GEOLOGICA CARPATHICA, JUNE 2008, 59, 3, 237—245
www.geologicacarpathica.sk
Paleomagnetic investigations of the basal Borové Formation in
the Liptov Depression (Central-Carpathian Paleogene basin)
IGOR TÚNYI
1
, JURAJ JANOČKO
2
and STANISLAV JACKO
2
1
Geophysical Institute, Slovak Academy of Sciences, Dúbravská cesta 9, 845 28 Bratislava, Slovak Republic; geoftuny@savba.sk
2
Department of Geology and Mineralogy, Technical University Košice, Letná 9, 040 01 Košice, Slovak Republic;
juraj.janocko@tuke.sk; stano.jacko@tuke.sk
(Manuscript received October 10, 2007; accepted in revised form January 25, 2008)
Abstract: The results of the paleomagnetic investigation from 9 localities of the Central-Carpathian Paleogene basal
Borové Formation in the Liptov Depression (Central Slovakia) demonstrate complicated tectonic evolution in the cen-
tral area of the Western Carpathians. The eastern rotations are predominant in the southern and western rotations in the
northern margins of the Liptov Depression. Paleodeclinations vary from 92° to 269° and paleoinclinations from 7° to
59°. The dextral and sinistral fault systems explain different values of paleorotations in relatively closely situated
localities. The obtained results generally support the model of tectonic escape from the south-west to north-east direc-
tion. Low inclination in some localities offers various explanations.
Key words: Eocene, Western Carpathians, Liptov Depression, Borové Formation, paleomagnetic directions.
Introduction
Geological investigations in the Liptov Depression (northern
Slovakia) have been carried out since the second half of the
19th Century. Geological mapping together with complex pet-
rographical, stratigraphical, paleontological, geophysical and
hydrogeological researches gave comprehensive information
about the geology of the entire depression. The construction of
the waterwork Liptovská Mara enabled detailed study of this
interesting section.
All data about geology of the Liptov Depression to the
1980s are summarized in the monograph by Gross & Köhler
(1980). The geological investigation of this area was very lim-
ited in the last 20 years. All the measured paleomagnetic rock
samples belong to the basal Borové Formation (Fig. 1).
Tertiary geology of the Liptov Depression
The Liptov Depression is one of the largest Central-Car-
pathian depressions. It is situated in the northern part of Slova-
kia and has the form of an extensive field depression 50 km
long, its width ranging to maximum of 15 km. The depression
is surrounded by the Ve ká Fatra, Nízke Tatry, Západné Tatry
and Chočské Pohorie Mts. The Váh river forms the axis of the
depression.
The Liptov Depression is formed by the Central-Carpathian
Paleogene sedimentary rocks overlain by Quaternary deposits
of variable thickness. In the basement of the depression there
are Mesozoic sedimentary rocks of the Tatric, Fatric (Krížna
Nappe) and Hronic (Choč Nappe) Units. The Paleogene sedi-
mentary succession belongs to the Subtatric Group and con-
sists of four formations: basal Borové Formation, mostly
claystone Huty Formation, flysch-like Zuberec Formation and
prevailingly sandstone Biely Potok Formation.
This paper is focused only on the basal Borové Formation.
This formation (in sense Gross et al. 1984) discontinuously
borders the Liptov Depression. After the Laramian phase of
folding (on the Cretaceous/Tertiary boundary) the greater part
of the Western Carpathians was a part of dry land. During the
larger part of the Eocene the Liptov Depression was covered
by sea. While the present Nízke Tatry Mts represented a barri-
er for the marine transgression (Krá 1977; Gross & Köhler
1980), the area of the present Západné Tatry Mts was – at
least in some periods – covered by a shallow sea.
It is known that the transgression into the area of Liptov De-
pression was gradual and advanced from the northwest and
north resulting in a diachronous age of the basal deposits. The
marine transgression lasted about 5 Myr (40—35 Ma – Barto-
nian to Priabonian in the sense of Serra-Kiel et al. 1998). The
transgression was slowed down by the Štrba transverse eleva-
tion (submarine high?) in the eastern part of depression cov-
ered by sea till the late Priabonian.
