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, DECEMBER 2013, 64, 6, 419—435 doi: 10.2478/geoca-2013-0029
Geochronology and petrogenesis of granitoid rocks from the
Goryczkowa Unit, Tatra Mountains (Central
Western Carpathians)
JOLANTA BURDA
1
, ALEKSANDRA GAWĘDA
1
and URS KLÖTZLI
2
1
University of Silesia, Faculty of Earth Sciences, Będzińska 60, 41-200 Sosnowiec, Poland;
jolanta.burda@us.edu.pl; aleksandra.gaweda@us.edu.pl
2
University of Vienna, Department of Lithospheric Research, Althanstrasse 14, 1090 Vienna, Austria; urs.kloetzli@univie.ac.at
(Manuscript received January 7, 2013; accepted in revised form October 16, 2013)
Abstract: The geochemical characteristics as well as the LA-MC-ICP-MS U-Pb zircon age relationship between two
granitoid suites found in the Goryczkowa crystalline core in the Western Tatra Mountains were studied. The petrological
investigations indicate that both granitoid suites were emplaced at medium crustal level, in a VAG (volcanic arc granites)
tectonic setting. However, these suites differ in source material melted and represent two different magmatic stages:
suite 1 represents a high temperature, oxidized, pre-plate collision intrusion, emplaced at ca. 371 Ma while suite 2 is late
orogenic/anatectic magma, which intruded at ca. 350 Ma. These data are consistent with a period of intensive magmatic
activity in the Tatra Mountain crystalline basement. The emplacement of granitoids postdates the LP-HT regional meta-
morphism/partial melting at ca. 387 Ma and at 433—410 Ma, imprinted in the inherited zircon cores.
Key words: Western Carpathians, Tatra Mountains, U-Pb zircon geochronology, Goryczkowa granitoids.
Introduction
The crystalline basement of the Tatra Mountains is one of
several Variscan crystalline complexes in the Central West-
ern Carpathians (CWC; Fig. 1a). The granitoid rocks, which
are the most important constituents of the Tatra Mountains
crystalline core, have intruded a series of metamorphic rocks
(e.g. Gawęda et al. 2000; Burda & Klötzli 2011). The origin
of this magmatism is related to continent—continent collision
during the Devonian and Carboniferous (e.g. Poller et al.
2000, 2001; Burda et al. 2011). In spite of recent U-Pb zir-
con age dating many uncertainties persist regarding the ori-
gin, development and timing of the granitoid magma
batches. The still unsolved problem is the origin and age of
the so-called Goryczkowa granitoids.
The granitoids form a main portion of the Goryczkowa
Unit, representing a fragment of the crystalline core, displaced
during the Alpine folding and thrusting event, which formed
the Carpathian arc. At present, crystalline fragments form
three cores of the Giewont Nappe in the northern part of the
Tatra massif (Fig. 1c). Accessible WR (whole rock) Rb-Sr iso-
chron data pointed to an age of 300—290 Ma for granitoid
rocks emplacement while the Goryczkowa gneisses yielded an
Rb-Sr isochron age of 413 ± 10 Ma (Burchart 1968).
The main purpose of this study is to discuss the petrogene-
sis and zircon U-Pb ages of two types of Goryczkowa grani-
toids. As a result we verify the currently published opinions
about the petrological and classification autonomy of the
Goryczkowa granitoids. In order to better constrain the em-
placement ages, inter-relations and evolution of these grani-
toids, field observations, major and trace element chemistry
and LA-MC-ICP-MS (Laser Ablation Multi-Collector Induc-
tively Coupled Plasma Mass Spectrometry) U-Pb zircon age
calculations were combined with studies of zircon morphology
and internal structures. The results are compared with pub-
lished petrological data and time constraints. The inherited
components, present in granitoid rocks are also discussed to
understand the trace element signatures of both granitoid suites.
Geological setting
The crystalline basement of the Tatra Mountains is one of
several crystalline basement units in the Alpine belt of the
Central Western Carpathians. It comprises polygenetic
Variscan granitoids that are volumetrically predominant and
an early Variscan migmatitic metamorphic envelope (e.g.
Gawęda 2001; Burda & Gawęda 2009; Burda & Klötzli
2011).
In the polygenetic granitoid pluton four petrographic types
of granitoids were distinguished (Kohút & Janák 1994). The
common Tatra granodiorite-tonalite forms a volumetrically
predominant tongue-shaped intrusion, dated at 368—350 Ma
(Poller et al. 2000, 2001; Burda et al. 2011). Quartz-diorites
(I-type mingled hybrid, interpreted as magmatic precursors)
are present as sills inside the metamorphic envelope, in the
border zone of the common Tatra granite (Gawęda et al.
2005). The mingling-mixing processes between the common
Tatra type and quartz-diorite precursors were dated to
368 ± 8 Ma (Burda et al. 2011). The High Tatra granite
(I/S-type) predominates in the eastern part of the massif
(Fig. 1b) and is characterized by the abundance of mafic en-
claves and xenoliths of country rocks (Gawęda 2009). Pub-
lished zircon U-Pb data suggest an emplacement age of
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Fig. 1. The geology of the Tatra Mountains: a – simplified geological sketch of the Carpathian chain; b – geological map of the Tatra
Mountains Block (after Kohút & Janák 1994; Bac-Moszaszwili 1996; Gawęda et al. 2005); c – simplified geological map of the study area
in the northern part of the Tatra crystalline basement (Giewont Nappe) with sample locations.
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345—335 Ma (Gawęda 2008; Burda 2010; Burda et al. 2013).
The age of the mafic microgranular enclaves (341 Ma; Poller
et al. 2001) falls into this range.
Goryczkowa-type granitoids were distinguished in the
northern part of the Goryczkowa crystalline core (Fig. 1b) as
the grey biotite monzogranite with oriented fabric (Morozewicz
1914; Kohút et al. 2009), associated with pink, porphyritic
leucocratic granites (Fig. 2a). The age of both granites re-
mains largely imprecise, ranging from 300—290 Ma (Burchart
1968), 365—353 Ma (Kohút & Siman 2011) to 356 ± 8 Ma for
leucocratic granite (Burda & Klötzli 2007).
The crystalline complex is covered by nappes of Mesozoic
sedimentary rocks, which also include fragments of the crys-
talline basement (Fig. 1b,c). One of these nappes is the
Giewont Nappe (Jurewicz 2006 and references therein),
which was formed by overthrusting of the sedimentary
rocks, together with the underlying crystalline basement,
now present as the crystalline cores of the nappe. These
cores are exposed in Goryczkowa, Małołączniak and Ciem-
niak Units (Fig. 1c). They comprise metamorphic rocks,
leucogranites (called alaskites) associated with migmatites
(Jaroszewski 1965; Burchart 1968) and interpreted as the ef-
fects of accretionary prism partial melting (Gawęda 2001),
comparable with those found in the Western Tatra Moun-
tains (ca. 360 Ma; Gawęda 2001; Burda & Gawęda 2009)
and two suites of granitoid rocks: granodiorite-tonalite,
called Goryczkowa type granitoids and muscovite alkali-
feldspar granites (Burchart 1968, 1970). For the latter, pre-
liminary U-Pb zircon dating pointed to an intrusion age of
356 ± 8 Ma (Burda & Klötzli 2007).
