GeolCarp_Vol61_No3_211

www.geologicacarpathica.sk

GEOLOGICA CARPATHICA, JUNE 2010, 61, 3, 211—225 doi: 10.2478/v10096-010-0012-5

Reconstruction of Cenozoic paleostress fields and revised tectonic

history in the northern part of the Central Western Carpathians

(the Spišská Magura and Východné Tatry Mountains)

RASTISLAV VOJTKO , EVA TOKÁROVÁ†, UBOMÍR SLIVA and IVANA PEŠKOVÁ

Department of Geology and Paleontology, Faculty of Natural Sciences, Comenius University, Mlynská dolina G, 842 15 Bratislava,

Slovak Republic; vojtko@fns.uniba.sk; sliva@fns.uniba.sk; peskova@fns.uniba.sk

(Manuscript received June 29, 2009; accepted in revised form December 11, 2009)

Abstract: This study investigates the chronology of paleostress evolution and faulting in the northern part of the
Central Western Carpathians (Spišská Magura and Východné Tatry Mts). Paleostress analysis of brittle and semibrittle
structures of the Eocene—Oligocene succession of the Central Carpathian Paleogene Basin (CCPB) supplemented by
measurements in the Triassic sequence of the Krížna Nappe, revealed the existence of six tectonic regimes during the
Cenozoic. Orientation of the paleostress field before the deposition of the CCPB was characterized by the E-W oriented
compression. After this compression, the paleostress field rotated approximately 40—50°, and NW—SE directed com-
pression took place in the Early Miocene. During the latest Early Miocene, the extensional tectonic regime with fluctua-
tion of

orientation between NW-SE to NE-SW dominated. The Late Badenian—Pannonian is characterized by a new

compressive to strike-slip tectonic regime during which the principal maximum stress axis

progressively rotated

from a NW-SE to a NE-SW position. Uplift and tilting of the Tatra Massif took place during this stage. The neotectonic
stage (Pliocene to Holocene) is characterized by extensional tectonic regime with the two directions of tension. The first
one is oriented in the E-W direction and could be considered older and the second one, NNW-SSE tension is considered
to be Late Pliocene to Quaternary in age. In general, orientation of the stress fields shows an apparent clockwise rotation
from the Oligocene to Quaternary times. This general clockwise rotation of the Oligocene to Quaternary paleostress
fields could be explained by both the effect of the counter-clockwise rotation of the ALCAPA microplate and by the
regional stress field changes.

Key words: Central Western Carpathians, Spišská Magura Mts, Východné Tatry Mts, structural analysis, neotectonics,
paleostress reconstruction, fault-slip data.

Introduction

The Spišská Magura Mts – are situated in the northern part
of the Central Western Carpathians (CWC, Fig. 1). They are
surrounded by the Východné Tatry Mts and Levočské vrchy
Mts in the south, by the Pieniny Klippen Belt in the north-
east and the Podhale Basin in the west. The studied area con-
sists predominantly of the Eocene to lowermost Miocene
sedimentary succession of the Central Carpathian Paleogene
Basin (CCPB).

The tectonic evolution of the northern part of the Central

Western  Carpathians  and  its  surroundings  has  been  recon-
structed  using  data  from  over  350  fault  slips,  90  fold  axes
and 200 tension gashes. The collected data have been used to
determine  paleostress  field  orientation  and  evolution.  The
majority  of  studied  outcrops  are  in  the  bedrock  exposures
along  the  Biela  Voda,  Javorinka  and  Biela  rivers  and  their
tributaries.  Eocene  to  Oligocene  rocks  of  the  CCPB  in  this
area  are  faulted,  fractured  and  folded.  Most  fault  surfaces
contain one or more sets of striae produced during different
deformation episodes. The superposition of striae was useful
for  the  separation  of  faults  into  the  homogeneous  groups.
The  investigated  area  offers  quite  a  good  opportunity  to
study brittle deformation and to attempt the determination of
the states of stress associated with the faulting and folding.

A normal dip-slip movement along fault zones of the moun-

tain  front  and  related  folding  of  Paleogene  sedimentary  se-
quences during the Neogene was a common view of geologists
in the last century (Gross 1973; Gross et al. 1980; Mahe  1986).
However, new research into the Cenozoic tectonics in the Cen-
tral Western Carpathians pointed out the importance of strike-
slip and oblique-slip faulting developed during transpressional
and  transtensional  tectonic  regimes.  During  these  tectonic  re-
gimes,  varied  tectonic  structures  (faults,  folds,  extensional
veins, stylolites etc.) have been recorded in the host rocks.

The purpose of this paper is (a) to describe the regional and

local  geological  settings,    fault-slip  and  fold  measurements
and determinations that were made, (b) to summarize the re-
sults of fault and fold measurements and their kinematic deter-
minations,  and  (c)  to  present  the  results  of  dynamic  analysis
oriented  predominantly  to  the  paleostress  field  determination
by  a  simple  geometric  analysis  based  on  the  assumption  of
Bott  (1959)  and  testing  for  rupture  and  friction  laws;  shear
stress  vs.  normal  stress  (Angelier  1979,  1994).  This  paper
summarizes knowledge concerning the direction and distribu-
tion of paleostress axes determined from fault-slip data, fold,
tension  gashes  and  relationships  of  mesostructures  observed
in  the  field.  However,  we  are  dealing  neither  with  a  detailed
kinematic  interpretation  of  the  stress-induced  deformation,
nor with the magnitudes of the stress tensor parameters.

