Granitoids in Poland, AM Monograph No

Granitoids in Poland, AM Monograph No. 1, 2007, 307-317

Multistage evolution

of the granitoid core in Tatra Mountains

Edyta Jurewicz

Abstract: Tatra Mountains, the northernmost part of the Central Western Carpathians, are
composed of a Variscan crystalline basement covered by Mesozoic sedimentary complexes.
Investigations of the crystalline core of the Tatra massif indicated multistage granitoid magmatism.
The first magmatic events took place in the Early Devonian, and were followed by events in the
Late Devonian/Early Carboniferous. During the Carboniferous, when diorites and younger granites
intruded, the older granites were affected by high-grade metamorphism. During the Triassic,
Jurassic and Early Cretaceous, the crystalline core of Tatra Mountains as a part of the Austroalpine
basin became covered by sediments. Nappe-thrusting and folding processes occurred during the
Late Cretaceous. In the Paleogene, the Tatra massif was buried again and covered by carbonate
deposits and a post-orogenic flysch sequence. The uplift of the Tatra massif and appearance of the
mountain range in morphology took place in the Late Miocene.

Key words: granite, nappe-thrusting, shear zone, crystalline cap, rotational uplift, Tatra

INTRODUCTION

Tatra Mountains are the northernmost part of the Central Western Carpathians. They are
composed of a Variscan crystalline basement and its sedimentary complexes (Fig. 1)
belonging to the Tatric-Fatric-Veporic nappe system (Andrusov 1968; Mahel’

1986;

Plašienka et al. 1997). Their crystalline core is composed of two older structural
elements: the predominantly metamorphic sequences of Western Tatra Mts. and the
granitoid rocks of High-Tatra Mts. (e.g.

Putiš 1992; Janák 1994). The crystalline core of

Tatra Mts. is overlain by Mesozoic sedimentary sequences, which correlate well with the
Austroalpine units (Häusler et al. 1993; Plašienka et al. 1997). Three groups of structural
units (Figs. 1 and 2) comprise the Mesozoic sedimentary strata (Kotański 1963):
1) the High-Tatric autochthonous sedimentary cover;
2) the High-Tatric nappes divided into:

a) Czerwone Wierchy nappe;

b) the Giewont nappe, distinguished by the presence of a crystalline core (the so-

called “Goryczkowa type of granites”);

3) the Sub-Tatric nappes divided into:

a) the Krížna nappe;
b) the Choč nappe.

Nappe-thrusting and folding in Tatra Mts. are of Late Cretaceous age and are traditionally
linked with the Mediterranean orogenic phase (Andrusov 1965). The Tatra massif is
overlapped by carbonate deposits of the so-called Nummulitic Eocene and a post-
orogenic Paleogene flysch sequence (e.g. Bieda 1959; Gedl 1999). In the topographic
sense the Tatra massif emerged to the surface due to its Miocene rotational uplift

307

(northerly tilting, see Sokołowski

1959;

Piotrowski

1978;

Bac-Moszaszwili et al. 1984;

Jurewicz 2000). The asymmetric uplift caused that the Tatra massif is bounded from the
south (Figs. 1 and 3) by the Sub-Tatra fault (Uhlig 1899). The youngest sediments in the
Tatra Mts. area are related to Pleistocene glaciations and Holocene erosion-accumulation
processes.

Fig. 1. Schematic geological map of Tatra Mts. and related area; compiled after Fusán et al. (1967),
Bac-Moszaszwili et al. (1979), Birkenmajer (1979) and Jurewicz (2005).