Analytical methods
Rock samples weighing about 25 kg were collected from
the two main varieties of granitoids from the Goryczkowa
and Małołączniak crystalline cores (Fig. 1c).
Whole-rock samples were analysed by ICP-ES (Inductively
Coupled Plasma Emission Spectrometer) for major and LILE
(large-ion lithophile) trace elements and by ICP-MS (Induc-
tively Coupled Plasma Mass Spectrometry) for HFSE (high
field strength elements) and REE in the ACME Analytical
Laboratories, Vancouver, Canada, using sets of internation-
ally accepted standards, according to procedures described on
http://acmelab.com. REEs are normalized to C1 chondrite
(Sun & McDonough 1989).
Fig. 2. Photographs of the granitoids from the Goryczkowa crystalline core: a – equigranular biotite granodiorite (sample G1 – suite 1)
and alkali-feldspar granite (sample G2 – suite 2). The length of the pen is 10 cm; b – oriented texture of biotite granodiorite (suite 1);
c – porphyritic alkali feldspar granite (suite 2) with a fragment of the alkali feldspar porphyrocryst showing the internal graphic inter-
growths with quartz, flowing in the muscovite-quartz-feldspar groundmass; d – allanite crystal in amphibole-bearing monzogranite (suite 1).
Abbreviations: Pl – plagioclase, Kfs – K-feldspar, Qtz – quartz, Bt – biotite, Ms – muscovite, Hbl – hornblende, All – allanite.
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Microprobe analyses of main and accessory minerals were
carried out in the Inter-Institution Laboratory of Microanalyses
of Minerals and Synthetic Substances, Warsaw (CAMECA
SX-100 electron microprobe; 15 kV, 20 nA, 4 s counting time
for peak and background, 1—5 µm beam diameter), using sets
of internationally recognized natural and synthetic standards.
Mineral abbreviations used here follow those proposed by
Whitney & Evans (2010). Zircon crystals from both granitoid
suites (samples G1 and G2 collected from the top of Beskid)
were separated using standard techniques (crushing, hydro-
fracturing, washing, Wilfley shaking table, Frantz magnetic
separator and handpicking). The separation was carried out
in the Institute of Geological Sciences, Polish Academy of
Sciences, Cracow. Zircon grains were selected for morpho-
logical study using scanning electron microscopy and then
imaged by panchromatic cathodoluminescence using a FET
Philips 30 electron microscope (15 kV and 1 nA) at the Fac-
ulty of Earth Sciences, University of Silesia, Sosnowiec. Zir-
con
206
Pb/
238
U and
207
Pb/
206
Pb ages were determined using a
193-nm solid state Nd-YAG (neodymium-yttrium aluminium
garnet) laser coupled to a Nu PLASMA HR multi collector
ICP mass spectrometer in the Geochronology Laboratory, In-
stitute of Geology at the University of Vienna. Ablation in a
He atmosphere was either spot- or raster-wise according to the
zircon CL zonation patterns. Spot analyses were 15—25 µm in
diameter whereas rastering line widths were 10—15 µm with a
rastering speed of 5 µm/sec. The calculated intercept values
were corrected for mass discrimination by reference to mea-
surements of the zircon standard Plesovice (337.13 ± 0.37 Ma;
Sláma et al. 2008) made during the analytical session. The fi-
nal U/Pb ages were calculated with 2 errors using the
Isoplot/Ex version 3.00 program (Ludwig 2003). Details of
analytical procedures and data reduction schemes are given in
Klötzli et al. (2009).
Petrography and mineral chemistry
The granitoids of the Goryczkowa can be subdivided into
two main suites (Fig. 2a; Burchart 1970). Representative
samples of both suites were collected from the Beskid Mt,
Goryczkowa Czuba and Świńska Valley, all located in the
so-called Goryczkowa and Małołączniak crystalline cores of
the Giewont Nappe (Fig. 1c).
Suite 1 is represented by biotite granodiorite, amphibole-
biotite tonalite and quartz-diorite (Fig. 2), traditionally called
Goryczkowa type granitoids (Morozewicz 1914; Kohút et al.
2009). It is the most abundant granitoid type of Goryczkowa
crystalline core. Biotite granodiorite is a medium-grained
rock with oriented texture and typical plagioclase “augen”
coated by biotite and amphibole (Fig. 2b). The main mineral
components are plagioclase porphyrocrysts showing oscila-
tory zonation (An
32—12
), quartz, biotite (#fm = 0.555—0.557,
Ti = 0.346—0.436 a.p.f.u.; Table 1), amphibole (Mg-horn-
blende; Table 2), K-feldspar (Or
88—91
Ab
10—6
Cn
2—3
). Apatite, zir-
con, Ti-magnetite and monazite-(Ce) are present as
accessories. The amphibole-biotite tonalite and quartz-dior-
ite are composed of plagioclase (An
45—62
), amphibole, biotite
Table 1: Micro-chemical compositions and crystal chemical formulae of micas from both granitoid suites. Explanations: #fm = (Fe + Mn)/
(Fe + Mn + Mg); MsC – muscovite core; MsM – muscovite margin.
Sample
Suite 1
Suite 2
Component
Bt1-G4 Bt2-G4 Bt3-G1 Bt4-G1 MsC-G1
MsM-G1
Ms1-G2 Ms2-G2
SiO
2
37.18 36.70 35.82 35.75 45.67 45.58
48.01
46.08
TiO
2
2.62
3.18
3.00
3.81
0.63
0.49
0.04
0.43
Al
2
O
3
16.05
15.23
16.65
17.08
33.38
33.19
33.86
32.83
Cr
2
O
3
0.01
0.06
0.03
0.02
–
–
–
–
V
2
O
5
0.15
0.18
0.02
0.04
–
–
–
–
MgO
13.58
13.30
9.43
9.23
1.02
0.81
1.21
1.31
MnO
0.23
0.20
0.24
0.27
–
0.04
0.00
0.05
FeO
15.67
16.41
20.69
19.83
3.57
4.03
1.77
3.52
BaO –
–
–
–
–
–
0.12 0.13
Na
2
O
0.08
0.11
0.11
0.11
–
–
–
–
K
2
O
9.53
9.82
9.79
9.69
10.74
10.73
10.87
11.00
H
2
O
calc
4.00
3.96
3.91
3.94
4.37
4.42
4.52
4.35
F –
–
–
–
0.12
–
0.02
0.31
Total
99.10 99.15 99.69 99.77 99.50 99.29
100.42 100.01
Crystal-chemical formula calculated for 22 O
2–
Si
5.578
5.552
5.489
5.445
6.178
6.188
6.356
6.273
Al
IV
2.422
2.448
2.511
2.555
1.822
1.812
1.644
1.727
Al
VI
0.416
0.267
0.496
0.51
3.498
3.498
3.639
3.464
Ti
0.295
0.361
0.346
0.436
0.064
0.05
0.004
0.043
V
0.015
0.018
0.002
0.005
–
–
–
–
Cr
0.002
0.007
0.003
0.002
–
–
–
–
Mg
3.037
2.999
2.154
2.035
0.206
0.164
0.238
0.261
Mn
0.029
0.023
0.031
0.035
–
0.005
–
0.006
Fe
1.966
2.077
2.652
2.526
0.404
0.457
0.195
0.393
Ba –
–
–
–
–
–
0.006 0.007
Na
0.023
0.032
0.033
0.032
–
–
–
–
K
1.824
1.918
1.914
1.884
1.853
1.858
1.836
1.872
#fm
0.396
0.412
0.555
0.557
0.662
0.730
0.450
0.595
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(#fm = 0 .396—0.414 and Ti = 0.295—0.361 a.p.f.u.; Table 1),
quartz, allanite-epidote and titanite. Amphibole is represented
by tchermakite, tchermakitic-hornblende, ferrian-magnesio-
hornblende to magnesio-hornblende, locally overgrown by
secondary actinolite-tremolite (Table 2). Epidotes show nor-
mal zonation from allanite cores to REE-epidote on the rims
(Table 3), which is typical of high-pressure magmatic epi-
dote (Schmidt & Poli 2004). K-feldspar is present as a minor
component. Accessories are represented by Ti-magnetite—
ilmenite, zircon, and apatite. Secondary minerals are repre-
sented by zoned post-magmatic muscovite (#fm = 0.662—0.730;
Ti = 0.064—0.050 a.p.f.u.; Table 1) epidote and titanite.
