GEOLOGICA CARPATHICA
, DECEMBER 2018, 69, 6, 545–557
doi: 10.1515/geoca-2018-0032
www.geologicacarpathica.com
Deep contact of the Bohemian Massif and
Western Carpathians as seen from density modelling
LENKA ŠAMAJOVÁ
1,
, JOZEF HÓK
1
, MIROSLAV BIELIK
2,3
and ONDREJ PELECH
4
1
Department of Geology and Palaeontology, Faculty of Natural Sciences, Comenius University in Bratislava, Mlynská dolina, Ilkovičova 6,
842 15 Bratislava, Slovak Republic;
samajova7@uniba.sk
2
Department of Applied and Environmental Geophysics, Faculty of Natural Sciences, Comenius University in Bratislava, Mlynská dolina,
Ilkovičova 6, 842 15 Bratislava, Slovak Republic
3
Earth Science Institute of the Slovak Academy of Sciences, Dúbravská cesta 9, 840 05 Bratislava, Slovak Republic
4
State Geological Institute of Dionýz Štúr, Mlynská dolina 1, 817 04 Bratislava 1, Slovak Republic
(Manuscript received July 24, 2018; accepted in revised form November 28, 2018)
Abstract: Density modelling was carried out along five profiles oriented across the expected deep contact between
the Bohemian Massif and the Internal Western Carpathians in western Slovakia. The density models reveal the continuation
of the Bohemian Massif beneath the External and Internal Western Carpathians tectonic units. The eastern margin of
the Bohemian Massif is situated at depth south-east of the surface outcrops of the Pieniny Klippen Belt and changes its
position in the surveyed area. The contact of the Internal Western Carpathians with the Bohemian Massif and External
Western Carpathians is subvertical. This sharp contact is manifested as the transtension to extension zone towards
the surface.
Keywords: gravimetry, crustal structure, tectonics, continental collision, Pieniny Klippen Belt.
Introduction
The Bohemian Massif (BM) is part of the European Palaeo-
zoic Platform and was tectonically individualized during
the Variscan orogeny (Schulmann et al. 2009). It forms
the fore land of the Eastern Alps and Western Carpathians.
The Brunovistulicum (Dudek 1980; Kalvoda et al. 2008)
forms the eastern most part of the BM. The basement rocks of
the Brunovistulicum consist of granitoids, migmatites and
schists. This basement is unconformably overlain by the Lower
to Upper Palaeozoic sedimentary cover.
The Western Carpathians belong to the European Alpine
orogenic chain. They are divided into two main zones accor-
ding to the period of individualization of tectonic units.
The accretionary prism of the External Western Carpathians
(EWC) was thrust onto the BM during the Miocene. The EWC
consist mainly of Upper Cretaceous to Palaeogene flysch-type
sediments separated into numerous rootless thrust sheets situa-
ted above the BM. The Internal Western Carpathians (IWC)
consist of three groups of nappes including the Palaeozoic
crystalline basement rocks and mostly Mesozoic sediments
tectonically emplaced during the Cretaceous (Hók et al. 2014).
The surface contact between the EWC and IWC is represented
by the intensely tectonically deformed zone of the Pieniny
Klippen Belt (PKB).
The contact of the BM with the Alpine–Carpathian thrust
belt varies along strike significantly. The BM rocks are under-
thrust below the Eastern Alps for more than 100 km (e.g.,
Schmid et al. 2004). The extension of the BM eastward beyond
the PKB and the extent of its underthrusting below the IWC is
a long discussed problem (e.g., Grecula & Roth 1978; Buday
& Suk 1989; Stráník et al. 1993; Tomek 1993; Tomek & Hall
1993; Bielik et al. 2004). In the interpretation of seismic
profiles passing from the BM or EWC to the IWC the term
“the Pieniny crust” was proposed to denote the rocks situated
mostly below the EWC and/or on the contact of the BM
and IWC (Vozár et al. 1999). A similar concept was used
in geophysical modelling of the crustal structure across
the European Palaeozoic Platform, Western Carpathians and
Pannonian Basin within the framework of the CELEBRATION
2000 seismic experiment (e.g., Hrubcová et al. 2010; Janik et
al. 2011; Hrubcová & Środa 2015) as well as in the interpreta-
tion of the magnetotelluric profile MT-15 (Bezák et al. 2014).