CRYSTALLINE MASSIF OF WESTERN TATRA

The massif is composed of metamorphic rocks, mainly metagneisses, migmatites and
mica-schists (metasedimentary rocks), as well as orthoamphibolites and orthogneisses.
Two tectonic units can be distinguished within the crystalline core (Janák 1994; Poller et
al. 2000). The lower unit, composed of medium-grade metasedimentary rocks (mica-
schists), is exposed in Western Tatra Mts. only. Based on kyanite-staurolite relics which
resulted in upper amphibolite facies conditions, Janák (1994) recognised the pressure and
temperature of ca. 700 MPa and 640ºC. Investigations on garnet-bearing mica-schists
after Gurk (1999 in: Poller et al. 2000) show medium P-T conditions with 600-900 MPa
and 650-750ºC. The upper unit is divided into two parts. The lower one comprises older
granites (orthogneisses), paragneisses and amphibolites and bears evidence of high-grade
metamorphism: 1000-1400 MPa and 700-800ºC (Janák et al. 1996). The higher part of

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of oceanic crust and Middle Devonian to Early Carboniferous continental collision.
During this interval, two main magmatic events took place in Tatra Mts. (op. cit.).
Based on U-Pb zircon data, older and younger granitoids can be distinguished. The older
granitoids, which are the igneous precursor of the orthogneisses and which intruded in
Lower Devonian strata (405 Ma), are connected with subduction-related melting (Poller
et al. 1999). The associated high pressure metamorphism (Janák et al. 1996) was
interpreted as anatectic melting within the continental crust (Poller et al. 2000). The
younger granitoids are dated as Late Devonian/Early Carboniferous (between ~350-360
Ma – op. cit.). During this interval, continent collision took place; subsequently, when the
younger granites appeared, the older granites were affected by high-grade metamorphism.
At the beginning of the Variscan continent collision (Laurussia and Gondwana), the High
Tatra diorites appeared. The age of the intrusion at 341±5 Ma is documented by U-Pb
single zircon data of Poller and Todt (2000). During the final stage of Variscan continent
collision, the High Tatra granites intruded (Fig. 4 part 1). These granites have an
intrusion age of 314±4 Ma (op. cit.). According to

Ar/

Ar and Rb/Sr methods

(Burchart 1968; Maluski et al. 1993; Janák 1994; Kohút, Sherlock 2003), the isotopic age
values of the granitoids range between 300-330 Ma. The depth of the magma intrusion
was estimated at 18-22 km, what corresponds to 500-600 MPa and 450-550ºC (Kohút,
Janák 1994).

GEODYNAMIC EVOLUTION

OF THE CRYSTALLINE CORE OF TATRA MOUNTAINS

Variscan stage. During this stage the first tectonic deformation of the crystalline
basement was connected with NW-SE thrusting of the upper unit onto the lower unit
(Fritz et al. 1992; Janák 1994). The second tectonic deformation is connected with W-E
extension. Both stages of deformation yielded in ductile behaviour (Kohút, Janák 1994).

Alpine stage. The Variscan orogenic belt collapsed in the Late Permian (Plašienka et al.
1997). The Tatric-Fatric-Veporic convergence zone of Central Western Carpathians
involved a basinal area that originated due to Early Jurassic rifting of Variscan
continental crust (Plašienka 2003).

Within Western Carpathians sea spreading could be linked with the eastward lateral
propagation of the Alpine Tethys rift (Dumont et al. 1996). After Plašienka (2003), four
principal rifting phases can be distinguished based on bathymetric evolution. Two Early
Jurassic rifting phases, being the result of lithospheric stretching and breakdown of the
epi-Variscan Triassic platform (Fig. 4 parts 2-4), were accompanied by crustal heating
documented by a radiometrically dated thermal event in the Tatric basement around 200
Ma (Maluski et al. 1993; Kral’ et al. 1997). However, at that time, no volcanism activity
can be observed in the sediments. The next two rifting phases resulted from the break-up
of the South Penninic – Vahic Ocean in the Middle Jurassic and the North Penninic –
Magura Ocean in the Early Cretaceous (Plašienka 2003).

