PERMIAN-TRIASSIC EVOLUTION OF THE GREAT HUNGARIAN PLAIN 299
GEOLOGICA CARPATHICA, 54, 5, BRATISLAVA, OCTOBER 2003
GEOCHRONOLOGICAL CONSTRAINTS OF THE VARISCAN,
PERMIAN-TRIASSIC AND EO-ALPINE (CRETACEOUS) EVOLUTION
OF THE GREAT HUNGARIAN PLAIN BASEMENT
, WOLFGANG FRANK
and RALF SCHUSTER
Natural History Museum, Ludovika tér 2, H-1083 Budapest, Hungary; firstname.lastname@example.org
Institute of Geology, University of Vienna, Althanstrasse 14, A-1090 Vienna, Austria; email@example.com
Geological Survey of Austria, Rasumofskygasse 23, A-1031 Vienna, Austria; firstname.lastname@example.org
(Manuscript received September 11, 2002; accepted in revised form March 11, 2003)
Abstract: Core samples of metamorphic basement rocks from the Great Hungarian Plain (Tisza Megaunit) were studied
by petrographic and geochronological methods (Ar-Ar, Rb-Sr, Sm-Nd). On the basis of microtextural features of Al
polymorphs in metapelites a regional distribution pattern was found, which correlates with geochronological age groups.
This pattern confirms the earlier established tectonic subdivision of the basement of the Great Hungarian Plain, except
for the Algyõ basement-high, which has to be considered to represent a separate unit. A muscovite concentrate from a
granite sample of the Mecsek Subunit yielded a Variscan Ar-Ar age of 299 Ma. The medium-grade metapelites of the
Villány-Bihar Subunit are characterized by kyanite porphyroblast and sillimanite. Typical Ar-Ar muscovite ages are ca.
310 Ma and prove a Variscan cooling age of the metamorphic assemblages. In the NE part of the unit ages in the range
of 202266 Ma indicate a later thermal overprint. The staurolite and andalusite-bearing gneisses of the Békés-Codru
Subunit yielded Variscan cooling ages of ca. 320 Ma. In contrast, the rocks from the Algyõ basement-high experienced
their first metamorphic imprint in Early Permian time. Based on a Sm-Nd garnet isochron the high-temperature/low-
pressure assemblages, including andalusite+K-feldspar±sillimanite formed ca. 275 Ma. An amphibolite facies, eo-
Alpine (Cretaceous) overprint in the stability field of kyanite+staurolite+garnet is proved by Ar-Ar muscovite ages in
the range of 8295 Ma. It was followed locally by an Early Tertiary deformation. Considering the lithologies and the
metamorphic and structural evolution, the Algyõ-high shows many similarities to the Saualm-Koralm Complex of the
Austroalpine unit. Like the latter and the Baia de Aries nappe complex in the Apuseni Mountains, it obviously represents
an eo-Alpine thrust sheet.
Key words: Tisza Megaunit, Hungary, basement, Variscan, Permian and eo-Alpine metamorphism, Ar-Ar, Rb-Sr and
Numerous studies are dealing with the paleogeographical evo-
lution of the ALCAPA region (internal Eastern Alps-Car-
pathians-Pannonian Basin: Neubauer 1992). Traditionally the
pre-Alpine arrangement of the tectonic units is based on the
facies evolution of the Mesozoic cover series (e.g. Haas et al.
1995). However recent petrological and geochronological
studies result in detailed knowledge about most of the crystal-
line basement units, giving additional arguments for various
tectonic reconstructions. These studies have shown, that be-
sides a widespread Variscan metamorphic imprint, an eo-Al-
pine and also a Permo-Triassic imprint are important over
large areas (Árkai 1991; Lelkes-Felvári et al. 1996, 2001;
Thöni 1999; Hoinkes et al. 1999; Plaienka et al. 1999; Haas
et al. 2001; Schuster et al. 2001).
The Pannonian Basin is located in the centre of the ALCA-
PA region. The main tectonic elements, forming the basement
of this Tertiary basin are the Tisza Megaunit in the SE and the
Pelsó Megaunit to the NW. They are separated by the mid-
Hungarian line a major tectonic element of regional impor-
tance with a complex history (Csontos & Nagymarosy 1998)
(Fig. 1). Contradictory opinions exist about the Permo-Meso-
zoic location of the Tisza Megaunit. In the palinspastic recon-
struction by Stampfli & Mosar (1999) the Tisza Megaunit is
located between the Southalpine and the Austroalpine units.
The European affinity of its Permo-Mesozoic cover series was
recognized by Géczy (1973) and Haas et al. (1995). Accord-
ing to Buda (1992) and Buda et al. (1999) the granitoids of
Mecsek Mts can be related to the Moldanubian Zone of the
Central European Variscides.
Klötzli et al. (in print) assume a position of the Tisza Mega-
unit east of the Austroalpine units of the Eastern Alps, in the
vicinity of the Bohemian Massif and the Carpathians. One
reason for the contrasting opinions is the incomplete knowl-
edge about the basement of the Pannonian Basin, which is
mostly covered by Neogene sediments. Especially the area of
the Great Hungarian Plain (GHP), located east of the river
Danube is exclusively known from boreholes (Fig. 2).
In this paper petrological and geochronological data are
given for the metamorphic rocks of the Tisza Megaunit, in the
area of the Great Hungarian Plain. Geochronological age data
prove a Variscan metamorphic imprint and give arguments for
an eo-Alpine and also a Permo-Triassic imprint in some areas.
The basement of the GHP consists of metamorphic rocks,
Permian and Mesozoic sediments and volcanic rocks. The
300 LELKES-FELVÁRI, FRANK and SCHUSTER
presence of Carboniferous sediments was also discussed, but
not proved by biostratigraphic data (Jámbor 1998). Sporadi-
cally occurring, overlying Permian rhyolites and sandstones
were considered to prove a general pre-Alpine age of the me-
dium-grade metamorphic evolution in the basement. Ubiqui-
tous Lower Triassic sediments were considered as general
overstep-sequences in all units (Kovács et al. 2000). Miocene
conglomerates represent the most widespread sedimentary
cover, containing the basement rocks as pebbles.
Szepesházy (1978) established the lithostratigraphic corre-
lation of the sub-surface units in the GHP with the main tec-
tonic units of the Apuseni Mountains (Romania). According
to Szederkényi (1984) two main units make up the Tisza
Megaunit, the Central Hungarian Autochthon and the South
Hungarian Nappe. Fülöp (1994) distinguished three tectonic
units on the base of crystalline rock-types and Mesozoic sedi-
mentary facies zones (Fig. 2). These units, the Mecsek (MU),
Villány-Bihar- (VBU), and Békés-Codru Subunits (BCU) rep-
resent Cretaceous tectonic units. The first two represent the
autochthon of Szederkényi (1984) and the Kunságia Terrane
of Kovács et al. (2000) respectively, whereas the latter is
equivalent to the South Hungarian Nappe of Szederkényi
(1984) and the Békésia Terrane by Kovács et al. (2000).
Szepesházy (1978) considered a pre-Assyntian (Baikalian)
and Assyntian age of metamorpism, lacking any radiometric
data that time. According to Árkai et al. (1985) a medium
pressure first metamorphism was followed by a low pressure
overprint. Szederkényi (1996) distinguished three metamor-
phic imprints: 1) A high-pressure event responsible for eclog-
ites occurring in a narrow belt in the VBU, extending from
SW Transdanubia to the east of the Tisza river. This event
was assumed to be Caledonian in age (400440 Ma). 2) The
main metamorphic evolution was characterized by two
Variscan stages: the earlier (330350 Ma), related to medium
pressure-medium temperature (MPMT) conditions can be
traced in the whole basement with frequent kyanite as the
polymorph. The second phase occur-
ring in the BCU was characterized by low-pressure (LP) con-
Fig. 1. Tectonic map of the ALCAPA region with the distribution of the pre-Tertiary outcrop areas.
PERMIAN-TRIASSIC EVOLUTION OF THE GREAT HUNGARIAN PLAIN 301
ditions and radiometric ages in the range of 270330 Ma. 3)
Alpine ages of 7564 Ma were interpreted as contact effects of
Late Cretaceous magmatic bodies. However, the detailed cor-
relation of geochronological data with metamorphic evolution
and formation of mineral assemblages is still poorly under-
Eo-Alpine regional metamorphism in the basement of the
GHP was first reported by Árkai et al. (1998). It caused a very
low to low-grade prograde metamorphism in the Permo-
Mesozoic rocks beneath overthrust, polymetamorphic
Variscan basement rocks, and tectonic slices along the main
Alpine thrust zones. The K-Ar ages of fine-grained micas sep-
arated from basement rocks also show Alpine retrogression
within strongly tectonized metamorphic slices (Árkai et al.