The aim of the paper is to bring a new insight on the contact
of the BM, EWC and IWC in the western part of Slovakia
(Fig. 1) on the basis of density modelling, taking into account
geological, geophysical and structural data.
Geological background
The surface geological structure of the investigated area
contains the Tatricum, Fatricum and Hronicum tectonic units
of the IWC (Fig. 2). The Tatricum includes the Variscan crys-
talline basement and the Mesozoic cover (autochthonous)
sediments with a small portion of upper Palaeozoic sediments.
The Tatricum is the lowermost tectonic unit in this area.
The Fatricum and Hronicum are structurally higher nappes
containing mostly Mesozoic sedimentary sequences thrust
over the Tatricum. The PKB represents the frontal part of
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the IWC composed mainly of Jurassic and Cretaceous sedi-
ments which underwent several phases of folding and faulting
during the Late Cretaceous to Miocene (Plašienka & Soták
2015; Hók et al. 2016). The Upper Cretaceous sediments
overlie a tectonically disintegrated Tatric basement and its
Mesozoic cover in the Považský Inovec Mts. (Hók et al.
2016; Pelech et al. 2016, 2017) and were also penetrated in
the Soblahov borehole (SBM-1, Fig. 2; Maheľ 1985) below
the Fatric nappes. The afore-mentioned Upper Cretaceous to
Palaeogene sediments (Gosau Group) are present on top of
the Hronicum and PKB tectonic units. The tectonic units of
the Northern Calcareous Alps are interpreted in the pre-
Cenozoic basement of the Vienna Basin (Fusán et al. 1987;
Wessely 1992a).
The BM rock complexes below the EWC sediments are
represented mainly by crystalline rocks (Picha et al. 2006).
On the other hand, Wessely (1992b) suggested the occurrence
of the autochthonous Mesozoic sediments of the BM in the deep
substratum of the Vienna Basin. On the contrary, borehole
Berndorf-1 situated c. 35 km south-west of Vienna penetrated
two Mesozoic nappes of the Calcareous Alps, Rhenodanubian
Flysch, Molasse sediments and finally the crystalline base-
ment of the BM without the autochthonous Mesozoic cover
sediments (Wachtel & Wessely 1981). Therefore, we assume
none or an insignificant portion of the autochthonous Mesozoic
sediments above the crystalline complexes of the BM in
the deep basement of the investigated area.
The EWC are represented in the investigated territory by
the Magura Group of nappes characterized by the Palaeogene
and Upper Cretaceous flysch sediments on the surface (Biely
et al. 1996). The EWC rock sequences were thrusted generally to
the NW due to subduction of their substratum below the IWC
Fig. 1. Simplified geological map of the Bohemian Massif,
Eastern Alps and Western Carpathians junction (modified
after Lexa et al. 2000). BM — Bohemian Massif;
EA — Eastern Alps; EWC — External Western
Carpathians; IWC — Internal Western Carpathians.
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(Kováč 2000). Thrusting continuously advanced in time from
SW to NE along the outer/northern EWC margin during
the early to late Miocene (Jiříček 1979; Kováč 2000). The shif-
ting of the active subduction and/or thrusting along the Car-
pathian arc caused reorientation of the palaeostress field and
thereby the kinematic character and orientation of the acti-
vated faults in the IWC domain (Nemčok et al. 1989; Fodor
1995; Hók et al. 2016). These processes led to strike slip fault
activity and were one of the reasons for the lateral extrusion
and counter clockwise rotation of the IWC during the Miocene
(Ratschbacher et al. 1991; Kováč 2000). The Neogene sedi-
ments overlie the crystalline, Mesozoic and Palaeogene rock
sequences with a significant angular unconformity.
Data
The gravity data used in this study were obtained from
a Bouguer anomaly map (Pašteka et al. 2014) that was gridded
with 200 m interval. Topography data were taken from
Fig. 2. Simplified tectonic map of the western part of Slovakia (modified after: Began et al. 1984; Maglay et al. 2006; Ivanička et al. 2007;
Polák et al. 2011; Fordinál et al. 2012a; Potfaj et al. 2014) with position of gravimetric profiles and deep boreholes (Biela 1978; Leško
et al. 1982; Michalík et al. 1992).
