GeolCarp_Vol69_No4_382

GEOLOGICA CARPATHICA

, AUGUST 2018, 69, 4, 382–409

doi: 10.1515/geoca-2018-0023

www.geologicacarpathica.com

Integrated biostratigraphical, sedimentological and

provenance analyses with implications for

lithostratigraphic ranking: the Miocene Komjatice

depression of the Danube Basin

KATARÍNA ŠARINOVÁ



, SAMUEL RYBÁR

EVA HALÁSOVÁ

, NATÁLIA HUDÁČKOVÁ

MICHAL JAMRICH

, MARIANNA KOVÁČOVÁ

and MICHAL ŠUJAN

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

842 15 Bratislava, Slovakia;



sarinova@fns.uniba.sk

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

842 15 Bratislava, Slovakia

(Manuscript received February 12, 2018; accepted in revised form May 31, 2018)

Abstract: The Komjatice depression, situated on the Danube Basin’s northern margin, represents a sub-basin of

the Neogene epicontinental Central Paratethys Sea and Lake Pannon. The paper provides an insight into the character of

sediment provenance evolution by study of well cores (ZM-1, IV-1, MOJ-1, VR-1 wells). A modern combination of

provenance, sedimentology and biostratigraphy together with the reported redefinition of Pannonian formations resulted

in a new lithostratigraphy of the study area. Moreover, newly published volcanic rock age data were used for calibration

of biostratigraphy. The overall age span of the sedimentary fill is occupied only by late Badenian–Sarmatian (Serravallian)

to Pannonian (Tortonian–Messinian) strata: 1) the basal alluvial sediments of the newly defined Zlaté Moravce

Formation; 2) late Badenian–Sarmatian (Serravalian) marine sediments of the Vráble-Pozba Fm., connected with tectonic

opening of the depression; 3) Pannonian (Tortonian) coarse grained sediments of the Nemčiňany Fm. with an erosional

base; 4) Pannonian (Tortonian–Messinian) predominantly fine-grained, basin floor to slope Ivanka Fm., sandy deltaic

Beladice Fm. and predominantly muddy, alluvial Volkovce Fm. In the middle Miocene provenance is situated in

Paleozoic sequences and Neogene volcanic rocks occurring currently in the NE. During the late Miocene, provenance is

changed to the NNW (Tribeč Mts.), although the transport from the NE also remained.

Keywords: Neogene, Danube Basin, biostratigraphy, age calibration by volcanic rock provenance analysis, Zlaté

Moravce Fm.

Introduction

The Komjatice depression forms a NE bay of the Danube

Basin. It is bordered by the Tribeč Mts. in the N-NW and by

Pohronský Inovec and Štiavnické vrchy Mts. in the E and SE

(Fig. 1). The depression was opened by simple-shear mecha-

nism (Hók et al. 2016) along the Mojmírovce fault zone and

later influenced by thermal subsidence linked to cessation of

volcanic activity (e.g., Kováč et al. 2018). The last stage is

marked by marginal basin inversion (e.g., Šujan et al. 2016).

The Pre-Cenozoic basement is built up by crystalline com-

plexes of the Tatric and Veporic units and their cover and

nappe units (Gaža & Beinhauerová 1976; Fusán et al. 1987a, b;

Hók et al. 1999, 2016). The surrounding Pohronský Inovec and

Štiavnické vrchy Mts. are formed by Neogene volcanic rocks

(Fig. 1). Exploration wells, drilled in the 1960s and 1970s are

essential for the geological research. Lithologies of the

Neogene fill together with petrography of selected cores are

descri bed in the final drilling reports. These were summarized

by Biela (1978a) and include biostratigraphic ranking based

on the benthic foraminifera assemblages. This dataset was

used for multiple studies which focused on subsidence history,

depositional systems and tectono-sedimentary evolution of

the Komjatice depression (e.g., Gaža & Beinhauerová 1976;

Lankreijer et al. 1995; Hók et al. 1999, 2016; Kováč et al.

2006, 2010, 2011; Lénárt & Hók 2013). However, for bio-

stratigraphic correlations planktonic foraminifera and calca-

reous nannofossil assemblages are the most suitable tools.

In the studied area only the ŠVM-1 Tajná well was

processed by modern methods (Kováč et al. 2006, 2008).

Calcareous nannofossils were also analysed from

a part of the ZM-1 well (Ozdínová 2012) and IV-1 well

(Zahradníková et al. 2013). Sarmatian fish fauna was descri-

bed from ŠVM-1 Tajná and JVM-2 by Chalupová (2006).

In addition to biostratigraphic data, the first cosmogenic

Be/

Be nuclides dating from VR-1 well, was published by

Šujan et al. (2016). Recently new K/Ar and Rb/Sr age data

from volcanic rocks, which form the eastern edge of

the basin, have been published by Lexa & Pécskay (2010)

and Chernyshev et al. (2013). These enabled indirect dating

of volcanic material in the basin fill. From this point of

view, the presented study is aimed at the reevaluation of

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, 2018, 69, 4, 382–409

(2010). The heavy fraction was separated using heavy liquid

from the 0.25–0.10 mm fraction (10 g) and studied under

the binocular microscope. The specified heavy minerals were

confirmed by EDAX analysis of microprobe CAMECA SX 100

(State Geological Institute of Dionýz Štúr). Selected heavy

minerals and plagioclase were analysed by WDS analysis of

microprobe CAMECA SX 100. Garnets were calculated to

8 cations and their molecule composition was calculated after

Locock (2008). Together with the chemical composition of

garnets mineral inclusions were observed. For provenance

evaluation a modification of Suggate & Hall’s (2014) diagram

was used. Epidote / allanite were calculated to 8 cations, spinel

to 3 cations and tourmaline to 31 anions. Feldspars were

calculated to 8 anions. Bentonite was confirmed by X-ray dif-

fraction on the Department of Mineralogy and Petrology,

Comenius University in Bratislava.

Foraminifera have been obtained from 100 g of well core

material, which was diluted by hydrogen peroxide and wet

sieved (0.071 and 1 mm). The binocular stereoscopic micro-

scope (Olympus SZ75) and the biological polarizing micro-

scope were used for determination of foraminifera and

the scan ning electron microscope QUANTA FEG 250 was

used for their imaging (Institute of Electrical Engineering,

SAS). The obtained residua were split into approximately 300

specimens (if possible). Determination of foraminifers is

based on Loeblich & Tappan (1992), Cicha et al. (1998),

Łuczkowska (1974) and Holbourn et al. (2013). Due to the poor

preservation of the foraminiferal tests some stay in open

nomenclature.

Calcareous nannofossil smear slides were prepared by

the standard method of decantation. The aim was to count

300 species from each sample (if possible). For microscopic

evaluation Olympus BX 50, objective with 100× magnifi-

cation and oil immersion was applied. Camera Olympus

Infinity 2, with QuickPHOTO CAMERA 2.3 software was

used to create photo documentation. Nannofossil determina-

tion was supported by MIKROTAX webpage and papers from

fellow workers dealing with the Central Paratethys.

Standard palynological processing was used to extract

the organic matter. The samples were treated with cold HCl

(35 %) and HF (40 %) to remove carbonates and silica.

The organic matter was separated from the undissolved parti-

cles using heavy liquid ZnCl

(density 2 g/cm

). Samples were

not oxidized at any stage. The palynological slides were pre-

pared with glycerin, and alcohol as the mounting medium.

Analyses were performed under the Leica light microscope

combined with Nomarski interference contrast (NIC).

Dinocyst taxonomy is in accordance with Lentin & Williams

(1998) and biozonation according to Bakrač et al. (2012) and

Magyar et al. (1999a, b).

Biostratigraphy

To confirm age assignment multiple samples were analysed

for calcareous nannofossil, foraminiferal assemblages and

paly nomorphs including dinocysts (Figs. 2, 3; Suppl. 1; for

the fauna list see Suppl. 2). Palynomorphs are generally well

preserved, but the proportion of dinocysts and sporomorphs

changes in the individual samples. Due to bad preservation

a part of the studied fossils stays in the open nomenclature.

Additionally, samples contained pieces of coal, palynomorphs,

Halicoryne aff. morelleti algae, Porifera spicules, Ostracoda

valves, Echinoid spines, Osteichthyes bones, teeth and scales.

In the VR-1 well pyritized diatom valves are also present,

whereas in the ZM-1 well Limacina sp. (Spiratella) remains

were observed.

From the MOJ-1 well all studied samples were barren for

nannofossils and dinocysts. In the foraminiferal assemblages

the benthic species prevail (Suppl. 1). In the lower part (2100–

2095 m) rare Bogdanowiczia pocutica (Bathysiphon pocutica)

is present. A sample from a depth of 2010–2005 m contains

rich Halicoryne aff. morelleti remains. In the following sam-

ples, the benthic Elphidium sp. div. and Quinqueloculina–

Miliolina specimens are dominant. In the depth of

1848–1851 m Elphidium hauerinum and small echinate

elphidia (E. josephinum, E. aculeatum) together with miliolids

are present, but their ratio varies in the cores. In the depth of

1795–1798 m few elphidia are present. Planktic Globigerinella

obesa and other fragments of the lower Miocene foraminifers,

like Lenticulina sp. are found in the depth of 960–955 m.

From the IV-1 well, the first sample was taken from the muddy

interval of a gravity flow (2316–2311 m). The nannofossil

assemblage is dominated by Braarudosphaera bigelowii and

B. bigelowii parvula, but the association does not contain

biostratigraphical markers (Suppl. 1). Eocene and Oligocene

redeposits are also observed. The following interval (2093–

1956 m) is barren for dinocysts, with an exception of reworked

?Deflandrea sp. in the depth of 2090–2093 m. On the other

hand, benthic foraminifera Elphidium sp. and species of

Quinqueloculina–Miliolina genera are dominant. Elphidia

prevail in the lower part; while in the depth of 2045–2040 m

miliolids dominate. Foraminiferal assemblages include Poro

sononion sp., reworked foraminiferal tests of Cassigerinella

globulosa and Haplophragmoides sp. Halicoryne aff. morelleti

algae is also present (2045–2040 m). Bolivina sarmatica is

found in the depth of 1956–1961 m. First occurrences of

the dinocysts Virgodinium sp., Spiniferites sp. and freshwater

algae Spirogyra, Zygnema, Ovoidites are identified in the depth

of 1758–1763 m. Autochthonous Pannonian (Tortonian) nano-

fossil Reticulofenestra tegulata and dinocysts Virgodinium

asymmetricum, Spiniferites bentori pannonicus are observed

in the depth of 1603–1612 m. These dinocysts together with

Well

WGS 84 decimal

WGS 84 degrees minutes seconds

Longitude

Latitude

ZM-1

18.37121

48.37382

18°22’16.35” E

48°22’25.74” N

VR-1

18.26955

48.27331

18°16’10.37” E

48°16’23.92” N

IV-1

18.13928

48.22312

18°08’21.42” E

48°13’23.24” N

MOJ-1

18.06612

48.19925

18°03’58.04” E

48°11’57.29” N

Table 1: Coordinates of the studied wells.

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oblongus, Achomosphaera sp., Chytroeisphaeridia cariacoensis

(750–755 m); Virgodinium asymmetricum, V. transformis,

Pontiadinium pecsvaradensis, Impagidinium spongianum,

Chytroeisphaeridia cariacoensis (703–707 m) and V. asym

metricum, P. pecsvaradensis (603–607 m).

The lower part of the ZM-1 well is barren for index fossils.

Only poor nannofossils are observed in the depth of 1555–

1551 m (Suppl. 1). However, the following well cores con-

tained poor and badly preserved foraminiferal assemblages. In

the depth of 1405–1410 m possible (? undetermined) aggluti-

nated foraminifera or testaceans, glyptostrobus seeds and cone

parts are present. In the depth of 1346–1351 m, remains of

Nonion communis, Bulimina elongata, Haplophragmoides sp.,

Reticulophragmium sp., Bathysiphon sp., Uvigerina semi

ornata, Haplophragmoides wilsoni, Spirorutilus carinatus

(Fig. 2), together with dinocysts Melitasphaeridium choano

phorum, Cleistosphaeridinium placacanthum and Cretaceous

reworked foraminifers are present. For the depth of 1253–

1258 m an abundant and diversified foraminiferal association

is typical, but tests are fragmented and show signs of dissolu-

tion. The most abundant are Bolivina dilatata maxima, Melonis

pompilioides (Fig. 2), Angulogerina angulosa, Valvulineria

complanata, bryozoans and ostracoda valves. Nannofossil

assemblages from this interval (1351–1201 m) contain Braa

rudosphaera bigelowii bigelowii, Calcidiscus leptoporus,

C. premacintyrei, C. macintyrei, C. tropicus, Helicosphaera

walbersdorfensis, H. wallichii, Holodiscolithus macroporus,

Reticulofenestra pseudoumbilicus, Sphenolithus abies, Umbi

lico sphaera rotula (Fig. 3). The association in the depth of

1046–1051 m is highly dominated by the foraminifer Bolivina

dilatata maxima (Fig. 2) and by poorly preserved Calcidiscus

spp. nannofossils. Reticulofenestra tegulata acme (Fig. 3) is

present in the depth of 1010–1005 m. Spiniferites bentori pan

nonicus (653–658 m) is also present in the depth of 599–604 m

together with Impagidinium spongianum. I. spongianum and

Spirogyra are found in the depth of 551–556 m.

Lithology and composition of Neogene fill

MOJ-1 well

The leucocratic granite in the depth of 2099–2129 m

(Figs. 4, 5) is composed of Qz, Pl, Mc, Or, Ms and Zrn.

Fissures in the granites are filled by secondary carbonates.

The basal part of the Neogene fill (2099–1790 m; Figs. 4, 5)

is composed of massive, lithic, medium-grained sandstones to

fine-grained conglomerates, which interfinger with laminated

mudstones. Mudstones include sporadic, lenticular sandy

ripples. In the depth of 1790–1640 m the character of the sedi-

mentary fill changes (Fig. 5). According to well logs and

description of cuttings (Tanistrák 1969) three major gravelly–

sandstone intervals divided by muddy horizons were recog-

nized. Fine-grained conglomerates and sandstones are poorly

sorted and display intervals with normal gradation and rare

mud intraclasts (max. 3 cm). Normally graded conglomerates

and sandstones are followed by ripples forming flaser struc-

ture. The top of the ripples is coated by carbonized plant frag-

ments (Fig. 5). The sedimentary interval between 1640–980 m

displays a heterolithic character but sandstones dominate.

