GeolCarp_Vol61_No5_437

www.geologicacarpathica.sk

GEOLOGICA CARPATHICA, OCTOBER 2010, 61, 5, 437—447 doi: 10.2478/v10096-010-0026-z

Introduction

The  Western  Carpathians  are  characterized  by  a  complicat-
ed,  fragmented  crustal  structure  which  was  formed  during
the Hercynian, Paleo- and Neo-Alpine orogenic stages. This
inhomogeneity of the crustal structure is the main source of
complicated  features  of  the  magnetic  field  (Fig. 1).  Recent
works  from  geology  (Fusán  et  al.  1987;  Biely  et  al.  1996;
Plašienka  et  al.  1997;  Bezák  et  al.  2008)  and  geophysics
(Bielik  1995,  1998;  Vozár  et  al.  1999,  2003;  Kubeš  et  al.
2001;  Bielik  et  al.  2006),  are  helpful  for  explanation  of  the
deep  sources  of  magnetic  anomalies  in  the  new  magnetic
map of Slovakia (Kubeš et al. 2008).

The beginning of regional geomagnetic measurements

within the area of the Slovak Republic is dated to the end of
the 1950s and beginning of the 1960s. The first results were
obtained  by  measuring  the  vertical  component  of  the  mag-
netic  field  in  the  Východoslovenská  nížina  Lowland  (Man
1961) and in the Podunajská nížina Lowland (Man 1962). A
synoptic  airborne  mapping  of  former  Czechoslovakia  (the
scale  1 : 200,000,  magnetic  and  radiometric  measurements,
2 km flight-line spacing, permalloy detector) was carried out
almost  at  the  same  time  (1957—1960).  In  the  framework  of
the  above-mentioned  mapping,  the  area  of  Slovakia  was
measured, though without regions where the Neogene volca-
nic  rocks  are  found.  These  were  omitted  with  the  remark
“heavily disturbed magnetic field”. The results of this map-
ping  are  contained  in  the  pack  of  the  aeromagnetic  maps
1 : 200,000 (Mašín 1963).

Magnetic field of the Western Carpathians (Slovakia):

reflections on the structure of the crust

PETER KUBEŠ

, VLADIMÍR BEZÁK

2,1

, UDOVÍT KUCHARIČ

, MIROSLAV FILO

†

JOZEF VOZÁR

, VLASTIMIL KONEČNÝ

, MILAN KOHÚT

and AUGUSTÍN GLUCH

State Geological Institute of Dionýz Štúr, Mlynská dolina 1, 817 04 Bratislava, Slovak Republic; ludovit.kucharic@geology.sk

Geophysical Institute, Slovak Academy of Sciences, Dúbravská cesta 9, 845 28 Bratislava, Slovak Republic;

Geological Institute, Slovak Academy of Sciences, Dúbravská cesta 9, 840 05 Bratislava, Slovak Republic; jozef.vozar@savba.sk

(Manuscript received February 16, 2010; accepted in revised form June 10, 2010)

Abstract: A new digital magnetic map of Slovakia on the scale of 1 : 200,000 and 1 : 500,000 was compiled at the end of
2008 as the output of database magnetic objects from the whole territory of Slovakia at a scale of 1 : 50,000. The variable
geological structure of the West Carpathian crust is depicted in the equally variable magnetic field of this region. A
sizable number of magnetic anomalies with manifold character have been recognized. The basic anomalies distribution
was divided into two groups: anomalies connected with rocks of the pre-Neogene basement and anomalies which origi-
nate in Neogene and Quaternary volcanic products. Most of the significant anomalies in the pre-Neogene basement
were interpreted, modelled and consequently its geological and tectonic classification was worked out. On the basis of
the anomalous field features, the following sources of anomalies have been distinguished: a) known, located on the
surface, or at shallow depths verified by boreholes, mainly expressed by simple morphology, b) deep-seated and ex-
pressed by complicated morphology, reinterpreted or newly interpreted and also problematic. According to our present
knowledge the interpretations are insufficient and remain open for further investigation. The above mentioned sources
of magnetic anomalies are classified in terms of tectonic provenience to the main tectonic units.

Key words: Slovakia, magnetic field, magnetic map, geological and tectonic interpretation.

A systematic detailed airborne mapping of the Slovak Re-

public  1 : 25,000  (250 m  flight-line  spacing;  1 second  sam-
pling  frequency)  was  initiated  in  1974,  with  simultaneous
application of the airborne proton magnetometry and gamma-
ray  spectrometry.  The  all  crystalline  cores  were  covered  by
this mapping to the end of 1983 (Malé Karpaty Mts, Považský
Inovec  Mts,  Tribeč  Mts,  Strážovské  vrchy  Hills,  Malá  Fatra
Mts,  Slovenské  Rudohorie  Mts,  Branisko  and  Čierna  hora
Mts)  including  interjacent  depressions.  These  measurements
also  included  the  all  Neogene  volcanic  mountains  (Central
Slovak area, Slanské vrchy Mts and Vihorlat Mts) as well as
parts  of  the  Inner  Carpathian  Paleogene  (Skorušinské  vrchy
Hills,  Chočské  vrchy  Hills,  Šarišská  vrchovina  Highlands)
and  the  basins  situated  in  the  South  of  Slovakia  (Lučenecká
kotlina, Rimavská kotlina and Košická kotlina basins). A sig-
nificant  part  of  the  Levočské  vrchy  Hills  was  covered  in  the
years 1991—1992. This technology was applied to a total area
of 26,160 km

(Gnojek & Janák 1986).