The granitoids of suite 2 are leucocratic porphyritic alkali-
feldspar granites, showing cross-cutting relations to the
Goryczkowa type granitoid rocks (Fig. 2a). The most pro-
nounced feature of these granites is the presence of large (up
to 2 cm in length) crystals of pink perthitic alkali feldspars,
showing internal graphic intergrowths with quartz, all flowing
in a medium- to coarse-grained matrix of plagioclase (An
7—13
),
K-feldspar (Or
97
Ab
3
—Or
93
Ab
7
), quartz and abundant musco-
vite (Fig. 2c). Accessory phases comprise apatite, zircon and
monazite-(Ce). Muscovite is chemically zoned, with TiO
2
content in the range of 0.43—0.04 (0.040—0.004 a.p.f.u.) and
#fm = 0.450—0.595 (Table 1).
Geochemistry and geotectonic interpretation
The granodiorite—tonalite—quartz-diorite rocks (suite1) are
peraluminous (ASI = 1.11—1.26) with silica contents around
63—70 wt. %, calc-alkaline (Fig. 3a), characterized by
Na
2
O > K
2
O and low Rb/Sr ratio = 0 .05—0.12. In the Frost &
Frost (2008) geochemical classification these rocks belong
to the magnesian family (Fig. 3b). The chondrite-normalized
(Sun & McDonough 1989) REE patterns show moderate
LREE enrichment (Ce
N
/Yb
N
= 18.12—24.18) while an Eu
anomaly is almost absent (Eu/Eu* = 0.82—1.00; Table 4,
Fig. 4). Temperatures calculated on the basis of Zr-geother-
mometer of Watson & Harrison (1983) for these rocks are in
the range of 767—803 °C (Table 4).
Table 2: Chemical composition and crystal-chemical formulae of primary (Amph) and secondary (Trem—Act) amphibole crystals.
Component [wt. %]
Amph 1
Amph 2
Amph 3
Trem 1
Act 1
SiO
2
44.16
43.69
44.36
51.45
54.71
TiO
2
0.83
0.96
0.60
0.01
0.05
Al
2
O
3
10.59
10.99
10.62
2.82
0.89
Cr
2
O
3
0.00
0.02
0.03
0.00
0.02
FeO
16.14
16.11
15.27
13.76
13.86
MnO
0.50
0.52
0.41
0.45
0.68
MgO
11.33
11.06
11.97
16.09
14.55
CaO
11.77
11.72
10.83
10.46
12.12
Na
2
O 1.00
1.16
0.85
0.22
0.40
K
2
O
0.77
0.83
0.60
0.06
0.07
F
0.21
0.20
0.17
0.00
0.00
Cl
0.07
0.06
0.07
0.00
0.00
H
2
Oamp
1.80
1.78
1.78
2.02
2.06
Fe
2
O
3
(calc)
4.37
6.42
10.74
13.69
0.78
FeO
9.74
10.33
5.60
1.44
13.16
O=F,Cl
–0.11
–0.10
–0.09
0.00
0.00
Total 99.75
99.64
98.55
98.99
99.36
Formula per 23 O
2–
(13 cations)
Si 6.518
6.471
6.530
7.378
7.932
Al
IV
1.482
1.529
1.470
0.476
0.068
Al
VI
0.360
0.388
0.372
0.000
0.083
Ti 0.092
0.107
0.066
0.001
0.006
Cr 0.000
0.002
0.003
0.000
0.002
Fe
3+
0.784
0.716
1.190
1.478
0.085
Fe
2+
1.208
1.279
0.690
0.173
1.596
Mn 0.062
0.065
0.051
0.055
0.084
Mg 2.494
2.442
2.627
3.439
3.145
Ca 1.862
1.860
1.708
1.608
1.882
Na 0.287
0.333
0.243
0.062
0.111
K 0.144
0.157
0.113
0.010
0.013
(Na+K) (A)
0.293
0.350
0.113
0.010
0.013
Mg/(Mg+Fe
+2
) 0.674
0.656
0.792
0.952
0.663
Fe
+3
/(Fe
+3
+Al
VI
) 0.685
0.648
0.762
1.000
0.505
Species Mg-Hbl
Tschermakite
Mg-Hbl
Ferri-tremolitic
Hbl
Actinolite
T (°C)
873
885
865
605
618
uncertainty (σ
est
)
22
22
22
30
34
P(S) [kbar]
5.8
6.1
5.8
–
–
NNO
0.70
0.5
1.1
–
–
logfO
2
–11.70
–11.60
–11.4
–
–
uncertainty (σ
est
)
0.4
0.4
0.4
–
–
H
2
O
melt
[wt. %]
7.80
7.8
8.1
–
–
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The leucocratic porphyritic alkali feldspar granites of
suite 2 are peraluminous (ASI = 1.09—1.29) with silica con-
tent in the narrow range 70—73.8 wt. %, characterized by
K
2
O > Na
2
O as well as high Rb/Sr ratio =1.97—2.56 and plot in
a shoshonitic field (Fig. 3a). They plot as magnesian and fer-
roan melts (Fig. 3b). The chondrite-normalized REE diagram
shows a weak LREE enrichment (Ce/Yb)
N
= 1.94—5.69 and
negative Eu anomaly (Eu/Eu* = 0.419—0.709; Table 4,
Fig. 4). The leucogranites show low Zr and Y contents
(31.0—19.0 ppm and 6.3—1.5 ppm respectively). Tempera-
tures calculated on the basis of the Zr-geothermometer of
Watson & Harrison (1983) for this rock are in the range of
642—682 °C (Table 4).
Comparing both granite suites, the suite 1 granodiorite-to-
nalite is characterized by higher MgO, Fe
2
O
3
, TiO
2
, Ba, Zr,
Ce, Nd, Sm and Y concentrations then suite 2 leucogranites
(Table 4; Fig 5). Granite discrimination diagrams (Pearce et
al. 1984) point to a VAG (volcanic arc granites) geotectonic
Table 3: Representative microanalyses and crystal-chemical formulae (25 O
2—
) of magmatic epidote-allanite and secondary REE-epidote
minerals.
regime of all the analysed rocks (Fig. 6a,b). On a R1-R2 dia-
gram (Batchelor & Bowden 1985) the suite 1 granitoids plot
in the pre-plate collision field, while the suite 2 rocks could
be classified as late orogenic or anatectic granites (Fig. 3c).