Amphibole and garnet used for isotope determinations were
hand-picked under a binocular microscope. The coarsest mus-
covite and biotite (up to several mm) from the samples were sepa-
rated on a vibrating table and by grinding in alcohol, and a frac-
tion of 0.10.2 mm was analysed. The age dating was performed
in the Laboratory of Geochronology, University of Vienna.
To remove surface contaminations mineral concentrates
used for Sm-Nd and Rb-Sr analyses were leached in 2.5 M
HCl before decomposition for 5 minutes at about 50 °C.
Chemical sample digestion and element separation followed
the procedure outlined by Thöni & Jagoutz (1992). Overall
blank contributions are
0.2 ng for Nd and Sm, and
2 ng for
Rb and Sr. Nd and Sm concentrations were determined by iso-
tope dilution, using a mixed
Nd spike, and run as
metals on a Finnigan
MAT 262 multicollector mass spec-
trometer. Nd was ionized using a Re double filament. Within-
run isotope fractionation was corrected for
0.7219. All errors quoted in Tables 1 and 2 correspond to 2
of the block mean (1 block = 10 isotope ratios). The
ratio for the La Jolla international standard during the course
of this investigation was 0.511900±6 (9 runs). Errors for the
Nd ratio are ±1%, or smaller, based on iterative sam-
ple analysis and spike recalibration. Sr and Rb concentrations
were determined using a VG
Micromass M 30 and Ta fila-
ments. Through the course of this study the value for the NBS
987 Sr standard was 0.71011±6 (12 runs). Maximum errors
Sr ratios are estimated to be ±1 %.
Ar age determinations the mineral concentrates
were irradiated at the 9MW ASTRA reactor at the Austrian
Research Centre Seibersdorf or at the Institute of Isotopes
Budapest and analysed using standard procedures with a VG-
Fig. 2. Geological sub-surface map of the Great Hungarian Plain. The main structural elements and the locations of the investigated logs are shown.
302 LELKES-FELVÁRI, FRANK and SCHUSTER
IA [Ma] PA [Ma] TGA [Ma]
K-Fs+Pl+Ms+Qtz Ar-Ar Ms
Sarkadkeresztúr-ÉNY-2/4 Sark-ÉNY-2 40704073
Földes-6/2 whole rock
5400 Fisons Isotopes
mass spectrometer. Age calculation
was done after corrections for mass discrimination and radio-
active decay using the formulas given in Dalrymple et al.
(1984). The J-values are determined with internal laboratory
standards, calibrated by international standards including
muscovite Bern 4M (Burghele 1987) and amphibole MMhb-1
(Samson & Alexander 1987). The errors given on the calculat-
ed age of an individual step include only the 1
error of the
analytical data. The error of the plateau and total gas ages in-
cludes an additional error of ±0.4 % on the J-value, based on
repeated measurements of the standard.
The samples used for isotope analyses are described in the
Crystalline rocks of the logs were investigated by petro-
graphic and geochronological methods. During the first phase
of this research more than a thousand thin sections were in-
vestigated from all the tectonic units mentioned above to get
an overall picture of the main characters of the metamorphic
rocks. It turned out that the microtextural features of Al
polymorphs in metapelites are useful to group the rocks into
regional units, which can be correlated with the geochrono-
logical age groups.
In the following section, we describe characteristic features
of the investigated samples grouped according to the classical
tectonic subdivision of the GHP of the quoted authors. Sam-
Table 1: Sample localities, characteristic index minerals and age data of the investigated samples.
Table 2: Sm-Nd and Rb-Sr isotopic data from the Algyõ base-
ment-high and the Villány-Bihar Subunit.
Fig. 3. Lithologies of the Villány-Bihar and Békés-Codru Subunits.
A Retrogressed eclogite, Mezõsas-2/22742280 m. B Kyan-
ite-bearing micaschist, Szarvas-8/4. C Staurolite-garnet-bearing
micaschist, Szarvas-8/4. D Cataclastic, staurolite-bearing mic-
aschist, Öcsöd-3/1. E Kyanite-sillimanite-bearing gneiss, Szegh-
alom-15/4. F Staurolite-garnet-bearing micaschist, Álmosd-1/10.
G Mylonitic garnet micaschist, Földes-12/3. H Staurolite-an-
dalusite-bearing micaschist, Ruzsa-7/8. Photos AE and H: plane-
polarized light; F and G: crossed-polarized light. Lettering in the in-
dex of minerals refer to the proposed age of the mineral:
V=Variscan, P=Permo-Triassic, A=eo-Alpine.
PERMIAN-TRIASSIC EVOLUTION OF THE GREAT HUNGARIAN PLAIN 303
304 LELKES-FELVÁRI, FRANK and SCHUSTER
PERMIAN-TRIASSIC EVOLUTION OF THE GREAT HUNGARIAN PLAIN 305
ple locations and additional information are given in Table 1
and Figs. 58.
Metamorphic rocks of this subunit crop out outside the
GHP, to the west of the river Danube in Transdanubia, in the
Mórágy Hill. Starting from there a long, SW to NE directed
granitoid range, flanked by gneisses and micaschists is known
in the subsurface basement of the GHP. Al
tions were not described from this area until now.
The VBU is a composite subunit with internal thrusts,
where cataclastic crystalline rocks were thrust over differently
metamorphosed Mesozoic sedimentary and magmatic rock se-
quences (Pap 1990; Árkai et al. 1998). Sillimanite is wide-
spread among Al
polymorphs, and kyanite porphyro-
blasts occur in some lithologies. Retrogressed eclogites were
described from several logs along a zone exceeding 50 km,
parallel to the confining lineaments (M. Tóth 1995, 1997). A
new occurrence of retrogressed eclogite was identified in the
log Mezõsas-2. At present it is the easternmost occurrence in
this narrow eclogite belt.
Even if the high-pressure minerals are almost completely
destroyed by later overprint, the eclogitic origin is document-
ed by the microfabrics (Fig. 3A). The eclogite facies assem-
blage included garnet
quartz+apatite+rutile. Garnets are up to 1 mm in diameter. In
many cases they exhibit typical atoll-shapes with cores re-
placed by symplectites of biotite and plagioclase. The latter are
interpreted as remnants of a Ca-rich, high-pressure garnet
which has been partly or fully replaced during an amphibolite
facies overprint, whereas the rims (garnet
) remained stable.
Omphacite is not preserved. However the typical symplectite
textures of diopside and plagioclase replacing omphacite are
very common. Greenish hornblende crystals up to 1 mm are of-
ten surrounded by epidote and/or carbonate. During a green-
schist facies overprint diopside has been replaced by fine-
grained, faint green mineral aggregates including chlorite.
Fig. 4. Lithologies of the Algyõ basement-high. A Mylonitic
garnet micaschist, Dorozsma-38/2/1: Garnet porphyroblast (G
with large inclusions of biotite and plagioclase within a fine-grained
mylonitic matrix (S
) composed of biotite+plagioclase+quartz+
chlorite. B Mylonitic kyanite-biotite schist, Dorozsma-38/2/1:
fine-grained kyanite pseudomorph after andalusite in a fine-grained
biotite-rich matrix. The kyanite aggregate is replaced by sericite
along the edges. CD Staurolite kyanite-bearing micaschist,
Újszentiván-2/9. E Garnet-staurolite-bearing S-C mylonite, For-
ráskút-12/6. FG Mylonitic garnet-K-feldspar-bearing mic-
aschist, Dorozsma-7/10. H Garnet-bearing micaschist with
graphite pigment: Ferencszállás-K-6/3. The photos AF and H:
plane polarized light; G: crossed-polarized light. Lettering in the in-
dex of minerals refer to the proposed age of the mineral:
V=Variscan, P=PermianTriassic, A=eo-Alpine.
Ar age data from the Mecsek- and Villány-Bihar Subunit. Muscovites, biotite and hornblende yield ages in the range of 317±4
to 293±2 Ma. They represent Variscan cooling ages. The younger age from Álmosd is interpreted as a rejuvenated Variscan age.
306 LELKES-FELVÁRI, FRANK and SCHUSTER
Essential rock-types of VBU are fine-grained biotite-pla-
gioclase gneisses interlayered with coarse, K-feldspar-bearing
augengneisses, amphibolites and biotite-amphibole gneisses.
