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, FEBRUARY 2015, 66, 1, 19—36 doi: 10.1515/geoca-2015-0008
Intensive low-temperature tectono-hydrothermal overprint
of peraluminous rare-metal granite: a case study from the
Dlhá dolina valley (Gemericum, Slovakia)
KAREL BREITER
1
, IGOR BROSKA
2
and PAVEL UHER
3
1
Institute of Geology, Czech Academy of Sciences, v.v.i., Rozvojová 269, CZ-16500 Praha 6, Czech Republic; breiter@gli.cas.cz
2
Geological Institute of the Slovak Academy of Sciences, Dúbravská 9, 840 05 Bratislava, Slovak Republic; geolbros@savba.sk
3
Department of Mineralogy and Petrology, Faculty of Natural Sciences, Comenius University, Mlynská dolina G, 842 15 Bratislava,
Slovak Republic; puher@fns.uniba.sk
(Manuscript received June 4, 2014; accepted in revised form December 10, 2014)
Abstract: A unique case of low-temperature metamorphic (hydrothermal) overprint of peraluminous, highly evolved
rare-metal S-type granite is described. The hidden Dlhá dolina granite pluton of Permian age (Western Carpathians,
eastern Slovakia) is composed of barren biotite granite, mineralized Li-mica granite and albitite. Based on whole-rock
chemical data and evaluation of compositional variations of rock-forming and accessory minerals (Rb-P-enriched
K-feldspar and albite; biotite, zinnwaldite and di-octahedral micas; Hf-(Sc)-rich zircon, fluorapatite, topaz, schorlitic
tourmaline), the following evolutionary scenario is proposed: (1) Intrusion of evolved peraluminous melt enriched in
Li, B, P, F, Sn, Nb, Ta, and W took place followed by intrusion of a large body of biotite granites into Paleozoic
metapelites and metarhyolite tuffs; (2) The highly evolved melt differentiated in situ forming tourmaline-bearing
Li-biotite granite at the bottom, topaz-zinnwaldite granite in the middle, and quartz albitite to albitite at the top of the
cupola. The main part of the Sn, Nb, and Ta crystallized from the melt as disseminated cassiterite and Nb-Ta oxide
minerals within the albitite, while disseminated wolframite appears mainly within the topaz-zinnwaldite granite. The
fluid separated from the last portion of crystallized magma caused small scale greisenization of the albitite; (3) Alpine
(Cretaceous) thrusting strongly tectonized and mylonitized the upper part of the pluton. Hydrothermal low-temperature
fluids enriched in Ca, Mg, and CO
2
unfiltered mechanically damaged granite. This fluid-driven overprint caused forma-
tion of carbonate veinlets, alteration and release of phosphorus from crystal lattice of feldspars and Li from micas,
precipitating secondary Sr-enriched apatite and Mg-rich micas. Consequently, all bulk-rock and mineral markers were
reset and now represent the P-T conditions of the Alpine overprint.
Key words: rare-metal granite, low-temperature overprint, Western Carpathians, Slovakia.
Introduction
Huge number of ore-bearing granitic systems of different
geochemical types (S-, A-, I-type) have been described
through the world and many genetic models and strategies
for the detection of hidden Sn-W and Ta-bearing mineral de-
posits were proposed (Beus & Zalashkova 1962; Koval
1975; Kovalenko & Kovalenko 1976; Frolov 1978; Taylor &
Strong 1985; Tischendorf et al. 1989; Lehmann 1990; Štem-
prok 1993; Seltmann et al. 1994; Štemprok et al. 1994; Haa-
pala 1995; Breiter et al. 1999; Jarchovský 2004; Bastos Neto
et al. 2009; Küster 2009; Solomovich et al. 2012). The ma-
jority of ore-bearing objects examined in detail are preserved
in their “primary” high-temperature magmatic to early hy-
drothermal stage which involves magmatic crystallization
and the complex of immediately following relatively high-
temperature “autometasomatic” processes, like feldspatization
and greisenization. Sn-W granite-related mineral deposits/
occurrences which underwent HP—HT (high pressure—high
temperature) regional metamorphism have only rarely been
described. The examples include Cetoraz (Němec & Páša
1986) and Kovářová near Nedvědice (Losos & Vižda 2006),
both in the Moldanubian block of the Bohemian Massif,
Czech Republic.
In this study, a unique case of LT (low-temperature) meta-
morphic (tectono-hydrothermal) overprint of ore-bearing Li,
P, F, Sn, W, Nb, Ta-rich, rare-metal S-type granite is de-
scribed. The hidden Permian granite occurring in the Dlhá
dolina valley (Western Carpathians, Gemeric Superunit,
eastern Slovakia) underwent intensive Alpine (Cretaceous)
overprint (Radvanec et al. 2004; Petrasová et al. 2007).
However, the chemical composition of the rock-forming and
indicative accessory minerals from the Li-bearing granites
discovered by drilling in 1980 located in Dlhá dolina are still
insufficiently characterized (Dianiška et al. 2002). The
neighbouring Li-bearing granites from the Surovec body and
Vrchsútová contain Li-rich phengitic mica which was formed
during Alpine metamorphism from primary zinnwaldite series
and muscovite (Petrík et al. 2014). We evaluate compositional
variations of the rock-forming and accessory minerals in the
context of bulk-rock vertical chemical zoning of the Dlhá do-
lina granite body, in comparison with a wide range of world-
wide rare-metal granites, as important potential sources of
critical metals, such as Sn, Nb, Ta, Li and W.
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Geological setting and sampling
Geological background
Within the Western Carpathians, the rare-metal granites
are developed only in the Gemeric Superunit as co-called
specialized S-type granites due to their special ore-bearing,
Li-Sn-W-Nb-Ta mineralization (Uher & Broska 1996). The
first outcrop of tin mineralization in the granites was detected
near the Hnilec village (e.g. Baran et al. 1970, 1971; Drnzí-
ková et al. 1975). Hidden P, F, Li, Nb, Ta, Sn-rich granite
represents a strongly fractionated small granite pluton com-
posed of barren biotite granite, mineralized Li-mica granite
and albitite. The granite was discovered in the Dlhá dolina
valley close to the village of Gemerská Poloma (Fig. 1) on
the basis of heavy mineral prospection (Tréger & Matula
1977). About twenty inclined exploration boreholes were re-
alized to recognize the shape and composition of the pluton
(Malachovský et al. 1983, 1992). Among them, the 912.9 m
long hole DD-3 was the deepest and this work describes the
main geochemical findings from this drillhole.
The Dlhá dolina pluton was emplaced within the inten-
sively folded Lower Paleozoic volcano-sedimentary com-
plex of the Vlachovo Formation, metamorphosed in the
greenschist-facies during Variscan orogeny (Carboniferous).
Moreover, the granites and metamorphic rocks were over-
printed by Alpine (Cretaceous) regional metamorphism,
which reached ~ 600 to 700 MPa and ~ 400 °C (Petrasová et
al. 2007). The country rocks composed mainly of phyllites,
metarhyolites and their metapyroclastic equivalents as well
as layers or lenses of coarse-grained metadolomites and
strongly steatitized magnesites with a talc deposit near Gemer-
ská Poloma (Kilík 1997; Petrasová et al. 2007; Vozárová et
al. 2010). The U-Pb SHRIMP dating of zircon from the
Fig. 1. Simplified map of the studied area. 1 – specialized S-type granite bodies (a – Podsútová, b – Hnilec, c – Delava, d – Surovec,
e – Betliar), 2 – undistinguished Paleozoic metamorphic rocks of the Gemeric Superunit (phyllites, metasandstones, metavolcanics),
3 – metarhyolite tuffs, 4 – phyllites, 5 – Veporicum (paragneisses, granitoids), 6 – Silicicum (limestone, dolomite; Lower Triassic to Upper
Jurassic), 7 – Meliaticum (Late Permian to Upper Jurassic), 8 – Sediments of Inner Carpathians, 9 – Quaternary sediments with streams.
Fig. 2. Cross-section through the borehole DD-3, in the Dlhá dolina
pluton (acc. to Malachovský et al. 1992, strongly modified).
metamorphosed rhyolitic rocks of the Vlachovo Formation
gave Late Cambrian age (494 ± 1.6 Ma – Vozárová et al.
2010). According to the drilling survey (Malachovský et al.
1992), the hidden Dlhá dolina granite pluton forms a NE-SW
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oriented, 2 km long and 200 to 1000 m wide granite body (di-
mensions at sea level). The actual shape of the pluton is deter-
mined through multiple NE-SW trending, to the SE inclined,
local Alpine thrusting. The original upper contact of the plu-
ton was probably generally flat with two cupolas with diame-
ters of about 500 m rising about 200 m above the entire
pluton. The SW-cupola, cut by the borehole DD-3 (Fig. 2),
had more steep contacts and its upper part was filled by albi-
tite, while within the more flat-shaped NE cupola only mild
greisenization took place (Malachovský et al. 1992).
The age of the granite intrusion is probably similar to that
of the nearest outcropping Hnilec granite body, which is in-
terpreted on the basis of zircon U-Pb dating of granites (Poller
et al. 2002) and Re-Os in molybdenite dating of Sn-W-Mo
mineralization (Kohút & Stein 2005) as Late Permian (~ 260
to 250 Ma)
Sampling and description of granites
We studied samples from the core of the deepest DD-3
borehole located in the Dlhá dolina valley at an altitude of
800 m above see level, 1.8 km to the NW from the Volovec
hill (1212 m a.s.l.) (Fig. 1). Each sample for chemical analysis
(Table 1) consisted of several fragments (2—6 pieces, 3—5 kg
in the whole) from the macroscopically homogeneous sec-
tion of the core. Polished thin sections were prepared from
the most typical rock pieces.
The pluton is composed of two co-magmatic constituents:
the deeper suite of barren biotite granites, and the upper suite
of highly fractionated, rare-metal Li-mica granites and quartz
albitite. While the deeper suite probably forms a larger body
with generally flat upper contact, the upper suite forms cupola-
like bodies with steep contacts located between the deeper
suite and its metamorphic envelope. Alpine (Cretaceous) tec-
tonic processes (thrusting, mylonitization) affected the whole
pluton, but the intensity of deformation is highly variable.