Results of zircon investigations
Suite 1 granitoids (sample G1)
Zircon crystals are generally clear, colourless, and vary in
length from ca. 50 to 250 µm. All zircons are euhedral, dif-
fering only in their aspect ratios which range from 1:1 to 1:4
(Fig. 7). The characteristic feature of these crystals is the
high content of long-prismatic (length/width ratio >3) zir-
cons (43 %). In most zircons the [110] prism is better devel-
oped than [100], with the [211] bipyramid dominating over
the [101]. They correspond to subtypes L2—L3 and S2—S3
Magmatic epidote–allanite (Fig. 4c)
Secondary REE-epidote (Fig. 6c)
#1 #2 #3 #4 #1 #2 #3 #4
SiO
2
33.02 32.81 32.64 32.72 32.84 36.16 33.64 37.71
P
2
O
5
0.01 0.19 0.07 0.08 –
0.12 –
0.11
TiO
2
1.19 0.99 0.87 0.66 0.35 0.31 1.78 0.07
ThO
2
–
0.43 0.53 1.11 0.47 0.16 0.03 –
UO
2
0.06 –
0.06 –
0.07 –
–
–
Al
2
O
3
16.00 17.49 17.81 17.86 18.21 22.46 8.98 23.64
V
2
O
3
0.05 0.10 0.03 0.06 0.07 0.07 0.22 0.06
Fe
2
O
3
16.73 13.57 13.46 12.66 12.77 12.97 17.33 12.92
Y
2
O
3
0.01 0.03 0.02 0.03 0.13 0.06 –
–
La
2
O
3
3.63 4.66 4.14 3.39 2.42 0.51 0.04 0.06
Ce
2
O
3
8.58 8.25 8.24 7.24 6.74 1.55 –
0.05
Pr
2
O
3
1.08 0.56 0.68 0.71 1.13 0.15 –
–
Nd
2
O
3
3.07 2.81 2.84 3.38 4.36 1.18 –
0.05
Sm
2
O
3
0.19 0.47 0.14 0.34 0.44 0.17 –
0.05
Gd
2
O
3
0.22 0.07 0.19 0.13 0.34 0.01 0.15 0.02
MgO
0.49 1.08 1.01 0.88 0.87 0.14 0.04 0.04
CaO
13.63 14.26 14.44 14.76 14.60 20.48 35.10 23.16
MnO
0.22 0.25 0.31 0.25 0.31 0.33 0.22 0.21
Na
2
O
0.01 –
0.02 0.08 0.06 – 0.02 0.01
H
2
O
calc
1.68 1.68 1.68 1.66 1.67 1.82 1.72 1.89
Total
99.87 99.70 99.18 98.00 97.85 98.65 99.27 100.05
Crystal-chemical formulae recalculated for 25 O
2–
/16 cations
Si
5.905 5.843 5.834 5.895 5.909 5.946 5.854 5.990
P
0.002 0.029 0.011 0.012 –
0.017 –
0.014
Ti
0.161 0.132 0.116 0.089 0.047 0.038 0.234 0.008
Th
–
0.017 0.022 0.046 0.019 0.006 0.001 –
U
0.003
– 0.002
– 0.003
–
–
–
Al
3.372 3.671 3.752 3.793 3.862 4.353 1.842 4.425
V
0.006 0.014 0.005 0.008 0.010 0.009 0.031 0.007
Fe
2.251 1.818 1.811 1.716 1.729 1.605 2.270 1.544
Y
0.001 0.003 0.002 0.003 0.012 0.005 –
–
La
0.240 0.306 0.273 0.225 0.161 0.031 0.003 0.003
Ce
0.562 0.538 0.539 0.478 0.444 0.093 –
0.003
Pr
0.070 0.036 0.044 0.047 0.074 0.009 –
–
Nd
0.196 0.179 0.181 0.218 0.280 0.069 –
0.003
Sm
0.011 0.029 0.009 0.021 0.027 0.009 –
0.003
Gd
0.013 0.004 0.011 0.008 0.020 0.001 0.009 0.001
Mg
0.130 0.287 0.268 0.238 0.232 0.034 0.010 0.009
Ca
2.610 2.722 2.765 2.849 2.814 3.608 6.545 3.941
Mn
0.033 0.038 0.046 0.038 0.047 0.045 0.032 0.034
Na
0.002 –
0.005 0.029 0.022 0.000 0.008 0.003
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Fig. 3. Various plots of the Goryczkowa granites: a – plot on K
2
O
versus SiO
2
after Pecerillo & Taylor (1976); b – plot on FeO*/
(FeO* + MgO) versus SiO
2
after Frost & Frost (2008); c – multi-
cationic R1-R2 diagram after de La Roche et al. (1980). Fields
are numbered according to Batchelor & Bowden (1985): 1 – man-
tle fractionates, 2 – pre-plate collision suites, 3 – post-collision
suites, 4 – late orogenic magmas, 5 – anorogenic suites, 6 – syn-
collisional
(anatectic)
suites.
R1 = 4Si—11(Na + K)—2(Fe + Ti);
R2 = 6Ca + 2Mg + Al. Circles – granitoids from suite 1; Squares –
granitoids from suite 2.
Fig. 4. Rare earth elements patterns, normalized to C1 chondrite
(after Sun & McDonough 1989), in Goryczkowa granites. The shaded
areas show the range of REE patterns of quartz-diorites from the
Tatra Mountains (after Gawęda et al. 2005) and High Tatra monzo-
granites (after Gawęda 2009).
(Fig. 8a; Pupin 1980). CL investigations show that oscillatory
zoning is the prominent textural feature, with growth bands
varying between fine and broad within individual grains
(Fig. 9). Luminescence of growth zoning is variable and
mostly moderate. Sporadically, zircons are composed of
cores with well-developed oscillatory zoning, indicative of
original growth from the melt (Fig. 9; grains: G1_IV_11,
G1_III_02, G1_III_15). Some grains have interior domains
brighter compared with the external parts. These interior do-
mains have boundaries parallel to external oscillatory zoning
(Fig. 9; grains G1_IV_08, G1_III_10) as they are not consid-
ered to be inherited cores. The external domains occur mainly
as euhedral pyramidal tips with oscillatory zoning, which ap-
pear dark under CL (corresponding to relatively high U con-
tents and higher degrees of metamictization, Fig. 9).