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the Topographic Institute (2012). Five profiles were extracted
from these grids in a NW–SE direction across the Malé
Karpaty Mts., Biele Karpaty Mts. and Považský Inovec Mts.
(Fig. 2).
The quantitative interpretation of gravity anomalies (as well
as other potential fields) depends not only on the quality of
methods used for forward and inverse gravity modelling but
significantly also on the knowledge of rock densities and
crustal geometries (physical properties, Šimonová & Bielik
2016). The densities of the surface and subsurface geological
units forming the studied region were taken from the paper
(Šamajová & Hók 2018). In this paper the laboratory-deter-
mined densities of the Western Carpathian rocks (e.g., Eliáš &
Uhmann 1968; Biela 1978; Fusán et al. 1987; Stránska et al.
1986; Ibrmajer et al. 1989; Šefara et al. 1987) have been sys-
tematically and in detail processed and analysed into the map
of the tectonic units of the Western Carpathians with
the values of the natural densities of the individual tectonic
units. The geological structure of the investigated area consists
of the Cenozoic and Mesozoic sediments underlain by crystal-
line complexes of different tectonic affinity (Table 1).
Input densities of the lower part of the upper crust, lower
crust, mantle lithosphere and asthenosphere were determined
by an analysis of the results of Lillie et al. (1994); Bielik
(1995, 1998); Hrubcová et al. (2005, 2010); Alasonati Tašárová
et al. (2008, 2009, 2016); Šimonová & Bielik (2016) and
Šimonová et al. (2019). In the last five papers, densities were
calculated by transformation of the seismic P wave velocities
into densities using two empirical relationships of Christensen
& Mooney (1995) and Sobolev & Babeyko (1994).
The surface and subsurface structure of the uppermost part
of the upper crust was constrained using the geological maps
(see Geological map of Slovakia 2013) supplemented by own
structural information from surface and seismic profiles 7HR,
8HR (Vozár et al. 1999).
Rock lithology, tectonic affiliation and sediment thickness
were primarily constrained by borehole data [e.g., DV-1
(Dobrá Voda-1, 48°36’48.13” N, 17°33’59.05” E; Michalík
et al. 1992); Lu-1 (Lubina-1, 48°46’36.69” N, 17°43’28.44” E;
Leško et al. 1982); O-1 (Obdokovce-1, 48°30’31.43” N, 18°03’
6.81” E); Š-5 (Špačince-5, 48°29’29.81” N, 17°37’6.19” E);
Tr-5 (Trakovice-5, 48°24’29.31” N, 17°42’18.55” E); LNV-7
(Lakšárska Nová Ves-7, 48°33’57.52” N, 17°11’6.75” E);
see Biela (1978)]. The results of previous studies were also
applied: e.g., Bielik (1988); Kilényi & Šefara (1989); Kováč
(2000); Makarenko et al. (2002); Bielik et al. (2005).
In deep density modelling it is necessary to take into account
the gravity effects of the Moho discontinuity and the lithosphere–
asthenosphere boundary (LAB). Over the last two decades,
new results from seismic international projects of the CELE-
BRATION 2000, ALP 2002 and SUDETES 2003 have con-
tributed exceptional knowledge about the crustal thickness in
the area of Central Europe (e.g., Grad et al. 2006; Środa et al.
2006; Brückl et al. 2010; Hrubcová et al. 2010; Janik et al.
2011; Malinowski et al. 2013; Hrubcová & Środa 2015). For
completeness, it should be noted that the Moho depth calcula-
tions were performed by integrated modelling (e.g., Zeyen et
al. 2002; Dérerová et al. 2006; Kaban et al. 2010; Grinč et al.
2013; Alasonati Tašárová et al. 2016). Based on integration of
these results Bielik et al. (2018) have compiled the Moho
depth map in the Carpathian–Pannonian region, and the depth
of Moho was taken from this study. We used as reference
an average density for the lower lithosphere of 3.3 g.cm
-3
.
