411
LATE MIOCENE COUNTERCLOCKWISE ROTATION OF THE PIENINY ANDESITES
GEOLOGICA CARPATHICA, 55, 5, BRATISLAVA, OCTOBER 2004
411419
LATE MIOCENE COUNTERCLOCKWISE ROTATION OF THE
PIENINY ANDESITES AT THE CONTACT OF THE INNER AND
OUTER WESTERN CARPATHIANS
EMÕ MÁRTON
1
, ANTEK K. TOKARSKI
2
and DÓRA HALÁSZ
3
1
Eötvös Loránd Geophysical Institute of Hungary, Palaeomagnetic Laboratory, Columbus 1723, H-1145 Budapest, Hungary;
paleo@elgi.hu
2
Polish Academy of Sciences, Institute of Geological Sciences, Research Centre in Cracow, Senacka 13, 31-002 Cracow, Poland;
ndtokars@cyf-kr.edu.pl
3
Báthory út 7, H-1054 Budapest, Hungary; dora.halasz@hungary.org
(Manuscript received March 12, 2003; accepted in revised form December 16, 2003)
Abstract: The Pieniny andesite line is a 20 km long zone, which cuts obliquely the contact between the Pieniny Klippen
Belt which separates the Inner and Outer Western Carpathians and the Magura Nappe (the innermost nappe system of the
Outer Western Carpathians). The andesites (dykes and sills) were formed during two intrusion phases. The older dykes
are subparallel to the andesite line, while the younger ones are perpendicular to it. Formerly, the andesites were thought
to be of Sarmatian age, recently obtained K/Ar ages are in the 10.813.5 Ma range. For paleomagnetic study, we drilled
macroscopically fresh material from both generations of the andesites. The samples were subjected to detailed alternat-
ing field and thermal demagnetization. Isothermal remanence acquisition experiments, Curie-point measurements and
microscopy analysis of polished sections were carried out in order to identify magnetic minerals. The results are as
follows. The second phase andesites and some sites in the first phase andesites have complex natural remanent magneti-
zations (NRM) with two stable components: one is isolated below, and the other above the Curie-point of magnetite. It is
remarkable that thermal demagnetization was often needed to reveal all components of the NRM although the rocks we
studied were Neogene igneous rocks which are considered ideal targets for the less time-consuming alternating field
method. The lower temperature component follows a great circle containing the expected stable European direction of
corresponding age. The higher temperature component has counterclockwise rotated declination. The remaining sites of
the first phase andesites have practically a single component remanence, which corresponds to one or the other of the
directions described above. The components with counterclockwise rotated declinations cluster around an overall-mean
direction of D=133°, I=56° with k=26, α
95
=12° (based on 7 site-mean paleomagnetic directions). Neither the magnetic
minerals, nor their degree and type of alteration are different in the two generations of andesites. Thus, the agents of
remagnetization were probably hot fluids acting after the emplacement of the second generation dykes. The tectonic
implication of our results is that the Pieniny andesite area must have rotated counterclockwise, after emplacement of the
second phase dykes.
Key words: Western Carpathians, Neogene andesites, paleomagnetism, complex magnetic remanence, CCW rotations.
Introduction
The Carpathian orogenic belt (Fig. 1) is subdivided into the
Inner Western Carpathians (in some tectonic models they are
called the Internides, e.g. Mahe¾ 1986; Plaienka et al. 1997)
and the Outer Western Carpathians. In the West Carpathian re-
gion, the Outer Carpathians are separated from the Inner Car-
pathians by the Pieniny Klippen Belt. Both the Inner and Out-
er Carpathians are characterized by complicated nappe
structures, but the time of nappe transport is different for the
two areas. In the former, it is of Late Cretaceous age, while for
the latter it is of Paleocene (Tokarski & wierczewska 1998)
through Late Miocene age (Wójcik et al. 1999). The Pieniny
Klippen Belt is a narrow zone of Mesozoic and Tertiary strata
that underwent extreme shortening and wrenching (Birkenma-
jer 1986 and references therein).
The contacts of the Pieniny Klippen Belt with the Outer and
Inner Carpathians are subvertical (Birkenmajer 1986). The
Belt was folded first during the Late Cretaceous through Pale-
ocene, then in the Early Miocene (Birkenmajer 1986 and ref-
erences therein). The Pieniny andesite line (Fig. 2), the object
of the present paleomagnetic study, obliquely cuts the Pieniny
Klippen Belt and the Magura Nappe which is the innermost
nappe in the studied part of the Outer Carpathians. The Pien-
iny andesite line is clearly younger than the folding in the
Magura Nappe (Birkenmajer 1986; cf. wierczewska &
Tokarski 1998).