Reconstruction of Cenozoic paleostress fields and revised tectonic

history in the northern part of the Central Western Carpathians

(the Spišská Magura and Východné Tatry Mountains)

213

CENOZOIC PALEOSTRESS FIELDS AND REVISED TECTONIC HISTORY OF CENTRAL W CARPATHIANS

Geological setting

The Western Carpathians extend from the eastern end of

the Eastern Alps toward the northeast, and are divided by the
Pieniny  Klippen  Belt  into  the  External  and  Central  Western
Carpathians  (e.g.  Andrusov  1958;  Andrusov  et  al.  1973;
Plašienka  1999).  The  investigated  region  has  a  complicated
geological structure and, being located at this boundary zone,
is  affected  predominantly  by  strong  strike-slip  deformation
along  this  zone  (Mastella  1975;  Ratschbacher  et  al.  1993;
Kováč & Hók 1996; Mastela et al. 1996; Marko et al. 2005).

The External Western Carpathians consist predominantly

of  Lower  Cretaceous  to  Lower  Miocene  flysch  formations
deposited  on  an  oceanic  crust  (e.g.  Oszczypko  1992,  1998;
Oszczypko-Clowes  &  Oszczypko  2005;  Golonka  et  al.  2005
for the pre-Oligocene evolution) and/or a thinned continental
crust  (e.g.  Winkler  &  Slączka  1992; Jurewicz  2005).  During
the Late Oligocene to Middle Miocene subduction, the flysch
formations  were  detached  from  their  basement  and  thrust
northward over the European Platform (Oszczypko & Ślączka
1989; Kováč et al. 1993; Plašienka et al. 1997; Kováč 2000).

The Pieniny Klippen Belt is a large-scale narrow shear zone

forming the boundary which separates the accretionary wedge
of the External Western Carpathians and the Central Western
Carpathians. This zone includes the Kysuce, Czorsztyn, Orava
and Klape successions, and is composed of Jurassic to Creta-
ceous rocks (Birkenmajer 1986; Jurewicz 2005; Plašienka &
Jurewicz 2006; Plašienka et al. 2007). The deformation began
during the Late Cretaceous (documented by synorogenic flysch
formation),  but  the  main  brittle  deformation  in  the  Pieniny
Klippen Belt occurred during the Paleogene to Neogene. The
Eocene  to  Oligocene  was  characterized  by  dextral  transpres-
sion  which  changed  to  Neogene  dextral,  later  sinistral
transpression and finally to sinistral transtensional tectonic re-
gimes (Fodor 1995; Kováč 2000; Pešková et al. 2009).

The investigated territory of the Tatra Mts is located in the

Central Western Carpathians which is composed of the Tatric
and Fatric Units (e.g. Nemčok et al. 1993, 1994). The Tatric
Unit is formed by the Variscan basement which consists of the
Lower  Paleozoic  metamorphic  sequences  (para-  and  ortho-
gneisses, mica schist and migmatite). These metamorphic se-
quences  have  been  intruded  by  the  Variscan  granitoids.  The
basement  is  covered  by  an  autochthonous  sedimentary  se-
quence with a stratigraphic range from Permian to mid-Creta-
ceous. The Tatric Unit is overthrust by the Fatric Unit (Krížna
Nappe), which was derived from the area between the Tatric
and Veporic realms (Biely & Fusán 1967). It consists mainly
of  the  Triassic  to  middle  Cretaceous  sedimentary  sequences
(the  Anisian  Gutenstein  Limestone  and  Carnian  Carpathian
Keuper are present in the study area). The age of the thrusting
is  documented  by  the  deposition  of  synorogenic  flysch  (the
Poruba  Formation)  during  the  Albian  to  Early  Turonian  in
the  Tatric  cover  sequences  (Andrusov  et  al.  1973).  The  up-
permost nappe structure is formed by the Hronic Unit (Choč
Nappe)  which  is  not  present  in  the  studied  area.  These
nappes form a substratum of the Eocene to earliest Miocene
sedimentation of the CCPB.

The Central Carpathian Paleogene Basin (Podtatranská sku-

pina Group in the sense of Gross et al. 1984, 1993) is extended

over approximately 9,000 km

. Its sedimentary succession is

predominantly  composed  of  deep-marine  siliciclastic  sedi-
ments  several  hundred  meters  to  several  kilometers  thick
(Soták et al. 2001). The CCPB is interpreted as a forearc basin
situated  behind  the  Outer  Carpathians  accretionary  wedge
(Royden & Báldi 1988; Tari et al. 1993; Kázmér et al. 2003).
The basement and the southern boundary of the CCPB is com-
posed of the Central Carpathian units, and its northern bound-
ary  is  the  Pieniny  Klippen  Belt  (Fig. 1),  which  represents  a
transpressional strike-slip zone related to a microplate bound-
ary (Balla 1984; Csontos et al. 1992; Plašienka 1999). The in-
verted Paleogene basin of the Spišská Magura Mts is situated
between  the  Tatra  Mts  and  the  Pieniny  Klippen  Belt.  In  the
east, it is bounded by the Ružbachy fault and by the Mesozoic
complexes of the Ružbachy Massif and in the west it gradual-
ly  passes  into  the  Podhale  Basin  (Figs. 1,  2).  The  Paleogene
complex of the Spišská Magura Mts is a part of the CCPB and
is  formed  by  the  Borové  Formation,  Huty  Formation  and
Zuberec Formation (Marschalko & Radomski 1970; Gross et
al. 1984; Janočko & Jacko 1999; Janočko et al. 2000a,b). The
sedimentary deposits of the lower part of the Huty Formation
in  the  Spišská  Magura  Mts  are  atypical  and  this  formation
can be considered to be coeval with the Šambron (Szaflary)
Member  developed  in  northern  part  of  the  Polish  Podhale
Basin (Watycha 1959; Westwalewicz & Mogilska 1986; Gedl
2000; Soták et al. 2001). This member can be related to global
cooling and fall of the sea level (Janočko & Jacko 1999; Soták
et al. 2001).

