GeolCarp_Vol59_No4_295

GEOLOGICA CARPATHICA, AUGUST 2008, 59, 4, 295—306

www.geologicacarpathica.sk

An apatite-rich enclave in the High Tatra granite (Western

Carpathians): petrological and geochronological study

ALEKSANDRA GAWĘDA

University of Silesia, Faculty of Earth Sciences, Będzińska st. 60, 41-200 Sosnowiec, Poland; gaweda@us.edu.pl

(Manuscript received June 25, 2007; accepted in revised form March 14, 2008)

Abstract: A mafic, coarse-grained apatite-rich enclave found in the High Tatra granite, Western Carpathians, is an
ultrapotassic rock with mixed (mantle-crustal) geochemical and mineralogical signatures. A U-Pb zircon age dates the
intrusion at 345 ± 5.1 Ma. Zircon cores preserve ages of 361 ± 7.6 Ma and 391 ± 4.6 Ma. The apatite-rich rock could be
interpreted as a cumulate material related to common Tatra granite of comparable age (360—340 Ma). This rock, of very
unusual mineralogy, is an atypical cumulate formed in rocks of granitoid composition.

Key words: Variscan, High Tatra Mts, petrology, apatite-rich cumulate, U-Pb zircon dating.

Introduction

Granites usually contain enclaves of various origins. Some are
co-genetic with the host granite magma (autoliths), some are
mingled magmas of more basic types, others are restite and
many show no genetic links (xenoliths). All enclaves are a
record of the hidden history of the granite they are enclosed in.
The role of mafic magma in granite plutonism was underlined
in the first half of the XX

century and is still under active in-

vestigation (Pitcher 1997; Vincenzo & Rocchi 1999; Barbarin
2005). The rock- and mineral chemistry of mafic enclaves car-
ries information about the source, origin and evolution of the
mantle contribution to the processes involved in granitoid
magmatism and also about the source mantle, existing beneath
the crust at the time of magma generation.

Phosphorus-rich magmatic rocks are not a common lithology

in the Earth’s crust. Apatite-rich lamprophyres related to peralu-
minous,  post-collisional,  1.8 Ga  granitoid  intrusions  occur  in
the Fennoscandian Shield (Konopelko et al. 1998; Eklund et al.
1998).  Enclaves  of  biotite-apatite  rocks  in  early  Variscan
(368 Ma)  granites  have  been  described  from  the  Achala
Batholith, Argentina; these are interpreted as cumulates (Dorais
et  al.  1997).  Internal  structures  of  granitoid  rocks  (sensu  lato)
resembling  depositional  features  and  interpreted  as  a  result  of
accumulation of early-formed crystals (cumulates) are relatively
scarce and restricted to magmas rich in water and flourine, low-
ering the melt viscosity (Collins et al. 2006).

In this paper, new data from an apatite-rich mafic enclave

from the High Tatra granite are presented. They help to define
and constrain a poorly known magmatic episode in the
Variscan history of the Tatra Mountains, a part of the Central
Western Carpathians.

Geological setting and sampling

The Tatra Mountains crystalline core is composed of four

petrographic types of granitoids: common Tatra granodiorite-
tonalite (360—340 Ma), Goryczkowa Granite (356 Ma),

quartz-diorite (341 Ma) and the youngest High Tatra granite
(314 Ma) (Kohút & Janák 1994; Poller et al. 2001; Gawęda et
al. 2005; Burda & Klötzli 2007). All intrude a metamorphic
envelope outcropping mainly in the western part of the Tatra
massif (Fig. 1).

The eastern part of the Tatra Mts (High Tatra Mts) is com-

posed of two main types of granite – a meso-Variscan S-type
(340—360 Ma)  and  a  late-Variscan  hybrid  I/S-type  (ca.
314 Ma). The latter is rich in various types of enclaves includ-
ing  metasedimentary  xenoliths,  diorites  (mafic  precursors),
mafic  magmatic  enclaves  (MME),  schlieren  and  felsic  blobs
(Pawlica  1918;  Janák  1993;  Gawęda  2005;  Gawęda  et  al.
2005; Gawęda 2007a,b). Two basic petrographic types, biotite
monzogranite  and  porphyritic  granite,  were  distinguished
among the High Tatra type (Gawęda 2007b). All of the granite
pulses,  differing  in  age  and  chemistry,  form  one  composite,
polygenetic  pluton.  The  granite  components  of  the  pluton
show VAG (Volcanic Arc Granites) geochemical characteris-
tics and isotopic signatures that suggest continuous melting of
heterogeneous  metasediments  during  subduction  of  oceanic
crust  under  the  continental  wedge  and  during  which  interac-
tion  with  mantle  melts  was  significant  (Poller  et  al.  2001;
Gawęda 2007b).

In the upper part of the Batyżowiecka (Batizovská) Valley,

at  about  1950 m  on  the  western  slopes  of  Gerlach  Mt,  a  ca.
0.9 m enclave of mela-syenite with numerous K-feldspar phe-
nocrysts was discovered in the porphyritic variety of the High
Tatra granite (Figs. 1, 2a). The contact between the mafic en-
clave and the leucocratic porphyritic granite is sharp. The maf-
ic  enclave,  the  host  granite,  their  contact  zone  and  different
petrographical  types  of  granites  (including  quartz  diorites)
were sampled over the distance of ca. 100 m.

Analytical methods

Microscopic observations were made using a BX-60 Olym-

pus microscope at the Faculty of Earth Sciences, University of
Silesia, Sosnowiec, Poland. Microprobe analyses of minerals

296

GAW

and  BSE  photographs  were  carried  out  on  a  CAMECA  SX-
100 electron microprobe in the Inter-Institution Laboratory of
Microanalysis of Minerals and Synthetic Substances, Warsaw,
using sets of natural and synthetic standards. Major and trace
elements  were  analysed  by  XRF  and  ICP-MS  at  the  ACME
Analytical  Laboratories,  Vancouver,  Canada.

Sr/

Sr and

143

Nd/

144

Nd isotopic ratios were measured using a VG sector

54 mass spectrometer at the Department of Geochronology,
Institute of Geological Sciences, Polish Academy of Sciences,
Warsaw. Values of

Sr/

Sr were normalized to SRM 987

(

Sr/

Sr = 0.710266 ± 17, n = 5). Values of

143

Nd/

144

Nd were

normalized to JNd-1 (

143

Nd/

144

Nd = 0.512107 ± 15, n = 10).

Zircons crystals were separated using standard techniques in-
volving crushing, hydrofracturing, washing, Wilfley table,
magnetic separator and handpicking at the Institute of Geolog-
ical Sciences, Polish Academy of Sciences, Kraków. 75 zircon
grains were selected for morphological studies by (SEM). Zir-
con and apatite morphology (SEM), their internal structures
(CL) as well as 7 zircons selected for dating were imaged by
SEM and CL using a FET Philips XL 30 electron microscope
(15kV and 1nA) at the University of Silesia, Sosnowiec.

