GeolCarp_Vol64_No6_419

www.geologicacarpathica.sk

GEOLOGICA CARPATHICA

, 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

, ALEKSANDRA GAWĘDA

and URS KLÖTZLI

University of Silesia, Faculty of Earth Sciences, Będzińska 60, 41-200 Sosnowiec, Poland;

jolanta.burda@us.edu.pl; aleksandra.gaweda@us.edu.pl

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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BURDA, GAWĘDA and KLÖTZLI

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GEOLOGICA CARPATHICA, 2013, 64, 6, 419—435

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

10—6

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

37.18 36.70 35.82 35.75 45.67 45.58

48.01

46.08

TiO

2.62

3.18

3.00

3.81

0.63

0.49

0.04

0.43

16.05

15.23

16.65

17.08

33.38

33.19

33.86

32.83

0.01

0.06

0.03

0.02

–

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

0.08

0.11

–

9.53

9.82

9.79

9.69

10.74

10.73

10.87

11.00

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–

5.578

5.552

5.489

5.445

6.178

6.188

6.356

6.273

2.422

2.448

2.511

2.555

1.822

1.812

1.644

1.727

0.416

0.267

0.496

0.51

3.498

3.639

3.464

0.295

0.361

0.346

0.436

0.064

0.05

0.004

0.043

0.015

0.018

0.002

0.005

–

0.002

0.007

0.003

0.002

–

3.037

2.999

2.154

2.035

0.206

0.164

0.238

0.261

0.029

0.023

0.031

0.035

–

0.005

–

0.006

1.966

2.077

2.652

2.526

0.404

0.457

0.195

0.393

Ba –

–

0.006 0.007

0.023

0.032

0.033

0.032

–

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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GEOLOGICA CARPATHICA, 2013, 64, 6, 419—435

(#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

—Or

), quartz and abundant musco-

vite (Fig. 2c). Accessory phases comprise apatite, zircon and
monazite-(Ce). Muscovite is chemically zoned, with TiO

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

O > K

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

/Yb

= 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

44.16

43.69

44.36

51.45

54.71

TiO

0.83

0.96

0.60

0.01

0.05

10.59

10.99

10.62

2.82

0.89

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

O 1.00

1.16

0.85

0.22

0.40

0.77

0.83

0.60

0.06

0.07

0.21

0.20

0.17

0.00

0.07

0.06

0.07

0.00

Oamp

1.80

1.78

2.02

2.06

(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

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

1.482

1.529

1.470

0.476

0.068

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

0.784

0.716

1.190

1.478

0.085

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

) 0.674

0.656

0.792

0.952

0.663

/(Fe

+Al

) 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

)

P(S) [kbar]

5.8

6.1

5.8

–

NNO

0.70

0.5

1.1

–

logfO

–11.70

–11.60

–11.4

–

uncertainty (σ

est

)

0.4

–

melt

[wt. %]

7.80

7.8

8.1

–

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GEOLOGICA CARPATHICA, 2013, 64, 6, 419—435

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

O > Na

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)