The hinge zone of the Podhale Synclinorium is composed

of the Brzegi Member which is considered to be a distal facies
of the Biely Potok Formation (Fig. 2; Watycha 1959; Gedl
2000; Sliva 2005). The sediments are Bartonian to Early Mio-
cene in age (Olszewska & Wieczorek 1998; Gedl 2000).

Methods

Fault-slip and paleostress analysis

Faults and striae on the fault surfaces are very often present

in rock masses and therefore kinematic and dynamic analysis
of  fault-slip  data  is  a  very  popular  tool  for  reconstruction  of
the paleostress fields. Standard procedures for brittle fault-slip
analysis  and  paleostress  reconstruction  are  now  well  estab-
lished (Etchecopar et al. 1981; Michael 1984; Angelier 1990,
1994). In our work, the obtained data were registered into the
NeotAct  PostgreSQL  database  and  were  pre-processed  using
the LoCon software developed at the Department of Geology
and Paleontology, Comenius University by Rastislav Vojtko.
Later, these data were used in the Dieder and Shear modules
using  the  TENSOR  software  package  developed  by  Damien
Delvaux  (Delvaux  1993;  Delvaux  &  Sperner  2003).  The
DIEDER program is an improved version of the Right Dihe-
dron method of Angelier & Mechler (1977). It provides a de-
termination of the four parameters of the reduced stress tensor
and  also  allows  a  preliminary  separation  of  the  fault  popula-
tion into a homogeneous subset, broadly compatible with the
computed  stress  tensor.  Note  that  only  complete  fault-slip
data,  fault  plane  with  slickenside  lineation  and  known  slip

214

VOJTKO, TOKÁROVÁ, SLIVA and PEŠKOVÁ

sense, are considered (for more details see Delvaux & Sperner
2003). The SHEAR program is an inversion method which is
based on the assumption of Bott (1959) that slip on a plane oc-
curs in the direction of the maximum resolved shear stress.
Fault data were inverted to obtain the four parameters of the
reduced stress tensor:

(maximum principal stress axis),

(intermediate principal stress axis) and

(least principal

stress axis) and the ratio of principal stress differences is ex-
pressed by the formula:

Φ = (σ

—

)/(

—

This parameter

Φ defines the shape of the stress ellipsoid

(Angelier 1989, 1994). The interpretation of results is also dis-
cussed  for  two  important  aspects:  the  quality  assessment  in
view  of  the  World  Stress  Map  standards  (Zoback  1992;
Sperner et al. 2003) and the numerical expression of the stress
regime as Stress Regime Index for regional comparisons and
mapping  (Delvaux  &  Sperner  2003).  In  accordance  with  the
new  ranking  scheme  for  the  World  Stress  Map  project  the
quality ranges from A (best) to E (worst), and is determined as
a function of threshold values of a series of criteria. The stress
regime can be expressed numerically using an index

Φ’, rank-

ing from 0.0 to 3.0 and defined as follows (see Delvaux et al.
1997):

Φ’=Φ where σ

is vertical (extensional stress regime);

Φ’=2—Φ where σ

is vertical (strike—slip stress regime);

Φ’=2+Φ where σ

is vertical (compressional stress

regime).

Orientations of the stress axes (S

– maximum horizontal

compression axis, S

– minimum horizontal compression

axis, and S

vertical axis), and the stress regime (

Φ’between

0—1 for extensional regime, 1—2 for strike-slip regime, and
2—3 for compressional regime) are fully described by the
average S

azimuth (as defined in the World Stress Map by

Müller et al. 2000) and the average stress regime index

Φ’

as defined above.

These methods (especially the inversion method) have some

limitations which were the subject of criticism and its results
were under discussion in specific situations (e.g. Dupin et al.
1993; Pollard et al. 1993; Nieto-Samaniego & Alaniz-Alvarez
1996; Twiss & Unruh 1998; Maerten 2000; Roberts & Ganas
2000). The basic point of stress computation by the inversion
method is that regional stress tensor is spatially and temporal-
ly homogeneous in the whole-rock mass. These computations
are influenced generally by the three effects which can occur
in palaeostress analysis: 1) effect of ratio between the width
and length of a fault; 2) effect of the Earth’s surface (topoef-
fect); 3) effect of interaction between two or more faults (for
further information see Pollard et al. 1993). These effects can
misinterpret results of the paleostress analysis, but their in-
fluence is in most cases slight (Angelier 1994; Vojtko 2003).

Geometrical analysis of folds

The analysis of fold orientation was carried out using bed-

ding planes, fold axes and planes measured during the field
investigation. The principal deformational axes show the re-
lationship to the fold geometry. The principal strain axis (A)

Fig. 2. Lithostratigraphical divisions of the Central Carpathian Pa-
leogene Basin fill with respect to Slovak and Polish terminology
(c.f. Soták 2001).

