and geological model in regard to hydrocarbon prospec-

tion. EGRSE, Spec. Issue, 6, 1, 2–55.

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.

Kováč M. 1985: Origin of Jablonica formation conglomerates in the

light of pebble analysis. Geol. Zbor., Geol. Carpath. 36, 1, 95–105.

Kováč M. 2000: Geodynamic, paleogeographic and structural evolu-

tion of the Carpathian-Pannonian region in Miocene – A new

view on the Neogene basins of Slovakia. Veda, Bratislava, 1–204

(in Slovak) .

Kováč M., Krystek I. & Vass D. 1989: Origin, migration and dis-

apearance of the West Carpathians sedimentary basins during the

Neogene. Geologické práce, Správy 88, 45–58.

Kováč M., Šutovská K., Baráth I. & Fordinál K. 1992: Planinka

formation, sediments of Ottnang and Lower Karpathian age in

northern part of the Malé Karpaty Mts. Geologické práce,

Správy 96, 47–50 (in Slovak with English summary).

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

paleobathymetry and relative sea-level changes in the Danube

Basin and adjacent areas. Geol. Carpath. 50, 4, 325–338.

Kováč M., Grigorovič A.A., Brzobohatý R., Fodor L., Harzhauser M.,

Oszczypko N., Pavelič D., Rögl F., Saftič B., Sliva Ľ. &

Stránik Z. 2003: Karpatian Paleogeography, Tectonics and

Eustatic Changes. In: The Karpatian – a Lower Miocene Stage of

the Central Paratethys. Masaryk University, Brno, 49–72.

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

A., Baráth I., Maglay J. & Minár J. 2011: Late Miocene and

Pliocene history of the Danube Basin: inferred from develop-

ment of depositional systems and timing of sedimentary facies

changes. Geol. Carpath. 62, 6, 519–534.

Kováč M., Márton E., Oszczypko N., Vojtko R., Hók J., Králiková S.,

Plašienka D., Klučiar T., Hudáčková N. & Oszczypko-

Clowes M. 2017a: Neogene palaeogeography and basin evolu-

tion on of the Western Carpathians, Northern Pannonian domain

and adjoining areas. Global Planet. Change 155, 133–154.

Kováč M., Hudáčková N., Halásová E., Kováčová M., Holcová K.,

Oszczypko-Clowes M., Báldi K., Less Gy., Nagymarosy A.,

Ruman A., Klučiar T. & Jamrich M. 2017b: The Central Para-

tethys palaeoceanography: a water circulation model based on

microfossil proxies, climate, and changes of depositional envi-

ronment. Acta Geologica Slovaca 9, 2, 75–114.

Kováč M., Halásová E., Hudáčková N., Holcová K., Hyžný M.,

Jamrich M. & Ruman A. 2018a: Towards better correlation of

the Central Paratethys regional time scale with the standard geo-

logical time scale of the Miocene Epoch. Geol. Carpath. 69, 3,

283–300.

Kováč M., Márton E., Klučiar T. & Vojtko R. 2018b: Miocene basin

opening in relation to the north-eastward tectonic extrusion of

the ALCAPA Mega-Unit. Geol. Carpath. 69, 3, 254–263.

Králiková S., Vojtko R., Hók J., Fügenschuh B. & Kováč M. 2016:

Low-temperature constraints on the Alpine thermal evolution of

the Western Carpathian basement rock complexes. J. Struct.

Geol. 91, 144–160.

Maglay J. (Ed.), Pristaš J., Nagy A., Fordinál K., Elečko M., Havrila

M., Bušek S., Kováčik M., Hók J., Baráth I., Kubeš P., Kucharič

Ľ., Malík P., Klukanová A., Liščák P., Ondrášik M., Zuberec J.,

Baláž P., Čurlík J., Ševčík P., Kernátsová J., Vaněková H.,

Harčová E., Boorová D., Zlinská A., Žecová K., Siráňová Z.,

Tuček Ľ., Tkáčová H. & Tkáč J. 2011: Explanations to the Geo-

logical map of the Podunajská nížina — Trnavská pahorkatina at

a scale of 1:50,000. Štátny Geologický Ústav Dionýza Štúra,

Bratislava, 1–322 (in Slovak).