The high quality results from the areal measurements of the

vertical (Z) component in the Východoslovenská nížina Low-
land  and  Podunajská  nížina  Lowland  have  been  recalculated
in  T (the total vector of the magnetic field) and incorporated
into the data set from the airborne proton magnetometry. This
produced a database of  T anomalies covering about 70 % of
the  territory  of  Slovakia.  Many  of  the  registered  anomalies
have been interpreted by Gnojek in Vozár et al. (1999).

The rest of the territory mainly the high-elevation areas

(Ve ká Fatra Mts, Vysoké Tatry Mts, Nízke Tatry Mts) and
the Flysch of the Eastern part of Slovakia were measured by

439

MAGNETIC FIELD OF THE WESTERN CARPATHIANS (SLOVAKIA)

ground application of the proton magnetometry with the
density of 1—3 points/km

(Kubeš et al. 2008). This produced

a comprehensive database of magnetic anomalies T, which is
the basis for the new magnetic map of the Slovak Republic.

Methodology

Many anomalies recognized by airborne measurements

have been verified by the ground survey. The interpretation
of younger magnetic rocks (Neogene and Quaternary) is fur-
ther  complicated  by  the  abundance  of  normal  and  reverse
magnetic  polarization.  All  the  measurements  were  reduced
to  the  normal  magnetic  field  (IGRF  1995  –  International
Geomagnetic Reference Field).

The density of the measurements is sufficient for construc-

tion of a map with a scale of 1 : 50,000. Every difference in
the magnetic field above 15 nT can be considered as anoma-
lous and should be explained by a geological reason. Most of
the measured magnetic anomalies were interpreted in detail
in separate publications (Kubeš et al. 2002; Filo et al. 2003;
Bezák et al. 2004b; Kubeš & Kucharič 2005).

The interpretations of subsurface anomalies in this work

are almost without changes, but some new possibilities of in-
terpretation are indicated in the group of deep seated sources
of anomalies. A classification of anomaly sources has been
done in concordance with a new Tectonic map of the Slovak
Republic (Bezák et al. 2004a).

The newest investigation utilizing the magnetic database

(Kubeš et al. 2001) was carried out by Rozimant et al. (2009)
in which the relation between Curie point and the depth of
the magnetic crust in Slovakia was studied.

Modelling of the anomaly sources was done by the meth-

odology of Talwani & Heirtzler (1964) and geophysical soft-
ware Oasis Montaj.

The interpretation of the thickness of volcanic complexes

is  based  on  geological  knowledge  about  the  horizontal  and
subhorizontal  bedding  of  lower  margin  magnetic  active
rocks  deposited  on  environments  with  non-magnetic  or
slightly  magnetic  content.  The  relation  between  geological
objects, relief of the field and magnetic field changes in the
three altitude levels (80 m, 500 m and 2000 m) indicates that
a  magnetically  active  volcanic  complex  with  a  thickness  of
100 m invokes at a height of 500 meters an anomaly with an
amplitude of about 40 nT. In other words, a magnetic anom-
aly with a magnitude of 100 nT at an altitude of 500 m above
the terrain represents a volcanic complex with a thickness of
200 m, a value of 200 nT, means a thickness of 500 m, and
finally  a  value  of  400 nT  indicates  a  thickness  of  almost
1000 m.  The  thickness  of  the  volcanic  complex  from  the
Slanské vrchy Hills, and Vihorlat Mts was interpreted simi-
larly (Beneš 1971). In this case it was ascertained, that a vol-
canic  complex  with  a  thickness  of  100 m  recalls,  at  the
altitude of 300 m an anomalous effect of 70 nT, a thickness
of  about  500 m  causes  an  anomaly  of  about  350 nT  and  a
thickness  of  almost  1000 m  is  depicted  by  an  anomaly  of
about 700 nT. The interpretation of the thickness of volcanic
complexes  is  given  in  the  Atlas  of  geophysical  maps  and
profiles (Kubeš et al. 2001).

Magnetic properties of minerals and rocks

The intensity of the magnetic properties of rocks depends

directly on magnetic minerals, the (ferrimagnetic) content of
magnetic minerals and on concentration within the rock vol-
ume as well. These are magnetite, ulvöspinel, maghemite, il-
menite and pyrrhotite. On the other hand, ulvöspinel,
ilmenite and hematite are common examples of antiferri-
magnetism and therefore the resultant magnetic susceptibility
is not so impressive, due to internal magnetic structure.

Bulk magnetic susceptibility ( – KAPPA) is the main

parameter for rocks distinguishing from the magnetic point
of view and according to this, magnetic rocks within Slova-
kia can be separated into the following groups:

• Practically non-magnetic – less than 300*10

—6

units

of SI;

• Very slightly magnetic – = 300—1000*10

—6

units of SI;

• Slightly magnetic – = 1000—10,000*10

—6

units of SI;

• Magnetic – = 10,000—50,000*10

—6

units of SI;

• Strongly magnetic – above 50,000*10

—6

units of SI.

A voluminous magnetic properties study has been carried

out on samples collected from natural and artificial outcrops
and selected boreholes, as well. The magnitudes of magnetic
susceptibility  and  remanent  magnetic  polarization  (RMP)
were assessed. Magnetic properties are given in the Table 1,
according to data given by Husák & Stránska (1980), Grecu-
la  &  Kucharič  et  al.  (1985,  1992)  and  Gregorová  et  al.
(2003). Variability in the parameters under study is obvious
(this  is  the  typical  feature  of  magnetic  rocks)  and  therefore
the significance of average values is only on the informative
level.