The mudstones are laminated; commonly bioturbated and

ripples form flaser to wavy bedding. They rarely include

articu lated shells of Congeria czizeki (1253–1261 m) and

fragmented limnocardid bivalves (1000–1005 m; Fig. 5).

In the sandstones normal gradation and lamination is high-

lighted by carbonized plant fragments. In the lower part

(1600–1300 m) the sandstones are better sorted and grains are

more rounded. The sorting and roundness decreases again

in the depth range from 1300 to 1000 m. The sediment in

the interval of 980–395 m is characterized by alteration of

sandstones and mudstones with red mottles, but sandstones

are slightly more abundant. In the well cores we recognize

rip-up clasts, rhizoids and bioturbations (Fig. 5).

The sandstones and conglomerates are composed of mono-

crystalline quartz (Qz), epiclastic carbonates, Qz+mica schists,

granitoid, polycrystalline Qz, microcline (Mc), orthoclase

(Or), plagioclase (Pl), rare muscovite (Ms), chlorite (Chl),

garnet (Grt), zircon (Zrn), turmaline (Tur) and rutile (Rt).

In the basal part, carbonate overgrowth, foraminifera test, Glt

and framboidal Py were observed. In addition, carbonate fis-

sures which cut mineral grains, were present (depth 2050 m;

Fig. 6), which indicates disintegration after lithification.

The mineral maturity (amount of monocrystalline Qz)

increases upwards. The most pronounced change in the com-

position is the presence of intensively coloured Chl and Bt

at a depth above 980 m. The amount of carbonate cement

decreased upward, however the sample from the depth of

1397 m is heavily cemented with several generations of

carbonate including poikilitic cement and carbonate clasts

covered by iron oxides. A sample from the depth of 705 m also

contains poikilitic cement.

Heavy mineral associations were analysed from four sandy

samples (depth 1760 m, 2×1000 m and 550 m). Their compo-

sition is the same for all samples. Among transparent heavy

minerals Grt (20–44 %) and Tur (4–26 %) dominate. Small

amounts of Zrn, Ap, Rt, staurolite (St) and sillimanite (Sil <

2 %) occur. The association is completed by Ilm (7–17 %), Glt

(up to 0.5 %) and framboidal pyrite (Py) together with limo-

nite minerals (21–60 %). Samples from 1000 m rarely contain

epidote (Ep) and magnesio-ferri-hornblende. Associations

from depths of 1000 and 1760 m also show a strong leucoxe-

nization, manifested by the presence of ferric oxide / hydroxide

coating mineral grains (mainly carbonates). Framboidal pyrite

is oxidized. In the depth of 550 m oxidation is minimal and

moreover crystalline pyrite was also documented. Additionally,

zonal Tur with a schorl core and dravite rim is found. Other

Tur of dravite composition did not show significant zoning.

IV-1 well

The dark-grey to grey-green basement rocks show an orien-

ted porphyroclastic–mylonite texture (2390 m; Figs. 7, 8).

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They contain white blasts (0.5–3 cm) made up of recrys tallized

Qz, Pl, minor Kfs or by aggregates of these minerals. The space

between the blasts is occupied by microcrystalline Qz, Chl and

by dispersed opaque minerals. At the depth of 2355 m light

grey phyllonitic to porphyroblastic rocks with pink-coloured

carbonate veins occur (Fig. 8). Less deformed parts have

a similar composition as the underlying rocks, but the degree

of Fs sericitization increases and the intensively coloured Chl

is absent. The pseudomatrix is formed by sericite. In the inten-

sively deformed parts the ribbons are formed by recrystallized

Qz, moreover laminas of idiomorphic Tur (Table 2, Fig. 6a)

and opaque minerals are found. Both sampled levels display

cataclastic crushing. From the accessory minerals Zrn, Rt and

Py occur.

The base of the Neogene fill is composed of poorly sorted

conglomerates and sandstones (2350–2140 m, Fig. 7). Normal

gradation, erosional surfaces, lamination and ripple cross-

lamination is observed (Fig. 8). The diameter of the clasts does

not exceed 10 cm. In the conglomerates grey micritic carbo-

nates occur, which yield rare foraminifera and calcite veins.

Other present carbonates yield pelmicrosparite, sparite to

recrys tallized textures. Carbonate breccia and carbonate silt-

stone clasts occur. It is important to note, that carbonate clasts

are less rounded, than the siliciclastic lithoclasts. They are com -

po sed of granitoid to metagranitoid and sandstones. The large

granitoid fragments are heavily shattered, and the fissures are

filled with calcite (Calc). Sandstones and meta-sandstones are

ranked to quartz arenite, arkose to meta-greywacke with seri-

citic pseudomatrix. Clasts corresponding to Bt schist are also

found. Quartz phyllite, shale, chert and melaphyre are less

abundant. Melaphyre clasts with intersertal and rarely diorite

texture include Pl phenocryst in dark groundmass. Amygdales

and pseudomorphs are filled by Qz and microcrystalline Qz

(Fig. 6). Additionally, a fragment of Permian felsite with mag-

matically corroded Qz and a fragment of pseudotachylite is

found. Mineral grains are mainly composed of polycrystalline

Qz, Or, Pl and Tur. Carbonate cement is present in all samples.

The overlying part from the depth of 2140–1930 m is domi-

nated by mudstones and sandstones. The mudstones are

commonly bioturbated and contain rare leaf (Zelkova sp.) and

fish fossils (Pleuronectiformes; Zahradníková et al. 2013).

In the sandstones two types of structures occur: the first is

characterized by gradation and the second by horizontal and

ripple-cross lamination (Fig. 8). Pillow structures and synse-

dimentary folds are abundant in both sandstone types. The grain

composition is enriched by shales to phyllites and large leaves

of Chl, Ms and Bt. In the binding material Glt and foraminifers

occur. From volcanites, only one clast is observed, but the size

of the clast does not allow its assignment to Paleozoic or

Neogene volcanics. The carbonate cement is poikilitic in

some samples, while clay intraclasts are common. In the depth

of 1930–1650 m para-conglomerates (gravel: 14–25 %,

sand: 49–56 %, lutite: 25–30 %) are present (Figs. 7, 8). Well

rounded clasts are max. 3–5 cm in diameter and are accompa-

nied by armoured mud intraclasts and synsedimentary fold

structures. The debris composition is dominated by granitoids,

additionally a small amount of white Neogene volcanic clasts

are present. They are composed of Pl phenocryst in altered

glassy groundmass. The remaining intervals were poorly

sampled, or were not sampled at all. Nonetheless the SP and

RT log trends can provide some data on the lithology, which is

confirmed by the core 5 which drilled massive mudstones

(Fig. 8).

Heavy minerals were analysed from five samples (depth

2240, 2160, 1960, 1760 and 1705 m). Their mineral compo-

sition is similar. Among transparent heavy minerals Grt (16–

53 %) dominate, while Tur, St, Ap, Rt, Zrn are less abundant

(< 8 %). Both dravite and schorl Tur are observed. Ilm creates

6–42 % and oxidized framboidal pyrites with minerals of

limo nite group create 5–26 %. Glt is present mainly in the depth

of 2240–1960 m (5 to 6 %) and decreases in the depth of

1760–1705 m to < 1 %. In the first interval one magnesio-

chromite spinel (Mg

0.52

0.46

0.01

1.18

0.77

0.04

) is

detected. On the other hand, Ep appeared in the second

interval.

VR-1 well

Basement rocks drilled in the VR-1 well are composed of

metamorphosed pink quartzites together with lila-brown

shales and overlying dolomite with layers of black graphitic

shale (Gaža 1968; Biela 1978a). From these rock types

only the brecciated microcrystalline dolomite (Figs. 9, 10) is

pre served.

Conglomerates from the base of the Neogene fill were not

present in the archive (2460–2300 m). Only original petro-

grafic analyses describing poorly rounded, variegated clasts

(max. 3 cm in diameter) of siltstones, claystones, shales, sand-

stones and rare, limonitized diabase grains with ophitic texture

were reported by Gaža (1968).

The overlying interval is marked by abundant epiclastic vol-

canic material (2300–1860 m). The sequence starts with nor-

mally graded conglomerates and sandstones with rounded

clasts (Fig. 10). They pass into poorly sorted, coarse-grained

sandstones with armoured mud intraclasts. The lower white

and green coloured part (up to 2055 m) consists of rhyolitic

vitroclasts, spherulites, spherulitized vitroclast, pumice, Kfs,

Pl (An

23–29

; Fig. 11, Table 3), Qz phenocrysts (observed mag-

matic corrosion) and rare heavily altered Bt (Fig. 6). This part

also contains greenish crystalloclastic fine-grained tuff clasts,

which rarely include vitroclasts and volcanic lithoclasts. These

tuff fragments showed signs of deformation and bending

around clastic grains. Non-volcanic lithoclasts are fairly rare.

They are composed of granitoid, metaarkose, quartz arenite,

phyllite/shale, Qz-mica schist, polycrystalline Qz and Zrn.

At the depth of 2055 m, the composition of the volcanic mate-

rial changes. Intermediate volcanic lithoclasts with porphy-

ritic, intersertal and pilotaxitic texture dominate and lithoclasts

with perlite texture are very rare. They are composed of Pl

phenocrysts (An

40–63

; Fig. 11, Table 3) and pseudomorphs after

mafic minerals (Px?) ± Bt (Fig. 6). From phenocrysts Qz, Bt,

zonal and sieved Pl and pseudomorphs after mafic minerals

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filled by Chl are present. Chloritized tuffaceous matrix is

responsible for the green-grey sediment colour and its share

decreases upward. However, rhyolitic lithoclasts are still

present. At the depths of 2055 m and 1904 m carbonatized

tuffite layers are cut by multiple veins (Fig. 10).

The overlying heterolithic interval (1860–1310 m) is domi-

nated by sandstones with occasional coal seams and abundant

carbonized plant fragments. Within sedimentary structures

lamination, ripple-cross lamination, small scale cross-beds,

bioturbation, normal gradation, mud intraclasts and convolute

bedding are observed, (Fig. 10). The amount of volcanic litho-

clasts decreases, whereas content of stable minerals (Qz,

Zrn, Tur, Rt, Grt) and non-volcanic rock fragment increases.

The amount of the carbonate cement, sorting and roundness of

grains increases as well. The composition of non-volcanic

lithoclasts is enriched by micritic carbonates, cherts and fossil

remnants. In the depth up to 1550 m Glt is documented.

In the depth of 1310–1250 m, a change in the lithological

appearance is observed. This interval is composed of para-con-

glomerate to poorly sorted, coarse-grained sandstone with

approximately 7 % gravel (max. 1 cm in diameter), which

includes abundant cardiids (Fig. 10). The volume of the sandy

and lutite fraction is the same (50 %). Sandy and gravelly

layers are rarely supplemented by muddy intercalations. Clast

composition remains the same.

The upper parts (1250–395 m) are characterized by altera-

tions of mudstones and minor sandstones. The matrix is pre-

dominantly red in colour. Lamination, bioturbation, synsedi -

mentary folds, carbonized plant fragments, leaves (Ulmus

pyramidalis) and dreisenids are present (Fig. 10). The fine-

grained sands consist of Qz, Fs, Ms, Chl and rarely observed

carbonate crystals.

Heavy minerals were analysed from four sandy samples

(depth 1450, 1305, 1250 and 950 m) and one lutite sample

(depth 500 m). Mineral composition is nearly identical in all

samples, but representation of individual minerals at the 500 m

depth is significantly affected by overall grain-size of the sam-

ple. Grt (7–44 %) and Ilm (18–43 %) dominated in the sandy

samples; in the lutite sample Grt create 3 %. Ap, St, Tur (dra-

vite), La

0.21-0.24

0.40-0.43

allanite (Table 2), Zrn and Rt did not

Neogene fill

Mylonite basement

Neogene fill

Well

ZM-1

VR-1

MOJ-1

IV-1

IV-1/21

Well

VR-1

core

rim

core

rimI

rimII

core

rim

core

rim

Min.

