GeolCarp_Vol54_No6_409

ORIENTATIONS OF PALEOSTRESSES IN LIMESTONES OF THE WEST CARPATHIAN FLYSCH 409

GEOLOGICA CARPATHICA, 54, 6, BRATISLAVA, DECEMBER 2003

409416

ORIENTATIONS OF PALEOSTRESSES IN THE JURASSIC

LIMESTONES ON THE FRONT OF THE WEST CARPATHIAN FLYSCH

NAPPES (PAVLOV HILLS, SOUTH MORAVIA)

JOSEF HAVÍØ

1,2

and ZDENÌK STRÁNÍK

Czech Geological Survey, Leitnerova 22, 658 69 Brno, Czech Republic; havir@ipe.muni.cz; stranik@cgu.cz

Institute of Physics of the Earth, Masaryk University, Tvrdého 12, 602 00 Brno, Czech Republic

(Manuscript received September 23, 2002; accepted in revised form March 11, 2003)

Abstract: The paleostress analysis was applied at 16 sites in the Mesozoic limestones, which are tectonically incorpo-

rated into the Cretaceous and the Paleogene strata on the front of the West Carpathian flysch nappes (South Moravia,

Czech Republic). 25 solutions were obtained. These solutions can be divided into two groups. The first group represents

the paleostress field with predominantly NW-SE compression and NE-SW extension connected with the Early Neogene

movements of the dánice Nappe. The azimuth of eigenvector of acceptable

axes varies from 97° up to 167°. This

variability can be explained by rotation of individual tectonic slices of the dánice Nappe during the movement of this

nappe. The different tectonic scales probably rotated in different directions (anticlockwise rotation in the case of some

scales, clockwise rotation in the case of others). The second group of solutions represents the paleostress field with NE-

SW compression and NW-SE extension.

Key words: Neogene, Outer Western Carpathians, Waschberg-dánice Belt, paleostresses.

Introduction

Tectonic movements are closely related to the orientations of

the principal stress axes. The orientations of the principal

stress axes can be computed by analysis of the orientations of

kinematic indicators on activated brittle failures. Similarly,

the character of movements along the significant tectonic

structures could be determined from the known orientation of

the principal stress axes.

The paleostress analysis based on the investigation of the

fault striae data was carried out at 16 sites situated in the small

area (about 20 km

) of the Pavlov Hills region (South Mora-

via, Czech Republic). In this way, more detailed knowledge

about the character of the paleostress fields affecting this part

of the Outer Western Carpathians was obtained. The aim of

this article is to inform about the results of this analysis and to

contribute to better knowledge of structural and paleostress

evolution within the outermost part of the junction area of the

Western Carpathians and Eastern Alps.

Geological and structural setting

The Pavlov Hills region is situated in the outermost part of

the outer units of the Carpathian flysch belt, near the front of

the Waschberg-dánice Belt (Fig. 1). The tectonic slices of

the Klentnice Formation (Oxfordian to Tithonian) and the

Ernstbrunn Limestones (Late Tithonian?Hauterivian, see

Stráník et al. 1999) form the N-S to NNE-SSW orientated

klippen in this region. The Upper Cretaceous sediments of the

Klement Formation and the Pálava Formation were transgres-

sively deposited on the Ernstbrunn Limestones. The imbricat-

ed tectonic slivers of the Mesozoic sediments were detached

from the European Platform, tectonically transported and in-

corporated into the frontal zone of the dánice Nappe (Pícha

& Stráník 1999; Stráník et al. 1999). Originally, these Meso-

zoic sediments were deposited on the eastern slope of the Pav-

lov carbonate platform, which was situated on the western

margin of the dánice area (Eliá & Eliáová 1986). The Low-

er Miocene sediments found between two tectonic slices in the

borehole Pavlov Hills-1 (Stráník et al. 1962) prove the Styrian

age of the origin of this imbricated structure, contemporane-

ous with the final stage of the overthrust of the dánice

Nappe.

The greater part of the dánice Nappe is formed by the Ter-

tiary sediments of the Nìmèice Formation (Middle Eocene to

Lower Oligocene in the studied region), the Menilitic Forma-

tion (Oligocene) and the dánice-Hustopeèe Formation (Ege-

rian) (Stráník et al. 1999).

