GEOLOGICA CARPATHICA, 49, 3, BRATISLAVA, JUNE 1998
THE BREAKDOWN OF MONAZITE IN THE WEST-CARPATHIAN
VEPORIC ORTHOGNEISSES AND TATRIC GRANITES
and PAVOL SIMAN
Geological Institute, Slovak Academy of Sciences, Dúbravská cesta 9, 842 26 Bratislava, Slovak Republic; firstname.lastname@example.org
Slovak Geological Survey, Mlynská dolina 1, 815 00 Bratislava, Slovak Republic
(Manuscript received June 26, 1997; accepted in revised form March 24, 1998)
Abstract: The complete breakdown of monazite was observed in metagranites of the Veporic Superunit while only
slight alteration of monazite occurs in unmetamorphosed Tatric granitoids (Tribeè Mts., Malá Fatra and Stráovské
vrchy Mts.). Monazite breakdown is probably a result of the reaction monazite+annite+anorthite+quartz+fluids giv-
ing apatite+allanite+muscovite. During monazite breakdown its margins are replaced outward by apatite corona,
allanite rim and REE-rich epidote. In extreme cases monazite cores are fully consumed by apatite which occupies the
place of the former monazite. The result of such breakdown is grains with apatite cores and the allaniteREE epidote
rims. The monazite breakdown in the Veporic Superunit occurred under conditions of amphibolite facies during an
Alpine metamorphic event, although the proccess of breakdown had probably already started during the Variscan
metamorphosis. In the case of monazite from Tatric granites initial breakdown of monazite was found in the context
of Variscan subsolidus granite alteration. Only restricted mobility of the REE is supposed during the breakdown of
Key words: Alpine metamorphism, REE mobility, monazite, allanite, granite, metagranite.
Monazite and allanite are two of the most frequent primary
magmatic LREE acccessory mineral phases of granitoids,
however, they show an antipathetic relationship either
monazite or allanite is present in granitoids, or one of them
strongly prevails in paragenesis (Lee & Dodge 1964; Lya-
khovich 1968; Gromet & Silver 1983; Broska & Uher 1991;
Montel 1993). Generally monazite is typical of S-type, Ca-
poor or peraluminious granitoid accessory mineral paragen-
esis, while allanite is reported mainly from I-type granitoids
(Snetsinger 1967; Parrish 1990).
Both monazite and allanite can also form during meta-
morphism, where they show the dichotomy known from the
felsic magmas. Accessory monazite is rare in the green-
schist facies, rare to scarce in amphibolite facies, and quite
abundant in the granulite facies of metamorphic rocks. On
the contrary, allanite or REE-rich zoisite is common at low-
er metamorphic grades (Overstreet 1967). However, in the
Ori Dome low-grade slates (Central Pyrenees) poikiloblas-
tic monazite was described, which nucleated on small detri-
tal grains during anchimetamorphic conditions. In green-
schist facies this monazite is replaced by allanite (Bons
1988). Metamorphic monazite, as grey Eu-rich monazite, is
also known from greenschist facies (Donnot et al. 1973;
Read et al. 1987), but monazite was also reported in stauro-
lite-kyanite metamorphic grade (Mohr 1984) or staurolite-in
isograde in conditions of 525
C and 3 kb (Smith & Barreiro
1990). Franz et al. (1996) described monazite in Bavaria
newly formed at ca. 450700
C in low pressure
metapelites. The possible origin of monazite from break-
down of allanite or allanite hornblende and apatite in the au-
gen gneisses from the Swedish-Norwegian province in Cpx-
in and Opx-on isograde showed Bingen et al. (1996).
The aim of the paper is to describe the monazite being re-
placed by allanite which we have found in the Western Car-
pathian granites and metagranites. The first replacement of
monazite by allanite was reported from pegmatite in North
Carolina (Murata et al. 1957) and some remarks on this al-
teration phenomenon in the alkalic complex of the Vish-
nevyje gory can be found in Yeskova & Ganzyeva (1964).
The origin of deuteric allanite and sphene during chloritiza-
tion of biotite in the Dartmoor Granite was described by
Ward et al. (1992). Secondary allanite as a product of chlori-
tization was also reported from the Bohus Granite in SW
Sweden (Eliasson & Petersson 1996). The recent work of
Finger et al. (1998) brings a modern and comprehensive de-
scription of monazite breakdown in localities from the Austri-
an part of the Alps and from the Southern Bohemian Massif.
