GeolCarp_Vol52_No3_183

GEOLOGICA CARPATHICA, 52, 3, BRATISLAVA, JUNE 2001

183—190

STRUCTURAL HISTORY OF THE PORVA BASIN

IN THE NORTHERN BAKONY MTS (WESTERN HUNGARY):

IMPLICATIONS FOR THE MESOZOIC AND TERTIARY TECTONIC

EVOLUTION OF THE TRANSDANUBIAN RANGE

AND PANNONIAN BASIN

ADA KISS

, BALÁZS GELLÉRT

and LÁSZLÓ FODOR

1**

Department of Applied and Environmental Geology, Eötvös University, Múzeum krt. 4/a, 1088 Budapest, Hungary; ada@ludens.elte.hu

(Manuscript received April 5, 2000; accepted in revised form October 17, 2000)

Abstract: The authors made geological mapping and microtectonic measurements in the Northern Bakony Mts., around
the Porva Basin. Using structural observations, a new structural-geological map was made for this area. Four tectonic
phases were separated by the analysis of stress field. Map-scale neptunian dikes represent the Jurassic rifting episode.
For  this  phase  NNE-SSW  tension  was  estimated.  NW-SE  compression  of  Albian  (?)  age  resulted  in  gently  dipping
reverse and conjugate strike-slip faults. In the Ottnangian—Sarmatian  (18.5—11  Ma)  a  strike-slip  type  stress  field  with
NNW-SSE compression developed. This phase formed mainly NW-SE striking dextral and conjugate shorter sinistral
strike-slip faults. NW-SE striking half-grabens formed along strike-slip or oblique-slip faults. Motion resulted in post-
sedimentary tilting of the Eocene-Oligocene sequences toward the master faults. A late Miocene extensional phase with
WNW-ESE  tensional  directions  was  also  determined.  During  this  phase  the  earlier  half-grabens  were  reactivated,  al-
though with slightly different slip on boundary faults. Some of the young half-grabens are connected by transfer faults,
which had a strike-slip character. Ottnangian-Sarmatian strike-slip faults occurred during the rifting phase of the Pannonian
Basin,  their  main  activity  was  coeval  with  important  stretching  in  the  northeastern  Pannonian  Basin.  These  relatively
local strike-slip faults could accommodate differential extension between the northern and southern Pannonian Basin.
On  the  other  hand,  the  newly  recognized  Late  Miocene  tensional  phase  indicate,  that  the  post-rift  evolution  of  the
Pannonian Basin was associated with considerable crustal extension.

Key words: Cretaceous, Miocene, Pannonian Basin, Bakony Mts, structural geology, strike-slip fault, half-graben,
stress field.

Introduction

The  Bakony  Mts  are  situated  in  the  Transdanubian  Range,
southeast of the Danube Basin (Fig. 1). According to its Mi-
ocene  structural  setting,  the  Bakony  Mts  are  on  the  hanging
wall of the detachment fault running down from the Kőszeg-
Rechnitz Penninic window (Tari 1996). While modern tecton-
ic  analysis  has  been  made  in  the  Danube  Basin  (e.g.  Tari
1994),  the  northern  Bakony  is  a  relatively  unknown  area  in
this respect. Here the last systematic structural work was done
by Mészáros (1983) describing ESE-WNW oriented Miocene
dextral faults. The largest one, the Telegdi Roth Line has a 4.7
km dextral separation (Fig. 1) (Mészáros 1983; Kókay 1976)
and runs just south of the studied area.

Although detailed geological maps cover the Northern Ba-

kony Mts (Császár 1982; Gyalog & Császár 1990), the lack
of paleostress data prevented the kinematic interpretation of
faults. Bergerat et al. (1984) and Maros (pers. commun.)
measured only a few sites, while Fodor et al. (1999) reported
results from few additional locations. In our paper we present
new paleostress data and other observations from the Porva
Basin, Northern Bakony. The description of fault pattern, its
kinematic character and the structural evolution can be used
as analogy in other areas around the Danube Basin. In addi-

tion, some of the new data can have implications for the
structure of the whole Pannonian region.