The LAB have been obtained by 2D integrated lithospheric
modelling (Dérerová et al. 2006; Grinč et al. 2013) as well as
integrative 3D modelling (LitMod) combining in a self-con-
sistent manner concepts and data from thermodynamics,
mineral physics, geochemistry, petrology and solid Earth geo-
physics (Alasonati Tašárová et al. 2009, 2016). The results of
Dérerová et al. (2006) and Alasonati Tašárová et al. (2016)
were also applied to the modelling process. In the studied area
the course of the LAB is almost horizontal and it varies from
115 km in the north-west to 110 km in the south-east. Based on
gravity modelling in the Western Carpathians and in
the Carpathian–Pannonian region (Lillie et al. 1994; Bielik
1998), we used as reference density for the asthenosphere 3.27
g.cm
-3
. To make the resultant models display a good reso lution
of the deep and subsurface structures, the LAB is not shown
on Figs. 3–7.
GM-SYS software
The GM-SYS software (GM-SYS User’s Guide for
version 4.9, 2004) was used for 2D forward modelling along
Table 1: The densities of characteristic tectonic units and rock
sequences participating in geological structures of the modelled
profiles (e.g., Eliáš & Uhmann 1968; Biela 1978; Fusán et al. 1987;
Stránska et al. 1986; Ibrmajer et al. 1989; Šamajová & Hók 2018).
Tectonic units
Density [g·cm-3]
EXTERNAL WESTERN CARPATHIANS
MAGURA UNIT
2.65 –2.67
PIENINY KLIPPEN BELT
2.69 –2.70
INTERNAL WESTERN CARPATHIANS
Neogene and Quaternary sediments
2.30 –2.65
Palaeogene sediments
2.64 –2.67
Late Cretaceous sediments
2.66 –2.67
HRONICUM
Mesozoic sediments
2.71–2.75
Late Palaeozoic volcanosedimentary complexes
2.74 –2.83
FATRICUM
Mesozoic sediments
2.68 –2.70
TATRICUM
Mesozoic sediments
2.70
crystalline schists
2.80
S - type / I - type granitoids
2.70 –2.72
BOHEMIAN MASSIF
2.78
lower crust
3.00
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the selected profiles. It is interactive software for calculating
the gravity response of the geological models. 2D models
consist of closed polygons with a spe cific density assigned.
The calculation of gravitational response of the model bodies
is based on the formulae of Talwani et al. (1959), with Won
and Bevis’s algorithm (GM-SYS User’s Guide 4.9, 2004).
To eliminate edge-effects, the GM-SYS software allows
modelling of a profile with an indefinite length (30,000 km
on each side of a model). The starting models were based on
the seismic, magnetotelluric, borehole and surface geological
data. The rock densities used for modelling were determined
by laboratory measurements of the surface, borehole and
well-logging samples (see Table 1). The final models were
interactively modified until a reaso nable fit was obtained
between the measured and calculated gravity data. In this
study, the maximum deviation between calculated and
observed gravity reaches ± 0.95 mGal.
Modelling results
Profile PF-1
Profile PF-1 passes from the Vienna Basin through the Malé
Karpaty Mts. into the Danube Basin (Figs. 2 and 3). This
profile was constructed parallel to seismic profile 8HR (see
Vozár et al. 1999; Bielik et al. 2004).
Surface geology is interpreted according to geological maps
(Polák et al. 2011; Fordinál et al. 2012a; Geological map of
Slovakia 2013). The faults within the Vienna Basin are inter-
preted according to Němec & Kocák (1976). The horst struc-
ture of the Malé Karpaty Mts. is limited by normal faults.
The Litava (Leitha) fault (Marko & Jureňa 1999) is situated on
the north-west side and the Malé Karpaty fault (Bezák et al.
2004) in the south-east. The Hronicum was penetrated by
several boreholes below the Neogene sediments in the Vienna
Basin (Kysela & Kullmanová 1988), while the Tatric crystal-
line basement occurred below the Neogene sediments in
the Danube Basin (e.g., Biela 1978). The Palaeogene sediments
of the Gosau Group are squeezed in the south-verging struc-
ture of the Hronic nappe on the surface (Polák et al. 2011).
The Profile PF-1 consists of several local gravity anomalies.