Generally, the intensity of deformation increases upwards. In-
tact rocks, namely granites unaffected by deformation and/or
metasomatism, are preserved only in the centers of large tec-
tonic blocks. Rocks from the depth of 681 to 691 m (tourma-
line granite), 577 to 582 m (topaz granite) and 459 to 461 m
(quartz albitite) can best represent the primary magmatic stage
of this system. The principal granite types from the deepest to
the apical part of the cupola have the following succession:
consisting of subhedral K-feldspar, albite (An
08
),
quartz and partly chloritized biotite. The typical acces-
sory minerals comprise apatite, zircon, schorlitic tour-
maline and almandine garnet.
(1) Distinctly porphyritic biotite granite in the depth
of 880 to 913 m is grey coloured, composed of phe-
nocrysts of K-feldspars (up to 3 cm) and quartz (up to
1 cm) in fine-grained groundmass of K-feldspar, albite
(An
06
), quartz, and biotite, mostly altered to a mixture
of chlorite and phengitic mica. Zircon, apatite, il-
menite, rutile and tourmaline are characteristic acces-
sory mineral phases. Many tectonic planes are covered
by secondary chlorite and phengitic muscovite.
(2) Slightly porphyritic biotite granite in the depth
of 720 to 880 m is pink-coloured and composed of
phenocrysts of twinned K-feldspars (up to 15 mm) and
quartz (up to 8 mm) in medium-grained groundmass
The upper intrusive suite (Li-mica granites)
(3) Li-biotite granite with tourmaline (hereinafter
tourmaline granite) forms the lower part of the ore-
bearing intrusion in the depth of 620 to 720 m. This is
grey, coarse to medium grained (3—8 mm) leucogran-
ite, composed of albite (An
04
), K-feldspar, quartz and
Li-Fe mica. Black tourmaline (schorl) forms common
disseminated grains ( < 1 mm) and occasionally aggre-
gates up to 15 mm in size. The K-feldspar locally
forms phenocrysts up to 12 mm in size. Accessory
phases are apatite, zircon, monazite, xenotime, wol-
framite, wolframixiolite, columbite, cassiterite, ura-
ninite, thorite, goyazite, fluorite, etc. Upwards the
tourmaline granite gradually changed into topaz granite.
(4) Zinnwaldite granite with topaz (hereafter topaz
granite) forms the medium part of the intrusion at the
depth of 554 to 620 m. This part of the granite cupola
was affected with strong deformation and metasoma-
tism and only the domain at the depth of ca. 575 to
590 m is preserved in a nearly primary shape. The gran-
ite is light grey to white in colour, fine- to medium-
grained and leucocratic, composed of albite (An
02
),
P-enriched K-feldspar, snow-ball textured quartz, and
zinnwaldite. Zircon, apatite, fluorite, monazite, xeno-
time, Nb-rich wolframite (mainly ferberite), columbite-
group minerals, W-rich ixiolite-like phase, ilmenite,
cassiterite, uraninite, and Bi-sulfosalts occur among
the accessory minerals. Some discontinuity planes are
coated with fluorite. The uppermost part of this unit (in
depth of 555 to 575 m) is strongly mylonitized.
(5) Quartz albitite to albitite (hereinafter albitite)
forms the uppermost part of the cupola at the depth of
454 to 554 m. This rock type is usually hololeucocratic,
fine- to medium-grained, composed of albite (An
01
),
quartz and K-feldspar in highly variable amounts
(Ab > Qtz > >Kfs). The modal content of albite varies in
the range 50—90 vol. %, mostly 70—90 vol. %. In some
parts, apatite and/or muscovite are present as major
constituents. Intercalations of K-feldspar- and mica-
enriched facies in the depth of 490 to 495 m approach
the composition of topaz granite. Some parts of the al-
bitite body were silicified and these quartz ( + apatite)
enriched domains were originally described as “greis-
ens” (Malachovský et al. 1992). The genesis of these
quartz-rich rock and real extension of high-tempera-
ture metasomatism ( = greisenization) remains ques-
tionable, due to strong mylonitization. In zones of
intensive mylonitization, feldspars were replaced by a
young generation of quartz and phengitic mica. Dis-
seminated cassiterite, Nb-Ta oxide minerals (ferro-
columbite to manganocolumbite, Nb-Ta-rich rutile)
and U-phases (uraninite, brannerite) were found
through the whole albitite body without specific rela-
tion to the silicified areas.
The deeper intrusive suite (biotite granites)
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Analytical methods
Whole-rock analyses
The major element analyses were performed by wet tech-
nique at the Czech Geological Survey, Praha. The control
analyses of the international whole-rock reference materials
yield a total error (1-sigma) of ± 0.5 %. Trace element analy-
ses were obtained in the ACME Labs, Vancouver, using
ICP-MS method after melting with lithium borate.
Cathodoluminescence (CL)
The CL images of the selected samples were obtained us-
ing a microscope HC2-LM (Lumic), accelerating voltage
14 kV, and current density 10—40 µA/mm
2
. The images were
captured with an Olympus C-5060 digital camera (setting:
ISO 400, exposure time 1—10 sec) at the Department of Geo-
logical Sciences, Masaryk University, Brno, Czech Republic.
EMPA analyses of minerals
Silicate minerals and apatite were analysed using a CAM-
ECA SX100 electron microprobe in the Geological Institute,
Czech Academy of Science in Praha, at an accelerating
voltage and beam current of 15 kV and 10 nA, respectively,
and with a beam diameter 2 µm. The following standards
were used: P – apatite, Si, Mg, Ca – diopside, Ti – rutile,
Al, Na, – jadeite, Fe – magnetite, Mn – MnCr
2
O
4
,
Ba – BaSO
4
, K – leucite, Rb – RbCl and F – fluorite.
Zircon was analysed using a CAMECA SX100 electron mi-
croprobe at the Dionýz Štúr State Geological Institute, Bratis-
lava, using accelerating voltage of 15 kV and sample current
of 40 nA. The following standards were used for calibration:
P and Ca – apatite, As—GaAs, Nb – ferrocolumbite, Si and
Zr – zircon, Hf—HfO
2
, Th—ThO
2
, U—UO
2
, Al—Al
2
O
3
Sc—ScPO
4
, Y—YPO
4
, La—LaPO
4
, Ce—CePO
4
, Pr—PrPO
4
,
Nd—NdPO
4
, Sm—SmPO
4
, Eu—EuPO
4
, Gd—GdPO
4
, Tb—TbPO
4
,
Dy—DyPO
4
, Ho—HoPO
4
, Er—ErPO
4
, Tm—TmPO
4
, Yb—YbPO
4
,
Lu—LuPO
4
, Fe – fayalite, and Mn – rhodonite. We used em-
pirically determined correction factors applied to the follow-
Table 1: Studied samples from the borehole DD-3 Dlhá dolina.
ing line overlaps: Th
→U, Dy→Eu, Gd→Ho, La→Gd,
Ce
→Gd, Eu→Er, Gd→Er, Sm→Tm, Dy→Lu, Ho→Lu,
Y b
→Lu, and Dy→As. The matrix effects were corrected
using the PAP procedure.
Whole-rock geochemistry
Typical whole-rock chemical analyses are shown in Ta-
ble 2. Contents of some elements and their relations are visu-
alized in Fig. 3.
Both intrusive suites have different geochemical character-
istics. The lower suite of biotite granites, although variable
in texture, is chemically homogeneous. It is slightly peralu-
minous (ASI=1.1) and alkaline (75.0—75.6 wt. % SiO
2
,
12.2—13.1 wt. % Al
2
O
3
, 0.6 wt. % CaO, 2.8—3.2 wt. % Na
2
O,
4.8—5.3 wt. % K
2
O) with low contents of fluxing elements
(about 0.01 wt. % Li
2
O, 0.12—0.14 wt. % P
2
O
5
, 0.2 wt. % F).
The contents of trace elements (425—459 ppm Rb,
20—31 ppm Sr, 10—11 ppm Nb, 24—30 ppm Sn, 73—93 ppm Zr,
21—30 ppm Ce and 24—30 ppm Y) are comparable with other
biotite and two-mica granites in the Gemeric Superunit,
especially in its western part (Hnilec area – Broska &
Uher 2001).
The upper ore-bearing intrusive suite as a whole shows a
much higher grade of geochemical specialization. In com-
parison with the foregoing biotite granites, the Li-mica gran-
ites are depleted in Si, Ti, Fe, K, Zr, Y, REE, and enriched in
Al, Na, Li, P, F, Cs, Ga, Nb, Rb, Sn, Ta, and W. The con-
tents of Fe, Mg, Ca, Ba, Sr, U, and Th are scattered and
strongly influenced by late processes. Going from the lower
tourmaline- to the upper topaz-bearing facies, the content of
Si decreases (73 to 71 wt. %), while contents of other index
elements increase: P (0.3 to 0.6 wt. % P
2
O
5
), F (0.5 to
1.5 wt. % F), Li (0.05 to 0.3 wt. % Li
2
O), Nb (22 to 63 ppm),
and W (8 to 82 ppm).
Albitite in the uppermost part of the cupola is rich in Na (up
to 9.4 wt. % Na
2
O), Ga (ca. 50 ppm), Sn (400—900 ppm),
Ta (40—95 ppm) and poor in K (0.5—1.8 wt. % K
2
O), F (ca.
0.1 wt. %), and Rb (87—118 ppm). Secondary processes (silic-
ification, mylonitization, sericitization, carbonatization) are
Sample No.