Twenty two LA-MC-ICP-MS U-Pb measurements on
fourteen crystals were made (Fig. 9; Table 5). All data points
are concordant within the assigned error (Fig. 10). Sixteen
analyses from the oscillatory-zoned zircon yield a concordia
age of 371 ± 6.0 Ma (MSWD = 1.6, Fig. 10a, group A). Four
inherited cores plot as 433 ± 21 Ma (MSWD = 3.1, Fig. 10b,
group B) and two other give an age of ca. 2650 Ma and
2530 Ma (Table 5).
Suite 2 granitoids (sample G2)
The zircons are euhedral, mainly normal-prismatic crys-
tals with aspect ratio 1 : 2 to 1 : 6. Grain size varies in length
from ca. 50 to 250 µm (Fig. 11). Zircons appear clear, co-
lourless to pink. In most crystals [110] prisms are better de-
veloped than [100] and the [211] bipyramid dominates over
the [101], what make them very similar to the population of
the suite 1 (Figs. 8a,b). The main difference from the
suite 1 is that some of crystals show larger [100] prisms and
[211] pyramids. These features correspond to subtypes J2
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Table 4: Chemical composition and selected petrological indica-
tors of granitoid rocks from the crystalline cores, Tatra Moun-
tains. Major element and trace element concentrations in wt. %
and ppm, respectively. Explanations: G – Goryczkowa crystalline
core; M – Małołączniak crystalline core; LOI – lost of ignition;
Eu/Eu* = Eu/( Sm·Gd); ASI=Al
2
O
3
/(CaO + Na
2
O + K
2
O—3.33 P
2
O
5
)
in molecular units.
(Fig. 12, crystal G2_III_02) and S22 (Pupin 1980). Most
grains are characterized by well-developed oscillatory zon-
ing, ranging from fine to broad and display variable lumi-
nescence. The majority of grains lack discernible, inherited
cores, but where preserved, cores are rounded, zoned and
distinct from enclosing rims by virtue of luminescence and
truncated zoning (Fig. 12; grains G2_IIb_15, G2_III_12).
These features suggest that the internal domains are detrital
zircon cores that underwent physical abrasion before the
formation of the overgrowth. The cores sometimes make up
about 80—90 % of the grains by volume, although most fre-
quently the overgrowths predominate. The cores show
well-developed oscillatory zoning indicating an igneous
(felsic) source. The boundary between core and overgrowth
is marked by an irregular light band (Fig. 12; grains
G2_IIb_15, G2_III_12).
Seventeen LA-MC-ICP-MS U-Pb measurements on thir-
teen crystals were made (Fig. 12; Table 6). All data points
are concordant within the assigned error. Twelve spot anal-
yses span a range in dates from 387 to 350 Ma, with five
inherited cores giving substantially older dates of ca.
1780 Ma and 420 Ma (Fig. 12; Table 6). Nine analyses
from the oscillatory-zoned zircon (subtype L2-S3) yield a
concordia age of 350 ± 4.7 Ma (MSWD = 0.68; Figs. 12, 13;
Table 6 – group A) while three analyses from the oscillatory-
zoned zircon (subtype J2-S22) yield a concordia age of
387 ± 11 Ma (MSWD = 2.9; Figs. 12, 13; Table 6 – group B).
Two inherited cores yield an age of 412 ± 9 Ma (MSWD = 3;
Fig. 12; Table 6 – group C), two others are discordant and
one yields a concordant age of ca. 1773 ± 55 (Fig. 12; Ta-
ble 6 – groups D and E).
Fig. 5. Primitive mantle normalized (after Sun & McDonough 1989) trace element diagram of analysed granitoids. G – Goryczkowa crys-
talline core; M – Małołączniak crystalline core.
Suite 1
Suite 2
Sample
No.
G1 G3 M5 G2 G4 M6
SiO
2
66.34 63.61 70.87 73.94 73.1
73.87
TiO
2
0.56 0.75 0.29 0.06 0.03 0.02
Al
2
O
3
16.82 17.47 15.53 14.62 15.06 13.91
Fe
2
O
3T
3.65 4.48 2.25 0.78 0.42 0.46
MnO
0.06 0.07 0.04 0.02 0.005 0.08
MgO
1.48 1.59 1.08 0.18 0.09 0.00
CaO
2.71 4.03 1.67 0.41 0.58 0.44
Na
2
O
4.26 4.52 4.17 2.86 2.89 3.81
K
2
O
2.46 1.55 2.52 5.91 6.68 5.46
P
2
O
5
0.21 0.29 0.12 0.21 0.13 0.09
LOI
1.30 1.40 1.20 1.00 1.00 0.68
Total
99.85 99.76 99.74 99.99 99.985 98.82
Sr
632.8
838.2
603.2 81.3
79.8
42.0
Ba
780.9 550
1234
418.9
179
213.0
Rb
78.9
41.3
52.3 208.9
157.5
90.0
Th
10.2
11.2
7.0 3.5
1.6
0.54
U
1.8
1.3
1.3 1.1
2.8
0.63
Ga
20.5
18.5
17.3 20.6
14.6
12.0
Ni
7.1
5.3
5.5 2.6
1.1
9.0
Cr
75
130
13.7 89
48
33
Zr
171
155.7
124
31
25.2
19
Hf
4.8
4.3
3.4 1.4
1.5
1.0
Y
9.8
7.3
8.3 6.3
4.6
1.5
Nb
7.4
5.4
3.5 10.5
10.5
1.3
Ta
0.6
0.2
0.3 1.4
5.1
1.2
La
26.3
28.6
23.6 3.6
1.7
2.1
Ce
58.9
58.8
48
9.3
4.3
5.3
Pr
7.04 6.23 5.51 1.26 0.5
0.6
Nd
27
25.2
20.5 4.8
2.1
2.11
Sm
4.5
4.03 3.44 1.5
0.48 0.58
Eu
0.93 1.15 0.92 0.32 0.06 0.1
Gd
2.68 3.05 2.77 1.27 0.4
0.63
Tb
0.43 0.38 0.33 0.24 0.12 0.13
Dy
1.91 1.67 1.65 1.18 0.65 0.63
Ho
0.28 0.29 0.28 0.19 0.12 0.14
Er
0.85 0.71 0.71 0.46 0.46 0.42
Tm
0.13 0.11 0.11 0.07 0.09 0.1
Yb
0.78 0.67 0.73 0.45 0.61 0.65
Lu
0.11 0.09 0.11 0.07 0.11 0.11
ASI
1.193 1.109 1.259 1.289 1.183 1.090
Na
2
O/K
2
O 1.732 2.916 1.655 0.484 0.433 0.698
Rb/Sr
0.125 0.049 0.087 2.569 1.974 2.143
Nd/Th
2.647 2.250 2.929 1.371 1.313 3.907
REE
131.84 130.98 108.66 24.71 11.7
13.6
Eu/Eu*
0.819 1.003 0.911 0.709 0.419 0.506
Ce
N
/Yb
N
20.806 24.181 18.117 5.694 1.942 2.247
T
Zr
[°C]
793
768
780
682
663
643
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Fig. 7. Secondary electron (SEM) images of selected zircon crystals from granodiorite (sample G1– suite 1). Zircon crystals with numbers
in frames are also imaged by CL in Figure 9. See text for description.
Fig. 6. Plot of the Goryczkowa granites in the Pearce et al. (1984) discrimination diagrams. Abbreviations: VAG – volcanic arc granites,
syn-COLG – syn-collisional granites, WPG – within-plate granites, ORG – ocean ridge granites. Circles – granitoids from suite 1;
Squares – granitoids from suite 2.
Fig. 8. Typological frequency distribution of euhedral zircon crystals from (a) granodiorite, sample G1, suite 1, and from (b) leucogranite,
sample G2, suite 2 (according to the classification of Pupin 1980).
428
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Fig. 9. Compiled cathodoluminescence (CL) images showing the range of textures observed in zircon crystals from granodiorite
(sample G1 – suite 1). See text for details. The white rectangles and circles show the approximate location of laser ablation trenches (con-
firmed by re-inspecting grains under cathodoluminescence after the dating session) and are not to scale. The numbers refer to the analytical
data presented in Table 5.