Zircons were dated by LA-ICP-MS at the Geochronology

Laboratory, Institute of Geology, University of Vienna. Zir-
con

206

Pb/

238

U and

207

Pb/

206

Pb ages were determined using a

193 nm solid state Nd-YAG laser (NewWave UP193-SS) cou-
pled to a multi-collector ICP-MS (Nu Instruments HR). Spot
analyses were 15—25 µm in diameter. Line widths for rastering
were 10—15 µm with a rastering speed of 5 µm/sec. The calcu-
lated

206

Pb/

238

U and

207

Pb/

206

Pb intercept values were correct-

ed for mass discrimination from analyses of standards 91500
(Wiedenbeck  et  al.  1995)  and  Plešovice  (Slama  et  al.  2006)
measured  during  the  analyses  using  a  standard  bracketing
method. The correction involves regression of standard mea-
surements  by  a  quadratic  function.  A  common  Pb  correction
was  applied  to  the  final  data  using  the  apparent

207

Pb/

206

age and the Stacey-Kramers (1975) Pb evolution model. The

Fig. 1. Simplified geological map of the Tatra Mts massif with the location of the apatite-rich enclave sampling point (compilation after Kohút
& Janák 1994; Gawęda et al. 2005). 1 – metamorphic cover, 2 – anatectic leucogranites, 3 – common Tatra granite, 4 – High Tatra granite,
5 – Goryczkowa granite, 6 – sedimentary cover, 7 – main faults: a – identified, b – assumpted, 8 – sampling point.

Fig. 2. Photos of apatite-rich enclave: a – Field photograph of the
apatite-rich enclave. Geological hammer as a scale. b – Micropho-
tograph of the apatite-rich enclave. Note the quartz grains, mantled
by mica and titanite. Abbreviations: Kfs – K-feldspar, Pl – pla-
gioclase, Qtz – quartz, Bt – biotite, Ap – apatite, Tnt – titan-
ite, Ms – muscovite.

297

PETROLOGICAL AND GEOCHRONOLOGICAL STUDY OF THE HIGH TATRA GRANITE (WESTERN CARPATHIANS)

Sample No. G2-05 G1g-05 Mkn-05 G12g-05 G9d-05 CTG

1 2 3 4 5 6

6.13

51.35

38.68

37.25

46.18 60.30

Kfs

39.77 13.37 33.14 29.10 – 20.90

Qtz

4.37

18.56

16.42

19.65

6.73 16.60

Bt/Chl

30.77

9.63

6.05

7.00

41.99 1.40

4.49

2.91

4.05

4.60

0.70 0.40

0.10

–

0.96

1.00

0.65 0.25

Np+tnt

0.57

1.84

0.35

0.43

1.35 0.02

13.74

1.77

0.25

0.70

1.90 0.10

Zrn/Mnz

0.04

0.60

0.10

0.27

0.50 0.03

Table 1: Modal analyses of the apatite-rich enclave and the surround-
ing granitoid rocks. 1 – apatite-rich enclave, 2, 3, 4 – porphyritic
varieties of High Tatra type granites, 5 – quartz diorite, 6 – an ex-
ample of common Tatra type granite.

Component

Bt1c Bt1m Bt4c Bt4m Bt4r Ms1c Ms2c Ms2m

Ms2r

SiO

35.01 34.86 34.83 34.97 35.66 44.94 44.97 45.06 44.96

TiO

3.26 2.48 3.33 3.12 3.08 1.63 1.70 1.31 1.62

16.84 15.72 16.84 16.93 17.02 31.51 31.48 31.80 31.37

0.05 0.01 0.02 0.02 0.03 0.04 0.00 0.00 0.00

FeO

21.54 23.53

22.04 22.78 22.57 4.36 4.18 4.25 4.36

MgO

8.74 8.43 7.79 8.07

7.9

0.85 0.81 0.78 0.88

MnO

0.39 0.22 0.36 0.34 0.29 0.03 0.00 0.00 0.04

0.14 0.04 0.07 0.09 0.09 0.48 0.45 0.46 0.42

9.4

8.88

9.17 9.22 9.28 10.37 10.42 10.30 10.37

BaO

0.00 0.04 0.06 0.02 0.19 0.12 0.04 0.14 0.06

Total

95.37 94.21 94.51 95.56 96.11 94.33 94.06 94.09 94.08

5.414 5.497 5.44 5.421 5.484 6.174 6.184 6.192 6.187

2.586 2.503 2.56 2.579 2.516 1.826 1.816 1.808 1.813

0.483 0.419 0.539 0.514 0.569 3.275 3.286 3.342 3.275

0.380 0.294 0.391 0.364 0.356 0.168 0.176 0.135 0.168

0.006 0.001 0.003 0.002 0.004 0.004 0.000 0.000 0.000

2.785 3.103 2.878 2.952 2.903 0.501 0.481 0.488 0.502

2.016 1.981 1.814 1.864 1.811 0.174 0.167 0.159 0.180

0.051 0.030 0.048 0.044 0.038 0.003 0.000 0.000 0.005

0.041 0.013 0.022 0.026 0.026 0.128 0.120 0.123 0.113

1.854 1.786 1.828 1.823 1.822 1.817 1.829 1.805 1.821

0.000 0.003 0.004 0.001 0.011 0.006 0.002 0.007 0.003

0.574 0.607 0.607 0.608 0.612 0.739 0.742 0.754 0.731

Table 2: Microanalyses of biotite (Bt) and muscovite (Ms) with their crystal-chemical formu-
las (22 O

2—

) from the mela-syenite enclave. fm = Fe/(Fe + Mg + Mn); c – core, m – margin.

final U/Pb ages were calculated at 1

σ standard deviation us-

ing the Isoplot/Ex program – version 3.00 (Ludwig 2003).

Petrography and mineral characteristics

The porphyritic mafic enclave shows minor secondary alter-

ation (insignificant biotite chloritization) only in the 5 mm
thick contact zone. The enclosing porphyritic K-feldspar gran-
itoid is also slightly altered near the contact. The composition
of the host granitoid changes from K-feldspar syenogranite in
the 1 m contact zone to the porphyritic, K-feldspar-rich
monzogranite with quartz diorite enclave at about 50 m from
the contact and to biotite monzogranite further out. There is no
indication of cooling against the granite in the enclave and no

mineralogical zoning, but the narrow (about 1 cm) fine-
grained margin is noticeable inside the granite.

The medium-grained enclave (size of rock-forming miner-

als  fall  in  the  range  of  2—8 mm)  is  composed  of  K-feldspar
porphyrocrysts  ( ~ 30 mm),  biotite,  apatite,  albite,  quartz  and
muscovite (Table 1). The accessories ( < 1%) are monazite, xe-
notime,  epidote-allanite,  zircon,  magnetite-ilmenite-rutile  in-
tergrowths, titanite, chlorite and calcite. The Mafic Index (MI
=  biotite  +  apatite  +  opaque  minerals  +  titanite  +  epidote)  is
ca.  45 %  (Gawęda  2006).  A  weak  fabric  is  defined  by  Kfs
megacrysts and biotite-apatite alignment (Fig. 2b).

The Kfs euhedral porphyrocrysts show normal zoning in

BaO  content  from  1.86—0.91 wt. %  (0.035—0.024 Ba  a.p.f.u.)
in cores to 0.75—0.43 wt. % (0.014—0.008 Ba a.p.f.u.) at rims
(Fig. 3). Inclusions of albitic plagioclase, and falls in Ba con-
tent,  emphasise  the  zoning  of  the  host-feldspar  (Fig. 3).  The
matrix  plagioclase  is  also  albite  (Ab

—Ab

). Bi-

otite (fm = 0.644—0.598, Ti = 0.39—0.36 a.p.f.u.) is weakly
zoned with a slight drop in Ti content from core to rim (Ta-
ble 2). In general, the biotite chemistry compares with that of
the enclosing granite (Fig. 4). The TiO

content of the dis-

persed muscovite flakes in the range 1.3—1.7 wt. %, and fm in
the range 0.731—0.754 (Table 2) both reflect the magmatic
character of the white mica (Monier & Robert 1986). They are
chemically and optically homogeneous.