Depth (m)
Unit
Description
3626
459.0–461.6
Upper intrusive suite, albitites
Quartz albitite
3627
471.2–473.4
Slightly silicified albitite
3628
487.0–489.0
Strongly silicified (greisenized) and mylonitized albitite
3629
489.0–490.5 Apatite-rich
albitite
3630
504.2–507.7 Mylonitized
albitite
3631
559.0–561.7
Upper intrusive suite, Li-mica granites
Mylonitized topaz granite
3632
569.8–574.0
Mylonitized topaz granite
3633
577.4–582.4
Topaz granite, without alteration
3634
594.9–597.8
Mylonitized topaz granite
3635
607.9–611.4
Mildly mylonitized topaz granite
3636
627.4–633.9 Sericitized
tourmaline
granite
3637
657.9–664.0 Sericitized
tourmaline
granite
3638
681.6–691.5 Tourmaline
granite
3639
783.3–787.7
Deeper intrusive suite, biotite granites
Biotite granite
3640
870.2–873.8 Biotite
granite
3641
908.2–910.9 Porphyritic
biotite
granite
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Table 2: Bulk-rock chemical analyzes of studied granitoids (wt. %, trace elements in ppm).
responsible for local increase of Si (up to 79.7 wt. % SiO
2
),
Mg (up to 0.87 wt. % MgO), Ca (up to 1.37 wt. % CaO),
P (up to 0.80 wt. % P
2
O
5
), and Sr (up to 153 ppm).
Mineralogy
Feldspars
Biotite granites contain perthitic K-feldspar (Ab
04
, max.
0.14 wt. % BaO, Rb-free) in association with slightly zoned
altered albite (An
03—08
). The K-feldspar is locally enriched in
phosphorus (max. 0.4 wt. % P
2
O
5
, 0.015 apfu P), while albite
is P-free (Table 3).
Li-mica granites contain pure albite (An
00—01
) and Ba-free
perthitic K-feldspar (Ab
02
). The content of Rb in Kfs increases
upwards from 0.1 wt. % Rb
2
O in tourmaline granite to ca.
0.4 wt. % Rb
2
O (0.013 apfu Rb) in topaz granite and is not
influenced by the low-temperature alteration. In contrast, the
primary high content of phosphorus in both feldspars is pre-
served only rarely in the core of some grains (up to
0.54 wt. % P
2
O
5
in Kfs and 0.30 wt. % P
2
O
5
in albite). The
majority of feldspar grains are actually P-free, but contain
plenty of µm-sized inclusions of secondary apatite.
Rock
Quartz
albitite
Silicified and
mylonitized
albitite
Mylonitized
topaz granite
Topaz
granite
Tourmaline
granite
Biotite
granite
Porphyritic
biotite granite
Sample
3626
3628
3631
3633
3638
3640
3641
SiO
2
72.81
79.69
69.21
71.68
73.24
74.96
75.57
TiO
2
0.01
0.02
0.02
0.03
0.06
0.10
0.14
Al
2
O
3
15.80
11.33
16.30
15.66
14.11
13.06
12.21
Fe
2
O
3
0.05
0.263
0.27
0.18
0.46
0.44
0.82
FeO
0.09
0.33
0.45
0.51
0.58
0.83
1.19
MnO
0.005
0.021
0.037
0.050
0.022
0.037
0.056
MgO
0.14
0.66
1.66
0.02
0.26
0.16
0.18
CaO
0.43
0.87
1.81
0.72
0.70
0.56
0.56
Li
2
O
0.005
0.018
0.021
0.282
0.050
0.010
0.012
Na
2
O
9.37
0.92
1.54
4.13
3.57
3.22
2.85
K
2
O
0.61
3.46
4.94
4.36
4.66
5.26
4.87
P
2
O
5
0.30
0.52
0.45
0.49
0.27
0.12
0.12
F
0.08
0.31
0.29
1.38
0.48
0.18
0.21
LOI
0.46
1.74
3.41
1.15
1.08
0.92
0.89
H
2
O–
0.04
0.06
0.07
0.05
0.06
0.03
0.04
Total
100.17
100.08
100.35
100.11
99.4
99.81
99.62
ASI
0.94
1.66
1.46
1.22
1.16
1.09
1.11
Nb/Ta
1.0
1.4
2.9
3.3
2.9
4.0
4.8
Zr/Hf
6.3
6.0
9.0
10.5
19.9
24.5
28.2
Ba
15
47
40
58
96
84
81
Be
1
2
2
2
6
7
6
Cs
3.9
26
51
74
52
14
20
Ga
51
25
45
40
27
20
20
Hf
4.8
4.5
2.7
2.4
2.9
3
3.3
Nb
70
138
83
601
22
9.7
10
Rb
100
744
1209
1698
802
459
436
Sn
654
926
198
92
57
25
24
Sr
52
118
57
187
24
20
22
Ta
71
96
29
189
7.6
2.4
2.1
Th
6.5
8.2
6.9
9.4
11
14
15
U
21
26
24
24
26
17
19
W
4.3
13
8
82
8.4
6.1
5.5
Zr
30
27
24
25
58
73
93
Y
0.4
1.3
2.3
5
17
24
30
La
0.2
0.5
1.2
0.6
5.4
9.2
12.9
Ce
0.4
0.9
2.5
2.1
12.3
21.4
30.2
Pr
0.06
0.14
0.31
0.31
1.53
2.59
3.67
Nd
<0.3
0.6
1.2
1.3
5.5
8.9
13.4
Sm
0.09
0.29
0.45
0.69
1.84
2.6
3.44
Eu
0.05
0.08
0.16
<0.02
0.07
0.15
0.2
Gd
0.11
0.38
0.41
0.6
1.96
2.65
3.6
Tb
0.02
0.07
0.08
0.19
0.5
0.62
0.81
Dy
0.08
0.31
0.36
0.93
3.18
4.09
5.26
Ho
<0.02
0.05
0.05
0.12
0.58
0.84
1.09
Er
0.04
0.12
0.17
0.36
1.63
2.61
3.24
Tm
<0.01
0.02
0.03
0.07
0.27
0.44
0.52
Yb
<0.05
0.1
0.28
0.56
1.71
3.04
3.49
Lu
<0.01
0.02
0.04
0.07
0.23
0.44
0.49
24
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Fig. 3. Harker diagrams and chondrite normalized REE patterns of the Dlhá dolina granitic rocks. The atomic Zr/Hf-value (x-axis) is the most
stable indicator of magma fractionation in the case of altered rocks. For comparison, representative analyses of Hnilec granites (unpublished
data by I. Broska), Surovec granites (Petrík et al. 2011) and pure magmatic rare-metal granites from the Podlesí, western Krušné hory/Erzge-
birge, Czech Republic (unpublished data by K. Breiter) are shown. a – Zr/Hf vs. Al
2
O
3
, b – Zr/Hf vs. P
2
O
5
, c – Zr/Hf vs. F, d – Zr/Hf
vs. Li
2
O, e – Zr/Hf vs. Rb, f – Zr/Hf vs. Ta, g – Zr/Hf vs. Sn, h – chondrite normalized REE patterns. HREE in the albitite are lower
than the detection limits of ICP-MS. Chondrite values according to Mc Donough & Sun (1995).
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Albitite contains only pure albite (An
< 01
). Like
the Li-mica granite, this albite equilibrated with
hydrothermal fluids and contains numerous inclu-
sions of secondary apatite. Some grain cores con-
tain max. 0.4 wt. % P
2
O
5
(0.015 apfu P).
Micas
Micas originated in all episodes of granite evo-
lution: magmatic crystallization, high-temperature
alteration (greisenization), and low-temperature
Alpine overprint. The later processes have not
only produced a new population of mica, but also
re-equilibrated mica grains crystallized during the
earlier episode, so the micas represent genetically
the most complicated mineral group.
The most important signature of the magmatic
micas is, along with their texture, relatively high
contents of F, Li, and Rb. While it is not techni-
cally possible to analyse Li using the electron
microprobe, high contents of F and Rb are the
most important indicators of the magmatic ori-
gin of a particular mica. Biotite from the deeper
intrusive suite is poor in Mg (#Mg 0.25—0.30)
and Rb (0.10—0.14 wt. % Rb
2
O) and free of fluo-
rine ( < 0.1 wt. % F) (Fig. 4, Table 4). Associated
Fe-dominant chlorite (chamosite) is relatively
slightly Mg-depleted (#Mg 0.15) in comparison
with the biotite.
In the whole body of tourmaline and topaz
granites, only the sample from the depth of
ca. 580 m contains mica, which can be consid-
ered as primary magmatic mica. This zin-
nwaldite forms typical bright brownish flakes
0.5 mm in size containing inclusions of zircon
and ore minerals. The fresh cores are relatively
rich in Fe (9.4 wt. % FeO, 1.15 apfu Fe),
Rb (up to 1.5 wt. % Rb
2
O, 0.14 apfu Rb) and
F (up to 7.7 wt. % F, 3.7 apfu F), while slightly
altered rims are enriched in Al (up to 24 wt. %
Al
2
O
3
, 4.0 apfu Al) and depleted in all the afore
mentioned
elements
(6.1—7.0 wt. % FeO,
0.13—0.78 wt. % Rb, 4.7—5.9 wt. % F). Contents
of SiO
2
are scattered between 48.5—49.4 wt. %
(7.0—7.4 apfu Si). Using the published equations
for correlation between contents of Li and Si,
Li-contents in the mica cores should be ca.
3.8—4.0 wt. % Li
2
O ( ~ 2.2 apfu Li – Breiter et
al. 2005) or 4.8—5.0 wt. % Li
2
O ( ~ 2.7 apfu
Li – Tischendorf et al. 1999). According to
bulk-rock Li-contents, the lower values seem to
be more realistic.
The micas from all other samples from the
“Li-mica granites” are to variable degrees al-
tered: enriched in Al (30—32 wt. % Al
2
O
3
), Mg
(up to 1.9 wt. % MgO), and depleted in Fe (4.3
to 0.3 wt. % Fe), Rb ( < 0.3 wt. % Rb
2
O), and F
( < 2.4 wt. % F). This mica should be termed as
phengitic muscovite.
Table 3:
Representative
compositions
(in
wt. %)
and
empirical
formulae
(based
on
8
oxygen
atoms)
of
alkali
feldspars.
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Fig. 4. Diagrams of mica composition (recalculated on the basis of 22 atoms of oxygen). a – Diagram Si vs. Fe+Mg+Mn shows different
trends in magmatic micas from the Nejdek-Podlesí pluton, Czech Republic (unpublished data by K. Breiter) and low-temperature altered
micas from the Dlhá dolina pluton. For comparison, published analyses of micas from near Surovec and Dlhá dolina granites (Petrík et al.