During the Middle Jurassic, the High-Tatric sedimentation zone formed an isolated
elevation surrounded by the Vahic basin in the north and Fatric basin in the south. The
submerging of part of the High-Tatric area during the Batonian may have been caused by
tectonic block movements accompanied by neptunian dykes (Łuczyński 2001) and
possibly also by normal faulting within the granitoid core (Fig. 4 parts 4-5).
Synsedimentary normal faulting and blocks rotation could be observed in the
autochthonous cover of the crystalline core in the Kominy Tylkowe succession, where
a listric normal fault caused rotation of the hanging wall from horizontal to steeper dip
and increase of sediment thickness (Jurewicz 2002, 2005). Evidence of tectonic activity

310

and increase of sediment thickness (Jurewicz 2002, 2005). Evidence of tectonic activity
during the Early Berriasian may be carbonate scarp breccia and basic volcanics
(limburgite and tufite interbeds) at Osobita Mt. (Lefeld et al. 1985; Staniszewska,
Ciborowski 2000).

Fig. 4. Changes in the burial depth of the crystalline basement during the tectonic evolution of
Tatra Mts. (Jurewicz 2005).
1) Age of intrusion and P-T condition: 310-290 Ma after Rb-Sr isochron data (Burchart 1968),
330±3 Ma Ar/Ar dating in muscovite (Maluski et al. 1993), 500 MPa, 600-630

C after xenoliths in

calc-silicate metamorphic rocks of -Tatra (Janák 1993), 341±5 Ma and 700-750

C – High-Tatra

diorites and 314±4 Ma – High-Tatra granites after single zircon data (Poller, Todt 2000);
2) subaerial erosion; 3), 4), 5) extension and normal faulting; 6) Late Cretaceous thrusting and
napping processes: 75±1 Ma – age related to the main period of shearing, 66.6±1.5 Ma – intense
mylonitic events (Maluski et al. 1993), P ~145-170 MPa, T~212-254°C (Jurewicz, Kozłowski
2003), 7-8 km burial depth during the Late Senonian (Kováč et al. 1994), 7) plunging during the
Paleogene extension stage, 8) rotational uplifting (in total ~40

northwards – Jurewicz 2000),

exhumation and erosion, start of uplift: 36-10 Ma after fission track ages (Burchart 1972); 70-50
Ma from the depths of 10-11 km (225

C) and 30-15 Ma from depths of 5 km (100

) (Kováč et al.

1994), 11 Ma for the granitoids of High-Tatra Mts. and 20-12 Ma for the crystalline core of
Western Tatra Mts. after apatite fission-track analysis (Struzik et al. 2002), a) granitoids, b)
metamorphic rocks, c) Carboniferous (?), d) Triassic sandstone, shale and carbonate, e) Jurassic
carbonate and radiolarite, f) Cretaceous reef limestone and flysch, g) High-Tatric autochthonous
cover, h) High-Tatric nappe, i) Krížna nappe, k) Choč nappe, l) Central Carpathian Paleogene, m)
crystalline caps.

The Late Cretaceous (post-Turonian) nappe-thrusting and folding proceeded from the
south, gradually engaging the more northward sedimentary zones (Fig. 4 part 6). During
the latter phase of nappe-thrusting processes some parts of the crystalline basement of the
Giewont nappe were detached and thrusted onto the sedimentary rocks of the Czerwone
Wierchy nappe. As a result, tectonic caps of crystalline rocks originated (the so-called
“Goryczkowa Island” composed of Goryczkowa-type granites). The last stage of Alpine
folding and napping due to basement shortening within the Central Carpathians included
the underthrusting of the crystalline massif together with the sedimentary cover under the
previously arisen Krížna and Choč nappes, forming the High-Tatric nappes and folding

311

of the autochthonous cover. The thrust-folding of the Choč, Krížna and High-Tatric
nappes took place underwater and at considerable overburden pressure (~6-7 km) and
with a geothermal gradient (~30ºC/km).

Reconstruction of the stress field on the base of fault plane and striae systems indicates
that during nappe-thrusting either a relative change of the largest stress orientation (σ

)

from NW to N and NNE took place, or at a stable compression orientation the counter-
clockwise rotation of the basement occurred. The effect of this rotation were the changing
directions from NW to NNE of thrust faulting within the granitoid core and nappe-
thrusting within the sedimentary cover (in total ~45º

around the vertical axis).