= 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

, TiO

, 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

33.02 32.81 32.64 32.72 32.84 36.16 33.64 37.71

0.01 0.19 0.07 0.08 –

0.12 –

0.11

TiO

1.19 0.99 0.87 0.66 0.35 0.31 1.78 0.07

ThO

–

0.43 0.53 1.11 0.47 0.16 0.03 –

0.06 –

0.07 –

–

16.00 17.49 17.81 17.86 18.21 22.46 8.98 23.64

0.05 0.10 0.03 0.06 0.07 0.07 0.22 0.06

16.73 13.57 13.46 12.66 12.77 12.97 17.33 12.92

0.01 0.03 0.02 0.03 0.13 0.06 –

–

3.63 4.66 4.14 3.39 2.42 0.51 0.04 0.06

8.58 8.25 8.24 7.24 6.74 1.55 –

0.05

1.08 0.56 0.68 0.71 1.13 0.15 –

–

3.07 2.81 2.84 3.38 4.36 1.18 –

0.05

0.19 0.47 0.14 0.34 0.44 0.17 –

0.05

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

0.01 –

0.02 0.08 0.06 – 0.02 0.01

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

5.905 5.843 5.834 5.895 5.909 5.946 5.854 5.990

0.002 0.029 0.011 0.012 –

0.017 –

0.014

0.161 0.132 0.116 0.089 0.047 0.038 0.234 0.008

–

0.017 0.022 0.046 0.019 0.006 0.001 –

0.003

– 0.002

– 0.003

–

3.372 3.671 3.752 3.793 3.862 4.353 1.842 4.425

0.006 0.014 0.005 0.008 0.010 0.009 0.031 0.007

2.251 1.818 1.811 1.716 1.729 1.605 2.270 1.544

0.001 0.003 0.002 0.003 0.012 0.005 –

–

0.240 0.306 0.273 0.225 0.161 0.031 0.003 0.003

0.562 0.538 0.539 0.478 0.444 0.093 –

0.003

0.070 0.036 0.044 0.047 0.074 0.009 –

–

0.196 0.179 0.181 0.218 0.280 0.069 –

0.003

0.011 0.029 0.009 0.021 0.027 0.009 –

0.003

0.013 0.004 0.011 0.008 0.020 0.001 0.009 0.001

0.130 0.287 0.268 0.238 0.232 0.034 0.010 0.009

2.610 2.722 2.765 2.849 2.814 3.608 6.545 3.941

0.033 0.038 0.046 0.038 0.047 0.045 0.032 0.034

0.002 –

0.005 0.029 0.022 0.000 0.008 0.003

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GEOLOGICA CARPATHICA, 2013, 64, 6, 419—435

Fig. 3. Various plots of the Goryczkowa granites: a – plot on K

versus SiO

after Pecerillo & Taylor (1976); b – plot on FeO*/

(FeO* + MgO) versus SiO

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

426

BURDA, GAWĘDA and KLÖTZLI

GEOLOGICA CARPATHICA

GEOLOGICA CARPATHICA, 2013, 64, 6, 419—435

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

/(CaO + Na

O + K

O—3.33 P

)

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

66.34 63.61 70.87 73.94 73.1

73.87

TiO

0.56 0.75 0.29 0.06 0.03 0.02

16.82 17.47 15.53 14.62 15.06 13.91

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

4.26 4.52 4.17 2.86 2.89 3.81

2.46 1.55 2.52 5.91 6.68 5.46

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

632.8

838.2

603.2 81.3

79.8

42.0

780.9 550

1234

418.9

179

213.0

78.9

41.3

52.3 208.9

157.5

90.0

10.2

11.2

7.0 3.5

1.6

0.54

1.8

1.3

1.3 1.1

2.8

0.63

20.5

18.5

17.3 20.6

14.6

12.0

7.1

5.3

5.5 2.6

1.1

9.0

130

13.7 89

171

155.7

124

25.2

4.8

4.3

3.4 1.4

1.5

1.0

9.8

7.3

8.3 6.3

4.6

1.5

7.4

5.4

3.5 10.5

10.5

1.3

0.6

0.2

0.3 1.4

5.1

1.2

26.3

28.6

23.6 3.6

1.7

2.1

58.9

58.8

9.3

4.3

5.3

7.04 6.23 5.51 1.26 0.5

0.6

25.2

20.5 4.8

2.1

2.11

4.5

4.03 3.44 1.5

0.48 0.58

0.93 1.15 0.92 0.32 0.06 0.1

2.68 3.05 2.77 1.27 0.4

0.63

0.43 0.38 0.33 0.24 0.12 0.13

1.91 1.67 1.65 1.18 0.65 0.63

0.28 0.29 0.28 0.19 0.12 0.14

0.85 0.71 0.71 0.46 0.46 0.42

0.13 0.11 0.11 0.07 0.09 0.1

0.78 0.67 0.73 0.45 0.61 0.65

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

O/K

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

/Yb

20.806 24.181 18.117 5.694 1.942 2.247

[°C]

793

768

780

682

663

643

429

GEOCHRONOLOGY AND PETROGENESIS OF GRANITOID ROCKS (GORYCZKOWA UNIT, W CARPATHIANS)

GEOLOGICA CARPATHICA

GEOLOGICA CARPATHICA, 2013, 64, 6, 419—435

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

206

207

238

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

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

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

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

431

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GEOLOGICA CARPATHICA

GEOLOGICA CARPATHICA, 2013, 64, 6, 419—435

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

206

207

238

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

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

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

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

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.