Total monazite breakdown in West-Carpathian metagran-
ites from the Veporic Superunit is described in this contribu-
tion. We also report a low-degree monazite alteration during
postmagmatic subsolidus activity of the fluids in non or (an-
chi)-metamorphic Tatric granites.
Migmatites with signs of a high degree of monazite break-
down belong to the Veporic basement which consists of three
basic lithotectonic units (Bezák 1994). The lower unit occurs
mainly in the southern part of the Veporic basement, the mid-
dle unit is thrust over the lower unit, the upper unit is present
162 BROSKA and SIMAN
in separate tectonic remnants beyond the studied area. The
lower unit consists of Lower Paleozoic metamorphites of the
greenschist facies (mica schists, albitic gneisses, chlorite-
muscovite schists). The middle unit comprises a broader
scale of metamorphites starting from the upper part of the
greenschist facies up to the upper part of the amphibolite fa-
cies. The age of the above mentioned metamorphites is uncer-
tain, but probably Proterozoic to Early Paleozoic. The studied
migmatites come from the locality Lipové village in the mid-
dle unit (loc. 4 in Fig. 1). According to Siman et al. (1996a)
the P-T conditions for the earliest metamorphism of the host
rocks with migmatite structure and with the tonalite composi-
tion (Fig. 2) were 680730
C at 400600 MPa and around
C for a retrograde branch. The degree of Alpine
overprint is a matter of discussion, but the minimum tem-
perature estimate is T 480510
C and around 7 kbars (Si-
man et al. l.c.).
By contrast, only low degrees of monazite breakdown
were observed in the granites of the Tatric Superunit (Fig.
1). The Tatric granites which form the cores of the crystal-
line basement in the central Western Carpathians belong to
the two main Carboniferous granite groups: S-type granites
are the most widespread granite type, while I-type granites
(Petrík et al. 1994), which include mainly granitoids known
as the Sihla type sensu lato are less frequent (Broska &
Petrík 1993). No metamorphism, or only anchimetamor-
phism is known in these granites, but strong subsolidus
overprint of the primary mineral assemblage is their typical
phenomenon. Monazite alteration was found in the Tribeè
Granite (I-type), Malá Fatra Mts. and Malá Magura Granite
(both S-type). Biotite granite in the Tribeè Mts. occurs in
the form of veins 10.1 m in size which cut the undifferenti-
ated biotite tonalite host rocks near the Kozliov elevation
point. The occurrences in the Malá Fatra Mts. come from
the Bystrièka quarry (leucocratic granodiorite), in the Malá
Magura two mica granite showing monazite breakdown was
found in the Chvojnica Valley (Fig. 1).
Petrography and mineral composition
Migmatite from the Veporic Superunit
The host migmatites with a high degree of monazite
breakdown consist of well developed paleosom and neosom
up to 5 mm thick (Fig. 2). They are peraluminious meta-
greywacks (lacking Al
phases and containing quartz,
plagioclase, biotite, phengite, ±K-feldspar, chlorite). Synge-
netic ductile deformation associated with partial melting in
the whole hybrid complex was observed. Plagioclase forms
partly retrogressed to granoblastic aggregates of more or
less sodic grains filled with sericite±zoisite. In the most de-
formed places plagioclase is replaced by albite and/or seric-
ite felt. The maximum anorthite content is in the range of
. Quartz represents mylonitic crushed grains or
it is recrystallized into granoblastic aggregates. K-feldspar
is found as cataclastic and from place to place shows per-
thitic texture. White mica has a phengitic composition, bi-
otite has Mg/(Mg+Fe) from 0.33 to 0.57, Al
0.6 to 1, TiO
is up to 3 wt. % (Siman et al. 1996a). Two
types of garnet occur in the migmatites. The older garnet has
almandine-pyrope compositions, the younger garnet forming
rims around older garnets (sometimes isolated grains) with
3340 % grossularite molecule (Siman et al. 1996a).
Granites from the Tatric
The strong sericitization of plagioclases, chloritization
and epidotization of the biotites are characteristic alterations
of the main mineral assemblages in these Tatric granites.