Subordinate micaschists contain kyanite porphyroblasts
(Fig. 3B) and staurolite (Fig. 3C,D). Garnet is a common
component in all lithotypes. Several pre- syn- and post-tecton-
ic types can be distinguished. Small garnet inclusions in pla-
gioclase are typical. Kyanite is present as up to some mm in
size, and sometimes deformed porphyroblasts. It is often re-
placed by sericite or coarse-grained muscovite. In one case
kyanite replacement by sillimanite has been observed (pers.
comm. by Zachar; Fig. 3E). Sillimanite is generally associated
with biotite flakes, occurring along borders of quartz rods and
as microveins cutting earlier structures. Andalusite was found
in one log forming a coarse-grained andalusite-quartz-vein.
In the NE part of the VBU Al
polymorphs are not
known. In the area of Álmosd coarse-grained micaschists and
amphibolites are present (see also Árkai 1987). The mic-
aschists are characterized by a mica-rich matrix and assem-
blages containing staurolite and garnet (Fig. 3F). Garnet
forms round grains, often present as inclusions within stauro-
lite. Garnet is also present as atoll-shaped crystals with cores
replaced by biotite and quartz. Late staurolite idioblasts con-
tain intrafolial folds marked by graphite pigment. Postkine-
matic biotite, muscovite and chlorite idioblasts measuring up
to 8 mm crosscut the schistosity planes. Quartz-rich bands
show static recrystallization with fine mica flakes and stauro-
lite poikiloblasts with quartz inclusions. Near to Földes mylo-
nitic micaschists (Fig. 3G), marbles and carbonate-mic-
aschists occur together with amphibolites.
There is a distinct contrast compared to the northern subunit
as no solitary kyanite porphyroblasts occur here, but instead
andalusite porphyroblasts are common in a northernmost nar-
row zone. In other areas Al
polymorphs were not found.
The coarse-grained andalusite-bearing gneisses contain au-
gens of feldspars and coarse muscovite flakes embedded in a
finer-grained mica matrix, often showing S-C structure. The
main foliation (S
) is defined by muscovite, biotite and idio-
blasts of ilmenite. Coarse mica flakes contain porphyroblasts
of garnet, staurolite and plagioclase. The S
foliation occurs as
relics of crenulations outlined by white mica within plagio-
clase. Garnet makes up solitary idioblasts in the matrix and is
included in staurolite. It is partially replaced by coarse biotite
flakes and/or chlorite. Staurolite idioblasts are marginally re-
placed along fractures by sericite and chlorite. Large biotite
flakes are strongly kinked. Plagioclase occurs as augens, some
of them with strong zoning and as porphyroblasts partially
overgrowing also the main schistosity S
. Andalusite porphy-
roblasts invade all pre-existing textures. They are partially re-
placed by sericite (Fig. 3H).
In the surroundings of the village of Algyõ a structural
basement-high has long been known. In this area lithologies
are varied with different types of gneisses, micaschists, am-
phibolites, chlorite schists, quartzites, pure and impure mar-
bles. Most of the rocks exhibit clear indications for a poly-
metamorphic history, with the whole range of typical defor-
mational microtextures. Minor texturally prograde rocks with-
out later overprint also occur.
Banded, mylonitic gneisses represent a very characteristic
lithology. They are fine-grained and dark-coloured, due to
high biotite content and graphitic pigment. In between there
are light-coloured layers of quartz and feldspar up to several
cm thick. Pre-mylonitic garnet porphyroblasts up to 2 cm in
diameter are frequent. Typically they contain coarse-grained
inclusions of biotite and plagioclase (Fig. 4A), indicating a
pre-mylonitic coarse-grained microtexture of the rocks. Por-
phyroblasts of K-feldspar and relics of staurolite occur in
some cases. There are also patches of fine-grained kyanite
(Fig. 4B). Szederkényi (1984) interpreted them as relics of
pre-existing andalusite and our investigations support this
idea. However they also partly represent former staurolite or
sillimanite. Staurolite and K-feldspars attain more than 1 cm
in diameter (Fig. 4C,F).
An overprint in the stability field of kyanite+staurolite+
garnet occurred contemporaneously to a ductile deformation
of the rocks. Deformation caused the development of a mylo-
nitic foliation S
, defined by fine-grained biotite, plagioclase
and quartz (Fig. 4E), as well as by newly formed muscovite.
The pre-existing garnet, staurolite and K-feldspar crystals act-
ed as porphyroclasts with respect to S
. In many cases the gar-
net porphyroblasts were broken and overgrown by a younger
garnet generation. The latter is rich in inclusions and also
present as tiny, anhedral grains in the matrix (Fig. 4F,G). The
K-feldspars were ductilely deformed and are preserved as au-
gens with subgrains along the crystal edges (Fig. 4F,G). Stau-
rolite was partly or fully replaced by fine-grained idioblasts
of kyanite and staurolite (Fig. 4C,D). The kyanite pseudo-
morphs are elongated within the mylonitic foliation. A green-
schist facies retrogression of various degrees caused chlori-
tization of garnet and the formation of chlorite and sericite in
In logs from Ferencszállás graphite-rich micaschists occur
with a fine-grained, mica-rich matrix overgrown by garnet
porphyroblasts and large biotite flakes (Fig. 4H).
Ar analytical data and age spectra are presented
in Figs. 58, the Rb-Sr and Sm-Nd analytical data in Table 2
and Figs. 6 and 9. All geochronological analytical data are
available from the authors.
Muscovite from a granitoid (sample Cegléd-3/13) yielded
an Ar-Ar plateau age of 299±4 Ma (Fig. 5). This age is in
agreement with other Variscan ages from this subunit (Klötzli
et al. in print).
From the eclogite zone an amphibole separate from an am-
phibolite (Szeghalom-16/4) has been dated. It yields a plateau
PERMIAN-TRIASSIC EVOLUTION OF THE GREAT HUNGARIAN PLAIN 307
Fig. 6. Ar-Ar and Rb-Sr age data from Földes in the NE-part of the Villány-Bihar Subunit. The ages in the range of 266±3 Ma to
200±2 Ma are interpreted as rejuvenated Variscan ages.
type Ar release pattern with an age of ca. 310±6 Ma and an
oldest age domain of 323 Ma. The low temperature steps
show a staircase pattern with minimum ca. 250 Ma and an ex-
cess Ar content in the first two steps (Fig. 5).
Sillimanite and kyanite-porphyroblast bearing rocks sup-
plied plateau-type Ar-Ar muscovite ages in the range of
297±2317±3 Ma (Ártánd-1/10, Szarvas-8/4, Biharkeresztes-
16/1), whereas an age of 293±2 Ma were obtained on a biotite
(Szarvas-8/4). Also a muscovite concentrate, separated from a
cataclastic micaschist from a tectonic slice near to the north-
ern border of the unit, yielded a plateau-type age spectra with
an age of 317±4 Ma (Öcsöd-3/2; Fig. 5). These data are in the
range of typical Variscan cooling ages.
From the NE part of this subunit younger Ar-Ar ages have
been determined (Fig. 6). Muscovite and biotite from Földes
yield plateau type Ar-spectra of 266±4 Ma (Földes-12/3) and
223±2 Ma (Földes-6/2). Rb-Sr dating of biotite from a biotite-
bearing amphibolite (Földes-6/2) yields 200±2 Ma (Fig. 6).
Although there is no large spread in the
Sr ratio, the
age is well defined, but it is either a typical Variscan or an Al-
pine age value. From a staurolite-garnet micaschist from Ál-
mosd-1/10 a saddle-shaped Ar-Ar muscovite age pattern of
ca. 202±2 Ma was obtained with a distinct rejuvenation at the
Plateau type Ar-Ar muscovite ages from the main part of
this subunit are in the range of 305±3 Ma to 322±4 Ma, mea-
sured from coarse-grained andalusite-bearing gneisses (Ru-
zsa-7/8, Ruzsa-D-1/3, Sarkadkeresztúr-ÉNY-2/4, Mezõ-
gyán-1/5; Fig. 7). Gneisses without andalusite from this subunit
also fit this range (Ásotthalom-11/2, Kelebia-3/9).
Additionally, a log from Pusztaföldvár (P-222/6) with a
narrow but rather intense ductile deformation zone, exhibiting
postkinematic growth of white micas, was investigated. Mus-
covite yields a plateau-type age pattern of 309±3 Ma with no
significant rejuvenation in the low temperature steps. From a
diaphtoritic mylonite (Szeged-11/6) two separates of fine-
grained (0.10.2 mm) white mica, contaminated by a small
amount of chlorite were measured. The purer sample yielded an
Ar-Ar age of 317±3 Ma, whereas the other gave 301±3 Ma.