Mandić O., de Leeuw A., Bulić J., Kuiper K.F., Krijgsman W. &

Jurišić-Polšak Z. 2012: Paleogeographic evolution of the Southern

Pannonian Basin:

Ar/

Ar age constraints on the Miocene

continental series of Northern Croatia. Int. J. Earth Sci. 101,

1033–1046.

Marko F. & Kováč M. 1996: Reconstruction of the Miocene tectonic

evolution of the Vadovce depression based on the analysis of

structural and sedimentary record. Mineralia Slovaca 28, 81–91.

Marko F., Fodor L. & Kováč M. 1991: Miocene strike-slip faulting

and block rotation in Brezovské Karpaty Mts. (Western Car-

pathians). Mineralia Slovaca, 23, 3, 89–200.

Martini E. 1971: Standard Tertiary and Quarternary calcareous

nannoplankton zonation. In: Farinacci A. (Ed.): Proceedings of

second Planktonic Conference, Roma, Vol, 2, 739–765.

482

CSIBRI, RYBÁR, ŠARINOVÁ, JAMRICH, SLIVA and KOVÁČ

GEOLOGICA CARPATHICA

, 2018, 69, 5, 467–482

Mišík M. 1986: Petrographic-microfacial analysis of pebbles and

interpretation of sources areas of the Jablonica conglomerates

(Lower Miocene of the NW margin of the Malé Karpaty Mts.).

Geol. Zbor. Geol. Carpath. 37, 4, 405–448.

Mitchum R.M. Jr. & Vail P.R. 1977: Seismic stratigraphy and global

changes of sea-level. Part 6: Stratigraphic interpretation of

seismic reflection patterns in depositional sequences: In Payton

C.E. (Ed.): Seismic Stratigraphy — Applications to Hydro-

carbon Exploration. American Association of Petroleum Geolo

gists, Memoir 26, 135–144.

Nichols G. 2009: Sedimentology and Stratigraphy. Blackwell Science

Ltd., London, 1–335.

Ogg J.G., Ogg G. & Gradstein F.M. 2016: A concise geologic time

scale. Elsevier. New York, 1–234.

Ozdínová S. 2008: Badenian calcareous nannofossils from Seme-

rovce ŠV-8 and Cífer-1 boreholes (Danube Basin). Mineralia

Slovaca 40, 141–150.

Pagáč I. 1959: Final report of the Cífre-2 well. Open file report —

Geofond, Bratislava, 1–14 (in Slovak).

Pettijohn F.J. 1975: Sedimentary rocks. Third edition. Harper & Row,

New York, 1–628 .

Polák M., Plašienka D., Kohút M., Putiš M., Bezák V., Maglay J.,

Olšavský M., Havrila M., Buček S., Elečko M., Fordinál K.,

Nagy A., Hraško Ľ., Németh Z., Malík P., Liščák P., Madarás J.,

Slavkay M., Kubeš P., Kucharič Ľ., Boorová D., Zlínska A.,

Síráňová Z. & Žecová K. 2012: Explanations to the Geological

map of the Malé Karpaty Mts. at scale 1:50,000. MŽP SR,

Štátny geologický ústav Dionýza Štúra, Bratislava, 1–309 (in

Slovak) .

Powers M.C. 1953: A new roundness scale for sedimentary particles.

J. Sediment. Petrol. 23, 117–119.

Ratschbacher L., Merle O., Davy Ph. & Cobbold P. 1991: Lateral

extrusion in the Eastern Alps. Part 1, Boundary conditions and

experiments scaled for gravity, Tectonics 10, 245–256.

Rider M.H. & Kennedy M. 2011: The geological interpretation of

well logs. 3

Revised edition. RiderFrench Consulting Limited,

1–440.

Rybár S., Kováč M., Šarinová K., Halásová E., Hudáčková N.,

Šujan M., Kováčová M., Ruman A. & Klučiar T. 2016: Neogene

changes in palaeogeography, palaeoenvironment and the prove-

nance of sediment in the Northern Danube Basin. Bull. Geosci.

91, 2, 367–398.

Sant K., V. Palcu D., Mandic O. & Krijgsman W. 2017: Changing seas

in the Early–Middle Miocene of Central Europe: a Mediter ranean

approach to Paratethyan stratigraphy. Terra Nova. 29, 273–281.