Recent paleomagnetic studies on Paleogene flysch in the In-
ner Carpathians (Podhale and Levoèa Basins) revealed that the
Internides must have rotated about 60° counterclockwise
(CCW), after the Oligocene (Márton et al. 1998a,b, 1999a).
Sporadic paleomagnetic observations for the Magura flysch
(Márton et al. 2000) also suggest CCW rotation of similar
magnitude for the central segment (south of Cracow). In addi-
tion, there are several paleomagnetic observations from the
foredeep of the Western Carpathians which indicate moderate
CCW rotations (Márton et al. 1999b, 2001) of post-Karpatian
age in the western segment, post-Badenian age in the central
segment and probably post-Pannonian age in the eastern seg-
ment (Karpatian, Badenian, Pannonian are Central Paratethy-
412
MÁRTON, TOKARSKI and HALÁSZ
an stage names; for correlation with the Mediterranean stages
refer to Rögl 1996, and Fig. 8). The upper age limit of the ro-
tations is not yet constrained, apart from a single Upper Bade-
nian paleomagnetic result (showing no rotation) from the
Nowy S¹cz Basin (a piggyback basin sitting on the Outer Car-
pathians). We decided, therefore, to start a new paleomagnetic
study on the Pieniny andesites, which, at the time of our first
sampling (1997), were thought to be of Sarmatian age
(Birkenmajer et al. 1987).
In the 1960s, Birkenmajer & Nairn (1968) carried out pale-
omagnetic investigation on the Pieniny andesites. They used
the standard paleomagnetic technique of partial alternating
field (AF) demagnetization to distinguish between unstable
and stable natural remanent magnetization (NRM) compo-
nents. With this method, they obtained statistically acceptable
results only for some sites in the western part of the andesite
line, which were mostly characterized by steep inclinations
and reversed polarity. However, one site had a definitely
CCW rotated direction. Subsequently, Kruczyk (1970) studied
the paleomagnetic and rock magnetic properties of the second
phase andesites, and obtained statistically well-defined paleo-
magnetic directions for 4 sites, also with steep inclinations and
reversed polarity. Though the majority of the statistically sat-
isfying paleomagnetic directions obtained by the above named
authors did not indicate CCW rotation, the one site (belonging
to the first phase) which did, suggested that rotation could
have occurred during the activity of the andesite volcanism.
This explains our interest in the Pieniny andesites.
Geology and sampling
The Pieniny andesite line is a 20 km long zone consisting of
andesite sills and dykes, which cut Jurassic-Cretaceous and
Paleogene strata of the Pieniny Klippen Belt and Paleogene
strata of the Magura Nappe (Fig. 2). The andesite intrusions
were formed during two successive phases of intrusive activi-
ty (Birkenmajer 1986, 1996). The older set of intrusions com-
prises numerous dykes striking subparallel to the Pieniny
Klippen Belt. The younger set consists only of three NNW
SSE striking dykes, which cut the Magura Nappe at the west-
ern termination of the andesite line. According to Birkenmajer
(1986, 1996), the older phase intrusions formed contempora-
neously with transverse strike-slip faulting. The faulting con-
tinued after the cessation of the older intrusive phase. The
younger phase intrusions follow transversal strike slip faults.
The intrusions are hypabyssal dykes of small (510 m wide)
to moderate (over 100 m wide) size, and are composed of sev-
eral types of andesites, the most common being augite-am-
phibole andesite (Birkenmajer 1996 and references therein);
the igneous activity is related to the southward subduction of
the Outer Carpathian basin lithosphere (Birkenmajer & Péc-
skay 1999 and references therein).
From the older phase intrusions we drilled samples from 3
abandoned quarries and 2 natural outcrops, from the second
phase, two dykes were sampled, in 2 abandoned quarries. In
all cases, the samples were distributed between different parts
of the intrusions so that our samples represented rocks that
cooled at different rates and acquired their magnetization at
Fig. 1. The location of the Pieniny andesite line in the general
framework of A the Carpathians and B in relation to the In-
ner and Outer Western Carpathians.