Fig. 10. Concordia plots of LA-MC-ICP-MS U-Pb zircon analytical results from granodiorite (sample G1 – suite 1). Open error ellipses
are isotope ratios of individual grain spots: a – the main group of analyses (n = 11) of oscillatory zoned zircons; b – inherited cores
(xenocrysts) with oscillatory, magmatic zoning. Inherited cores at ca. 2560 Ma not shown on diagram. Thick error ellipse corresponds to
the 2 and 95% confidence errors of the calculated concordia ages.
429
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Fig. 11. Secondary electron (SEM) images of selected zircon crystals from leucogranite (sample G2 – suite 2). Zircon crystals with num-
bers in frame are also imaged by CL in Figure 12. See text for description.
Table 5: LA-MC-ICP-MS U-Pb zircon data from granodiorite (sample G1 – suite 1). Explanations: * – final blank corrected intensities
in µV; # – final blank corrected intensities in mV; 2SD – the 2 sigma standard deviation (in percent); Rho – error-correlation between
the
206
Pb/
238
U and
207
Pb/
235
U ratios.
Discussion
Ages of granitoids
The zircon LA-MC-ICP-MS U-Pb data from suite 1 pro-
vide the first constraint on the crystallization ages of the
Goryczkowa type granitoids at ca. 371 ± 6.0 (Fig. 10a; Ta-
ble 5). This age is older than the Rb-Sr isochron age of
300 Ma given by Burchart (1968, 1970) and comparable
with the upper limit of granitoid magmatism in the Gorycz-
kowa Unit (ca. 370 Ma) suggested by Kohút & Siman
(2011). The Late Devonian age was also obtained from a to-
nalite in the Branisko Mts (Kohút et al. 2010), from hybrid
granitoids in the Western Tatra Mts (Burda et al. 2011) and
from an enclave-bearing tonalite and associated dykes of the
Tribeč Mts (Broska et al. 2013).
Zircon crystals from suite 2 (sample G2) are character-
ized by oscillatory zoning with intermittent dissolution sur-
faces (Fig. 12) representing corrosion or resorption events
during evolution of a zircon crystal (e.g. Vavra 1990,
Final blank corrected intensities
Final mass bias and common Pb corrected ratios
Concordia
Group File name
204
Pb
*
206
Pb
#
207
Pb
#
238
U
#
207
Pb/
206
Pb 2SD (%)
207
Pb/
235
U 2SD (%)
206
Pb/
238
U 2SD (%) Rho age (Ma)
G1_IV_01/1
2.495 0.383 0.031 16.76
0.0550
9.2
0.4641
17.7
0.0608
15.7
0.48
G1_IV_01/2
1.896 1.359 0.085 39.45
0.0580
4.8
0.4723
11.3
0.0593
10.2
0.13
G1_IV_03/1
0.895 0.562 0.046 25.34
0.0530
5.4
0.4187
10.4
0.0561
9.2
0.49
G1_IV_03/2
2.561 1.777 0.105 52.16
0.0560
3.0
0.4459
5.8
0.0576
5.1
0.19
G1_IV_08/1
1.069 0.263 0.024 11.77
0.0616
2.5
0.4848
8.9
0.0599
4.3
0.27
G1_IV_08/2
7.209 1.407 0.101 47.16
0.0695
15.6
0.4949
34.3
0.0599
24.6
0.10
G1_IV_10/1
0.607 0.692 0.056 30.03
0.0532
5.4
0.4440
10.4
0.0600
9.2
0.59
G1_IV_10/2
0.730 0.122 0.011 5.37
0.0564
3.7
0.4640
7.4
0.0597
6.4
0.37
G1_IV_11/1
1.138 0.208 0.019 10.53
0.0599
10.2
0.4261
20.2
0.0565
17.7
0.45
G1_III_02/1
2.015 0.261 0.024 11.51
0.0577
2.7
0.4285
5.2
0.0580
4.6
0.41
G1_III_04/1
1.964 2.413 0.138 75.30
0.0561
7.4
0.4388
14.4
0.0583
12.7
0.38
G1_III_06 2.452
4.183
0.252
123.85 0.0549 14.9 0.4445 28.9 0.0584 25.5 0.21
G1_III_10/1
1.369 1.236 0.072 36.64
0.0564
24.4
0.4325
47.4
0.0569
41.9
0.50
G1_III_10/2
1.858 0.610 0.039 19.66
0.0643
5.5
0.4948
10.8
0.0591
9.1
0.06
G1_III_16
1.434 1.423 0.089 41.75
0.0591
9.0
0.5174
18.3
0.0624
15.9
0.41
A
G1_III_25
0.701 0.386 0.032 17.68
0.0568
4.0
0.4266
7.8
0.0585
6.9
0.65
371 ± 6.0
G1_IV_11/2
0.980 0.816 0.051 22.07
0.0619
6.1
0.5416
11.8
0.0650
10.4
0.63
G1_IV_15
2.754 0.326 0.028 9.58
0.0715
73.4
0.5508
14.2
0.0685
12.6
0.11
G1_III_02/2
0.586 0.281 0.024 10.47
0.0557
7.6
0.5341
14.8
0.0699
13.0
0.49
B
G1_III_04/2
2.306 0.299 0.027 8.75
0.0765
9.8
0.5903
20.8
0.0690
15.0
0.06
433 ± 21
G1_III_09
4.966 14.01 2.591 53.22
0.1705
2.6
11.057
5.0
0.4690
4.4
0.54 2529 ± 47
C
G1_III_15
3.663 15.21 2.976 50.71
0.1801
3.9
12.595
8.1
0.4990
7.1
0.44 2648 ± 76
430
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Fig. 12. Cathodoluminescence (CL) images of selected zircon crystals from leucogranite (sample G2). All grains have a prismatic habitus
characteristic for a magmatic origin. See text for description. The white rectangles and circles show the approximate location of laser abla-
tion trenches and are not to scale. The numbers refer to the analytical data presented in Table 6.
1994). These crystals belong to two typological groups on
the Pupin’s (1980) diagram (Fig. 8b). The first typology
group (L2—L3 to S2—S3 subtypes) with intermittent disso-
lution surfaces, plots in the upper part of the diagram and
yields a concordia age of 350 ± 5 Ma (Figs. 8b, 13a). The
second group plots in the lower part of the typology dia-
gram (S22 and J2 subtypes) and yields an age of
387±11 Ma (Figs. 8b, 13b).
In both suites inherited cores giving substantially older
dates of 433 ± 21 Ma (suite 1; Table 5) and 412 ± 9 Ma (suite 2;
Table 6) indicate the presence of a magmatic component in
the melted source. These ages are in agreements with the
whole-rock Rb-Sr dating (413 Ma) and support the early
thesis about the Early Silurian age of the thermal event in
the Tatra Mountains (Burchart 1968, 1970). Similar ages
from oscillatory zoned zircon cores, indicating Caledonian
(450—460 Ma) magmatism, found recently in the High
Tatra Mts (Burda et al. 2013), are in accordance with find-
ings of Late Ordovician-Early Silurian magmatic episodes
in the Veporic crystalline complex (ca. 470 Ma; Janák et al.
