GeolCarp_Vol52_No2_79

GEOLOGICA CARPATHICA, 52, 2, BRATISLAVA, APRIL 2001

79—90

WHOLE-ROCK CHEMISTRY AND GENETIC TYPOLOGY

OF THE WEST-CARPATHIAN VARISCAN GRANITES

IGOR BROSKA and PAVEL UHER

Geological Institute, Slovak Academy of Sciences, Dúbravská cesta 9, 842 26 Bratislava, Slovak Republic

(Manuscript received June 9, 2000; accepted in revised form March 15, 2001)

Abstract: The geochemistry of 166 new whole-rock analyses from West-Carpathian Variscan granitic rocks are pre-
sented on the basis of their division into four principal groups: S-, I-, A- and specialized S-type (S

). The contribution

shows some discrimination diagrams which are useful for the recognition of these principal granite groups and also give
a possible outline of the geodynamic scenario of their origin. All studied groups belong to mainly crustal aluminic (S

S-type) and aluminocafemic (I-, A-, partly S-type) associations, mantle-derived cafemic dioritic rocks are rare. Gener-
ally, the S- and I-type groups show predominantly Na

O/K

O ratio > 1, whereas A- and S

-type granites usually exhibit

O/K

O < 1. I-types are more Si-poor and Fe, P-rich than other groups, however, a part of the S

-type group belongs

to the P-rich evolved granites (>0.2 wt. % P

) and the A-types are generally very poor in P. The Zr vs. SiO

diagram

clearly discriminates Zr and Si-rich hypersolvus A-type from other groups, similarly the A-types show the highest Zr/Hf-
ratio and Y contents (>20 ppm). Ba-Sr and Sr-Rb diagrams successfully divide plagioclase-rich I-type from S-, A-type
and especially from K,Na-feldspar-rich S

-type. The newly modified Rb-Ba-Sr diagram reliably discriminates the groups:

poorly (I, S), mildly (S, A, rarely I) and strongly evolved granites (S

, rarely S and A) were recognized. REE rock/

chondrite normalized diagram discriminate all groups: REE-rich I-type without Eu-anomaly, from REE-rich A-type with
negative Eu-anomaly and REE-poor S- and especially S

-type with pronounced negative Eu-anomaly. In this sense of the

geotectonic position, the S- and I-type can be considered as orogenic granites, in contrast, the A-type and S

-type

granites are post-orogenic members.

Key words: Western Carpathians, geochemistry, granitic rocks, S-, I-, A-, S

- types.

Introduction

New analytical data, for the most part unpublished have been
gathered in chemical laboratories at Ottawa University, Cana-
da and in Memorial St. John’s University, Canada. These data
permit a new study of the chemical variability of granitic rocks
in the Western Carpathians. A subset of the samples which
were analysed and published previously (mainly “ZK” series,
Cambel & Walzel 1982; “BP” series, Uher et al. 1994) were
re-analysed. Consequently, this set is the first complete large
database of major and trace elements of all principal genetic
types of West Carpathian Variscan granitic rocks.

Geochemical studies of the West-Carpathian granites until

now, usually did not take into account variations between the
genetic groups of the granites but they were based mainly on
the  investigation  of  granitic  groups  according  to  the  IUGS
classification  and  composition  variations  between  granites,
granodiorites  and  tonalites.  The  West-Carpathian  Variscan
granitic rocks were considered as genetically more-or-less co-
herent  group  which  shows  primary  differentiation  caused
mainly  by  fractional  crystallization.  Tonalite,  granodiorite  to
granite  sequences  were  regarded  as  common  differentiation
trend characterized by the decreasing of compatible elements,
such as P, Zr, Hf, Cr, Ni, Co, V, and by the increasing of in-
compatible  elements,  such  as  Rb,  Sn    (e.g.  Cambel  &  Vili-
novičová  1981;  Cambel  &  Vilinovič  1987;  Jacko  &  Petrík
1987; Hovorka & Petrík 1992; Kohút & Janák 1994). Occa-
sionally, besides the crystal fractionation, wall-rock assimila-
tion has been emphasized (Jacko & Petrík 1987). In the past,

the  granite  rock-forming  minerals  (feldspars,  micas)  were
studied  in  detail  (e.g.  Macek  et  al.  1979,  1982;  Petrík  1980,
1982b; Vilinovičová 1989). Later geochemical granite subdi-
vision  into  I-  and  S-types  were  realized  (Klomínský  et  al.
1981; Cambel & Petrík 1982; Cambel et al. 1985), the subdivi-
sion of the Ve ká Fatra granites into two separate independent
groups on the basis of bulk rock compositions was proposed
(Kohút 1992).

Using the fundamental mineralogical criteria, especially ac-

cessory  mineral  assemblages,  zircon  typology  and  allanite-
monazite dichotomy, together with geochemical and isotopic
data led to a subdivision of the West-Carpathian granites, into
monazite-ilmenite  and  allanite-magnetite  group  (Broska  &
Uher  1991;  Broska  &  Gregor  1992;  Petrík  &  Broska  1994).
Later,  the  identification  of  post-orogenic  A-type  granites
mainly  on  the  basis  of  zircon  typology  and  trace-element
chemistry (Uher & Gregor 1992; Uher & Broska 1996) shed a
new light on the understanding of granite development in the
Western Carpathians. It resulted to the division of the West-
Carpathian  granites  into  S-,  I-,  A-type  groups  (Petrík  et  al.
1994).

The aim of this paper is to characterize Variscan West-Car-

pathian granites on the basis of 166 new analyses in terms of
recently used genetic classification, based on S, I, A typology
(Chappell & White 1974; Whalen et al. 1987), except the De-
vonian metagranites (orthogneisses), which were not included
into the sample set. For this purpose, we subdivided studied
set of West-Carpathian granite analyses into the four geochem-
ical groups: (1) S-type granites, meso-Variscan (2) I-type,

80 BROSKA and UHER

meso- + late-Variscan, (3) A-type, post-Variscan and (4) post-
Variscan specialized rare-element S-type granites (S

-type).

Despite plotting of numerous discrimination diagrams of

granitic rocks, we present only the most distinctive ones in or-
der to demonstrate the chemical variability of the granite
groups. The contribution also illustrates an outline of the pos-
sible geotectonic scenario of the West-Carpathian Variscan
granites in sense of their time and spatial relationship.

