Acta Geologica Hungarica, Vol. 45/4, pp. 359–371 (2002)
Paleogene igneous activity along the easternmost
segment of the Periadriatic-Balaton Lineament
Kálmán Benedek
Department of Petrology and Geochemistry, Eötvös University,
Lithosphere Fluid Research Laboratory, Budapest
In the Pannonian Basin three Paleogene igneous regions can be outlined, namely the Zala Basin
Shear Zone, the Velence Mts and the Recsk Region. These igneous regions are aligned along the
easternmost Periadriatic-Balaton Lineament System.
The igneous bodies are built up mostly by effusive rocks (andesite, dacite and basaltic andesite);
however, intrusive rocks (tonalite, diorite) have been identified as well. The radiometric age of the
effusive and intrusive rocks is scattered around 30 Ma, which falls into the range of the igneous
bodies aligned along the Periadriatic Line (Bergell, Adamello, Riesenferner, Karawanke, etc.).
Nevertheless, an Eocene onset of the magmatic activity in the Pannonian Basin is accepted on the
basis of biostratigraphic data.
As major and trace element composition range of the Paleogene igneous suites in the Pannonian
Basin are basically the same, they are thought to have undergone the same pre-crystallization history.
Geochemical characteristics of these calc-alkaline igneous rocks suggest that the magmatic activity
represents a post-syncollisional volcanic arc environment.
Key words: Paleogene, igneous rocks, Pannonian Basin, geochemistry, age, Periadriatic-Balaton
Magmatic Belt
Introduction
The Periadriatic Line (PL), one of the most spectacular geologic formations in
the Alps, developed as a result of dextral transpression (Schmid et al. 1989). As a
consequence of the Cretaceous closure of the Tethys, oceanic lithosphere was
subducted southward beneath the African microplate (Schmid et al. 1996). The
age of the magmatic activity along the PL is scattered around 30 Ma (von
Blanckenburg and Davies 1995), which postdates collision between Europe and
Africa (Schmid et al. 1996). Therefore, these igneous rocks are post-syncollisional
and not related to active subduction (Kagami et al. 1991; Schmid et al. 1996; Pamic
and Palinkaš 2000). The Periadriatic-Balaton Magmatic Belt (PBMB) is built up
mostly by intrusive bodies (Bergell, Adamello, Riesenferner, Karawanke, etc.);
however, either dykes (lamprophyre, shoshonite and andesite) in the Alps
(Deutsch 1984; Venturelli et al. 1984) or eroded pebbles of effusive rocks (mostly
andesite and dacite) in the Perialpine molasses (Frisch et al. 1998; Benedek et al.
2001) are present.
Address:
Received:
K. Benedek: H-1117 Budapest, Pázmány Péter sétány 1/c., Hungary
e-mail: [email protected]
2 April, 2002
0236–5278/2002/$ 5.00 © 2002 Akadémiai Kiadó, Budapest
360
K. Benedek
The pre-Neogene basement of the Pannonian Basin is built up by two
megatectonic units: the ALCAPA Terrane in the north and the Tisia Terrane in the
south (Csontos 1995; Kovács et al. 2000). The ALCAPA Terrane includes the
Bakonyia Terrane, whose southern boundary is outlined by the Balaton
Lineament, which is accepted to be the eastern continuation of the PL (Kázmér
and Kovács 1985; Fodor et al. 1998; Haas et al. 2000). The Bakonyia Terrane was
displaced horizontally eastward in the early Miocene (Majoros 1980; Tari et al.
1993; Fodor et al. 1998; Frisch et al. 1998) as a consequence of continental
convergence between the Adriatic microplate (Africa) and stable Europe. Thus,
the position of the Bakonyia Terrane at 30 Ma was somewhere between the
Eastern and Southern Alps (Kázmér and Kovács 1985; Frisch et al. 1998, Fig. 2b).
Along the extensively deformed zone of the easternmost Periadriatic-Balaton
Lineament System (PBLS) three Paleogene igneous regions can be outlined in the
Pannonian Basin from SW to NE (Csillag et al. 1980; Zelenka et al. 1983): the Zala
Basin Shear Zone (ZBSZ), the Velence Mts and the Recsk Region (Fig. 1).
The aim of the present paper is to give an overview of the easternmost
segment of the PBMB, focusing only on the lava rocks. Note that explosive rocks
are also present in the Pannonian Basin (Fig. 1); however, they are beyond the
scope of the paper.