413
LATE MIOCENE COUNTERCLOCKWISE ROTATION OF THE PIENINY ANDESITES
Fig. 2. Paleomagnetic sampling localities in the Pieniny andesite line. Identification numbers are used in Table 1, in the Figures and
throughout the text.
different times even within the same intrusion. Such sampling
strategy was especially important in the quarries of the young-
er generation dykes, in order to ensure that the secular varia-
tion of the Earths magnetic field be averaged out in the over-
all paleomagnetic mean direction. Luckily, in both quarries of
the younger dykes, the contact was clearly exposed; due to
this situation, it was possible to distribute the sampling sites so
that some were very close to the contact, others inside the
dykes (the contact rock itself could not be sampled, because it
was too weathered). Samples were oriented in the field with
both, magnetic and sun compasses.
Paleomagnetic measurements and results
From each core, sister specimens were cut, measured and
demagnetized in the Paleomagnetic Laboratory of the Eötvös
Loránd Geophysical Institute of Hungary. From most samples
one specimen was AF demagnetized in several steps, till the
NRM (natural remanent magnetization) signal was destroyed
or up to 200 mT; the other specimen was thermally demagne-
tized, in increments. During thermal demagnetization, suscep-
tibility was monitored. Low-field magnetic susceptibility
anisotropy was measured for each site. We found that the de-
gree of anisotropy was low, characteristically 12 percent, the
magnetic fabric was foliated, and the susceptibility maxima
had near-vertical orientation. These features are characteristic
of tectonically un-deformed, near-vertical dykes.
AF demagnetization efficiently eliminated most of the
NRM signal. However, the magnetic vector often followed a
great circle trend and the direction had not stabilized even in
high AF fields. On the other hand, thermal demagnetization,
sometimes up to the Curie-point of hematite (680 °C), was
successful in revealing the components of the NRM.
According to the behaviour and complexity of the NRM,
the studied rocks may be subdivided into 3 groups as follows:
1. AF demagnetization is sufficient to eliminate the NRM
signal, which only has a single component (Fig. 3, specimen
PL 495A);
2. thermal method is needed to demagnetize the NRM, in-
stability sets in above the Curie-point of magnetite (Fig. 3,
specimen PL 209B);
3. only thermal demagnetization separates the components of
the complex NRM (Figs. 4, 5). Information about the identified
components for each site or locality (in the latter case the sam-
pled sites from the same locality yielded identical results) and
the method of successful demagnetization is given in Table 1.
It is important to note, that all samples from the second gen-
eration dykes (Fig. 5) belong to group 3. Their NRM is char-
acterized by a dominant reversed polarity component (compo-
nent b) and a small, but well-defined component of high
unblocking temperature (component c). The latter persists till
the Curie-point of hematite.
Not far from the quarries of the second generation dykes, in-
trusions belonging to the first generation were also sampled.
At one site near the Monument (PL 219222) and at two sites
from Czorsztyn (PL 492494 and PL 495497) the NRM had
one component, where the direction was similar to component
c of the second generation dyke throughout AF or thermal de-
magnetization. The remaining samples behaved similarly to
samples from the second generation dykes (compare Fig. 4
and Fig. 5) or they exhibited a single component NRM with
414
MÁRTON, TOKARSKI and HALÁSZ
Fig. 3. Pieniny andesites, first phase intrusions. Examples of simple NRM with CCW rotated declination (PL 495A) and with strange direc-
tion (PL 209B). In the latter, the magnetic signal became extremely unstable above 590 °C, but the unstable part is not shown in the diagram.
Left hand side: orthogonal projection, where solid/open symbols represent projections of the NRM vector onto the horizontal/vertical plane.
Right hand side: stereographic projections with all upper hemisphere data; insert: normalized NRM intensity (open symbols) and susceptibil-
ity (full symbols) as a function of temperature.
Fig. 4. Pieniny andesites, first phase intrusions. A typical example of complex NRM. Thermal demagnetization. Left hand side: orthogonal
projection of the NRM vector; the last four steps are also shown enlarged. Right hand side: change of direction on stereographic projection
(all upper hemisphere directions), with an insert of normalized intensity and susceptibility versus temperature. Key as in Fig. 3.
415
LATE MIOCENE COUNTERCLOCKWISE ROTATION OF THE PIENINY ANDESITES
Fig. 5. Pieniny andesites, second phase intrusions. A typical example of demagnetization behaviour, where three components are resolved
(see Table 1). Left hand side: orthogonal projection of the NRM vector; the last 5 steps are also shown enlarged. Right hand side: the change
of direction at high temperatures is clear on the stereographic projection (all upper hemisphere directions). Insert: normalized intensity and
susceptibility versus temperature. Key as in Fig. 3.
strange directions, which was consistent for each of the sites
(Table 1, PL 321324, 325328).