Geological setting

In the research area the oldest surface formation is the Up-

per Triassic dolomite (Hauptdolomit Formation, Fig. 2), show-
ing  typical  intertidal  sedimentary  features.  Dachstein  Lime-
stone,  the  most  frequent  Mesozoic  sedimentary  rock
surrounding the basin, was also generated in a shallow marine
environment  (Haas  1995).  Different  Lower  Jurassic  shallow
and deep-water limestones follow it. Middle Jurassic to Early
Cretaceous  limestones  mainly  represent  pelagic  sediments.
The  late  Early  Cretaceous  shallow  water  crinoidal  limestone
(Tata  Formation)  and  the  Senonian  siliciclastic  sequence  in-
cluding  coal  beds  (Csehbánya  Formation)  have  very  limited
extension (Lelkes 1990; Császár & Haas 1984) but an impor-
tant tectonic role. Middle Eocene sediments are represented by
two  basic  types:  (1)  the  lower,  nummulitic  Szőc  Limestone
Formation  and  (2)  the  upper,  deep  water  glauconitic  Padrag
Marl  Formation  with  tuffitic  horizon  (Fig.  8).  These  Eocene
sediments were formed at increasing water-depth. The thickest
Tertiary sedimentary fill of the Porva Basin is the fluvial Csat-

Present addresses: *Hungarian Oil Company, Batthyányi út 45, Budapest, 1039 Hungary; bgellert@mol.hu

**Geol. Inst. of Hungary, Stefánia út 14, Budapest, 1143 Hungary; fodor@mafi.hu

184 KISS, GELLÉRT

and FODOR

ka  Formation  (Fig.  2).  The  detrital  succession  contains  silt-
stone, sandstone and conglomerate with predominantly exotic
quartz  and  metamorphic  pebbles  (Korpás  1981).  The  age  of
these  strata  is  Upper  Oligocene—Early  Miocene  (Egerian—
?Eggenburgian), accumulated as sediments of alluvial and/or
torrent rivers. Loess, slope and alluvial sediments were formed
in the Quaternary (for clarity, they are not shown in Fig. 2).

Methods

Structural mapping included the control or modification of

faults shown by earlier maps (Gyalog & Császár 1990). We
modified the location, connection, and, if it was possible to de-
termine, the kinematics of faults. During this step, a digital ter-
rain model was applied for better resolution of morphotectonic
elements.

Microtectonic measurements represented an important part

of the fieldwork. Microtectonic data was evaluated by the
method of Angelier (1984). Stereograms drawn by the soft-
ware show the measured data and also the calculated principal
stress axes. Outcrop-scale observations, the determined stress
axes and the apparent map offset of formations were used to
determine the kinematics of faults (Fig. 2). We also used bore-
hole data to construct a new geological map without Quaterna-
ry formations.

Structural description and kinematic analysis

The oldest structural phase known from this area belongs to

the  Jurassic  (Fig.  3A).  The  interpreted  NNE-SSW  oriented
tensional  stress  field  induced  the  development  of  neptunian
dikes  filled  by  Lower  Jurassic  crinoidal  (Hierlatz)  limestone

Fig. 1. The study area, the Porva Basin is situated in the Northern Bakony Mts. Pre-Tertiary formations are shown.

186 KISS, GELLÉRT

and FODOR

spite tilted beds. There was an important tilting event during
the late Early Cretaceous, when the synform structure of the
Transdanubian Range was formed (Tari 1995). The striae de-
veloped before (or during) this tilting event, so they can be-
long to an early deformational phase.

Along the Great Western Fault (Fig. 2) there is map-scale ar-

gument for pre-Tertiary (probably mid-Cretaceous) deforma-
tion. On the eastern block Middle Eocene (and Egerian?) sedi-
ments directly cover the Upper Triassic Dachstein Formation,
while the western block contains the complete Jurassic-Creta-
ceous sequence. Relative vertical motion and erosion occurred
before the Eocene.