Occurrences of the West-Carpathian

Variscan granitic rocks

Variscan magmatic activity is manifested by intrusions of

several granitoid plutons, separated tectonically in the princi-
pal  West-Carpathian  Alpine  superunits:  Tatric,  Veporic  and
Gemeric (Plašienka et al. 1997) Fig. 1. The granites often oc-
cur  as  sheet-like  bodies  (Kohút  &  Janák  1994)  or  laccoliths
(Lexa & Bezák 1996) and they are emplaced into metapelites
to metapsammites of amphibolite facies, locally contact ther-
mal metamorphism caused by granitoid intrusions occurs (e.g.
Krist et al. 1992).  The protolith of the granites was represent-
ed mostly by the metapelites, metagreywackes or older meta-
granites (Petrík 2000). The inhomogeneties in Sm/Nd system

are interpreted as the evidence of contamination and/or mag-
ma mixing (Kohút et al. 1996, 1999a) and a Proterozoic recy-
cling component in granite protoliths  is supposed (Kohút et
al. 1995, 1999a). At the present tectonic position, relatively
large granitic plutons crop out in the Tatric and Veporic Su-
perunits, in contrast to small and mostly hidden granitic bod-
ies  in  the  Gemeric  Superunit.  The  Velence  granites  in  the
Trans-Danubian Superunit (Hungary), occur to the N of the
Balaton  lineament  and  belong  to  the  Western  Carpathians
(cf. Plašienka et al. 1997). U-Pb and Rb-Sr isotope dating of
the  West-Carpathian  granitic  rocks  reveal  a  relatively  wide
time span of their origin, around 150 Ma (e.g. Cambel et al.
1990;  Petrík  &  Kohút  1997;  Petrík  2000;  Uher  &  Broska
2000; Poller et al. 2000).

Typology of the West-Carpathian

Variscan granitic rocks

S-type granites

They represent peraluminous biotite and two-mica granites

to granodiorites locally accompanied by numerous pegmatites.
They are characterized by the dominance of monazite-(Ce)

Fig. 1. Schematized geological map of the distribution of Variscan West-Carpathian granites. Explanations: MK – Malé Karpaty Mts, T –
Tribeč Mts, PI – Považský Inovec Mts, SMM Suchý and Malá Magura Mts, MF – Malá Fatra Mts, VF – Ve ká Fatra Mts, NT – Nízke
Tatry Mts, VT – Vysoké Tatry Mts, V – Velence Mts (Hungary).

WHOLE-ROCK CHEMISTRY AND GENETIC TYPOLOGY OF VARISCAN GRANITES 81

over allanite-(Ce) or absence of allanite accompanied with xe-
notime-(Y).  The  allanite-monazite  dichotomy  or  antagonism
has  been  observed  in  the  West-Carpathian  granitic  rocks  for
over three decades (e.g. Hovorka & Hvož ara 1965; Chovan &
Határ 1978; Hvož ara 1979; etc.), and together with zircon ty-
pology, and presence of almandine and ilmenite, it became one
of  the  basic  criteria  for  the  genetic  subdivision  of  the  West-
Carpathian granites into the S- and I-type granite groups (Bros-
ka  &  Uher  1991;  Broska  &  Gregor  1992;  Petrík  &  Broska
1994).  Zircon  typology  of  the  S-type  granites  (mainly  S

1-2

6-7

, L

1-2

, G

subtypes) indicates low-temperature crustal alu-

minous character of the granites according to the Pupin (1980)
classification. Apatite locally show a dusky brown (smoky) co-
lour due to minute carbon-bearing inclusions, which indicates
low fO

conditions of crystallization (Broska et al. 1992).

These  features  are  typical  for  peraluminous  granitic  rocks
which represent the most abundant granite type in the Western
Carpathians. They have been  formed probably by biotite and/
or  muscovite  dehydration  melting  of  upper  crustal  quartzo-
feldspathic rocks, such as greywackes, due to crustal thicken-
ing  and  prograde  metamorphism  during  Carboniferous  colli-
sion  (Petrík  et  al.  1994).  In  accordance  with  isotopic  dating
(e.g.  Cambel  et  al.  1990;  Krá   et  al.  1997),  the  monazite-(il-
menite)-bearing  granites  formed  during  the  Meso-Variscan,
Lower Carboniferous period with the culmination of formation
at about 350 Ma.

I-type granites

I-type, allanite-bearing granites are metaluminous to slightly

peraluminous biotite (leuco)tonalites to granodiorites, rarely
biotite to muscovite-biotite granites, locally with pink K-feld-
spar phenocrysts. Except of allanite-(Ce), the typical primary
accessory mineral assemblage is represented by magnetite and
titanite. Zircon typology (mainly S

, S

subtypes) indicates a

medium-temperature  crustal  to  crustal-mantle  character.  The
U-Pb zircon and Rb-Sr wall-rock dating show a wide age span
of  I-type  group  granite  formation,  from  meso-Variscan,  Late
Devonian—Early  Carboniferous  (~370—340  Ma)  to  late-
Variscan, Late Carboniferous (~310—290 Ma) – Broska et al.
(1990), Bibikova et al. (1990), Cambel et al. (1990), Michalko
et al. (1998). On the basis of recent data, their origin is con-
nected with lower crustal continental melting with a contribu-
tion of infracrustal or mantle material (Petrík et al. 1994; Ko-
hút  et  al.  1999).  Locally  abundant  microgranular  mafic
enclaves  in  these  granites,  which  are  products  of  mixing  of
melts, as well as the bulk chemistry is evidence for such pro-
cesses (Broska & Petrík 1993).

A-type granites

The recognition of the zircon typology with dominant high-

temperature and high-alkaline P- and D- zircon subtypes in
granites was the first impulse for the determination of these
post-orogenic A-type granites (Uher & Gregor 1992; Uher et
al. 1994). They form small intrusions of biotite leucogranites
to granite porphyries with hypersolvus, transsolvus to subsol-
vus textures (Uher & Broska 1996). The accessory mineral as-

semblage includes allanite-(Ce), magnetite or ilmenite, rarely
monazite-(Ce) (Uher & Broska 1996). U-Pb isotopic geochro-
nology of zircon showed the Permian to Triassic age of the A-
type granites (Uher & Pushkarev 1994; Putiš et al. 2000).