The variability in the presented results of the magnetic

properties is mainly influenced by the following factors:

a) concentration and type of magnetic minerals;
b) magnetic properties of individual minerals;
c) type of magnetic mineral distribution in the rocks;
d) type and intensity of metamorphoses and tectonic ac-

tivity;

e) weathering processes.
As we have mentioned earlier, the values presented in Ta-

ble 1 are very roughly informative. Especially class of meta-
morphosed rocks is greatly variegated depending on the type
of metamorphic processes.

On the basis of the data obtained, we can state that the

group with practically no magnetic rocks includes the Qua-
ternary sediments, Neogene sediments without volcanic frac-
tion,  sediments  of  the  Flysch  Belt  and  Paleogene  units  and
almost  the  whole  filling  of  the  Mesozoic.  The  group  of
slightly  magnetic  rocks  comprises  fine-grained  volcaniclas-
tics, several types of slates, and metamorphites from the low-
er  part  of  green  schist  facies,  acid  Permian  volcanics  and
most of the granites. The group of moderate magnetic rocks
is  represented  by  medium-grained  Neogene  volcaniclastics,
intermediate  Permian  volcanics,  amphibolites  and  some
types  of  mica  schists,  gneisses  and  granitoids.  Coarse-
grained  volcaniclastics,  breccias,  and  unfaulted  products  of
andesite volcanism, paleobasalts, ultramafic bodies from the
Meliaticum and Ochtiná tectonic unit and Rochovce granite
are assigned to the group of strongly magnetic rocks.

440

KUBEŠ, BEZÁK, KUCHARIČ, FILO, VOZÁR, KONEČNÝ, KOHÚT and GLUCH

In spite of remarkable variability in their magnetic proper-

ties, the basic knowledge of volcanic rocks about direct de-
pendency between basicity and magnetic properties is valid.
Moreover magnetic parameters can be extremely diminished
in the central parts of Neogene volcanic zones where the sec-
ondary alteration (propylitization, adularization, silicifica-
tion) was recognized. In this regard originally magnetic rock
may be inverted completely into a non-magnetic medium.

Granitoids belong to special group, because for a long pe-

riod they were considered as a non-magnetic medium within
the territory of Slovakia. Verification of the Rochovce mag-
netic anomaly, by a deep borehole, ascertained the occur-
rence of magnetic granite of the Cretaceous age.

Since then we have learned that magnetic anomalies can

also be created by tonalites, as well as by the special types of
granites with mafic enclaves. Our contribution does not dis-
cuss the event of secondary magnetite creation in the pro-
cesses of mechanical deformation and repetitive alterations,
which are responsible for increase of magnetic properties
(Grant et al. 1985). Clarification of these factors requires ad-

Table 1: Magnetic properties of rocks.

ditional investigation. Some works have appeared regarding
magnetic anisotropy study connected with tectonic-meta-
morphic events in the Veporicum (Hrouda et al. 2002).

Similarly, the group of metamorphosed rocks – mica

schists, para- and ortho-gneisess mainly provide an extremely
large range of bulk magnetic susceptibility and therefore are
almost impossible to rank into one uniform category.

A review of the main magnetic complexes and their

tectonic classification

The values for the intensity of magnetic field in Slovakia

occupy a very wide interval extending from —1000 to
+1100 nT, and thus produce variable types of magnetic
anomalies depending on volume, shape, depth and magnetic
properties of disturbing bodies.

Even a first view of the magnetic map (Fig. 1) shows, that

a completely different magnetic field was recognized above
areas, where Neogene and Quaternary volcanics occur.

KAPPA . 10

–6

[SI]

RMP [nT]

ROCKS

Number

of samples

min max X

average

min max X

average

Pre-Neogene
Quartz porphyrs, porphyroids

61.54

831.60

253.71

1.22

188.56

60.90

Granites

664

708.38

24.24

612.00

0.76

Granodiorites and tonalites

710

27444.60

369.64

1094.68

10.82

Quartz diorites

16723.64

5085.32

368.72

95.05

Albitic-chloritic slates

365.75

44.96

1207.28

48.51

Chloritic-sericitic slates

Biotitic phyllites

487.70

25.67

1.22

0.06

Chloritic-sericitic phyllites

Mica-schists, Kohút zone, South Veporicum unit

7193.36

1115.71

164.84

43.62

Mica-schists, North Veporicum and Tatricum units

244

859.10

77.22

8.88

0.66

Paragneisses

124

36999.50

1343.81

307.47

13.05

Orthogneisses

156

19651.00

832.89

117.55

6.68

Migmatites

116

698.59

95.94

32.73

1.32

Amphibolites and other mafic rocks

253

104800.01

3481.98

1649.16

78.15

Serpentinites

162

74746.44

11832.94

8826.32

613.78

Quartzites (Paleozoic)

727.22

132.26

14.70

1.90

Dark phyllites (Paleozoic)

17343.48

5238.67

11434.46

4563.38

Arkose (Paleozoic)

Quartzites (Mesozoic)

616.07

49.20

19.00

1.77

Variegated shales (Mesozoic)

792.54

209.25

2.64

0.72

Sandy shales (Mezozoic)

Basalts (Hronicum)