Srl

Drv

Srl

Drv

Srl

Drv

Aln

SiO

36.63

36.70

36.82

36.19

36.64

37.98

34.54

36.60

37.65

37.88

37.13

SiO

31.32

30.89

TiO

0.53

0.66

0.44

1.77

0.87

0.05

0.29

0.16

0.22

0.14

0.15

TiO

0.77

1.41

29.28

32.73

34.98

28.69

32.33

32.05

33.25

32.24

31.91

32.72

32.41

14.40

13.85

0.02

0.03

0.07

0.00

0.04

0.00

FeO

15.56

15.63

FeO

9.58

6.94

5.83

11.84

7.81

5.77

15.11

3.09

4.01

2.61

3.68

MgO

0.66

0.64

MgO

5.94

5.95

5.68

5.27

5.96

7.98

0.69

10.28

9.66

10.06

9.57

MnO

0.76

0.36

CaO

0.30

0.57

0.54

0.31

0.65

0.05

0.09

0.12

0.26

0.16

0.14

SrO

0.05

0.06

MnO

0.00

0.02

0.06

0.01

0.00

0.10

0.02

0.01

0.00

0.06

CaO

10.31

9.94

2.57

1.78

1.71

2.59

1.93

2.20

1.88

2.58

2.48

2.49

2.46

0.01

0.03

0.02

0.01

0.04

0.03

0.01

0.00

0.06

0.02

0.03

0.06

0.12

0.13

0.00

0.27

0.00

ThO

1.83

0.61

0.01

0.00

0.01

0.00

0.01

0.00

0.01

0.00

0.04

0.01

3.59

3.67

3.74

3.59

3.68

3.73

3.40

3.70

3.74

3.77

3.72

6.78

6.63

10.40

10.64

10.83

10.42

10.67

10.80

10.24

10.71

10.84

10.92

10.77

11.43

12.30

0.51

0.34

0.42

0.26

0.31

0.35

0.17

0.00

0.14

0.18

0.03

1.08

1.27

Total

99.37

100.04

101.13

101.02

100.95

100.97

100.10

99.51

100.98

100.94

100.17

2.89

3.77

O=F

0.00

0.11

0.00

0.28

0.36

6.123

5.995

5.909

6.033

5.967

6.109

5.863

5.939

6.035

6.028

5.993

0.40

0.37

0.000

0.005

0.091

0.000

0.033

0.000

0.137

0.061

0.000

0.007

0.17

0.32

3.000

0.05

0.04

5.769

6.000

5.638

6.000

0.00

0.12

0.231

0.000

0.362

0.000

0.13

0.19

0.000

0.03

0.06

0.000

0.04

0.09

0.000

0.295

0.524

0.000

0.172

0.075

0.515

0.103

0.030

0.138

0.158

0.19

0.24

0.067

0.081

0.054

0.222

0.107

0.007

0.036

0.020

0.026

0.016

0.018

Total

99.31

99.32

0.000

2.996

2.981

0.002

0.004

0.009

0.000

0.006

0.000

0.004

0.019

0.000

1.619

1.556

1.249

1.449

1.359

0.948

1.448

1.914

0.174

2.487

2.308

2.386

2.301

0.056

0.102

0.000

0.002

0.008

0.002

0.000

0.001

0.015

0.002

0.001

0.000

0.008

0.095

0.091

1.340

0.948

0.782

1.651

1.064

0.776

2.145

0.419

0.538

0.347

0.497

1.245

1.262

0.000

0.062

0.030

Li*

0.342

0.222

0.269

0.174

0.200

0.228

0.114

0.000

0.092

0.113

0.017

1.056

1.027

0.053

0.099

0.092

0.056

0.113

0.009

0.017

0.020

0.045

0.027

0.024

0.003

0.832

0.565

0.532

0.837

0.610

0.686

0.619

0.811

0.771

0.768

0.771

0.040

0.013

0.004

0.003

0.009

0.007

0.001

0.012

0.005

0.003

0.006

0.011

0.001

0.000

0.110

0.333

0.366

0.101

0.275

0.304

0.352

0.164

0.181

0.198

0.194

0.400

0.435

3.998

4.000

3.999

3.998

4.000

3.853

4.000

3.999

3.998

4.000

0.239

0.236

0.000

0.144

0.000

REE

0.183

0.238

0.002

0.000

0.001

0.002

0.000

0.003

0.000

0.001

0.002

0.000

Table 2: Selected analyses of tourmaline (*calculated to stoichiometry) and allanite.

397

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exceed 3 %. The amount of framboidal pyrite and limonite

minerals increases upward from 4 % (in the depth 1450 m) to

55 % (in the depth 1250 m). Samples from the depth of 950

and 500 m no longer contain pyrite, but the sample from

the depth of 950 m is leucoxenized and the content of limonite

minerals is 62 %. In contrast, the lutite sample from the depth

of 500 m has only 7 % of limonite minerals. Associations of

the sandy samples are completed by monazite and rock frag-

ments formed by Na

0.40

0.54

-rich mica with inclusions of

chloritoid and staurolite (Fig. 12).

ZM-1 well

The basement rocks in the ZM-1 well were not present in

the repository. However, in the original report (Gaža 1970)

grey metamorphosed arkose with carbonate veins (depth

below 1956 m) is assigned without a doubt to the Paleozoic

basement (Fig. 13). The lower limit of the Neogene fill in

the ZM-1 well is questionable due to the lack of the disputed

well cores (Fig. 13). From this interval, only a core from

the depth of 1711–1708 m is preserved, which has similar

character as sedimentary rocks from the depth of 1558–1448 m.

These sediments are represented by fine-grained conglome-

rates, sandstones and mudstones. In the grey mudstones,

synsedimentary folding, abundant carbonized plant fragments

and red mottles are observed (Fig. 14). The mudstones are

often cut by scours and filled with fine-grained conglomerates.

The conglomerate and light coloured sandstones are normally

graded. Clasts are poorly rounded and locally poorly imbri-

cated. In their composition the Qz, Qz-sericitic and carbonate

shale lithoclasts strongly dominate. Altered granitoids to

meta-granitoids, meta-greywacke, meta-arkose, chert/felsite,

quartz arenite, arkose, lithic sandstone and micritic to recrys-

tallized carbonates are also included. In the upper part (above

1495 m) altered volcanic lithoclasts appear and their volume

increases upward. From mineral grains altered Fsp, Bt, Zrn

and opaque minerals occur. Some granitoid grains are

carbonatized.

A significant change in the modal composition is observed

at a depth of 1410–1007 m. At the base of the interval (depth

1405–1410 m) weakly consolidated, greenish, massive volca-

nic sandstones with tuffaceous matrix are present (gravel

1–4 %, sandy fraction 44–55 %, lutite fraction 44–53 %).

Volcanic origin is represented by altered volcanic lithoclasts,

vitroclasts and Pl. Mafic minerals except altered Bt are not

preserved. Inside these sandstones, well sorted polymict con-

glomerates with normal to inverse gradation and well rounded

pebbles (1–2 cm diameter) are present (Fig. 14). They contain

poikilitic calcite cement. Abundant volcanic lithoclasts yield

intersertal and porphyritic texture with Pl phenocrysts and

pseudomorphs after mafic minerals (Px ± Amp) often filled by

calcite in microlithic glass. Nonvolcanic lithoclasts in both

types are composed of quartz arenite, arkose, meta-arkose,

greywacke with strong ore pigment, lithic sandstone, siltstone

and altered granitoids. These volcanic sandstones pass into

grey mudstones. In the mudstone, intercalation of coarse-

grained volcanic conglomerate (depth 1351–1346 m) and ben-

tonite (1310–1305 m) appears (Fig. 14). Volcanic conglomerate

with subrounded to poorly rounded pebbles cannot be clearly

classified because of the ratio between core diameter (10 cm)

and the clast diameter (up to 6 cm). The conglomerate is

unsorted and is formed entirely by volcanic lithoclasts of

andesite to dacite with porphyritic texture. The composition

of the lithoclasts and matrix is approximately the same.

Pronounced rusty colour of the matrix is a result of a stronger

alteration. Lithoclasts with microcrystalline groundmass are

light pink to grey and yield large phenocryst (about 0.5 cm) of

reddish-brown, idiomorphic Bt, and Pl (An

74-65

in the core to

in the rim; Fig.11, Table 3). Opacitic Amp phenocrysts

are dominantly of magnesio-hastingsite composition, less fre-

quently of magnesio-ferri-hornblende composition (Šarinová

& Rybár 2018). They are often replaced by secondary minerals.

Rare magmatically corroded Qz, Kfs and augite are also present

(Fig. 6). The white bentonite layers contain glass shards, Qz,

Pl and Bt in smectite matrix. Above the bentonite, mudstones

dominate and include rare, graded sandstone layers. Coarse-

grained sandstones with poikilitic carbonate cement (1255 m)

contain well-rounded cloudy volcanic epiclasts, shale, grani-

toid, carbonates, quartz arenite, arkose, Qz, sericitized Or, Pl,

Bt and Tur. At the depth of ~1100 m fine-grained deposition is

terminated by the second layer of coarse-grained volcanic

conglomerate (the clasts reach up to ~10 cm; Fig. 14). Their

composition corresponds to the composition of volcanic con-

glomerate from the depth of 1350 m, but one green clast of

an andesitic tuff is also found. The volcanic conglomerate

passes into poorly sorted, chaotic, rusty coloured, sandy vol-

canic paraconglomerate and coarse-grained sandstone (gravel:

4–11 %, sand: 39–60 %, lutite: 28–57 %). These chaotic

conglomerates are composed of rounded andesite clasts, hea-

vily altered volcanic lithoclasts and elongated mud intraclasts

(Fig. 14). Heavy synsedimentary deformation and poorly

Fig. 11. Composition of feldspars in volcanic lithoclasts from ZM-1

and VR-1 well. * data taken from Šarinová & Rybár (2018).

398

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GEOLOGICA CARPATHICA

, 2018, 69, 4, 382–409

preserved ripples are also documented. The diameter of litho-

clasts decreases upward from 5 to 2 cm. Well rounded, lithi-

fied clasts of older volcanic rocks are similar to those in

the underlying volcanic lithoclasts. Strongly altered, friable

clasts with the rusty-brown, hyaline to pilotaxitic volcanic

groundmass contain phenocryst of Bt, Pl, Amp, Px and

probably orthopyroxene pseudomorphs filled by secondary

minerals (Šarinová & Rybár 2018). The sandy matrix addi-

tionally includes Pl, Bt, Amp, Px, vitroclastic and crystallo-

clastic tuff clasts, arkose, granitoid, shale and polycrystalline

Qz. The interval is closed by layered pale grey mudstone.

Another significant change in the composition of sediments is

observed in the depth of 1000–700 m. From the coarse clastic

interval the core from the depth of 954–959 m was only avai-

lable. Laminated sandstone with indistinct ripples, and abun-

dant carbonized plant fragments, occurs together with poorly

sorted conglomerate with synsedimentary folds and erosional

contacts (Fig. 14). In this interval, altered volcanic lithoclasts

are represented only by a small percentage. The dominating

non-volcanic lithoclasts are composed of altered granitoid,

mylonite, Qz to Qz–Ser shale, sandstone, Qz, Kfs, Pl and chlo-

ritized Bt. The drilling report (Gaža 1970) of several consecu-

tive cores describes 3 to 10 cm long clasts composed of shale/

phylite, quartz arenite, granitoid, greywacke and volcanite.

A fine-grained interval follows in the depth of 700–340 m and

is dominated by laminated mudstones with minor carbonized

plant fragments. In the depth of 551–556 m a layer of poorly

sorted, coarse-grained, sandstone to graded conglomerate is

documented. Fine-grained conglomerate with crystalline car-

bonate cement showed a similar composition as the previous

sample.

Heavy minerals were analysed from sandstones (1450 m)

and volcanic sandstones to sandy conglomerates (1410 m,

1050 m and 1005 m). During the validation of mineral compo-

sition by microprobe, the polished section from the depth of

1450 and 1410 m contained only a small number of picked

grains. From transparent minerals Ap 4–6 % dominated, Grt

makes up 1–6 % and Tur 1–3 %. Zrn, Rt, Sp and Cpx (augite)

are also present. One Tur with schorl core and dravite rim is

part of a lithoclast consisting of Qz, Ms, Ab and Ap (Fig. 12).

Sandstone from the depth of 1450 m consists of 71 % of limo-

nite minerals, 12 % of pyrite (including framboidal) and 1 %

of Ilm. On the other hand, volcanic sandstone from the depth

of 1410 m is composed of 25 % of Ilm, 18 % of limonite and

limonitized pyrite and idiomorphic Bt (37 %). Volcanic sand-

stones to conglomerates from the depth of 1050 m and 1005 m

contain different amphibole rich associations (47–79 %).

The associations are completed by Ilm together with Mag

(16–45 %), Py (2–7 %), Ap (1–3 %), Px (1.6 %), Zrn, Tur, Rt,

Ttn and Grt (less than 1 %). The composition of Amp (cum-

mingtonite, magnesio-hornblende, magnesiohastingsite) and

Px (augite) was published by Šarinová & Rybár (2018).

Garnet

Garnets were present in all samples, therefore they were

selected for further study. The ZM-1 well is not statistically

evaluated, since only one Grt was analysed. Grt are divided

into seven groups based on different molecule composition

(Fig. 15): a) Alm

Sps

from MOJ-1 clearly corresponds to

a granite source; b) Prp

11-21

Alm

69-82

are abundant and contain

inclusions of Chl, Rt and Zrn. They correspond to fields of

well

VR-1 rhyolite clasts

VR-1 andesite clasts

ZM-1 Bt-Amp andesite/dacite clasts

depth

2104 - 2109

1450 - 1250

1346 - 1351

1099 - 1

104

type

Kfs

Phen.

matrix

Phen.

matrix

Phen.

matrix

Phen.

matrix

SiO

64.74

64.62

61.49

62.42

54.94

55.32

53.40

53.55

54.07

53.77

55.04

51.77

55.69

49.04

55.77

52.50

48.32

65.08

54.18

65.24

18.55

18.20

23.78

23.12

27.37

27.41

27.48

28.90

28.16

28.22

28.10

30.26

27.97

32.54

28.43

29.78

32.30

20.29

28.66

20.79

SrO

0.13

0.1

0.05

0.03

0.08

0.06

0.07

0.05

0.12

0.09

0.1

0.09

0.10

0.08

0.07

FeO

0.05

0.08

0.12

0.1

0.91

0.57

1.04

0.39

0.81

0.79

0.22

0.44

0.18

0.28

0.41

0.34

0.48

0.27

0.51

0.24

MgO

0.00

0.03

0.04

0.03

0.02

0.06

0.00

0.02

0.04

0.00

0.03

0.00

0.02

0.04

0.00

0.03

0.02

BaO

0.39

0.25

0.89

0.47

CaO

0.13

0.15

5.55

4.79

11.17

10.80

11.62

12.1

11.89

12.02

11.17

13.68

10.59

15.90

.11

12.90

16.09

0.29

11.15

0.46

2.58

1.29

7.76

8.02

5.01

5.10

4.77

4.32

4.61

4.38

5.02

3.61

5.67

2.93

5.38

4.38

2.47

3.78

4.95

4.15

12.98

14.56

0.90

0.89

0.41

0.34

0.39

0.33

0.28

0.27

0.23

0.60

0.30

0.10

0.47

0.21

0.09

10.63

0.37

10.20

Total

99.43

99.17

99.78

99.49

99.88

99.60

98.83

99.67

99.90

99.55

99.90

100.48

100.52

100.89

101.67

100.24

99.87

101.24

99.91

101.58

2.987

3.000

2.744

2.784

2.495

2.509

2.459

2.435

2.457

2.451

2.488

2.352

2.502

2.231

2.484

2.383

2.223

2.936

2.456

2.921

1.008

0.996

1.251

1.215

1.465

1.492

1.549

1.508

1.516

1.497

1.621

1.481

1.745

1.492

1.593

1.751

1.078

1.531

1.097

0.003

0.001

0.002

0.001

0.003

0.002

0.003

0.002

0.003

0.002

0.003

0.004

0.034

0.022

0.040

0.015

0.031

0.030

0.008

0.017

0.007

0.01

0.015

0.013

0.018

0.010

0.020

0.009

0.000

0.002

0.003

0.002

0.001

0.004

0.000

0.001

0.002

0.000

0.002

0.000

0.001

0.003

0.000

0.002

0.001

0.007

0.005

0.016

0.008

0.007

0.265

0.229

0.543

0.525

0.573

0.590

0.579

0.587

0.541

0.666

0.510

0.775

0.530

0.627

0.793

0.014

0.541

0.022

0.231

0.1

0.671

0.693

0.441

0.449

0.426

0.381

0.406

0.387

0.440

0.318

0.494

0.258

0.465

0.385

0.220

0.330

0.435

0.360

0.764

0.862

0.051

0.023

0.020

0.023

0.019

0.016

0.014

0.035

0.017

0.006

0.026

0.012

0.006

0.612

0.021

0.582

cat. sum

5.006

4.991

4.992

4.981

5.005

4.992

5.019

4.991

5.000

4.992

4.991

5.014

5.028

5.016

5.019

5.015

4.996

5.007

5.002

Table 3:

Selected analyses of feldspar from volcanic lithoclasts (Phen.–phenocrysts, matrix–crystals from groudmass).