In the Szczawnica area, the Bryjarka locality was overprint-
ed in the present geomagnetic field (and is therefore not dis-
cussed further); the Jarmuta locality exhibited a strange direc-
tion. At Krocienko, no stable end point was reached on
demagnetization, but a component for each of the sampled
sites could be defined (Table 1).
When we plot all the identified NRM components (except
Bryjarka) on a stereonet, we can identify two sets of data
(Fig. 6). One is characterized by easterly declination and re-
versed polarity or in one case, westerly declination and nor-
mal polarity (Fig. 6A), so that the directions are counterclock-
wise rotated with respect to the stable European reference
direction. The other directions appear to define a great circle,
which contains the stable European reference direction for
2010 Ma (Fig. 6B).
Magnetic minerals
Detailed thermal demagnetization of the NRM has revealed
that most of the NRM unblocks below the Curie-point of
magnetite. However, in several samples another component
exists, which resides in a mineral with higher unblocking tem-
peratures. In order to obtain more information about the carri-
ers of both NRM components, we carried out IRM (isothermal
remanent magnetization) acquisition experiments, measured
Curie-points (susceptibility versus temperature curves) and
made microscopy observation on polished sections.
Fig. 6. Pieniny andesites. Paleomagnetic directions on a stereo-
graphic projection. A Components exhibiting CCW rotation with
reversed (open circles) or normal (full circle) polarity; B compo-
nents interpreted as later overprints in a stable European framework.
Open circles: vectors pointing upward; full circles: vectors pointing
downward; star: stable European reference direction calculated
from data by Besse & Courtillot (1991). The parameters of the pole
of the remagnetization great circle drawn through the isolated com-
ponents for the Pieniny andesites are: D=119°, I=3° and α
95
=7.3°.
If we include the stable European reference direction, the parame-
ters change only slightly to D=118°, I=4° and α
95
=8.7°.
Although the NRM in several samples did not unblock
completely until the Curie-point of hematite, the IRM acquisi-
tion curves suggest that the dominant magnetic mineral is
magnetically soft and there is only a weak signal from hard
416
MÁRTON, TOKARSKI and HALÁSZ
Table 1: Summary of the paleomagnetic directions (D° and I°) with (k, α
95
°) statistical parameters (Fisher 1953) from the Pieniny andes-
tites. Key: n/no: used/collected samples. Numbers with PL prefix refer to Fig. 2 and are used throughout the text. a, b, c, are the compo-
nents of the NRM when the NRM is complex. Components were defined using principal component analysis (Kent et al. 1983). In Re-
mark column the stability range of the NRM (component) is indicated.
Locality
n/no
D (°)
I (°)
k
=
95
(°)
Remark
Pieniny andesites, 1
st
phase intrusions
1 W¿ar Mts, Monument
PL 215218
a
4/4
303
+33
27
17
NRM300 °C
b
4/4
209
53
369
5
300610 °C
c
4/4
139
56
30
17
610670 °C
PL 219222
4/4
157
62
3120
2
NRM670 °C, NRM120 mT
2 Czorsztyn
PL 321324
4/4
214
+31
297
5
NRM640 °C
PL 325328
4/4
33
+40
273
6
NRM640 °C
PL 492494
3/3
140
38
292
7
NRM140 mT
PL 495197
3/3
142
45
1032
4
NRM140 mT
3 Szcsawnica,
Jarmuta Quarry
PL 209214
6/6
28
79
165
5
150590 °C
4 Szcsawnica,
Bryjarka Quarry
PL 469472
4/4
352
+49
80
10
NRM390 °C
PL 473475
3/3
357
+88
269
8
NRM25 mT
PL 476478
3/3
13
+70
465
6
NRM550 °C, NRM25 mT
5 Krocienko, Zakijowski
stream
PL 479481
3/3
312
+51
1101
4
NRM25 mT
Pieniny andesites, 2
nd
phase intrusions
6 W¿ar Mts, S. Quarry
PL 316320
a
5/5
356
+34
18
19
NRM350 °C
b
5/5
176
86
51
11
350550 (585) °C
c
4/5
87
61
36
16
585640 °C
7 W¿ar Mts, N. Quarry
PL 459468
a
5/10
331
+70
120
7
1825 mT
b
10/10
181
73
165
4
25 mT525 (575) °C
c
9/10
125
71
67
7
630670 °C
magnetic minerals in some samples (e.g. Fig. 7, PL 214,
PL 216b); the Curie-point characterizes magnetite or a some-
what oxidized magnetite (Fig. 7).