216

VOJTKO, TOKÁROVÁ, SLIVA and PEŠKOVÁ

which has the value

ρ 104/0° with rotational angle +33° us-

ing the equation:

ρ=dip direction (S

) ± 90°.

A similar procedure was utilized for all sites disrupted by

the  tilting  and  allowed  to  separate  fault  structures  into  two
groups  on  the  basis  of  relation  to  tilting.  Thus  the  rotated
faults are older than the unrotated faults. The older faults have
been divided into three homogeneous subsets and the younger
faults  also  into  three  homogeneous  subsets.  After  this  proce-
dure,  it  was  possible  to  compute  reduced  paleostress  tensors
correctly (Fig. 3).

Data

Data obtained in the field from fault-slips, folds and exten-

sional veins were used to reconstruct paleostress evolution in
the study area. Data, collected in the Paleogene and Mesozoic
sedimentary sequences, provide evidence that major deforma-
tional structures of the polyphase evolution resulted from re-
verse, strike-slip and normal faulting during the Neogene.

Meso-scale brittle failure structures used to study the

state(s) of paleostress associated with faulting were measured
at 14 sites. Fault orientation measurements and slip determina-
tions made in the field, and results of geometrical and mathe-
matical data analyses are presented in Fig. 4.

The fold data were measured mainly in the Eocene to Oligo-

cene sedimentary sequences of the CCPB, less in the Krížna
Nappe. The folds were used for determining the orientation of
maximum  shortening.  Statistically,  the  mean  trend  of  fold
axes  is  75/11°  (calculated  from  both  bedding  attitudes  and
fold axes measurements), the data are quite robust and suggest
the  NNW-SSE  shortening  with  maximal  fluctuation  of  ±30°
(Fig. 5a,  Table 1).  The  fold  axial  planes  are  mainly  inclined
towards the north and they are considered to be generated by
the  “backthrust”  tectonics  with  a  general  southern  vergency
during the Early and predominantly Middle Miocene (D

and

stages). The fold set is almost pervasively developed

along the northern boundary of the Tatra Mts and south of
the Pieniny Klippen Belt. The folds are open to close with in-
terlimb angles from 30° to 70°. The folds are often associated
with the reverse faults (Fig. 6f).

Extension directions inferred from the total orientation pat-

tern of extension vein walls and fibres show a preferred orien-
tation  of  tension  at  the  azimuth  of  78°  (Fig. 5b),  less  at  the
azimuth of 118°. We measured extensional veins at 16 locali-
ties and their orientations were also used to estimate deforma-
tional  history  and  state  of  paleostress.  Characteristically,  the
least  principal  axis  determined  from  all  veins  (formed
throughout the deformation history) is generally perpendicular
to the most frequently observed NW-SE compresional axis of
the  transpressional  tectonic  regime.  Development  of  the
NNW-SSE vein system is older or partly synchronous with re-

Table 1: Orientation of principal fold axes. Explanations: Site – Code of locality; n – number of fold data used for determination of stress
orientations; n

– total number of fold data measured; A – axis of maximum elongation; B – intermediate axis (fold axis) and C – axis of

maximum shortening.

Site n n

C B A

Tatranská Javorina — Javorinka valley (GPSinfo: N49°12'13", E019°32'57"), the Brzegy Beds
PPTJA03A

172/27

076/11

326/61

Tatranská Javorina – Biela Voda (GPSinfo: E20°07'54''; N49°17'29''), the Brzegy Beds
PPTJA04A 9 13

150/20

58/5

313/70

PPTJA04B 3 13

181/9

90/5

329/80

PPTJA04C 1 13 – – –
Ždiar — Biela creek (GPSinfo: E20°18'04''; N49°15'21''), the Huty Formation
PPZDI06A

180/18

96/18

228/64

PPZDI06B

35/22

291/31

154/50

Lendak — Rieka stream (GPSinfo: E20°20'26''; N49°15'38''), the Huty Formation
KKLEN01A 4 4 151/39

57/6

320/50

Osturňa IV. (GPSinfo: E20°15'54''; N49°20'22''), the Zuberec Formation
KKOST04A

313/16

45/9

163/72

KKOST04B 1 12

182/0

272/17

95/73

Podspády — Príslop creak (GPSinfo: E20°11'33''; N49°17'02''), the Zuberec Formation
PPTJA01A

343/16

77/12

201/70

PPTJA01B

51/0

141/17

325/73

Podspády – Nový creak (GPSinfo: E20°10'24''; N49°16'18''), the Borové Formation
PPTJA02A

166/35

272/22

28/47

Ždiar — Bachledova valley (GPSinfo: E20°18'28''; N49°16'13''), the Huty Formation
PPZDI02A

172/27

76/11

326/61

Ždiar — Tokáreň mount (GPSinfo: E20?16'02''; N49?15'38''), the Huty Formation
PPZDI08A

59/0

149/7

329/83

Ždiar — Strednica (GPSinfo: E20?13'43''; N49?15'56''), the Huty Formation
PPZDI07A

172/27

76/11

326/61

Jurgów — Bialka (GPSinfo:E20°07'15''; N45°22'45'' ), the Brzegy Beds
PPJUR01A

114/16

272/73

22/6

PPJUR01B

335/1

65/8

237/82

218

VOJTKO, TOKÁROVÁ, SLIVA and PEŠKOVÁ

spect to tilting, whereas the second NNE-SSW vein system is
synchronous with, or postdates tilting.