Neogene. During the Eocene the western part of the Alpine-Carpathian convergence
underwent a change from subduction to collision. The Miocene subduction of the North-
European continental crust beneath the northern margin of the Central Carpathian massifs
caused the shearing of the granitoid massif of Tatra Mts. at the depth of about 10 km and
its overthrust onto the sedimentary rocks of the North-European platform (Fig. 4 part 8)
(Lefeld, Jankowski

1987;

Bielik et al. 2005). The shearing was possible due to the

appearance of more brittle behaviour resulting from crust cooling and decrease of the
geothermal gradient (which reached 30ºC during Late Cretaceous folding – Jurewicz,
Bagiński 2005) due to subduction of cold continental crust.

The uplift of the Tatra massif and appearance of the mountain range in morphology
above the surrounding Orawa-Nowy Targ foredeep is linked with the Late Miocene uplift
of the Central Carpathian massifs. The uplift for Tatra Mts. from below 5 km (100ºC), as
documented by apatite fission-track data after Burchart (1972), indicated the uplift age at
about 26-10 Ma. After Kováč et al. (1994) uplifting of the Tatric pre-Alpine complexes
started from the depths of 10-11 km (225ºC) about 70-50 Ma ago and reached the depth
of 5 km (100º) 30-15 Ma ago. Fission-track data in relation to the stage of the Tatra uplift
from 2 km (60ºC) indicate an interval between 7-2 Ma (Baumgart-Kotarba, Král 2002).
The most recent apatite fission-track analysis of the uplift (Struzik et al. 2003) indicated
ca. 11 Ma for the granitoids of High Tatra Mts., 20-12 Ma for the crystalline core of
Western Tatra Mts. and 7.6 (±1.2) Ma for the flysch sandstones from Podhale. The latter
authors, similarly as Baumgart-Kotarba and Král (2002), pointed to the uneven and
higher uplift of High Tatra Mts. Also the structural analysis of granitoids of High Tatra
Mts. indicates a western plunge of the B axis ~265/15° obtained due to stress field
reconstruction after slickenside striation on the fault planes (Jurewicz 2000, 2002), what
might have connection with the asymmetric uplift of Tatra Mts.

The uplift of the Tatra block was accompanied by the formation of the Sub-Tatric fault in
the south, recognized already by Uhlig (1899), as well as by the folding of the Podhale
flysch in form of a basin (Gołąb 1959; Mastella 1975). The Sub-Tatric fault, along which
the Tatra massif contacts with the Paleogene flysch of the Liptov trough (Figs. 1 and 3),
is a polygenetic and multiply activated tectonic fault system, consisting of several
segments (Uhlig 1899; Mahel

′

1986;

Sperner

1996;

Hrušecký et al. 2002; Sperner et al.

2002). The uplift of the Tatra block was rotational in character. The rotation angle
comprising: the dip of the Nummulitic Eocene and the Mesozoic sedimentary cover,
erosion gradient of the Tatra granitoid core and the displacement along the Sub-Tatric
fault is different in the estimations of particular authors. Piotrowski (1978) accepted 20º,
whereas Bac-Moszaszwili (1995) – 30-35º. A rotation angle of 40º was evaluated on the
basis of the reconstruction of the stress field obtained after the striation analysis on low-
angle dipping faults in the granitoid core of High Tatra Mts. (Jurewicz 2000).

312

According to some authors, i.e. Kotański (1961) and Sperner (1995), the Sub-Tatric fault
is a reverse fault; however, the concept of a normal dip-slip character of this fault prevails
(Mahel’ 1986; Hrušecký et al. 2002). The reverse character of this fault – as calculated
by Sperner (1995) – would be responsible for displacement in the range of 29 km, with
what would be connected the manifestations of metamorphism, and what was questioned
i.e. by Petrík et al. (2003) and Kohút and Sherlock (2003). The age of the Sub-Tatric fault
is inseparably connected with the Tatra Mts. uplift documented by fission-track data.
Kohút and Sherlock (2003) linked the commencement of its activity (36-28 Ma) with
pseudotachylites and showed its syn-sedimentary character (during the sedimentation of
the Central Carpathian Paleogene flysch sequence). The large-scale detachment character
of the Sub-Tatric fault is well visible in the reflection seismic profile of Hrušecký et al.
(2002).