Polished sections were prepared from the specimens that
had provided the IRM acquisition and susceptibility versus
temperature curves (11 representative specimens). In all sec-
tions, magnetite was identified, both as phenocrysts and as
smaller grains in the matrix; mafic-magnetite alteration was
also observed in all sections.
Hematite as martite (in magnetite) characterizes both the
second and first generation intrusions from the W¿ar Moun-
tains (sometimes it is without structure, which suggests that
martitization occurred during the formation of magnetite in a
strongly oxidizing environment), but is not typical in the Szcza-
wnica area. Hematite also occurs in the samples from the
W¿ar Mountains (and in Jarmuta Quarry) as spots and along
fissures, but it is lacking in Bryjarka and Krocienko.
Small magnetite and hematite grains occasionally occur
together as inclusions in mafic minerals. Sulphides, mostly
chalcopyrite, are observed in all samples, although their fre-
quency is variable: they are rare in the first phase intrusions
of the W¿ar Mountains, and frequent in the second phase in-
trusions. They are also abundant in samples from Kro-
cienko.
Discussion and conclusions
Analysis of the NRM, magnetic mineralogy experiments
and inspection of polished sections did not reveal any charac-
teristic differences between the first and second phase intru-
sions. The most important common features of the two phases
are:
1. NRM components indicating counterclockwise rotation;
2. other components defining a great circle, which contains
the expected stable European paleomagnetic direction;
3. (oxidized) magnetite as the principal magnetic mineral;
4. high-temperature and hydrothermal alteration of the
magnetite (as well as other minerals, like opacitization of
amphiboles).
The component indicating counterclockwise rotation of the
second phase dykes resides in a mineral with higher unblock-
ing temperature (higher oxidation state) than magnetite; the
same is true for the first phase intrusions, except three sites
(Table 1, PL 21922, PL 49294, PL 49597), where this
component is observed in the magnetite unblocking tempera-
ture range. The enumerated common features have the follow-
ing implications:
First, the area intruded by the Pieniny andesites must have
rotated counterclockwise after formation of the 2
nd
phase
417
LATE MIOCENE COUNTERCLOCKWISE ROTATION OF THE PIENINY ANDESITES
Fig. 7. Magnetic experiments aiming at identification of the magnetic minerals in the Pieniny andesites. Second phase intrusion (PL 463)
and first phase intrusions (PL 214 with non-rotated declination only, PL 216B with complex NRM). Left hand side: isothermal remanent
magnetization (IRM) acquisition curves. Right hand side: susceptibility versus temperature curves. IRM acquisition curves show exclusively
(PL 463) or dominantly (PL 214, PL 216B) low coercivity magnetic minerals, which may be oxidized magnetite, according to the suscepti-
bility versus temperature curves, in PL 463 and PL 216B and typical magnetite in PL 214.
dykes. Second, although the samples are fresh to the naked
eye, the effects of high temperature oxidation and hydrother-
mal alteration are observed under the microscope, in samples
with a single component NRM of rotated declination as well
as in samples with complex NRM. This means that the pro-
cess responsible for overprinting postdates even the hydro-
thermal activity and may be attributed to hot fluids imprinting
partial thermoremanent magnetization on the pre-existing
thermoremanent or chemical remanent magnetization.
Normally, it is taken for granted that fresh magnetite in
andesites carries a primary magnetization, while the oxidized
varieties carry a secondary remanence. In the Pieniny andesite
line, there seems to be no correlation between NRM compo-
nents and magnetic minerals in this sense.
The non-westerly components appear to be younger than
the CCW rotated ones, since they lie along a great circle that
contains the stable European reference direction (Fig. 6B).
The andesites were, therefore, emplaced and oxidized before
418
MÁRTON, TOKARSKI and HALÁSZ
the final rotation of the area. The inferred hot fluids, on the
other hand, overprinted the NRM after the counterclockwise
rotation event.