Review of the Cenozoic stresses and chronology of

faulting

The evolution of the orogen, the age of the principal defor-

mational events, basin evolution and destruction, and also the
relative chronology of these structures are also important pre-
conditions of successful paleostress analysis. The separated
phases in the study area were also compared to regions which
have similar Oligocene to Quaternary evolution (Kováč &
Hók 1996; Fodor et al. 1999; Jacko & Janočko 2000; Pešková
et al. 2009).

Tectonic regime before and during the sedimentation of the
CCPB sedimentary sequence (Late Cretaceous to Oligocene)

The oldest recorded deformational phase (D

) is character-

ized by the E—W compression and N—S extension (Paleocene—
pre-Middle  Eocene).  This  strike-slip  tectonic  regime  was
determined  predominantly  in  the  Mesozoic  rocks  of  the
Krížna  Nappe  (Figs. 4a,  7)  where  it  is  very  common.  Com-
pressive  stresses  were  resolved  mainly  by  movements  along
WNW-ESE trending sinistral and WSW-ENE trending dextral
shears. These faults are pre- and synsedimentary with respect
to the CCPB, because of the similar orientation of paleostress
field  was  seldom  observed  in  sites  located  in  the  CCPB
(Fig. 7), where the principal compressional axis (

) is slight-

ly rotated (about 30°) into the WNW-ESE position.

Tectonic regimes after sedimentation of the CCPB sedimen-
tary sequence and before tilting of the Tatra Massif (Eggen-
burgian to Badenian)

After deposition of the CCPB sequences, the new strike-slip

to compressive deformational phase (D

) characterized by

Fig. 5. Contour plot of all measured and constructed fold axes and Rose
diagram of extensional veins. a – Contour plot of fold axes. Report
counting: number of data points 98, number of points in maximum
30 (= 30.61%), number of contours 8, distance between contours
3.75 (= 3.83 %). Contours shown data points in %: 3.75 pts = 3.83 %,
7.50 pts=7.65 %, 11.25 pts=11.48 %, 15.00 pts=15.31 %, 18.75 pts=
19.13 %, 22.50 pts = 22.96 %, 26.25 pts = 6.79 %, 30.00 pts=30.61 %.
Lambert projection, lower hemisphere. b – Rose diagram of exten-
sional veins. Report rose: total data 204, class interval 15°, symmetri-
cal (0—180°) non-weighted data, and maximum 20.10 %.

NW-SE  compression  and  NE-SW  tension  started  in  the
Eggenburgian  (Table 2).  This  is  the  oldest  tectonic  regime
which  was  well  identified  in  the  Oligocene  sediments
(Fig. 7). The principal maximum (

) and the least (

) prin-

cipal stress axes were subhorizontal, while the principal in-
termediate axis (

) was in subvertical position. This phase is

predominantly  characterized  by  N-S  oriented  sinistral  strike-
slip  and  W-E  oriented  dextral  strike-slip  faults,  sporadically
with NE-SW trending reverse faults. Nice examples of this de-
formation are Zakopane – Biały Creek, Ždiar – Blaščatská
dolina  Valley,  Tatranská  Javorina  –  Javorinka  and  Jurgów
localities.

The extensional tectonic regime (D

) occurred at the end

of this deformational phase and can be divided into two sub-
phases. The older one is dominantly NE-SW oriented ten-
sion (D

) and the second one is generally oriented in a

NNW-SSE direction (D

). Note that the evaluation of the

subphase chronology was solved using successive fault slips
where the older fault population is offset by younger faults.
The NE-SW tension is poorly preserved and is considered to
be the final stage of the NW—SE compression (Fig. 7). The
tension is characterized predominantly by neoformed normal
and less by inherited oblique-normal faults (Fig. 6c).

Tectonic regimes during and after tilting of the Tatra Massif
(Sarmatian to Quaternary)

During the tilting of the Tatra Massif a new compressional

to transpressional tectonic regime (D

) occurred. Evolution

of this tectonic regime is complex, but generally consists of
two subphases which were tenuously dated at Sarmatian to
Pannonian.

The first subphase (D

) is mainly characterized by the

compressional tectonic regime with orientation of the princi-
pal  maximum  stress  axis  in  the  NNW-SSE  direction.  The
stress relaxed on the newly formed E-W conjugate reverse or
NW-SE  dextral  strike-slip  faults  (Fig. 4d).  Fault  structures
activated during this subphase were observed at many places
in  the  study  area  (Fig. 7,  Table 2)  and  are  accompanied  by
remarkable folds (Fig. 5a). This deformation event occurred
just  before  the  tilting  of  the  Tatra  Massif.  The  conspicuous
reverse faulting with SSE vergence dominates this deforma-
tional  stage  (Fig. 6a,b,d)  which  is  connected  with  back-
thrusting  in  the  northern  part  of  the  Central  Western
Carpathians  (e.g  Plašienka  et  al.  1998;  Marko  et  al.  2005;
Pešková  et  al.  2009).  Deformation  is  also  characterized  by
widespread  folding  under  semi-brittle  to  brittle  conditions.
Generally, the folds are open to close.

The predominantly compressional tectonic regime was

continuously followed by a pure transpressional tectonic re-
gime of the second subphase (D

) which occurred during

the  final  stage  of  the  Tatra  Massif  tilting.  During  this  N-S
compression and perpendicular tension, the NNW—SEE dex-
tral and NNE—SSW sinistral strike slip faults were activated
as  newly  formed  or  inherited  on  weakness  planes.  This
deformation  is  very  conspicuous  at  many  localities  (Fig. 7,
Table 2).