The dánice Unit is thrust to the NW over the Neogene sed-

iments of the Carpathian Foredeep deposited on the SE margin

of the Bohemian Massif. In the northern part of the Pavlov

Hills region, the narrow tectonic slices of the Pouzdøany Unit

are developed in front of the dánice Nappe. The eastern part

of the dánice Unit is covered by the Neogene sediments of

the Vienna Basin. In the basement of the Vienna Basin, the

dánice Unit dips under the Magura Nappe.

The Pavlov Hills region is affected not only by oblique

thrusts developed during the movements of nappes, but also

by significant strike-slip shear zones and oblique-slip trans-

verse faults. The imbricated fabric of the dánice Unit is dis-

turbed by the NW-SE to E-W trending faults on the front of

412 HAVÍØ and STRÁNÍK

cases of less numerous data sets, the orientations of principal

stresses were estimated with the use of the graphical method

of Angelier & Mechler (1977).

The program BRUTE3 tests all possible reduced tensor

configurations (by selected increments) against analysed data

sets and chooses the acceptable tensors, which satisfy the lim-

its (Hardcastle & Hills 1991). The first tested factor is the

maximum limit of 25° for angular difference

between the

rake of maximum shear stress and the rake of measured stria-

tions. Secondly, the value of the shear component of stress

was compared with the minimum value following from the

Coulomb criteria for the reactivated faults.

The reduced tensor has four degrees of freedom. Three an-

gular variables of the acceptable reduced tensor describe the

acceptable orientations of the principal stress axes. Fourth

variable is the shape ratio

defined by Angelier (1975) as

)/(

). The shape ratio was tested in the range

from 0.1 to 0.9, program BRUTE3 does not test the limit val-

ues

=0 and

=1.

The orientations of the principal stress axes of acceptable

tensors could be contoured to show the range of the accept-

able results (Fig. 2). For each principal axis the relevant

eigenvector of orientation matrix was computed as the aver-

age orientation. The mean value of the angular difference

between the rake of maximum shear stress and the rake of

measured striations was used as criteria for the selection of the

best solution. The best solutions are reduced tensors with

the least mean value of

The contoured diagrams were also used for separation of

heterogeneous data (Fig. 2). Solutions, which are acceptable

for any sub-set of data, are displayed in diagram. This con-

toured diagram shows several groups of possible solutions.

Found possible solutions were used as a criterion for separa-

tion of data by the program SELECT (Hardcastle & Hills

1991).

Computed orientations of principal paleostresses

25 solutions (see Table 1) based on the analyses of fault ge-

ometries were obtained at 16 sites in the Pavlov Hills region

(Fig. 3). 21 solutions were computed by program BRUTE3.

Four solutions were determined by the graphical method of

Angelier & Mechler (1977). Two main groups of solutions

were distinguished according to orientations of the principal

axes. These groups are the following:

1. group of predominantly NW-SE compression and/or NE-

SW extension;

2. group of NE-SW compression and NW-SE extension.

Predominantly NW-SE compression and/or NE-SW

extension

19 solutions of the analyses carried out at 12 sites shows

predominantly NW-SE compression and NE-SW extension.

Most of these solutions have gently dipping

and

axes.

Computed solutions are represented by sub-horizontal

axis

and steep

axis only at two sites (sites 111 and 118).

Fig. 3. Geological scheme of the Pavlov Hills region (after Stráník

et al. 1999, modified and simplified) with marked studied sites (grey

circles). White arrows show computed orientations of horizontal

principal stresses (see text for more information).