Specialized S-type granites

Specialized tin-bearing biotite-muscovite to muscovite

leucogranites, and rare granite porphyries from the Gemeric
Superunit (the Spiš-Gemer type) are the most evolved S-type
granites in the Western Carpathians. Locally greisen and albi-
tite cupolas with disseminated rare element Li, Sn, Nb, Ta, W,
F mineralization occur (Malachovský 1992 in Grecula 1995).
Accessory minerals of the Spiš-Gemer granites comprise tour-
maline (schorl to foitite), almandine, topaz, zircon, apatite, lo-
cally also rare monazite-(Ce), cassiterite, wolframite and Nb-
Ta phases (e.g. Faryad & Dianiška 1993). Zircon of S

subtype predominate. The character of zircon typology is dis-
tinct and distinguished these granites from the rest of the
West-Carpathian granites (Jakabská & Rozložník 1989; Bros-
ka & Uher 1991). The granites show Permian Rb-Sr WR and
mineral ages and they are characterized by very high initial Sr
isotope ratios, I

above 0.720 (Kovách et al. 1986; Cambel et

al. 1990). The Permian age was also constrained by monazite
probe dating (Finger & Broska 1999) and single-grain isotopic
dating of zircon (Poller et al. 2000).

Analytical methods

All 166 analyzed samples were obtained from the crushed

homogenized rocks of 3—12 kg in weight. Major elements and
Rb, V, Cr, Co, Ni, Zn, Sr, Ba, Th and U of the rocks were de-
termined by XRF at Ottawa University (Canada), and REE, Y,
Nb,  Ta,  Zr  and  Hf  by  ICP-MS  in  Memorial  University  of
Newfoundland (Canada). The analytical procedure of ICP-MS
was as follows: (1) sintering of a 0.2 g sample aliquot with so-
dium  peroxide,  (2)  dissolution  of  the  sinter  cake,  separation
and  dissolution  of  REE  hydroxide-bearing  precipitate,  (3)
analysis by ICP-MS using the method of internal standardiza-
tion to correct for matrix and drift effects. Natural rocks and
pure quartz reagent (blank) were used as reference standards.
For detailed information on the ICP-MS method see Jenner et
al. (1990) and Longerich et al. (1990).

Results

Major element geochemistry

Representative chemical analyses of the major elements of

all four geochemical granite groups are presented in Table 1,
statistical parameters are shown in the Table 2. The complete
data used for the construction of diagrams are available as
Table 3 on request in the Editorial Office or from the au-
thors.

The chemical analogue of the modal IUGS classification

by Streckeisen & Le Maitre (1979) using the Mielke & Win-
kler mesonormative calculation (1979), shows the preva-

82 BROSKA and UHER

lence of tonalites and granodiorites in the I-type granite
group, the S-type type of granitic rocks are granites, grano-
diorites, rarely tonalites and the A- as well as the S

-type be-

long to feldspar granites and syeno- as well as monzo-granites
(Fig. 2).

Another rock classification diagram expressing the balance

between characteristic peraluminous minerals (e.g. micas, gar-
nets) and metaluminous Al-poor, Ca-rich minerals (e.g. horn-
blende, epidote, titanite) after Debon & Le Fort (1983) shows
the  distinct  peraluminous  character  of  practically  all  studied
West-Carpathian  rocks  except  part  of  the  subaluminous  and
metaluminous  I-type  tonalites  and  diorites.  The  diagram  re-
veals their dominantly crustal origin, with aluminic to alumi-
nocafemic associations (Fig. 3). Cafemic association (field IV)
is represented almost only by amphibole-biotite-bearing dior-
ites as well as microgranular mafic enclaves of tonalite-diorite
composition in I-type granites, which indicate their mantle ori-
gin (cf. Debon & Le Fort 1983). Amphibole-bearing tonalites
are very rare in this region, and the majority of granitic rocks
belong to biotite and two-mica types. S-type and specialized
S-type granites are plotted in field I (Ms>Bt), which is in ac-
cordance  with  the  petrographic  data.  Biotite-bearing  A-type
leucogranites  (~4—5  vol.  %  Bt)  and  especially  biotite-rich  I-
type granites (~5—10 vol. % Bt) lie in the Bt>Ms (II) and Bt
(III) fields (Fig. 3).

A Na

O/K

O vs. SiO

diagram is plotted in Fig. 4. The

prevalence of Na

O over K

O is dominant for the S- and I-type

granites as was described earlier (e.g. Hovorka & Petrík 1992),
on the contrary, the A-type and S

-type granites show the

prevalence of K

O. The I-type granitic group shows a regular

trend of decreasing Na

O/K

O vs. SiO

content, whereas the

S-types exhibit distinctly scattered Na

O/K

O values and the

A- and S

-type granites are almost invariably below the value

of 1 (Fig. 4). Locally, high albite content, especially in the S-
type, cause the shift of Na

O/K

O ratio over 3. Other litho-

phile elements, as Mg, Ti and Mn do not discriminate the
West-Carpathian granite types distinctly.

The iron content is slightly higher in the A-type granites

than in the I- and S-type granites, whereas the specialized S-
type granites show generally low iron (Fig. 5).

Decreasing of P

content during the differentiation pro-

cess, caused mainly by apatite fractionation, is well docu-
mented for the I- and A-type granites while P

vs. SiO

distribution in both S- and S

-type granites show large irreg-

ularities (Fig. 6). The P

content in S-type decreases with

SiO

only in early less fractionated members (<70 % SiO

whereas the more fractionated and peraluminous granites
(>70 % SiO

) reveal scattered to increased content of P

(Fig. 6). The A-type granites form a distinct group with the
lowermost P

and apatite contents in comparison to the I-

and S-type granites.

Trace element geochemistry

Although zirconium and hafnium systematically decrease

with increasing of SiO

, there are a significant differences in

the distribution of these elements for A-type granites in com-
parison to the other granite groups (Fig. 7). The Hf vs. Zr dia-
gram shows a high positive correlation (R = 0.98, Fig. 8), how-

Fig. 3. A-B multicationic diagram (Debon & Le Fort 1983) of the
Variscan West-Carpathian granitic rocks.