Two types of apatite (0.2—2 mm ) were identified: Ap

–

unzoned isometric clear apatite crystals (Figs. 2b, 5a,c;
Table 3a) and prevailing Ap

– xenomorphic crystals with a

patchy internal structure marked by differences in Fe, Y, Na
and Mg contents and with inclusions of HREE-rich xenotime

and zircon (Fig. 5a,b,d; Table 3b), poiki-
loblastically intergrown with biotite
flakes.

Zircons, from 15—100

µm in size, oc-

cur as inclusions in Ap

, in biotite and in

opaque  minerals.  In  the  classification  of
Pupin  (1980),  the  zircon  morphologies
are  widely  distributed  with  populations
typical  of  high-temperature  mantle-de-
rived  magmas  (J

1—2

), lower-temperature

crustal-derived magmas (S

6—7

—S

16—17

) and

mixtures of both (S

21—24

, Figs. 6, 7). Zir-

con inclusions in apatite are of J

type

only (Fig. 5d,e). All of the zircon crystals
have cores with Zr/Hf ~ 43—55 and rims
with Zr/Hf ~ 19.5—42 (Fig. 7; Table 4).

Zoned euhedral epidotes show transi-

tions  from  allanite  cores  to  REE-bearing
epidote at the rims (Table 5), as is typical
of  magmatic  epidote  crystals.  Secondary
zoizite + titanite  fringes  the  overgrow  the
REE-epidote  (Table 5).  Unzoned  Ce-
monazite crystals (Table 3b) occur as in-
clusions  in  biotite,  apatite  and  opaque
minerals,  locally  the  decomposition  of
monazite  and  formation  of  REE-epidote
is  observed.  Opaque  minerals  occur  as
aggregates  of  intergrown  ilmenite,  mag-
netite  and  rutile  in  varying  proportions

298

GAW

(Table 6) and suggest the decomposition of an original ul-
vöspinel under oxidizing conditions. The opaque crystals host
tiny inclusions of calcite and are overgrown by titanite coro-
nas. The titanite may be a product of secondary reaction be-
tween Ti-rich opaque minerals and calcite.

Whole-rock geochemistry

The rock is characterized by low SiO

and a very high P

reflecting the high apatite content (Table 7). However, it is
quartz (3.60) and corundum (4.34) normative (Gawęda 2006)
as biotite is the main rock-forming aluminosilicate and prima-
ry muscovite is present. Petrographical observations (i.e. man-
tling of the quartz by micas and titanite, Fig. 2b) suggest that the
quartz could have been physically wedged into the enclave.

The Fe

, TiO

, Ba, Rb, total REE, Zr, Hf, Y contents are

high and that of Sr moderate (Table 6; Fig. 8a,b,c,d). REE
fractionation, dominated by HREE fractionation, is weak
(Ce

/Yb

= 3.16; Table 7). The rock is characterized by a pro-

nounced negative Eu anomaly (Eu/Eu* = 0.354; Table 7; Fig. 9)
and a low Sr/Sr* value (Sr/Sr* = Sr

√[Ce

×Nd

] = 0.135), es-

pecially when compared to the other Tatra granitoids (com-
pare Table 7 and Gawęda 2007b). The ASI index (ASI = Al/
[Ca + K + Na—3.33P]) recalculated against the molecular P

content equals 1.499 and the sample plots in the peraluminous
field of Maniar & Piccoli (1989), while without correction to
phosphorus the sample is metaluminous (ASI = 0.837). As the
rock is corundum normative and magmatic micas are volu-
metrically important components the first value is considered
here. The K

O/Na

O ratio is equal to 3.93, so the rock can be

classified as ultrapotassic (Fig. 8e). The agpaitic index
([K

O + Na

O]/Al

[molar]) is 0.61. Sr prevails over Rb (Rb/

Sr = 0.467) and Nd over Th (Nd/Th = 6.526; Fig. 8d). Zr/Hf at
32.41 is typical of most crustal rocks.

Fig. 3. Cs and Ab distribution profiles in alkali feldspar phenocryst.
Scale in micrometers.

Fig. 4. Plot of biotite composition in the Ti [a.p.f.u.]/fm space. For
comparison biotites from porphyritic granites, monzogranites and
diorites were used.

Fig. 5.  Examples  of
SEM and BSE images
of  apatite  and  zircon.
a  –  BSE  image  of
isometric Ap

(analyt-

ical points of apatite 1
& 2) and xenomorphic
Ap

(point 3), inter-

grown  with  biotite
(grey).  b  –  BSE  im-
age  of  xenomorphic
Ap

with patchy inter-

nal  structure  (analyti-
cal  points  4—7  ade-
quate  to  analyses  in
Table 3a) and dissolu-
tion embayments. c –
SEM  image  of  Ap

d  –  SEM  image  of
hipidiomorphic  Ap2
with  zircon  inclusion
(pointed  by  arrow).
e – SEM image of J2
zircon crystal.

299

PETROLOGICAL AND GEOCHRONOLOGICAL STUDY OF THE HIGH TATRA GRANITE (WESTERN CARPATHIANS)

Sample

Xen 1

Xen 2

Mon 1

35.13 35.01 29.60

44.19

43.12

0.00

0.03

0.06

13.71

0.03

0.15

29.09

0.07

0.04

3.25

0.43

0.70

12.67

0.57

0.72

2.31

2.66

2.85

1.51

4.09

3.73

0.12

4.89

0.32

1.20

0.84

0.09

2.97

0.00

0.71

0.73

0.00

0.24

0.00

0.52

0.50

0.10

SiO

0.15

0.16

0.20

0.67

0.69

0.18

ThO

0.00

0.10

4.33

PbO

0.00

0.03

Total 98.552 97.238 97.51

Apatite

Ap 1

Ap 2

Analysis

No.

1 2 3 4 5 6 7

42.54 40.69 42.03 42.48 40.14 42.91 41.91

SiO

0.02 0.03 0.00 0.03 0.01 0.02 0.00

0.00 0.04 0.02 0.01 0.05 0.03 0.05

ThO

0.00 0.00 0.06 0.09 0.00 0.03 0.08

0.09 0.21 0.24 0.01 0.12 0.06 0.14

0.15 0.11 0.23 0.24 0.34 0.17 0.19

0.02 0.01 0.18 0.24 0.03 0.01 0.01

0.03 0.05 0.04 0.11 0.17 0.00 0.16

0.13 0.10 0.00 0.01 0.15 0.00 0.16

0.02 0.03 0.05 0.10 0.07 0.00 0.01

CaO

54.52 55.17 54.43 54.76 55.23 55.52 55.20

MnO

0.14 0.19 0.22 0.14 0.31 0.00 0.14

SrO

0.03 0.04 0.02 0.01 0.04 0.02 0.08

0.06 0.06 0.15 0.11 0.18 0.07 0.10

0.00 0.00 0.00 0.05 0.00 0.00 0.06

2.71 3.63 3.25 2.12 3.90 2.43 2.12

0.03 0.04 0.04 0.02 0.04 0.01 0.02

Total 100.41

100.40

100.73

100.26

100.78 101.26

100.43

Table 3: a – Selected microanalyses of apatite. b – Selected xe-
notime and monazite microanalyses.