The preceding deformational phase (D

) most likely

passed continuously into a transtensional tectonic regime

221

CENOZOIC PALEOSTRESS FIELDS AND REVISED TECTONIC HISTORY OF CENTRAL W CARPATHIANS

the second one is ENE—SWS oriented tension (D

) which is

considered  to  be  younger  than  the  previous  one.  However,
there are no direct data to prove this assumption. A Pliocene
to Quaternary extensional tectonic regime was also observed
in  the  northern  part  of  the  Orava  region  (Pešková  et  al.
2009).  These  deformation  subphases  have  been  recorded  at
many  localities  (Fig. 7)  and  their  reduced  stress  tensors  are
described in Table 2.

Site n n

α Q Φ'

Ždiar — Blaščatská dolina quarry (GPSinfo: E20°17'13''; N49°16'11''), the Huty Formation

PPZDI01A

107

317/5

204/78

48/11

0.14

11.73

1.86

PPZDI01B 13 107 106/85 262/4 352/3 0.36

4.19 C 0.36

PPZDI01C

107

98/74

226/9

318/12

0.51

3.47

0.51

PPZDI01D

107

172/4

81/6

298/82

0.39

7.44

2.39

PPZDI01E 32

107 351/6 122/82 261/7 0.12

7.21 A

1.88

PPZDI01F

107

332/0

62/16

241/7

0.25

7.78

2.25

PPZDI01G

107

190/78

62/7

331/9

0.38

2.54

0.38

PPZDI01H

107

126/83

2340/6

250/4

0.41

8.19

0.41

Ždiar — Bachledova dolina quarry (GPSinfo: E20°18'28''; N49°16'13''), the Huty Formation

PPZDI02A

44/77

247/11

156/4

0.31

8.14

0.31

PPZDI02B

278/74

145/11

53/11

0.58

11.59

0.58

PPZDI02C

61/74

314/5

222/16

–

PPZDI02D

257/25

153/27

9/58

–

PPZDI02E

351/70

253/3

162/20

0.52

6.03

0.52

PPZDI02F

126/73

321/17

230/4

0.49

7.82

0.49

Tatranská Javorina — Biela Voda (GPSinfo: E20°07'54''; N49°17'29''), the Zuberec Formation

PPTJA04A

216/82

44/7

314/1

0.43

6.94

0.43

PPTJA04B

335/10

66/7

191/78

0.40

10.17

2.40

PPTJA04C

166/2

76/2

218/88

0.72

5.30

2.72

PPTJA04D

195/77

22/13

292/2

0.21

4.31

0.21

Podspády — Nový creek (GPSinfo: E20°10'24''; N49°16'18''), the Huty Formation

PPTJA02A

109/38

206/8

306/51

–

PPTJA02B

160/52

206/8

356/37

–

Podspády — Príslopský creek (GPSinfo: E20°11'33''; N49°17'02''), the Zuberec Formation

PPTJA01A

105/70

272/20

3/4

–

PPTJA01B

4/16

273/2

176/74

–

Tatranská Kotlina — quarry (GPSinfo: E20°18'49''; N49°13'53''), the Gutenstein Limestone

PPVTA01A

91/0

1/83

181/7

0.20

8.07

1.8

PPVTA01B

140/7

231/10

15/78

–

KKLEN01A

169/76

47/7

316/12

0.74

6.60

0.74

Ždiar — road (GPSinfo: E20°16'30''; N49°16'13''), the Carpathian Keuper Formation

PPZDI03A

284/38

107/52

15/1

0.62

16.01

1.38

PPZDI03B

246/74

118/10

26/13

0.41

4.70

0.41

PPZDI03C

265/88

21/1

111/2

0.37

12.8

0.37

PPZDI03D

181/20

294/47

76/36

0.36

4.68

0.36

PPZDI03E

1/22

96/12

212/65

0.35

8.47

2.35

PPZDI03F

203/17

324/60

105/25

0.22

10.56

1.78

Ždiar — Biela (GPSinfo: E20°18'09''; N49°15'12''), the Carpathian Keuper Formation

PPZDI04A

329/11

236/13

98/73

0.47

15.82

2.47

PPZDI04B

31/85

206/5

296/0

0.50

9.57

0.5

Ždiar — Biela (GPSinfo: E20°18'04''; N49°15'21''), the Borové & Huty Formations

PPZDI06A

150/6

241/11

29/77

0.47

5.20

2.47

Ždiar — Tokáreň (GPSinfo: E20°16'02''; N49°15'38''), the Tokáreň Beds

PPZDI08A

168/23

19/64

263/12

0.51

6.99

1.49

PPZDI08B

160/78

349/12

259/2

–

Jurgów (GPSinfo: E20°16'02''; N49°15'38''), the Brzegy Beds

PLJUR01A

114/16

272/73

22/6

–

PLJUR01B

335/1

65/8

237/82

–

Table 2: Paleostress tensors from fault slip data. Explanations: Site – Code of locality; n – number of fault used for stress tensor determina-
tion; n

– total number of fault data measured; S1=

σσσσσ

, S

σσσσσ

and S

σσσσσ

– azimuth and plunge of principal stress axes; R=

Φ – stress ratio

—S

);

αα

αα–mean slip deviation (in °); Q – quality ranking scheme according to the World Stress Map Project (Sperner et al. 2003);

R’ – tensor type index as defined in the text (for further information see Delvaux et al. 1997).