Fig.  2.  Mesonormative  Q’-ANOR  diagram  of  the  Variscan  West-
Carpathian  granitic  rocks.  Explanations:  aG  –  alkali-feldspar
granite;  sG – syenogranite; mG – monzogranite; Grnd – gra-
nodiorite; T– tonalite; D – diorite (without BMF-8).

Fig. 4. Na

O/K

O vs. SiO

plot of the Variscan West-Carpathian

granitic rocks documenting the discrimination of the A-type gran-
ites. Na

O/K

O ratio below 1 is characteristic for the post-orogenic

granites.

ever, the diagram reveals a different trend for the A-type in
comparison with the rest of granite groups due to the higher
Zr/Hf ratio.

WHOLE-ROCK CHEMISTRY AND GENETIC TYPOLOGY OF VARISCAN GRANITES 83

Binary Ba vs. Rb and Sr vs. Rb and the ternary Rb-Ba-Sr

diagram (modified after El Bouseily & Sokkary 1975) clear-
ly discriminate relatively poorly evolved I- and S-type group
from mildly to highly evolved S-, A- and especially S

-type

granite groups (Figs. 9—11).

Chondrite-normalized rare earth element data show distinct

differences among S-, I- and A-type granites. The average pat-
terns of the normalized values show the highest value of the
REE and especially HREE for the A-type group (Fig. 12). The
HREE enrichment of the A-type group is documented also by
high  yttrium  concentrations  –  more  than  20  ppm  (Fig.  13).
The  higher  contents  of  the  LREE  are  characteristic  of  the  I-
types in comparison with both S-types, nevertheless the HREE
average  content  is  almost  identical  for  both  granite  groups
(Fig. 12). The similar slope of the rock/chondrite normalized
plot indicate similar differentiation tendencies of the S- and I-
type granites: Ce

/Yb

is 11.4 and 16.7, respectively. On the

contrary, the S

- and A-type granite groups clearly reveal

HREE enrichment: Ce

/Yb

is 2.8 and 5.6, respectively. The

more  pronounced  Eu-negative  anomaly  is  typical  of  special-
ized  S-type  granites  (Eu/Eu*  =  0.2)  and  for  the  A-type  (Eu/
Eu*  =  0.4),  on  the  other  hand  it  is  only  0.6  for  the  S-type
group, and the I-type group has an insignificant Eu-anomaly
(Eu/Eu* = 0.8).

Discussion

Geochemistry

The results show differences between all four groups of

Variscan  West-Carpathian  granitic  rocks.  The  mesonorma-
tive Q’-ANOR diagram (Fig. 2) is generally concordant with
older  modal  and  mesonormative  diagrams  (Petrík  1982a),
however, studied differentiated I-type granites lie mainly in
granodiorite  and  monzogranite  fields,  whereas  common  to-
nalite  compositions  were  described  by  Petrík  (1982a).  The
multicationic A-B diagram (Debon & Le Fort 1983) reveals
generally  aluminous  crustal±alumino-cafemic  character  of
all granite groups, although with some tendency of I-type to
metaluminous mainly mantle domain which is typical of am-
phibole-bearing  dioritic  rocks  and  enclaves  (Fig.  2).  These
results are in accordance with mainly crustal character of S-,
A- and especially S

-type groups and with some mantle con-

tribution in the origin of the I-type group (Petrík et al. 1994;
Uher & Broska 1996; Petrík & Kohút 1997).

The exclusive character of the A-type group is documented

in Na

O/K

O vs. SiO

and FeO vs. SiO

plots (Figs. 4, 5)

which reflects presence of the K-feldspar and annite-rich bi-

Fig. 5. FeO

tot

vs. SiO

plot of the Variscan West-Carpathian granit-

ic rocks.

Fig. 6. P

vs. SiO

plot of the Variscan West-Carpathian granitic

rocks.

Fig. 7. Zr vs. SiO

plot of the Variscan West-Carpathian granitic

rocks.

Fig. 8. Hf vs. Zr plot of the Variscan West-Carpathian granitic
rocks.

84 BROSKA and UHER

dominate over Na

O is evident also for the S

-type group,

whereas, S- and especially I-type group are sodium-rich (Fig.
4). Consequently, the older meso- and late-Variscan granites
are mainly plagioclase-bearing rocks, whereas the post-
Variscan A- and S

-type exhibit K-feldspar dominance.

The very low P

contents in the A-type group (Tables 1—

3,  Fig.  6)  is  comparable  with  other  anorogenic  granites
world-wide (cf. Whalen et al. 1987), and it should be one of
the  typical  feature  of  A-type  granites,  reflected  in  low
amount of apatite in these Ca, P-poor rocks. Low P contents
in the A-type granites could be explained by formation from
melt-depleted lower crust after main granite production dur-
ing Variscan orogeny. The I-type group shows negative cor-
relation  between  P

vs. SiO

due to apatite preferential

precipitation in the early differentiation members. On the
contrary, scattered P

contents is the consequence of the

higher P

solubility with increasing A/CNK in late frac-

tionated members (Pichavant et al. 1992). Moreover, positive
correlation between P

and SiO

in more evolved mem-

bers of S- and especially S

-type groups (>70 wt. % SiO

) is

connected with incompatible behaviour of P in strongly pera-
luminous,  alkali-  and  fluid-rich  magmas  which  resulted  in
enrichment of P and its entry into alkali feldspar structure in
fractionated  alkali-rich  leucogranites  (e.g.  Pichavant  et  al.
1992;  London  1992,  1998;  Breiter  1998).  Such  a  trend  is
characteristic  especially  for  phosphorus-rich  rare-element
peraluminous  granites  of  the  Spiš-Gemer  type  (S

-group)

where K-feldspar contains up to 0.5 wt. % P

(Broska et

al. in prep.).