Geological background and petrography
Zala Basin Shear Zone (ZBSZ)
The Mesozoic basement, consisting mainly of Triassic and Cretaceous units,
and Eocene sequences in the ZBSZ are covered by thick Miocene sediments
(Kõrössy 1988). The Paleogene igneous series were divided into two subgroups
by Benedek (2002).
In the south (Pusztamagyaród–Nagybakónak Zone), intrusive rocks (tonalite
and minor diorite) have been identified in drilling cores (Fig. 1). The northern
boundary of the intrusive body is outlined by a characteristic dextral strike-slip
fault. The intrusive rocks show hypidiomorphic texture and consist of
plagioclase, amphibole, biotite, quartz, rutile, apatite, zircon, opaque minerals,
rare potassium feldspar and garnet. In the tonalite, rare mafic enclaves (max. size
of 20 cm in diameters) occur with texture identical to that of their host rock.
In contrast, the northern segment of the ZBSZ (Bak–Nova half-graben) is
mostly characterized by andesite, dacite and explosive igneous rocks (Fig. 1).
These rocks, showing porphyritic texture, contain plagioclase, amphibole, biotite,
quartz, clino- and orthopyroxene, opaque minerals, rutile, apatite, zircon and
garnet. Andesite and dacite contain abundant mafic inclusions of rounded or
irregular shape and chilled texture. Benedek (2002) suggested that a portion of
the andesite and dacite is dyke-like in appearance.
It was concluded by the author (Benedek 2002) that the ZBSZ did not function
uniformly in tectonic aspects during the Paleogene; thus, effusive and intrusive
Acta Geologica Hungarica 45, 2002
50km
N
Lak
A
N
la
E
a
eB
I
ton
MID
Mór
32.3 ± 1.0
32.0 ± 1.4
Ad-2, -3
Ság-2
44.2 ± 3.4
39.9 ± 4.1
35.4 ± 4.3-(50.5 ± 4.4)
V E L E N C E
M T S .
O N
Bfv-1
A T
30.7 ± 1 B A L
Á
Z A L A - B A S I N
S H E A R Z O N E
Sümeg
R
B
L
s
de
ar
i
Alps
in
D
Eastern
Carpa
E
L I N
Pannonian
Basin
Si-1, and -2
Bu-2, and -3
Úh-1
Bakony Mts.
29.1 ± 1.2-(37.8 ± 1.4)
31.2 ± 1.4-32.9 ± 1.3
36.8 ± 2.6; 42.5 ± 2.6
33.2 ± 1.8-38.7 ± 3.0
Csv-18
32.7 ± 4.7
34.8 ± 3.7
Tó-1
20°E
R E C S K
R E G I O N
37 ± 10
th
P E S T P L A I N
B U D A M T S .
32.2 ± 0.9 Kl-1
Budapest
34.3 ± 1.3
32.5 ± 0.5
Bö-1
Kálvária hill
36 ± 17
Ci-2
19°E
ia
n
s
Fig. 1
Locations of Paleogene magmatic rocks in the Pannonian Basin with a compilation of available geochronological data (Baksa, 1975;
Balogh, 1985; Nagymarosy et al. 1986; Darida-Tichy 1987; Horváth and Tari 1987; Dunkl and Nagymarosy 1992; Benedek 2002)
33.9±1.4
33.0±1.5
30.4±1.5
28.6±1.8
27.9±1.3
34.9±1.4
31.6±1.3
31.1±2.8
29.3±1.2
31.6±1.3
34.9±1.4
33.9±1.3
27.3±1.1
32.5±1.4
27.1±1.4
26.0±1.2
27.9±1.1
47°N
18°E
boreholes penetrating Paleogene effusive rocks
data from stratigraphic evidence
K/Ar, U/Pb data from massive
boreholes penetrating Paleogene intrusive rocks
magmatic rocks
transcurrent fault zone
FT data from massive magmatic rocks
FT, K/Ar, Ar/Ar data from tuff layers
cities
of Tertiary sediments
R E C S K main exposure areas of the Paleogene
Surface/subsurface outcrops of
igneous regions
volcanic rocks
17°E
H
A
G
N
U
N
A
I
R
A
D
Ó
N
R
E
N
I
L
48° N
Paleogene igneous activity along the easternmost segment of the Periadriatic-Balaton Lineament
361
Acta Geologica Hungarica 45, 2002
362
K. Benedek
suites were juxtaposed during the escape period of the Bakonyia Terrane. The
andesitic and dacitic series was placed by Frisch et al. (1998) to the southeast of
the hidden Tauern Window. The intrusive series was eastward relative to the
effusive zone at 30 Ma, very close to the location of the recent Karawanke
tonalite. The intrusive zone most likely represents a strike-slip duplex due to the
Miocene dextral displacement along the PBLS.