Sample

Zr1(c1) Zr1(c2) Zr1(m) Zr1(r) Zr2(c) Zr2(m) Zr3(c1) Zr3(c2) Zr3(m)

SiO

31.98 31.91 31.13 32.15 31.92 31.98 32.15 31.27

32.18

ZrO

65.65 65.75 65.00 64.08 65.28 65.04 66.08 65.49

65.71

HfO

1.04

1.08

1.35

2.87

1.18

2.17

1.08

1.32

1.92

0.09

0.05

0.22

0.10

0.05

0.06

0.08

0.54

0.47

0.32

0.12

0.43

0.16

0.46

0.22

0.11

0.14

0.11

0.05

0.08

0.11

0.05

0.11

0.03

0.08

CaO

0.26

0.00

0.14

0.37

0.18

0.00

0.17

0.00

Total

99.69 99.37 98.04 99.89 99.21 99.68 99.92 98.55 100.09

0.989

0.981

0.996

0.991

0.981

0.992

0.990

0.994

0.999

0.969

0.989

0.983

0.993

1.002

0.988

0.009

0.010

0.012

0.025

0.011

0.019

0.010

0.012

0.017

0.001

0.000

0.002

0.001

0.000

0.001

0.009

0.008

0.005

0.002

0.007

0.003

0.008

0.004

0.002

0.001

0.000

0.001

0.009

0.000

0.005

0.012

0.006

0.000

0.006

0.000

Zr/Hf

55.108 53.151 42.034 19.493 48.299 26.167 53.418 43.316

29.879

Table 4: Microanalyses of zircon crystals and their crystal-chemical formulae.

U-Pb zircon dating and isotope geochemistry

U-Pb dating of 7 zircon crystals representing both J and S

morphological types (Fig. 7) reveal three generations of ages.
The oldest age of 391 ± 4.6 Ma (Fig. 10a; Table 8a) was found
in zircon cores and one mantle. Two zircon mantles and one
core provide an age of 361 ± 7.6 Ma (Fig. 10b; Table 8b). Zir-
con rims, and one core with magmatic zoning, yielded the
youngest age of 345 ± 5.1 Ma (Fig. 10c; Table 8c). One homo-
geneous inner core was dated to ca. 700 Ma and one core with
oscillatory zonation to ca. 430 Ma (Table 8d).

The apatite

Sr/

Sr can be considered to be the rock initial

ratio as apatite contains little or no Rb, assuming no isotopic
disturbances occurred (Tsuboi & Suzuki 2003). The apatite

Sr/

Sr value of 0.707620, lower than whole-rock IR

345

Sr/

Sr ratio (Table 9) suggests either a mixed mantle/crust-

Fig. 6. The position of zircon crystals morphology on Pupin’s
(1980) typological diagram.

300

GAW

al origin for the rock or, perhaps, some disturbance of a prima-
ry value. A three point errorchron based on apatite, Kfs and
the host whole rock suggests an age of 312 ± 530 Ma
(IR

312

= 0.70740). The rock is characterized by an IR

345

value of 0.511901,

345

and crustal residence age

= 1.341 (Table 9). It is worth mentioning that both the Sr

and Nd isotopic characteristics of the apatite rock resemble
those found in most Variscan granitoid rocks (Kohút et al.
1999).

Discussion

The origin of the apatite-rich rock and its systematic position

Low SiO

and high CaO contents reflect the high apatite

content. The high Al

content and peraluminous character

of the rock are due to the high contents of biotite and musco-
vite; both minerals are peraluminous—biotite because of its
significant siderophyllite component. The modal and chemi-

Component Al-ep9 Al-ep10 Al-ep11 Al-ep12 Al-ep16 Al-ep13 Al-ep14 Al-ep15 Ep-r-1 Ep-r-2

rim mantle

core

mantle rim secondary

SiO

33.75

32.63

33.32

32.6

31.98

32.89

33.85

34.89

37.32

37.45

TiO

0.1

0.19

0.12

0.17

0.22

0.13

0.06

0.11

0.01

0.04

19.35 18.06 19.08 18.06 17.65 18.69 19.98 20.36 21.66 22.09

0.63

0.07

0.42

0.19

0.38

0.05

0.19

0.21

0.29

0.56

FeO

12.59 13.65 12.97 13.46 12.82 12.75 12.34 13.03 14.01 13.65

MnO

0.79

1.18

0.7

0.87

0.54

0.79

0.58

0.19

0.11

MgO

0.18

0.22

0.19

0.22

0.26

0.20

0.15

0.14

0.00

CaO

14.91 12.83

14.6

13.2

12.19

14.16

15.61

17.1

22.66

22.59

SrO

0.00

0.18

0.33

2.10

3.21

2.18

3.20

3.77

3.00

1.59

1.67

0.04

0.00

5.08

7.11

5.50

6.90

8.84

7.11

4.32

3.66

0.08

0.00

0.62

0.81

0.61

0.71

0.97

0.75

0.53

0.41

0.03

0.00

2.40

2.74

2.92

3.10

3.70

2.70

2.24

1.72

0.04

0.08

0.65

0.54

0.66

0.59

0.74

0.64

0.61

0.32

0.02

0.04

0.44

0.48

0.50

0.43

0.40

0.72

0.50

0.07

0.14

ThO

0.01

0.19

0.21

0.14

0.10

0.00

0.14

0.08

0.02

0.12

0.00

0.03

0.01

0.00

0.01

0.03

Total

93.60 93.91 93.96 93.94 94.93 94.02 93.12 94.79 96.66 97.22

6.169

6.166

6.144

6.15

6.089

6.151

6.180

6.193

6.219

6.180

0.014

0.027

0.016

0.024

0.032

0.018

0.008

0.015

0.002

0.005

4.168

4.022

4.146

4.016

3.960

4.119

4.300

4.259

4.255

4.296

1.924

2.156

2.000

2.124

2.041

1.995

1.883

1.935

1.952

1.884

0.122

0.190

0.109

0.138

0.140

0.085

0.123

0.087

0.027

0.015

0.050

0.063

0.051

0.061

0.075

0.055

0.041

0.037

0.000

0.001

2.920

2.596

2.884

2.669

2.487

2.836

3.053

3.252

4.046

3.993

0.000

0.018

0.032

0.142

0.223

0.148

0.222

0.264

0.207

0.107

0.109

0.002

0.000

0.340

0.492

0.371

0.476

0.616

0.487

0.289

0.238

0.005

0.000

0.041

0.056

0.041

0.049

0.067

0.051

0.035

0.027

0.002

0.000

0.157

0.185

0.192

0.209

0.252

0.180

0.146

0.109

0.002

0.005

0.041

0.035

0.042

0.038

0.049

0.041

0.038

0.019

0.001

0.002

0.027

0.030

0.029

0.031

0.027

0.025

0.044

0.030

0.004

0.007

0.001

0.008

0.009

0.006

0.004

0.000

0.006

0.003

0.001

0.004

Table 5: Selected microanalyses of epidotes and their crystal-chemical formulae (25 O