The content and behaviour of trace elements during differ-

entiation processes clearly characterize the differences be-
tween the S-, I- and A-type granitic rocks. Of special impor-
tance are the findings on the compatibility or incompatibility
of trace elements during differentiation. Some elements, such
as Sr, Sc, V, Zr, Cr and Co behave compatibly in all granite
types. Low Th and U content are not suitable for discrimina-
tion purposes as was formerly proposed by Yates et al.
(1982). On the contrary, Zr is a very useful element for gran-
ite discriminations. The Zr vs. SiO

diagram (Fig. 7) strongly

discriminates  some  of  the  A-type  group  from  each  other:
high and irregular distribution of Zr (Tables 1—3) is another
characteristic  feature  of  alkali  granites  (e.g.  Whalen  et  al.
1987). Very strong positive Hf vs. Zr correlation (Fig. 8) in-
dicates the close and exclusive relationship between zirconi-
um and hafnium in granitic magmas which resulted in crys-
tallization  of  zircon  as  an  essential  Zr,  Hf-bearing  phase  in
all studied groups of granitic rocks. Different Zr/Hf ratio in
hypersolvus A-type group in comparison to the other granites
is probably related to contrasting solubility of Zr and Hf in
(per)alkaline Al-poor F-rich A-type magmas in comparison
to peraluminous H

O-rich S- and I-type granites. This is also

reflected in higher Zr/Hf ratios in zircon from post-orogenic
and anorogenic granite suites (Pupin 1992) and is also docu-
mented for zircon of West Carpathian A-type group (Uher &
Broska 1996).

The geochemical separation among granite types is strong-

ly apparent in the distribution of Rb, Sr and Ba, which are
concentrated mainly in the feldspars and micas. The highest
contents of Rb show specialized S- and A-type groups due to

Fig. 10. Sr vs. Rb plot of the Variscan West-Carpathian granitic
rocks.

Fig. 11. Rb-Ba-Sr ternary discrimination diagram of the Variscan
West-Carpathian granitic rocks. Explanations: 1 – poorly evolved
granites, 2 – mildly evolved granites, 3 – highly evolved granites.

Fig. 9. Ba vs. Rb plot of the Variscan West-Carpathian granitic
rocks. Note: The Turčok type represents anomalous A-type granite
with low Rb content (Gemeric Superunit).

otite in the granite group (Uher & Broska 1996). These
geochemical features are generally prominent in A-type
granites (Whalen et al. 1987). The tendency of K

O to pre-

WHOLE-ROCK CHEMISTRY AND GENETIC TYPOLOGY OF VARISCAN GRANITES 85

their  higher  level  of  fractionaction  and  K-feldspar  enrich-
ment. On the contrary, less evolved, plagioclase-rich I- and
S-type granites exhibit the highest Ba and Sr but the lowest
Rb  contents  (Tables  1—3,  Figs.  9—11).  A  general  Rb-Sr-Ba
differentiated trend toward the specialized granites described
by El Bouseily & Sokkary (1975) is evident also in the West-
Carpathian granitic suites (Fig. 11). However, in our opinion,
fields such as “anomalous or normal granites, granodiorites
etc.” in the diagram of El Bouseily & Sokkary (1975) do not
discriminate the natural granite types properly and they are
inadequatly  defined,  in  addition  some  of  the  West-Car-
pathian granites s.s. plot in the granodiorite field or vice ver-
sa. Therefore, we propose new categories for this ternary Rb-
Ba-Sr  diagram  according  to  their  degree  of  differentiation:
poorly-evolved,  mildly-evolved,  to  highly  evolved  granites
(Fig. 11). Such modification of the diagram allow us to use
Rb, Sr and Ba as the important discrimination parameters for
the  classification  of  the  West-Carpathian  Variscan  granite
suites and could be more generally useful.

REE,Y-distribution as well as the presence or absence of a

negative Eu-anomaly also discriminate all four geochemical
groups of the West Carpathian granites (Tables 1—3, Figs. 12,
13). Again, the A-type group strongly differs from each other
with high Y contents, generally over 20 ppm (Fig. 13). The Y

and HREE enrichment in the A-type granites is due to the high
content  of  zircon  and  locally  also  the  presence  of  xenotime-
(Y) and garnet (Uher & Broska 1996). The bulk REE distribu-
tion is controlled by essential REE-bearing phases, such as al-
lanite-(Ce),  monazite-(Ce)  and  xenotime-(Y),  however  a
contribution of almandine and zircon for bounding of HREE
and  Y  as  well  as  apatite  for  LREE-fixing  is  also  important
(e.g. Wark & Miller 1993). The wider range of the rare earth
elements abundance for the S-, but also for A-type granite, in
comparison with I-type is also a significant feature of the bulk-
rock chemistry of the West-Carpathian granites.  Although the
I-type granite set also comprises  differentiated dykes, the rare
earth elements pattern range is narrower mainly in the LREE
part of the diagram and max/min REE values are around 10, in
contrast to max/min REE values for the S-types of around 100
due to their more heterogeneous nature. We can only speculate
that such a difference in pattern is a result of the composition-
ally different precursor of I-type granites as well as their rapid
ascent and differentiation.

Fig. 13. Y vs. SiO

plot of the Variscan West-Carpathian granitic

rocks.

Fig. 12. Averages of the chondrite normalized REE patterns of the
Variscan West-Carpathian granitic rocks.

Fig. 14. Simplified geodynamic evolution of the principal granitic
groups in the Western Carpathians.

86 BROSKA and UHER

Table 1: Representative chemical analyses of the basic group of the West-Carpathian Variscan granites. Main elements (in wt. %), trace ele-
ments V to U (in ppm) are analysed by XRF, REE’s, Zr, Hf, Nb and Ta (in ppm) by ICP-MS. (Abr. tr. = trace content). Explanations: MK –
Malé Karpaty Mts, T – Tribeč Mts, PI – Považský Inovec Mts, MF – Malá Fatra Mts, SGR – Slovenské rudohorie Mts (Gemeric Supe-
runit), Vepor – Slovenské rudohorie Mts (Veporic Superunit), V – Velence Mts (Trans-Danubian Superunit, Hungary), PKB – Pieniny
Klippen Belt (pebbles).

Sample

ZK-48

T-87

Z-4/89

I-3

BMF-1

ZK-13

GZ-1

GZ-15

T-88

T-60/86

VG-54

ZK-118

BP-1

BP-35

VG-86

VE-4

type

Mts.