Velence Mts
The effusive material of the Velence Mts (Fig. 1) is partly buried by Neogene
clastic sediments. In rising to the surface, the magma intersected Lower Paleozoic
slates, Carboniferous granites and Permo-Triassic carbonate sediments (DaridaTichy 1987). In the central part of the volcanic area hydrothermally altered rocks
occur at the surface. In this area the original rocks, which could have been
pyroclastics and lavas, were affected by multiphase alteration (Molnár 1996).
Close to this volcanic center, a small dioritic subvolcanic body has been
penetrated (Pázmánd-2). Józsa (1983) described abundant andesitic dyke swarms
crosscutting the adjacent Carboniferous granite. The lava rocks include andesites
and basaltic andesites, but basalts, dacites and trachyandesites were also
described (Darida-Tichy 1987). The porphyiritic constituents are represented by
plagioclase, amphibole, biotite, clino- and orthopyroxene, quartz and, in some
samples, garnet. Mafic inclusions of chilled texture are hosted by a variety of
different effusive rocks (Józsa 1983).
Recsk region
During the Paleogene a calc-alkaline subvolcanic body and its dykes (Fig. 1)
were emplaced into Triassic carbonates (Baksa 1975) in the Recsk region. In the
central part of the area subvolcanic andesite (and diorite) has been identified. In
the porphyritic andesite plagioclase, amphibole, biotite, apatite, rutile, quartz and
opaque minerals are the main rock-forming minerals. The primary rocks
(andesite, diorite) were affected by different secondary alterations (for details see
Baksa 1975). The carbonate host rock was thermally altered by the subvolcanic
body.
Contemporaneously, an andesitic stratovolcano was built up on the surface.
The basement of the volcanic succession is Triassic limestone (Földessy 1975). The
volcano consists of lava and pyroclastic rocks. The lava is mainly porphyritic
andesite containing plagioclase, amphibole, biotite, quartz, opaque minerals,
garnet, zircon and apatite. The entire volcanic succession is crosscut by
subsequent andesitic dykes.
Acta Geologica Hungarica 45, 2002
Paleogene igneous activity along the easternmost segment of the Periadriatic-Balaton Lineament
363
The age of the Paleogene igneous rocks
Zala Basin Shear Zone
Eocene marl was deposited over the Mesozoic basement in the ZBSZ, the
upper part of which (Bartonian) was interfingered with volcanogenic sediments
(Kõrössy, 1988). The marl deposited between the NP (nannoplancton) 15/16 zone
boundary and NP18 (about 42–43 and 38Ma) and the oldest volcanoclastic layers
are known from the NP16 zone (about 42–43 Ma; Nagymarosy, pers. com.). Based
on this observation, the entire volcanic succession was accepted as Eocene
(Kõrössy 1988). However, new K/Ar data measured on mineral separates
(amphibole, biotite, plagioclase) from the intrusive and effusive rocks, are
scattered from 28.6±1.8 Ma to 33.9±1.4 Ma and from 26.0±1.2 Ma to 34.9±1.4 Ma,
respectively (Fig. 1, Benedek 2002). As Eocene sediments have not been identified
over the intrusive rocks in the southern part of the ZBSZ (Kõrössy 1988), the
radiometric ages are considered to be the formation ages. On the other hand, a
detailed petrographic study of effusive rocks in the northern part of the ZBSZ, an
XRD study and paleontological data of the interfingering Eocene marl deposits
suggest that simultaneous emplacement of the effusive and the sedimentary
rocks is doubtful. It is suggested that the andesite and dacite were emplaced as
dykes in the Eocene marl; thus, the effusive rocks can be considered to be of
Oligocene age as indicated by radiometric data. It is noteworthy that also Balogh
et al. (1983) reported an Oligocene K/Ar age 30.7±1 Ma) of a small tonalite body
on the NE of the Zala Basin shear zone along the Balaton Line (Balatonfenyves).
Velence Mts
The onset of the volcanic activity in the Velence Mts is emplaced in the Middle
Eocene by observing the interfingering oldest tuffaceous layers and the shallow
marine Middle Eocene sediments (Darida-Tichy 1987). However, the radiometric
age determination of the massive andesite and subvolcanic diorite yielded
29.1±1.2 Ma and 31.2±1.4 Ma, respectively (Balogh 1985), which suggests the
presence of Oligocene igneous rocks, too (Fig. 1).