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

432

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GEOLOGICA CARPATHICA, 2013, 64, 6, 419—435

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

, 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

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]

ratios in suite 1 grani-

toids are relatively high (1.3—2.13), while positive U anomaly
[Th/U]

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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GEOLOGICA CARPATHICA, 2013, 64, 6, 419—435

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.

References

Bac-Moszaszwili M. 1996: The uplift of the Tatra massif in Tertiary

and Quaternary. In: The Tatra National Park — Nature and man.
Zakopane, Oct. 6

—9

1995, Conference proceedings, 68—71.

Balintoni I., Balica C., Ducea M.N., Chen F., Hann H.P. & Sab-

liovschi V. 2009: Late Cambrian-Early Ordovician Gondwanan
terranes in the Romanian Carpathians: a zircon U-Pb prove-
nance study. Gondwana Res. 16, 119—133.

Balintoni I., Balica C., Ducea M.N., Zaharia L., Chen F., Cliveti

M., Hann H.P., Li L-Q. & Ghergari L. 2010: Late Cambrian-
Ordovician northeastern Gondwana terranes in the basement of
the Apuseni Mountains, Romania. J. Geol. Soc. London 167,
1131—1145.

Batchelor R.A. & Bowden P. 1985: Petrogenetic interpretation of

granitoid rock series using multicationic parameters. Chem.
Geol. 48, 43—55.

Blundy J.D. & Holland T.J.B. 1990: Calcic amphibole equlibria and

a new amphibole-plagioclase geothermometer. Contr. Mineral.
Petrology 104, 208—244.

Broska I. & Petrík I. 2011: Accessory Fe-Ti oxides in the West-

Carpathian I-type granitoids: witnesses of the granite mixing
and late oxidation processes. Miner. Petrology 102, 87—97.

Broska I., Petrík I., Be’eri-Shlevin Y., Majka J. & Bezák V. 2013:

Devonian/Mississippian I-type granitoids in the Western
Carpathians: A subduction-related hybrid magmatism. Lithos
162—163, 27—36.

Burchart J. 1968: Rubidium-strontium isochron ages of the crystal-

line core of the Tatra Mountains, Poland. Amer. J. Sci. 266, 10,
895—907.

434

BURDA, GAWĘDA and KLÖTZLI

GEOLOGICA CARPATHICA

GEOLOGICA CARPATHICA, 2013, 64, 6, 419—435

Burchart J. 1970: Rocks of the Goryczkowa “crystalline island” in

the Tatra Mountains. [Skały krystaliczne wyspy Goryczkowej
w Tatrach.] Stud. Geol. Pol. 32, 7—183 (in Polish).

Burda J. 2010: Internal structures and dating of complex zircons

from High Tatra massif granodiorites, Poland. 10

Interna-

tional conference – Methods of absolute chronology, 22—25
April Gliwice, Poland, Abstracts & Programme, 79.

Burda J. & Gawęda A. 2009: Shear-influenced partial melting in the

Western Tatra metamorphic complex: geochemistry and geo-
chronology. Lithos 110, 373—385.

Burda J. & Klötzli U. 2007: LA-MC-ICP-MS U-Pb zircon geochro-

nology of the Goryczkowa type granite – Tatra Mts., Poland.
Pol. Tow. Mineral. Prace Spec. 31, 89—92.