2—

Sample sp1 Ilm1 sp2 Ilm2 sp3 Ilm3 sp4

FeO

31.06 41.35 30.71 40.87 31.3 40.85 30.73

66.37 4.04 55.6 3.77 66.52 4.49 67.8

MnO

0.05 3.87 0.64 4.65 0.00 4.18 0.07

MgO

0.00 0.06 0.00 0.06 0.04 0.06 0.00

0.07 0.00 0.05 0.00 0.07 0.00 0.06

0.81 0.00 0.41 0.00 0.47 0.00 0.43

0.24 0.01 0.15 0.00 0.21 0.00 0.06

TiO

1.81 50.46 11.32 50.81 1.38 50.24 1.03

Total

100.41 99.78 98.88 100.16 99.99 99.82 100.18

0.986 0.875 0.975 0.862 0.994 0.865 0.975

1.896 0.077 1.588 0.072 1.900 0.086 1.937

0.002 0.083 0.019 0.100 0.000 0.090 0.002

0.000 0.002 0.000 0.002 0.002 0.002 0.000

0.002 0.000 0.002 0.000 0.002 0.000 0.002

0.020 0.000 0.010 0.000 0.012 0.000 0.011

0.005 0.001 0.003 0.000 0.004 0.000 0.001

0.052 0.960 0.323 0.964 0.039 0.957 0.029

Table 6: Selected microanalyses of magnetite (sp) and ilmenite (Il)
and their crystal-chemical formulae (for 4 O

2—

and 3 O

2—

respectively).

Notice: sp2 and Ilm2 are not in equilibrium

301

PETROLOGICAL AND GEOCHRONOLOGICAL STUDY OF THE HIGH TATRA GRANITE (WESTERN CARPATHIANS)

Table 7: Whole-rock analyses of major and trace elements in the
apatite-rich enclave (G2-05), the selected granitoids (G1g-05, Mkn-
05, G12g-05) and quartz-diorite enclave (G9d-05). T

– tempera-

ture calculated according to Watson & Harrison (1983) procedure.
CTG – an example of common Tatra granite.

Sample
No.

G2-05 G1g-05 Mkn-05

G12g-05

G9d-05 CTG

SiO

48.89 62.9

64.74 66.66 61.07 75.62

TiO

1.23 0.65 0.52 0.58 0.77 0.11

16.21 18.87 17.78 17.04 17.91 13.48

7.98 3.23 3.19 3.61 5.89 0.67

MnO

0.11 0.02 0.04 0.05 0.09 0.01

MgO

2.7

1.92 1.23 1.13 2.73 0.13

CaO

7.21 1.67 1.48 2.41 3.33 0.94

1.67 4.71 3.88 4.49 4.31 3.07

6.57 3.56 5.14 2.39 2.33 5.10

5.08 0.25 0.32 0.28 0.36 0.15

LOI

2.00 2.30 1.60 1.50 1.3 0.90

C(tot)

0.04 0.15 0.02 0.05 0.01 0.03

S(tot)

0.01 0.01 0.01 0.01 0.01 0.01

Total

99.7

100.24 99.95 100.2 100.11 100.18

ASI

1.499 1.301 1.228 1.199 0.821 0.957

384.3

319.5

445.4

499.6 735.2 370.1

2538.5

1093.7

2421.9

705.7 681.9 1477.4

179.6

91.9

110.4

73.2 107.5 131.4

25.1

15.9

9.3

9.9 2

0.4

8.7

1.7

1.8

2.6 19.3 1.0

20.5

20.6

103

47.9 48.0

125

126

115

9.0

440.8

205.8

159.1

143.8 122

41.7

13.6

6.0

4.2

3.9 3.6 1.5

401.1

16.8

26.1 22

5.1

19.7

8.5

8.8

11.3 8.6 2.7

1.0

0.5

0.8 0.6 0.3

105.70 49.70 14.20 39.90 17

4.40

266.60 104.60 29.40 84.90 65.6 9.20

36.90 11.98 3.36 10.37 129.6 1.12

163.80 42.80 12.20 41.00 14.13 4.10

54.10 8.50 3.00 9.40 50.6 1.20

6.78 1.69 0.69 1.56 8.6 0.59

63.48 5.89 2.98 7.78 1.58 0.94

12.23 0.91 0.66 1.35 6.01 0.18

72.06 3.99 4.58 7.65 0.84 0.99

14.07 0.56 0.96 1.49 4.24 0.18

35.49 1.36 3.00 4.29 0.72 0.47

4.64 0.20 0.44 0.64 1.91 0.08

23.27 1.15 2.49 3.70 0.3 0.39

3.00 0.19 0.37 0.57 1.62 0.09

Eu/Eu* 0.354 0.730 0.657 0.600 0.672 1.698
(Ce/Yb)

3.157 25.061 12.950 11.655 22.042 6.500

[ºC] 752 822 797 801 754 695

Fig. 7. CL and SEM images of zircon crystals used for U-Pb dating.
Analytical lines and points marked not to scale.

cal  composition  of  the  apatite-rich  rock  cannot,  in  any  case,
represent liquid, so it cannot be interpreted as a microgranular
enclave.  There  are  a  number  of  ways  in  which  the  enclave
rock may have originated. It may be (a) restite, (b) cumulate,
(c) recrystallized metasediment or (d) magmatic rock unrelat-
ed to the host granite. The lack of a negative Ce-anomaly and
the high REE, Ba, Zr, Y and Hf contents (Table 8) tell against
it being a P-rich metasediment (see Dorais et al. 1997). More-
over, there is no field and mineralogical evidence that the en-
clave  was  a  metasomatized  country  rock.  The  negative  Eu
anomaly and the high LILE content are atypical of restite. On
the other hand, a magmatic origin is supported by the internal
structures of minerals (zonation).

303

PETROLOGICAL AND GEOCHRONOLOGICAL STUDY OF THE HIGH TATRA GRANITE (WESTERN CARPATHIANS)

Table 8: LA ICP-MS isotope data from zircon grains from apatite-rich enclave. For the loca-
tion of the analytical points (sample numbers) see Fig. 7. U and Pb concentrations were not de-
termined because sample weighing was not possible.

Isotope

parameter G2-05 G9d-05 G12g-04 CTG

Rb [ppm]

179.6 107 73.2 111.3

Sr [ppm]

384.3

735.2 499.6 370.1

Sr/

Sr WR

0.713624±11

0.707074±11 0.709021 0.711642

Rb/

Sr WR

1.352949

0.421059 0.423972 0.886077

Sr/

Sr Ap

0.707620±11

– – –

Sr/

Sr Kfs

0.710478±21

– – –

Rb/

Sr Kfs

0.680109

– – –

345

0.706980 0.705006 0.707126 0.707038

Sm [ppm]

54.1

8.6 6.7 1.2

Nd [ppm]

163.8

50.6 32.1 4.1

143

Nd/

144

Nd WR

0.512463±5

0.512472±8 0.512360±13 0.512410±28

147

Sm/

144

0.199678

0.102753 0.126188 0.176948

143

Nd/

144

Nd Ap

0.512618±15

– – –

345

0.511901 0.512103 0.511944 0.511894

345

–3.548 0.902 –2.318 –3.580

[Ga]

1.341 0.989 1.242 1.353

Table 9: Isotopic analyses of apatite-rich rock, its mineral separates and comparable rock-types.
G2-05 – apatite rich enclave, G9d-05 – quartz—diorite enclave, G12g-04 – porphyritic variety
of High Tatra type granite, CTG – an example of common Tatra granite. Errors are given in 2

σ.