Recsk region
Unfortunately, few detailed radiometric age data of the subvolcanic body and
the stratovolcano of the Recsk region have been published. The subvolcanic body
of Recsk is considered to be Priabonian, because its basement and cover fall into
the Nummulites fabianii zone. Up to the present only one radiometric age (37±10
Ma) of the subvolcanic andesite has been published (Baksa 1975, Fig. 1).
Similarly to the subvolcanic body, the age of the andesitic stratovolcano of
Recsk has been accepted to be Priabonian on the basis that the volcanic material
of the stratovolcano intercalates with marine sediments which contain
Acta Geologica Hungarica 45, 2002
364
K. Benedek
Nummulites fabianii (Földessy 1975). Also the basement and the cover of the
stratovolcano contain of Nummulites fabianii. However, it is important to note that
some pyroclastic layers are thought to be Oligocene in age (Földessy 1975).
Geochemistry
Whole rock geochemistry
The compilation of available major and trace element data (Downes et al. 1995;
Benedek, 2002) suggests that there is no significant difference in the geochemical
range of the igneous suites from the ZBSZ, Velence Mts. and the Recsk region
(Figs 2, 3). This implies that these samples underwent a similar pre-crystallization
evolution. The K2O–SiO2 and the AFM (not shown) diagram of the igneous rocks
show that the analyzed samples fall in the field of high-K to medium-K calcalkaline series. The studied samples range from basaltic andesite through
andesite to dacite; thus, truly primitive, basaltic and highly evolved rhyolitic
magmas have not been found. Values of TiO2, Al2O3, Fe2O3 and MgO decrease
with increasing SiO2, whereas Na2O increases (not shown). These general trends
of calc-alkaline magmas are thought to be consistent with fractionation of main
rock-forming minerals (plagioclase, olivine, clinopyroxene, amphibole, Downes
16
K2O+Na2O wt%
14
Phonolite
12
Tephriphonolite
10
8
Ttrachydacite
Phonotephrite
Foidite
Tephrite
Basanite
6
Rhyolite
Trachyandesite
Basaltic
trachyandesite
Trachybasalt
4
Dacite
Basalt
Andesite
Picrobasalt
2
40
45
Basaltic
andesite
50
55
SiO2 wt%
60
65
70
75
Fig. 2
Na2O+K2O (wt%)-SiO2
(wt%) diagram of the
Paleogene
magmatic
rocks in the Pannonian
Basin. Analytical data
were taken from Downes
et al. (1995) and Benedek
(2002). Legend: X –
intrusive rocks from the
Zala Basin shear zone, O
– effusive rocks from the
Zala Basin shear zone, n –
Recsk region (andesite), p
– Velence Mts (andesite)
et al. 1995). Alternatively, magma mixing process can also be responsible for
similar trends (Gill 1981).
Trace element values of Ni, Cr in the samples studied are low (Ni=4–128 ppm,
Cr=10–155 ppm) and do not correlate with SiO2. The highest concentrations of
Acta Geologica Hungarica 45, 2002
Paleogene igneous activity along the easternmost segment of the Periadriatic-Balaton Lineament
100
Sample/MORB
Fig. 3
MORB-normalized
(Sun and McDonough
1989) trace element
pattern of the Paleogene magmatic rocks
in the Pannonian
Basin. Analytical data
were
taken
from
Downes et al. (1995)
and Benedek (2002).
Legend: dashed lineintrusive rocks from
the Zala Basin shear
zone,
solid
lineeffusive rocks from the
Zala Basin shear zone,
n – Recsk region, p –
Velence Mts
365
10.0
1.00
0.10
0.01
Sr K Rb Ba Th NbCe P Zr Sm Ti Y Yb Sc Cr Ni
Ni and Cr were found in a pyroxene-amphibole andesite from the Velence Mts,
and diorites from the ZBSZ. Th, Rb and Sr (LILE) behave incompatibly
throughout the entire magmatic suite in the MORB-normalized trace element
diagram (Fig. 3). All samples are depleted in Nb relative to Ce and Th which is a
characteristic feature of subduction-related magmatic rocks (Downes et al. 1995).
The Lan/Ybn ratio is 4–23 in intrusive and 5–25 in effusive rocks; the Ce/Yb ratio
is 13–55 in intrusive and 13–65 in effusive rocks. These ratios are within the
characteristic range of melting in a garnet-bearing source region (Patino et al.