Burda J. & Klötzli U. 2011: Pre-Variscan evolution of the Western

Tatra Mountains: new insights from U-Pb zircon dating. Miner.
Petrology 102, 99—115.

Burda J., Gawęda A. & Klötzli U. 2011: Magma hybridization in

the Western Tatra Mountains granitoid intrusion (S-Poland,
Western Carpathians). Miner. Petrology 103, 19—36.

Burda J., Gawęda A. & Klötzli U. 2013: U-Pb zircon age of the

youngest magmatic activity in the High Tatra granites (Central
Western Carpathians). Geochronometria 40, 2, 134—144.

Chappell B.W., White A.J.R. & Wyborn D. 1987: The importance

of residual source material (restite) in granite petrogenesis. J.
Petrology 28, 6, 1111—1138.

Clemens J.D. & Stevens G. 2012: What controls chemical variation

in granitic magmas? Lithos 134—135, 317—329.

De la Roche H., Leterrier J., Grandclaude P. & Marchal M. 1980:

A classification of volcanic and plutonic rocks using R

-dia-

grams and major element analysis – its relationships with cur-
rent nomenclature. Chem. Geol. 29, 183—210.

Finger F., Roberts M.P., Haunschmid B., Schermaier A. & Steyrer

H.P. 1997: Variscan granitoids of Central Europe: their typology,
potential sources and tectonothermal relations. Miner. Petrology
61, 67—96.

Frost B.R. & Frost C.D. 2008: A geochemical classification for

feldspathic igneous rocks. J. Petrology 49, 1955—1969.

Gaab A.S., Poller U., Todt W. & Janák M. 2003: Geochemical and

isotopic characteristics of the Muráň gneiss complex, Veporic
unit (Slovakia). J. Czech Geol. Soc. 48, 52.

Gawęda A. 2001: Alaskites of the Western Tatra Mountains: A

record of Early-Variscan collisional stage in the Carpathians
pre-continent. Univ. Silesia Publ. House, Monograph. Ser.,
1997, Katowice, 1—142 (in Polish, English abstract).

Gawęda A. 2007: Mega-xenolith from Velicka Valley (High Tatra

Mountains, Western Carpathians): an example of exploding ele-
phant. Pol. Tow. Mineral. Prace Spec. 31, 115—118.

Gawęda A. 2008: Apatite-rich enclave in the High Tatra granite,

Western Carpathians: petrological and geochronological study.
Geol. Carpathica 59, 4, 295—306.

Gawęda A. 2009: Enclaves in the High Tatra Granite. Univ. Silesia

Publ. House, Monograph. Ser., 2637, Katowice, 1—180 (in Polish,
English abstract).

Gawęda A. & Golonka J. 2011: Variscan plate dynamics in the Cir-

cum-Carpathian area. Geodin. Acta 24, 3—4, 141—155.

Gawęda A. & Szopa K. 2011: The origin of magmatic layering in

the High Tatra granite, Central Western Carpathians – impli-
cations for the formation of granitoid plutons. Earth Env. Sci.
T. R. So. 102, 129—144.

Gawęda A., Doniecki T., Burda J. & Kohút M. 2005: The petrogene-

sis of quartz-diorites from the Tatra Mountains (Central Western
Carpathians): an example of magma hybridisation. Neu. Jb.
Miner. Abh. 181, 1, 95—109.

Gawęda A., Winchester J.A., Kozłowski K., Narębski W. & Holland

G. 2000: Geochemistry and paleotectonic setting of the amphi-
bolites from the Western Tatra Mountains. Geol. J. 35, 69—85.

Janák M., Finger F., Plašienka D., Petrík I., Humer B., Méres Š. &

Lupták B. 2002: Variscan high P-T recrystallization of Ordovi-
cian granitoids in the Veporic unit (Nízke Tatry Mountains,
Western Carpathians): new petrological and geochronological
data. Geolines 14, 38—39.

Jaroszewski W. 1965: Geological structure of the upper part of

Kościeliska Valley in the Tatra Mts. Acta Geol. Pol. 15, 4 (in
Polish, English abstract).