ORIENTATIONS OF PALEOSTRESSES IN LIMESTONES OF THE WEST CARPATHIAN FLYSCH 413

Site

Solution

Rock

Stress tensor

Method

best solution

eigenvectors

stress ratio

101

101A

318/20

216/28

313/23

219/8

0.3-0.7

BRUTE3

101B

180/10

294/66

161/15

251/24

0.1-0.4

BRUTE3

102

102A

EL, KF

315/50

47/2

313/47

46/2

0.1-0.3

BRUTE3

103

103A

150/10

60/0

334/20

71/9

0.5-0.9

BRUTE3

104

104A

146/30

238/2

155/32

63/3

0.3-0.5

BRUTE3

104B

50/0

140/51

226/5

137/24

0.1-0.4

BRUTE3

104C

180/10

90/0

167/9

263/5

BRUTE3

105

105A

310/10

43/17

130/0

221/6

0.1-0.4

BRUTE3

106

106A

110/0

200/20

292/1

198/16

0.1-0.3

BRUTE3

107

107A

326/30

229/13

321/31

227/8

0.5-0.8

BRUTE3

109

109A

30/50

134/11

31/57

146/13

0.7-0.9

BRUTE3

109B

210/10

110/45

203/4

108/47

0.1-0.3

BRUTE3

111

111A

EL, KF

280/10

34/66

277/3

160/74

BRUTE3

111B

EL, KF

NW-SE

NE-SW

114

114A

280/60

75/28

276/52

74/40

BRUTE3

114B

293/30

54/42

300/40

60/37

BRUTE3

116

116A

ESE-WNW

NNE-SSW

117

117A

42/44

157/28

34/30

142/28

BRUTE3

117B

NW-SE

NE-SW

118

118A

EL, KF

340/10

239/47

334/10

235/54

BRUTE3

118B

EL, KF

328/20

228/34

326/11

204/57

0.3-0.4

BRUTE3

118C

EL, KF

349/30

230/40

341/23

233/36

0.2-0.6

BRUTE3

118D

EL, KF

310/10

219/47

125/14

225/35

0.1-0.5

BRUTE3

118E

EL, KF

154/40

267/25

157/63

240/3

0.1-0.4

BRUTE3

118F

NE-SW

NW-SE

Table 1: Solutions of paleostress analysis computed by program BRUTE3 (Hardcastle & Hills 1991) or determined by the graphical

method of Angelier & Mechler (1977). EL Ernstbrunn Limestone, KF Klement Formation.

Mostly steep strike-slip or oblique-slip faults correspond to

the discussed orientation of the principal stresses. The sinistral

and dextral strike-slips trend NNW-SSE to NNE-SSW and

NW-SE to E-W, respectively. There is significant variability

in the trend of the thrusts and oblique thrusts. Predominantly,

they are dipping to the E. At the Janiùv vrch site (118) N-S to

NNW-SSE trending oblique normal faults were also mea-

sured.

In the cases of solutions determined by program BRUTE3,

the azimuth of eigenvector of acceptable

axes varies from

97° up to 167° (Fig. 4). At sites 104 and 118 on the northern

margin of Svatý kopeèek and at site 111 near Soutìska, the

crossing of several fault structures used for the determination

of discussed paleostresses was observed.

At site 111 near Soutìska, the eastwards dipping thrusts of

Ernstbrunn Limestones over the sediments of the Klement

Formation and the Pálava Formation were used for determina-

tion of orientation of paleostress field with E-W to WNW-

ESE maximum compression. The thrusts are cut by younger

WSW-ENE oriented steep oblique thrusts which were active

under NW-SE compression.

At the Svatý kopeèek (104) and Janiùv vrch sites (118) the

duplex fabric of the Ernstbrunn Limestone was observed

(Fig. 5). The duplex fabric originated between larger moder-

ately dipping faults, which were repeatedly reactivated

(strike-slips, oblique thrusts). At the Janiùv vrch site (118),

the tectonic planes bounding individual tectonic slices trend

E-W to NW-SE. Striations on these planes prove oblique-slip

movements. The resulting solutions show the sub-horizontal

axis oriented NW-SE or NNW-SSE and the

axis dip-

ping towards SE or ESE. The dip of the

axis is about 50° in

the case of local field determined from duplexes (solution

Fig. 4. Orientation of eigenvectors of the acceptable

axes (max-

imum compression) and

axes (maximum extension) determined

by program BRUTE3. Upper diagrams point diagrams of ori-

entations of eigenvectors (Lambert projection, lower hemisphere);

lower diagrams histograms of strikes of eigenvectors (fre-

quency of histograms is 10°).

414 HAVÍØ and STRÁNÍK

118A) and about 35° in the case of other solutions determined

from the large thrusts and from strike-slip faults (solutions

118B, 118C and 118D). Some oblique thrusts and strike-slip

faults are cut by the tectonic boundaries of duplexes. On the

other hand, some other thrusts and strike-slip faults cut the du-

plex fabric. These facts prove the activity of the oblique

thrusts and strike-slip faults both before and after the forming

of the duplex fabric (Fig. 6). The azimuth of eigenvector of

acceptable

axes varies from 125° up to 161°, in the case of

individual solutions from site 118. The faults older than duplex

fabric correspond mostly to the NNW-SSE orientation of

axis, the faults younger than duplex fabric correspond mostly to

the NW-SE orientation of

axis. At the Janiùv vrch site

(118), the youngest paleostress field (solution 118E) is repre-

sented by sub-horizontal NE-SW

axis and steep

axis.