2000).
Benedek (2002) compared the composition of intrusive rocks (tonalite, diorite)
from the ZBSZ to that of some Periadriatic plutons. Close geochemical similarity
of the Karawanke (~30 Ma; Scharbert 1975) and the intrusive rocks from the
ZBSZ has been successfully demonstrated. It is noteworthy that Karawanke
tonalite is similar in composition to other Paleogene tonalite bodies along the PL,
such as Bergell, Adamello, and Riesenferner. However, the Pohorje tonalite
(Pamic and Palinkaš 2000) is enriched in LILE, La, and Ce relative to those of
other Periadriatic intrusives, suggesting a slightly different evolution. Furthermore, the age of this intrusive body is early Miocene (Deleon 1969; Márton et al.
2002). The close analogy of the age data and geochemistry of the Periadriatic
intrusives including Karawanke (Scharbert 1975; Blanckenburg and Davies 1995),
and the intrusive rocks from the ZBSZ supports a genetic relationship between
these bodies.
Acta Geologica Hungarica 45, 2002
366
K. Benedek
Clinopyroxene as an indicator of tectonic environment
Clinopyroxene is one of the first crystallizing phases in igneous environments
and its composition can reflect initial composition of coexisting melt. The low
(0.0301–0.0512) Al2O3/SiO2 ratio of clinopyroxenes studied in andesite from the
ZBSZ and the Velence Mts. (Downes et al. 1995; Benedek 2002) reflects tholeiitic
or calc-alkaline primary magma (LeBas 1962). Leterrier et al. (1982) constructed a
series of discriminant diagrams in order to distinguish magmatic host rocks based
on the composition of clinopyroxenes. These diagrams confirm that the samples
have been originated from an orogenic calc-alkaline suite (Fig. 4). Using discriminant functions of Nisbet and Pearce (1977), clinopyroxene composition data
fall within the field of volcanic arc basalts and oceanic floor basalts (Fig. 4),
though the oceanic floor basalt origin can be excluded based on the geological
background (Frisch et al. 1998).
The relationship of intrusive and effusive igneous rocks
In the ZBSZ the intrusive and effusive rocks have a similar radiometric age. As
their whole rock composition range is basically the same, a series of hydrous
mineral analyses (amphybole, biotite) has been carried out in order to compare
their crystallization history.
Amphiboles and biotites in the intrusive rocks are fresh, whereas in the
effusive rocks they vary from unaltered to corroded, remelted or opaquemineral-rimmed even in the same thin section. Amphibole phenocrysts are
magnesium-hornblende in the intrusive samples, whereas in effusive rocks they
are tschermakite based on the classification of Leake et al. (1997).
The log (XF/XCl) vs. XMg diagram (Fig. 5; Munoz and Swenson 1981; Munoz
1984; Morrison 1991) for hydrous minerals is a very informative tool to compare
halogen composition of a variety of different igneous rocks. The diagram shows
that amphiboles and biotites have a higher XF/XCl ratio in effusive rocks than in
intrusive rocks. Some of the effusive amphiboles and biotites developed a thin,
Fe-Ti-oxide-rich, corroded or remelted rim (Benedek and Szabó 2000), which
indicates that they were outside of their stability field and re-equilibrated when
the magma was ascending to the surface. Rutherford and Hill (1993) described a
similar reaction rim around amphibole from the Mount St. Helens (USA) in dacite
and explained the texture as a consequence of decreasing H2O in the coexisting
melt (degassing) while rising to the surface. Therefore, it is most likely that the
amphibole and biotite in effusive rocks from the ZBSZ were incapable of being in
equilibrium with coexisting melts. As fluorine is generally partitioned into the
melt phase and chlorine into the separated fluid phase during degassing of
magma (Dingwell et al. 1985; Webster and Holloway 1990; Caroll and Webster
1994), it is expected to see increasing fluorine and decreasing chlorine content in
the melt phase. This process provides a reasonable explanation for higher
Acta Geologica Hungarica 45, 2002
Paleogene igneous activity along the easternmost segment of the Periadriatic-Balaton Lineament
0.18
Ti
A
0.09
Alkaline basalt
Tholeiitic or
calc-alkaline basalt
0
0.5
0.05
0.8
Ca+Na
1.1
B
Non-orogenic basalt
0.25
0
Orogenic
basalt
0
0.75
Ca
-1.2
-1.1
-1
1
-0.9
C
-0.8
VAB
WPA
F2
Ti+Cr
Fig. 4
Discrimination diagrams of
clinopyroxenes studied in
andesite from the Zala Basin
shear zone and the Velence
Mts. (Downes et al. 1995;
Benedek 2002). (A-B) The
host magma of the clinopyroxenes
studied
is
tholeiitic or calc-alkaline in
character and the magmatism took place in an
orogenic
environment
(Leterrier et al. 1982). The
elements are calculated as
cationic values. (C) The
composition of the clinopyroxenes studied fall within
the field of volcanic arc
basalt and oceanic floor
basalt. Discriminant functions (F1, F2) were calculated
after Nisbet and Pearce
(1977). Abbreviations: volcanic arc basalt (VAB), oceanfloor basalt (OFB), withinplate tholeiitic basalt (WPT),
within plate alkalic basalt
(WPA). Legend: O – effusive
rocks from the Zala Basin
shear zone, p – Velence Mts
367
OFB
-0.7
-2.4
VAB
OFB -2.5
-2.6
WPT
F1
fluorine and lower chlorine content in amphiboles and biotites from the effusive
rocks compared to those in intrusive rocks.