83145.94

11957.23

7428.36

430.41

Neogenous+Quaternary volcanics
Rhyolites 271

18.84

19230.62

2996.82

6.28

9663.66

1127.76

Rhyolite pyroclastics

144

310.23

13175.44

3999.10

14.44

2346.21

299.56

Rhyodacites 25

1760.91

15398.56

7067.51

18.84

1283.63

241.15

Dacites 10

7283.54

16973.58

12743.38

296.67

3594.80

1372.93

Pyroxenic andezites

1595

89.18

74480.80

23789.90

18.84

61898.19

2460.13

Amfibol-pyrox. andezites

7443.06

28437.10

16844.22

1458.84

2559.60

2200.76

Amfibol-biotit. andezites

215

639.30

47787.03

16748.76

10.05

5319.91

1307.87

Propylitized andezites

230

628.00

100.48

251.20

11.30

Pyrox. andesites pyroklastics

1802

339.12

44834.18

10304.22

18.59

24586.20

865.76

Bazaltic andesites

1369.04

26398.61

13367.61

405.94

5966.88

2385.27

Alkalic bazaltes, bazanites

2135.20

94137.20

30990.54

18.97

19123.86

5393.64

Basalts pyroclastics

18.84

8626.21

4270.40

2.14

1501.05

565.58

Quartz diorite (propylitized.)

435

43960.00

12220.88

728.48

242.41

441

MAGNETIC FIELD OF THE WESTERN CARPATHIANS (SLOVAKIA)

Fig. 2.

Tectonic

division

Slovakia

(after

Biely

al.

1996)

and

ntours

magnetic

anomalies.

Anomalous

magnetic

fields

caused

Neovolanics:

–

the

Central

Slovakian

volcanic

field;

–

the

Eastern

Slovakian

volcanic

field;

–

buried

volcanics

the

Podunajská

nížina

lowland;

–

buried

volcanics

the

Východoslovenská

nížina

lowland;

–

the

Southern

Slovakian

volcanic field. Contours of magnetic anomalies in pre-Neogene u

nits: solid line – surface and subsurface anomalies; dash line

– deep-seated sources, numbers indicate depth of upper edge of

anomaly

source

from

the

surface.

Core

mountains:

–

Malé

Karpaty,

–

Považský

Inovec,

–

Tríbeč,

–

Strážovské

vrchy,

–

Malá

Fatra,

–

Veká

Fatra,

–

Vysoké

Tatry,

–

Nízke

Tatry.

442

KUBEŠ, BEZÁK, KUCHARIČ, FILO, VOZÁR, KONEČNÝ, KOHÚT and GLUCH

These areas are depicted on the Fig. 2. Magnetic field is very
variegated from both the morphological and polarity changes
points of views. In spite of the very impressive features, the
sources of the field are typically superficial – in the Central
Slovak volcanic area. Deeper-seated volcanites, which create
extensive anomalies in the Podunajská nížina Lowland
(Gnojek & Kubeš 1991) and the Východoslovenská nížina
Lowland (Gnojek et al. 1991), possess a smoother character
of measured field and lower values as well.

The Western Carpathians are fundamentally structured in

the sense of the Tectonic map of Slovakia (Bezák et al. 2004a)
into Outer and Inner parts. The Outer Carpathians are com-
posed of the accretion prism of Flysch Belt nappes, which are
overthrusted onto the European Platform. The NW and N mar-
ginal part of Slovak territory contains anomalies caused by the
effect of deep-seated Proterozoic rock complexes of the Euro-
pean Platform (Brunia), beneath the Flysch Belt.

The Inner Western Carpathians are created by three main

Paleo-Alpine  crustal  units  (Tatricum,  Veporicum  and  Ge-
mericum) and the superficial nappe systems of the Fatricum,
Hronicum,  Meliaticum,  Turnaicum  and  Silicicum  (Fig. 2).
The  crustal  units  contain  fragments  of  Hercynian  tectonic
units. These tectonic units contain basic magmatic complex-
es,  which  are  the  sources  of  magnetic  anomalies.  There  are
basic  volcanites  in  Mesozoic  complexes  of  the  Meliaticum
and  Upper  Paleozoic  complexes  in  the  Hronicum  and
Ochtiná Unit (Vozárová & Vozár 1988). The Early Paleozoic
primarily  Hercynian  tectonic  units  in  the  Gemericum    also
contain  basic—ultrabasic  volcanics  (Rakovec,  Klátov  and
Gelnica tectonic units). All these complexes are depicted on
regional geological maps 1 : 50,000 (Bajaník et al. 1984).

The crystalline basement in the Tatricum and Veporicum

comprises complexes of amphibolites and basic types of
granitoids which are the source of magnetic anomalies. A pe-
culiarity is an occurrence of mica schist complexes in the
Southern Veporicum which possess high values of magnetic
susceptibility. A special type is the Rochovce granite of Cre-
taceous age located in the contact zone between the Vepori-
cum and Gemericum.

Other type of magnetic anomaly sources are deep seated,

mainly in the basement of Neogene basins. Physical proper-
ties and tectonic coherence enable highly probable interpre-
tations in some cases. Some of these rocks are verified by
boreholes.

Over 60 magnetic anomalies in the territory of Slovakia

(Fig. 2), induced by variable scales of petrographic types and
age classifications have been recognized and described. It is
necessary to stress that not all magnetic bodies are reflected
on the presented map, due to its delimited proportion in rela-
tion to the network of measurements.

Compendium of magnetic anomaly sources

Anomalies on the magnetic map of Slovakia can be divid-

ed into the following basic groups:

• Magnetic anomaly sources in the pre-Neogene units;
• Magnetic anomaly sources induced by Neogene and

Quaternary volcanic products.