Two solutions with different azimuth of the

axes were

also determined at the Svatý kopeèek site (104). This azimuth

is 155° in the first case and 167° in the second case.

The discussed fact shows that paleostresses with the predom-

inantly NW-SE compression and NE-SW extension affected

the Ernstbrunn Limestone in the Pavlov Hills region during

more than one stage of movements along faults. Individual

stages probably passed each into other continuously. The dif-

ferences between solutions representing individual stages of

fault activity could be explained by one of two hypotheses:

rotation of the principal paleostress axes be-

tween individual stages and change of the value of

principal stresses;

rotation of faulted block of affected rocks be-

tween individual stages and change of the value of

principal stresses. The anticlockwise block rotation

is presumed by Fodor (1991, 1995) in the West Car-

pathian flysch nappes. The solutions determined at

site Janiùv vrch (118) show the possibility of the

clockwise rotation of the Svatý kopeèek block.

At Dívèí hrad site (114) situated on the northern

boundary of the Pavlov Hills region, the

and

axes significantly dip to the NW and NE respective-

ly. Two similar solutions were determined from the

N-S oriented faults. The plunge of measured stria-

tions varies from 48° to 83°. On some fault planes

more than one striation was measured, different stri-

ations correspond to different dip of the principal

paleostresses. The determined orientation of the

principal paleostresses shows the significant north-

ward tilting at site 114 (Fig. 7). During the predom-

inantly NW-SE compression and NE-SW exten-

sion, the block rotation around the probably

sub-horizontal EW axis occurred. The value of the

angle of this rotation was probably about 20°30°.

The significant dip of all striations could be ex-

plained by continuing rotation after the end of fault

movements connected with the NW-SE compres-

sion.

The strike-slip faults and oblique thrusts used for

determination of the discussed paleostress dislocate

not only the Ernstbrunn Limestone, but also the

overlaying Upper Cretaceous sediments of the Kle-

ment Formation. It means that the predominantly

Fig. 5. Scheme of the duplex fabric of the Ernstbrunn Limestone observed in

the Svatý kopeèek quarry (site 104). Diagrams (Lambert projection, lower

hemisphere) show measured orientations of planes bounding individual tectonic

horses (grat circles), arrows show sense of displacement. Striations on the tec-

tonic planes bounding individual horses (tectonic slices) prove oblique move-

ments along these planes (not dip-slip movements).

NW-SE compression could be active after the Late Creta-

ceous. In the Pavlov Hills 1 borehole, the tectonic slice of the

Lower Karpatian sediments were found (Stráník et al. 1962).

It proves the existence of Karpatian (or younger?) predomi-

nantly NW-SE compression.

NE-SW compression and NW-SE extension

In the case of five solutions, the maximum compression is

oriented NE-SW and maximum extension is oriented NW-SE.

The E-W trending sinistral and N-S to NNE-SSW trending

dextral strike-slips correspond to this orientation of principal

axes. At site Kotel (109), the fault population attributed to this

paleostress also contains NW-SE trending sinistral strike-slip

faults. The NE-SW compression and NW-SE extension was

found at sites situated both in the southern and northern parts

of the studied area. Individual faults which geometrically cor-

respond to this orientation of principal paleostresses were also

measured at some other sites. It shows the regional signifi-

cance of this paleostress field. The NE-SW compression and

NW-SE extension affected the whole Pavlov Hills region. The

less frequent fault striae data corresponding to this paleostress

field could be explained by older age or smaller intensity of

this paleostress field in comparison with the predominantly

NW-SE compression.

ORIENTATIONS OF PALEOSTRESSES IN LIMESTONES OF THE WEST CARPATHIAN FLYSCH 415

of the Carpathian units to the NE (Kováè 2000;

Nemèok et al. 1998b). Thus the contact of the Bo-

hemian Massif and the Western Carpathians was

strongly affected by the lateral movement of the

West Carpathian units. During the Neogene sinis-

tral transpression, the Carpathian flysch nappes

were obliquely thrust onto the eastern margin of the

Bohemian Massif. The last movements of the

dánice Nappe terminated during the Karpatian in

the southern Moravia region (Kováè 2000).