As the intrusive bodies were crystallized completely a deep magma chamber
(about 7–15 km using Al-in hornblende geobarometers; Benedek and Szabó 2000,
using methods of Hammarstrom and Zen 1986; Hollister 1987; Johnson and
Rutherford 1988; Schmidt 1992); therefore, significant volatile loss could not
occur during their evolution. On the other hand, the fluid composition in the
melts of the effusives could undergo partitioning on the way to the surface,
slowly becoming fluorine rich. These phenomena can be explained in that
effusive volcanism took place on an extensively faulted and fractured lithosphere
relative to the intrusive magmatism.
Acta Geologica Hungarica 45, 2002
368
K. Benedek
1.8
Amphibole
Conclusions
log (XF/XCl)
log (XF/XCl)
Paleogene igneous occurrences in
the Pannonian Basin are aligned
along the SW–NE trending Peri0.6
adriatic-Balaton Lineament System.
Based on the published data, the
0
following conclusions can be
0.5
0.6
drawn:
X Mg
1. Paleogene igneous rocks in the
2
Pannonian Basin are represented
Biotite
by effusive (basaltic andesite,
1.5
andesite, dacite, trachyandesites)
1
and intrusive (tonalite, diorite)
rocks.
0.5
2. The radiometric age of the
0
igneous rocks dated is mostly
Oligocene (around 30 Ma), though
-0.5
0.3 0.4 0.5 0.6
stratigraphic data suggest Eocene
X Mg
onset of the Paleogene magmatic
activity, too.
Fig. 5
3. The chemical composition
Log (XF/XCl) vs. XMg plot of amphibole and biotite
range
of the igneous rocks from the
compositions from the intrusive and effusive rocks
studied volcanic regions is similar
in the Zala Basin shear zone (Benedek 2002). Cl, F
and it is analogous to other igneous
and Mg are given in mole fraction. Legend: Xintrusive rocks from the Zala Basin shear zone, Orocks aligned along the Periadriatic
effusive rocks from the Zala Basin shear zone
Lineament in the Alps.
4. The presence of intrusive and
effusive rocks indicates that magmatic activity was taking place under differing
tectonic environments.
5. Based on radiometric age and geochemical data, Hungarian Paleogene
igneous rocks are suggested to be the easternmost prolongation of the
Periadriatic-Balaton Magmatic Belt.
1.2
Acknowledgements
Csaba Szabó (ELTE) is thanked for comments and the helpful review of the
manuscript. József Jósvai and Csaba Bokor (Hungarian Oil Company, MOL Rt.)
are gratefully acknowledged for useful comments and for permission to publish
this work. The author is also grateful to L. Fodor (MÁFI), A. Nagymarosy (ELTE),
I. Dunkl (University of Tübingen) and Zs. Nagy (University of Missouri-Rolla) for
helpful comments. The author also thanks T. Zelenka (Hungarian Geological
Survey) and J. Pamic (Croatian Academy of Sciences) for their helpful reviews.
Acta Geologica Hungarica 45, 2002
Paleogene igneous activity along the easternmost segment of the Periadriatic-Balaton Lineament
369
This is the No 7 publication of the Lithosphere Fluid Research Lab of the
Department of Petrology and Geochemistry at Eötvös University, Budapest.
References
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