399

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granitoids and orthogneisses (Fig. 15); c) Prp

21-31

Alm

63-68

indi-

cate more Mg-rich provenance from gneiss (Suggate & Hall

2014; Fig. 15); d) Prp

7-18

Sps

29-40

Alm

41-43

(two Grt from MOJ-1)

compositionality corresponds to Bt gneiss of the Tribeč Mts.

(Ivanička et al. 1998); e) Grs

8-24

Alm

52-83

composition is typical

for low grade metapelite to amphibolite (Suggate & Hall 2014;

Fig. 15). This group yields inclusions of Zrn, Al

SiO

, Ilm, Qz

and Chl; f+g) Grs

9-24

Prp

10-21

Alm

59-69

with inclusion of Amp, Rt

and Bt attributed to Neogene volcanic source or metabasites.

This group yields Grt from the volcanic lithoclast of the VR-1

well (Fig. 12). A slightly different projection of the six Grt

(f group) from the MOJ-1 and VR-1 wells (Fig. 15) is caused

by low content of Sps molecule (˂ 2 %). Sps molecule in

the g group varies from 2.2 to 10 %, with the highest peak

in-between 4 to 6.5 %. Two Grt from the f group also contain

Prp

21-31

(VR-1, MOJ-1), which can indicate an ultrabasic

source (Suggate & Hall 2014).

Interpretation

Provenance

The wide spread late Badenian–Sarmatian sediments are

limited by the Mojmírovce fault zone (e.g., Biela 1978a; Hók

et al. 1999). The composition of non-volcanic sediments from

the basal part of the Neogene fill is generally identical in all

the analysed wells, but variation in the volume of individual

lithotypes occurs. The tectonically disturbed granitoid clasts

without Bt from the IV-1 well correspond to the leucocratic

granite forming the basement of the MOJ-1 well. Leucocratic

granites are typical for the top of granitoid plutons and their

remnants are preserved in the Tribeč part of the Tribeč Mts.

(Ivanička et al. 1998). According to the MOJ- 56, 57, 65 wells

(Biela 1978a), the footwall of the Mojmírovce fault zone (Fig. 1)

was built up by granitoids, which formed the source before

the Pannonian (Tortonian). The higher content of granitoid

clasts in the VR-1 well can be explained by erosion of

the Tribeč Mts. or denudation of Cenozoic granitoids during

the development of the Štiavnica stratovolcano (Konečný et

al. 1998). Due to small areas of exhumation of Cenozoic

grani toids, the source in these granitoids cannot be fully

excluded, but it is unlikely. Provenance of the Bt gneisses

observed in the IV-1 well and described in the IV-4 and 6 wells

(Čermák 1976c, 1977a) can be derived from the Tribeč Mts.

(Ivanička et al. 1998). Arkose, arkosic meta-greywacke, shale,

melaphyre and rare paleorhyolite clasts indicated the presence

of Paleozoic sediments in the source area. Arkosic metagrey-

wacke can be derived from the Paleozoic cover unit of

the Cen tral Western Carpathians. Presence of non-metamorpho-

sed arkose and melaphyre lithoclasts is typical for the Permian

sequence of the Hronic units. These rocks outcrop in the Nor-

thern, Rázdiel part of the Tribeč Mts. (Vozárová & Vozár

1988). On the other hand, quartz arenite, greywacke, clay-

sericitic shales and melaphyre layers were also described from

the pre-Cenozoic basement of the Pohronský Inovec Mts. and

vicinity (GK-5, 6, 12, 13, 14, PKŠ-1, VIK-1 wells; Biela

1978b; Fusán et al. 1987a, b). In this area, Paleozoic com-

plexes are covered mainly by volcanics of the 4

stage of

the Štiavnica Stratovolcano. This does not exclude provenance

from this area, since the onset of the volcanic activity is asso-

ciated with the end of deposition of non-volcanic sediments.

From this point of view, the transport direction from the NE is

obvious, especially in the ZM-1 well, where shale fragments

dominate. In addition, the presence of the lithoclast with tur-

maline (Fig. 12) in the heavy fraction of the ZM-1well (depth

1450 m) showed that the non-volcanic material comes from

the first cycle of erosion. The abundant fragments of pink-

coloured quartz arenite to subarkose can be attributed to

the Lower Triassic of the Lúžna Fm., as well as to the Upper

Triassic of the Carpathian Keuper Fm. (Ivanička et al. 1998).

Both formations are present in the Tribeč Mts., but the pink-

coloured subarkose to arkose and violet-coloured claystone

(Gaža 1968) of the Carpathian Keuper Fm. (Biela 1978a) was

also described from the top of the Pre-Cenozoic basement of

the Vr-1 well. Their presence in the immediate basement sug-

gests that they could form the margin of the depocentre.

Therefore, the provenance of pink quartz arenite to subarkose

can be found on the SW, as well as on the N rim of the depres-

sion. Micritic carbonates with small amounts of allochems are

typical for the Triassic. At present such carbonates emerge to

the surface in the Tribeč Mts. In addition, carbonate and shale

alternations were described in MOJ-7, 8 and 29 wells which

are located N and NW from the MOJ-1 and IV-1 wells (Biela

1978a; Fusán et al. 1987b; Fig. 1). The Mesozoic basement in

these wells is covered only by Pannonian sediments, which

means that carbonates formed the margin of the depression

during the Sarmatian (late Serravallian) time. Towards

the south, carbonate rocks were also found in the basement of

the VR-1, POZ-1, 2, 4 and Podhájska-1 wells (Biela 1978a).

In this case, carbonates are covered by sediments of late

Fig. 12. a — andesite volcanic lithoclasts from the VR-1 well (1250–

1309 m); b — detail of andesite clasts with Grt (BSE); c — metapelite

clasts with zonal Tur (ZM-1, BSE); d — mica with Cld, VR-1/c20,

1450–1455 m.

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Different, finer grained development of basal sediments

from the MOJ-1 well can be attributed to the position on

a basement elevation of the Tribeč Mts. The high content of

monocrystalline Qz and the very low amount of mica indicates

that the granitoid source is similar to that of the underlying

granite. The second major source is represented by carbonates.

Both rock types can be linked to the Tribeč Mts., which con-

firms a local provenance.

In the MOJ-1 and IV-1 wells only a minor change of prove-

nance was observed upwards. This is documented by large Bt,

Bt-granitoid debris and by higher amounts of shale to phyllite

clasts. The occurrence of granitoids with Bt indicates

an increase in the influence of the Tribeč Mts. provenance.

The shale debris generally means a relatively near source area,

because of their rapid mechanical decay. They can still be

derived from the basement, which was exhumed on the foot-

wall of the Mojmírovce fault zone.

The admixture of volcanic material appears in sediments

of late Badenian–Sarmatian (Serravalian) age, mainly in

the eastern to central part of the depression (ZM-1 and VR-1

wells). In the ZM-1 well, a gradual transition from non-volca-

nic to volcanic epiclastic sediments manifested by an increase

in volume of volcanic clasts was observed. Volcanic sand-

stones and andesite pebbles (1405–1410 m) indicate reworking

of volcanites from the 1

stage of the Štiavnica Stratovolcano

development. Based on mineral composition and felsic,

microlithic groundmass the coarse-grained Bt –Amp ± Px

andesite to dacite conglomerate (1405 m, 1100 m) can be

linked to the Studenec Fm. (3

volcanic stage; Šarinová &

Rybár 2018). Today the Studenec Fm. outcrops on the surface

between Nová Baňa town and Stará Huta village (Fig. 1;

Konečný et al. 1998). Mudstone and sandstone intercalations

from in-between volcanic conglomerates (1405–1100 m) indi-

cate calming of volcanic activity and recycling of older depo-

sits. Based on the fossil residues recycling of Oligocene,

Cretaceous (Ozdínová 2012) and Badenian sediments is

proved. The presence of strongly altered volcanic clasts of

reddish-brown colour (Fig. 14) and fresh phenocrysts of Px

and Amp (Fig. 6h), inside the overlying chaotic conglomerate

(1046–1051 m), indicated short transport by gravity flow

mechanism. Admixture of new cummingtonite-bearing volca-

nic lithoclasts indicate deposition connected with the 4

stage

of the Štiavnica stratovolcano (Šarinová & Rybár 2018).

However, volcanic conglomerates, sandstones, bentonite and

other clasts of volcanic origin clearly confirm the dominance

of volcanic provenance. From the point of view of provenance,

it is interesting, that rhyolite material and spherulites, which

occur abundantly in the VR-1 well, are not observed in the ZM-1

well. This fact points to two separate source areas; first for

the vicinity of the ZM-1 and second for the vicinity of the VR-1,

both coming from the NE. Rhyolite and spherulite clasts,

which significantly dominated in the depth of 2207–2104 m in

the VR-1 well, can be derived from the Jastrabá Fm. The clo-

sest outcrops of the Jastrabá Fm. are situated to the NE of

Nová Baňa town (Fig. 1). This provenance is supported by

similar composition of Pl phenocrysts from the VR-1 well

(Table 3) and rhyolites from the Jastrabá Fm. (Demko 2010).

Additionally, the presence of rhyolite conglomerate near

Tekovské Nemce village confirms transport from this area.

At the depth of 2055 m, a rapid change to andesite character of

volcanic debris is observed. This fact can be interpreted in

two ways: 1) by deep erosion, which started by removal of

the Jastrabá Fm. and continued to erode the relatively older

Priesil and Inovec Fm., or 2) by onset of andesite volcanic

activity during the transportation of rhyolite epiclasts.

The second option is in contradiction with the evolutionary

stages of the Štiavnica Stratovolcano (Konečný et al. 1998;

Chernyshev et al. 2013), but the new ages of the Jastrabá Fm.

from Nová Baňa town (12.31–12.03 Ma by Lexa & Pécskay

2010) and the Priesil to Inovec fms. (13–12.2 Ma by

Chernyshev et al. 2013) allow us to think in this direction.

This possibility is supported by the absence of andesite clasts

in rhyolite sandstones and conglomerates just as in the base

of the rhyolite interval. However, this can be explained by

the incompleteness of the well core material or by river

avulsion.

In the upper part of the VR–1 well, the content of the stable

material increases upward. Admixture of altered andesite and

rhyolite lithoclasts, including the idiomorphic quartz crystals,

points to recycling of older deposits. Also, less abundant

Fig. 15. Garnet provenance diagram after Suggate & Hall (2014;

G +A+ S = Grossular +Andradite + Schorlomite): a–c — origin in grani-

toide to gneiss: a — granite, b — low Mg gneiss, c — Mg-rich

metapelite or gneiss; d — ?Bt-paragneiss; e — low grade metapelites

(mica schist) to amphibolites; f, g — intermediate to basic rocks:

f — ?meta basite, g — andesite.

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sandstone clasts can be explained by recycling of the older fill,

although the presence of mica with St and Cld intergrowths

(Fig. 12) indicate the first cycle of erosion of mica-schists.

This can be explained by the continued erosion of the base-

ment rock in the volcanic field. In contrast to previous wells,

the presence of the volcanic source in fine-grained, hetero-

lithic sediments of the IV-1 well is documented only by

Grs

9-24

Prp

10-21

Alm

59-69

garnets (Fig. 15) and by rare volcanic

clasts (1760 m).

In the upper part of the wells (Pannonian/Tortonian–

Messianian age), the amount of material derived from cover

and nappe units, as well as from the Neogene volcanics

decreases. On the other hand, the amount of clasts derived

from granitoids increases. The composition of the clast in

the ZM-1, MOJ-1 and IV-1 wells corresponds to the adjacent

parts of the Tribeč Mts. Admixture of well-rounded volcanic

lithoclasts in the ZM-1 well and altered Neogene volcanic

clasts in the IV-1 well indicated continual but already less

significant volcanic provenance and a relatively long trans-

port. The para-conglomerate from the Serravallian–Pannonian

boundary with well-rounded clasts indicates reworking of

underlying sediments. This is manifested by: 1) composition

similarity; 2) presence of intraclasts; 3) presence of chloritized

Bt which was derived from underlying volcanic-rich sedi-

ments (ZM-1); 4) high content of ferric oxide in the heavy

fraction (IV-1) as well as 5) by the presence of Sarmatian (late

Serravalian) allochthonous nanofossils (IV-1, VR-1, ZM-1).

The fine-grained development of the VR-1 well does not allow

comments on the evolution of provenance in the central part of

Komjatice depression.

The composition of the heavy minerals corresponds to

the stated provenance, where the presence of St, Cld, Sil, Tur,

Grs

8-24

Alm

52-83

and Prp

7-18

Sps

29-40

Alm

41-43

garnets indicate ori-

gin in the metasediments and Bt paragneiss of the Tribeč Mts.