The sediments of the basal Borové Formation are very di-
verse in composition. Depressions in the relief below the
Eocene transgressive rocks were locally filled by carbonate
breccias. Gross & Köhler (1980) assume their terrestrial origin
as continual debris material originated during the pre-trans-
gressive time span lasting more than 30 Myr. The rock types
in the lowermost part of the Borové Formation reflect rock
composition of the Mesozoic basement: generally,
dolomite
breccias, conglomerates and organodetric to organogenic
limestones on the Cretaceous marly limestones. The higher
parts of formation are characterized by alternation of the
above mentioned rocks. Fine-grained varieties with abundant
organic remnants often predominate.
The Borové Formation has a specific character at some
places in the NE part of the Liptov Depression (Hybica, Hru-
bý Grúň). In the very shallow and warm sea the biothermal
limestones of reef character originated directly on the Meso-
238
TÚNYI, JANOČKO and JACKO
zoic basement. The maximal thickness of the Borové Forma-
tion is about 100 m.
Description of localities
Middle Eocene
Liptovské Matiašovce
In the cut of the road to the village of Huty, west of the vil-
lage of Liptovské Matiašovce beyond the surrounding con-
crete wall, dolomitic sandstones to conglomerates are found.
In the upper part of the outcrop they alternate with sandy nu-
mulite limestones. This type of deposit originated near the
shore in shallow sea water. The age of the deposit is about
39 Ma (the latest Bartonian in sense of the stratigraphic chart
in Serra-Kiel et al. 1998 and Gross et al. 1984). This locality is
situated in a tectonically very exposed region near the crossing
of the Choč-Subtatric fault with a transverse fault.
Late Eocene (Priabonian)
Partizánska upča
The sampling locality is situated in an abandoned quarry
1.5 km south of the village of Partizánska upča near the road
to the village of Liptovská Lužná. In this outcrop the Mesozoic
substratum (marl limestones of Early Cretaceous) is overlain by
organogenic limestone with bank disintegration in a transgres-
sive position. The limestone is locally very weathered. The
abundant organic remnants enable us to date this limestone as
earliest Priabonian (37—38 Ma; Gross et al. 1984).
Hrubý Grúň
About 2.5 km NE of the village of Východná on the margin
of road to the elevation point Hrubý Grúň near a small water-
works, weathered Triassic dolomites are found with a thin lay-
er of red soil on the surface. Transgressive grey-white to pink
sandy limestones contain clasts of Triassic dolomites from the
underlying basement. These limestones locally have biother-
mal to reef character and contain very rich organic remnants.
The limestones are 37—39 Ma in age (Late Eocene—early Pria-
bonian; Gross et al. 1984).
Velinok
The abandoned quarry near the railway track, about 300 m
NW of the railway station at Podtureň reveals the lower part of
Triassic dolomites lying on Mesozoic basement. In the upper
part of the quarry in transgressive position organogenic sandy
limestones are Late Eocene in age (early to middle Priabonian,
36—37 Ma; Gross et al. 1984).
Fig. 1. Situation map of the investigated area (thick line framed part).
239
PALEOMAGNETIC INVESTIGATIONS IN THE LIPTOV DEPRESSION (CENTRAL-CARPATHIAN PALEOGENE)
Ve ká Pálenica
Rocks of the Mesozoic Krížna Nappe (Keuper) are found in
the lower part of an abandoned quarry, near the road from Pod-
banské to Štrbské Pleso, about 800 m west of the gamekeeper’s
lodge Tri Studničky. Organodetritic limestones of the Borové
Formation occur above them. The upper part of this outcrop is
covered by nonmarine sediments (Quaternary). The limestones
are penetrated by many fissures. The damaged fossils suggest a
shallow-water, probably surf zone environment. The limestones
are Late Eocene in age (35—37 Ma; Gross et al. 1984).
Hybe
The abandoned quarry 1 km west of the village of Hybe,
near the old road to Liptovský Hrádok. The former wall of this
quarry consists of thick sandstone banks. Unlike other locali-
ties, the sandstones are without organic remnants probably as
a result of lower salinity sea water near the river mouth. The
assumed age of these sandstones is 35—37 Ma (Late Eocene;
Gross et al. 1984).