2002; Gaab et al. 2003) and Tatric crystalline basement
(450 and 430 Ma; Kohút et al. 2008; Putiš et al. 2009).
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Table 6: LA-MC-ICP-MS U-Pb zircon data from leucogranite (sample G2 – suite 2). Explanations: * – final blank corrected intensities
in µV; # – final blank corrected intensities in mV; 2SD – the 2 sigma standard deviation (in percent); Rho – error-correlation between
the
206
Pb/
238
U and
207
Pb/
235
U ratios.
Fig. 13. Concordia plots of LA-MC-ICP-MS U-Pb zircon analytical results from leucogranite (sample G2 – suite 2). Open error ellipses
are isotope ratios of individual grain spots: a – the main group of analyses (n = 9) of oscillatory zoned zircons (zircon L2—S3) with moderate
luminescence; b – xenocrysts (zircons J2—S22) with oscillatory, magmatic zoning. Inherited cores at ca. 1780 Ma and 420 Ma not shown
on the diagram. Thick error ellipse corresponds to the 2 and 95% confidence errors of the calculated concordia ages.
That allow us to suggest possible connections to the Rebra-
Tulghes Terrane (Inner Eastern Carpathians), which docked
to the SW margin of Baltica (Balintoni et al. 2009) and the
470—460 Ma magmatic episode in the Somes Terrane of the
Southern Carpathians (Apuseni Mountains; Balintoni et al.
2010) and consequently shows the intense, collision-related,
tectono-magmatic event. The presence of “Caledonian”
magmatic zircons also poses a question about the plate dy-
namics in the Circum-Carpathians area in the Early Paleozoic
and participation of the Avalonian-Cadomian crust in the
Variscan tectono-thermal episodes (see discussion in: Gawęda
& Golonka 2011).
Problem of source rocks and tectonic setting of the grani-
toid magma
Major elements chemistry, as proved by Patiño Douce
(1999), can indicate the character of melted material. Melts
derived from amphibolites and mafic pelites have lower al-
kali and aluminium contents, but are enriched in calcium,
titanium, iron and magnesium. Suite 1 granitoids are, how-
ever, peraluminous, which is typical of melted felsic sources.
Suite 1 granitoids plot in the field of melts generated from am-
phibolite—pelite sources (calc-alkali I-type granites; Patiño
Douce 1999; Fig. 14).
Final blank corrected intensities (in V)
Final mass bias and common Pb corrected ratios
Concordia
Group File name
204
Pb
*
206
Pb
#
207
Pb
#
238
U
#
207
Pb/
206
Pb 2SD (%)
207
Pb/
235
U 2SD (%)
206
Pb/
238
U 2SD (%) Rho age (Ma)
G2_IIb_03 0.984 0.413 0.017 9.97 0.0540 1.6 0.4101 3.0 0.0550 2.7 0.44
G2_IIb_15/1 1.271 1.741 0.106 62.37 0.0544 4.6 0.4103 9.0 0.0552 7.9 0.32
G2_III_08/1 1.110 0.413 0.017 10.40 0.0545 2.8 0.4112 5.4 0.0545 4.8 0.17
G2_III_08/2 0.902 0.500 0.041 22.26 0.0558 3.3 0.4285 6.5 0.0566 5.7 0.30
G2_III_11 0.981 0.526 0.041 22.88 0.0534 3.7 0.4129 7.1 0.0557 6.3 0.52
G2_III_12/1 0.675 0.304 0.013 7.43 0.0525 3.9 0.4154 7.6 0.0575 6.7 0.29
G2_III_20 1.398 0.413 0.017 9.80 0.0539 3.2 0.4171 6.2 0.0567 5.5 0.43
G2_IV_01 1.206 0.208 0.017 9.21 0.0574 3.4 0.4231 6.6 0.0561 5.8 0.38
A
G2_IV_04/1 0.755 0.704 0.039 23.77 0.0527 4.1 0.4016 8.0 0.0563 7.0 0.27
350 ± 4.7
G2_III_02 1.126 1.242 0.076 36.11 0.0552 9.4 0.4564 11.1 0.0618 9.0 0.30
G2_III_06 0.941 0.236 0.021 10.38 0.0616 2.4 0.4790 4.7 0.0612 4.1 0.35
B
G2_IV_03 1.662 0.841 0.060 28.00 0.0604 5.0 0.4667 10.0 0.0590 8.6 0.27
387 ± 11
G2_III_10 1.356 0.234 0.021 9.65 0.0617 3.0 0.5185 5.8 0.0646 5.1 0.24
C
G2_III_14 1.096 0.763 0.061 28.88 0.0551 1.8 0.5048 3.5 0.0653 3.1 0.41 412 ± 9
G2_IIb_15/2 4.029 0.705 0.068 17.17 0.0897 11.3 0.8751 22.0 0.0679 19.5 0.51
D
G2_IV_04/2
10.697 1.708 0.185 55.88 0.1106 22.3 0.8626 44.6 0.0567 37.1 0.08 disc.
E
G2_III_12/2 3.003 7.271 0.875 42.41 0.1110 3.4 4.7313 6.6 0.3185 5.8 0.57
1773 ± 55
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Fig. 14. Chemical composition of Goryczkowa granitoids in major
oxide diagrams after Patiño Douce (1999). Outlined fields denote
compositional fields of experimental melts derived from partial
melting of felsic pelites, metagreywackes and amphibolites. Circ-
les – granitoids from suite 1; Squares – granitoids from suite 2.
Computed oxygen fugacity, expressed as logfO
2
, falls in the
narrow range from —10.4 to —11.7, and the computed water
content in the melt was at 7.8—8.1 wt. % (Ridolfi et al. 2010;
Table 2). The oxygen fugacity is higher in relation to values
computed for I-type granites from the Inner Carpathians and
High Tatra Mountains (compare: Gawęda 2009; Broska &
Petrík 2011). Calculations of the accessible published data
point out that the relatively similar oxygen fugacities (logfO
2
in the range of —12 to —13) could be found in the hybrid
quartz-diorites and associated granitoids from the Western
Tatra Mountains (Burda et al. 2011). High oxygen fugacity in
suite 1 could be interpreted as the primary magmatic feature,
as high-Ca plagioclase is preserved (An
45—62
), so magmatic
deanorthitization process, proposed by Broska & Petrík
(2011) was observed only sporadically. Pressure—temperature
calibrations, based on amphibole and plagioclase composi-
tions, indicated 5.8—6.3 kbar (Schmidt 1992) and 780—810 °C
(Blundy & Holland 1990), which agree with Zr-geothermo-
metry (Table 4). The calculations are consistent with the pres-
ence of magmatically zoned allanite-epidote, which is stable
in dioritic-tonalitic magmas in pressures above 6 kbars with
water content near 9 wt. % and oxygen fugacity above QMF
(Quartz-Magnetite-Fayalite) buffer (Schmidt & Poli 2004).
This all suggests at least lower crustal/upper mantle prov-
enance of the melt parental for the suite 1 granitoids. Such
contradictory features and source rocks interpretations are
typical of magmas resulting from mixing/mingling of differ-
ent magmas (compare Burda et al. 2011) and these complex
processes could be suggested for the suite 1 granitoids.