The basicity of the plagioclase is mainly An
, the biotite
in the Tribeè locality is relatively Mg-rich, with Fe/(Fe+Mg)
ranging from 0.40.5, on the other hand in the S-type gran-
ites from the Malá Magura and Malá Fatra Mts. there are
Fe-rich biotites with Fe/(Fe+Mg) above 0.6 and more Ti-
rich in comparison with the I-type in the Tribeè Mts. (Petrík
& Broska 1994; Broska et al. 1997). The Malá Fatra granite
almost lost its biotite due to its strong alteration to chlorite
and white mica and only part of the monazite grains inside
of biotite or former biotite are attacked by fluids and
Fig. 1. Geological outlines of the crystalline basement of the West-
ern Carpathians with the localities of the monazite breakdown ob-
servation. The light shaded area represents the granite bodies of
the Tatric units. The darker shade filling represents the areal distri-
bution of the hybrid complex in the Veporic Superunit, which is a
structure of host migmatites and orthogneisses with a high degree
of monazite breakdown (locality Lipové for example), arrows ap-
prox. indicate the position of the studied localities: 1 Tribeè
Mts., Velèice village, 750 m W from the elevation point Kozliov.
Outcrop on the slope. 2 Malá Fatra Mts. Kra¾ovany, Bystrièka
quarry. 3 Stráovské vrchy Mts., Suchý, Chvojnica Valley. 4
Slovak Ore Mts. Kokava/Rimavica, 2 km from Kokava direction to
oltýska, outcrop on the road near the village of Lipové.
Fig. 2. Example of migmatite structure from the Lipové locality
(hybrid complex, Veporic Superunit). Scale bar is 1 cm.
THE BREAKDOWN OF MONAZITE IN THE WEST- CARPATHIAN VEPORIC ORTHOGNEISSES 163
changed to allanite. The chemical compositions of the gran-
ites with altered monazites as well as migmatite from the
Veporic Superunit are presented in Table 1.
Monazite, a common accessory phase in the migmatite
and metagranites from the Veporic Superunit is transformed
into apatite and allanite-epidote in the way which was first
observed and described in the Granatspitze Granite Tauern
Window, Penninic Unit, Eastern Alps (Finger et al. 1998)
(Fig. 3A). The size of grains is around 10
m but in some
cases monazite reaches up to 200
m. The monazite grains
are surrounded by tiny grains of apatite which always con-
tinues outwards as allaniteepidote, with irregular shapes
which often penetrate into the biotite grains (Fig. 3A). Cas-
es where only unhomogeneous apatite is surrounded by al-
lanite-epidote rim are also present, and in this case no mon-
azite remnants in the cores of the apatiteallaniteepidote
mineral complex have been observed. Such phenomena rep-
resent the last stage of the monazite transformation when
the monazite is completely replaced by newly-formed apa-
tite and allanite minerals (Fig. 3B). The rim forming allanite
consists of two principal phases the inner part which is
richer in REE elements, the outer part which has epidote
composition (Fig. 3A, Table 2). The inner part of allanite-
epidote phase respects the monazite morphology, the outer-
most epidote phase has low integrity, and often fills cracks
and spaces within sheets in the biotite.
During replacement the phosphorus anion from monazite is
fixed in apatite, REEs enter the allanite and epidote. The el-
ements nourishing the growing allanite, such as silica, iron
and aluminium as well as OH groups come from annite, and
calcium mainly from anorthite components. It is possible to
express the breakdown of monazite in the form of a hypothet-
ical reaction where hydrogen comes from dissociated water:
monazite + annite + anorthite + quartz + fluids = apatite +
allanite + muscovite (or K-feldspar)
or in chemical form:
(OH,F) + 3CaLaFe
(OH,F) + KAl(Si
We suggest that the reaction was activated by the origin
of phosphoric acid on the monazite rim. The apatite, which
originated firstly on the monazite rim could later be the
transport medium for exsolvus of the REE from the mona-
zite outward into the allaniteepidote, is inhomogeneous
and free of the REE. Probably it was in gel form and per-
haps the recent mosaic or grained polycrystalic structure of
apatite (Fig. 3a,b) indicate this stage. In this sense the apa-
tite is the memory of the role of the phosphoric acid in the
monazite breakdown processes.
The monazite breakdown recorded in the Alps and the
Southern Bohemian Batholith is known only from the granite
lithologies which were overprinted by Alpine metamorphism
under amphibolite facies. On the other hand metapelite lithol-
ogy brings an opposite effect, when during these metamor-
phic conditions new monazite is formed Finger et al. (l.c.).
The breakdown of the monazite in the Tatric granites is
not so widespread, and the processes produce only small
fringes of allanite without an intercalated apatite zone.