Fig. 5. Relation between striae and bedding. On the left side model
tilting occurred after the faulting so the striae are parallel with the
bedding plane. That is, what we can observe on the stereogram of
the Cretaceous phase (Fig. 4). On the right side tilting happened be-
fore the faulting thus the striae and bedding plane are not parallel.

Fig. 4. Microtectonic measurements in lower Cretaceous limestones
(upper 3 diagrams) and Dachstein Limestone (the lower 3). During
middle  Cretaceous  deformation,  gently  dipping  thrust  and  strike-
slip faults were generated due to NW-SE compression. Stereograph-
ic  projections  use  Schmid  net,  lower  hemisphere.  Arrows  on  fault
projections  correspond  to  sense  of  shear,  strike-slip  (double),  away
and  toward  circle  centre  (normal,  reverse  faults).  Stars  with  five,
four, three branches are

. Black arrows out of the circle are

projections of

and

to horizontal.

Fig. 3. A – Jurassic brittle deformation is represented by a map-
scale neptunian dike (location in Fig. 2, cross section – B). Here
Jurassic limestone (

) occurs as a sedimentary dike in Upper Tri-

assic Dachstein Limestone (

). For this phase NNE-SSW tension

was estimated.

Fig. 6. Microtectonic data of the early to Middle Miocene phase.
Measurements were made on Dachstein Limestone (Cuha Valley),
Eocene Szőc Formation (Csesznek) and Oligocene Csatka Forma-
tion (Fenyőfő/1). Data of the site Cuha Valley are from Gyetvai et
al. (1997), reinterpreted.

Probably the most significant structural phase occurred dur-

ing the Ottnangian—Karpatian—Badenian—Sarmatian in the Ba-
kony Mts including the Porva Basin. The stereogram belong-
ing  to  this  phase  shows  that  the  direction  of  maximal
horizontal  stress  is,  NNW-SSE  (Fig.  6).  This  stress  field
formed mainly NW-SE striking dextral and conjugate shorter
sinistral  strike-slip  faults.  These  faults  are  several  km  long
(Bacskor Hill Fault, Porva Fault, Great Western Fault, Fig. 2),
are trending NW-SE, and are partly running out of this area.
Shorter  sinistral  fault  is  present  at  the  Templom  Hill  Fault
(Fig.  2).  NW-SE  striking  dextral  faults,  which  are  important
structural  elements  also  in  the  next  phase,  could  have  been
generated  as  early  as  during  this  phase,  on  the  basis  of  the
stress field.

The Late Miocene stress field shows predominantly exten-

sional features (Fig. 7). The direction of minimal stress axis
was WNW-ESE. Normal faults were associated with oblique-
slip faults. Most of the determined map-scale faults reactivate
older strike-slip faults with oblique-slip kinematics.

Half-graben tectonics belongs to the last two phases (Fig.

8). Half-grabens were controlled by normal-dextral (like Porva

STRUCTURAL HISTORY OF THE PORVA BASIN IN THE BAKONY MTS 187

Fig. 7. Microtectonic measurements of Late Miocene phase. The
youngest affected rock is Pannonian. A WNW-ESE tension direc-
tion was determined.

Fig. 8. A – Ideal block diagram of post-Oligocene half-grabens. B
– Cross section of the Porva half-graben with fifteen-fold vertical
exaggeration (location on Fig. 2).

and  Ménesjárás  half-grabens),  as  well  as  by  ”pure”  normal
faults  (like  Almás  half-graben).  The  generated  basinal  do-
mains are asymmetrical, dipping toward the master faults. No
major  sediment  thickening  occurs  toward  the  faults  either  in
the  Eocene  or  in  the  Upper  Oligocene—lowermost  Miocene

Fig. 9. A – The Hódos graben was formed during the last (Pannon-
ian) tectonic phase on the northern part of the research area. B –
shows the idealized block diagram of a similar transfer zone, which
connects the Rhine and the Saône grabens (Bergerat 1977).

formations, suggesting post-sedimentary formation of half-
grabens.