In this tectonic unit the age of the oldest mineral assem-
blage was determined by Sm-Nd analyses from garnet and ky-
anite-bearing mylonites (Dorozsma-7/10). The isochron, cal-
culated from a porphyroclastic garnet separate (Grt
) and a
feldspar concentrate (Fs) yielded a Permian age of 273±7 Ma
(Fig. 9). Additional analyses of a leached garnet (Grt
) and the
leachate (L) do not fit exactly to the isochron. However, all
ages that can be calculated between the four data points are in
the range of 287 to 242 Ma and indicate a Permian age.
The cooling age of the following, amphibolite-grade over-
print was determined by Ar/Ar analyses on muscovites: six
yielded plateau or plateau-type ages. Four of them fall into the
narrow range of 82±188±2 Ma (Ferencszállás-K-3/5, Fer-
encszállás-13/18, Üllés-31/7/1, Újszentiván-2/9), and two
spectra exceed 90 Ma and exhibit slightly disturbed and sad-
dle-shaped patterns (Ferencszállás-K-6/3, Kiszombor-7/4).
Compared with the other samples, they have the same crystal-
lization and deformation history. The reason for the higher
ages is uncertain. Limited rejuvenations of ca. 70 Ma in low-
temperature steps are present in four of the samples. Two S-C
mylonites, attaining biotite-grade at Forráskút-12/6 and chlo-
rite-grade at Algyõ-52/5 supplied saddle-shaped age pattern
of the relict micas with distinctly lower total gas ages of 58±1
and 70±1, proving a distinct rejuvenation after the Late-Creta-
ceous cooling. The youngest ages from the low-temperature
steps are 53 and 42 Ma respectively, which indicate an Early
Tertiary deformation (Fig. 8).
308 LELKES-FELVÁRI, FRANK and SCHUSTER
Fig. 8. Ar-Ar muscovite ages from the Algyõ basement-high. The data in the range of 82 Ma to 95 Ma are interpreted as eo-Alpine cool-
ing ages. The lower values (5870 Ma, Algyõ-52 and Forráskút-12) represent rejuvenated and disturbed spectra from relictic white micas
from low-grade S-C mylonites, deformed during the Early Tertiary.
Fig. 7. Ar-Ar muscovite ages from the Békés-Codru Subunit. The age data in the narrow range of 323 Ma to 305 Ma reflect cooling ages
of the Variscan tectonometamorphic event.
PERMIAN-TRIASSIC EVOLUTION OF THE GREAT HUNGARIAN PLAIN 309
In this chapter the distribution of the Al
and the new geochronological age data is discussed, with re-
spect to the established tectonic subdivision of the basement
of the GHP. After that the metamorphic histories of the base-
ment blocks are compared to each other.
Metamorphic evolution of the Villány-Bihar Subunit
The main stages of the metamorphic evolution in the VBU
are an eclogite facies imprint preserved only within metabasic
rocks, and a subsequent amphibolite- and greenschist facies
overprint. The eclogite facies assemblage included garnet
+apatite+rutile+ore. The eclogites exhibit several stages of
retrograde overprints, causing the formation of different types
of symplectites. During an amphibolite facies overprint most
of the high-pressure minerals were destroyed and an assem-
blage including garnet
+ore developed. Greenschist facies retrogression is
displayed by chloritization of diopside and the crystallization
of epidote and carbonate.
M. Tóth (1997) proposed two distinct metamorphic cycles
for the PTt evolution of the eclogitic rocks. In this model
the first event caused the eclogite facies imprint, with pres-
sures up to 1012 kbar and 600650
C. For this event a Cale-
donian age was suggested (Szederkényi 1996). It was fol-
lowed by exhumation to greenschist facies crustal levels. The
subsequent amphibolite facies event and the following green-
schist facies retrogression have been proposed to be Variscan
in age. However, there are no geochronological age data
available, giving the age of the eclogite facies event. From our
petrographic investigations the eclogite facies assemblage and
the overprinting amphibolite facies assemblage can be placed
within the frame of a single clockwise PTt evolution path.
The investigated metapelites of the VBU show clear evi-
dence of a medium- to high-pressure amphibolite facies meta-
morphic event. In the metapelites assemblages of garnet+ ky-
anite+ staurolite are followed by the formation of sillimanite
and later greenschist facies retrogression. This clockwise P
Tt path can be correlated with the post-eclogite facies evolu-
tion of the eclogites. Cooling ages measured with several
methods on different lithologies yielded ca. 308±3317±3 Ma
and point to a Variscan age of this tectonothermal event. As
there are no indications for an older metamorphic assemblage
in the country rocks, and as we could not find indications for a
two stage metamorphic evolution in the eclogites we favour
an early Variscan age of the eclogite facies event.
Several samples yielded Ar-Ar muscovite ages younger
than typical Variscan cooling ages in the NE part of this sub-
unit. A plateau type age of 297±2 Ma from Ártánd is only
slightly younger, whereas coarse muscovite fishes from a
mylonitic micaschist without kyanite from Földes yield a re-
markably younger age (266±3 Ma). Important for the interpre-
tation of this area is the Rb-Sr biotite age of 223±2 Ma from
the same locality (see below). Also a muscovite from the tex-
turally undisturbed amphibolite facies metamorphic rocks of
Álmosd yielded a saddle-shaped Ar-Ar spectra of 202±2 Ma
and a distinct rejuvenation in the low-temperature steps.
These younger ages of the NE part of the VBU might reflect
an independent Permian event, or a rejuvenation of Variscan
ages during a later, Cretaceous overprint.
One argument for a PermianTriassic age comes from the
geochronological age data: to open and fully reset the Ar-Ar
isotopic system in muscovite, temperatures of at least up to
C are necessary. At these temperatures a total reset of the
Rb-Sr biotite ages can be expected. Therefore the Rb-Sr bi-
otite age of ca. 220 Ma supports a Triassic cooling of the
rocks. Ar-Ar muscovite ages in the range of 280 to 190 Ma to-
gether with Rb-Sr biotite ages of 225 to 150 Ma have been
found in several parts of the Austroalpine crystalline base-
ment unit, where the Cretaceous overprint did not exceed low-
ermost greenschist facies conditions. These data are interpret-
ed as reflecting cooling from a high to a lower geothermal
gradient, during a Permo-Triassic extensional event (Schuster
et al. 2001). Our data from the VBU are definitely too scarce
to justify such an interpretation. However, similar data were
recently published from the Szeghalom structural basement-
high (Balogh in M. Tóth et al. 2000). A series of ten K-Ar
data on amphibole concentrates yielded three age groups of
315, 260 and about 220 Ma.
On the other hand several facts argue for an eo-Alpine over-
print of the rocks: the existence of a Cretaceous event along
the northern border of the VBU is well documented by Árkai
et al. (1998). Fine-grained (<2
m) mica from Mesozoic sedi-
ments situated beneath overthrust complexes, as well as from
polymetamorphic rocks of the overthrust tectonic slices yield-
ed Cretaceous ages in the range of 64 to 99 Ma. Very low- to
low-grade metamorphic conditions were reached during my-
lonitic and cataclastic deformation of the rocks. In our data
this Cretaceous overprint is hardly visible, because we inves-
tigated the coarse white mica flakes belonging to the main
Variscan mineral assemblages. For example the cataclastic
gneisses from log Öcsöd represent crystalline rocks thrust
over Cretaceous metabasites. Its coarse-grained muscovite
yielded an age of 317±3 Ma, but there is also a fine-grained
sericite present in the sample, which has not been investigated
during this study.
Fig. 9. Sm-Nd garnet isochron from the Algyõ basement-high. The
age is interpreted as the formation age of the high-temperature/
low-pressure assemblage of the rocks.
310 LELKES-FELVÁRI, FRANK and SCHUSTER
Another argument is that the Triassic facies evolution of the
VBU is characterized by a clastic Upper Triassic (Keuper)
succession. Such a sedimentary environment is not expected
when a Permian lithospheric thinning associated with pro-
grade metamorphism took place (Schuster et al. 2001).
However, at present we have to leave it open, whether the
younger ages in the NE part of the VBU are due to rejuvena-
tion caused by an eo-Alpine overprint or a prolonged cooling
history during PermianTriassic times. Further investigations
are in progress to solve this question.