TECTONIC STRUCTURES

On the basis of structural analysis, three groups of structures can be distinguished, the
development of which was initiated in three tectonic stages:
The pre-Alpine structures sensu lato, with relicts of structures linked with the late
Variscan extension distinguished by Kohut and Janák (1994), as well as those developed
during the Early Jurassic rifting of the Variscan continental crust (Plašienka, Prokešová
1996; Plašienka 2003). Deformations in these zones are of semiductile character. Within
the shear zones represented by mylonites and cataclasites, small folds, often of a drag-
fold character, S-C structures and elongation lineation can be distinguished. The ductile
deformations are often associated with numerous slip planes. The dips of shear planes,
with regard to the Neogene rotation, are rather steep (ca. 60

°) and more typical of normal

faults than low-angle dipping thrusts, whereas the sense of movement determined e.g. in
the Galeria Cubryńska Ridge on the basis of S-C fabrics indicates a reverse fault, what
testifies for its multiple reactivation. Zones of this type were also reactivated in the
presence of the Neogene stress field as sinistral slip-oblique faults, what is connected
with slickenside striations on the epidote-coated wallrocks.

The Alpine structures, linked with horizontal NW and N compression and the resulting
thrust folding, which in the granitoid core are marked by the presence of low-angle
dipping thrust faults with thinned fault fissure, and planar slickenside surfaces coated
with quartz, epidote and chlorite. The primary dips of these planes obtained from rotation
to positions prior to the Neogene uplift were southward-directed. These faults do not bear
traces of activation during younger tectonic phases. Data obtained from fluid inclusions
studies (Jurewicz, Kozłowski 2003) proved that synkinematic quartz on planar
slickenside surfaces (connected with Alpine thrust-napping) crystallized at higher
pressures and lower temperatures (145-170 MPa, 212-254°C) than the quartz veins in the
mylonitic zones (130-163 MPa, 264-316°C). The pressure values of 145-170 MPa for the
structures linked with Alpine thrust folding allow to estimate the depth of the
deformation processes at 6-7 km.

Neogene structures, linked with the rotational uplift of the Tatra block (Piotrowski
1978; Kováč et al. 1994; Sperner 1996; Jurewicz 2000) and the accompanying 106-120º
extension. During this stage several sinistral strike-slip faults or oblique-normal-slip
faults were formed and the activation of older mylonitic zones took place, where
detachment along the walls and a strike-slip movement occurred (Jurewicz 2002). These
faults were formed in the present position of the Tatra block and do not require rotation.
The convergence of the orientation of some older mylonitic zones in the present position

313

of the Tatra block with the position of faults developed in the Neogene could be
responsible for the activation and rejuvenation of the older zones.
During the Pleistocene and Holocene, a crucial role in the geomorphic evolution of Tatra
Mts. was played by glaciations, after the retreat of which isostatic movements could take
place. The neotectonic activity in Tatra Mts., PKB and related areas has been documented
by different methods. Grodzicki (1979) investigated the nature of neotectonic movements
on the base of corrosional etching horizons in caves. Baumgart-Kotarba

(1981, 2001)

carried out morphometric analyses of river terraces in Podhale and Orawa. Rączkowski et
al. (1984) and Zuchiewicz (e.g. 1998) analyzed the variability of vertical movements on
the basis of indirect evidence, provided by geomorphological mapping, construction of
various morphometric maps based on mathematical transformation of present-day
topography, and use of mathematical techniques to model theoretical longitudinal river
profiles and valley network and statistically process the drainage pattern parameters.

Makowska and Jaroszewski (1987) concluded on the neotectonic activity of Tatra Mts.
based on precise levelling data. These data might suggest a continuing rotational uplift of
the Tatra massif. Evidence of neotectonic activity in the study area could be the
earthquake which took place in the end of December 2004 (4.7 magnitudes in Richter
scale). Its epicentre was located near the Czarny Dunajec village and could be correlated
with the activation of a NNW-SSE strike-slip fault marked on the map and termed the
Czarny Dunajec fault (Fig. 1).

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