The Vienna Basin is represented by a gravity low (values vary
from −10 mGal to −55 mGal). The Palaeogene sediments of
the EWC (Magura Unit) are underthrust below the Hronicum
in the Vienna Basin. The PKB is interpreted below the Hro-
nicum and above the EWC sediments (see Kysela &
Kullmanová 1988). This interpretation is comparable to
the Austrian part of the Vienna Basin (Wessely 1992a), but
the Flysch sediments have incomparably greater thickness.
Fig. 3. The profile PF-1. The Malé Karpaty Mts. asymmetric horst structure is bordered on the north-west by the significant transtension zone
of the Leitha fault (Möller et al. 2011) linked with the neotectonic Zohor – Plavecká Depression (Maglay in Fordinál et al. 2012b).
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The tectonic contact between the Vienna Basin and the Malé
Karpaty Mts. is represented by a significant horizontal gradient
of 5.3 mGal/km. A gravity high with an amplitude of ~24 mGal
correlates with the occurences of the Malé Karpaty Mts. sur-
face The fault between the Malé Karpaty Mts. and the Danube
Basin is also characterized by a horizontal gradient 3.42 mGal/
km. Both horizontal gravity gradients indicate a tectonic con-
tact of the Malé Karpaty Mts. horst structure with the Vienna
and Danube Basins.
The Danube Basin gravity low reflects a large thickness
(≥ 3 km) of the low density Neogene sediments, infilling
the Danube Basin. While the tectonic boundary between
the BM and the EWC decreases gradually in the SE direction
(0 –30 km of profile), the contact of the BM with the IWC is
very steep (30 –35 km of profile).
Profile PF-2
Profile PF-2 (Figs. 2 and 4) was constructed across the docu-
mented boreholes (Biela 1978; Michalík et al. 1992). The sur-
face geology is interpreted according to geological maps
(Began et al. 1984; Potfaj et al. 2014; Geological map of
Slovakia 2013) and the structural research. Mainly normal
faults with a negligible oblique component of movement
disrupt the Brezovské Karpaty elevation structure. The Gosau
Group sediments are preserved in the transtension zone con-
tinuing from the Vienna Basin area (Fig. 2) to the Myjavská
pahorkatina Upland (Fig. 4).
The calculated gravity includes two gravity lows and one
gravity high located between them. A significant gravity high
is caused by the structure of the Brezovské Karpaty Mts.,
which are split by a system of faults with a horizontal gravity
gradient of 2.66 mGal/km. The high gravity anomaly of
the Brezovské Karpaty Mts. is the result of superposition of
gravity effects related to the Mesozoic sediments, the Tatric
crystalline basement and the upper/lower crustal boundary,
which are in an elevated position. A tectonic contact between
the Brezovské Karpaty Mts. and Blatné Depression is con-
firmed again by the sharp gravity gradient (3.5 mGal/km).
Neogene and Quaternary sediments of the Blatné Depression
are the cause of a significant gravity low.
The shape of the gravity profile in a NW direction from
the Brezovské Karpaty Mts. reflects the huge thickness of
the Magura flysch sediments, which are characterized by
lower density. The deep contact between the BM and EWC
with the IWC along this profile is similar to the situation on
profile PF-1. The difference lies in the elevated position of
the BM lower crust (0 –18 km of the profile). The contact area
between the EWC and IWC is very steep.
Profile PF-3
Profile PF-3 (Figs. 2 and 5) is oriented along seismic
profile 7HR in a NW–SE direction (see Vozár et al. 1999).
The surface geology is taken from geological maps in
a scale 1:50,000 (Began et al. 1984; Maglay et al. 2006;
Ivanička et al. 2007; Potfaj et al.2014; Geological map of
Slovakia 2013).
Two gravity highs correlate very well with structures of
the Čachtické Karpaty Mts. and the Považský Inovec Mts.
(Fig. 5). The contacts of these structural highs with the Blatné
Depression are characterized by observable horizontal gravity
gradients of ~1.8 mGal/km and 2.16 mGal/km at the contact
with the Čachtické Karpaty Mts. and the Považský Inovec
Mts., respectively. The largest gravity gradient is interpreted
on the SE margin of the Považský Inovec Mts. It indicates
clearly that the tectonic contact of these mountains with the
Rišňovce Depression is almost vertical. The low density
sediments filling the Blatné Depression are the source of
a significant gravity low.