Magnetic anomalies in the pre-Neogene units

Due to tectonic competence and lithology magnetic anom-

aly sources in the pre-Neogene units can be allocated as fol-
lows (Fig. 2):

Magnetic anomaly sources inside superficial nappes of the
Inner Western Carpathians

A – mafic volcanics of the Hronicum
B – mafic and ultramafic volcanics of Meliaticum

Magnetic anomaly sources inside the Paleozoic basement of
the Gemericum

C – mafic, ultramafic volcanics and phyllites of the

Ochtiná tectonic unit

D – amphibolites and gneisses of the Klátov tectonic unit
E – mafic metavolcanics of the Rakovec tectonic unit
F – metavolcanics of the Gelnica tectonic unit

Magnetic anomaly sources in crystalline complexes of the
Tatricum and Veporicum

G – amphibolites and metamorphic rocks with interca-

lation of mafic rocks

H – mica schists of lower Hercynian tectonic unit
I – basic varieties of Hercynian granitoids

Special type of deep-seated anomaly sources

J – Rochovce granite
K – Cadomian basement in the Northern zone of the

Western Carpathians (Brunia)

L – combination of effects of Cadomian (?) basement

in the Southern zone and its overlying units

M – ultramafic rocks
N – problematic magnetic anomaly sources.

In terms of morphology of anomalous field and probability

of interpretation we can distribute anomaly sources into two
groups:

a) located on the surface or at a shallow depth or deep-

seated but verified by boreholes (group A—K and M);

b) deep-seated, newly interpreted or reinterpreted and

problematic (group L and N).

Surface and subsurface anomaly sources

Permian basic and intermediate volcanic products from the

Ipoltica Group (Vozárová & Vozár 1988) in the Hronicum
(group A) caused the largest magnetic anomalies in the Malé
Karpaty Mts (A

, A

) in the southern part of Strážovské

vrchy (A

) and in the Nízke Tatry Mts (A

, A

). All these

volcanics are depicted in the regional maps with a scale of
1 : 50,000 (Mahe & Cambel 1972; Mahe 1982; Biely et al.
1993; Ivanička et al. 2007).

The Slovak karst territory in the South of Slovakia is char-

acterized by the presence of a large number of bordered anom-
alies (B

—B

) with different amplitude (50—300 nT) which are

assigned to the Meliaticum (Mello et al. 1996). The dominant
sources  of  these  anomalies  are  serpentinites  whose  develop-
ment is fragmented due to tectonic activity and whose exten-
sion  is  small  as  well  as  the  amplitudes  of  the  anomaly  field.
Apart  from  the  serpentinites,  metabasalts,  green  shales  and
glaucophanites are developed here as well.

443

MAGNETIC FIELD OF THE WESTERN CARPATHIANS (SLOVAKIA)

Anomalies in the Gemericum are found in the partial

Ochtiná (C

—C

), Klátov (D

), Rakovec (E

—E

), and Gelnica

—F

) tectonic units. Phyllites and shales, often with a high

content of carbon component, represent the dominant rocks of
the Ochtiná tectonic unit (Vozárová & Vozár 1988). Part of
this unit is composed of mafic and ultramafic metavolcanics.
The position of the unit in question is located in the northern
part of the Gemericum, where it forms a narrow belt on the sur-
face, but its subsurface parts can be interpreted very well thanks
to magnetic results from the footwall of the Neogene unit.

A typical feature of the Klátov tectonic unit is the predomi-

nance of amphibolites, which are associated with gneisses, ser-
pentinized  spinel  peridotites  (antigorite  serpentinite)  and  a
negligible amount of crystalline carbonate as well (Spišiak et al.
1985). The Rakovec tectonic unit is a typical volcano-sedimen-
tary formation with basic volcanites which are the main source
of  anomalies.  The  magnetic  anomalies  in  the  Gelnica  tectonic
unit are of local provenience and in most cases are generated by
basic  volcanics  from  a  bimodal  (diabase—keratophyre)  forma-
tion,  occurrences  of  which  have  been  recognized  both  on  the
surface and at a shallow depth (Bajaník et al. 1984).

An anomalous effect of the amphibolite body in the crys-

talline of the Tatricum and Veporicum possessing a remark-
able extension was recognized in the area to the NW of the
Malé Karpaty Mts (G

). According to the magnetic field con-

figuration and modelling it is obvious, that the amphibolite
bodies are not so thick (less than 300 m). On the other hand,
the anomaly may be clarified as tonalite occurrences seated
near the surface. Similarly, anomalies detected in the
Považský Inovec Mts (G

, G

) are also caused by amphibo-

lites. Less remarkable anomalies belong to amphibolite bod-
ies with interpreted thicknesses of less than 300 m within the
eastern part of the Tribeč Mts (G

). Amphibolites contribute

to the anomalies in the Slovenské rudohorie Mts together
with the Muráň orthogneisses (G

). The aggregate thickness

of this complex is around 750 m. Amphibolites are responsi-
ble for anomalies within the Nízke Tatry Mts (G

, G

) and

Západné Tatry Mts (G

). Amphibolite bodies are depicted on

the regional geological maps 1 : 50,000 (Mahe & Cambel
1972; Klinec 1976; Biely et al. 1993; Nemčok et al. 1993;
Ivanička et al. 1998, 2007).