2011, 2014) are also shown. b – Diagram Fe vs. Mg in micas documents depletion in Fe and enrichment of Mg during Alpine LT alter-
ation of the Dlhá dolina and Surovec granites. Rare phlogopite (4.0—4.5 apfu Mg) found in the mylonitized albitite do not match the field of
this diagram. Remember, these diagrams are not IMA-classification diagrams of micas.
Zircon
It forms euhedral to subhedral crystals, usually 50 to 150 µm
in size, scattered in quartz, albite and muscovite. The crystals
are commonly partly to totally metamict, in some cases with
tiny inclusions or intergrowths of xenotime-(Y), ThSiO
4
phase
(thorianite or huttonite), uraninite, cassiterite, and (W)-Nb-Ta
oxide minerals (Fig. 5). Composition of zircon strongly de-
pends on the fractionation degree of parental granitic rock: con-
centrations of Hf and Sc generally increase from less fraction-
ated biotite granites to the most fractionated topaz-zinnwaldite
granite and quartz albitite or from core to rim (Table 5).
The HfO
2
content and Zr/Hf wt. ratio attain 1.4—4.1 wt. %
and 38—13 in biotite granites, 2.0—2.6 wt. % and 30—20 in tour-
maline granite, 3.3—13 wt. % and 14.5—3.5 in topaz granite, and
6.6—12 wt. % and 7.9—4.0 in albitite, respectively (Fig. 6a).
Fig. 5. BSE photomicrographs of zircon from the Dlhá dolina granites. a – Elongated zircon crystal with inclusions of fluorapatite (anhedral
black), xenotime (larger white) and thorite/huttonite (smaller white), biotite granite (sample 3641); b – Zircon crystals (dark grey) with xeno-
time intergrowths (pale grey) and thorite/huttonite (white), tourmaline granite (sample 3638); c – Zircon crystal (dark grey) with ferrocolum-
bite (pale grey) and W-rich ixiolite/columbite phase (white), tourmaline granite (sample 3638); d – Euhedral zircon crystal with diffuse
zoning, mylonitized topaz granite (sample 3634); e – Zircon crystals and intergrowths of uraninite + ferrocolumbite + microlite phase (white)
in muscovite, mylonitized topaz granite (sample 3634); f – Zircon (grey) with numerous tiny inclusions of uraninite, rarely cassiterite (white)
in association with W-rich ixiolite/columbite phase (large white mineral, upper part of figure), topaz granite (sample 3633).
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Table 4:
Representative
compositions
(in
wt. %)
and
empirical
formulae
(based
on
22
oxygen
atoms)
of
micas.
Contents
of
Li
2
O
were
calculated
only
in
primary
magmatic
Mg-free
micas
according to algorithms by
Breiter et al. (2002).
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Table 5:
Representative
compositions
of
zircon
(in
wt. %,
contents
of
La,
Pr,
Nd,
Sm,
Eu,
Tb,
Ho,
Tm,
Lu,
and
Mn
are
under
detection
lim
it
of
EMPA).
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Fig. 6. Chemical composition of zircon from Dlhá dolina granites in atoms per formula unit. a – Zr vs. Hf, b – Zr/Hf vs. Sc, c – Zr/Hf
vs. P, d – Zr/Hf vs. As.
In both suites contents of Sc increased upwards, while con-
tents of Y decreased: from 0.0—0.2 to 0.1—0.7 wt. % Sc
2
O
3
and
0.2—1.6 to 0.2—0.5 wt. % Y
2
O
3
in biotite granites, and from
0.1—0.3 to 0.8—2.8 wt. % Sc
2
O
3
(Fig. 6b) and 0.5—1.0 to
0.0-0.6 wt. % Y
2
O
3
in Li-mica granites. However, zircon from
the topaz granite occasionally shows irregular Y, HREE-rich
zones with 1 to 2 wt. % Y
2
O
3
. Contents of REEs in zircon are
generally low to moderate, heavy REE (HREE – Gd to Lu)
apparently prevail over light REE (LREE – La to Eu), at-
taining 0.3 to 1 wt. % HREE
2
O
3
in all studied granite types.
The contents of phosphorus attain 0.1 to 3.8 wt. % P
2
O
5
(up to 0.1 apfu P, Fig. 6c), it positively correlates with triva-
lent A-site cations, especially Sc and Y. Moreover, zircon
from the most evolved granites reveals elevated niobium con-
centrations: up to 0.4 wt. % Nb
2
O
5
in albitite and up to
0.9 wt. % Nb
2
O
5
(0.013 apfu Nb) in topaz granite. Slightly el-
evated contents of Al (up to 0.25 wt. % Al
2
O
3
; 0.01 apfu Al),
Fe (max. 0.6 wt. % Fe
2
O
3
; 0.015 apfu Fe), Ca (up to
1.0 wt. % CaO; 0.03 apfu Ca) and Sr (max. 0.1 wt. % SrO;
0.002 apfu Sr) are characteristic mainly for the (metamic-
tized?) zircons from the topaz granite. Elevated contents of As
(up to 0.5 wt. % As
2
O
3
; 0.008 apfu As, Fig. 6d) in some zir-
cons from topaz granite and albitite may indicate reequilibra-
tion with hydrothermal fluid during greisenization.
The compositional relationships indicate a presence of
HfZr
—1
, ScP(Zr,Hf)
—1
Si
—1
, YP(Zr,Hf)
—1
Si
—1
, and especially
(Sc,Y)(P, As,Nb)(Zr,Hf)
—1
Si
—1
substitutions in the majority
of analysed zircon crystals. However, limited AlPSi
—2
, ber-
linite-type substitution could also play a role. Uranium-rich
compositions commonly show positive correlation with Fe
and Ca.
Fluorapatite
Fluorapatite in the biotite granites should be considered as
a magmatic mineral. It forms homogeneous, mostly isometric
grains, 20—50 µm across. Fluorapatite is sometimes included
in mica; in other cases it is interstitial. It is fully saturated
in fluorine and relatively poor in Mn (0.1—1.4 wt. % MnO,
up to 0.1 apfu Mn), but slightly enriched in Ce (max.
0.3 wt. % Ce
2
O
3
).
Fluorapatite within the Li-mica granites and albitite was
strongly affected by the Alpine low-temperature processes.
Individual crystals or their parts differ greatly in intensity
and colour of CL: from intensive yellow through red and
violet to yellowish-grey. The intensity of CL generally in-
creases with increasing contents of Mn, Fe, and Sr, but with-
out clear correlation to one of the above mentioned elements.
The distribution of Mn, Fe, and Sr is highly variable not only
between samples, but also within individual grains (Table 6).
Maximum contents of minor elements in fluorapatite from
Li-mica granites attain 3.0 wt. % MnO (0.22 apfu Mn),
0.6 wt. % FeO (0.05 Fe), and 1.8 wt. % SrO (0.09 apfu Sr).
Within albitite, including their silicified (greisenized) parts,
fluorapatite variegated in even broader intervals as in the
granites: 0—3.3 wt. % MnO (0.25 apfu Mn), 0—0.6 wt. % FeO
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(0.05 Fe), and up to 7.5 wt. % SrO (0.39 apfu Sr). As in Li-mica
granites, all fluorapatites are F-saturated and free of Cl and Ce.
Tiny fluorapatite grains disseminated in feldspars or filling
small cracks in older minerals show conspicuous bright yel-
low colour in CL, but they are too small to be analyzed.
Topaz
Euhedral, probably late-magmatic interstitial crystals of
topaz, up to 1 mm in size, were encountered only in the to-
paz granite. The crystals show fine oscillatory zoning and
tiny cracks filled by secondary fluorapatite. Topaz is fully
saturated in fluorine ( ~ 2.0 apfu F) and slightly enriched in
phosphorus (up to 0.2 wt. % P
2
O
5
;
≤0.005 apfu P, Table 7).
Tourmaline
Fine grains of tourmaline (max. 0.1 mm across), bluish in po-
larized light, scarcely occur in the biotite and tourmaline gran-
ites. Macroscopically black tourmaline, brownish in polarized
light, is common in the lower part of the younger intrusive
suite. It is disseminated as small individual grains or forms
aggregates up to several cm across. According to its chemical
composition, both varieties of tourmaline should be termed as
schorlitic tourmaline with Fe/(Fe + Mg) ratio between 0.60 to
0.95 and a low concentration of F (up to 0.2 wt. %) (Table 8).
Discussion
Evolution of micas in the Dlhá dolina pluton
To distinguish the primary high-temperature (Variscan) and
low-temperature (Alpine) micas and to assess the degree of
secondary overprint of the former, we examined several dia-
grams (Fig. 4a,b). Already published analyses of micas from
the Surovec granite and the Dlhá dolina topaz granite (Petrík
et al. 2011, 2014) and representative analyses of pure mag-
matic micas from the peraluminous P-F-Li rich granitic sys-
tem of Nejdek-Podlesí, western Krušné hory Mts (Breiter
2002; Breiter et al. 2005) are plotted in all diagrams for com-
parison. All micas from the DD-3 borehole are rich in alumina
containing 4.8—5.3 apfu Al (Table 4). The content of Al in the
octahedral position usually reached 3.3—3.5 apfu, which indi-
cated that most of the analysed micas are di-octahedral. The
exceptions are altered biotite from the biotite granites (Al
VI
~
3)
Table 6: Representative composition (in wt. %) and empirical for-
mulae (based on 12.5 oxygen atoms) of fluorapatite (contents of Ti,
Al, Mg, Ba, Rb, Ce, and Cl are under the detection limit of the micro-
probe). Content of F fitted to the maximum amount of
(F + Cl + OH) = 1 when overestimated by analysis.