Štrba
Some 500 m east of the village of Štrba before crossroads to
Nižná Šuňava village in an abandoned quarry, sandy lime-
stones are exposed. Frequent occurrence of Bryozoa demon-
strates a deeper (neritic) sea environment (Zágoršek 1996).
The limestones were deposited in the Late Eocene (35—37 Ma;
Gross et al. 1984).
Kolombiarok
In an abandoned cut of the railway, north of the elevation
point Kolombiarok, the Triassic dolomites are overlain by a
body of the bryozoan sandy limestone. The composition of
bryozoan species suggests origin of the sediments in a deep-
er sea environment (up to 200 m deep; Zágoršek 1996). In
the upper part, the body is covered by mudstones of the Huty
Formation. About 80 % of the volume of the body consists
of bryozoan zoariums. The rock is Late Eocene in age (35—
37 Ma; Gross et al. 1984).
Važec
The youngest Paleogene locality in the Borové Formation in
the Liptov Depression is exposed in an abandoned quarry near
the old road from Východná to Važec (2 km west of Važec,
south of the highway). In this quarry irregularly bedded car-
bonate sandstones with organic remnants form the upper part
of the Late Eocene (late Priabonian, 34—35 Ma; Gross et al.
1984).
Methods of paleomagnetic measurements
All the paleomagnetic measurements were performed in the
Paleomagnetic Laboratory of the Geophysical Institute of the
SAS in Bratislava. Thermal demagnetization was carried out
on the demagnetizing system MAVACS. The demagnetiza-
tion was done with thermal step of 50 °C from the room tem-
perature up to 650 °C. After each thermal step the
magnetization and magnetic bulk susceptibility were mea-
sured on the spinner generator JR-5 and Kappa-bridge KLY-3
respectively (all instruments were produced by AGICO
comp.). The demagnetization graphs, so-called Zijderveld dia-
grams of the XY and XZ components and stereographic pro-
jections of the direction of magnetization (Figs. 2—3) were
analysed. The mean paleodirection of each locality was calcu-
lated using the Fisher statistics (Fisher 1953).
Table 1: Paleomagnetic characteristics of the Paleogene rocks from the Liptov Depression. N – number of collected samples; n – number
of used samples; D°, I° – declination and inclination of mean direction for the position in situ (BBC – before bedding correction) and for
position after bedding correction (ABC); k,
α
αα
αα°
95
– statistical parameters (k – parameter of precision,
α°
95
– half angle of the cone of re-
liability containing the mean paleodirection with accuracy 95%, Fisher 1953); J – average value of remanent magnetization of samples in
natural state measured in units nT;
κκκκκ – mean value of bulk magnetic susceptibility of samples in natural state in units SI (uSI).
240
TÚNYI, JANOČKO and JACKO
The characteristic paleodirection of the measured sample
was chosen according to demagnetization graphs (Figs. 2—3).
Two methods were used for analysis of the paleomagnetic
data. At the first method, we considered the vectors of rema-
nent magnetization as primary data. In the second method, we
took vector differences between the steps of demagnetization,
which means the change of direction from temperature T
i
to
temperature T
i + 1
. The division of the thermal steps into three
intervals (20—200 °C, 200—400 °C and 400—650 °C) was per-
formed and used in both analyses. The characteristic direction
was chosen according to Fisher statistical parameters from the
six results (2 methods, 3 thermal intervals). Several samples
with remagnetization and a large dispersion of magnetization
directions were rejected. Characteristic components were cho-
sen mostly in the temperature range 200—400 °C with the
Zijderveld plot going to the end point.
The Figs. 4—6 present the stereoprojections of paleodirec-
tions for all 9 investigated localities together with the mean di-
rection and the circle into which the mean direction lies with
95% probability. Table 1 presents data from the measured pa-
leomagnetic characteristics. We can see that all the investigat-
ed rocks were weakly magnetized. Magnetization varies from
0.009 nT (loc. Štrba) to 0.084 nT (loc. Liptovské Matiašovce).