The tourmaline zonality from schorl core to dravite rim

(Fe/Fe + Mg = 0.63– 0.26), found in the MOJ-1 well, is opposite

to the zonality described in tourmaline rich horizons from

the Lúžna Fm. of the Tribeč Mts. (Vozárová et al. 2003).

Schorl component increases towards the rim (Fe/Fe+Mg =

0.14– 0.23) in dravite laminas from the basement rocks of

the IV-1 well, just as in the Lúžna Fm. Identical zonality as in

the MOJ-1 well is found in a Tur from schist lithoclast found

in the ZM-1 well (Table 2; Fig. 12). This excludes Tur prove-

nance from the Lúžna Fm. and confirms transport from the NE.

Alm

Sps

(MOJ-1 well) and Prp

11-21

Alm

69-82

garnets (MOJ-1,

IV-1 and VR-1 wells) together with schorls (Fe/Fe+Mg =

0.92–0.94; IV-1) correspond to granitoid provenance. Occur-

rence of magnesio-chromite in the heavy fraction of the IV-1

well points to recycling of the lower part of the Neogene fill,

which contains melaphyre clasts. Grs

9-24

Prp

10-21

Alm

59-69

garnet

probably derived from Neogene volcanic rocks reach the MOJ-1

well and confirm the existing transport direction from the NE.

The presence of rare Hbl in the MOJ-1 well can be derived

from granitoid rocks, but Hbl of similar composition is found

in Neogene volcanic-rich horizons of the ZM-1 well (Šarinová

& Rybár 2018).

The Cretaceous, Paleogene and Badenian fossils (Kováč et

al. 2006, 2008; Ozdínová 2012; Zahradníková et al. 2013; our

results) point to the presence of such sediments in the source

area and/or their recycling. It is possible to speculate, that

Badenian sediments were derived from the SE, for example,

from the northern part of the Želiezovce depression (Kováč et

al. 2018). The Cretaceous and Paleogene sediments may have

formed the cover of the Central Western Carpathian units.

Stratigraphy

The original assignment of sediments based mainly on

benthic foraminifera species as in Biela (1978a), is modified

based on the new results from biostratigraphy and indirect

dating of volcanic material. The assignment of formations is

also affected by determination of the Nemčiňany Fm. and by

genetic redefinition of the Pannonian (Tortonian–Messinian)

sedimentary formations (Sztanó et al. 2016).

Several biostratigraphical markers are applied from the pre-

sented foraminiferal assemblages: the late Badenian (early

Serravallian) Bogdanowiczia pocutica; the Sarmatian (late

Serravallian) Elphidium hauerinum (Fig. 2), Nonion biporus

and also Anomalinoides dividens acme; and the Pannonian

?Trochammina kibleri (Fig. 2). Recorded nannofossil markers

are: the Sarmatian association with Calcidiscus pataecus

(sensu Schütz et al. 2007; Galović & Young 2012; Galović

2017; Fig. 3), Calcidiscus tropicus acme (Fig. 3) together with

rare specimens of Calcidiscus macintyrei; and the Pannonian

Isolithus semenenko and Reticulofenestra tegulata (Fig. 3).

The dinocysts Virgodinium asymmetricum, V. transformis,

Spini ferites bentori pannonicus, S. bentori oblongus, Pontia

dinium pecsvaradensis, P. obesum assigned to the Spiniferites

bentori oblongus Zone (Sütő-Szentai 1988) are used for

the verification of the early Pannonian (Tortonian) age. This is

the most diverse and rich assemblage calibrated with Biochron

~10.8 Ma (Magyar et al. 1999a), Congeria banatica–

Lymnocardium gorjanovici–Gyraulus tenuistriatus Cenozone

(Vrsaljko 1999) and NN9a-b to NN9b Zone (Bakrač et al.

2012).

Upper Badenian–Sarmatian (Serravallian)

The presence of Bogdanowiczia pocutica in the lowermost

part of the MOJ-1 well (2100–2095 m) indicates late Badenian

(early Serravallian) age. The pre-tectonic age of these sedi-

ments is supported by the presence of veins cutting through

mineral grains in the depth of 2046–2050 m (Fig. 6).

The Sarma tian (late Serravallian) age of the following hetero-

lithic sediments (2010–1795 m) is documented by the presence

of algae Halicoryne aff. morelleti and Elphidium hauerinum

with FO in the upper part of the early Sarmatian (sensu Piller

& Harzhauser 2005) in the Paratethys (Cicha et al. 1998).

These results are consistent with Biela (1978a) and the strata

can be assigned to the Vráble Fm. The following coarse-

grained interval from the Sarmatian–Pannonian boundary was

originally assigned to the Sarmatian (Biela 1978a). The newly

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defined, coarse-grained marginal Nemčiňany Fm. (Sztanó et

al. 2016) corresponds to these sediments much better.

The Sarmatian (late Serravallian) age of the basal sediments

from the IV-1 well (2355–1950 m; Biela 1978a) is supported

by the presence of a poor nannofossil assemblage (2315 m)

including Cyclicargolithus floridanus. Its last common occur-

rence can be found at the NN6/NN7 (Martini 1971) zones

boundary. A clear stratigraphic assignment of these deposits

comes from heterolithic sediments that overlie the coarse clas-

tics of the IV-1 well (Figs. 7, 8). Here the NN6 was recognized

in the depth of 2090–2093 m (Zahradníková et al. 2013).

Moreover, the Sarmatian age of these sediments is supported

by the presence of Halicoryne aff. morelleti and Elphidium

hauerinum (2093–2040 m), as well as by Bolivina sarmatica

in the depth of 1961–1956 m.

In the case of the VR-1 well, non-volcanic conglomerate

from the base of the Neogene fill was originally assigned to

the middle Badenian (Langhian), while volcanic conglome-

rates and sandstones were assigned to the late Badenian

(Serravallian; Biela 1978a). These assignments were based on

benthic foraminiferal assemblages in the overlaying sediments.

In this study, the first abundant, but poorly preserved marine

nannofossils and dinocyst ?Cleistosphaeridinium placa

canthum from the depth of 1801–1804 m indicates late

Badenian–Sarmatian (Serravallian) age. The Sarmatian age

(NN6; 1750–1203 m), has been set based on a small Calci

discus resembling C. pataecus? and higher numbers of Calci

discus species starting to appear in the depth of 1745–1750 m

including the C. tropicus acme (1203 m; Suppl. 1). Within

the foraminifera assemblage the Anomalinoides dividens acme

(1745–1750 m), indicates the base of marine Sarmatian

sediments. Occurrence of Nonion biporus with Elphidium

hauerinum (up to 1250 m) supported this assignment.

However, biostratigraphic sterility of underlying sediments

(~1850 m–2300 m) can be explained by the dominance of

coarse- grained volcanic material. In addition, the present vol-

canic material indicates Sarmatian age. Rhyolite clasts which

appear from the depth of 2207 m (Figs. 6, 10) can be linked to

the Jastrabá Fm. outcropping NE of Nová Baňa town (Fig. 1).

This interpretation is suggested by the presence of the rhyolite

conglomerate occurring near Tekovské Nemce village.

Original dating of rhyolites in the vicinity of Nová Baňa town

yield a cooling age of 14.4 ± 0.5 Ma from Bt and 13.8 ± 0.3 Ma

from volcanic glass (Repčok 1981 in Konečný et al. 1998).

New K/Ar dating of rhyolites from the vicinity of Nová Baňa

yield an age of 12.31 ± 0.44–12.03 ± 0.38 Ma, with a mean of

12.19 Ma (Lexa & Pécskay 2010). Nevertheless, the latest

K/Ar and Rb/Sr dating for the whole Jastrabá Fm. is in

the interval between 12.2 ± 0.8 and 11.4 ± 0.4 Ma (Chernyshev

et al. 2013). Additionally, the Sarmatian (late Serravallian) age

of these sediments is supported by the high content of ande-

sitic material in the overlaying sediments (2055 m and above).

In this depression, andesites of the 4

stage of the Štiavnica

stratovolcano (especially Priesil Fm.) formed an elevation on

the surface. In the past, the Priesil and Inovec Fm. were

assigned to the late Badenian–Sarmatian (intra Serravallian)

boundary (Konečný et al. 1998). The new absolute dating by

K/Ar and Rb/Sr indicates an age of 13–12.2 Ma (Chernyshev

et al. 2013), although the authors discussed age ranges from

12.7 to 12.2 Ma. The age limits of both Jastrabá and Priesil

fms. do not contradict the observed sedimentary record and

indicated a Sarmatian (late Serravallian) age of these deposits.

Presence of poorly preserved nannofossils indicating late

Badenian age (1801–1804 m), can be explained by recycling

of older strata during opening of the depression accompanied

by volcanic activity. The sandy, gravity flow character of

the deposits connected with rapid sedimentation, tectonic

activity and volcanism supports this fact. According to this

point of view, the non-volcanic conglomerates from the basal

part of the Neogene fill are older than 12.2 Ma.

The base of the Neogene fill in the ZM-1 well is questio-

nable and cannot be commented because of lack of core

samples. The question about the assignment of the non-meta-

morphosed sandstones from the interval 1904–1804 m remains.

Gaža & Beinhauerová (1976) assign these rocks to the Carbo-

niferous and Biela (1978a) describes a core fragment from

a depth of 1900 m as a possible Pre-Cenozoic rock. The fol-

lowing ochre and brick-red coloured arkosic sandstones

(1590 m), which were marked as Permian (Gaža & Bein-

hauerová 1976) were not found in the repository. However,

based on presence of the mottled mudstones (Fig. 11) and

other structures typical for an alluvial environment (1553–

1558 m) it is likely, that the colouring was caused by pedo-

genesis, and not by Permian arid deposition. The presence of

micritic carbonate clasts (1711 m) is also not typical for

the composition of the Permian sediments of the Hronic unit

(Vozárová & Vozár 1988). As suggested by Biela (1978a),

similar lithological composition of samples from the depth of

1711–1448 m supports this view and points to the Neogene

age. However, these sediments are biostratigraphically barren.

A Cenozoic age is indicated by a poor nannofossil assemblage

(1555–1551 m). Although the first foraminifera tests are

observed in the depth of 1405–1410 m, biostratigrafical

markers such as Nonion communis, Bulimina elongata and

Uvigerina semiornata are present no sooner than at the depth

of 1351 m. Extremely high content of pyrite and molds with

small remains of dissolute, calcareous tests indicate that

the assemblage represents only a fraction of the original asso-

ciation. According to the present foraminifera markers in

the upper parts of the well, a late Badenian association typical

for “agglutinated zone” is assumed. The dinocysts Melita

sphaeridium choanophorum and Cleistosphaeridinium placa

canthum from this depth (1351 m) can be correlated with

the NN6 Zone. Dominance of Bolivina dilatata maxima

(1258–1046 m) is typical for the late Badenian. However,

fragmented tests, signs of dissolution (1255 m, 1051 m) and

size sorting of smaller forams suggest reworking from

the older late Badenian strata. Presence of the NN6 Zone in

the depth of 400–1200 m was first mentioned by Ozdínová

(2012). This is consistent with the presented results, where

calcareous nannofossils showed the NN6 Zone (1351–1201 m).

Late Badenian affinity is based on the common Calcidiscus

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premacintyrei, Helicosphaera walbersdorfensis, H. wallichii,

Sphenolithus abies, Reticulofenestra pseudoumbilicus, Umbi

lico sphaera rotula, Holodiscolithus macroporus, Braarudo

sphaera bigelowii bigelowii (Suppl. 1). Numerous poorly

preserved Calcidiscus in the depth of 1051–1046 m indicate

a Sarmatian age. Redeposition of fossil assemblages is sup-

ported by observed slump structures and intraclasts (1051–

1000 m; Fig. 11). Apart from biostratigraphy, indirect dating

of volcanic material was possible. Based on the texture and

mineral composition, the Bt–Amp ± Px andesite to dacite from

coarse-grained conglomerates (1350 and 1100 m) is assigned to

the Studenec Fm. (Figs. 6, 11). Original dating of the Studenec

Fm. by K/Ar method was set to 15.2 ± 0.1 Ma (Konečný et al.

1969 in Konečný et al. 1998) and by the FTA method to

14.8–16.4 Ma (Repčok 1978, 1979, 1980, 1981 all in Konečný

et al. 1998). These ages did not line up with biostratigraphy

(Konečný et al. 1998). Nonetheless, the new K/Ar and Rb/Sr

data yield an age of 13.1 ± 0.3 Ma to 12.4 ± 0.1 Ma (Chernyshev

et al. 2013); although the authors discuss an age range of

13.1–12.7 Ma. In the ZM-1 well, only the altered, rusty-brown

volcanic lithoclasts from the chaotic conglomerate (1051–

1005 m) can be assigned to the 4

stage of the Štiavnica strato-

volcano evolution (Šarinová & Rybár 2018; Figs. 6, 11) with

an age of 12.7–12.2 Ma (Chernyshev et al. 2013). Based on

the above mentioned information, the late Badenian–Sarmatian

(Serravallian) age of this volcanosedimentary interval can be

considered, in contrast to the original assignment (Gaža &

Beinhauerová 1976; Biela 1978a). Nonvolcanic terrestrial

sediments from the basal part are older than 12.7 Ma.

The actual stratigraphy (Vass 2002) assigned the late

Badenian (early Serravallian) sediments to the Pozba Fm. and

Sarmatian (late Serravalian) sediments to the Vráble Fm., both

with littoral to shelf character. The formations defined based

on their age are difficult to use, especially when the NN6 Zone

is typical for both formations. In addition, environments are

normally time transgressive, therefore genetically-defined

formations are more suitable for interpretations. Because of

the impossibility of the strict separation of the marine sedi-

ments into the Pozba and Vráble formations, they are included

in the merged Vráble–Pozba Fm. (Fig. 16). The actual defini-

tion (Vass 2002) does not include the underlying alluvial sedi-

ments. For the alluvial to fluvial sediments a new formation is

defined, with the name adopted from the stratotype section in

the Zlate Moravce-1 well = Zlaté Moravce Formation.