In the Late Miocene phase the complex Hódos graben was

formed (Fig. 9). It can be divided into 4 parts. Graben domains
I., II. and IV. were bounded by normal faults or oblique faults
with sinistral component. These domains are connected to
each other and limited on the north by E-W striking transfer
zones of the segment III. and I. (Fig. 9). These transfer faults
were formed because of geometric reasons.

Discussion and conclusion

Early Jurassic deformation is represented by a NNE-SSW

tension. The stress axis is similar to the supposed stress field
that can be deduced from the paleogeographical elements de-
scribed by Vörös & Galácz (1998) for the whole Bakony Mts
or documented in the Gerecse (Fodor & Lantos 1998). We can
connect this Early Jurassic tectonic event with the disruption
(rifting) of the Upper Triassic carbonate platform of the Trans-
danubian Range.

The gently dipping thrust and strike-slip faults formed by

NW-SE compression are syn- or pre-tilting structures. These
small-scale  structures  can  correspond  to  the  main  phase  of
Cretaceous structural evolution of the Transdanubian Range,
when  the  Permo-Mesozoic  succession  was  folded,  and  de-
tached from its pre-Alpine basement (Tari 1995). The resulting
synclines and reverse faults occur all around the Porva Basin
(Fig. 1A), north and east of it (Gyalog & Császár 1990), west
of the basin (Bakonybél thrust, Tari 1994), south of the Herend
fault (Mészáros 1968). The estimated compressional direction
(NNW-SSE)  of  Tari  (1995)  and  also  the  measured  data

188 KISS, GELLÉRT

and FODOR

Fig. 10. Main Miocene structures, stress trajectories (main figures), structures and stress axes (insets) for the Pannonian-Carpathian region
and for the northern Bakony, respectively; after Fodor et al. (1999) and this work (see also Figs. 1, 2).

Middle Miocene phase; note paral-

lel dextral faults in the Bakony Mts. ESB – East Slovak Basin; BH – Bacskor Hill; GW – Great Western, P – Porva dextral faults.

Late Miocene phase; note normal or oblique normal faults with ESW-NW tension in the Bakony Mts., probably due to continuing eastward
pull in the Eastern Carpathians. H – Hódos; P – Porva; A – Almás half grabens.

(WNW-ESE) of Fodor & Koroknai (2000) in the southern Ba-
kony correspond to our computed data. Similar a late Early
Cretaceous stress field was recorded in the Balaton Highland
by Dudko (1991) where compression created large thrust
faults (Fig. 1A).

We observed one Baremian and two Aptian sites deformed

during this phase. This shows that at least part of the (tilting)
folding is clearly post-Aptian. Combining with the upper time
constraint (Mészáros 1968), the deformation could be placed
in the early Albian (Fodor & Koroknai 2000). However, an
early Aptian event is not excluded (e.g. Haas 1996), because
the Aptian crinoidal limestone contains clasts from different
Jurassic and Upper Triassic formations (Lelkes 1990).

One of the most important phases of structural evolution of

the Porva Basin happened in the late Early to Middle Miocene.
In this phase a strike-slip stress field developed with NNW-
SSE compression and perpendicular tension.

This stress field operated other map-scale strike-slip faults,

such as the Telegdi Roth Line (Fig. 1), which has 4.7 km dex-
tral separation. It corresponds to a stress field estimated from
the fault pattern of Mészáros (1983) and the few published

stress  field  data  (Bergerat  et  al.  1984;  Fodor  et  al.  1999).
Transpressional dextral faults were described on the northern
edge of the Bakony (Csesznek Zone, Fig. 1B, Kiss & Gellért
2000) and on the south (Herend fault, Mészáros 1968). Dextral
faulting  could  be  associated  with  domino-type  rotation  of
blocks (Tari 1991). Numerous measurements have been made
in  the  Oligocene—Early  Miocene  Csatka  Formation  at
Fenyőfő, thus the tectonic phase can be specified as post-Ege-
rian. This wrenching probably started in the Ottnangian in the
Várpalota Basin (Fig. 1B, Kókay 1996). Displaced Badenian
strata  indicate,  that  the  main  period  could  be  Sarmatian
(Mészáros 1983).