Profile PF- 4
Profile PF-4 (Figs. 2 and 6) is constructed between deep
boreholes Lubina-1 (Leško et al. 1982) and Obdokovce-1
(Biela 1978). The geological structures were taken from geo-
logical maps (Ivanička et al. 2007; Potfaj et al.2014; Pristaš et
al. 2000; Geological map of Slovakia 2013) and original geo-
logical and structural data including geological and structural
mapping. The Eocene sediments of the EWC are underthrust
below the flat-lying PKB and the Palaeogene sediments
(Gosau Group) in borehole Lubina-1 (see L-1 in Figs. 2 and 6;
Leško et al. 1982). From this point of view the PKB is
a detached structure thrust above the EWC sediments in
the western part of Slovakia during the post-Eocene time.
The borehole Obdokovce-1 (O-1) reached the Mesozoic sedi-
ments of the Tatricum cover only (Biela 1978).
The resultant density model is characterized by two alterna-
ting local gravity highs and gravity lows. The gravity high
situated on the NW side of the profile is related to a gravity
effect of the Mesozoic sediments belonging to the Hronicum.
The elevation of the BM basement contributes to this anomaly,
too. Both gravity lows reflect the presence of the Blatné and
Rišňovce Depressions. A significant gravity high between
them is caused by a horst structure of the Považský Inovec
Mts. Both sides of this structural high are accompanied by sig-
nificant gravity gradients reflecting its tectonic contact with
the neighbouring basins. In detail, the gradient on the SE
side of the Považský Inovec Mts. (3.7 mGal/km) is larger
than on the NW (2.0 mGal/km). The sharp gradient corre-
sponds to the Majcichov normal fault (Bezák et al. 2004)
within the norhern part of the Danube Basin. The top of
the BM basement creates an elevation with a minimum depth
of ~8 km beneath the Čachtické Karpaty Mts. Towards the SE,
BM dips sharply under the IWC.
Profile PF-5
Profile PF-5 (Figs. 2 and 7) follows the course of the mag-
netotelluric profile MT-15 (Bezák et al. 2014). It is also paral-
lel to the part of seismic profiles S04 (Hrubcová et al. 2010)
and 6HR (Vozár et al. 1999). The surface geology is taken
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Fig. 4. The profile PF-2. Mesozoic rocks sequences of the Tatricum and Fatricum are not distinguished due to similar lithostratigraphy and
densities of their sediments. The transtension zone is still well recognizable between the Pieniny Klippen Belt and NW margin of the Brezovské
Karpaty Mts. (see Fig. 3).
Fig. 5 The profile PF-3. The margin of BM is situated below the elevation structure of the Čachtické Karpaty Mts.
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Fig. 6 The profile PF-4. The margin of BM is shifted below the Blatné Depression. ČK = Čachtické Karpaty Mts.
Fig. 7. The profile PF-5. Three tectonic slices are supposed within the imbricate structure of the Pieniny Klippen Belt (see Geological map of
Slovakia 2013).
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from geological maps (Began et al. 1984; Ivanička et al. 2007;
Pristaš et al. 2000; Geological map of Slovakia 2013).
The crystalline complexes of the Tatricum are thrusted over
each other as well as over the sub-autochthonous cover unit in
the Považský Inovec Mts. (Ivanička et al. 2007; Pelech 2015).
The tectonic position of imbricate structures of the PKB and
the Hronicum/Fatricum is verifiable on a geological map
(Geological map of Slovakia 2013; see also Hók et al. 2009;
Pešková 2011).
The observed Bouguer gravity data along the profile PF-5
(Fig. 7) are separated into two components, regional and
local. The regional gravity trend reflects increasing Moho
depth from the EWC region to the IWC in the NW–SE direc-
tion. While in the EWC it has a depth of about 35 km, in
Fig. 8. Trace of the Bohemian Massif margin on a simplified tectonic map.