Metamorphic evolution of the Békés-Codru Subunit
Assemblages containing andalusite and staurolite indicate
low-pressure amphibolite facies conditions along the northern
border of the BCU from Ruzsa in the SW to Mezõgyán in the
NE for the dominant metamorphic imprint. Muscovite from
these coarse-grained assemblages yielded cooling ages in the
range of 305322 Ma. The same range was also obtained from
rock types without andalusite. A mica-rich fraction from a
mylonitic micaschist coming from Szeged, from the flank of
the Algyõ basement-high also fits this range, even if the Ar-
pattern shows distinct rejuvenation in the low-temperature
Metamorphic evolution of the Algyõ basement-high
From the basement-high in the surroundings of Algyõ a se-
ries of samples with characteristic features have been investi-
gated, which are not known from other locations in the Tisza
Megaunit. On the basis of the microfabrics at least two meta-
morphic events can be distinguished in most of the samples:
in the samples from Dorozsma: a first, coarse-grained assem-
blage including garnet
+quartz±muscovite developed. Relics of kyanite aggregates
render possible the former presence of andalusite and silli-
manite. The occurrence of andalusite, sillimanite and K-feld-
spar clearly indicate high temperature/low pressure character-
istics and high-amphibolite to granulite facies conditions.
Considering the Sm-Nd garnet isochron age this association
formed in Permian time at ca. 275 Ma.
Several previous papers deal with the P-T conditions of the
first metamorphic imprint in the Algyõ basement-high.
Szederkényi (1984) found 570630
C at about 2 kbar in am-
phibolites from Algyõ. In contrast Horváth & Árkai (2002)
C and 810 kbar from Ferencszállás.
The latter conditions are far outside the stability field of an-
dalusite and sillimanite. A possibility to explain this misfit is
to suppose that the Algyõ basement-high itself is a composite
Fig. 10. Sub-surface map of the Great Hungarian Plain, showing the distribution of the index minerals and the geochronological age data.
Kyanite porphyroblasts and sillimanite is restricted to the VBU, while andalusite porphyroblasts are widespread in the BCU. Kyanite and
andalusite porphyroblast-bearing rocks of the VBU and BCU supplied exclusively Variscan ages. In the NE part of the VBU, in the area
of Földes and Álmosd ages younger than typical Variscan cooling ages were found. The Algyõ-high is characterized by ubiquitous kyan-
ite aggregates, a Permian age of garnet porphyroclasts and middle Cretaceous to Tertiary Ar-Ar muscovite ages.
PERMIAN-TRIASSIC EVOLUTION OF THE GREAT HUNGARIAN PLAIN 311
unit. Partly it consists of rocks with a first Variscan assem-
blage of medium- to high-pressure characteristics, whereas
other parts got their first imprint during a Permo-Triassic
high-temperature/low-pressure event. At first sight this inter-
pretation might seem to be unlikely, but in the Austroalpine
unit such a situation has been observed (Schuster et al. 2001)
(see also discussion below).
The second event caused the formation of the main assem-
+plagioclase ± muscovite+
quartz and a contemporaneous mylonitization of the rocks.
With respect to the equilibrium assemblage kyanite+stauro-
lite+garnet, medium-pressure amphibolite facies event can be
assumed. Recently conditions of 650680
C at 59 kbar
have been published for this overprinting event (Horváth &
Árkai 2002). At present the exact timing of the peak of this
metamorphic imprint is unknown. However, all investigated
samples yielded Ar-Ar muscovite cooling ages in the range of
82 to 95 Ma, without any older relics. Similar ages by Balogh
& Pécskay (2001) were also reported. These data indicate an
eo-Alpine age of the imprint. After the metamorphic peak a
greenschist facies overprint occurred. It caused sericitization
and chloritization during ongoing deformation. The intensity
of this overprint is variable in the different samples. It might
explain the younger Ar-Ar muscovite ages of 58 to 70 Ma.
Algyõ basement-high and Austroalpine Saualm-Koralm
On the basis of the new results the rocks from the Algyõ-
high exhibit a completely different evolutionary history com-
pared to other basement rocks of the Tisza Megaunit. As men-
tioned in Lelkes et al. (2001, 2002) the very special
lithologies of the Algyõ-high resemble the metamorphic suc-
cession of the Saualm-Koralm Complex and the Strallegg
Complex of the Austroalpine domain in the Eastern Alps. The
latter forms eo-Alpine thrust sheets, which hold high tectonic
positions in the eo-Alpine nappe stack (Weissenbach 1975;
Frank 1987; Krohe 1987; Schuster et al. 2001). They were af-
fected by Permo-Triassic lithospheric extension (Habler &
Thöni 2000; Schuster et al. 2001), and an intense eo-Alpine
tectonometamorphic overprint (Frank 1987; Thöni & Miller
1996). Lithospheric extension caused a high-temperature/low-
pressure metamorphic imprint in the stability field of an-
dalusite and sillimanite and the formation of gabbroic intru-
sions and numerous anatectic pegmatites. The Cretaceous
overprint reached eclogite and following amphibolite facies
conditions and the pre-existing andalusite and sillimanite
were replaced by kyanite aggregates. This was accompanied
by mylonitization during exhumation processes including N-
to NW-directed thrusting.
The microtextural features of the Algyõ basement-high are
very similar to those of the Saualm-Koralm Complex and give
additional argument for the metamorphic history discussed
Contrasting metamorphic evolutions
In the past, several authors proposed pre-Variscan meta-
morphic evolution for parts of the crystalline basement in the
GHP. However, at present either geochronological age data or
undoubted microtextural observations prove such interpreta-
The oldest available age data in the range of 300 Ma to 330
Ma have been measured on hornblende and muscovite by the
K-Ar and Ar-Ar method. As they derive from medium-grade
rocks, they have to be interpreted as metamorphic cooling
ages. They indicate a Variscan age of the dominant tectono-
thermal imprint. At present nothing is known about the exact
timing of the eclogite facies event, or about the timing of the
metamorphic peak in the VBU or BCU.
For the understanding of the Variscan geodynamic evolu-
tion of the area, it would be important to know if the an-
dalusite in the BCU developed contemporaneously to the
pressure peak and the kyanite formation, or synchronously to
the temperature peak and the sillimanite formation in the
VBU. In the first case a completely different tectonic setting is
evident, whereas in the second case only different metamor-
phic conditions during the exhumation of the rocks can be as-
sumed. However, as kyanite porphyroblasts overgrown by sil-
limanite and andalusite occur in different basement blocks,
and no other Al
polymorph have been found in the an-
dalusite-bearing lithologies, there is no microtextural evi-
dence about the relative age relationship of these minerals in
the units of the GHP. This is in contrast to the SW part of the
Tisza Megaunit in Transdanubia: in the Mecsek Subunit both
kyanite and andalusite are known from the same rock and an-
dalusite is a late crystallization phase overgrowing kyanite
(Lelkes-Felvári et al. 1989; Török 1990).
A key point in understanding the contrasting histories of the
Algyõ basement-high with respect to the surrounding BCU,
are the ages of the andalusite-bearing mineral assemblages. In
the BCU andalusite is well preserved and like the coexisting
garnet, it is Variscan in age. On the other hand, in the Algyõ-
high andalusite is totally transformed into kyanite aggregates
during the eo-Alpine tectonothermal event; one would con-
clude that lithologies from the BCU were the precursor rocks
of the Algyõ-high. The important observation, that the first
generation of garnet in the Algyõ basement is Permian in age
although only demonstrated up to now in a single sample
is not compatible with this assumption. The Permian gar-
net age is likely also because of the remarkable analogies of
the Algyõ-high and the Austroalpine Saualm-Koralm Com-
There is another remarkable difference in the tectonic evo-
lution of the different crustal blocks in the GHP. In the VBU
Lower Permian rhyolites are only described from one restrict-
ed area, and tectonic contacts of the Mesozoic sediments to
the crystalline basement rocks are proved in several places. As
the rocks cooled down at about 310 Ma, they stayed in a shal-
low crustal level since that time, and we do not know when
they reached the surface. In contrast, in the BCU Lower Per-
mian rhyolites and Lower Triassic redbeds are overlying the
basement with a sedimentary contact (Majoros 1998). For this
reason the basement rocks formed the surface in late Paleozo-
ic times. As the Algyõ-high experienced a Permian metamor-
phic imprint, located in middle crustal levels at that time,
consequently, there are no Permian-Triassic sediments in strat-
312 LELKES-FELVÁRI, FRANK and SCHUSTER
According to Tari et al. (1999) the Algyõ basement-high
represents a metamorphic dome, which formed as a core com-
plex during Miocene extensional processes. In this model the
lower part of a Variscan crustal section experienced a thermal
overprint in Cretaceous times and was exhumed by a Tertiary
fault system. On the basis of the new data such an interpreta-
tion is unlikely with respect to the contrasting evolution of the
surrounding BCU. As mentioned before, the rocks of the Al-
gyõ-high are not the result of eo-Alpine, overprinted litholo-
gies of the BCU. Furthermore, they experienced not only a
Cretaceous thermal overprint, but also mylonitic deformation.