The Paleogene and the Early Neogene WNW-

ESE to NNW-SSE orientation of maximum com-

pression is documented from the junction area of

the Western Carpathians and Eastern Alps (for in-

stance Fodor 1991, 1995; Marko et al. 1995; Nem-

èok et al. 1998a; Peresson & Decker 1997). This

orientation corresponds well to the results discussed

in this article. Paleostress field is represented by

predominantly NW-SE compression and NE-SW

extension was computed at a number of sites in the

Pavlov Hills region. The determined WNW-ESE to

NNW-SSE compression was connected with the

nappe movements during the OligoceneEarly Mi-

ocene transpression in the westernmost Car-

pathians. The Cenozoic NW-SE to NNW-SSE com-

pression significantly affected the eastern margin of

the Bohemian Massif. For instance, the Neogene

NW-SE compression was found at several sites on

the south-eastern margin of the Nízký Jeseník re-

gion and in the Maleník block (Havíø 2002).

Fodor (1991, 1995) has supposed the stable N-S

orientation of maximum compression in the west-

ernmost Carpathians and easternmost Eastern Alps

during the OligoceneEarly Miocene and anticlock-

wise block rotation which affected the observed

faults. The blocks rotated in a broad zone affected

by sinistral transpression.

The rotation of the tectonic blocks should be tak-

en into account. This possible rotation, which ac-

companied the movement of the dánice Nappe,

can explain the time and space variation of the ori-

entation of the principal stresses found in the Pav-

lov Hills region. The variability of the orientation of

individual klippen in the Pavlov Hills region can

also be explained by this rotation (Stráník et al.

At the Kotel site (109) near the Klentnice, two different pa-

leostress fields with NE-SW compression and NW-SE exten-

sion were found. This fact shows that the Mesozoic blocks on

the front of the West Carpathian flysch nappes were probably

affected by the NE-SW compression and NW-SE extension

during more (at least two) different tectonic episodes.

The orientations of paleostresses in relation

to the tectonic development

While the collision started in the Alpine region already dur-

ing the Eocene, in the Carpathian region continuing subduc-

tion caused the Oligocene to Miocene large-scale movements

Fig. 6. Scheme of relative ages of paleostress fields at the Janiùv vrch site

(118). Orientations of principal stresses are computed by program BRUTE3

(Hardcastle & Hills 1991) solutions 118A, 118B, 118C, 118D and 118E

or determined using the method of Angleier & Mechler (1977) solution

118F (Lambert projection, lower hemisphere). For symbols see Fig. 2 (see text

for more information).

1996). The different tectonic scales (or tectonic blocks) proba-

bly rotated in different directions. In the case of some blocks,

the anticlockwise rotation can be supposed, other blocks were

affected by clockwise rotation. The value of angle of the dis-

cussed rotation can be estimated as up to 40°.

During the Early Badenian the orientation of the principal

stresses was changed in the junction area of the Western Car-

pathians and Eastern Alps. After termination of nappe move-

ments, the maximum compression axis was turned to NNE-

SSW, while maximum extension was WNW-ESE (for

instance Fodor 1991, 1995; Marko et al. 1995; Nemèok et al.

1998a; Peresson & Decker 1997). This orientation of the prin-

cipal stresses was connected with transtensional regime. In the

Vienna Basin, the transtension is proved by the negative flow-

416 HAVÍØ and STRÁNÍK

er structures (Hubatka & Krejèí 1996). The NE-SW compres-

sion and NE-SW extension were also found at several sites in

the Pavlov Hills region. Some of these determined solutions

can correspond to the discussed transtensional regime. But

two different solutions computed at site 109 show that the ex-

istence of an other (probably older) stress field with similar

orientation of the principal stresses also has be taken into ac-

count.

Conclusion

The results of paleostress analysis show that two paleostress

fields played dominant roles during Cenozoic tectonic devel-

opment in the Pavlov Hills region.

The first paleostress field is represented by predominantly

NW-SE compression and NE-SW extension. This paleostress

field is connected with the Early Neogene movements of the

dánice Nappe. The variability of the orientation of principal

stresses can be explained by rotation and tilting of individual

tectonic scales during movement of the nappe.

The second paleostress field is characterized by NE-SW

compression and NW-SE extension. The field with this orien-

tation of the principal stresses affected the Mesozoic blocks

on the front of the West Carpathian flysch nappes during

more (at least two) different tectonic stages. One (younger)

tectonic stage can correspond to the Badenian (or younger?)

transtensional regime.

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Fig. 7. Orientations of principal stresses computed at the Dívèí hrad

site (114) (Lambert projection, lower hemisphere) and scheme of

orientation of striations on steep NS trending faults. Plunge of stri-

ations varies due to northward tilting (see text for more informa-

tion). For other symbols see Fig. 2.