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the IWC it is 30 km. The first local gravity anomaly correlates
well with the PKB (Oravicum) structures and the Hronic
sediments presented below the Neogene infill of the Blatné
Depression, and the second one with the Považský Inovec
Mts. rock complexes. The local short-wavelength gravity low
is the result of the larger thickness of the Blatné Depression
sediments. The contact between the Blatné Depression and
the Považský Inovec Mts. is steep (charac terized by the hori-
zontal gradient of 3.2 mGal/km). This significant density
boundary is formed by the contact between the EWC and IWC
as well as by the contact between the BM and IWC towards
the deeper part of the model (14–17 km of profile). The BM is
partly underthrust below the IWC. In contrast to the magneto-
telluric profile MT-15, the BM margin is localized below
the north-west margin of the Považský Inovec Mts. The exis-
tence of the so called “Pieninic crustal block” (Bezák et al.
2014), was not confirmed. A manifestation of this crustal
block is not evident on the magneto telluric profile or on
the gravimetric profile.
Discussion and conclusion
Gravity modelling takes into account the available geolo-
gical and geophysical knowledge, which have been obtained
in the studied region. However, only the results of the reflec-
tive seismic profiles 3T (Tomek 1993; Tomek & Hall 1993;
Bucha & Blížkovský 1994), 7HR and 8HR (Vozár et al. 1999)
and the interpretation of the magnetotelluric profile MT-15
(Bezák et al. 2014) could be used in modelling deeper struc-
tures. Moreover, the investigated area is outside of all 2D
seismic refraction profiles CELEBRATION 2000 (Grad et al.
2006; Środa et al. 2006; Malinowski et al. 2005; Janik et al.
2009, 2011; Hrubcová et al. 2005), ALP 2002 and SUDETES
2003 (Brückl et al. 2003, 2007, 2010; Hrubcová et al. 2008,
2010). We also took into account the results of 3D integrated
modelling (Alasonati Tašárová et al. 2008, 2009 2016).
The only seismic refraction profile SUDETES 2003 SO4
(Hrubcová et al. 2010) running through the north-east edge of
the surveyed area has proved valuable, because our final
idea related to the deep contact of the Bohemian Massif and
the Western Carpathians is supported by the results of this
profile.
2D gravity modelling carried out on five profiles oriented
across the expected contact between the Bohemian Massif
(BM) and the Internal Western Carpathians (IWC) reveal
the BM margin situated south-east of the outcrops of
the Pieniny Klippen Belt (Oravicum). The surface projection
of the contact between the BM margin and the IWC basement
is bent to the south-east (Fig. 8). The deep contact of the BM
and IWC is linked towards the surface with the extensional
to transtensional structures (in today’s picture), although
the deep contact itself is considered to be compressional to
transpressional (Bielik 1995). The amount of underthrusting
of the BM under the IWC is not considerable in
the investigated territory. This distinguishes the Western
Carpathians from the Eastern Alps (c.f. Alasonati Tašárová et
al. 2016).
The Oravicum represents a shallow structure detached from
its own basement and thrust together with the Fatricum and
Hronicum cover nappes over the External Western Carpathian
(EWC) sediments. According to the results obtained from
the borehole Lubina-1 (Leško et al. 1982), the age of thrusting
can be dated to the Oligocene in western Slovakia. The Lower
Miocene post-thrusting sediments are unconformably overlap-
ping the western part of the Pieniny Klippen Belt (e.g., Potfaj
et al. 2014).
The so called “Pieniny crust” (Vozár et al. 1999; Hrubcová
et al. 2010; Janik et al. 2011; Bezák et al. 2014) is not
recognizable in the geophysical fields or in the results of
gravity modelling within the study area. Like occurrence of
the “Pieniny crust”, the presence of the Penninicum oceanic
crust remnants (Váhicum Unit sensu Plašienka 1997) could not
be interpreted in terms of gravimetric data in the footwall
of the Tatricum.
Acknowledgements: This work was supported by the Slovak
Research and Development Agency under the contracts nos.
APVV-0212-12, APVV-16-0146, APVV-16-0121, APVV-16-
0482 and APVV-17-0170, by the VEGA Slovak Grant Agency
under projects nos. 1/0141/15 and 2/0042/15 and by the grants
of Comenius University No. UK/268/2017. Thanks also to
the comments of the reviewers which helped to clarify some
aspects of the original manuscript.
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