SGR

Vepor

PKB

Vepor

SiO

69.67

71.37

72.95

73.44

68.26

74.05

71.21

72.85

64.63

74.30

64.57

65.55

74.49

71.85

70.72

76.87

TiO

0.40

0.37

0.19

0.21

0.34

0.11

0.04

0.21

0.79

0.12

0.80

0.78

0.15

0.27

0.33

0.05

15.64

14.87

14.62

14.00

16.71

14.65

16.14

14.89

16.30

13.87

16.34

16.26

13.18

14.09

15.00

12.59

FeO

to t

1.96

2.31

1.59

1.75

2.49

1.15

1.53

1.32

4.40

1.12

4.29

4.06

1.86

2.10

2.48

0.63

MnO

0.05

0.04

0.03

0.04

0.02

0.07

0.02

0.07

0.05

0.03

0.02

0.06

0.01

MgO

0.85

0.87

0.36

0.71

1.60

0.24

0.91

1.77

0.25

1.62

1.56

0.09

0.82

0.99

0.04

CaO

2.61

1.73

1.19

1.18

2.81

0.34

0.30

0.26

3.55

0.89

3.59

3.24

0.36

1.25

0.26

0.50

3.88

3.54

4.21

3.27

5.09

0.27

5.92

3.41

4.22

4.26

4.36

4.22

3.73

5.63

2.09

2.96

3.10

3.02

3.18

4.39

1.89

4.46

1.25

3.19

2.34

4.00

2.54

2.16

5.16

1.54

5.28

5.37

0.13

0.18

0.12

0.10

0.06

0.23

0.21

0.15

0.28

0.12

0.29

0.34

0.03

0.07

0.16

0.02

LOI

0.80

1.30

0.80

0.70

1.30

2.90

1.00

1.50

1.30

0.70

1.70

2.30

0.60

2.40

1.80

0.90

TOTAL

99.09

99.61

99.25

99.43

99.70

99.78

97.85

98.72

99.65

100.17

100.52

99.68

100.04

99.17

99.94

tr.

119

101

138

400

173

300

113

209

233

277

289

482

261

203

498

852

193

860

850

170

143

111

154

133

240

237

268

247

422

129

0.75

0.84

0.46

0.77

0.34

5.46

2.38

1.19

0.59

0.85

1.35

0.53

1.07

1.18

1.22

1.56

830

854

844

988

327

117

150

1105

602

1263

1144

499

358

347

14.07

11.62

10.96

9.09

6.94

17.73

8.12

26.82

15.18

11.1

23.01

11.31

28.23

44.68

30.33

30.57

32.32

25.52

25.38

36.04

28.52

13.97

2.84

13.33

43.66

17.73

52.52

61.97

48.96

64.45

17.38

14.74

64.45

49.94

50.97

75.34

59.14

26.49

6.82

25.83

87.9

36.15

116.75

124.77

104.96

131.49

36.95

30.2

7.35

5.64

5.86

8.63

6.79

3.11

0.92

3.68

10.21

4.37

14.12

14.15

12.08

15.75

4.41

3.99

27.21

21.15

22.56

31.69

25.91

11.56

3.17

14.48

38.47

16.35

55.61

50.58

45.86

60.47

16.96

14.89

5.0

3.8

4.32

6.48

4.79

2.87

1.27

3.86

6.45

3.45

10.27

8.24

8.77

11.77

4.51

3.89

1.08

1.1

0.7

0.93

1.03

0.45

0.02

0.3

1.58

0.6

2.38

1.87

0.68

1.64

0.59

0.19

3.97

2.84

3.21

4.73

3.19

2.9

1.28

4.46

4.61

2.79

7.27

5.18

7.42

9.98

4.89

3.83

0.52

0.4

0.43

0.53

0.37

0.56

0.3

0.79

0.6

0.4

0.92

0.61

1.02

1.56

0.84

0.68

2.85

2.28

2.25

2.41

1.72

3.5

1.73

5.22

3.11

2.27

4.71

2.89

6.05

9.25

5.19

4.69

0.51

0.43

0.39

0.32

0.26

0.58

0.24

0.99

0.57

0.42

0.84

0.46

1.13

1.79

1.04

1.02

1.38

1.11

0.97

0.69

0.6

1.45

0.62

2.88

1.49

1.13

2.42

1.09

3.16

5.0

3.04

3.27

0.19

0.15

0.13

0.09

0.2

0.09

0.45

0.21

0.16

0.36

0.13

0.45

0.74

0.46

0.52

1.26

0.95

0.83

0.42

0.62

1.17

0.55

2.99

1.27

1.05

2.19

0.94

2.83

4.69

2.83

3.9

0.19

0.14

0.13

0.07

0.1

0.15

0.06

0.43

0.19

0.14

0.32

0.14

0.43

0.68

0.4

0.63

An explanation of the Eu-anomaly is found mainly in the

different oxygen fugacity or water activity of the primary
melts. In concordance with Puchelt & Emmermann (1976),
Williams (1997), Sha & Chappel (2000), we regard the nega-
tive anomaly as an indicator of lower fO

provided that the

whole rock was not depleted in europium. The negative Eu-
anomaly originated under reducing conditions, when europi-
um occurs only in the divalent state and it is incorporated
into plagioclase. Lower fO

or water activity in the melts in

comparison with I-type granites was actually assumed for S-
type groups also on the basis of Fe

-rich accessory mineral

paragenesis (presence of almandine and ilmenite, absence of
magnetite, allanite and titanite). Biotite composition indicat-
ed the I-type granitoids originated in relatively oxidized and

water-rich conditions (about 5—6 wt. % of water), on con-
trary, the S-type granites crystallized from a relatively re-
duced magma with low water content (2—3 wt. % ) (Petrík &
Broska 1994; Petrík & Kohút 1997). The oxidized conditions
in the I-type melt provided the trivalent state of Eu and it ex-
plains, why europium was not able to fractionate with feld-
spars in these granites.

Geodynamic scenario of granite origin

The compositional variations and differences among the

granitic groups of the Western Carpathians reflected their
genesis including the geotectonic position and source rocks.
The geotectonic position of the S and I-type granites was

WHOLE-ROCK CHEMISTRY AND GENETIC TYPOLOGY OF VARISCAN GRANITES 87

Table 2: Average and ranges of granitic rock compositions (distribution see in the Fig. 1). Note: 6 diorite analyses are not presented.

S-type n = 78

spec. S-type n = 22

I-type n = 29

A-type n = 30

Sample

av.

st. dev.

max.

min.

av.

st. dev.

max.

min.

av.

st. dev.

max.

min.

av.

st. dev.

max.

min.