From the tectonic point of view, the most important ques-
tion is the age of the andesites. An older than Late Badenian
age would permit us to connect the counterclockwise rotation
of the Pieniny andesites to the rotation of the Inner Western
Carpathians (and perhaps to movements in the Outer Western
Carpathians and in the Foredeep). In this case, the Upper Bad-
enian strata filling the Nowy S¹cz Basin (Fig. 1b, Oszczypko
et al. 1991) exhibiting a paleomagnetic declination (D=188°,
I=42°, k=36, α
95
=9°, based on 8 samples) which is aligned
with the stable European reference declination (8°) would sig-
nify the termination of the large scale movements of the Car-
pathians. However, recently obtained K/Ar ages for several
sites of the Pieniny andesite line (Birkenmajer & Pécskay
1999, 2000) confirm the Sarmatian age of both intrusive phas-
es (Fig. 8). These young age estimates imply that the rotation
of the Pieniny andesite line took place in post-Sarmatian
times, due to local tectonic causes. It would be tempting to
connect the rotation to the sinistral strike-slip movement
along the Pieniny Klippen Belt, which was postulated in some
tectonic models (e.g. Birkenmajer 1986 and references there-
in). Unfortunately, the strike-slip movement pre-dates a post-
Sarmatian rotation.
The present study on the Pieniny andesites reinforces the
conclusion that paleomagnetic results, even from Miocene or
younger magmatic rocks, must be treated with caution, when
based on partial demagnetization. Full demagnetization may
reveal components which are small, but well defined (like the
component with high unblocking temperature in the second
phase andesites from the Pieniny andesite line), not only in a
Fig. 8. Ages of Pieniny Mts andesites (after Birkenmajer & Pécskay 2000) and of the Neogene fill (fresh water sediment) of the Nowy S¹cz
Basin (after Oszczypko et al. 1992). The latter is dated biostratigraphically by the overlying marine strata.
specimen (Fig. 4), but also on a site level (e.g. good statistical
parameters in Table 1, components 6c and 7c). Our results
from the Pieniny andesites make clear that thermal demagneti-
zation greatly enhances the reliability of data (since AF de-
magnetization, which is routinely applied to young igneous
rocks, may not lead to the identification of all NRM compo-
nents) and demonstrates that with careful demagnetization
and component analysis it is possible to separate tectonically
significant paleomagnetic signals, even in the presence of
large overprint NRM components.
Acknowledgment: We are obliged to Krzysztof Birkenmajer
and Zoltán Pécskay for precise information on the location of
exposures. Nestor Oszczypko guided us to the Jarmuta Quarry
and was helpful with digging out our car when we were hope-
lessly lost in the Carpathian mud. Ania wierczewska and
Krzysztof Nejbert supervised the petrographic analysis, car-
ried out by Dóra Halász. This work was financially supported
by the exchange program between the Polish and Hungarian
Academies and by the Hungarian Scientific Research Fund
(OTKA) Project No. T034364.
References
Besse J. & Courtillot V. 1991: Revised and synthetic apparent polar
wander paths of the African, Eurasian, North American and In-
dian Plates, and true polar wander since 200 Ma. J. Geophys.
Res. 96, B3, 40294050.
Birkenmajer K. 1986: Stages of structural evolution of the Pieniny
Klippen Belt, Carpathians. Studia Geol. Pol. 88, 732.
Birkenmajer K. 1996: Miocene andesite intrusions in the Pieniny
area, their geological forms and their distribution basing on
419
LATE MIOCENE COUNTERCLOCKWISE ROTATION OF THE PIENINY ANDESITES
geological and magnetic studies. Geol. 22, 1525 (in Polish).
Birkenmajer K. & Nairn A.E.M. 1968: Paleomagnetic studies of
Polish rocks. III. Neogene igneous rocks of the Pieniny Moun-
tains, Carpathians. Ann. Soc. Géol. Pologne 38, 475489.
Birkenmajer K. & Pécskay Z. 1999: K-Ar dating of the Miocene
andesite intrusions, Pieniny Mts, West Carpathians, Poland.
Bull. Pol. Acad. Sci., Earth Sci. 47, 155169.
Birkenmajer K. & Pécskay Z. 2000: K-Ar dating of the Miocene
andesite intrusions, Pieniny Mts, West Carpathians, Poland: a
supplement. Studia Geol. Pol. 117, 725.
Birkenmajer K., Delitala M.C., Nicoletti M. & Petrucciani C. 1987:
K-Ar dating of andesite intrusions (Miocene), Pieniny Klippen
Belt, Carpathians. Bull. Pol. Acad. Sci., Earth Sci. 35, 1119.