However, the apatite zone is most probably also present in
the monazite-allanite grains, and is not detectable in the
studied samples only as a result of its small size. The pro-
cess of monazite breakdown is found in the S-type, granite
but also in the I-type, especially in the more evolved or dif-
ferentiated varieties of the Tatric Superunit.
Because the subsolidus fluids were able to transform
monazite to allanite only in the restricted form (Ward et al.
1992; Eliasson & Petersson 1996), the high degree of mona-
zite breakdown from Lipové (Veporic Superunit) could be a
result of metamorphic processes. In the case of the primary
monazite from the non-metamorphic Tatric granites, where
only initial breakdown of monazite was observed, the mon-
azite breakdown should coincide with chloritization during
subsolidus pervasive alteration of these granites. On the
other hand, the high degree of monazite breakdown in the
Lipové migmatite suggests the overprint of monazite during
Tribeè Malá Fatra
Table 1: Chemical analyses of the host rocks of altered monazites.
Sample BGM-1 and BMF-1 represent granodiorites, sample T-37
is biotite monzogranite. VM-4/90 represents a typical migmatite to
orthogneiss of the hybrid complex of the Veporic basement.
164 BROSKA and SIMAN
metamorphosis, and it should be similar to the process
known from the Alpine terrain in the Tauern Window
(Granatspitz granite gneiss), Austro-Alpine Unit (Raabal-
pen Massif, Winnebach migmatite gneiss, Sulztal granite
gneiss, Zinken granite gneiss) and the Moravian Unit in the
Eastern Bohemian Massif (Witersfeld gneiss, Bitesch
gneiss) (Finger et al. 1998). The observed breakdown of
monazite in all the mentioned cases occurred in the am-
phibolite facies (500600
C and 47 kbar) (Finger et al.
1998 and references therein).
The monazite zoning (Fig. 3A, Table 2), indicating its
magmatic origin (Lipové locality) in the formerly felsic
magmatite of Devonian age, is also preserved during mona-
zite breakdown in the monazite cores. Felsic magmatites
from the early Variscan stage (Devonian age) are known,
apart from the Veporic hybrid complex, also in the Western
and Low Tatras, Ve¾ká Fatra (Petrík & Kohút in press). Af-
ter the emplacement of the Devonian felsic magma, intru-
sions of the layered magmas into shear zones are known
from this area, as a process accompaning the main Variscan
metamorphic event, which reaches amphibolite facies in
this area and with the formation of orthogneisses and mig-
matites. The breakdown of monazite in the Lipové meta-
granites, in this sense, started as a result of this prograde
metamorphism of the amphibolite stage and deformation
during thrusting together with the Hercynian thickening and
the following relaxation (Siman et al. 1996a,b), which is
dated by the main Variscan granite intrusions of the S-type
granites (Cambel et al. 1990) ca. 350330 Ma.
The P-T conditions during the Alpine metamorphism
which contributed to the breakdown of the monazite in the
Veporic Superunit, especially in its southern part, are being
widely discussed at present. In this region the Alpine meta-
morphic assemblages as well as the mineral zoning indicate
Table 2: Representative microprobe analyses of the grain 1 and 2 in the migmatite from Veporic Superunit. The points of analyses are in
the BSE images (see Fig. 3). The measure conditions: 20kV, 20 nA, 3 M beam diameter, using ZAF corection and natural and synthetic
standards. Jeol Superprobe 733.
THE BREAKDOWN OF MONAZITE IN THE WEST- CARPATHIAN VEPORIC ORTHOGNEISSES 165
a progressive trend of metamorphism (Méres & Hovorka
1991; Kováèik et al. 1996). According to Kováèik et al.
(1996), the Alpine regional metamorphism occurred at tem-
peratures estimated between 350 and 500
C and under low
to medium pressure conditions (300 MPa) i.e. in greenschist
metamorphic conditions. According to these authors, the
Alpine regional metamorphism is characterized by infiltra-
tion metamorphism and relatively high fluid pressure,
which could have contributed to the reduction of lithostatic
pressure. The model implying convective fluid flows, oper-
ating due to higher heat flow as well as differences in per-
meability of the rocks, seems to fit the geodynamic interpre-
tation of the Alpine metamorphism of the southern Veporic
Superunit (Kováèik et al. 1996). On the other hand the latest
geothermobarometric calculations give higher P-T condi-
tions during peaks of metamorphism: 550600
C and 800
1000 MPa (Janák et al. 1997; Plaienka et al. 1997), which
represents the amphibolite facies (epidoteamphibolite sub-
facies). According to Plaienka et al. (1997), the Alpine
metamorphism in the southern Veporic Superunit was
caused by burial of the Veporic basement as well as its Per-
momesozoic cover during the Cretaceous collisional events.