In contradiction, suite 2 granitoids show simple mineral
composition as well as enrichment in alkali and alumina,
typical of muscovite-dehydration partial melting of felsic
pelites (Patiño Douce 1999; Fig. 14), which is consistent
with simple mineral composition and peraluminous charac-
ter (Table 4), while rock-textures suggest disequilibrium at
the early stages of crystallization (Fig. 2c).
The contrasting features of both granitoid suites are in
agreement with their geotectonic positions on R1-R2 dia-
gram (Fig. 3c).
Trace elements also support the difference between grani-
toids: suite 1 shows low Rb/Sr and high Nd/Th ratios, typical
of lower crustal or mantle-related melts, while high Rb/Sr, to-
gether with lower Nd/Th point out upper crustal, highly frac-
tionated character of the suite 2 granitoids. The higher LREE
content in suite 1 (Fig. 5) and consequently higher REE frac-
tionation (Fig. 4; Table 4) is a consequence of the allanite-
epidote presence (Table 3), sporadically associated with
monazite, governing the REE budget in oxidized magmas.
Primitive mantle-normalized [Th/U]
N
ratios in suite 1 grani-
toids are relatively high (1.3—2.13), while positive U anomaly
[Th/U]
N
ratios in the range of 0.14—0.78 is typical of suite 2
granitoids (Fig. 5). As uranium is usually mobilized in highly
oxidized melts, the predominace of Th over U in suite 1
granitoids might reflect a contribution from relatively Th-en-
riched mantle and/or crustal fluids during melting (Kemp &
Hawkesworth 2005), supported by the predominance of Th
over U in magmatic epidote (Table 3). However, the common
presence of secondary muscovite, influencing the ASI value,
might also cause the mobilization of some elements.
Both granitoids show VAG affinity (Fig. 6a,b) which is
typical of Central European granitoid magmatism (Finger et
al. 1997; Gawęda & Golonka 2011). In primitive mantle-
normalized multi-element diagrams (Sun & McDonough
1989) negative Nb and Ta anomalies in suite 1 granitoids are
more prominent, suggesting typical arc setting (Thirwall et
al. 1994), while granitoids of suite 2 show only Nb negative
anomaly while Ta is enriched (Fig. 5), suggesting another
process (fractional crystallization?), overlapping the typical
source characteristic.
The problem of zircon inheritance
The distributions of inherited zircon cores in both rock
suites also support the observed differences. In suite 1
granitoids the magmatic inherited cores (433 Ma) pre-
vailed, while only two inherited cores pointing to ages of
ca. 2659—2530 Ma were found. In suite 2 leucogranites the
inherited zircon crystals, showing ages older than Variscan,
form a population with a broad spectrum of inherited core
ages (1780—387 Ma). Such variation can be expected in
melts derived from mainly metasedimentary precursors and
are reconciled with crustal heterogeneity.
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In low temperature melts the zircon solubility is conse-
quently low and most of the pre-existing zircon crystals
might remain undissolved. This allows preservation of the
inherited components (Scott et al. 2011), but it does not ex-
plain why no new overgrowths were formed on pre-existing
zircon crystals. Additionally, the presence of older, inherited
components required the assimilation of the country rocks.
That opens the problem of the energy, necessary for the as-
similation. Whatever is the mechanism of assimilation: the
mechanical disintegration or chemical dissolution, it is an
energy-consuming process, resulting in a considerable de-
gree of crystallization, what makes the magma relatively im-
mobile (Clemens & Stevens 2012). On the other hand, if the
magma brings enough heat and vapour pressure for country
rocks assimilation and contamination (e.g. by MASH
process = Melting, Assimilation, Storage and Homogeniza-
tion, supposed to occur during deep-seated melting), the par-
tial corrosion of the older zircon crystals should be observed,
followed by later magmatic overgrowths, as is commonly
noted (e.g. Gawęda 2008; Burda & Klötzli 2011). Such a
process can be avoided when inherited zircon crystals (J2
and S22 in the morphology diagram) are sheltered by the so-
called resister minerals (biotite, opaques, etc.; Chappell et al.
1987; Burda & Gawęda 2009), which are, however, absent
in the case of suite 2. In that case, to explain the presence of
a population of 387 Ma zircon crystals we assume the suite 2
represent the trapped magma portions, possibly associated
with disintegrated (exploded?) xenoliths (e.g. Gawęda 2007;
Gawęda & Szopa 2011), which possibly crystallized in dise-
quilibrium conditions. That could explain the presence of
graphic intergrowths of K-feldspars and quartz, typical of
disequilibrium growths and also the lack of corrosion/over-
growths on the 387 Ma zircon crystals.
Another aspect of inherited zircon presence could be visi-
ble in REE fractionation, which is anomalously low in
leucogranites of suite 2 (Fig. 4, Table 4). In case of the ana-
tectic melts flat REE patterns can be caused by the resister
minerals, like apatite consuming mainly LREE and zircon
carrying mainly HREE (e.g. Burda & Gawęda 2009).
Conclusions
1. The presented geochemical and geochronological re-
sults indicate that both granitoid suites, present in the
Goryczkowa and Małołączniak crystalline cores in the West-
ern Tatra Mountains, were formed in a VAG (volcanic arc
granites) tectonic setting, however, they represent two differ-
ent magmatic stages. Suite 1 granitoids were formed as a re-
sult of melting of amphibolite and/or mafic pelite, possible
during high temperature pre-plate collisional stage and intrud-
ed at ca. 371 ± 6 Ma. Suite 2 leucogranites represent melts
generated by muscovite-dehydration melting of felsic pelites
during late orogenic/anatectic event and intrusion at ca.
350 ± 5 Ma.
2. The presence of magmatic U-Pb zircon ages around
387 Ma supports the existence of a LP-HT partial melting
episode in the Tatra Mountains crystalline core in the Early
Devonian, predating the granitoid emplacement.
3. The abundance of inherited zircon crystals, primitive
trace elements chemistry, together with disequilibrium-related
rock structures, could be interpreted as a result of perturba-
tion in the crystallization course (undercooling, viscosity in-
crease, disequilibrium crystallization). That brings an
additional question about the reliability of temperature cal-
culation based on Zr content and importance of the REE dia-
grams interpretation in contaminated magmas.
4. The Goryczkowa type granitoids represent the same
magmatic episode and similar petrographical/geochemical
characteristics as described from Western Tatra Mountains
so distinguishing the Goryczkowa type as a separate type of
granite is not necessary.
5. The presence of inherited zircon cores, dated ca. 430—
410 Ma, in both granitoid suites, is a trace of the Avalonia—
Baltica collision, and suggests that melting of the Laurussia
continental crust participated in granitoid magma formation.
Acknowledgments: The Polish Ministry of Sciences and
Higher Education sponsored the investigations, by MNiSW
Grant No. 2 P04D 003 29 (given to JB) and MNiSW Grant
No. N 307 027837 and DEC-2012/07/B/ST10/04366 (given
to AG). Additional funds from Austrian Science Fund FWF
(START Project 267-N11 and Project P18202-N10 given to
UK) is deeply acknowledged. Ewa Teper MSc is thanked for
the assistance during CL investigations, while Piotr
Dzierżanowski PhD and Mrs Lidia Jeżak are thanked for
their help during microprobe work. Comments provided by
the journal reviewers to anonymous referee, Milan Kohút
and Monika Kusiak are gratefully acknowledged.
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