Sample
3628 3628 3628 3641 3631
Rock
Albitite Albitite Albitite
Topaz
granite
Biotite
granite
Colour
in
CL violet red yellow yellow yellow
SiO
2
0.00 0.00 0.00 0.06 0.00
FeO
0.00 0.00 0.62 0.28 0.00
MnO
0.00 0.00 2.77 1.42 0.60
CaO
55.85 55.83 48.50 53.75 54.05
SrO
0.00 0.00 5.67 0.00 1.85
Na
2
O
0.00 0.00 0.08 0.13 0.05
K
2
O
0.00 0.00 0.00 0.13 0.00
P
2
O
5
42.82 42.51 41.20 41.94 42.08
F
3.61 3.75 3.66 3.75 3.75
F=O
–1.52 –1.62 –1.55 –1.56 –1.56
Total
100.75 100.56 100.89 99.87 100.81
Si
0.001
0.001
0.001
0.005
0.000
Fe
0.000
0.001
0.046
0.019
0.002
Mn
0.002
0.000
0.206
0.102
0.043
Ca
4.968
4.990
4.570
4.855
4.906
Sr
0.000
0.000
0.289
0.000
0.091
Na
0.000
0.000
0.013
0.021
0.008
K
0.000
0.000
0.000
0.014
0.000
P
3.010
3.002
3.067
2.993
3.018
F
0.947
0.989
1.000
1.000
1.000
SiO
2
32.37
32.58
32.33
32.39
32.56
Al
2
O
3
56.09
55.72
55.68
55.42
55.67
FeO
0.00
0.00
0.00
0.06
0.04
MnO
0.00
0.00
0.07
0.00
0.08
P
2
O
5
0.00
0.08
0.21
0.19
0.08
F
20.72
20.80
20.76
21.39
20.84
F=O
–8.76
–8.80
–8.78
–9.05
–8.81
Total
100.42
100.39
100.27
100.41
100.45
Si
0.987
0.994
0.988
0.992
0.994
Al
2.016 2.004 2.005 2.000 2.002
Fe
0.000 0.000 0.000 0.002 0.001
Mn
0.000 0.001 0.002 0.000 0.002
P
0.000 0.002 0.005 0.005 0.002
F
1.998 2.007 2.006 2.072 2.011
Table 7: Representative composition (in wt. %) and empirical for-
mulae (based on 5 oxygen atoms) of topaz from the sample 3633.
Contents of elements Ti, Mg, Ca, Ba, Rb, Na, and K in all cases
lower than detection limit 0.05 wt. %.
Rock
Tourmaline
granite
Tourmaline
granite
Biotite
granite
Biotite
granite
Sample 3638
3638
3641 3641
Colour brown brown blue blue
SiO
2
33.94
35.99
35.89
36.18
TiO
2
0.90
0.26
0.12
0.02
Al
2
O
3
28.87
29.83
30.42
34.41
FeO
18.68
12.12
14.91
13.63
MgO
0.58
4.53
3.06
1.63
MnO
0.24
0.11
0.19
0.14
CaO
0.02
0.03
0.60
0.15
Na
2
O
2.80
2.81
2.50
1.97
K
2
O
0.07
0.07
0.06
0.05
F
<0.05
0.17
<0.05
0.00
F=O
–0.06
Total
86.20
85.86
87.76
88.18
Si
5.941 6.086 6.021
5.939
Ti
0.119 0.033 0.016
0.002
Al
5.955 5.944 6.015
6.657
Fe
2.734 1.713 2.091
1.871
Mg
0.151 1.141 0.765
0.398
Mn
0.035 0.016 0.028
0.020
Ca
0.003 0.005 0.108
0.027
Na
0.951 0.922 0.814
0.626
K
0.016 0.016 0.012
0.011
F
0.000 0.089 0.000
0.000
Table 8: Representative compositions (in wt. %) and empirical for-
mulae (based on 24 oxygen atoms) of tourmaline (contents of Ba,
Rb, P, and F are under the detection limit of EMPA).
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Fig. 7. Distribution of some chemical elements in the borehole DD-3, the Dlhá dolina pluton. a – Contents of Na
2
O, K
2
O, P, and F along
the borehole DD-3 (moving average of 5 adjacent samples, computed by authors from original data of Malachovský et al. 1992); b – Cor-
relation between Na
2
O and K
2
O in rocks from the borehole DD-3 (data from Malachovský et al. 1992). The sum of the alkali oxides in
magmatic rocks ranges between 8—10 wt. %; during fractionation contents of Na
2
O generally increased, while K
2
O decreased. Decrease in
Na
2
O in some samples is caused by mylonitization (in Li-mica granites) and silicification-greisenization (in albitite).
and zinnwaldite from the “fresh” topaz granite at the depth of
580 m (Al
VI
~
2.7—2.9). The low total of divalent elements
(Fe + Mg + Mn < 1 apfu, Fig. 4a) and especially the low content
of Fe (mostly < 1 apfu) is a logical counterpart of the high
Al
VI
. The unusually high content of MgO and thus high #Mg
(atomic ratio Mg/(Mg + Fe)) of the majority of micas from the
Dlhá dolina pluton is noticeable at the first view. With the ex-
ception of the relatively less tectonically affected sample of
the topaz-zinnwaldite granite (MgO < 0.1 wt. %, #Mg < 0.05),
the MgO and #Mg are substantially higher than usual in micas
from fractionated granites or leucogranites (Fig. 4b, compare
the compilation in Tischendorf et al. 1999).
Fig. 4b summarizes the changes in chemical composition
from slightly Fe-deficient, but still F, Li-rich zinnwaldite from
the topaz granite at a depth of 580 m, the Alpine Li-rich
phengite (altered primary Li-Fe mica) from the tourmaline
granite, to Mg-enriched F-free phengite from the uppermost
strongly mylonitized part of the topaz granite and albitite.
Published data from the Dlhá dolina granites (Petrík et al.
2014) are closer to the theoretical magmatic evolution than
our data, because they analysed the tectonically least affected
parts of the borehole DD-3, while we studied samples from
the whole core to ascertain the extent of post-magmatic
changes. Summarizing all the available data, following sce-
nario of mica evolution can be proposed:
! The deeper suite of biotite granites: primary annite was
partially chloritized and/or muscovitized. Timing of the al-
teration (post-magmatic vs. Alpine) is not clear;
! The upper suite, tourmaline granite: primary Li-mica
(protolithionite?) was partially muscovitized (Li, Fe, F-de-
creased), but not enriched in Mg;
! The upper suite, topaz granite: primary zinnwaldite is
preserved in tectonically undeformed domains. In deformed
parts, the mica was muscovitized (Li, F, Fe-decreased) pro-
ducing Li-rich phengite from the surface of mineral grains
downwards, and enriched in Mg;
! The upper suite, albitite: all textural types of mica repre-
sent Mg-rich muscovite (phengite), as a result of the Alpine
overprint. The primary character of these micas cannot be
deciphered, but part of the micas with relatively higher fluo-
rine (0.5—1.5 apfu F) could by remnants after primary zin-
nwaldite. The F-poor micas represent the low-temperature
Alpine generation.
Magmatic evolution of the Dlhá dolina pluton
Abrupt changes in contents of some chemical elements sup-
port sharp, intrusive contact between the lower barren and the
upper rare-metal granite suites in the Dlhá dolina pluton.
Moreover, these granites were tectonically modified (Fig. 2).
Both granite suites represent late-orogenic peraluminous
crustal melts. While the deeper intrusion formed a chemically
homogeneous body, the upper magma batch underwent differ-
entiation in situ resulting in remarkable stratification.
The direction and manner of crystallization of the upper
suite resulted mainly from a combination of two factors:
chemical stratification within the water- and fluxes-rich
magma batch (London 2014), and cooling. Petrasová et al.
(2007) estimated the metamorphic conditions in the country
rock during the intrusion of Li-mica granites near 100 MPa
and 430 °C. This means relatively shallow, nearly sub-volca-
nic conditions with a fast cooling rate of the granites.
The increase of Na, F, P, Li, and Rb combined with de-
crease of Si, K, Fe in the depth interval from 720 to 550 m
upwards (Fig. 7a) are mineralogically expressed in transition
of the tourmaline (+Li-rich biotite or protolithionite) to the
topaz ( + zinnwaldite) granite. The uppermost part of the to-
paz granite (in the depth of 575—550 m) is strongly affected by
shearing and primary character of the contact between topaz
granite and overlaying albitite is difficult to interpret. Presence
of some K-feldspar in approximately the lowermost 50 m of
the albitites (in the depth of 550—500 m) suggests that the con-
tact between topaz granite and quartz albitite was primarily
transitional. This transition is marked by increases of Na, Ga,
Nb, Ta, and Sn and decreases of K, Fe, P, F, Li, Rb, Cs, W, Y,
and REE. Contents of Si, Al, and Zr remain the same.
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The sum of the alkalis (Na
2
O + K
2
O) in all the rock facies
varies in a relatively narrow interval 8—10 wt. % (Fig. 7b)
and is consistent with fully magmatic origin of the albitite.
Albite grains in the albitite are enriched in phosphorus sug-
gesting their primary magmatic origin (London et al. 1993;
Breiter et al. 2002). Also the texture of non-mylonitized albi-
tite is consistent with crystallization from melt; no signs of
Na-metasomatosis were found. Thus, the upper part of the
magma batch should have been enriched in Na before the feld-
spar started to crystallize. We found no indications of later ad-
ditional metasomatic input of alkalis into the albitite.
Differentiation of crystallized hydrous silicate melt into
K- and Na-dominated domains is typical for layered aplite-
pegmatite systems (Jahns 1955; London 2014). Among litho-
phile elements, if we neglect the irregularities caused by the
low-temperature Alpine overprint, the primary magmatic con-
tents of Li, Rb, Sn, Nb, and Ta in tourmaline and topaz gran-
ites increased systematically upwards: ca. 400
→1200 ppm
Rb, 200
→1000 ppm Li, 50→250 ppm Sn, 2060 ppm Nb,
and 10
→100 ppm Ta. Sharp decreases of Rb- and Li-con-
tents in the albitite are caused by nearly complete disappear-
ance of Li-mica and an abrupt decrease of K-feldspar. The
systematic increase of Sn, Nb and Ta in the upper part of the
cupola does not correlate with the extent of greisenization
and suggests a mostly magmatic origin of disseminated
columbite in albitite. Distribution of Sn is much more scat-
tered, but the highest contents of Sn were encountered in the
Na-most enriched domains of the albitite body (Fig. 8). In
contrast, the highest contents of W were found in the topaz
granite. Decoupling of Nb + Ta and Sn and W during final
stage of fractionation of peraluminous F, Li-rich granite was
also described from the Podlesí granite stock, Krušné hory
Mts, Czech Republic (Breiter et al. 2007).