Therefore the proposed scenario would only be possible when
the BCU would have been thrust onto a basement wedge with
the characteristics of the Algyõ-high. This must have hap-
pened after the eo-Alpine tectonothermal event, and prior to
the formation of the core complex.
Therefore we interpret the Algyõ sequence as a tectonic
outlier of a Cretaceous metamorphic nappe system. A similar
interpretation has been already proposed by Dimitrescu
(1995), on the basis of lithological correlation. He compared
the sequence of the Algyõ basement with the Biharia Unit,
considered of that time the uppermost unit of the Biharia
nappe system in the Apuseni Mountains (Balintoni 1994).
Both units are characterized by carbonates, completely lack-
ing in the surrounding basement. Cretaceous Ar-Ar ages were
reported from the uppermost nappe of the Apuseni Mountains
(Baia de Arieº nappe-complex, Soroiu et al. 1969; Dallmeyer
et al. 1994, 1996, 1999). The exact timing of the emplacement
of this nappe, resting on top of a Variscan metamorphic base-
ment is unknown. As the Variscan basement of the BCU
shows a weak, low-temperature hydrothermal alteration, we
can exclude emplacement during the eo-Alpine tectonometa-
morphic event. The emplacement of the Algyõ-high is defi-
nitely younger than the main cooling of the rocks, which is
dated at ca. 80 Ma. The Ar-Ar age spectra of some micas
show indications for a younger thermal overprint causing mi-
nor rejuvenation up to 40 Ma. A possible solution would be
that the final emplacement of this unit occurred in the Early
The observed distribution of the Al
the new geochronological age data confirm the established
tectonic subdivision of the basement of the GHP, except for
the Algyõ basement-high, which has to be excluded from the
VBU and considered as a separate unit.
The distribution of the Al
polymorphs shows a clear
regional distribution: kyanite porphyroblasts together with sil-
limanite are restricted to the VBU, while andalusite porphyro-
blasts are widespread in the BCU. The Algyõ-high is charac-
terized by ubiquitous kyanite aggregates, which are
interpreted as pseudomorphs after pre-existing andalusite and
minor sillimanite and staurolite.
A granite of the Mecsek Subunit yielded an Ar-Ar musco-
vite age of ca. 300 Ma. Variscan cooling ages of ca. 310 and
320 Ma were found in the VBU and BCU, indicating
Variscan formation ages for the observed assemblages. Only
in the NE part of the VBU (Földes and Álmosd) were ages
younger than typical Variscan cooling ages measured. They
indicate a Permo-Triassic, or an eo-Alpine thermal overprint.
In the Algyõ basement-high a first Permo-Triassic HT/LP
event, with peak conditions at about 275 Ma is proved at least
for some lithologies. The Ar-Ar mica ages from this unit are
exclusively younger than middle Cretaceous. They demon-
strate the age of cooling after the amphibolite facies imprint
and subsequent deformational overprint of the rocks. Consid-
ering the metamorphic and structural evolution, the Algyõ-
high shows many similarities to the Saualm-Koralm Complex
of the Austroalpine. Similarly to the Baia de Arieº nappe-sys-
tem in the Apuseni Mountains, they might represent an eo-Al-
pine thrust sheet. It took place on top of the BCU after the
cooling of the rocks, in latest Cretaceous or Tertiary times.
The observed zonal distribution argues for distinct meta-
morphic histories of the different tectonic elements of the Tis-
za Megaunit. This implies that this terrane is not as homoge-
neous in a tectonic sense, as it has been presented in parts of
Acknowledgments: The Hungarian Oil and Gas Plc. is
thanked for providing core samples for investigations. T.
Szederkényi generously offered the thin section collection of
Szeged University for the microscopic survey of the base-
ment. Research was supported by the Grants 23940 and
37243 of the Hungarian Scientific Research Fund (OTKA),
by FARGON and by the Austrian Science Fund FWF, Project
P14525-GEO. The authors thank M. Jelenc for help with the
Sm-Nd isotope analyses. Discussion with B. Cserepes-Meszé-
na and A. Nusszer is greatly appreciated. J. Zachar is thanked
for providing photos. Constructive reviews by P. Árkai, M.
Janák and F. Neubauer is acknowledged.
Thin section description of the samples investigated by geochrono-
logical methods. Mineral names are abbreviated according to Kretz
Cegléd-1/13: Medium-grained granite with mineral assemblage of
Kfs+Pl+Qtz+Ms+Bt+Zrn. Ms is well preserved and up to 7 mm in size.
Kfs is altered. Bt is replaced by Chl+Cc+ore.
Öcsöd-3/2: Cataclastic St micaschist. The coarse-grained matrix is
composed of Bt+Ms+Pl+Qtz. St forms idioblasts up to 3 mm partly re-
placed by sericite.
Szarvas and Ártánd area: Ky bearing, fine- to medium-grained Qtz-
micaschists, Pl gneisses (Szarvas-8/4) and Mc gneisses (Ártánd-1/10).
The main foliation (S
) is defined by micas and elongated Qtz rods. Rel-
ics of S
are outlined in Pl microaugens by inclusions of Qtz, St, Grt and
Bt. Pl is rarely zoned (Ártánd). Postkinematic Ky idioblasts are partially
replaced by Ms and sericite. St idioblasts contain Bt inclusions and are
partially replaced by sericite. Sil fibres are associated to Bt. Grt makes
up small idioblasts and atoll-like crystals with cores filled up by
Biharkeresztes-16/1: Coarse-grained Sil-Pl gneiss. Mica-rich layers
PERMIAN-TRIASSIC EVOLUTION OF THE GREAT HUNGARIAN PLAIN 313
contain deformed Bt flakes and subordinate Ms. Abundant Sil is associ-
ated with Bt. Pl xenoblasts are replaced by sericite. Spn idioblasts are
evenly distributed. Late carbonate veins crosscut the rock.
Földes-6/2: Fine-grained mylonitic Bt-amphibole gneiss. Fine lami-
nae composed mainly of acicular Am, some Bt and ore alternate with
fine-grained Qtz-rich layers and coarser, Bt-rich layers containing also
Földes-12/3: Fine-grained mylonitic Bt-Ms gneiss with Pl-microau-
gens attaining 3.5 mm. Recrystallized polycrystalline Ms-fishes are em-
bedded in a Qtz matrix with very fine-grained Bt, some Ms and some
small Pl granoblasts. Grt idioblasts (0.75 mm) are included in Ms and
Pl, bigger crystals occur in the matrix.
Álmosd-1/9: Micaschist. Within a fine-grained Mu-rich matrix Grt
(4 mm) and St (9 mm) porphyroblasts occur. The S
of Grt idioblasts are
strongly discordant to the S
of the matrix. The cores of some atoll
shaped Grt crystals are filled with coarse Bt+Qtz. Small, round Grt
(2 mm) are included in St. Late St idioblasts contain intrafolial folds
marked by Gr. Bt idioblasts up to 8 mm crosscut the schistosity planes.
Qtz-rich bands show static recrystallization, containing fine mica flakes
and St poikiloblasts.
Szeghalom-176/4: Bt-amphibole gneiss, composed of nematoblasts
of Am (up to 2 mm), Bt flakes and granoblastic Qtz and Pl with relict
zoning. Grt up to 2.5 mm is partially or completely replaced by Pl, with
Grt relics as small islands. Pl is partially replaced by sericite. Bt up to
4 mm is almost completely replaced by Chl and Spn.
Ruzsa-7/8, Ruzsa-D-1/3, Sarkadkeresztúr-ÉNY-2/4, Mezõgyán-1/5:
Coarse-grained And-bearing gneisses, often showing S-C structures. Fs
augens and coarse Ms flakes are embedded in a finer-grained mica ma-
trix rich in Bt. The main foliation (S
) is defined by the micas, contain-
ing porphyroblasts of Grt, St and Pl. Relic of a crenulated cleavage S
outlined by Ms inclusions within Pl. Grt makes up solitary idioblasts in
the matrix or small inclusions in St. It is partially replaced by coarse Bt
flakes and/or Chl. St is marginally replaced by sericite and Chl. Bt
flakes are strongly kinked. Zoned Pl augens, occur also as late porphy-
roblasts including partially also S
. And porphyroblasts invade all pre-
existing textures. Idioblasts of Ilm are included in the porphyroblasts
and the matrix.
Kelebia-3/9: Pl gneiss with micro-augen texture. Elongated, poly-
crystalline augens of Pl (up to 3.5 mm) contain idioblasts of Grt
(0.25 mm), green Bt, Ms and Ap inclusions. Bt flakes (2 mm) are dis-
persed, small flakes of Ms occur in Qtz-rich domains and are intergrown
with Bt in mica-rich domains.