Six localities (Liptovské Matiašovce, Partizánska upča, Hru-
bý Grúň, Ve ká Pálenica, Štrba and Kolombiarok) provided
Fig. 2. Demagnetization graphs of thermal demagnetization of
sandy limestone of sample 8C from locality: 3 – Hrubý Grúň (Late
Eocene). The upper part of figure – stereographic projections of
paleodirections of remanent magnetization after each step of de-
magnetization. N – North. The largest point denotes the begining
of demagnetization. The full points – normal directions, hollow
points – reverse directions of magnetization. Lower part of figure –
thermal dependence of magnetization (curve J) and magnetic bulk
susceptibility (curve
κ); Zijderveld’s diagrams of XY and XZ compo-
nents of remanent magnetization (Mc Elhiny & Mc Fadden 2000).
Fig. 3. Demagnetization graphs of thermal demagnetization of
thick-bedded sandstone of sample 1C from locality: 6 – Hybe
(Late Eocene). (See Fig. 2.)
241
PALEOMAGNETIC INVESTIGATIONS IN THE LIPTOV DEPRESSION (CENTRAL-CARPATHIAN PALEOGENE)
rocks with negative values of magnetic bulk susceptibility and
three of them (Velinok, Hybe and Važec) with positive val-
ues. Negative susceptibility varied from —12.388
×10
—6
uSI to
—3.126
×10
—6
uSI and positive from 1.685
×10
—6
uSI to
37.454
×10
—6
uSI. Stereoprojections on Figs.4—6 show rather
good convergentions of paleodirections for each localities.
The halfangle of the circle of probability varies between 7.8°
(loc. Partizánska upča) and 13.7° (loc. Važec) (Table 1,
Figs. 4—6).
Fig. 5. Stereographic projec-
tions of paleodirections and
mean direction of 10 samples of
organodetrital limestones from
locality: 5 – Ve ká Pálenica
(Late Eocene); 22 samples
thick-bedded sandstones from
locality: 6 – Hybe (Late
Eocene); and 13 samples of or-
ganogenic sandy limestones
from locality: 4 – Velinok
(Late Eocene). (See Fig. 4.)
Discussion and conclusion
The Carpathian-Pannonian region consists of two indepen-
dently moving Inner Carpathian microplates ALCAPA and
Tisza-Dacia (Csontos et al. 1992; Csontos 1995; Kováč 2000).
Both microplates involve several superunits and complexes,
which trace the dynamics of the microplate movements
(Ratschbacher et al. 1989, 1991). The ALCAPA consists of
the belt of the Austroalpinicum, Pelso Unit and Transcar-
Fig. 6. Stereographic projec-
tions of paleodirections and
mean direction of 17 samples
of sandy limestones from local-
ity: 7 – Štrba (Late Eocene);
13 samples of sandy limestones
from locality: 8 – Kolombia-
rok (Late Eocene); and 13 sam-
ples of carbonate sandstones
from locality: 9 – Važec (Late
Eocene). (See Fig. 4.)
Fig. 4. Stereographic projec-
tions of paleodirections and
mean direction of 22 samples of
carbonate sandstones and con-
glomerates from locality: 1 –
Liptovské Matiašovce (Middle
Eocene); 19 samples of organo-
genic limestones from locality:
2 – Partizánska
upča (Late
Eocene); and 8 samples of
sandy limestones from locality:
3 – Hrubý Grúň (Late Eocene).
The mean direction is denoted by the Maltese cross (full for normal direction, hollow for reverse direction). The circle around main direc-
tion denotes cone of reliability in which the mean direction is present with a probability of 95% (Fisher 1953, Table 1). N denotes North.
242
TÚNYI, JANOČKO and JACKO
pathian Unit (Fuchs 1984; Kazmer & Kovács 1985; Csontos
et al. 1992). The paleomagnetic data suggests that individual
blocs of the Inner Carpathians belonging to the ALCAPA
generally had CCW rotation (Balla 1987; Márton & Márton
1989; Janočko & Kováč 2003).
The structural evolution of the Liptov Depression was in-
fluenced by the uplift of the Tatry and Choč Mts along the
Subtatric-Choč fault system. The activity of this system in
the Early Miocene also resulted in uplift of the Ružbachy
Mesozoic Island (Jacko 2002) in the eastern part of the sys-
tem that generated CCW rotation of the adjacent blocks. The
movement along the main W-E and/or NW-SE fault system
also resulted in the origin of NE-SW and N-S riedl structures
determining vertical segmentation of the pre-Tertiary base-
ment and Tertiary fill of the Liptov Depression. The southern
margin of the studied area is bounded by the Vikartovce
fault system and by the faults bounding the northern slopes
of the Nízke Tatry Mts generally having a W-E trend.