These structures are difficult to interpret and put in the Car-

pathian geodynamic framework, because they are very scarce
in other parts (see Fodor et al. 1999). Dextral strike-slip fault-
ing in the Porva Basin, particularly, the main Badenian-Sarma-
tian activity was coeval with important extension in the north-
eastern Pannonian Basin (e.g. East Slovak Basin, Kováč et al.
1995). One alternative explanation is that dextral faults ac-
commodate differential extension between the northeastern
and southern Carpathian-Pannonian area (Fig. 10A). The other

STRUCTURAL HISTORY OF THE PORVA BASIN IN THE BAKONY MTS 189

possible  scenario  is  that  NNW-SSE  compression  is  the  far-
field  sign  of  compression  and  dextral  transpression  in  the
southern Alps (Castellarin & Cantelli 2000) and in the south-
ern  Eastern  Alps  (Nemes  et  al.  1997;  Polinski  &  Eisbacher
1992), in Slovenia (Fodor et al. 1998) or in Croatia (Tomljen-
ović & Csontos 2001).

During the Late Miocene period long normal and dextral-

normal faults were working. They controlled the development
of half-grabens, and the tilting of the Eocene-Oligocene se-
quence. This phase activated the fault pattern of the Hódos
graben which is very similar (in geometry) to the Le Creusot-
Belfort transform zone, which connects the Saône and Rhine
grabens (Bergerat 1977).

This significant extension phase can be extended to the en-

tire Northern Bakony Mts (Fig. 1B). West and northwest from
the Porva Basin, maps (Gyalog & Császár 1990) indicate Pan-
nonian  sediments  bounded  by  E-W  to  NNE-SSW  trending
faults (Fig. 1B). On the southwest, the Ajka graben is limited
by en echelon, NNE oriented normal faults. Between the Ba-
kony and Vértes Hills, the dextral-normal boundary fault of the
Mór  graben  displaces  Pannonian  rocks  (Kóta  2001).  At  the
southern wing of Northern Bakony Mts Kókay (1996) reported
a late normal fault displacing the Telegdi Roth Line in the Vár-
palota  Basin  (Fig.  1B).  All  these  NNE-SSW  trending  faults
could  have  been  generated  by  ESE-WNW  tension.  Kókay
(1996) has dated the Várpalota fault as middle Pannonian. This
is in good agreement with our relative chronology while the
youngest  affected  rock  is  Pannonian  (Bakonyszentlászló,
Fig. 7).

This post-Middle Miocene extension phase has already been

determined in the vicinity of the Bakony. A stress field with
pure NW-SE minimal axes was measured in the Gerecse
(Bada et al. 1996) and in the Buda Hills (Fodor et al. 1994).

Altogether, ESE-WNW to SE-NW oriented tension seems

to be present in a considerable part of the Pannonian Basin
(Fig. 10B). The Late Miocene period is traditionally regarded
as a post-rift phase marked only by thermal subsidence (Roy-
den & Horváth 1988). Our data indicate noticeable crustal ex-
tension, which could be connected to final thrusting in the Car-
pathians (Fodor et al. 1999). The direction of trajectories of

are oriented to the Eastern Carpathian thrust front which was
still active at the beginning of the Late Miocene (Ma enco
1997).

Acknowledgment:  The  work  was  initiated  at  the  Depart-
ment of Applied and Environmental Geology of the Eötvös
University,  Budapest  as  a  student  work,  later  as  the  master
thesis of A. Kiss. The field work was partly supported by the
Hungarian  Science  Fundation  (OTKA),  Grant  T  22119.  E.
Boda  and  S.  Diószegi  from  the  bauxite  mine  at  Ba-
konyszentlászó helped in field measurements. The comments
of the reviewers improved the figures and text considerably.
All help is acknowledged here.