A long zone of magnetic anomalies (H

—H

) caused by

mica schists in a lower Hercynian tectonic unit in the sense
of Bezák et al. (1997a) has been observed in the Southern
Veporicum with the NE—SW orientation and with a length of
almost 50 km. An elongation of this zone in the pre-Tertiary
basement to the SW is interpreted by Gnojek (1989) as the
Hurbanovo line.

Mica schists were displaced to the surface in the time of

the paleo-Alpine transpression processes. They are depicted
on  the  geological  map  of  this  region  (Bezák  et  al.  1999).
That  is  a  reason  why  its  shape  is  complicated,  and  this  is
equally  reflected  in  the  shape  of  the  magnetic  field.  The
magnetic properties of the mica schists are so massive, that
their  effect  can  be  recognized  even  though  the  mica  schists
are covered by the 3 km thick granitoid complex of the mid-
dle tectonic unit. In contrast, the mica schists which are in-
terpreted as a member of the middle lithotectonic unit in the
sense of Bezák et al. (1997a) are mostly non-magnetic.

The average measured value of the magnetic field above the

basic varieties of the granitoid environment (group I) is from
40—100 nT. It is clear, that the highest values are detected
above the granite outcrops, or at shallow depths of less than
500 m. The granite bodies from the northern part of Považský
Inovec Mts (I

) and the central part of Tribeč Mts (I

) can also

be assigned to this group. In the majority of cases, magnetic
bodies showed relatively smaller spatial extension as well as a
smaller  thickness.  Amplitude  value  changes  are  not  so  re-
markable with regard to the depth of sources and their thick-
ness.  It  could  imply  deeper  source  localization,  higher
magnetic parameters and so also higher basicity. This assump-
tion can be documented by geological-geophysical interpreta-
tion  of  the  results  of  magnetic  anomalies  from  the
south-eastern part of the Malé Karpaty Mts (I

, I

), the south-

ern part of Považský Inovec Mts (I

), Rišňovská depresia De-

pression (I

) and from the Central part of Podunajská nížina

Lowland (I

, I

). In the area of the Malá Fatra Mts two anoma-

lous areas (I

) are delineated. The anomalies are sometimes ac-

companied by diminutive placement of amphibolites close to
the surface. The magnetic effect of granitoids has been observed
in the Vysoké Tatry Mts (I

, I

) and below the Paleogene sedi-

ments toward the East (I

) and the Ve ká Fatra Mts (I

A very expressive magnetic anomaly has been detected near

Rochovce village. It originates from the Rochovce granite
(J

) with high magnetite concentration. A structural borehole

KV-3 found granitoids with extraordinarily high magnetic
properties in the interval 600—1600 m (Hraško et al. 2002).

The anomalous field of the European Platform in the foot-

wall of the Western Carpathians

This field has a deep source character which can be inter-

preted as the Brunia Complex (North European Platform) in
the  sense  of  Dudek  (1980),  underlying  the  flysch  nappes.
The  Brunia  Complex  consists  of  magnetic  and  heavy  rocks
(gabroamphibolites,  basic  granitoids).  These  rocks  have  re-
gional  extensions  to  the  SW  into  Austria  (Gnojek  &  Heinz
1993) and to the NE into Poland (Żelazniewicz et al. 2009.)

The areas that belong to the NW part of Slovak territory

contain two significant magnetic anomalies (K

and K

). The

central part of the above mentioned anomalies are located out-
side Slovak territory. The sources of both anomalies are inter-
mediate, mafic, exceptionally ultramafic intrusive complexes
in the Cadomian basement. These complexes subside gradual-
ly towards the South almost to depths of about 10—12 km and
more (Pospíšil & Kadlečík 1991). Similar feature are assigned
to the anomaly field K

in the N of Slovakia.

Influence of the supposed Cadomian basement in Southern

Slovakia

On the basis of new data about the neo-Alpine tectonic de-

velopment  of  the  Western  Carpathians  (e.g.  Ratschbacher  et
al. 1991; Csontos et al. 1992; Horvath 1993; Plašienka et al.
1997; Bezák et al. 2004a) the south part of the Western Car-
pathians  consists  of  variable  tectonic  blocks-terranes    which
gradually closed the space of the Flysch basin. Tectonic units
of  the  Southern  Veporicum  and  Gemericum  were  placed  in

444

KUBEŠ, BEZÁK, KUCHARIČ, FILO, VOZÁR, KONEČNÝ, KOHÚT and GLUCH

the north part of this area, which contains members with very
high magnetic properties (mica schists, Ochtiná Group).

According to the 2D modelling results of anomalies (depth,

extension and shape) it is clearly impossible to clarify the char-
acter of the magnetic field in this region by the effects of these
bodies only (L

1—3

). That was a reason, along with the occurrenc-

es of heavy mass in this region (Grand et al. 2002), why an ad-
ditional source of magnetic field had to be added – the rocks
with similar magnetic parameters as the Brunia block possesses.
Such interpretation is supported by occurrences of xenoliths of
unknown  crystalline  rocks,  which  were  brought  by  magma  in
the  Fi akovo  area  (Konečný  2008).  This  complex  underlying
the  mica  schist  complexes  is  probably  an  older  basement  on
which have been deposited epicontinental mica schist packs.

Other regional anomalies (L

4—5

) are situated in the sur-

roundings of Rožňava town. The anomalies cover an area of
almost 300 km

. The upper edge of the magnetic complexes

is  interpreted  as  occurring  at  a  depth  4—4.5 km  below  the
surface. The extent of the anomalies and their magnetic and
gravity  properties  make  it  very  probable,  that  the  magnetic
echo  originates  from  a  combination  of  Ochtiná  Unit  rocks,
mica  schists  of  the  lower  Hercynian  unit  and  fragments  of
the Cadomian(?) basement.