The possibility of the temperature exceeding 500
some parts of the southern Veporic Superunit is also indicat-
ed by Krá¾ et al. (1996). The Alpine metamorphism in this
sense triggered the intensive breakdown of the monazite
(Fig. 3) as in the case of the Alpine terraine because the am-
phibolite facies was reached, which seems to be a neccessa-
ry condition for extensive development of this process (Fin-
ger et al. 1998). Although the high degree of monazite
breakdown reflects both the Late-Variscan and Alpine meta-
morphic events in a hybrid complex (the Lipové locality),
the contribution of Alpine metamorphism was more signifi-
cant which is the reason for monazite instability with areal
distribution in the southern Veporic Superunit. The mona-
zite breakdown is observable not only in the hybrid com-
plex (Fig. 1) but this phenomenon is also known in the adja-
cent area. Recently Hrako et al. (1997) described apatite
with allanite rim in Klenovec granites and also in the Rima-
vica Granite (oral communication).
The age of the Alpine metamorphism which caused the
monazite breakdown was determined as around 110 Ma by the
Ar method on amphiboles. Then, after the metamorphic
peak conditions, the Veporic Superunit was uplifted and younger
Ar/Ar ages of around 88 Ma are connected with the emplace-
ment of higher superficial nappes (Kováèik et al. 1996).
REE mobility: The monazite breakdown indicates a mo-
bility of the rare earth elements, but it seems that it was in
restricted form and the mobilization of REEs was on a local
scale only. It could be stated that the monazite grains pre-
served features of their primary magmatic zonality with in-
creasing LREE (La, Ce) towards the rim of the grains and
decreasing yttrium (Table 2), while the REE whole rock pat-
terns of the studied samples in the Tatric granites show no
significant anomalies (Broska et al. 1997). The diffusion of
the REE was continual which is evident from the REE pat-
tern of the monazite and its breakdown products, newly
formed allanite (Fig. 4). The rapid decrease of REE in al-
lanite to REE-epidote in the small distance to the outermost
rim of brokendown monazite also suggests that only limited
mobility of REE occurred.
Fig. 3. The BSE images of the analyzed grains from the magmatite (Hybrid complex, locality Lienica). The number of analyses are the
curent position of the analyses from Table 2. AGrain 1 consists of a monazite core (Mnz), apatite transition zone (Ap) and rim of allan-
ite-REE epidote (Aln). BGrain 2 has an apatite core and allanite-REE epidote rim. The analyses of grains A and B are given in Table 1.
Fig. 4. REE pattern of the monazite core and the newly-formed al-
lanite in the metagranite of the Veporic Superunit.
166 BROSKA and SIMAN
The replacement of primary magmatic monazite by meta-
morphic allanite and apatite was observed in the Lipové
migmatite and other metagranites from the Veporic Supe-
runit (Western Carpathians). The Alpine metamorphic event
caused the widespread breakdown of primary monazite in
the Veporic Superunit, although we presume that the mona-
zite transformation started already during the late-Variscan
orogenesis. The replacement is accompanied by formation
of a transition zone between these mineral phases which
consist of apatite. Apatite was formed from phosphoric acid
and it acted as a transport medium for the rare earth ele-
ments outward from monazite. Sometimes total breakdown
of monazite occurred. In this case monazite completely dis-
appeared and only apatite remains in the core of grains over-
grown by allanite and REE epidote. The monazite reaction
with biotite and anorthite which produced the allanite may
have been triggered by fluids with higher activity of phos-
phorus. The P-T conditions of this replacement were esti-
mated for amphibolite facies.
A much lower degree of monazite breakdown was ob-
served in the Tatric granites. In this case we concluded that
the monazite alteration coincided with pervasive alteration
of granites in the subsolidus stage.
Acknowledgement: This research was supported by Project
No. 150 of Lise-Meitner stipendium (Austria) and (Ga 4078
VEGA Slovak Acad. Sci.). The authors are thankful for crit-
ical comments and discussion with Prof. Dr. F. Finger from
Salzburg University, and also wish to thank Dr. Igor Petrík
from the Geological Institute of the Slovak Academy of Sci-
ances who helped improve the final version of the paper.