Jurewicz E. 2006: Petrophysical control on the mode of shearing in

the sedimentary rocks and granitoid core of the Tatra Moun-
tains during Late Cretaceous nappe-thrusting and folding, Car-
pathians, Poland. Acta Geol. Pol. 56, 2, 159—170.

Kemp A.I.S. & Hawkesworth J. 2005: Granitic perspectives on the

generation and secular evolution of the continental crust. In:
Rudnick R. (Ed.): The crust – Treatise on geochemistry 3.
Elsevier, Amsterdam, 349—410.

Klötzli U., Klötzli E., Günes Z. & Košler J. 2009: External accuracy

of laser ablation U-Pb zircon dating: results from a test using
five different reference zircons. Geostand. Geoanal. Res. 33, 1,
5—15.

Kohút M. & Janák M. 1994: Granitoids of the Tatra Mts, Western

Carpathians: Field relations and petrogenetic implications.
Geol. Carpathica 45, 5, 301—311.

Kohút M. & Siman P. 2011: The Goryczkowa granitic type –

SHRIMP dating of an original granodiorite-tonalite variety.
Mineralogia, Spec. Pap. 38, 113—114.

Kohút M., Poller U., Gurk C. & Todt W. 2008: Geochemistry and

U-Pb detrital zircon ages of metasedimentary rocks of the
Lower Unit, Western Tatra Mountains (Slovakia). Acta Geol.
Pol. 58, 371—384.

Kohút M., Madarás J. & Siman P. 2009: Centenary of the Gorycz-

kowa granite type (Tatra Mts.): The myth and reality. Geovestník,
8

Ann. Seminary of the Slovak Geol. Soc., 550—551.

Kohút M., Uher P., Putiš M., Broska I., Rodionov N. & Sergeev S.

2010: Are there any differences in age of the two principal
Variscan (I- & S-) granite types from the Western Carpathians?
– a SHRIMP approach. In: Kohút M. (Ed.): Dating of minerals
and rocks, metamorphic, magmatic and metallogenetic pro-
cesses, as well as tectonic events. State Geol. Inst. Dionýz Štúr,
Bratislava, 17—18.

Ludwig K.R. 2003: Isoplot/Ex version 3.00. A geochronological

toolkit for Microsoft Excel. Berkeley Geochronology Center,
Spec. Publ., No. 4.

Morozewicz K. 1914: Über die Tatragranite. Neu. Jb. Miner. Geol.

Paläont. 39, 289—345.

Patiño Douce A. E. 1999: What do experiments tell us about the rela-

tive contributions of crust and mantle to the origin of granitic
magmas? In: Castro A., Fernandez C. & Vigneresse J.L. (Eds.):
Understanding granites: Integrating new and classical tech-
niques. Geol. Soc. London, Spec. Publ. 168, 55—75.

Pearce J.A., Harris N.B.W. & Tindle A.G. 1984: Trace elements

discrimination diagram for the tectonic interpretation of granitic
rocks. J. Petrology 25, 4, 956—983.

Pecerillo A. & Taylor S.R. 1976: Geochemistry of Eocene calc-alka-

line volcanic rocks from the Kastamonu area, northern Turkey.
Contr. Mineral. Petrology 58, 63—81.

Poller U. & Todt W. 2000: U-Pb single zircon data of granitoids from

the High Tatra Mountains (Slovakia): implications for the geo-
dynamic evolution. Trans. Roy. Soc. Edin-Earth 91, 235—243.

Poller U., Janák M., Kohút M. & Todt W. 2000: Early Variscan

magmatism in the Western Carpathians: U-Pb zircon data from
granitoids and orthogneisses of the Tatra Mountains, Slovakia.
Int. J. Earth Sci. 89, 336—349.

Poller U., Todt W., Kohút M. & Janák M. 2001: Nd, Sr, Pb isotope

study of the Western Carpathians: implications for the Paleo-
zoic evolution. Schweiz. Mineral. Petrogr. 81, 159—174.