Ultramafic rocks

Other types of anomaly in the southern zones include ul-

tramafic rocks, which represent remnants of the Meliata
ocean subducted during the Jurassic period. These fragments
are tectonically transposed mainly on the contact between
the Western Carpathians and the Pelso Unit. The Komarovce
body is a representative example of these anomalies (Gnojek
& Vozár 1994).

The Komárovce magnetic anomaly (M

) is one of the big-

gest in Slovakia. It is situated SW of Košice city. The anomaly
reflects one of the largest ultramafic body in the Western Car-
pathians with an area of about 100 km

(Gnojek et al. 1991).

The borehole KO-1 drilled in the 1960s discovered an ultra-
mafic body at the depth of 943 m. The borehole was finished
at the depth of 1543 m and remained in the ultramafic rocks.

The Zbudza anomaly (M

) was detected in the northern

part of the East Slovak Basin. The borehole Zbudza-1 drilled
in the anomaly area caught a serpentinite body but only sev-
eral meters thick – probably a marginal part of a magnetic
body. The next anomaly was recognized to the south of Prešov
town (M

, Bzenov). The first interpretation of this anomaly

was made by Gnojek et al. (1991). As a source of the anomaly,
a body of ultramafic rocks is considered. The thickness of
the body is approximately 600 m and its roof is thought to lie
at a depth of 800 m. The declination of the magnetic body is
towards the north.

Deep sources of anomalies in the pre-Tertiary basement in

the South and East of Slovakia

The group of problematic sources of magnetic anomalies

—N

) in the bedrocks of the Tertiary sediments is the

most difficult to interpret, because they are located mainly at
very big depths and real knowledge about their origin is

lacking. In most cases there are anomalies from the Danube
Basin and the East Slovak Basin.

The most significant anomaly in the Podunajská nížina

Lowland is the Gabčíkovo anomaly (N

), which crosses the

frontier into Hungarian territory. After the first measurements
the  anomaly  has  been  reinterpreted  by  Gnojek  &  Kubeš
(1991).  Several  deep  boreholes  in  the  anomalous  area  were
drilled to the depth of almost 3000 m, long before this reinter-
pretation, but none has reached magnetic rocks in the Neogene
filling, or bedrock. We suppose on the basis of the tectonic sit-
uation  that  the  anomaly  sources  come  from  the  crystalline
complex of Tatricum, and/or Cadomian basement. Obviously,
the origin of these rocks will be in mafic complexes, because
heavy masses are detected in this area (Bielik et al. 1986).

Apart from these, the following two anomalies were de-

tected in this area – Krá ov Brod (N

) a Vlčany (N

), which

may be caused by basic differentiation of granitoids (Gnojek
& Kubeš 1991).

In the wider surroundings of Kolárovo town an extensive

but not very strong magnetic anomaly (N

) has been detected.

It  is  almost  identical  with  a  gravity  anomaly  (Sitárová  et  al.
1994).  According  to  the  interpretation  given  by  Bezák  et  al.
(1997b) the anomaly is caused by crystalline complex rocks,
or  mafic  remnants  of  a  Meliaticum  inside  the  suture  zone,
which  was  utilized  for  the  partial  body’s  asthenolite  rising
during  the  extension  process  in  the  Neogene.  The  interpreta-
tion of the Strekov anomaly (N

) is clear because it shows the

same features as the Kolárovo one (Filo in Kubeš et al. 2001).

From the depth localization point of view, the only excep-

tion is the Búč anomaly (N

). Due to its shallow position, it is

probably induced by mafic and ultramafic rocks in the Meso-
zoic bedrock. This anomaly probably does not belong to the
Western Carpathians but to a block of the Pelso Unit. The
source of the anomaly is only about 600 m below the surface.

The Bíňa anomaly (N

) in the Eastern part of the Po-

dunajská nížina Lowland probably derives from rocks of a
mica schist complex (Gnojek 1989). The depth of the roof of
this body is about 3—5 km. The anomaly is not located within
magnetic sediments. The interpreted length is 17 km, width
approximately 7 km. It is almost impossible to exclude the
influence of Cadomian basement.

The Východoslovenská nížina Lowland is characterized by

the dominant Sečovce anomaly N

(Gnojek et al. 1991;

Gnojek & Vozár 1994). According to our present knowledge
the  bedrock  complex  (Inačovce-Kričevo  Unit  sensu  Slavik
1974)  comprises  a  set  of  phyllites  of  variable  composition.
However, this complex cannot be the source of the anomaly.
The  boreholes  did  not  catch  the  bedrock  complex.  Therefore
the source of the anomaly is probably metamorphosed mafic
rocks  at  a  depth  of  6—8 km.  It  is  probable  that  the  Sečovce
anomaly is connected with exhumation of subducted crust of
the  North  Penninic  ocean  (Soták  et  al.  1993)  and  with  intru-
sion of the Tertiary asthenolite (Bielik et al. 1998).

The Šariš anomaly (N

) has been detected in the southern part

of the Šarišská vrchovina Upland. The upper edge of it is
thought to lie at a depth of 1.8—2.5 km. The reason for the mag-
netic field’s configuration may be occurrence of more basic
types of granitoid, but it is impossible to entirely exclude mafic
rocks showing a connection with the North European Platform.