References

Angelier J. 1984: Tectonic analysis of fault slip data sets. J. Geo-

phys. Res. B7, 5835—5848.

Bada G., Fodor L., Székely B. & Timár G. 1996: Tertiary brittle

faulting and stress field evolution in the Gerecse Mts., N. Hun-
gary. Tectonophysics 255, 269—289.

Bergerat F. 1977: La fracturation de lavant-pays jurassien entre les

Fossés de la Saône et du Rhin analyse et essai d’interprétation
dynamique. Rev. Géogr. Phys. Géol. Dynam. 19, 325—358.

Bergerat F., Geyssant J. & Lepvrier C. 1984: Neotectonic outline of

the Intra-Carpathian basins in Hungary. Acta Geol. Hung. 27,
237—251.

Castellarin A. & Cantelli L. 2000: Neo-Alpine evolution of the

Southern Alps. J. Geodynamics 30, 251—274.

Császár G. 1982. Geological map of the Bakony Mts. 1:20,000,

sheet Borzavár. Geol. Inst. of Hungary, Budapest.

Császár G. & Haas J. 1984: The Cretaceous in Hungary: a review.

Acta Geol. Hung. 27, 417—428.

Dudko A. 1991: Structural elements of the Balaton Highland.

Guidebook to fieldtrip, Hung. Geol. Inst., Budapest, 1—84 (in
Hungarian).

Fodor L. & Lantos Z. 1998: Liassic brittle structures in Gerecse.

Földt. Közl. 128, 375—396.

Fodor L., Magyari Á., Fogarasi A. & Palotás K. 1994: Tertiary tec-

tonics and Late Paleogene sedimentation in the Buda Hills,
Hungary. A new interpretation of the Buda line. Földt. Közl.
124, 129—305.

Fodor L., Jelen B., Márton E., Skaberne D., Čar J. & Vrabec M.

1998: Miocene-Pliocene tectonic evolution of the Slovenian
Periadriatic Line and surrounding area – implication for Al-
pine-Carpathian extrusion models. Tectonics 17, 690—709.

Fodor L., Csontos L., Bada G., Györfi I. & Benkovics L. 1999: Ter-

tiary  tectonic  evolution  of  the  Pannonian  basin  system  and
neighbouring  orogens:  a  new  synthesis  of  paleostress  data.  In:
Durand  B.,  Jolivet  L.,  Horváth  F.  &  Séranne  M.  (Eds.):  The
Mediterranean  Basins:  Tertiary  extension  within  the  Alpine
Orogen. Geol. Soc. London, Spec. Publ., 1—156.

Fodor L. & Koroknai B. 2000: Tectonic position of the Transdanubi-

an Range unit: a review and some new data. Vijesti Hrvatskoga
geološkog društva 37/3, 38—40.

Gyalog L. & Császár G. (Eds.) 1990: Geological map of the Bakony

Mts. (without Quaternary formations), 1:50,000. Geol. Inst. of
Hungary, Budapest.

Gyetvai G., Hegedűs T. & Ozsvárt P. 1996: Report about the area

between Kardosrét and Porva-Csesznek (Bakony Mts., Hunga-
ry). Student work, Dept. of Physical and Historical Geol.,
Eötvös University, Budapest, 1—47.

Haas J. 1995: Upper Triassic platform carbonates in the Northern

Bakony Mts. Földt. Közl. 125, 1—2, 27—64.

Haas J. (Ed.) 1996: Explanation to the Geological map of Hungary

without Cenozoic formations and to the Structural geological
map. Geol. Inst. Hungary, 1—185.

Kiss A. & Gellért B. 2000: Structural evolution of the Castle Hill of

Csesznek. Annual Meeting of Young Geoscientists, Hungarian
Geophysisists, Abstract volume, Debrecen, Hungary, 25 (in
Hungarian).