The Zlaté Moravce Formation

Lithology, facies: The Zlaté Moravce Fm. is dominantly

built up by grey mudstones, which are cut and filled by light

coloured conglomerates and sandstones. Red mottles, synsedi-

mentary folds, and carbonized plant fragments are common

(Fig. 14). Muddy horizons with red mottles and abundant car-

bonized plant fragments are interpreted as swamps or oxbow

lakes. Polymict conglomerate and sandstone are fine-grained,

poorly rounded and composed mainly of Qz-, Qz-sericitic and

carbonate shale lithoclasts. Altered granitoids to meta-granitoids

meta-greywacke, meta-arkose, chert/felsite, quartz arenite,

arkose, wacke, carbonates, Fsp, Bt and rare melaphyre are also

included. In the upper part, Neogene volcanic lithoclasts start

to appear. Presence of normal gradation, imbrications and ero-

sive surfaces points to deposition by traction currents. These

features clearly coincide with an alluvial environment, which

is partly supported by the cyclic character of the well logs

(Fig. 13).

Stratigraphic position, thickness: The thickness is more

than 270 m in the ZM-1 well and 160 m in the VR-1 well

(depth 2300–2454 m). The formation overlies pre Cenozoic

basement and passes into the marine Vráble-Pozba Fm. of late

Badenian–Sarmatian (Serravalian) age.

Fossils, age: The sediments are biostratigraphically barren.

The assumed age is Serravallian which is derived from

the cor re lation with the syn-rift packet defined on the seismic

lines 3/99 (Šályová & Mojžiš 2002) and 820/00 (provided by

Equis l.t.d).

Depositional environments: The Zlaté Moravce Fm. repre-

sents terrestrial sediment which was deposited on an alluvial

fan. These sediments continually pass into a fan delta environ-

ment belonging to the Vráble–Pozba Fm., what is documented

by marine fossils. In this context, the Zlaté Moravce Fm.

represents a proximal facies of the newly opened depocenters

(Komjatice, ?Rišňovce, ?Gabčíkovo depressions).

mudstone,lignite, sand and conglomerate (alluvial, fluvial)

a mudstone and sandstone

)

(shelf

b.conglomerate, sandstone (mass gravity flow)

(para)conglomerate, sandstone mass gravity flow

(

)

(

)

claystone, mudstone, siltstone deep lake

b. mudstone, sandstone (mass gravity flow)
c claystone, mudstone (slope progradation)

mudstone, lignite, sand deltaic

(

)

mudstone, sandstone (alluvial)

c mudstone, minor sandstone (slope progradation)

bentonite, volcanic conglomerate and sandstone

Fig. 16. Lithostratigraphy of the Komjatice depression.

406

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GEOLOGICA CARPATHICA

, 2018, 69, 4, 382–409

Representative outcrops and wells: The stratotype section

can be found in the ZM-1 well (1440–1711 m). The material

can be found in the repository of Nafta a.s. in Gbely town.

This formation is also recognized in the basal part of the VR-1

well, but unfortunately no core material is available in the

repository today.

Pannonian (Tortonian–Messinian)

The Pannonian (Tortonian–Messinian) age of the sedimen-

tary record was originally recognized by Biela (1978a). This

study refines the conclusion based on the Pannonian

(Tortonian) Reticulofenestra tegulata (1603–1612 m in IV-1;

1005–1010 m in ZM-1) and Isolithus semenenko acme

together with the lowermost occurrence acme of ?Trochammina

kibleri (1154 m of VR-1 well). The acme of Reticulofenestra

tegulata in the ZM-1 well is in contradiction with the original,

Sarmatian age (Biela 1978a). In this case, a younger, Pannonian

age is also supported by an erosional unconformity, significant

change in provenance and by a high degree of weathering.

Pannonian dinoflagellates are present in the ZM-1 (658–551 m),

IV-1 (up from 1763 m) and VR-1 wells (up from 1050 m).

In the VR-1 well, a dinoflagellate association can be correlated

with the NN9ab–NN9b Zone (755–603 m; Suppl. 1). This age

range is consistent with a 9.62 ± 0.57 to 9.14 ± 0.57 Ma age

based on

Be/

Be dating from overlying sediments (555–505 m;

Šujan et al. 2016).

The new assignment of the formations is affected by intro-

duction of the Nemčiňany Fm. and by genetic redefinition of

the Pannonian (Tortonian–Messinian) sedimentary formations

(Sztanó et al. 2016; Fig. 16). The Nemčiňany Fm. is defined as

basal, coarse-grained braided river to fan delta deposits repre-

senting pre-trangressive facies in marginal parts of Lake

Pannon. In the studied wells, the para-conglomerate and other

coarse-grained sediments from the Sarmatian–Pannonian

(Serravallian–Tortonian) boundary are assigned to the Nemč i-

ňany Fm. (Figs. 4, 7, 13, 16). In the past, these sediments were

often assigned to the upper part of the Vráble Fm. (MOJ-1,

ZM-1; Biela 1978a). It was caused by recycling or by fossil

sterility of the coarse-grained sediments, as well as by an

incorrect division of the underlying, volcanic sediments (ZM-1).

The time span of the Nemčiňany Fm. was determined by

Be/

Be dating from the Nemčiňany outcrop in the time span

of 11.72 ± 0.88 to 11.21 ± 1.23 Ma and from the ŠVM-1 well

(Fig. 1) in the time span of 11.23 ± 0.84 to 9.92 ± 0.63 Ma

(Šujan et al. 2016). In the central part of the depression (VR-1)

the Nemčiňany Fm. is not present, but the Sarmatian–

Pannonian (Serravallian–Tortonian) boundary (1208–1149 m)

is characterized by well preserved pollen and no dinocysts,

which indicates marginal conditions. Only the brackish lacus-

trine sediments without presence of terrestrial facies are

assigned to the Ivanka Fm. (Sztanó et al. 2016). This environ-

ment is supported by Isolithus semenenko acme, as well as by

the dinoflagellate assemblages. Additional evidence comes

from prevailing fine-grained lithology and from prograding

clinoforms observed on the reflection seismic lines 3/99

(Šályová & Mojžiš 2002) and 820/00 (provided by Equis

l.t.d). The change in grain size, which is also reflected in

the SP and RT log, indicates a change in deposition. At this

boundary, the deltaic deposition of the Beladice Fm. (Sztanó et

al. 2016) begins.

Discussion

The older interpretation of this area considered a wide age

range of the sedimentary fill (from middle Badenian to

Sarmatian/Langhian–Serravalian; Gaža & Beinhauerová 1976;

Biela 1978a; Hók et al. 1999 and others). The new indirect age

data based on volcanic material are inconsistent with older

interpretations. The new assignment is consistent with biostra-

tigraphy, if it is noted that the coarse grained gravity flow

character of deposits caused biostratigraphic sterility or

reworking of fossils. According to Hók et al. (1999) the late

Badenian to Sarmatian (Serravallian) sediments belong to one

depositional event, with continual transition from terrestrial to

marine environment (ZM-1, Vr-1 wells). The same facies are

older in the NE and younger in the SW, which is supported by

the presented provenance and biostratigraphic analysis.

Presence of late Badenian (early Serravallian) sediments in

the E (SE) can be explained by gradual tectonic opening of

the depression. In the late Badenian, the Komjatice depression

was not yet open. The deposition in the study area was proba-

bly connected to the margin of the older Želiezovce depres-

sion. The main phase of the deposition is associated with

opening of the depression in simple shear tectonic regime

(Hók et al. 2016). This led to the widening and deepening of

the depositional environment followed by rapid deposition.

Moreover, the syn-rift cycle is nicely observed on the reflec-

tion seismic line 820/00, which cuts through the VR-1 and

seismic line 3/99 (Šályová & Mojžiš 2002). Since the extent of

the Sarmatian (Serravallian) sediments is limited by the Moj-

mírovce fault system (Biela 1978a; Hók et al. 1999), the sea

level did not reach the top of the footwall. The total thickness

of the Sarmatian (Serravallian) sediments in the central part of

the depression reaches more than 1100 m (VR-1). It is similar

to the thickness of the Sarmatian sediments in the adjacent

Rišňovce depression (Fordinál & Elečko 2000). In contrast,

the Želiezovce depression contains lower Badenian (Lan ghian)

sediments and only a low thickness of late Badenian–

Sarmatian (Serravallian) deposits (e.g., Kováč et al. 2018).

The Sarmatian–Pannonian (Serravallian–Tortonian) boun-

dary is erosive. The increase of water level during the Pannonian

(Tortonian) is manifested by the deposition of coarse clastics

of the Nemčiňany Fm. in marginal parts of the depression

(Fig. 16). The deepwater environment of the Ivanka Fm. was

sustained by further tectonic subsidence on the Mojmírovce

Fault system (e.g., Gaža & Beinhauerová 1976; Hók et al.

1999). The cessation of the water level rise led to a gradual

filling up of the depression (Fig. 16). The sedimentation of

the deltaic Beladice Fm. and alluvial Volkovce Fm. followed

(Fig. 16). The widespread Pannonian sediments are no longer

407

KOMJATICE DEPRESSION — INTEGRATED BIOSTRATIGRAPHY, SEDIMENTOLOGY AND PROVENANCE ANALYSIS

GEOLOGICA CARPATHICA

, 2018, 69, 4, 382–409

limited by the Mojmírovce fault system (Biela 1978a; Hók et

al. 1999).

Conclusion

Combination of new results from biostratigraphy and indi-

rect dating of volcanic material brought changes to the assign-

ment of the sedimentary record especially in the VR-1 and

ZM-1 wells. In contrast to previous studies (Gaža &

Beinhauerová 1976; Biela 1978a; Harčár et al. 1988; Hók

1999; Vass 2002) and in agreement with Szatnó et al. (2016)

the formations are defined by their genetic origin. The new

stratigraphic assignment of the Komjatice depression can be

defined as follows (Fig. 16):

• Zlaté Moravce Fm.: a newly defined formation containing

alluvial deposits. The late Badenian–Sarmatian (Serravalian)

age is set based on its stratigraphic position. The Zlaté

Moravce Fm. represents the base of sedimentary fill linked

to initial opening of the depression.

• Vráble–Pozba Fm.: Late Badenian–Sarmatian (Serravalian)

age is documented by biostratigraphical markers and by

indirect dating of volcanic rocks. The deposition of marine

sediments is connected with the tectonic opening of

the depression.

• Nemčiňany Fm.: contains coarse-grained sediments from

the Sarmatian–Pannonian (Tortonian–Serravallian) boun-

dary. The most visible trend of erosion and recycling is

observed in the eastern part of the depression (ZM-1 well).

• The following Pannonian (Tortonian–Messinian) forma-

tions are divided based on their lithology, fossil assem-

blages, well log patterns and seismic reflection character

into: the predominantly fine-grained Ivanka Fm. (basin

floor to slope); the sandy deltaic Beladice Fm., and the pre-

dominantly muddy, alluvial Volkovce Fm.

The main transport direction in the late Badenian–Sarmatian

(Serravallian) time was from the NE to SW and the prove-

nance area contained Paleozoic rocks from the Hronic unit and

subsequently also Neogene volcanic rocks. The length of

transport was short in the eastern part and increased towards

the west. During the Pannonian (Tortonian–Messinian) time,

the main provenance area was located in the Tribeč Mts.,

although the direction of transport from the E remained.

Acknowlegements: This research was supported by the Slovak

research and development agency under the contracts No.

APVV-16-0121, APVV-0099-11, APVV-15-0575 & APVV-

14-0118. The authors wish to express their gratitude to the Mana-

gement of Nafta petroleum company and to Dr. Sliva for

allowing access to the well-core repository; to the Equis ltd.

for providing data (seismic line 820/00); to Dr. Bakrač and

Dr. Soliman for dinoflagellate taxonomy discussion;

Dr. Teodoridis for leaf taxonomy discussion; and to Dr. Kostič

for assistance with the QUANTA FEG 250. We express our

gratitude to the editor and to the reviewers for their insightful

comments which improved the manuscript.

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, 2018, 69, 4, 382–409

Supplement

Suppl. 1. Key biostratigraphic data: foraminifera (F), nannofossils (N) and palynomorfs include dinoflagellata (P).

U. Badenian = early Serravallian; Sarmatian = late Serravallian; Pannonian = Tortonian–Messinian; a) MOJ-1 well; b) IV-1 well;

c) VR-1 well; d) ZM-1 well.

a) Mojmírovce 1 well (MOJ-1)

Depth (m)

Core

Discipline

Zone / Subzone

Event

848–854

8/1/15cm

Unassigned

Barren

848–854

8/1/ 75cm

Unassigned

Barren

848–854

8/2/50cm

Unassigned

Barren

Other

Rhizoids

902–907

9/1/65cm

Unassigned

Barren

Other

Fe oxides

955–960

10/2/ 90cm

Unassigned

Reworked: Lenticulina sp., Globigerinella obesa

Other

Fe oxides, coal

955–960

10/3/75cm

Unassigned

Barren

Other

?Crab excrements, coal, Fe oxides

955–960

10/3/95cm

Unassigned

Barren

Other

Rhizoids

1000–1005

11/1/30cm

Unassigned

Barren

Other

Ostracod shells–also articulated, coal

1253–1261

16/1/55cm

Unassigned

Barren

1253–1261

16/3/50cm

Unassigned

Barren

1253–1261

16/6

Unassigned

Barren

1253–1261

16/7/30cm

Unassigned

Barren

Other

Gastropoda and Ostracoda fragments

1298–1303

17/1/25cm

Unassigned

Barren

Other

Coal

1298–1303

17/2/40cm

Unassigned

Barren

Other

1298–1303

17/3/40cm

Unassigned

Barren

Other

1298–1303

17/5/30cm

Unassigned

Barren

Other

Fe oxides

1351–1354

18/1–2/50

Unassigned

Barren

Other

1397–1401.5 19/1/60cm

Unassigned

Barren

Other

Ostracoda fragments

1397–1401.5 19/3/25cm

Unassigned

Barren

1451–1455

20b/2/50

Unassigned

Barren

Unassigned

Barren

Other

Ostracoda fragments, fish bones

1500–1511

21/2–3/50

Unassigned

Barren

Other

Coal

1500–1511

21/4–5

Unassigned

Barren

1795–1798

27/2–3/ 50

Unassigned

Barren

Sarmatian

Elphidium sp.