Discussion

Fault-slip analysis and paleostress reconstruction

The tectonic structures measured in the study area reveal

changes of paleostress fields during the Cenozoic Era. These
changes were caused by rotation of the paleostress field, by
spin rotation of crustal blocks (Márton et al. 1999) and by

222

VOJTKO, TOKÁROVÁ, SLIVA and PEŠKOVÁ

tilting of the Tatra Massif. It means that older deformational
phases are affected by these rotations. Based on this assump-
tion, it is possible to determine chronology of faulting in the
study area.

An important result of the paleostress reconstruction was

the E-W orientation of

and perpendicular

axes of the

strike-slip tectonic regime (D

) which has only been measured

in the Mesozoic rocks of the Fatric Unit and is considered to
be of Paleocene—Eocene age, because it is practically absent in
the Oligocene to lowest Miocene strata. This is in accordance
with the results of data measured in the Orava region (Pešková
et  al.  2009),  in  the  Slovenské  rudohorie  Mts  (Vojtko  2003)
and also in the hinterland (southern part) of the Western Car-
pathians  and  Pannonian  Basin  (e.g.  Fodor  et  al.  1992,  1999;
Budai et al. 2008). We assume that it is a former N-S compres-
sion event which was recorded and fixed in the host rocks be-
fore  the  Early  and  Middle  Miocene  counter-clockwise  spin
rotation of crustal blocks.

The tilting of the Tatra Massif had a crucial implication for

the kinematic interpretation and subsequently for the timing of
the paleostress stages. The tilting was most likely the result of
the  NNW—SSE  to  N—S  oriented  compression.  The  effect  of
tilting  caused  (1)  the  rotation  of  the  original  conjugated  re-
verse  faults  into  the  normal  faults  with  unordinary  very  low
(< 5°) north dipping planes with identical types of striae (min-
eral accretionary steps and slickenfibers); (2) the original nor-
mal faults rotated into position of the steeply (more than 75°)
north  dipping  reverse  faults  (Fig. 3).  The  faulting  was  ob-
served predominantly in the Blaščatská and Bachledova doli-
na  Valleys  and  in  the  bedrock  of  the  Biela  River  near  the
village of Ždiar. The youngest tectonic regime with the hori-
zontal NE-SW trending

is Late Neogene in age.

Tectonic evolution during the Cenozoic Era

The Paleogene to Middle Eocene tectonic processes were

controlled by approximately W-E oriented compression under
compressional  to  transpressional  tectonic  regimes.  Predomi-
nantly  during  the  Eocene  to  Oligocene,  the  studied  area  was
located  on  a  convergent  plate  margin  along  the  CWC  edge.
The flysch sedimentation occurred not only on the lower plate
(the Magura Basin), but also on the frontal part of the overrid-
ing  continental  plate  (CCPB).  The  flexure  of  this  overriding
continental plate was most likely generated by subcrustal ero-
sion of lower crustal elements of the overriding plate that had
been accreted to the upper plate during the preceding subduc-
tion period (Wagreich 1995; Kázmér et al. 2003), and/or ex-
tensional  collapse  of  the  overthickened  rear  of  the  External
Carpathian  thrust  wedge  (Sú ov  phase  –  Plašienka  2002;
Plašienka & Jurewicz 2006). The CCPB was formed as a mar-
ginal basin of the Paratethys. It shows a fore-arc position ex-
tended  on  the  destructive  plate  margin  and  behind  the  Outer
Carpathian  accretionary  wedge  (Soták  &  Starek  2000;  Soták
et al. 2001). The final collision of the Western Carpathian oro-
genic wedge with the North European Platform resulted in the
closure and destruction of the Paleogene fore-arc basin above
the active CWC thrust front during the Early Miocene (Kováč
2000). Based on the orientation of the compression of the D

phases (oblique to the Pieniny Klippen Belt), we assume that

subduction of the oceanic crust was oblique to the ALCAPA
(Alpine-Carpathian-Pannonian) microplate edge. Inversion of
the CCPB, connected with the D

deformational phase, is

dated to the Early Miocene (?Ottnangian), because the young-
est known sediments are Egerian—Eggenburgian in age (Soták
et  al.  2001).  The  youngest  known  sediments  of  the  Magura
Nappe  in  the  External  Western  Carpathians  have  the  same
age  (e.g.  Oszczypko  et  al.  2005).  Unlike  Sperner  (1996)  and
Sperner  et  al.  (2002),  we  suppose  that  the  D

1—3

tectonic re-

gimes  only  weakly  influenced  the  uplift  of  the  Tatra  Moun-
tains.  Compressive  structures  (approximately  E-W  trending
fold axes) are also developed in the Šambron-Kamenica Zone
which is connected with the Early Miocene compressional tec-
tonic  regime  (Plašienka  et  al.  1998).  However,  the  results  of
our paleostress analysis point out that the compressional tec-
tonic regime (D

4—5

) with the general N-S compression is most

probably younger, Middle Miocene in age.

Maximum intensity of uplift and tilting of the Tatra Moun-

tains is dated as Middle/Late Miocene based on fission-track
data from apatites (10—19 Ma – Kováč et al. 1994; 15 Ma –
Krá 1977; Baumgart-Kotarba & Krá 2002). The amount of
the Neogene uplift of the Tatra region is not precisely known.