Ásotthalom-5/6: Garnet-bearing Ms-Bt gneiss. Fine-grained mica-
rich layers contain deformed Bt flakes (up to 4 mm), partially altered to
Chl, Ms flakes crowded with small, postkinematic Ms. Grt up to 5 mm
is replaced by Bt. Subhedral grains of Pl (3.5 mm) are surrounded by Bt.
Polygonal Qtz-rich layers contain small Ms flakes.
Pusztaföldvár-222/6: Coarse-grained garnet-bearing micaschist with
strong Ms recrystallization. Bt is completely replaced by Chl and Spn
aggregates. Grt (2.5 mm) is replaced by Chl. Within a narrow ductile
shear zone Ms suffered grain size reduction and Chl and Cal appear as a
new mineral phase.
Szeged-15/5: Mylonitic micaschist with quartz ribbons. In the Ms-
rich, fine-grained matrix some Chl is present making up postkinematic
flakes and lenses along opacitic seams. Elongated porhyroclasts of Grt
(up to 1 cm) are replaced by carbonate and Chl. Pl xenoblasts contain
Algyõ-52/5: Mylonitic S-C quartz-micaschist. Qtz and mica-rich
bands alternate. It is cut by thin penetrative shear-plains with grain-size
reduction. Mica-rich bands are composed of deformed, recrystallized
Ms and Bt fishes set in a finer-grained matrix of decussate flakes of Ms
and Bt. Grt is broken, elongated and partially replaced by
Ms+Bt+Chl+ore. Pl forms polycrystalline augens and lenses with Bt in-
clusions and recrystallized mosaic structures.
Ferencszállás-K-3/5: Micaschist, gently folded with anastomosing
very fine, brittle, chloritic shear planes. In the matrix composed of de-
cussate flakes of Ms and finer-grained Bt round, broken Grt porphyro-
clasts occur. They are up to 3 mm and partially replaced by Bt and Chl.
Ferencszállás-K-6/3: Banded, fine-grained, slightly folded mic-
aschist. Late idioblasts of Grt (up to 2.5 mm) include folded trails of Gr,
slightly discordant to S
. Further they make up atolls with Qtz and Bt-
rich cores. Chl flakes (1.5 mm) occur in the pressure shadows of Grt.
Qtz-rich bands show static recrystallization.
Ferencszállás-13/18: Banded Ms-Bt paragneiss with mylonitic folia-
tion. Mica-rich bands composed of decussate Bt+Ms flakes alternate
with Qtz-rich bands with granoblastic textures. Pl contains relics of ear-
lier folds enhanced by Bt flakes. Prekinematic porphyroblasts of Grt are
up to 4 mm and show inclusions of Bt and Rt.
Üllés-31/7: Crenulated micaschist. Mica-rich bands of decussate
flakes of Bt+Ms alternate with Qtz+Pl-rich bands. Two generations of
St can be distinguished: St
attaining several mm occur as isolated relics
with uniform optical orientation within aggregates of Ky±St. They of-
ten have dark, fluid-inclusion-crowded rims. Small idioblasts of St
cur in the mica-rich, Gr-bearing matrix. Some are intergrown with Ky,
containing inclusion-rich cores. Grt
is broken and partly replaced by
Chl. Inclusion-rich cores are surrounded by clear rims composed of sev-
eral adjoining tiny crystals. Late shear plains S
marked by Bt crosscut
the mylonitic foliation S
Újszentiván-2/9: Plagioclase gneiss. Relic microfolded schistosity
), outlined by Gr pigment is enclosed in Pl and St. Anhedral grains of
Pl (5 mm) and porphyroblasts of Grt and St are set in a matrix, com-
posed of postkinematic flakes of Ms and Bt. St relics (up to one cm) are
surrounded by Ky aggregates and sericite. Grt
(6 mm) contains Ilm and
Qtz inclusions. Broken parts surrounded by strings of Grt
also make up
Kiszombor-7/4: Crenulated micaschist. Ms and Bt with strong postki-
nematic crystallization make up mica-rich layers. Qtz-rich granoblastic
bands bear some anhedral Pl. Broken and round Grt crystals up to
2.5 mm in size are partially replaced by Chl and Bt.
Forráskút-12/6: Mylonitic micaschist with S-C structure. Coarse,
polycrystalline Ms fishes and small augens of Pl are embedded in fine-
grained Qtz-rich granoblastic matrix with a penetrative schistosity, con-
taining very fine-grained Bt flakes. Small idioblasts of St (single crys-
tals or crystal groups, 0.250.5 mm) are cut by shear plains. Euhedral
rims of Grt idioblasts (up to 0.8 mm) contain inclusions from the mylo-
Dorozsma-7/10: Fine-grained, strongly foliated mylonitic micaschist
to gneiss. Porphyroclasts of Grt
, Kfs and Pl are embedded in a fine-
grained matrix composed of Ky+Bt+Qtz. Grt
shows inclusions of
coarse-grained Bt and Pl. Kfs forms up to one centimetre large crystals
with recrystallization at the crystal edges. The second Grt generation
) is rich in tiny inclusions, and forms rims around pre-existing Grt
and small idioblasts in Qtz-rich domains.
Árkai P. 1987: Contribution to the knowledge of the polymetamor-
phic basement of the Great Plain (Pannonian Basin, East Hun-
gary): the environment of the Derecske depression. Fragm.
Mineral. Palaeont. 13, 720
Árkai P. 1991: Alpine regional metamorphism of the different tec-
tonic domains in the Hungarian part of the Pannonian Basin.
In: Baud A., Thélin P. & Stampfli G. (Eds.): Paleozoic geody-
namic domains and their Alpidic evolution in the Tethys.
IGCP No 276 Newsletter No 2, Mémoires de Géologie, Lau-
sanne 10, 513.
Árkai P., Bérczi-Makk A. & Balogh Kad. 2000: Alpine low-T pro-
grade metamorphism in the post-Variscan basement of the
Great Plain, Tisza Unit (Pannonian Basin, Hungary). Acta
Geol. Hung. 43, 1, 4363.
Árkai P., Bérczi-Makk A. & Hajdu D. 1998: Alpine prograde and
retrograde metamorphism in an overthrusted part of the base-
ment, Great Plain, Pannonian Basin, Eastern Hungary. Acta
314 LELKES-FELVÁRI, FRANK and SCHUSTER
Geol. Hung., 41, 2, 179210.
Árkai P., Nagy G. & Dobosi G. 1985: Polymetamorphic evolution
of the South-Hugarian crystalline basement, Pannonian basin:
geothermometric and geobarometric data. Acta Geol. Hung.
Balintoni J. 1994: Structure of the Apuseni Mts. Romanian J. Tect.
Reg. Geol. 75, 2, 5157.
Balogh Kad. & Pécskay Z. 2001: K/Ar and Ar/Ar geochronological
studies in the Pannonian-Carpathians-Dinarides (PANCARDI)
region. Acta Geol. Hung. 44, 23, 281299.
Buda Gy. 1992: Tectonic settings of the Variscan granitoids occur-
ring in Hungary and some other surrounding areas. Terra Nova
Abstract Supplement 2, 10.
Buda Gy., Lovas G., Klötzli U.S. & Cousens B.L. 1999: Variscan
granitoids of the Mórágy Hills, (South Hungary). Ber. Dtsch.
Min. Gesell. 2, 2134.
Burghele A. 1987: Propagation of error and choice of standard in
Ar technique. Chem. Geol. 66, 1719.
Csontos L. & Nagymarosy A. 1998: The Mid-Hungarian line: a zone
of repeated tectonic inversions. Tectonophysics 297, 5171.
Dallmeyer R.D., Neubauer F., Pana D. & Fritz H. 1994: Variscan vs.
Alpine tectonothermal evolution within the Apuseni Moun-
tains, Romania: evidence from
Ar mineral ages. Rom. J.
Tectonics Reg. Geol. 75, 2, 6576.
Dallmeyer R.D., Neubauer F., Handler N., Fritz H., Müller W., Panã
D. & Puti M. 1996: Tectonothermal evolution of the internal
Alps and Carpathians: Evidence from
Ar mineral and
whole-rock data. Eclogae Geol. Helv. 89, 1, 203227.
Dallmeyer R.D., Panã D.I., Neubauer F. & Erdmer P. 1999: Tec-
tonothermal evolution of the Apuseni Mountains, Romania:
resolution of Variscan versus Alpine events with
ages. J. Geol. 107, 329352.
Dalrymple G.B., Alexander E.C., Lanphere M.A. & Kraker G.P.
1984: Irradiation of samples for
Ar dating using the
Geological Survey TRIGA reactor. U. S. Geol. Surv. Prof. Pa-
pers 1176, 155.