Bezák V., 1994: Proposal of the new dividing of the Western Car-
pathian crystalline based on the Hercynian tectonic building
reconstruction. Miner. slovaca, 26, 16 (in Slovak with En-
Bingen B., Demaiffe D. & Hertogen J., 1996: Accessory mineral
assemblage in amphibolite (allanite + titanite) to granulite
(monazite + thorite) facies metaluminious orthogneisses
(S.W. Norway). Geochim. Cosmochim. Acta, 60, 8, 13411354.
Bons A.J., 1988: Intracrystalline deformation and slaty cleavage
development in very low-grade slates from the Central
Pyrenees. Geol. Ultraiectina, 173.
Broska I. & Uher P., 1991: Regional typology of zircon and their
relationship to allanite/monazite antagonism (on example of
Hercynian granitoids of the Western Carpathians). Geol. Car-
pathica, 42, 271277.
Broska I. & Petrík I., 1993: Tonalite of the Sihla s.l.: a Variscan
plagioclase-biotite I-type magmatite in the Western Car-
pathians. Miner. slovaca, 25, 2328 (in Slovak with English
Broska I., Petrík I. & Benko P., 1997: Petrology of the Malá Fatra
granitoid rocks (Western Carpathians, Slovakia). Geol. Car-
pathica, 48, 1, 2737.
Cambel B., Krá¾ J. & Burchart J., 1990: Isotopic geochronology of
the Western Carpathian crystalline complex with catalogue of
data. Veda, Bratislava, 1183 (in Slovak, English summary).
Donnot M., Guigues J., Lulzac Y., Magnien A., Parfenpff A. & Pi-
cot P; 1973: Un nouveau type de gisement deuropium: la
monazite grise a europium en nodules dans les schistes paléo-
zoiques de Bretagne. Mineralium Deposita, 8, 718.
Eliasson T. & Petersson J., 1996: Deuteric accessory phases in the
Bohus granite, SW Sweden. GFF 118 Jubilee Issue.
Finger F., Broska I., Roberts M.P. & Schermaier A., 1998: Re-
placement of primary monazite by apatite-allanite-epidote co-
ronas in an amphibolite facies granite gneiss from the Eastern
Alps. Amer. Mineralogist, 83, 34, 248258.
Franz G., Andrehs G. & Rhede C., 1996: Crystal chemistry of monazite
and xenotime from Saxothuringian-Moldanubian metapelites, NE
Bavaria, Germany. Eur. J. Mineral., 8, 10971118.
Gromet L.P. & Silver L.T., 1983: Rare earth element distributions
among minerals in a granodiorite and their petrogenetic im-
plications. Geochim. Cosmochim. Acta, 47, 5, 925940.
Hrako ¼., Bezák V. & Molák B., 1997: Postorogenic peraluminous
two-mica granites and granite-porphyries in the Kohút Zone of
the Veporicum Unit (KlenovecZlatno area). Miner. slovaca,
29, 113135 (in Slovak, English abstract).
Janák M., Plaienka D., Schmidt S.T. & Frey M., 1997: Cretaceous
tectonometamorphic evolution of the Veporicum core com-
plex (Western Carpathians, Slovakia). In: Deformation mech-
anisms in nature and experiment. International Conference
Basel 17. 19. March 1997.
Kováèik M., Krá¾ J. & Maluski H., 1996: Metamorphic rocks in
the Southern Veporicum basement: their Alpine metamor-
phism and thermochronologic evolution. Miner. slovaca, 28,
185202 (in Slovak, English summary).
Krá¾ J., Frank W. & Bezák V., 1996: Hornblende
from the hornblende-bearing rocks of the Veporic unit. Miner.
slovaca, 28, 501513 (in Slovak, English summary).
Lee D.E. & Dodge F.C.W., 1964: Accessory minerals in some gra-
nitic rocks in California and Nevada as a function of Calcium
content. Amer. Mineralogist, 49, 16601670.
Lyakhovich V.V., 1968: Trace elements in the granitoid accessory
minerals. Nedra, 1309 (in Russian).
Maluski H., Rajlich P. & Matte P., 1993: Ar
dating of the In-
ner Carpathian Variscan basement and Alpine mylonitic over-
printing. Tectonophysics, 223, 313337.