The localities Hrubý Grúň, Velinok Ve ká Pálenica, Ko-
lombiarok and Važec show western paleodirection (Fig. 7 –
loc. 3, 4, 5, 8, 9). This is in agreement with the movement of
the ALCAPA block during the Miocene (Balla 1987; Márton
& Márton 1989; Túnyi & Márton 1996; Kováč 2000; Janoč-
ko et al. 2003).
The eastward paleorotations at the localities Liptovské Matia-
šovce, Partizánska upča, Hybe and Štrba (Fig. 7 – loc. 1 2,
6, 7) may be explained in several ways. One explanation is
that during the uplift of pre-Tertiary blocks along the southern
margin of the Central Carpathian Paleogene basin some of the
blocks were rotated into their present position.
The complicated movements of the blocks resulted in dif-
ferent values for their mean paleodeclinations as revealed by
data from the sampling sites located close to each other (e.g.
the distance between localities Štrba (loc. 7) and Kolombia-
rok (loc. 8) is only some 1.5 km; Fig. 7). This is also shown
in Figs. 8 and 9 where the localities belong to different
Fig. 7. Paleodirections of rocks from the localities after Table 1: 1 – Liptovské Matiašovce, 2 – Partizánska upča, 3 – Hrubý Grúň,
4 – Velinok, 5 – Ve ká Pálenica, 6 – Hybe, 7 – Štrba, 8 – Kolombiarok, 9 – Važec.
Fig. 8. Geological sketch map of the northern part of the Slovak Western Carpathians and its position in the Carpathian range (in the cir-
cle – situation of localities 7 and 8, see Fig. 9).
243
PALEOMAGNETIC INVESTIGATIONS IN THE LIPTOV DEPRESSION (CENTRAL-CARPATHIAN PALEOGENE)
Fig. 9. Position of the localities 7 and 8 (Štrba and Kolombiarok) in
the fault system of the Liptov Depression (detail of Fig. 8).
blocks separated by a fault system (Fig. 8). Similarly, the po-
sition of the localities Velinok and Hybe (Fig. 7 – loc. 4, 6)
in the area of a complicated fault system in the southern part
of the Liptov Depression could affect the different rotation
values obtained. The other relatively difficult interpretation
of paleodirection is the eastern rotation of the locality Lip-
tovské Matiašovce (Fig. 7 – loc. 1). This paleodirection is
interesting because rocks of the same age from
a not very distant locality Jóbova Ráztoka (re-
gion Orava, Túnyi & Köhler 2000) have a
western rotation. The explanation lies in the
dynamics of the Chočské pohorie Mts between
these localities. The emergence of this massif
by vertical pressure caused eastern rotation of
the block at the locality Liptovské Matiašovce,
while the block at Jóbova Ráztoka remained
outside influence of emerged body and pre-
served primary western paleodeclination.
Extremely large paleodeclination and small
inclination of paleodirection were obtained
from the locality Partizánska upča (Fig. 7,
Table 1 – loc. 2). One explanation presented
in the description of this locality is that the
rock was magnetized in the proximity of the
equator and that in the time of magnetization
(the Late Eocene) the equator was approxi-
mately in the SW-NE direction south of the Al-
pine and Carpathian system. The other
explanation is that the rotation of the block
caused extremely high pressure and during it
the rotated block was heated to a temperature
of 200—300 °C. During this heating the sedi-
mentary layers were also inclined. In this posi-
tion, the rock cooled and obtained a secondary
magnetization. Because the movements took
place not long after the origin of the rock, the
geomagnetic field caused secondary magneti-
zation that was practically the same as the orig-
inal one. The systematic error may be caused
by the correction of the inclination of layer.
The samples could sink only partly. Since we
do not know the position (the angle of inclination) of the
samples during magnetization, in the interpretation we con-
sider only paleodeclination.