Dimitrescu R. 1995: Contributii la corelarea unitãþilor de fundamen-
tale Munþilor Apuseni ºi Carpaþilor Meridionali cu cele din
depresiunea pannonicã ºi de peste dunãre. St. Cerc. Geologie
Frank W. 1987: Evolution of the Austroalpine elements in the Cre-
taceous. In: Flügel H.W. & Faupl P. (Eds.): Geodynamics of
the Eastern Alps. Deuticke, Wien, 379406.
Fülöp J. 1994: Geology of Hungary. Palaeozoic II. Akad. Kiadó,
Budapest, 1445 (in Hungarian).
Géczy B. 1973: The origin of Jurassic faunal provinces and the
Mediterranean plate tectonics. Ann. Univ. Sci. Budapest, R.
Eötvös Nom. Sect. Geol. 16, 99114.
Haas J., Kovács S., Krystyn L. & Lein R. 1995: Significance of Late
Permian-Triassic facies zones in terrane reconstructions in the
Alpine-North Pannonian domain. Tectonophysics 242, 1940.
Haas J. (Ed.) 2001: Geology of Hungary. Eötvös University Press,
Habler G. & Thöni M. 2000: Preservation of Permo-Triassic low-
pressure assemblages in the Cretaceous high-pressure meta-
morphic Saualpe crystalline basement (Eastern Alps, Austria).
J. Metamorph. Geol. 19, 679697.
Hoinkes G., Koller F., Höck V., Neubauer F., Rantitsch G. &
Schuster R. 1999: Alpine metamorphism of the Eastern Alps.
Schweiz. Mineral. Petrogr. Mitt. 79, 155181.
Horváth P. & Árkai P. 2002: Pressure-temperature path of
metapelites from the Algyõ-Ferencszállás area, SE Hungary:
thermobarometric constraints from coexisting mineral assem-
blages and garnet zoning. Acta Geol. Hung. 45, 1, 127.
Jámbor Á. 1998: Stratigraphy of the sedimentary Carboniferous for-
mations of the Tisza Unit. In: Bérczi I.& Jámbor Á. (Eds.):
Stratigraphy of Hungarian Geological Formations. MOL-
MÁFI, Budapest, 173185 (in Hungarian).
Klötzli U.S., Buda G. & Skiold T. (in print): The starting point for
the Mesozoic odyssey of the Mecsek Mountains granitoids
(Mórágy Unit, Tisia Terrane, Southern Hungary): Constraints
for zircon typology, U/Pb geochronology and whole rock Sr
Nd isotope systematics. Chem. Geol.
Kovács S., Haas J., Császár G., Szederkényi T., Buda Gy. & Nagy-
marosy A. 2000: Tectonostratigraphic terranes in the pre-Neo-
gene basement of the Hungarian part of the Pannonian area.
Acta Geol. Hung. 43, 3, 225328.
Kretz R. 1983: Symbols for rock-forming minerals. Amer. Mineral.
Krohe A. 1987: Kinematics of Cretaceous nappe tectonics in the
Austroalpine basement of the Koralpe region (Estern Austria).
Tectonophysics 136, 171196.
Lelkes-Felvári Gy., Mazzoli C. & Visoná D. 1989: Contrasting min-
eral assemblages in polymetamorphic rocks from South Trans-
danubia (Hungary). Eur. J. Mineral. 1, 143146.
Lelkes-Felvári Gy., Árkai P. & Sassi F.P. 1996: Main features of the
regional metamorphic events in Hungary: a review. Geol. Car-
pathica 47, 4, 257270.
Lelkes-Felvári Gy., Frank W. & Schuster R. 2001: Basement evolu-
tion of the Great Hungarian Plain: Variscan, Permo-Triassic
and Alpine metamorphism. In: Ádám A., Szarka L. & Szendrõi
J. (Eds.): Pancardi 2001, II. Abstracts PP8, Sopron.
Lelkes-Felvári Gy., Frank W. & Schuster R. 2002: Basement evolu-
tion of the Great Hungarian Plain: Variscan, Permo-Triassic
and Alpine metamorphism. Földt. Közl. 132, 1, 125127.
Majoros Gy. 1998: Permian sequences in the basement of the Great
Plain and Tokaj Mts. In: Bérczi I. & Jámbor Á. (Eds.): Stratig-
raphy Hung. Geol. Formations. MOL, MÁFI, Budapest, 217
224 (in Hungarian).
Neubauer F. (Ed.) 1992: ALCAPA, Geological evolution of the in-
ternal Eastern Alps and Carpathians and of the Pannonian Ba-
sin. The Eastern Central Alps of Austria. ALCAPA Field Guide,
Pap S. 1990: Overthrust sequences in the middle part of the territory
east of the Tisza. Hung. Geol. Inst. Spec. Publ. 136 (in Hun-
garian, with English abstract).
Plaienka D., Janák M., Lupták B., Milovský R. & Frey M. 1999:
Kinematics and metamorphism of a Cretaceous core complex,
the Veporic Unit of the western Carpathians. Phys. Chem.
Earth 24, 651658.
Samson S.D. & Alexander E.C. 1987: Calibration of the interlabora-
Ar dating standard, Mmhb-1. Chem. Geol. 66, 2734.
Schuster R., Scharbert S., Abart R. & Frank W. 2001: Permo-Trias-
sic extension and related HT/LP metamorphism in the Aus-
troalpine-Southalpine realm. Mitt. Gesell. Geol. Bergbaustud.
Österr. 45, 111141.
Soroiu M., Popescu G.H., Kasper U. & Dimitrescu R. 1969: Contri-
butions preliminaires à la geochronologie des massifs cristal-
lins des Monts Apuseni. Analele Stiintifice Univ. Al. I. Cuza,
Iasi, Geol., XV, 2533.
Stampfli G.M. & Mosar J. 1999: The making and becoming of
Apulia. Mem. Sci. Geol. 51, 1, 141154.
Szederkényi T. 1984: Crystalline basement of the Great Hungarian
Plain and its geological connections. D.Sc. Thesis, Budapest
Szederkényi T. 1996: Metamorphic formations and their correlation
in the Hungarian part of the Tisia megaunit (Tisia megaunit
terrane). Acta Min. Petr. Szeged 37, 143160.
Szepesházy K. 1978: Correlations of the metamorphic formations of
the Great Hungarian Plain and the Apuseni Mts. Magy. Áll.
Földt. Int. Évi Jel. 1978, 173184 (in Hungarian).
Tari G., Dövényi P., Dunkl I., Horváth F., Lenkey L., Stefanescu
PERMIAN-TRIASSIC EVOLUTION OF THE GREAT HUNGARIAN PLAIN 315
M., Szafián P. & Tóth T. 1999: Lithospheric structure of the
Pannonian basin derived from seismic, gravity and geothermal
data. In: Durand B., Jolivet L., Horváth F. & Séranne M. (Eds.):
The mediterranean basins: Tertiary extensions within the Alpine
orogen. Geol. Soc. London Spec. Publ. 156, 215250.
Thöni M. 1999: A review of geochronological data from the Eastern
Alps. Schweiz. Min. Petr. Mitt. 79, 209230.
Thöni M. & Jagoutz E. 1992: Some new aspects of dating eclogites
in orogenic belts: Sm-Nd, Rb-Sr and Pb-Pb isotopic results
from the Austroalpine Saualpe and Koralpe type locality (Car-
inthia/Styria, SE Austria). Geochim. Cosmochim. Acta 56,
Thöni M. & Miller Ch. (1996): Garnet Sm-Nd data from the Saualpe
and the Koralpe (Estern Alps, Austria): chronological and P-T
constraints on the thermal and tectonic history. J. Metamorph.
Geology 14, 453466.
Tóth M.T. 1995: Retrograded eclogite in the crystalline basement
of Tisza unit, Hungary. Acta Mineral. Petr. Szeged XXXVI,
Tóth M.T. 1997: Retrograded eclogite from the Kõrös complex
(Eastern Hungary): records of a two-phase metamorphic evolu-
tion in the Tisia composite terrane. Acta Mineral. Petr. Szeged
Tóth M.T., Schubert F. & Zachar J. 2000: Neogene exhumation of
the Variscan Szeghalom dome, Pannonian Basin, Hungary.
Geol. J. 35, 265284.
Török K. 1990: New data on the geothermometry and geobarometry
of the Somogy-Dráva basin, SW Transdanubia, Hungary. Acta
Mineral. Petr. Szeged XXXI, 1323.
Weissenbach N. 1975: Gesteinsinhalt und Seriengliederung des
Hochkristallins in der Saualpe. Clausth. Geol. Abh., Sdb. 1,