Time of the apatite-rich rock for-
mation

U-Pb zircon dating provides dif-

ferent  Variscan  ages.  Zircons  crys-
tallized early enough to be included
in biotite and apatite. In the context
of the geological history of the Tatra
Mts  massif,  cores  yielding  391 Ma
and  some  older  exceptions  possibly
reflect  the  metamorphic  events  and/
or  partial  melting  episodes  in  the
Tatra  Massif  (Fig. 10a,b;  Burda
2006,  2007;  Gawęda  2007b).  The
concordant  age  of  361 Ma  is  in  ac-
cordance  with  both  the  common
Tatra granite age (Poller et al. 2000)
and the age of Western Carpathians
Variscan

granite

magmatism

(365 Ma; Kohút et al. 1999) as well
as with the partial melting processes
in  the  Western  Tatra  Mts  (Burda
2006,  2007).  The  concordant  age
from  the  zircon  rims  (345 Ma;
Fig. 10c) compares closely with a U-
Pb  zircon  age  for  quartz  diorites
(341 Ma;  Poller  et  al.  2001),  a  WR
Rb-Sr  isochron  age  for  Western
Tatra  pegmatites  (ca.  345 Ma;
Gawęda  1995)  and  a  K-Ar  age  for
shear-zone  muscovite  (ca.  343 Ma;
Deditius 2004).

The Rb-Sr three-point errochron

age of ca. 312 Ma, and a zircon low-
er  intercept  U-Pb  age  of  314 ± 4 Ma
for  the  High  Tatra  granite  intrusion
(Poller  et  al.  2001),  are  consistent
with  300—330 Ma  Ar-Ar  age  of
Variscan uplift of the High Tatra Mts
(Janák 1994) and 298—318 K-Ar ages
of  shearing  (Deditius  2004)  and,
presumably,  final  cooling  of  the
Tatra crystalline massif.

Temperature and pressure determi-
nations

The thermometer of Watson &

Harrison  (1983),  based  on  rock  Zr
content,  applied  for  the  apatite-rich
rock,  provided  a  temperature  of
752

°C without correction for Ca in

apatite, while after correction the
calculated temperature increased to
890

°C. For the other Tatra granitoid

rocks the temperature intervals are
as follows: 822—797

°C for the Kfs-

rich pophyritic granites, 806—736

°C

for the biotite monzogranites and

304

GAW

822—753

°C for the quartz diorites (Gawęda 2007b), and the

correction for Ca in apatite is insignificant. As the rock chemi-
cal and mineralogical composition cannot be interpreted in
terms of liquid, both temperatures are of doubtful meaning.

For the apatite-rich rock, calculation of the Mt-Ilm exsolu-

tion (Spencer & Lindsley 1981) gave a temperature of exsolu-
tion in the range 680—668

°C in a growing oxygen fugacity re-

gime (log

= —16). The latter temperature range is similar

to earlier determinations for the High Tatra granitoids
(Grabowski & Gawęda 1999).

The flat REE profile of the enclave constrains the depth of

melt origin. High-pressure (22—32 kbar) melts in equilibrium

Fig. 10.

206

Pb/

238

U versus

207

Pb/

235

U Concordia plots for the analy-

sed zircon grains from apatite-rich enclave. 1 – concordia plot for
391 ± 4.6 Ma zircon cores, 2 – concordia plot for 361 ± 7.6 Ma zircon
core and mantles, 3 – concordia plot for 345 ± 5.1 Ma zircon rims.

with an eclogitic residue show highly fractionated HREE de-
pletion with low Yb contents, whereas low-pressure ( ~ 8 kbar)
melts with no residual garnet show weakly fractionated REE
patterns  (Luais  &  Hawkesworth  1994)  similar  to  that  of  the
enclave (Fig. 9). Magmatic zoned epidote with allanitic cores
(Table 4), that crystallized after biotite but before quartz and K-
feldspar, suggests a pressure  > 6—8 kbar. The temperature of the
crystal  mush  for  the  given  P  did  not  exceed  740—775

°C for

O > 9 wt. % (Schmidt & Poli 2004). Assuming the high con-

centration of volatiles in the magma, suggested by the lack of
“dry”  minerals  and  the  presence  of  biotite  as  the  predominant
mafic  mineral,  the  higher  temperature  limit  can  be  approved
(Schmidt & Poli 2004), covering temperatures revealed by Mt-
Ilm geothermometer, conspicuously consistent with zircon ther-
mometry.  Biotite  chemical  zoning,  although  weak,  means
growing oxygen fugacity as Ti is incorporated into oxides.

The presence of allanite-epidote also suggests the changes

in Ca activity in the melt as monazite crystallization typifies
low-Ca activity conditions, and allanite presence, high Ca ac-
tivity (Broska et al. 2000). Possibly, early apatite (Ap

) crys-

tallization lowered the Ca activity enabling monazite crystalli-
zation, and Ap

maintained it so. Afterwards, the remaining

Ca was used for allanite formation during more oxidizing con-
ditions while plagioclase is almost pure albite (Petrík & Bros-
ka 1994).

The zoned K-feldspars, and changes in barium content, can

be interpreted in terms of magma mixing and/or changing par-
ent-magma temperatures, water contents, crystallization of ad-
ditional minerals, etc. (Long & Luth 1986; Słaby et al. 2002).
As barium diffusivity in alkali feldspars is very low, zoning is
usually a primary feature. No features such as perthite coars-
ening  identify  the  influence  of  post-magmatic  fluids  in  the
subsolidus stage (see Brown & Parsons 1989). The perturba-
tions  observed  in  the  analysed  profile  (Fig. 3)  may  reflect
changes in the crystallization path due, in the main, to falling
water contents – favouring crystallization of the plagioclase
now trapped as inclusions in the Kf megacrysts. Increased Ba
in Kf near each albite inclusion could reflect increasing water
contents in the magma and/or new mantle magma input. After
the Ba decrease to the margin, the Kf megacryst rims show re-
newed  Ba-enrichment  (up  to  0.029  a.p.f.u.,  1.58 wt. %  BaO
– see Fig. 3). This may represent crystallization from a resid-
uum rich in water, and in Ba.

The calculated temperature interval of 700—800

°C is the

crystallization temperature of most of the rock-forming sili-
cates in the apatite-rich enclave as oxygen fugacity increased.
The Mt-Ilm geothermometry (680—668

°C) could reflect cool-

ing on intrusion of the crystal mush and the decomposition of
primary opaque mineral phases. The assumed pressure (6—
8 kbar) is at the higher end for the hybrid quartz diorite mag-
ma range (4—6 kbar; Gawęda et al. 2005). The enclave crystal-
lization and cooling temperatures compare with those of the
surrounding granites (Gawęda 2007b). Thus, the cooling his-
tory of the hosting granite may have been the key influence.

Speculative model of the apatite-rich magma formation

The apatite, which is the rock-forming mineral in the rock in

question, is a carrier of both F and P, elements significantly

305

PETROLOGICAL AND GEOCHRONOLOGICAL STUDY OF THE HIGH TATRA GRANITE (WESTERN CARPATHIANS)

lowering  the  magma  viscosity.  Fluorine  and  phosphorus  en-
richment  could  allow  formation  of  a  cumulate,  typical  rather
of basic and alkaline rocks (Collins et al. 2006). Here the term
cumulate  is  used  without  defining  the  specific  process  of  its
formation. That could be both crystal sorting caused by gravi-
ty or during magma flow in the stress field. The last possibility
is supported by the oriented fabric of the apatite-rich rock and
the presence of tectosilicates (micas).