SiO

71.84

2.89

77.45

63.02

72.04

2.83

75.93

65.30

67.82

3.60

74.30

62.51

72.86

2.45

78.93

68.65

TiO

0.26

0.19

0.89

0.02

0.17

0.73

0.04

0.57

0.32

1.25

0.09

0.24

0.10

0.46

0.05

14.90

0.99

18.48

12.84

14.78

1.67

19.18

13.07

15.35

1.18

18.85

13.50

13.77

0.88

15.69

12.45

tot

1.96

1.16

6.50

0.43

1.63

0.75

3.99

0.82

3.37

1.34

5.79

1.12

2.27

0.92

3.99

0.46

MnO

0.04

0.23

0.00

0.04

0.07

0.37

0.01

0.06

0.02

0.10

0.02

0.05

0.10

0.59

0.00

MgO

1.02

3.38

30.00

0.06

4.42

19.34

91.00

0.05

1.32

0.65

2.98

0.19

0.43

0.29

1.00

0.02

CaO

1.38

0.90

3.03

0.14

0.38

0.35

1.88

0.14

2.40

1.12

3.79

0.30

0.74

0.51

2.20

0.04

3.94

0.79

5.51

0.27

3.42

1.33

5.92

0.13

3.98

0.67

6.83

3.03

3.92

1.09

7.99

2.96

3.17

1.08

5.31

0.90

4.23

1.48

5.87

0.37

3.20

1.14

7.07

1.94

4.18

1.35

5.37

0.10

0.15

0.07

0.57

0.04

0.18

0.06

0.33

0.06

0.24

0.11

0.45

0.07

0.04

0.19

0.01

26.0

22.4

1.0

10.0

1.0

63.1

33.9

125

10.0

14.9

11.2

tr.

14.0

23.5

184

tr.

8.6

7.1

1.0

21.5

10.3

1.0

15.2

19.5

108

2.0

6.5

tr.

8.6

9.5

tr.

10.0

7.8

1.0

5.5

7.6

1.0

6.1

12.9

tr.

6.2

5.7

1.0

5.7

5.0

tr.

4.4

6.4

tr.

43.6

27.2

139

2.0

37.7

16.1

14.0

66.2

27.7

114

15.0

49.9

23.3

110

9.0

103.0

39.2

233

24.0

400.7

179.3

868

173.0

86.1

23.6

159

58.0

185.4

65.9

277

6.0

300.5

219.0

1056

10.0

24.8

15.4

7.0

599.2

242.8

906

81.0

74.8

65.4

344

10.0

113.1

60.6

272

18.0

82.8

47.5

214

26.0

185.6

79.1

309

46.0

241.7

132.2

649

64.0

8.1

2.9

1.0

11.2

4.0

1.0

11.1

4.4

5.0

15.1

3.8

9.0

693.4

399.0

2469

32.0

120.7

84.0

310

29.0

1100

365.2

2146

455.0

479.1

312.6

1294

29.0

22.7

12.5

tr.

12.4

10.2

0.0

37.8

17.8

5.0

38.6

17.9

3.0

8.2

6.2

tr.

19.2

17.7

8.0

11.2

6.3

4.0

19.4

7.5

10.0

2.5

1.7

tr.

20.5

62.2

298

2.0

4.1

2.9

tr.

3.4

2.2

tr.