The absence of signs of greisenization within the topaz and
tourmaline granite made any later supply of fluids (+ore ele-
ments) from the depth unlikely. Separation of greisenizing
fluids from the melt should appear in situ already during crys-
tallization of the tourmaline and mainly topaz granite. The
irregular, but dominantly steep joins may have formed via
hydrofracturing during “second boiling” of the residual melt.
Low degree of greisenization
According to the original description by Malachovský
et al. (1992) greisenization (early post-magmatic silicification)
along sub-vertical (?)cm-dm-scale joins affected only the
albitite.
Among 65 samples of 1—2 m long segments of the core
from the albitite (depth 454—554 m, Malachovský et al.
1992), only two samples from the depth 488 and 489.5 m con-
tain less than 1 wt. % of Na
2
O and should be designated as
greisen. Moreover, 7 samples contain 3.5—5.9 wt. % Na
2
O,
and another 56 samples contain more than 6.0 wt. % Na
2
O.
Thus, excluding the section 486—489 m, the range of silicifi-
cation (greisenization) of the albitite is minimal. Above that,
the Si-rich samples are Li-poor (<100 ppm Li) and Sn does
not correlate positively with Si, but with Na. The “greisens”
are slightly enriched in apatite; necessary phosphorus was
liberated from crystal lattice of altered albite. Summing up,
the range of greisenization in the DD-3 section and its influ-
ence on mineralization is minimal, if it occurs at all.
Low-temperature Alpine overprint
The conditions of the Alpine metamorphism in the Dlhá
dolina area were estimated at 350 °C and 180—280 MPa
(Radvanec et al. 2004), however distinctly higher pressures
( ~ 400 °C and 600—700 MPa) were reported by Petrasová et
al. (2007). The granite body was affected by shearing and
mylonitization. The intensity of mechanical deformation is
highly variable: zones composed of only relicts of magmatic
quartz flowing in aggregates of fine-grained phengitic mus-
covite alternate with nearly fresh primary granite and albi-
tite. The brittle deformation of granitoids was accompanied
by supply of fluids from dolomite, magnesite and talc bodies
to the granite cupola (Kilík 1997; Radvanec et al. 2004;
Petrasová et al. 2007). These fluids, enriched in Ca, Mg and
CO
2
, permeated the upper part of the granite body resulting
in crystallization of Ca, Mg-carbonates in thin joints and
small cavities. Carbonate minerals, inconspicuous under an
optical microscope, are clearly detectable on CL-images.
During this process, the whole-rock content of Mg was en-
riched up to 0.9 wt. % in mylonitized albitite and up to
1.7 wt. % in mylonitized topaz granite. Similarly, Ca was
enriched up to 1.4 and 2.9 wt. % in albite and granite, re-
spectively. Exhumation (end of the metasomatic processes)
was dated to 87.7 (±5.9 Ma) using zircon fission-track analy-
ses (Plašienka et al. 2007).
Comparison of the Dlhá dolina pluton with other Gemeric
granites
Three other granite bodies cropped out in the vicinity of
the Dlhá dolina pluton. The geographically closest body, the
Surovec granite, is also the most similar from the point of
view of chemical composition (enrichment in F, P, and Li),
mineralogy (topaz, zinnwaldite, P-rich primary feldspars),
and strong Alpine overprint. The bodies near Hnilec and
Betliar are B-specialized containing common tourmaline in
association with Li-poor micas.
Fig. 8. Contents of Na and Sn in 1—2 m long segments of the borehole
DD-3, the Dlhá dolina pluton (primary data from Malachovský et al.
1992). Enrichment of tin correlated well with high content of albite.
The “greisenized” samples poor in Na are relatively Sn-poor.
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The mineral composition of the Surovec body published
by Petrík et al. (2011, 2014) allows a comparison with the
Li-granites from the Dlhá dolina granite system, whereas
analogues of albitite and biotite granite were not found in the
Surovec body. In both localities, remnants of primary mag-
matic mineral assemblages alternate with domains of strong
Alpine low-temperature hydrothermal overprint. Increasing
intensity of the overprint is marked by nearly complete loss
of phosphorus in feldspars (from 1.5 to < 0.1 wt. % P
2
O
5
in Surovec, from 0.5 to < 0.1 wt. % P
2
O
5
in Dlhá dolina) and
transformation of primary zinnwaldite (5—11.5 wt. % FeO
in Surovec, 8.7—9.4 wt. % FeO in Dlhá dolina) to second-
ary Li-rich phengite (5—7.5 wt. % FeO in Surovec,
0.4—4.5 wt. % FeO in Dlhá dolina). Fluorapatite, which was
primarily Mn-rich (up to 6 wt. % MnO in Surovec and
3.3 wt. % MnO Dlhá dolina) was metasomatically strongly
enriched in Sr (up to 13.6 wt. % in Surovec and
5.7 wt. % SrO in Dlhá dolina). A specific feature of the Dlhá
dolina granites is the enrichment of secondary micas in mag-
nesium (commonly ~ 2 wt. % in phengitic muscovite and up
to 20 wt. % in flogopite), which may be attributed to the pro-
cesses of steatization of the nearby Gemerská Poloma talc
deposit (Kilík 1997; Radvanec et al. 2004). Topaz from both
localities differs significantly: while topaz from Surovec
granite is enriched in phosphorus (up to 1.2 wt. % F) and
relatively poor in F (14—15 wt. %, only 68—75 atom. %
of (F + OH)-site occupancy); topaz from Dlhá dolina is
P-poor (max. 0.2 wt. % P
2
O
5
), but F-rich (20—21 wt. % F,
~
100 atom. % of (F + OH)-site occupancy). The composition
of the Dlhá dolina topaz fits well with topaz from peralumi-
nous topaz-zinnwaldite granites in the western Erzgebirge
(Breiter & Kronz 2004), while the Surovec topaz was proba-
bly re-equilibrated during Alpine processes. The differences
in composition of topaz, apatite and secondary micas, and
the appearance of varied assemblages of hydrated secondary
phosphate minerals (Petrík et al. 2011) indicate somewhat
different P-T conditions and composition of Alpine hydro-
thermal fluids at the two localities.
We interpret the Dlhá dolina pluton as a combination of
two intrusive pulses: (i) biotite granites, and (ii) Li-mica
granites + albitite. Two-stage granite evolution has also been
reported from the nearby Betliar and Hnilec areas. However,
in Betliar, the first magmatic stage has formed evolved vola-
tile rich magmas which intruded into an open fault system as
sill-like bodies crystallizing as equigranular fine-grained gran-
ites followed by subsequent high-temperature post-magmatic
alteration. The second stage intrusion from a deeper seated
magmatic reservoir resulted in formation of the porphyric
granite body. The emplacement of both granite intrusions were
dated as Middle or Late Permian (Kubiš & Broska 2010).
In the Hnilec area, volatiles (mainly B, in a lesser amount
also F) concentrated in hydromagma under the carapace of
fast quenched fine-grained granites. Overpressure due to
separation of B-rich fluids caused hydrofracturing of roof
fine-grained granites and exocontact rocks. The F-rich por-
tion of the fluid greisenized some domains in the endocon-
tact. The porphyric to coarse-grained two-mica and biotite
granites are situated below this fine-grained metasomatized
and greisenized granite carapace (Kubiš & Broska 2005).
Comparison with other rare-metal granites worldwide
Two main genetically important issues should be dis-
cussed to correctly interpret the geological structure and de-
velopment of the Dlhá dolina pluton: (i) time/space relation
of the less- and more evolved rock types (biotite granites vs.
Li-mica granites), and (ii) relations between the most-
evolved ore-bearing granite facies, feldspatite and greisens.
The simplified vertical cross-section of the Dlhá dolina is
compared with several long time studied and thus well recog-
nized Sn, W, Nb, Ta-bearing plutons from the Krušné hory/
Erzgebirge and French Massif Central (Fig. 9). Among the
five compared profiles, only the Sn, W-mineralized Krásno
pluton (Jarchovský 1998, 2004) is composed of one intrusion.
In all other plutons, two intrusive units were recognized and
the more-evolved rock suites are situated in the upper part of
the profiles above the less-fractionated granites. Both suites
have sharp intrusive contacts, but they are interpreted as co-
magmatic. In Cínovec and Podlesí (both the Krušné hory,
Czech Republic), the younger Li-mica granite formed a
tongue-like body which intruded generally along the contact
plane between the older biotite granite and its envelope (Štem-
prok et al. 1994; Breiter et al. 2005). The origin of the Beau-
voir pluton (France) was interpreted in another way: the
more-evolved part of the melt, due to lower viscosity, intruded
faster and crystallized in the upper part of the cupola. The less
evolved more viscose part of the melt arrived later and re-
mained in the lower part of the known profile (Raimbault et al.
1995). In the Dlhá dolina, the relative age relation between the
lower and upper granite suites remains unresolved.
Comparing the Dlhá dolina magmatic system with well-
known Sn-W greisen deposits in the Krušné hory/Erzgebirge,
such as Geyer and Ehrenfriedersdorf (Hösel 1994) in (Ger-
many), and Krásno (Jarchovský 2004) and Cínovec (Štem-
prok & Šulcek 1969), both Czech Republic, the major
difference should be seen in the position of feldspar-rich
rocks (feldspatites, albitites) in the vertical evolution of the
granite cupola, and time/space relation between feldspatitic
rocks and greisenization. In the Krušné hory/Erzgebirge, the
greisens form the uppermost part of the cupolas. The interval
about 200 m thick below the greisen is occupied by leuco-
cratic mica-poor granite with individual layers of feldspatites
in its deeper part (Jarchovský 2004). Within the feldspatites,
facies with very different K/Na-ratio occur (K
2
O 2—8 wt. %,
Na
2
O 3—8 wt. %). Non-altered Li-F granite occurs below the
feldspatites. Feldspatization is a geologically younger or
contemporaneous process than greisenization. In contrast,
only Na-rich feldspatites were found in Dlhá dolina, forming
the uppermost part of the cupola. Greisen stringers cut the al-
bitite, which means that here the greisenization is somewhat
younger than the origin of feldspar-rich rocks. Vertical zon-
ality similar to that of the Dlhá dolina was described by Koval
(1975) as typical for the so-called muscovite-albite type of
rare-metal granites in the eastern parts of the former Soviet
Union. Moreover, 40 years ago Koval (l.c.) interpreted the
albite in Kazachstan and Transbaikalia as metasomatic sup-
porting an earlier model established by Beus (e.g. Beus &
Zalaškova 1962), but the overall zoning of plutons is con-
spicuously similar.