Méres . & Hovorka D., 1991: Alpine metamorphic recrystalization
of the pre-Carboniferous metapelites of the Kohút crystalline
complex (the Western Carpathias). Miner. slovaca, 23, 435442.
Mohr D.W., 1984: Zoned porphyroblasts of metamorphic monazite
in the Anakeesta Formation, Great Smoky Mountains, North
Carolina. Amer. Mineralogist, 69, 98103.
Montel J.M., 1993: A model for monazite/melt equilibrium and
application to the generation of granitic magmas. Chem.
Murata K.J., Rose H.J.jr, Carron, M.K. & Glass J.J., 1957: Sys-
tematic variation of rare-earth elements in cerium-earth min-
erals. Geochim. Cosmochim. Acta, 11, 141161.
Overstreet W.C., 1967: The geologic occurrence of monazite.
Geol. Surv. Prof. Pap., 530, 1327.
Parrish R.R., 1990: U-Pb dating of monazite and its aplication to
geological problem. Canad. J. Earth Sci., 27, 14311450.
Peindl, 1990: Variszische und alpidische Entwicklungs gesichte
des südöstlichen Raabalpenkristallins Steiermark. Unpub-
lished. PhD. theses Univ. Graz, 252
Petrík I., Broska I. & Uher P., 1994: Evolution of the Western Car-
pathian granite magmatism: age, source rock, geotectonic set-
ting and relation to the Variscan structure. Geol. Carpathica,
Petrík I. & Broska I., 1994: Petrology of two granite types from the
Tríbeè Mountains, Western Carpathians: an example of allanite
(+magnetite) versus monazite dichotomy. Geol. J., 29, 5978.
THE BREAKDOWN OF MONAZITE IN THE WEST- CARPATHIAN VEPORIC ORTHOGNEISSES 167
Petrík I. & Kohút M. (in press): The evolution of granitoid mag-
matism during the Variscan orogen in the Western Car-
pathians. In: Grecula P., Hovorka D., Plaienka D. & Puti M.
(Eds.): The Variscan and the Alpine evolution of the Western
Carpathians. GS SR, Bratislava.
Plaienka D., 1993: Brief outline of the West Carpathian structure
with an emphasis on the Mesozoic evolution. In: Pitonák P. &
Spiiak J., (Eds.): PAEWCR conference, Excursion guide,
Stará Lesná, 310.
Plaienka D., Janák M., Frey M. & Schmidt S.T., 1997: Structural
and metamorphic evolution of a Cretaceous core complex: the
Veporic superunit of the Central Western Carpathians (Slova-
kia). EUG 9 Abstracts, Starssbourgh, 158.
Poller U., Todt U., Janák M. & Kohút M., 1997: Pre-Variscan or-
thogneisses of the Western Tatra mountains: U-Pb single zircon
data by cathodoluminiscence controled dating (CLC-dating).
EUG 9, Abstracts, Starsbourgh, 488.
Read D., Cooper D.C. & McArthur J.M., 1987: The composition
and distribution of nodular monazite in the Lower Palaeozoic
rocks of Great Britain. Mineral. Mag., 51, 271280.
Siman P., Johan V., Ledru P., Bezák V. & Madarász J. 1996a: Defor-
mation and p-T conditions estimated in layered migmatites
from southern part of Veporicum crystalline basement (Western
Carpathians; Slovakia). Slovak Geol. Mag., 34, 209213.
Siman P., Madarász J., Kováèik M., Schulmann K. & Ledru P.,
1996b: Petrogenetic relationship between deformation and al-
teration on the example of the extension tectonics of the Ve-
poricum crystalline basement (Central Western Carpathians).
Slovak Geol. Mag., 34, 175178.
Smith H. A. & Barreiro B., 1990: Monazite U-Pb dating of stauro-
lite grade metamorphism in pelitic schists. Contr. Mineral.
Petrology, 105, 602615.
Snetsinger K.D., 1967: Accessory minerals in some Sierra Nevada
granitic rock as a function of calcium content. Amer. Mineral-
ogist, 52, 832842
Yeskova E.M. & Ganzeyev A.A., 1964: Rare earth elements in the
accessory minerals. Geochimija, 12671279 (in Russian).
Ward C.D., McArthur J.M. & Walsh J.N., 1992: Rare earth element
behaviour during evolution and alteration of the Dartmoor
granite, SW England. J. Petrology, 33, 4, 785815.