1847–1851

28/1–2

Sarmatian

Elphidium sp., E. josephinum, E. aculeatum, Ammonia parkinsoniana, Miliolidae

1847–1851

28/3–4/50

Sarmatian

Elphidium hauerinum, Aubignyna perlucida, Bolivina spp., Porosonion, Fissurina, Miliolidae

Unassigned

Phytoclasts, opaque

Other

Coal rest, Fe oxides

1905–1910

29/2–4

Unassigned

Barren

Other

Organic matter (algae)

2005–2010

Unassigned

Barren

Unassigned

Barren

Other

Dasycladacea Halicoryne aff. morelleti

2046–2051

32/4–5

Unassigned

Barren

Other

Rhizoids

2095–2100

33/1–2/50

Late Badenian

Bogdanowiczia pocutica (Bathysiphon pocutica)

KOMJATICE DEPRESSION — INTEGRATED BIOSTRATIGRAPHY, SEDIMENTOLOGY AND PROVENANCE ANALYSIS

GEOLOGICA CARPATHICA

, 2018, 69, 4, 382–409

b) Ivanka 1 well (IV-1)

Depth (m)

Core

Discipline

Zone / Subzone

Event

1506–1509

3/2/ 65cm

Unassigned

Barren

Pannonian

Virgodinium asymmetricum, Spiniferites bentori pannonicus, Impagidinium spongianum

1506–1509

3/3/ 50cm

Unassigned

Barren

Other

Gastropoda and ostracoda fragments, fish bones

Pannonian

Achomosphaera sp., Spiniferites bentori pannonicus, Impagidinium spongianum, Pontiadinium

pecsvaradensis

1603–1612

5/3

Pannonian

Reticulofenestra tegulata, Braarudosphaera bigelowii, B. bigelowii parvula and allochthonous

Cyclicargolithus floridanus, Reticulofenestra bisecta

Pannonian

Virgodinium asymmetricum, Spiniferites bentori pannonicus

1758–1763

8/2/

25cm

?Pannonian

Virgodinium sp., Spiniferites ssp., + Spirogyra, Zygnema, Ovoidites

1956–1961

12/3/50cm

Sarmatian

Bolivina sarmatica, Bolivina spp., Porosonion ex. gr. granosum

Other

Fish bones

1956–1961

12/4/50cm

Barren

Other

Organic matter, plant debris

1956–1961

12/5/50cm

Sarmatian

Ammonia tepida, Bolivina spp., Nonion spp., Miliolidae, reworked

Other

Dasycladacea Halicoryne aff. morelleti

1956–1961

12/6/80cm

Unassigned

Barren

2010–2015

13/4/50cm

Unassigned

Barren

2040–2045

14/1/65cm

Sarmatian

Nonion tumidulus, Miliolidae, Ammonia parkinsoniana, Elphidium sp., Streptochilus

Other

Acritarcha: Pterospermella sp., Dasycladacea Halicoryne aff. morelleti, pollen

2040–2045

14/2/45cm

Sarmatian

Nubecularia crasraformis, Nonion spp., Bolivina spp., Miliolidae, Haynesina depressula,

Elphidium sp.

2090–2093

15/1/50cm

Sarmatian

Ammonia tepida, Elphidium sp., Nonion spp., Miliolidae

reworked: Cassigerinella globulosa, Haplophragmoides sp.

Unassigned

Barren redep. ?Deflandrea (paleogene dino)

Other

Sponge spicules, Fe oxides, pyrite,

2090–2093

15/2/65cm

Unassigned

Barren

Unassigned

Barren

Other

Fish scales, coal, Fe oxides

2090–2093

15/3/30cm

? Sarmatian

Porosonion ex. gr. granosum, Miliolidae

Unassigned

Barren

Other

Organic matter

2158–2163

16/2/50cm

Unassigned

Barren

Other

Organic matter

2158–2163

16/3/50cm

Unassigned

Barren

Other

Organic matter

2274–2276

19/1/50cm

Unassigned

Barren

Other

Mollusca fragments

2311–2316

20/31

Unassigned

Braarudosphaera bigelowii, B. bigelowii parvula, Coccolithus pelagicus, Cyclicargolithus

floridanus, Reticulofenestra bisecta, R. haqii, R. pseudoumbilicus, Sphenolithus moriformis

Eocene, Oligocene redeposits Coccolithus formosus and Pontosphaera latelliptica

iii

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

GEOLOGICA CARPATHICA

, 2018, 69, 4, 382–409

c) Vráble 1 well (VR-1)

Depth (m)

Core

Discipline

Zone/Subzone

Event

603–607

3/3

Pannonian/

Tortonian/

NN9a-b

Virgodinium asymmetricum, Pontiadinium pecsvaradensis

703–707

5/1

Pannonian/

Tortonian/ NN9a-b

Virgodinium asymmetricum, V. transformis, Pontiadinium pecsvaradensis, Impagidinium

spongianum,

750–755

6/1

Pannonian/

Tortonian/ NN9a-b

Virgodinium asymmetricum, V. transformis, Impagidinium spongianum, Spiniferites bentori

pannonicus, Spiniferites bentori oblongus, Achomosphaera sp.

802–807

7/1

Pannonian/Tortonian/

NN9a-b

Virgodinium asymmetricum, V. transformis, Spiniferites bentori pannonicus, Spiniferites bentori

oblongus

802–807

7/2

Pannonian/

Tortonian/ NN9a-b

Virgodinium asymmetricum, V. transformis, Spiniferites bentori pannonicus, Spiniferites bentori

oblongus, Pontiadinium pecsvaradensis, P. obesum + Spirogyra, phytoclasts,

-corr. S.b.oblongus Biochron 10.8 Ma (Magyar et al 1999), Central Paratethyan Spiniferites

bentori oblongus zone (Suto-Szentai 1988) middle early Pannonian s.l.

802–807

7/4

Pannonian/Tortonian/

NN9a-b

Spiniferites bentori pannonicus, Spiniferites bentori oblongus, Pontiadinium pecsvaradensis,

P. obesum, V. transformis

900–905

9/1/ 40cm

Pannonian/Tortonian/

NN9a-b

Achomosphaera sp., Virgodinium asymmetricum, Pontiadinium pecsvaradensis, Spiniferites

bentori pannonicus, Spiniferites bentori oblongus

-corr. S.b.oblongus Biochron 10.8 Ma (Magyar et al 1999), Central Paratethyan Spiniferites

bentori oblongus zone (Suto-Szentai 1988) middle early Pannonian s.l.

950–955

10/1/ 50cm

Different palynofacies, more terrestrial and freshwater elements (Zygnema), aquatics (Nuphar),

plus redepozited dinoflagellata (e.g. Deflandrea); no dinocyst

950–955

10/4/ 50cm

Small ungular organic remnants, no dinocyst

950–955

10/3

Unassigned

Poor sample, Cyclicargolithus floridanus, Reticulofenestra pseudoumbilicus

1000–1005

11/1/ 50cm

Pannonian

Dinoflagellata div.gen. et sp.

1103–1108

13/1/50cm

Pannonian

Isolithus semenenko, Coccolithus miopelagicus, Cyclicargolithus floridanus, Calcidiscus?,

Ascidian spicules, Reticulofenestra sp.,

Panonnian

Milliammina fusca, M. subvelatina, Dogiellina sp.

Other

Fish remains, shark teeth

1103–1108

13/2/ 50cm

Dinoflagellata div.gen. et sp.

1103–1108

13/4

Unassigned

Barren

1149–1154

14/1/50cm

Pannonian

Coccolithus pelagicus, C. miopelagicus, Cyclicargolithus floridanus, Calcidiscus tropicus,

C. pataecus, Helicosphaera carteri, Rhabdosphaera sp., Umbilicosphaera rotula,

Reticulofenestra pseudoumbilicus, Acme Isolithus semenenko, reworking: Coccolithus

formosus, Microrhabdulus decoratus

Dogielina sp., poorly preserved Miliammina ovata, M. subvelatina, undeterminable

agglutinated foraminifera

Other

Fish teeth, Ostracoda shells

1149–1154

14/2/50cm

?Pannonian/

?Sarmatian

?NN6

Reticulofenestra pseudoumbilicus, Umbilicosphaera jafari, ?Isolithus semenenko, ABN

Coccolithus pelagicus, Reticulofenestra haqii, Cyclicargolithus floridanus, Paleogene

reworking Reticulofenestra bisecta, Pontosphaera latelliptica, Cretaceous reworking

Agglutinated foraminifera, Dogielina sp., Miliammina velatina, M. subvelatina

Rare organic remnants

Other

Ostracoda shells

1149–1154

14/3/50cm

?Pannonian/?Sarmatian

?NN6

Coccolithus pelagicus, C. miopelagicus, Cyclicargolithus floridanus, Reticulofenestra haqii,

Zygrhablithus bijugatus, Paleogene and Cretaceous reworking

Pannonian

?Trochammina kibleri, Dogielina sp.

Other

Fish teet, Ostracoda shells, pyrite concretions strongly prevails

1203–1208

15/1/50cm

NN6

Sarmatian

Coccolithus pelagicus, C. miopelagicus, Cyclicargolithus floridanus, Braarudosphaera

bigelowii parvula, Calcidiscus tropicus, C. pataecus?, Discoaster deflandrei,

R. pseudoumbilicus, Pontosphaera multipora, Sphenolithus abies, Paleogene discoaster

D. lodoensis, Pontosphaera latelliptica,

Ammonia tepida, Elphidium sp., Sinuloculina consobrina, reworked Badenian foraminifera

tests

Well preserved pollen, no dinocyst

Other

Carbonized floral rests, pyrite, fish bones, polens

1250–1255

16/1/50cm

NN6

Sarmatian

Coccolithus pelagicus, Calcidiscus tropicus, C. macintyrei?, C. premacintyrei, C. pataecus,

Pontosphaera latelliptica, Coccolithus miopelagicus, R. bisecta, Helicosphaera wallichii

2 specimens of Foraminifera tests Elphidium and Ammonia

Other

Coal, organic linnigs, dasycladaceans, fish bones

1250–1255

16/2/50cm

Sarmatian

Calcidiscus tropicus, C. pataecus, C. macintyrei, Braarudosphaera bigelowii parvula

1250–1255

16/3/45cm

NN6

Sarmatian

Calcidiscus tropicus, C. pataecus, C. leptoporus, Reticulofenestra pseudoumbilicus,

Sphenolithus abies

Barren

Other

Coal, fish bones

1250–1255

16/4/50cm

NN6

Sarmatian

Coccolithus pelagicus, Calcidiscus, C. tropicus, C. pataecus

Barren

1250–1255

16/4

NN6

Sarmatian

Coccolithus pelagicus, Calcidiscus, C. tropicus,

1304–1309

17/1/20cm

Unassigned

Poor sample, Coccolithus pelagicus

Autochtonnous can be test of Ammonia and Cibicides boueanus, Lower Miocene reworked

foraminiferal tests as Cassigerinella, Globigerina sp. and Nonion sp.

Other

Coal

1304–1309

17/5/20cm

NN 6

Sarmatian

Coccolithus pelagicus, Helicosphaera carteri, Calcidiscus, C. tropicus, C. leptoporus,

Sphenolithus abies, Reticulofenestra pseudoumbilicus

Autochtonnous can be tests of Ammonia Miocene reworked foraminiferal tests of big diameters

Cassigerinella, Globigerina sp. and Nonion sp

KOMJATICE DEPRESSION — INTEGRATED BIOSTRATIGRAPHY, SEDIMENTOLOGY AND PROVENANCE ANALYSIS

GEOLOGICA CARPATHICA

, 2018, 69, 4, 382–409

Depth (m)

Core

Discipline

Zone/Subzone

Event

1350–1355

18/2/50cm

NN6

Sarmatian

Coccolithus pelagicus, Calcidiscus tropicus, C. macintyrei, C. leptoporus?, C. patecus?,

Rhabdosphaera sp., Reticulofenestra pseudoumbilicus, Sphenolithus abies, Braarudosphaera

bigelowii bigelowii, Pontosphaera latelliptica, Prediscosphaera cretacea

Sarmatian

Ammonia tepida macrospheric, Elphidium macellum, E. josephinum, E. hauerinum

Other

Pyrite, Ca concretions, fish bones, coal

1350–1355

18/3/50cm

Unassigned

Barren

Sarmatian

Elphidium josephinum, Ammonia tepida, Porosinonion ex. gr. granosum, rare Badenian

redeposites

Other

Ca and Fe concretions, fish scales

1350–1355

18/4/50cm

Unassigned

Barren

Unassigned

Barren

Other

Coal

1405–1409

19/1/50cm

Unassigned

Barren

Unassigned

Barren

1405–1409

19/2/25cm

Unassigned

Barren

Sarmatian

Autochtonnous Nonion biporus, O/M redeposites

other

Pyritized valves of diatomace

1405–1409

19/2/80cm

NN6

Sarmatian

Acme Calcidiscus, C. tropicus + Coccolithus pelagicus

Unassigned

Barren

1405–1409

19/4/45cm

NN6

Sarmatian

Coccolithus formosus, Calcidiscus tropicus, C. premacintyrei, C. pataecus, C. leptoporus?

Discoaster variabilis?, Lanternithus minutus

Unassigned

Barren

Other

Coal

1405–1409

19/5/50cm

NN6

Sarmatian

Coccolithus pelagicus, Calcidiscus tropicus, C. premacintyrei

Unassigned

Small tests of foraminifera, probably all reworked Globigerina sp. div., Bulimina elongata

Other

Organic matter

1450–1455

20/2/10cm

Unassigned

Barren

Unassigned

Very bad preserved miliolidae foraminiferal tests

Other

Coal

1450–1455

20/3/10cm

Unassigned

Barren

Unassigned

Porosonion granosum, Ammonia parkinsoniana, Elphidium macellum

Other

Organic matter

1450–1455

20/4/50cm

Unassigned

Barren

Other

Organic matter

1450–1455

20/5/50cm

Unassigned

Barren

Nonion sp. indet

Other

Coal, organic matter, dasycladacea Halicornia sp.

1450–1455

20/8/50cm

Unassigned

Barren

Unassigned

Very rare reworked planktic foraminiferal tests as Globigerinita uvula

1505–1510

21/2/50cm

NN6

Sarmatian

Acme Calcidiscus, C. tropicus + C. pataecus?