445

MAGNETIC FIELD OF THE WESTERN CARPATHIANS (SLOVAKIA)

Anomalies N

(Nová Sedlica) and N

(Humenné) accord-

ing to our preliminary interpretation (deduced from contem-
porary knowledge), are caused by a Neogene volcanics at a
depth of more than 600 m. This is a completely new and as-
tonishing finding.

Magnetic anomaly sources caused by Neogene and Quater-
nary volcanism products

The strongest magnetic anomalies in the territory of the

Slovak Republic have been detected in the areas where the
Neovolcanite Mountains are developed. These are character-
ized by quick alternation of positive and negative anomalies
within a broad range – from —1100 to + 1000 nT.

The manifestation of Tertiary volcanic rocks within mag-

netic  maps  depends  on  several  factors  including:  magnetic
properties, normal, or reverse magnetic polarization, intensi-
ty  and  type  of  hydrothermal  alterations,  planar  and  vertical
extension of the magnetic body, volcanic complex composi-
tion,  conditions  of  morphology,  and  methodology  of  use  of
geomagnetic mapping.

From the above mentioned factors, which influence the

morphology and character of the magnetic field, perhaps the
most dominant magnetic parameters are bulk magnetic sus-
ceptibility and normal, or reverse magnetic polarization. The
rock complexes with reverse magnetic polarization are depict-
ed in the magnetic maps by negative magnetic anomalies.

The value of magnetic anomalies directly depends on their

planar  and  vertical  magnitude.  Volcanic  rock  bodies  with
small  areal  extensions  and  small  thickness  (less  than  30
meters)  need  not  be  depicted  by  a  real  anomaly  although
geological mapping proved its presence. However, in several
cases,  anomalies  were  detected  that  are  interpreted  as  mag-
netic  bodies  with  larger  dimensions  which  are  covered  by
non-magnetic materials of various thicknesses.

Maps of magnetic anomalies from the Central Slovak and

East  Slovak  Neogene  volcanic  mountains  compiled  by
Gnojek  (1989),  Filo  et  al.  (2003)  furnished  a  picture  of  the
three-dimensional  distributions  of  magnetic  active  volcanic
complexes.

Conclusion

The map presented in the contribution shows the first total

picture of the West Carpathian rock complexes forming the
whole territory of the Slovak Republic in the Earth’s magnetic
field. Almost all the measured anomalies have been described,
most of them modelled and assigned to tectonic units as well.

The most disturbed magnetic field (from the configuration,

intensity  values  and  polarity  changing  points  of  view)  has
been  ascertained  above  areas,  where  development  of  Neo-
gene  and  Quaternary  volcanics  took  place.  The  remanent
magnetic polarization dominates over induced magnetic po-
larization in these formations.

Since we were often forced to use only estimated input

data, where knowledge of magnetic properties is lacking, the
possible mistakes may result in questionable depth of the
magnetic body.

However, the morphological factor of the magnetic curve

is  the  most  decisive  characteristic  of  the  interpretation  pro-
cess  and  therefore  this  parameter  appears  the  most  signifi-
cant  for  the  study  of  tectonic  style.  The  shape  of  magnetic
bodies  is  linked  to  the  magnetic  curve  and  we  believe  this
link  is  a  crucial  contribution  to  further  uncovering  and  as-
sessing the geological pattern and development with respect
to particular localities.

The interpreted sources of magnetic anomalies have been

classified according to both the tectonic competence and the li-
thology. The variability of the West Carpathian tectonic pattern
as well as the sizeable depth of seating of volume magnetic
sources is a reason why their interpretation is not definite and
offers room for multi variant solutions. Apart from this, several
cases have been observed in which an anomaly is generated by
a superposition of various sources from different tectonic units.

The whole volume of recognized anomalies has been split

into  two  groups:  a)  known,  expressed  by  simple  morpholo-
gy,  located  on  the  surface,  at  shallow  depths  or  verified  by
boreholes,  b)  reinterpreted  or  newly  interpreted,  mostly
deep-seated  and  expressed  by  complicated  morphology  of
anomalous field and problematic, where interpretation is in-
sufficient according to our present knowledge.

Due to the fact that this is the first comprehensive descrip-

tion of magnetic anomalies in the whole territory of Slovakia
it is obvious that the origin of some anomalies remains un-
known or ambiguous. Therefore these magnetic rocks are
suitable for further investigation.

It is beyond question that the map itself will serve as a

suitable tool for structural and tectonic interpretations in the
future from the regional point of view.

Additional magnetic measurements from regions, where they

were missing, means an important step forward in the magnetic
field  characterization  within  the  Central  European  space.  The
complete magnetic picture of the Slovak Republic will be one
of the basic stones in the compilation of a magnetic map of Eu-
rope.  For instance it makes possible investigation of important
geotectonic  zones such as the Cadomian belt on the boundary
between the Bohemian Massif and the Western Carpathians and
its continuation beneath the Alps and to the NE into Poland.

It is also important to investigate oceanic complexes from

the point of view of reconstruction of the Alpine orogene.
The big challenge for the future is an integrated interpreta-
tion together with seismic and gravity data.

Acknowledgment: The authors dedicate this article in mem-
ory  of  our  colleague  RNDr.  Miroslav  Filo,  who  recognized
and  discussed  some  of  the  problems  considered  here.  This
contribution has been carried out in the framework of Project
No. 0705  (Magnetic  map  of  Slovak  Republic),  Project
No. 1606  (Updating  of  geological  structures  of  Slovakia),
Grants VEGA 0169, 2/0072/08 and APVT-51-002804.

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