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The highly fractionated S-type granites of the Moldanubian
and Saxothuringian zones of the European Variscides were
formed during the Late Carboniferous: granites in the western
and central Krušné hory/Erzgebirge at 318—327 Ma (Förster
& Römmer 2010), granites in the Moldanubicum (southern
Czech Republic and northern Austria) between 310—320 Ma
(Scharbert 1998), and the Beauvoir granite in French Massif
Central at 308 ± 2 Ma (Cheilletz et al. 1992). The early post-
orogenic A-type rare-metal granites in the eastern Krušné
hory/Erzgebirge is dated with still relatively large uncertainty
into the broad interval of ca. 320—305 Ma (see Förster &
Römmer (2010) and Breiter (2012) for discussion). The per-
aluminous Sn-bearing granites in Cornwall have distinctly
younger—Late Permian date (274—293 Ma – Chen et al.
1993). The granites of the Gemeric Superunit, including the
Dlhá dolina pluton, show only ~ 260 to 250 Ma age (Poller
et al. 2002; Kohút & Stein 2005). Therefore they are proba-
bly the youngest tin-bearing granites found in the Variscan
orogenic belt through the Europe, emplaced after termina-
tion of the Variscan orogeny. Moreover, the same age
(262 ± 4 Ma) is found in the hypersolvus rift-related A-type
granite from Turčok in the same Gemeric Superunit (Rad-
vanec et al. 2009; Uher unpublished data). However, the
Turčok granite shows different geochemical and mineralogi-
cal features in comparison to the Dlhá dolina granite: espe-
cially high Zr and REE but low Li, B, P, Sn, Ta and W
contents as well as dissimilar REE and Nb phases, reflecting
its metaluminous A-type character (Uher & Broska 1996;
Broska & Uher 2001; Uher et al. 2009). Consequently, the
Gemeric Permian S- and A-type granites do not represent an
analogy with the Krušné hory/Erzgebirge area, where both
fractionated S- and A-type members show enrichment in Li,
Sn, B, Ta, and W (Breiter 2012).
Conclusions
In the Dlhá dolina pluton (DD-3 borehole), the primary
character of contacts between different granite facies was
strongly tectonically modified during Alpine (Cretaceous)
thrusting; therefore, our interpretation concerning zoning,
magma differentiation and evolution, despite all objective
data, remains partly speculative. Nevertheless, taking into
account all available information from the Dlhá dolina area
and experience from better exposed ore-bearing plutons, we
are able to formulate the following genetic scenario:
! Intrusion of common peraluminous magma formed a large
body of biotite granites and intrusion of evolved peraluminous
melt enriched in Li, P, F, Sn, Nb, Ta, and W took place;
! The evolved melt differentiated in situ forming three dif-
ferent rock types: tourmaline-Li-biotite granite at the bot-
tom, topaz-zinnwaldite granite in the middle, and quartz
albitite to albitite at the top. The composition of primary
feldspar, micas, zircon and apatite document a relatively
high degree of magmatic fractionation;
! A crucial part of Sn, Nb, and Ta crystallized from the
melt as disseminated cassiterite and columbite within the al-
bitite, while disseminated wolframite appears mainly within
the topaz granite;
Fig. 9. Comparison of simplified vertical sections through different
rare-metal granite plutons (see text for details). DD-3 Dlhá dolina,
Slovakia (this work); PTP-3 Podlesí, Czech Republic (Breiter
2002); K-25 Krásno, Czech Republic (Jarchovský 1998); GBP-1
Beauvoir, France (Raimbault et al. 1995); CS-1 Cínovec, Czech Re-
public (Štemprok & Šulcek 1969).
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! Fluids separated from the last portion of crystallized mag-
ma (topaz-zinnwaldite granite) penetrated overlying albitite
and resulted in small scale greisenization. Phosphorus from al-
kali feldspars was partially released forming secondary apa-
tite. Disseminated bismuthinite originated at the same time;
! Much later, during Alpine thrusting, the upper part of
the pluton was strongly tectonized and mylonitized along
flat joins. Metamorphic Ca, Mg, and CO
2
rich fluids in
neighbouring metacarbonates penetrated the fractured gran-
ite, forming thin carbonate veinlets and filling small cavities.
These fluids also reacted with feldspars releasing the rest of
the phosphorus from their crystal lattice, and forming Mg-rich
mica varieties from magmatic and greisen micas. All bulk-
rock and mineral markers were reset and now represent the
P-T conditions of the Alpine overprint.
Acknowledgments: The granite samples were taken from the
deposited DD-3 borehole in the storage house of the State
Geological Institute of Dionýz Štúr on the basis of an official
permit. We thank Mrs. Kateřina Švecová (Masaryk University
Brno) for help with the cathodoluminescence analysis, Mr.
Patrik Konečný and Mrs. Viera Kollárová (D. Štúr State Geo-
logical Institute, Bratislava) and Mrs. Zuzana Korbelová
(Geological Institute CAS Praha) for assistance during elec-
tron-microprobe analyzing. Inspiring reviews by Igor Petrík
and Milan Kohút are acknowledged. This investigation was
supported by the Czech Science Foundation, Project
Nos. P210/14/13600S and RVO 67985831, the VEGA Project
No. 1/0257/13, and the APVV-0081-10 Project.
References
Bajaník Š., Ivanička J., Mello J., Pristaš J., Reichwalder P., Snopko
L., Vozár J. & Vozárová A. 1984: Geological map of the Slo-
venské Rudohorie Mts. – eastern part 1 : 50,000. D. Štúr Inst.
Geol., Bratislava.
Baran J., Drnzíková L. & Mandáková K. 1970: Sn-W ore mineral-
ization connected with the Hnilec granites. Miner. Slovaca 2,
159—165 (in Slovak).
Baran J., Drnzík E., Drnzíková L. & Mandáková K. 1971: Recent
results of verification of Sn-W anomaly in Medvedí Potok.
Miner. Slovaca 3, 151—153 (in Slovak).
Bastos Neto A.C., Pereira V.P., Ronchi L.H., De Lima E.F. &
Frantz J.C. 2009: The world-class Sn, Nb, Ta, F (Y, REE, Li)
deposit and the massive cryolite associated with the albite-en-
riched facies of the Madeira A-type granite, Pitinga Mining
District, Amazonas State, Brazil. Canad. Mineralogist 47,
1329—1357.
Beus A.A. & Zalaškova N.E. 1962: High-temperature postmagmatic
metasomatism in granitoids. Izvestiya AN SSSR, Ser. Geol.,
13—31 (in Russian).
Breiter K. 2002: From explosive breccia to unidirectional solidifi-
cation textures: magmatic evolution of a phosphorus- and fluo-
rine-rich granite systém (Podlesí, Krušné hory Mts., Czech
Republic). Bull. Czech Geol. Surv. 77, 67—92.
Breiter K. 2012: Nearly contemporaneous evolution of the A- and
S-type fractionated granites in the Krušné hory/Erzgebirge
Mts., Central Europe. Lithos 151, 105—121.
Breiter K. & Kronz A. 2004: Phosphorus-rich topaz from fraction-
ated granites (Podlesí, Czech Republic). Miner. Petrology 81,
235—247.
Breiter K., Förster H. & Seltmann R. 1999: Variscan silicic magma-
tism and related tin-tungsten mineralization in the Erzgebirge-
Slavkovský les metamollgenic province. Mineralium Depos.
34, 505—521.
Breiter K., Frýda J. & Leichmann J. 2002: Phosphorus and rubidium
in alkali feldspars: case studies and possible genetic interpreta-
tion. Bull. Czech Geol. Surv. 77, 93—104.
Breiter K., Škoda R. & Uher P. 2007: Nb-Ta-Ti-W-Sn-oxide minerals
as indicator of a peraluminous P- and F-rich granitic system evo-
lution: Podlesí, Czech Republic. Miner. Petrology 91, 225—248.
Breiter K., Müller A., Leichmann J. & Gabašová A. 2005: Textural
and chemical evolution of a fractionated granitic system: the
Podlesí stock, Czech Republic. Lithos 80, 323—345.
Broska I. & Uher P. 2001: Whole-rock chemistry and genetic ty-
pology of the West-Carpathian Variscan granites. Geol. Car-
pathica 52, 79—90.
Cheilletz A., Archibald D.A., Cuney M. & Charoy B. 1992: Ages
40
Ar/
39
Ar du leucogranite a topaze-lepidolite de Beauvoir et des
pegmatites sodolithiques de Chédeville (Nord du Massif Cen-
tral, France). Significance pétrologique et géodynamique. C. R.
Acad. Sci. 315, 326—336.
Chen Y., Clark A.H., Farrar E., Wasteneys H.A.H.P., Hodgson M.J.
& Bromley A.V. 1993: Diachronous and independent histories
of plutonism and mineralization in the Cornubian Batholith,
southwest England. J. Geol. Soc. 150, 1183—1191.
Dianiška I., Breiter K., Broska I., Kubiš M. & Malachovský P. 2002:
First phosphorus-rich Nb-Ta-Sn-specialised granite from the
Carpathians Dlhá dolina valley granite pluton, Gemeric Supe-
runit. Geol. Carpathica, Spec. Issue, 53 (CD-ROM).