Sztanó O., Kováč M., Magyar I., Šujan M., Fodor L., Uhrin A.,

Rybár S., Csillag G. & Tőkés L. 2016: Late Miocene sedimen-

tary record of the Danube / Kisalföld Basin: interregional corre-

lation of depositional systems, stratigraphy and structural evolu-

tion. Geol. Carpath. 67, 6, 525–542.

Šujan M., Kováč M., Hók J., Šujan M., Braucher R., Rybár S. &

de Leeuw A. 2017: Late Miocene fluvial distributary system in

the northern Danube Basin (Pannonian Basin System) deposi-

tional processes, stratigraphic architecture and controlling

factors of the Piešťany Member (Volkovce Formation). Geol.

Quarterly 61, 3, 521-548.

Vail P.E., Mitchum R.M. Jr. & Thompson S. III. 1977: Relative

changes of sea level from coastal onlap. In: Payton C.E. (Ed.):

Seismic Stratigraphy: Applications to Hydrocarbon Exploration.

American Association of Petroleum Geologists, Memoir 26,

63–82.

Vass D. 2002: Lithostratigraphy of Western Carpathians: Neogene

and Buda Paleogene. GÚDŠ, Bratislava, 1–200 (in Slovak).

Vass D., Nagy A., Kohút M. & Kraus I. 1988: Devínska Nová Ves

formation: Coarse-grained sediments on the south-eastern part

of Vienna Basin. Mineralia Slovaca 20, 109–122 (in Slovak with

English summary).

Wentworth Ch.K. 1922: A Scale of Grade and Class Terms for Clastic

Sediments. J. Geol. 30, 5, 377–392.

Whitney D.L. & Evans B.W. 2010: Abbreviations for names of

rock-forming minerals. Am. Mineral. 95, 185–187.

Zlinská A. 2015: Middle Miocene foraminifers from the sediemnts in

well HGP-3 (Stupava, Vienna Basin, Slovakia). Mineralia

Slovaca 47, 177–188 (in Slovak with English summary).

Calcareous nannofossils were studied from 5 core samples of

Cífer-2 well. Top sample core 13 is assigned to NN6 Zone (Martini

1971) based on the presence of Reticulofenestra pseudoumbilicus 6

and >7 μm, Helicosphaera wallichii and Sphenolithus abies. Core 14

contains Helicosphaera scissura, Coronocyclus nitescens and

Helicosphaera walbersdorfensis and is thus assigned to NN5 Zone.

Core 15 is poor in recovery due to tuffitic composition of the sedi-

ment. Entire sample

contains only Coccolithus pelagicus,

Reticulofenestra haqii, R. minuta and Thoracosphaera thus NN Zone

cannot be assigned. Core 20 contains Sphenolithus heteromorphus

a marker for NN5-NN4 zones but due to absence of Helicosphaera

ampliaperta (NN4–NN2) NN5 Zone can be suggested. Core 23 con-

tains Helicosphaera euphratis, Calcidiscus tropicus and

Reticulofenestra pseudoumbilicus so NN4 Zone is assigned. All stud-

ied samples contain reworking of Early Miocene (e.g., Reticulofenestra

lockeri, R. bisecta, R. stavensis) Oligocene (e.g., Isthmolithus recur

vus, Reticulo fenestra umbilicus), Eocene (e.g., Chiasmolithus gran

dis, Pontosphaera pulcheroides) and Late Cretaceous (e.g.,

Micula staurophora, Prediscosphaera cretacea, Watznaueria barne

siae) nanofossils.

Appendix 1

Calcareous nannofossils zonal markers found in the Cífer-2 well

Depth (m)

Core

Discipline

Zone / Subzone

Event

1350–1259.2

NN6

PRES Reticulofenestra pseudoumbilicus 6 and >7 μm, Helicosphaera wallichii, Sphenolithus abies

1405–1411

NN5

TOP Helicosphaera scissura, Coronocyclus nitescens, BASE Helicosphaera walbersdorfensis

1447–1451

Unassigned

Poor sample, PRES Coccolithus pelagicus, Reticulofenestra haqii, R. minuta, Thoracosphaera

1674–1680

NN5

PRES Sphenolithus heteromorphus, ABSENCE Helicosphaera ampliaperta

1857–1862

NN4

TOP Helicosphaera euphratis, BASE Calcidiscus tropicus, Reticulofenestra pseudoumbilicus