Kókay J. 1976: Geomechanical investigation of the southeastern

margin of the Bakony Mts. and the age of the Litér fault line.
Acta Geol. Hung. 20, 245—257.

Kókay J. 1996: Tectonic review of the Neogene Várpalota Basin.

Földt. Közl. 126, 417—446 (in Hungarian).

Korpás L. 1981: Oligocene—Lower Miocene formations of the

Transdanubian Central Mountains in Hungary. Ann. Hung.
Geol. Inst. 64, 1—140.

Kóta E. 2001: Structural geological analysis of the south-western

part of the Vértes Hills with GIS technique. Unpublished Mas-
ter thesis, Dept. Appl. Envir. Geol., Eötvös University, Budap-
est, 1—70 (in Hungarian).

Kováč M., Kováč P., Marko F., Karoli S. & Janočko J. 1995: The

190 KISS, GELLÉRT

and FODOR

East Slovakian Basin – A complex back-arc basin. Tectono-
physics 252, 453—466.

Lelkes Gy. 1990: Microfacies study of Tata Limestone Formation

(Aptian) in the northern Bakony Mountains, Hungary. Creta-
ceous Research 11, 273—287.

Ma enco L.C. 1997: Tectonic evolution of the outher Romanian

Carpathians. Ph.D. thesis, Vrije University, Amsterdam, Neth-
erlands, 1—160.

Mészáros J. 1968: Geological research of the surroundings of

Városlőd-Herend-Szentgál-Úrkút. A.R. Geol. Inst. Hungary
from 1966, 53—72 (in Hungarian).

Mészáros J. 1983: Structural and economic-geological significance

of strike-slip faults in the Bakony Mts. A. R. Geol. Inst. Hunga-
ry from 1981, 485—502 (in Hungarian).

Nemes F., Neubauer F., Cloething S. & Genser J. 1997: The Klagen-

furt basin in the eastern Alps: an intra-orogenic decoupled
flexural basin? Tectonophysics 282, 189—203.

Polinski R.F. & Eisbacher G.H. 1992: Deformation partitioning dur-

ing polyphase oblique convergence in the Karawanken Moun-
tains, southeastern Alps. J. Struct. Geol. 14, 1203—1213.

Royden L.E. & Horváth F. 1988: The Pannonian Basin. AAPG Mem-

oir 1—45.

Tari G. 1991: Multiple Miocene block rotation in the Bakony Moun-

tains, Transdanubian Central Range, Hungary. Tectonophysics
199, 93—103.

Tari G. 1994: Alpine Tectonics of the Pannonian basin. Ph.D. thesis,

Rice University, Texas, USA, 501.

Tari G. 1995: Eoalpine (Cretaceous) tectonics in the Alpine/Pan-

nonian  transition  zone.  In:  Horváth  F.,  Tari  G.  &  Bokor  Cs.
(Eds.):  Extensional  collapse  of  the  Alpine  orogene  and  Hy-
drocarbon  prospects  in  the  Basement  and  Basin  Fill  of  the
Western  Pannonian  Basin.  AAPG  International  Conference
and  Exhibition,  Nice,  France,  Guidebook  to  fieldtrip  No.  6.,
Hungary, 133—155.

Tari G. 1996: Extreme crustal extension in the Rába river extension-

al corridor (Austria/Hungary). Mitt. Gesell. Geol. u. Bergb.
Studenten Österr. 41, 1—18.

Tomljenović B. & Csontos L. 2001: Neogene-Quaternary structures

in the border zone between Alps, Dinarides and Pannonian ba-
sin (Hrvatsko Zagorje and Karlovac Basins, Croatia). Int. J.
Earth. Sci. in press.

Vörös A. & Galácz A. 1998: Jurassic paleogeography of the Trans-

danubian Central Range, (Hungary). Riv. Ital. Paleont. Stratigr.
104, 69—84.