Drnzíková L., Drnzík E., Mandáková K. & Baran J. 1975: Criteria of
tin and metallogenetic specialization of some granite types of the
Spiš-Gemer Ore Mountains. Miner. Slovaca 7, 53—59 (in Slovak).
Förster H.J. & Römmer R.L. 2010: Carboniferous magmatism. In:
Linnemann U. & Romer R.L. (Eds.): Pre-Mesozoic geology of
Saxo-Thuringia – from the Cadomian active margin to the
Variscan orogen. Schweizerbart. Stuttgart, 287—308.
Frolov A.A. 1978: Mineral deposits in stockworks. Nauka, Moskva,
1—264 (in Russian).
Haapala 1995: Metallogeny of the Rapakivi granites. Miner. Petrol-
ogy 54, 149—160.
Hösel G. (Ed.) 1994: Das Zinnerz-Lagerstattengebiet Ehrenfrieders-
dorf/Erzgebirge. Bergbau in Sachsen, 1, LFuB, Freiberg,
1—195.
Jahns R.H. 1955: The study of pegmatites. Econ. Geol. 50,
1025—1130.
Jarchovský T. 1998: Sn-W mineralization in the Krásno district. In:
Breiter K. (Ed.): Genetic significance of phosphorus in frac-
tionated granites – Excursion guide. Czech Geol. Surv., Praha,
77—92.
Jarchovský T. 2004: The nature and genesis of greisen stocks at
Krásno, Slavkovský les area – Western Bohemia, Czech Re-
public. J. Czech Geol. Soc. 51, 201—216.
Kilík J. 1997: Geological characteristic of the talc deposit in
Gemerská Poloma—Dlhá dolina. Acta Montanistica Slovaca 2,
71—80 (in Slovak).
Kohút M. & Stein H. 2005: Re-Os molybdenite dating of granite-re-
lated Sn-W-Mo mineralisation at Hnilec, Gemeric Superunit,
Slovakia. Miner. Petrology 85, 117—129.
Koval P.V. 1975: Petrology and geochemistry of albitized granites.
Nauka, Moskva, 1—258 (in Russian).
Kovalenko V.I. & Kovalenko N.I. 1976: Ongonites (topaz-bearing
quartz keratophyre) – subvolcanic analoques of rare-metal Li-F
granites. Nauka, Moskva, 1—124 (in Russian).
Kubiš M. & Broska I. 2005: Role of boron and fluorine in evolved
granitic rock systems (on example Hnilec area, Western Car-
pathians). Geol. Carpathica 56, 193—204.
36
BREITER, BROSKA and UHER
G
G
G
G
GEOL
EOL
EOL
EOL
EOLOGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPATHICA
THICA
THICA
THICA
THICA, 2015, 66, 1, 19—36
Kubiš M. & Broska I. 2010: The granite system near Betliar village
(Gemeric Superunit, Western Carpathians): evolution of a com-
posite silicic reservoir. J. Geosci. 55, 131—148.
Küster D. 2009: Granitoid-hosted Ta mineralization in the Arabian-
Nubian Shield: Ore deposit types, tectono-metallogenetic set-
ting and petrogenetic framework. Ore Geol. Rev. 35, 68—86.
Lehmann B. 1990: Metallogeny of tin. Lecture notes in earth sci-
ences. Springer, Heidelberg-Berlin 32, 1—211.
London D. 2014: A petrologic assessment of internal zoning in gra-
nitic pegmatites. Lithos 184—187, 74—104.
London D., Morgan G.B. VI, Babb H.A. & Loomis J.L. 1993: Be-
haviour and effects of phosphorus in the system Na
2
O—K
2
O—
Al
2
O
3
—SiO
2
—P
2
O
5
—H
2
O at 200 MPa (H
2
O). Contr. Mineral.
Petrology 113, 450—465.
Losos Z. & Vižda P. 2006: Mineralogy and genesis of the cassiterite
from Kovářová near Nedvědice. [Sborník mineralogie Českého
masívu a Západních Karpat]. University of Palacky in Olo-
mouc, 30—40 (in Czech). ISBN 80-244-1560-7.
Malachovský P., Turanová L. & Dianiška I. 1992: Final report on
mineral exploration from Gemerská Poloma. Unpubl. report,
Geofond archive, Bratislava, 1—180 (in Slovak).
Malachovský P., Dianiška I., Matula I., Kamenický J., Kobulský J.,
Hodermarský J., Fabian M., Radvanec M., Kozáč J., Vlasák
M., Mihalič A., Ščerbáková A., Seliga J. & Novoveský M.
1983: SGR – high temperature mineralization – Sn, W, Mo
ores. Unpubl. report, Geofond archive, Bratislava, 1—248 (in
Slovak).
McDonough F.V. & Sun S. 1995: The composition of the Earth.
Chem. Geol. 120, 223—253.
Němec D. & Páša J. 1986: Regionally metamorphosed greisens of
the Moldanubicum. Mineralium Depos. 21, 12—21.
Petrasová K., Faryad S.W., Jeřábek P. & Žáčková E. 2007: Origin
and metamorphic evolution of magnesite-talc adjacent rocks near
Gemerská Poloma, Slovak Republic. J. Geosci. 52, 125—132.
Petrík I., Kubiš M., Konečný P., Broska I. & Malachovský P. 2011:
Rare phosphates from the Surovec topaz-Li-mica microgranite,
Gemeric unit, Western Carpathians, Slovakia: the role of the
F/H
2
O in the melt. Canad. Mineralogist 49, 521—540.
Petrík I., Čík Š., Miglierini M., Vaculovič T., Dianiška I. & Ozdín
D. 2014: Alpine oxidation of lithium micas in Permian S-type
granites (Gemeric unit, Western Carpathians, Slovakia). Min-
eral. Mag. 78, 507—533.
Plašienka D., Broska I., Kissová D. & Dunkl I. 2007: Zircon fis-
sion-track dating of granites from the Vepor-Gemer-Belt
(Western Carpathians): constraints for the Early Alpine exhu-
mation history. J. Geosci. 52, 113—123.
Poller U., Uher P., Broska I., Plašienka D. & Janák M. 2002: First
Permian—Early Triassic zircon ages for tin-bearing granites
from the Gemeric unit (Western Carpathians, Slovakia): con-
nection to the post-collisional extension of the Variscan orogen
and S-type granite magmatism. Terra Nova 14, 41—48.
Radvanec M., Koděra P. & Prochaska W. 2004: Mg replacement at
the Gemerská Poloma talc-magnasite deposit, Western Car-
pathians, Slovakia. Acta Petrol. Sin. 20, 773—790.
Radvanec M., Konečný P., Ondrejka M., Putiš M., Uher P. &
Németh Z. 2009: The Gemeric granites as an indicator of the
crustal extension above the Late-Variscan subduction zone and
during the Early Alpine riftogenesis (Western Carpathians):
An interpretation from the monazite and zircon ages dated by
CHIME and SHRIMP methods. Miner. Slovaca 41, 381—394
(in Slovak with English resumé).
Raimbault L., Cuney M., Azencott C., Duthou J.L. & Joron J.L.
1995: Geochemical evidence for a multistage magmatic gene-
sis of Ta-Sn-Li mineralization in the granite at Beauvoir,
French Massif Central. Econ. Geol. 90, 548—596.
Scharbert S. 1998: Some geochronological data from the South Bo-
hemian Pluton in Austria: a critical review. Acta Univ. Caroli-
nae Geol. 42, 114—118.
Seltmann R., Kampf H. & Möller P. (Eds.) 1994: Metallogeny of
collisional orogens. Czech Geol. Surv., Praha, 1—448.
Solomovich L.I., Trifonov B.A. & Sabelnikov S.E. 2012: Geology
and mineralization of the Uchkoshkon tin deposit associated
with a breccia pipe, Eastern Kyrgyzstan. Ore Geol. Rev. 44,
59—69.
Štemprok M. 1993: Genetic models for metallogenic specialization
of tin and tungsten deposits associated with the Krušné hory-
Erzgebirge granite batholith. Res. Geol., Spec. Issue 15,
373—383.
Štemprok M. & Šulcek Z. 1969: Geochemical profile through an
ore-bearing lithium granite. Econ. Geol. 64, 392—404.
Štemprok M., Novák J.K. & David J. 1994: The association be-
tween granites and tin-tungsten mineralization in the Krušné
hory (Erzgebirge), Czech Republic. Monograph, Ser., Mineral
Depos. 31, 97—129.
Taylor R.P. & Strong D.F. (Eds.) 1985: Recent advances in the ge-
ology of granite-related mineral deposits. Canad. Inst. Mining
and Metallurgy, Spec. Vol., Montreal 39, 1—445.
Tischendorf G. (Ed.) 1989: Silicic magmatism and metallogenesis
of the Erzgebirge. Veröff. Zentralinst. f. Physik d. Erde, Pots-
dam 107, 1—316.
Tischendorf G., Gottesmann B. & Förster H.-J. 1999: The correla-
tion between lithium and magnesium in trioctahedral micas:
Improved equations for Li
2
O estimation from MgO data. Min-
eral. Mag. 63, 57—74.
Tréger M. & Matula I. 1977: New inditions of tin ore mineraliza-
tion in the Spiš-Gemer Ore Mountains and perspectives of
their prospecting. Geol. Průzkum 19, 262—265.
Uher P. & Broska I. 1996: Post-orogenic Permian granitic rocks in
the Western Carpathian-Pannonian area: Geochemistry, miner-
alogy and evolution. Geol. Carpathica 47, 311—321.
Uher P., Ondrejka M. & Konečný P. 2009: Magmatic and post-mag-
matic Y-REE-Th phosphate, silicate and Nb-Ta-Y-REE oxide
minerals in A-type metagranite: an example from the Turčok
massif, the Western Carpathians, Slovakia. Mineral. Mag. 73,
1009—1025.
Vozárová A., Šarinová K., Larionov A., Presnyakov S. & Sergeev
S. 2010: LateCambrian/Ordovician magmatic arc type volcan-
ism in the Southern Gemericum basement, Western Car-
pathians, Slovakia: U-Pb (SHRIMP) data from zircons. Int. J.
Earth Sci. 99 (Suppl 1), S17—S37.