Another, but still speculative explanation, could be the re-
lation of different sense of rotations to the position of the
sampled localities to a different layer of blocks separated by
regional transform faults. This is implied by the position of
the localities Partizánska upča, Hybe and Štrba (Fig. 7 –
loc. 2, 6, 7) in the southernmost part of the Central Car-
pathian Paleogene basin which is a prolongation of the
Vikartovce ridge. The northern boundary between the ridge
and Central Carpathian Paleogene basin could be a dextral
strike-slip fault which caused general clockwise rotation of
the localities occurring south of it. It is necessary to say that
also in this case the movements of small parts of blocks
played an important role.
Generally, it is possible to state that there are considerable
differences in the values of paleomagnetic directions. The
greatest declinations are found in the group of samples from
the locality Partizánska upča (92°– Fig. 7, loc. 2), while
the smallest occur in the group of samples from the youngest
locality Važec (—10° or 350° – Fig. 7, loc. 9).
An interesting result of the measurements is the low incli-
nation obtained from rocks sampled at locality Liptovské
Matiašovce (Fig. 7, Table 1 – loc. 1) and some other locali-
Fig. 10. Localization of the studied localities in the frame of international chronos-
tratigraphical scale of the Eocene (after Serra-Kiel et al. 1998).
244
TÚNYI, JANOČKO and JACKO
ties. According to Oberhänsli (1996), Bartholdy et al. (1999)
or Soták et al. (2002) during the Eocene two global periods
of warming were recorded, which were accompanied by
melting of glaciers (Early Eocene and upper part of Middle
Eocene) and two global periods of expressive cooling
(boundaries Early/Middle Eocene and Middle/Late Eocene)
also occurred. The samples from the Liptov Depression were
deposited during the second cooling interval. However, the
existence of reef and biothermal limestones (loc. Hrubý Grúň)
with typical subtropical fossils contradics this opinion. As
more possible we suppose that this sedimentary area was near-
er to the equator in the Eocene compared to the present time.
However, this is still an open question and requires further in-
vestigations. The obtained results may also be affected by fre-
quent change of geomagnetic field polarity, which occurred in
the Eocene, when the position of the Earth’s equator was un-
stable (Fig. 10). According to Fig. 11 we can compare the pa-
leodeclinations
of
the
Central-Carpathian
Paleogene
sediments from the Liptov Depression (loc. 1—9) with paleo-
declinations from the Levočské vrchy Mts (loc. 9—12; Márton
1996; Túnyi & Márton 1996) and Orava region (loc. 13—15;
Túnyi & Köhler 2000) as well as with flysch sediments from
the Oravská Magura Unit (loc. 16; Krs et al. 1991), Podhale
Unit (loc. 17—22; Márton et al. 1999) and Dukla Unit (loc. 23;
Márton 1996). Except one or two anomalously large, all pale-
odeclinations indicate western rotation of blocks from the
northern margin of the Western Carpathians arc and paleodec-
linations from the Liptov Depression and Orava region docu-
ment the complicated block system of the Inner Carpathians.
Acknowledgments: The authors are indebted to Eduard
Köhler for his cooperation during the field work and for pro-
Fig. 11. Paleodeclinations of the Paleogene sediments from the Liptov Depression (loc. 1—9; Liptovské Matiašovce, Partizánska upča,
Hrubý Grúň, Velinok, Ve ká Pálenica, Hybe, Štrba, Kolombiarok, Važec), Orava region (loc. 10—12; Zuberec, Oravský Biely potok, Jóbova
Ráztoka; Túnyi & Köhler 2000), Levočské vrchy Mts (loc. 13—15; Demjata, Šambrón, Švábovce; Túnyi & Márton 1996; Márton 1996),
Oravská Magura Unit (loc. 16; Krs et al. 1991), Podhale Unit (loc. 17—22; Poronin, Niedzica, Jurgów, Nowe Bystre, Bialy Dunajec, Male
Ciche; Márton et al. 1999) and Dukla Unit (loc. 23; Márton 1996).
viding the data about the age of the studied localities. The
work could be carried out with the support of the Project “Tec-
togenesis of Western Carpathian sedimentary basins” financed
by Ministry of Environment of Slovak Republic, Grant Agen-
cy VEGA in the Projects No. 4042, 1/1128/04 and 1/2170/05.
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