12.00

6.05

31.07

3.91

20.27

7.20

30.77

8.12

14.70

7.95

37.02

2.79

38.90

27.81

157.59

15.34

8.00

3.52

21.96

1.22

14.30

4.29

22.32

6.69

10.88

5.14

25.40

3.56

16.41

5.61

32.74

2.86

23.34

12.99

70.91

0.84

9.37

6.26

25.35

2.60

40.90

18.92

86.91

12.96

38.28

20.27

78.84

4.81

48.00

25.60

126.98

1.58

22.06

14.39

55.55

6.82

84.58

39.84

179.40

22.90

81.00

42.15

175.60

9.10

5.52

2.87

13.09

0.18

2.64

1.58

6.77

0.88

9.45

4.90

19.32

1.09

9.69

5.25

21.33

1.87

20.73

10.63

47.55

0.50

9.96

6.04

26.04

3.17

37.02

17.84

70.73

10.46

37.30

20.65

84.29

8.54

4.03

1.78

8.66

0.19

2.81

1.27

6.14

1.27

6.43

3.01

13.56

2.34

8.12

5.05

26.57

2.66

0.80

0.35

1.87

0.02

0.19

0.17

0.68

0.02

1.43

0.68

3.19

0.46

0.97

0.63

2.92

0.03

3.15

1.36

7.52

0.19

2.90

1.15

5.64

1.28

4.53

2.20

10.36

1.57

7.58

5.69

32.46

2.36

0.45

0.19

1.18

0.07

0.59

0.18

0.94

0.30

0.58

0.29

1.42

0.14

1.21

0.92

5.26

0.42

2.44

1.15

6.56

0.67

3.87

1.23

5.76

1.73

3.04

1.57

7.57

0.62

7.49

5.38

30.48

2.87

0.44

0.22

1.22

0.13

0.71

0.28

1.14

0.24

0.55

0.29

1.40

0.10

1.49

1.07

5.97

0.54

1.16

0.63

3.41

0.31

2.04

0.93

3.41

0.62

1.47

0.84

3.81

0.30

4.33

2.91

15.91

1.55

0.16

0.09

0.52

0.02

0.31

0.15

0.54

0.09

0.21

0.13

0.55

0.05

0.63

0.37

1.81

0.23

1.00

0.57

3.42

0.04

2.02

1.02

3.38

0.55

1.31

0.80

3.51

0.36

4.17

2.23

11.82

1.56

0.15

0.08

0.51

0.05

0.28

0.16

0.51

0.06

0.19

0.11

0.50

0.07

0.63

0.33

1.76

0.21

2.99

1.38

6.46

0.48

2.00

0.83

4.74

1.21

4.69

1.80

7.42

1.46

5.27

2.23

11.60

1.85

0.73

0.43

2.03

0.10

2.67

1.24

5.46

1.19

0.74

0.38

1.50

0.23

1.33

0.45

3.06

0.57

8.35

6.06

42.36

0.56

10.72

2.72

18.64

7.21

11.69

6.01

35.04

3.79

17.59

7.55

51.03

6.16

firstly discussed by Petrík et al. (1994), and the A-type gran-
ites  by  Uher  &  Broska  (1996).  In  addition,    we  propose  a
modified outline of the genesis of all four principal Variscan
granitic  groups  in  the  Western  Carpathians,  subdivided  ac-
cording to the presented mineralogical and geochemical cri-
teria  (Fig.  14).  Early  Carboniferous  continental  collision,
which  in  generally  operated  in  the  European  Variscides
(Matte 1986; Finger & Steyrer 1990; von Raumer & Neubau-
er 1993; Stampfli 1996 among others), led to crustal thicken-
ing along thrusting planes, formation of the Variscan nappes
and  partial melting of the lower crust in the zone of contrac-
tion  of  the  lithospheric  slab.  After  subduction  of  oceanic
crust along destructive active plate margins (Stampfli 1996),
the lower density of the continental crust, which is buoyant
and remains on the upper surface of the lithosphere,  led to
thickening  of  the  collided  continents  and  crust  (Fig.  14A).
Emplacement of the S-type granite, which originated mainly

from the metagreywacke protoliths (Petrík 2000) as well as
granites with transitional features between the S- and I-type
group  probably  from  the  amphibolite-bearing  lower  crust
(Kohút et al. 1999b), occurred in the extension zones, which
occur  locally  in  the  framework  of  the  continental  collision
(Schaltegger 1997) or in the upper part of the flexures of the
lithosphere plate (Fig. 14A) (c.f. Coward 1994). A local ex-
tension zone is indicated for example by  the presence of lac-
colith (Lexa & Bezák 1996) but also by the sheet-like shape
of the emplaced plutons (Kohút & Janák 1994). However, the
numerous  pegmatites  accompanying  the  S-type  granites  in
the Western Carpathians show the general collisional (com-
pression) conditions. On the other hand, post-collisional tec-
tonics associated with the gravitational instability of thicken-
ing  lithosphere  started  the  process  of  thinning  of  the
lithosphere  and  extensional  regime,  which  resulted  in  the
production  of  the  I-type  granites  with  lesser  pegmatite  for-

88 BROSKA and UHER

mation in the region. The origin of the I-type granites show
the distinct influence of the mantle or infracrustal contribu-
tion and process of their melting was triggered by heating of
the  crust  due  to  the  underplated  mafic  lithospheric  mantle
melt  (Fig.  14B)  which  was  primarily  activated  by  previous
detaching of the oceanic slab and its injection into the mantle
(Fig.  14A).  Uplift  into  a  vertical  tectonic  extensional  fault
system is followed by formation of larger batholiths (Hutton
1987)  in  the  middle  crust  which  is  observed  mainly  in  the
Veporic Superunit. The thermal influence of the huge cham-
bers  of  I-type  granite  melts  in  the  middle  crust  also  caused
the  partial  melting  of  the  middle  crust  and  origin  of  a  new
generation of the S-type granite (Hraško et al. 2000). The S-
and  I-type  granite  can  be  regarded  as  orogenic  granites.  In
contrast, the A-type granites which were formed in the Pan-
gaea  continent  (Late  Paleozoic  to  Mesozoic  supercontinent
– see e.g. Johansson 2000) belong already to post-orogenic
granite  suites  which  are  typically  distributed  in  European
Variscan terrain along the strike-slip lineaments and faults in
the  crust  (Bonin  1990)  (Fig.  14C).  The  process  of  A-type
granites  formation  is  associated  with  melting  of  granitic
sources  (Petrík  2000)  and  emplaced  during  extension  and
transtension  regime.  The  specialized  S-type  granites  (S

type), which occurred in the same period as the A-type gran-
ites,  were  probably  melted  from  the  muscovite  metapelites
(Petrík 2000) in the middle crust and during continuation of
the thermal event caused by underplated mafic melts, which,
through deep rifts to the mantle, also formed numerous vol-
canic  extrusions  in  the  Permian  or  Permian—Triassic  age
(Fig.  14C).  The  rifting  process,  which  opened  the  Meliata-
Hallstadt ocean in Triassic, could have been a thermal source
for melting of the middle crust.

Conclusions

The results presented generally support the subdivision of

the Variscan West-Carpathian granites into four genetic
geochemical groups based on older mineralogical, geochemi-
cal and isotope data.

The S-type group exhibits typical features of orogen-related

crustal granites with a relatively wide span of fractionation
level. The I-type group represents relatively poorly evolved
rocks enriched in compatible elements such as Ba, Sr, Zr and
REE’s with a possible contribution of mantle material during
their origin. The A-type group represents a specific post-oro-
genic hot and dry granite with a relatively high fractionation
level rich in compatible (REE, Y, Zr) as well as alkali elements
(K, Rb). The S

-type group belongs to the highly-evolved B,

Sn peraluminous and P-enriched suite with rare-element spe-
cialization (high Si, K, Ta, Sn, F, Rb, Nb). The different char-
acter of these principal granite groups in the Western Car-
pathians is reflected in their geotectonic positions. The S- and
I-type granites as representatives of the orogenic granites are
directly connected with collisional and extensional regime
during/after continent collission with a various contribution of
mantle lithospheric melt especially in the post-collisional tec-
tonics. On the other hand, the A- and S

granite types formed

in post-orogenic conditions.

Finally, the major and trace-element geochemistry together

with  the  accessory  mineral  paragenesis  clearly  document  a
complex  and  long  history  of  Variscan  granite  origin  in  the
West-Carpathian  area  from  early-orogenic  to  post-orogenic
stages  and  it  could  contribute  to  the  understanding  of  such
evolution in analogous orogenic belts.

Acknowledgements: The work was supported by NSERC Re-
search Grant and a Major Installation Grant to P. Černý, Univ. of
Manitoba, Winnipeg, Canada, during Post-Doctoral Fellowship
of P. U. in Canada. The evaluation of the samples was financed
by VEGA Grant #7074. The authors thank to M. Kohút and I.
Petrík for providing some samples for fruitful discussion which
improved the early version of the manuscript. We are also
grateful to D. Plašienka and W.E. Stephens for their comments
and to L. Zahradník for his assistance with PC. The paper is a
contribution to the UNESCO “International Geological Correla-
tion Project #373” headed by R. Seltmann.

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