Unassigned

Elphidium macellum, reworked globigerinids

Other

Coal

1505–1510

21/3/50cm

NN6

Sarmatian

Acme Calcidiscus, C. tropicus, C. leptoporus, Reticulofenestra pseudoumbilicus, R. haqii,

Reticulofenestra sp., Braarudosphaera bigelowii parvula, Coccolithus pelagicus, Paleogene,

C. formosus

Sarmatian

Cycloforina badenensis, Ammonia tepida, Elphidium josephinum, E. macellum, Porosononion

granosum, reworked planktic foraminiferal tests

Other

Coal, sponge spines

1505–1510

21/4/50cm

NN6

Sarmatian

Acme Calcidiscus, C. tropicus, Reticulofenestra pseudoumbilicus, Coccolithus pelagicus

Massive portion of reworked ?Upper Badenian foraminiferal benthos

Other

Fe crusts, organic matter

1550–1555

22/1/50cm

Unassigned

Poor sample, Coccolithus pelagicus, lots of organic matter

1550–1555

22/2/50cm

Unassigned

Poor sample, Coccolithus pelagicus, Cyclicargolithus floridanus, Reticulofenestra haqii,

R. pseudoumbilicus, lots of organic matter

Ammoniana tepida, Nonion sp., Globigerina sp.

Other

Organic matter, ostracods, porifera spines, dasycladacea Halicoryne aff. morelleti

1550–1555

22/3/50cm

Unassigned

Poor sample, Coccolithus pelagicus, lots of organic matter

Sarmatian

Ammonia tepida, Nonion sp.

Other

Halicornnia sp.

1550–1555

22/4/50cm

Unassigned

Poor sample, Reticulofenestra bisecta, lots of organic matter, pyrite

?Streptochilus sp., Cibicides boueanus, Ammonia tepida, Cycloforina badenensis,

Porosononion granosum

Other

Coal

1652–1657

24/2/50cm

NN6

Sarmatian

Calcidiscus acme, Calcidiscus tropicus, C. leptoporus/pataecus?, Coccolithus pelagicus,

Cyclicargolithus floridanus

Unassigned

Barren

Other

Organic matter

1652–1657

24/3/50cm

NN6

Sarmatian

Calcidiscus tropicus small Calcidiscus, Sphenolinithus abies?, Umbilicosphaera rotula, U.

jafari

Unassigned

Barren

Other

Poriferan spikes

1700–1705

25/1/50cm

Unassigned

Poor sample, Coccolithus pelagicus, Reticulofenestra bisecta

Unassigned

Barren

c) Vráble 1 well (VR-1) (continued)

KOMJATICE DEPRESSION — INTEGRATED BIOSTRATIGRAPHY, SEDIMENTOLOGY AND PROVENANCE ANALYSIS

GEOLOGICA CARPATHICA

, 2018, 69, 4, 382–409

d) Zlaté Moravce 1 well (ZM-1)

Depth (m.)

Core

Discipline

Zone/Subzone

Event

551–556

2/2

Pannonian

Impagidinium spongianum, Spirogyra

551–556

2/4

Pannonian

Impagidinium spongianum, Spirogyra

599–604

3/3

Pannonian

Impagidinium spongianum, Spiniferites bentori pannonicus

653–658

4/1

Pannonian

Spiniferites bentori pannonicus

954–959

10/1/50cm

Unassigned

Barren/?Thoracosphaera fragment

Unassigned

Barren

1005–1010

11/3,4/50 cm

Pannonian

ABN Reticulofenestra tegulata and Pontosphaera japonica, Reticulofenestra pseudoumbilicus,

R. haqii, R. minuta, Coccolithus pelagicus, Cyclicargolithus floridanus

Unassigned

Barren

1046–1051

12/2/50

Acme Bolivina dilatata maxima, Bulimina elongata, cassidulinids (reworked)

1046–1051

12/4

NN6 Sarmatian

Calcidiscus spp., C. leptoporus, Umbilicosphaera jafari

1099–1104

13/4/50cm

Unassigned

Barren

1145–1150

14/1

Unassigned

Barren

1201–1206

15/2

NN6

?Late Badenian

?Sarmatian

Helicosphaera walbersdorfensis, H. wallichii, H. carteri, Sphenolithus abies, Reticulofenestra

pseudoumbilicus, Calcidiscus premacintyrei, C. macintyrei, C. tropicus, C. leptoporus,

Umbilicosphaera rotula, Holodiscolithus macroporus, Braarudosphaera bigelowii bigelowii,

Rhabdosphaera sp., ABN Coccolithus pelagicus, Reticulofenestra haqii

1253–1258

16/2/50cm

Extremely rich and diversified assemblage dominated by Bolivina dilatata maxima, Melonis

pompilioides, Angulogerina angulosa, Valvulineria complanata

Other

Bryozoans, ostracoda valves

1253–1258

16/3

NN6

Late Badenian

Sphenolithus abies, Braarudosphaera bigelowii parvula, Reticulofenestra pseudoumbilicus,

Umbilicosphaera jafari, Holodiscolithus macroporus, ABN Coccolithus pelagicus,

Reticulofenestra haqii, reworked Coccolithus formosus, Arkhangelskiella cymbiformis

1346–1351

18/2/50cm

NN6

?Badenian

?Sarmatian

Calcidiscus premacintyrei, C. tropicus, Coccolithus pelagicus, Reticulofenestra haqii,

Cyclicargolithus floridanus, Sphenolithus abies, Umbilicosphaera jafari, Reticulofenestra

stavensis

Upper Badenian

Fragments of agglutinated foraminifers, Nonion communis, Bulimina elongata, Uvigerina

semiornata

Corr.with NN6/BulBol Melitasphaeridium choanophorum

1346–1351

18/3/50cm

Unassigned

Barren

Spirorutilus carinatus, Haplophragmoides wilsoni, Reticulophragmium, Bathysiphon sp.

Corr.with NN6/BulBol Cleistosphaeridinium placacanthum

1346–1351

18/4/50cm

Dominated by Haplophragmoides wilsoni, Reticulophragmium, Ammobaculites, Bathysiphon sp.

Unassigned

Phytoclasts, opaque

1346–1351

18/5/50cm

Unassigned

Barren

Agglutinated types of foraminifers dominated by Haplophragmoides wilsoni,

Reticulophragmium, Ammobaculites, Bathysiphon sp.

1405–1410

19/1/50cm

Unassigned

Barren

Unassigned

Possible agglutinated foraminifera or testaceans, Ammobaculites

Other

Organic matter, Glyptostrobus seeds and cones

1405–1410

19/2/50cm

Unassigned

Barren

Undetermined agglutinated foraminifera or testaceans

1494–1499

21/1/50cm

Unassigned

Barren

Unassigned

Barren

Unassigned

Barren

1494–1499

21/2

Unassigned

Barren

1494–1499

21/3/50cm

Unassigned

Barren

Unassigned

Barren

Unassigned

Barren

1494–1499

21/4/50cm

Unassigned

Barren

Unassigned

Barren

1494–1499

21/5

Unassigned

Barren

1553–1558

22/1/50cm

Unassigned

Barren/?Thoracosphaera, ?Reticulofenestra sp.

Unassigned

Barren

1708–1711

25/1/50cm

Unassigned

Barren

Unassigned

Barren

vii

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

GEOLOGICA CARPATHICA

, 2018, 69, 4, 382–409

a) Dasycladacean algae

Halicoryne aff. morelleti (Pokorný, 1948)

b) Foraminifera

Angulogerina angulosa (Williamson, 1858)

Anomalinoides dividens Łuczkowska, 1967

Bathysiphon Sars, 1872 sp.

Bogdanowiczia pocutica Pishvanova, 1967

Bolivina dilatata maxima (Cicha & Zapletalová, 1963)

Bolivina sarmatica Didkowski, 1959

Bulimina elongata d’Orbigny, 1826

Cassigerinella globulosa Egger, 1857

Chiloguembelina cubensis (Palmer, 1934)

Dogielina Bogdanovich & Voloshinova, 1949 sp.

Elphidium aculeatum (d‘Orbigny, 1846)

Elphidium hauerinum (d‘Orbigny, 1846)

Elphidium josephinum (d‘Orbigny, 1846)

Globigerina concinna Reuss, 1850

Globigerinella obesa (Bolli, 1957)

Haplophragmoides Cushman, 1910 sp.

Haplophragmoides wilsoni Smith, 1948

Melonis pompilioides (Fichtel & Moll, 1798)

Miliammina Heron-Allen & Earland, 1930

Miliammina fusca (Brady, 1870)

Miliammina subvelatina Venglinsky, 1975

Miliammina velatina Venglinsky, 1961

Nonion communis (d’Orbigny, 1846)

Porosononion granosum (d’Orbigny, 1846)

Quinqueloculina badenensis = Cycloforina badenensis (d’Orbigny,

1846)

Reticulophragmium Maync, 1955

Spirorutilus carinatus (d’Orbigny, 1846)

Trilobatus trilobus (Reuss, 1850)

?Trochammina kibleri Venglinsky, 1961

Uvigerina semiornata d’Orbigny, 1846

Valvulineria complanata (d’Orbigny, 1846)

c) Nannofossils

Arkhangelskiella cymbiformis Vekshina, 1959

Braarudosphaera bigelowii (Gran & Braarud, 1935) Deflandre, 1947

Braarudosphaera bigelowii parvula Stradner, 1960

Calcidiscus Kamptner, 1950

Calcidiscus leptoporus (Murray & Blackman, 1898) Loeblich &

Tappan, 1978

Calcidiscus macintyrei (Bukry & Bramlette, 1969) Loeblich &

Tappan, 1978

Calcidiscus pataecus (Gartner, 1967) de Kaenel & Villa, 1996

Calcidiscus premacintyrei Theodoridis, 1984

Calcidiscus tropicus (Kamptner, 1955) Varol, 1989 sensu Gartner,

1992

Coccolithus formosus (Kamptner, 1963) Wise, 1973

Coccolithus miopelagicus Bukry, 1971

Coccolithus pelagicus (Wallich, 1877) Schiller, 1930

Coronocyclus nitescens (Kamptner, 1963) Bramlette & Wilcoxon,

1967

Cyclicargolithus abisectus (Muller, 1970) Wise, 1973

Cyclicargolithus floridanus (Roth & Hay, in Hay et al., 1967) Bukry,

1971

Discoaster deflandrei Bramlette & Riedel, 1954

Discoaster lodoensis Bramlette & Riedel, 1954

Discoaster variabilis Martini & Bramlette, 1963

Helicosphaera carteri (Wallich, 1877) Kamptner, 1954

Helicosphaera recta (Haq, 1966) Jafar & Martini, 1975

Helicosphaera walbersdorfensis Muller, 1974

Helicosphaera wallichii (Lohmann, 1902) Okada & McIntyre, 1977

Holodiscolithus macroporus (Deflandre, in Deflandre & Fert, 1954)

Roth, 1970

Isolithus semenenko Luljeva, 1989

Lanternithus minutus Stradner, 1962

Microrhabdulus decoratus Deflandre, 1959

Micula staurophora (Gardet, 1955) Stradner, 1963

Pontosphaera japonica (Takayama, 1967) Nishida, 1971

Pontosphaera latelliptica (Báldi-Beke, in Báldi-Beke & Báldi, 1974)

Perch-Nielsen, 1984

Pontosphaera multipora (Kamptner, 1948 ex Deflandre in Deflandre

& Fert, 1954) Roth, 1970)

Prediscosphaera cretacea (Arkhangelsky, 1912) Gartner, 1968

Reticulofenestra Hay, Mohler & Wade, 1966

Reticulofenestra bisecta (Hay, Mohler & Wade, 1966) Roth, 1970

Reticulofenestra haqii Backman, 1978

Reticulofenestra hillae Bukry & Percival, 1971

Reticulofenestra minuta Roth, 1970

Reticulofenestra pseudoumbilicus (Gartner, 1967) Gartner, 1969

Reticulofenestra stavensis (Levin & Joerger, 1967) Varol, 1989

Reticulofenestra tegulata (Bóna & Gál, 1985; Ćorić & Gross, 2004)

Rhabdosphaera Haeckel, 1894

Sphenolithus abies Deflandre in Deflandre & Fert, 1954

Sphenolithus heteromorphus Deflandre, 1953

Sphenolithus moriformis (Bronnimann & Stradner, 1960) Bramlette

& Wilcoxon, 1967

Thoracosphaera Kamptner, 1927

Tribrachiatus orthostylus Shamrai, 1963

Umbilicosphaera jafari Muller, 1974

Umbilicosphaera rotula (Kamptner, 1956) Varol, 1982

Zygrhablithus bijugatus (Deflandre in Deflandre & Fert, 1954)

Deflandre, 1959

d) Palynomorfs

Achomosphaera Evitt, 1963

Cleistosphaeridinium placacanthum Deflandre & Cookson, 1955

Deflandrea Eisenack, 1938

Impagidinium spongianum Sütő-Szentai, 1985

Melitasphaeridium choanophorum (Deflandre & Cookson, 1955)

Harland & Hill, 1979

Pontiadinium obesum Sütő-Szentai, 1982

Pontiadinium pecsvaradensis Sütő-Szentai, 1982 *

Spiniferites Mantell, 1850

Spiniferites bentori (Rossignol, 1964) Wall & Dale, 1970 ssp.

oblongus Sütő-Szentai, 1986

Spiniferites bentori (Rossignol, 1964) Wall & Dale, 1970 ssp.

pannonicus Sütő-Szentai, 1986

Virgodinium Sütő-Szentai, 2010

Virgodinium asymmetricum Sütő-Szentai, 2010

Virgodinium transformis Sütő-Szentai, 2010

* Despite the Lentin and Williams index (2017 edition) with redefined

genus to ?Impagidinium, we used in whole manuscript the species

name Pontiadinium pecsvaradensis (= ?pecsvaradense) according

the Sütő-Szentai´s and Bakrac´s publications to be able to correlate

biozones.

Suppl. 2. Complete fauna and flora list: a) Dasycladacean algae; b) Foraminifera; c) Nannofossils; d) Palynomorfs.