The hybrid character of the apatite rock suggests some simi-

larities with quartz diorites of roughly the same age (ca.
341 Ma; compare data and discussion in Gawęda et al. 2005).
However, the differences in

345

and in T

values point out

the different source of both rock-types (compare: Table 9 and
Poller et al. 2001). The processes like cumulate formation or
fractional crystallization could not change the isotopic charac-
teristics  of  the  magma.  On  the  selected  Harker  diagrams
(Fig. 8a,b,c) diffuse trends links the apatite-rich enclave rather
to common Tatra granites then to quartz diorites. However, it
must be noted that most of the quartz-diorites occur as xeno-
liths  in  younger  (ca.  314 Ma)  High  Tatra  granites  and  were
subjected  to  secondary  recrystallization  (see  Gawęda  et  al.
2005). Moreover, the linear trends typically produced by mix-
ing/mingling and fractional crystallization processes could be
easily  destroyed  if  cumulates  were  produced  early  and  more
evolved liquids were mingled/mixed with the magmas differ-
ing in origin and chemistry (Collins et al. 2006).

Both the IR

345

and the apatite

Sr/

Sr ratios (0.706980

and 0.707620 adequately) could suggest at least mixed (I/S)
origin (Table 9). As the apatite

Sr/

Sr ratio is higher then

345

either system disturbance or the “foreign” character of

apatite  in  the  rock  can  be  suggested.  The  whole-rock  Rb-Sr
isotopic system may have been easily disturbed by a younger
episode  or  may  not  be  representative  of  the  real  whole-rock
value  if  the  enclave  size  (and  consequently  the  sample)  is
small. Another possibility is the assumption that during filter
pressing  of  the  cumulate  material  the  squeezed  melt  was
mixed and isotopically equilibrated with more mafic magma.
The presence of a large amount of interstitial liquid might influ-
ence the equilibration between the enclave and the host magma
(Elburg 1996). In fact, apatite Ap

crystals, showing deep disso-

lution embayments and irregular internal zoning (Fig. 5a,b),
could be interpreted in terms of magma mixing regime (Słaby
& Martin 2008). The incoherence between the U-Pb zircon dat-
ing (last marked episode at 345 Ma) and the Rb-Sr errorchrone
point out that more then one process affected the isotope system
and diffusion played an important role (Elburg 1996).

The measured apatite

143

Nd/

144

Nd ratio is lower than that in

the whole-rock sample, but higher than IR

345

(Table 9). Be-

cause of the slow diffusion the LREE are thought to be less
sensitive to secondary processes than Rb-Sr system (Pin et al.
1990). The calculated

345

value of —3.548 (Table 9) would

imply a crustal provenance for the enclave. As both

345

and

the calculated T

model age of the enclave (1.341 Ga, Ta-

ble 9) are similar to those calculated for common Tatra gran-
ites (sample CGT, Table 9, Gawęda, in print), and also fall in
the interval stated for typical West Carpathian Variscan gran-
ites (Kohút et al. 1999) it is possible that the enclave material
was in a crustal environment for a long time or it is genetically
linked with it.

Assuming the genetic link between the common Tatra gran-

ite  (360—340 Ma)  and  apatite-rich  cumulate  the  U-Pb  age  of
361 Ma, found in selected zircon grains (one core with mag-
matic  zonation  and  2  mantles)  together  with  345 Ma  zircon
rims,  can  mirror  one  prolonged  magmatic  process.  Such  a
long time span for a magmatic activity marks either the mag-
ma convection in the chamber and/or the replenishment by the
mafic magma pulses, forming together the prolonged magma
crystallization  and  formation  of  the  hybrid  features.  Such  a
conclusion is consistent with the presence of two MME types,
representing  two  mingling  episodes  (Gawęda,  in  print).  The
presence  of  the  cumulate  enclave,  showing  features  of  both
crustal- and mantle-derived magma influence, shed new light
on the origin and history of meso-Variscan granitoid magma-
tism, till now assumed to be purely S-type.

Concluding remarks

1. Chemical and mineralogical signatures suggest that the

apatite-rich enclave has a hybrid character with similarities to
the ca. 360—340 Ma common Tatra granite. It can reasonably
be interpreted as the cumulate fraction, formed by the crystal
accumulation, possibly during magma flow.

2. The present enclave mineralogy is a result of mostly mag-

matic processes (magma mixing/mingling), and changes in
water content, calcium activity and oxygen fugacity, usually
occurring during magma mixing.

3. The P-T history of the rock was partly overprinted by the

younger High Tatra granite. Petrographical and geochemical
data suggest that the temperature reached 740—775

°C 8 kbar

at the base of the crystal-mush layer.

4. The ca. 361—345 Ma hybrid apatite-rich rock is a unique

feature of the geology of the Tatra Mts massif that spans a his-
tory of the meso-Variscan magmatism.

Acknowledgments:  R.  Piwkowski  and  E.  Lichota,  Tatra
guides, are thanked for help during climbing, field work and
sample transportation. Dr P. Dzierżanowski and Mrs. L. Jeżak
helped with microprobing and E. Teper with zircon imaging.
Dr J. Burda did the zircon dating in Vienna University. Prof.
U. Klötzli provided the Lam-Tool computer program for U-Pb
data  correction  and  plotting.  Prof.  J.A.  Winchester  (Keele
University,  GB)  and  Dr  P.S.  Kennan  (University  College
Dublin,  Ireland)  are  thanked  for  English  corrections  and  for
discussions  during  the  investigation.  The  work  gained  sub-
stantially from advice from Prof. B. Bonin, Prof. E. Słaby and
from  reviewer’s  comments  by  Dr  I.  Broska,  Dr  I.  Petrík  and
Prof.  R.  Kryža.  Polish  Ministry  of  Sciences  and  Education
Grant No. 2 PO4D 05629 founded the research.

References

Backer M.B. & Wyllie P.J. 1992: High-presure apatite solubility in

carbonate liquids: implications for mantle metasomatism.
Geochim. Cosmochim. Acta 56, 3409—3422.

Barbarin B. 2005: Mafic magmatic enclaves and mafic rocks associ-

ated with some granitoids of the central Sierra Nevada
batholith, California: nature, origin, and relations with the

306

GAW

host. Lithos 80, 155—177.

Beard J.S. 2008: Crystal-melt separation and the development of iso-

topic heterogeneities in hybrid magmas. J. Petrology 49, 5,
1027—1041.

Broska I., Petrík I. & Williams C.T. 2000: Coexisting monazite and

allanite in peraluminous granitoids of the Tribeč Mountains,
Western Carpathians. Amer. Mineralogist 85, 22—32.

Brown W.L. & Parsons I. 1989: Alkali feldspars: ordering rates,

phase transformations and behaviour diagrams for igneous
rocks. Mineral. Mag. 53, 25—42.

Burda J. 2006: U-Pb zircon age of partial melting in metapelites from

the Western Tatra Mts. Miner. Pol., Spec. Pap. 29, 111—114.

Burda J. 2007: U-Pb zircon age of leucogranite formation ion the

crystalline basement of the Western Tatra Mts. Miner. Pol.,
Spec. Pap. 31, 85—88.

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

nology of the Goryczkowa type granite – Tatra Mts., Poland.
Miner. Pol., Spec. Pap. 31, 89—92.