The neotectonics of the Tatra Mountains area (D

) is very

interesting for the very high amplitude of mountain uplift and
remarkable features of their relief. Neotectonic evolution of
the area occurred along weakness planes, inherited faults and
neoformed fault structures. The Tatra Mountains were uplifted
and the area of the Podhale Synclinorium relatively subsided.
The uplift can be considered to be quite intensive and differen-
tiated and the relative uplift is estimated at about 350—450 m
according to correlation of Lower Pleistocene horizons (see
Nemčok et al. 1993).

Pliocene to Quaternary uplift of the Tatra Massif, especially

in  the  north-western  part,  was  studied  by  Bac-Moszaszwili
(1993).  Very  young  normal  faulting  along  the  W-E  trending
faults was also observed at the Vikartovce fault (Marko et al.
2008;  Vojtko  et  al.  2009)  which  can  be  correlated  with  the
Subtatra fault system. Active tectonics and movements along
the faults during the neotectonics phase in the Tatra Mts and
related  areas  has  also  been  documented  by  many  other  au-
thors  using  various  methods  (e.g.  Zuchiewicz  1995,  1998;
Baumgart-Kotarba  1981;  Birkenmayer  1986;  Baumgart-Ko-
tarba & Ślusarczyk 2001).

Relation to the Pieniny Klippen Belt

During the Early Miocene, the Pieniny Klippen Belt (PKB)

zone  was  under  dextral  transpression  with  the  development
of  positive  flower  structures  (e.g.  Ratschbacher  et  al.  1993;
Marko et al. 2005; Plašienka & Jurewicz 2006; Pešková et al.
2009). The internal boundary of the PKB was affected by re-
verse  faulting  and  folding  (Mastella  1975;  Mastella  et  al.
1996;  Kępińska  1997;  Plašienka  et  al.  1998).  Generally,  the
PKB is a subvertical narrow zone in which strike-slipping pre-
vailed and led to the formation of the typical block-in-matrix
tectonic style caused by pervasive brittle faulting (Birkenmayer
1996;  Plašienka  &  Jurewicz  2006).  Complex,  compressional
through  transpressional  to  transtensional  tectonic  regimes
along the PKB dominated during the Middle to Late Neogene.

223

CENOZOIC PALEOSTRESS FIELDS AND REVISED TECTONIC HISTORY OF CENTRAL W CARPATHIANS

Stresses were also relaxed by dextral strike-slips and oblique-
slips along synthetic shears parallel to the WNW-ESE trend-
ing PKB. During the Late Neogene to Quaternary, the sinistral
transtension along the PKB was followed by a general tension
which segmented the zone by dextral and normal NNE—SSW
to N—S faults (Fig. 1).

Conclusion

The reconstruction of the paleostress field was carried out

using the fault-slip, fold and vein data in the Spišská Magura
and  Tatra  region.  The  computer  analyses  of  structural  mea-
surements,  as  well  as  field  geological  and  structural  studies
show  a  generally  clockwise  rotation  of  the  paleostress  field
during the Neogene. One principal phase was distinguished as
being Paleocene to Oligocene, four phases as Miocene and the
last one as Pliocene to Quaternary in age (Fig. 7).

The E—W oriented compression and N—S tension are record-

ed in the Triassic sequences of the Fatric Unit and are very
poorly preserved in the sedimentary sequences of the CCPB.
This oldest tectonic phase (D

) is dated to the Paleocene—Oli-

gocene and indicates a pure strike-slip tectonic regime.

Post-sedimentary deformation of the CCPB (Early Mi-

ocene) was characterized by a compressional to transpression-
al tectonic regime (D

) which successively changed to an

extensional tectonic regime (D

) at the boundary between the

Early and Middle Miocene (more or less Karpatian to Early
Badenian stages).

The poorly preserved extensional tectonic regime of D

tec-

tonic phase finished most probably in the Badenian stage and
was replaced by a new compressional tectonic regime (D

)

with the NNW—SSE trending principal maximum stress axis
(

). The paleostress field rotated progressively clockwise

from the NNW—SSE to the N—S position and the Tatra Massif
was simultaneously tilted. This tectonic phase can be divided
into two subphases based on the relationship between the
faults and tilt rotation of the Tatra Massif. The older one (D

)

is a predominantly compressional less transpressional phase
with the orientation of the principal maximum paleostress axis
in the NNW-SSE direction. The structures of this subphase are
affected by tilting. The orientation of the

of the second sub-

phase (D

) is approximately in the N—S and the measured

structures are more or less in the autochthonous position. Dur-
ing this tectonic regime, intensive backthrusting which propa-
gated toward the south occurred. The last transpressive
tectonic regime (NE—SW oriented

) was tenuously dated to

the Pannonian stage (D

The youngest tectonic regime (D

) is characterized by an

extensional tectonics which can be divided into two sub-
phases. The first one (D

) is NW—SE and the second one is

ENE—SWS oriented tension (D

) and is considered to be

younger than the previous one based on the cross-cutting rela-
tionship of the observed faults.

Acknowledgments: This paper is based on the main part of
the diploma thesis undertaken during the years 2003—2005 by
Eva Tokárová who passed away in 2007. We dedicate this ar-
ticle to her memory. Our work was supported by the Slovak

Research and Development Agency under contracts Nos.
APVV-0158-06 and APVV-0465-06. The authors wish to
thank Damien Delvaux for the TENSOR, Eckart Wallbrecher
& Wolfgang Unzog for the Fabric7 software applications and
we are indebted to Lászlo Fodor and an anonymous reviewer
for careful reviewing and suggestions to improve the paper.

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