Fisher R. 1953: Dispersion on a sphere. Proc. Roy. Soc. London Ser.
A. 217, 295305.
Kent J.T., Briden J.C. & Mardia K.V. 1983: Linear and planar struc-
ture in ordered multivariate data as applied to progressive de-
magnetization of palaeomagnetic remanence. Geophys. J. Roy.
Astron. Soc. 75, 593621.
Kruczyk J. 1970: Paleomagnetic investigations of the Mt. W¿ar
andesites. Publ. Inst. Geophys. Pol. Acad. Sci. 35 (in Russian).
Mahe¾ M. 1986: Geological structure of the Czechoslovak Car-
pathians. Part I: Paleoalpine units. VEDA, Bratislava, 1510 (in
Slovak).
Márton E., Tokarski A. & Soták J. 1998a: Magnetic anisotropy, sed-
imentary transport and paleomagnetic directions in the Inner
Carpathian flysch. 6
th
New Trends in Geomagnetism.
Márton E., Tokarski A. & Soták J. 1998b: Inner West Carpathian
flysch: relation between paleomagnetic directions, principal
susceptibility axes and sedimentary transport direction. Car-
pathian-Balkan Geological Association, XVI Congress. Ab-
stracts, 370.
Márton E., Mastella L. & Tokarski A.K. 1999a: Large counterclock-
wise rotation of the Inner West Carpathian Paleogene Flysch
evidence from paleomagnetic investigation of the Podhale
Flysch (Poland). Phys. Chem. Earth (A) 248, 645649.
Márton E., Tokarski A.K. & Galicia Tectonic Group 1999b: North-
ward migration of North ALCAPA boundary during Tertiary ac-
cretion of the Outer Carpathians Paleomagnetic Approach.
Joint Meeting of EUROPROBE TESZ, PANCARDI and
GeoRift Projects. Rom. J. Tect. Region. Geol. 77, suppl. 1, 22.
Márton E., Tokarski A.K. & Nemèok M. 2000: Paleomagnetic con-
straints for the accretion of the tectonic units at the stable Euro-
pean margin, north of the western Carpathians. EGS XXV
General Assembly. Geophys. Res. Abstr. 2, 56.
Márton E., Tokarski A.K., Scholger R., Krejèí O., Stingl K. & Mau-
ritsch H.J. 2001: Molasse in front of the Outer West Car-
pathians: growing evidence for counterclockwise rotation.
Pannonian Basin, Carpathian and Dinaride system. Geological
Meeting on Dynamics of Ongoing Orogeny, PANCARDI Ab-
stracts. CP-19.
Oszczypko N., Stuchlik L. & Wójcik A. 1991: Stratigraphy of fresh-
water Miocene deposits of the Nowy S¹cz basin, Polish West-
ern Carpathians. Biul. Pol. Acad. Sci., Earth Sci. 39, 433445.
Oszczypko N., Olszewska B., lêzak J. & Strzêpka J. 1992: Mi-
ocene marine and brackish deposits of the Nowy S¹cz basin
(Polish Western Carpathians) New lithostratigraphic and
biostratigraphic standards. Biul. Pol. Acad. Sci., Earth Sci. 40,
8396.
Plaienka D., Grecula P., Puti M., Kováè M. & Hovorka D. 1997:
Evolution and structure of the Western Carpathians: an over-
view. In: Grecula P., Hovorka D. & Puti M. (Eds.): Geological
evolution of the Western Carpathians. Miner. Slovaca Mono-
graph, Bratislava, 124.
Rögl F. 1996: Stratigraphic correlation of the Parathethys Oligocene
and Miocene. Mitt. Gesell. Geol. Bergbaustud. (Wien) 41, 6573.
wierczewska A. & Tokarski A.K. 1998: Deformation bands and
the history of folding in the Magura nappe, Western Outer Car-
pathians (Poland). Tectonophysics 297, 7390.
Tokarski A.K. & wierczewska A. 1998: History of folding in the
Magura nappe, Outer Carpathians, Poland. In: H.-P. Ross-
manith (Ed.): Mechanics of faulted and jointed rock. Balkema
125130.
Wójcik A., Szyd³o A., Marciniec P. & Nescieruk P. 1999: The fold-
ed Miocene of the Andrychów region. Biul. Pol. Geol. Inst.
387, 191195.