Collins W.J., Wiebe R.A., Heally B. & Richards S.W. 2006: Replen-

ishment, crystal accumulation and floor aggradation in the
megacrystic Kameruka Suite, Australia. J. Petrology 47, 11,
2073—2104.

Deditius A. 2004: Characteristic and isotopic age of the muscovite

blasthesis from the mylonitic zones in the crystalline rocks of
the Western Tatra Mountains. University of Silesia Publishing
House, Geology, 16, 121—152 (in Polish, English abstract).

Dorais M.J., Lira R., Chen Y. & Tingey D. 1997: Origin of biotite-

apatite-rich enclaves, Achala batholiths, Argentina. Contr. Min-
eral. Petrology 130, 31—46.

Eklund O., Konopelko D., Rutanen H., Fröjdö S. & Shebanov A.D.

1998: 1.8 Ga Svekofenian post-collisional shoshonitic magma-
tism in the Fennoscandian shield. Lithos 45, 87—108.

Elburg M.A. 1996: Evidence of isotopic equilibration between micro-

granitoid enclaves and host granodiorite, Warburton Granodior-
ite, Lachlan Fold Belt, Australia. Lithos 38, 1—22.

Gawęda A. 1995: Geochemistry and Rb/Sr isochron age of pegma-

tites from the Western Tatra Mts. (S-Poland). Geol. Carpathica
46, 2, 95—99.

Gawęda A. 2005: P-T metamorphic evolution preserved in metapelit-

ic xenoliths from the High Tatra granite. Miner. Soc. Pol., Spec.
Pap. 25, 286—290.

Gawęda A. 2006: Apatite-rich rock from the High Tatra Granite,

Western Carpathians. Miner. Soc. Pol., Spec. Pap. 29, 127—130.

Gawęda A. 2007a: Mafic microgranular enclaves in the High Tatra Gran-

ite – preliminary report. Miner. Pol., Spec. Pap. 31, 111—114.

Gaweda A. 2007b: Variscan granitoid magmatism in the Tatra Moun-

tains – the history of subduction and continental collision.
Granitoids in Poland — AM Monographs No. 1, 319—332.

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.
Mineral. Petrology 191, 1, 95—109.

Grabowski J. & Gawęda A. 1999: Preliminary paleomagnetic study

of the High Tatra granites, Central Western Carpathians, Poland.
Geol. Quart. 43, 3, 263—276.

Janák M. 1993: Calc-silicate metamorphic rocks of the High Tatra

crystalline basement. Miner. Slovaca 25, 177—182 (in Slovak).

Janák M. 1994: Variscan uplift of the crystalline basement, Tatra

Mts., Central Western Carpathians: evidence from

Ar/

Ar la-

ser probe dating of biotite and P-T-t paths. Geol. Carpathica 45,
5, 293—300.

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., Kovach V.P., Kotov A.B., Salnikova E.B. & Savatenkov

V.M. 1999: Sr and Nd isotope geochemistry of Hercynian granitic

rocks from the Western Carpathians – implications for granite
genesis and crustal evolution. Geol. Carpathica 50, 6, 477—487.

Konopelko D., Eklund O. & Ivanikov V. 1998: 1.8 Ga phosphorus-

rich lamprophyre-granitoid complex in the Fennoscandian
shield: parental magmas and fractionation paths. Acta Univ.
Carolinae, Geol. 42, 1, 51—54.

Le Maitre R.W., Bateman P., Dudek A., Keller J., Lameyre Le Bas

M.J., Sabine P.A., Schmid R., Sorensen H., Streckeisen A.,
Woolley A.R. & Zenettin B. 1989: A classification of igneous
rocks and glossary of terms. Blackwell, Oxford, 1—193.

Long P.E. & Luth W.C. 1986: Origin of K-feldspar megacrysts in

granitic rocks: implication for the partitioning model for barium.
Amer. Mineralogist 71, 367—375.

Luais B. & Hawkesworth C.J. 1994: The generation of the continen-

tal crust: an integrated study of the crust forming processes in
the Archean Zimbabwe. J. Petrology 28, 921—953.

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

toolkit for Microsoft Excel. Berkeley Geochronology Center.,
Spec. Publ. 4.

Monier G. & Robert J.-L. 1986: Titanium in muscovites from two-

mica granites: substitution mechanism and partition with coex-
isting biotites. Neu. Jb. Mineral. Abh. 153, 147—161.

Pawlica W. 1918: Garłuchowskie calc-silicate rocks. Rozprawy

Wydziału Matematyczno-Przyrodniczego 13, 107—130 (in Polish).

Petrík I. & Broska I. 1994: Petrology of two granite types from the

Tribeč Mountains, Western Carpathians: an example of allanite
( + magnetite) versus monazite dichotomy. Geol. J. 29, 59—78.

Pitcher W.S. 1997: The nature and origin of granite. 2

edition.

Chapman & Hall, London—New York, 1—387.

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

study of the Western Carpathians: implications for the Paleozoic
evolution. Schweiz. Mineral. Petrogr. Mitt. 81, 159—174.

Pupin J.P. 1980: Zircon and granite petrology. Contr. Mineral. Pe-

trology 73, 207—220.

Schmidt M.W. & Poli S. 2004: Magmatic epidote. Rev. Mineral.

Geochem., MSA, 56, 399—430.

Slama J., Kosler J., Schaltegger U., Tubrett M. & Gutjahr M. 2006:

New natural zircon standard for laser ablation ICP-MS U-Pb
geochronology. Abstract WP05, Winter Conference on Plasma
Spectrochemistry, Tucson, 187—188.

Słaby E. & Martin H. 2008: Mafic and felsic magma interaction in

granites: the Hercynian Karkonosze pluton (Sudetes, Bohemian
Massif). J. Petrology 49, 2, 353—391.

Słaby E., Galbarczyk-Gąsiorowska L. & Baszkiewicz A. 2002: Man-

tled alkali-feldspar megacrysts from the marginal part of the
Karkonosze granitoid massif (SW-Poland). Acta Geol. Pol. 52,
4, 501—519.

Spencer K.J. & Lindsley D.H. 1981: A solution model for coexisting

iron-titanium oxides. Amer. Mineralogist 66, 1189—1201.

Stacey J.S. & Kramers J.D. 1975: Approximation of terrestrial lead

isotope evolution by a two-stage model. Earth Planet. Sci. Lett.
26, 207—221.

Tsuboi M. & Suzuki K. 2003: Heterogeneity of initial

Sr/

Sr ratios

within a single pluton: evidence from apatite strontium isotopic
study. Chem. Geol. 199, 189—197.

Vincenzo G.D. & Rocchi S. 1999: Origin and interaction of mafic

and felsic magmas in evolving late orogenic setting: the Early
Paleozoic Terra Nova Intrusive Complex, Antarctica. Contr.
Mineral. Petrology 137, 15—35.

Watson T.M. & Harrison E.B. 1983: Zircon saturation revisited: tem-

perature and composition effects in a variety of crustal magma
types. Earth Planet. Sci. Lett. 64, 295—304.

Wiedenbeck M., Alle P., Corfu F., Griffin W.L., Meier M., Oberli

F., von Quadt A., Roddick J.C. & Spiegel W. 1995: Three nat-
ural zircon standards for U-Th-Pb, Lu-Hf, trace element and
REE analyses. Geost. Newsletter, 19, 1—23.