www.geologicacarpathica.com
GEOLOGICA CARPATHICA
, JUNE 2016, 67, 3, 257–271
doi: 10.1515/geoca-2016-0017
Age and provenance of mica-schist pebbles from the Eocene
conglomerates of the Tylicz and Krynica Zone
(Magura Nappe, Outer Flysch Carpathians)
NESTOR OSZCZYPKO
1
, DOROTA SALATA
1
and PATRIK KONEČNÝ
2
1
Jagiellonian University, Institute of Geological Sciences, Oleandry 2a, 30-063 Kraków, Poland;
nestor.oszczypko@uj.edu.pl; dorota.salata@uj.edu.pl
2
State Geological Institute of Dionýz Štúr, Mlynská dolina 1, 817 04 Bratislava, Slovakia; patrik.konecny@geology.sk
(Manuscript received December 24, 2014; accepted in revised form March 10, 2016)
Abstract: During the Late Cretaceous to Palaeogene, the Magura Basin was supplied by clastic material from source
areas situated on the northern and southern margins of the basin, which do not outcrop on the surface at present.
The northern source area is traditionally connected with the Silesian Ridge, whereas the position of the southern one
is still under discussion. A source area situated SE of the Magura Basin supplied the Eocene pebbly para-conglomerates
containing partly exotic material. The studied clastic material contains fragments of crystalline rocks, and frequent
clasts of Mesozoic to Palaeogene deep and shallow-water limestones. Numerous mica schists, scarce volcanites and
granitoids as well as gneisses, quartzites and cataclasites were found in the group of crystalline exotic pebbles. Mona-
zite ages of “exotic” mica-schist pebbles from the Tylicz, Zarzecze and Piwniczna-Mniszek sections document
the Variscan 310±10 Ma age of metamorphic processes. The provenance of these exotic rocks could be connected with
a remote source area located SE of the Magura Basin, which could be the NW part of the Dacia Mega Unit. The idea is
strongly supported by palaeotransport directions from the SE, the absence of material derived from the Pieniny Klippen
Belt, the presence of shallow water limestones, typical facies of the Median Dacides belt and metamorphic age distri-
bution proved by monazite dating.
Key words: Magura Basin, palaeogeography, source areas, monazite age, mica-schist pebbles.
Introduction
The Outer Carpathian flysch basins were supplied with clas-
tic material derived both from external as well as internal
source areas, so-called “cordilleras” (Książkiewicz 1962;
Unrug 1968). Our palaeogeographical reconstructions of the
source areas are based on the investigations of “exotic” peb-
bles that were transported into sedimentary basins by subma-
rine gravity flows (see Książkiewicz 1962). The Eocene/
Oligocene deposits of the Tylicz and Krynica facies zone of
the Magura Basin contain fragments of sedimentary, igneous
and metamorphic rocks, derived from a continental type of
crust. The location of the source area in the present-day tec-
tonic configuration is unknown. Mišík et al. (1991) suggested
that carbonate material was derived from “the basement of
the Magura Basin”, that was exhumed during the Early/Mid-
dle Eocene. This material is fundamentally different from the
carbonates of the Czorsztyn/Oravicum of the Pieniny Klip-
pen Belt (PKB) which are currently located along the southern
boundary of the Magura Nappe. Alternatively, this clastic
material may have been derived from a Central Carpathian
source area type, located on the SE margin of the basin (e.g.,
tip of the ALCAPA Block, see Plašienka 2000). The aim of
this paper is to present results of the monazite dating of
metamorphic pebbles from the Tylicz, Mniszek-Piwniczna
and Zarzecze sections of the Krynica subunit of the Magura
Nappe and to identify possible sources for the pebbles.
Outline of geology and stratigraphy
Previous studies on the exotic pebbles
The “exotic” conglomerates in the Tylicz and Krynica zones
of the Magura Nappe (Fig. 1), have been studied for many
years (Jaksa-Bykowski 1925; Mochnacka & Węcławik 1967;
Wieser 1970; Oszczypko 1975; Oszczypko et al. 2006, Olszew-
ska & Oszczypko 2010). The first detailed description of
exotic pebbles from the Eocene deposits of the Beskid Sądecki
Range (Krynica zone) was given by Oszczypko (1975). This
author described granitoids, gneisses, phyllites and quartzites,
with a relatively small amount of basic volcanic rocks and
Mesozoic carbonates. The exotic carbonate material of the
Strihovce Sandstone, an equivalent of the Piwniczna Sand-
stone Member of the Magura Formation in Poland, has been
studied by Mišík et al. (1991). Recently Olszewska and Osz-
czypko (2010) studied the carbonate pebble population of the
Tylicz Conglomerate, which is dominated by deep-water Ju-
rassic–Lower Cretaceous sediments as well as fragments of
shallow-water limestones of Triassic, Upper Jurassic, Lower
and Upper Cretaceous, Palaeocene and Lutetian age.
Geological setting
The studied area is located in the south-eastern part of the
Magura Nappe, south of the boundary between the Bystrica
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and Krynica subunits (Fig. 1). The Krynica facies-tectonic
zone is composed of the Upper Cretaceous to Oligocene de-
posits (Birkenmajer & Oszczypko 1989; Oszczypko & Osz-
czypko-Clowes 2010). The oldest deposits are known from
the Muszyna-Złockie area, 5 km west of Krynica. They con-
sist of the Turonian-Maastrichtian, deep-water variegated
shales (Malinowa Fm.) with sporadic intercalations of thin -
bedded sandstones (Oszczypko et al. 1990). That formation
passes upwards into strongly tectonized, medium to thin -
bedded turbidites of the Maastrichtian/Palaeocene to Lower
Eocene (Ropianka Fm.), which are rich in calcite veins.
Higher up in the succession, thin-bedded turbidites occur
(Zarzecze Fm.), with intercalations of thick-bedded Krynica
sandstones and conglomerates of the Lower–Middle Eocene.
The youngest deposits of the Krynica facies zone in the
Krynica area belong to thick-bedded sandstones of the
Magura Fm. (Middle Eocene to Oligocene; see Oszczypko &
Oszczypko-Clowes 2010) and the recently discovered Lower
Miocene Kremna Fm. (Oszczypko et al. 2005; Oszczypko -
Clowes et al. 2013).
The stratigraphic thickness of the Magura Nappe reaches
at least 2.6 km. During overthrust movements and tectonic
repetitions, the total thickness of the flysch deposits in the
Krynica subunit increased up to 5.5–7.5 km, as shown by
magnetotelluric investigations (Oszczypko & Zuber 2002).
The Bystrica and Krynica subunits contact along the sub-ver-
tical thrust fault, which dips to the NE.
The Late Cretaceous to Oligocene flysch formations of the
Krynica succession were deposited in a deep-water basin
(Oszczypko 1992). Starting from the Early Eocene, the sedi-
mentary processes in the southern part of the Magura Basin
were accompanied by growth of the accretionary wedge (Osz-
czypko & Oszczypko-Clowes 2009). It is manifested by
shallowing of the basin and development of sub-marine
coarse-clastic fan sedimentation of the Magura Sandstone
Formation. At the turn of the Middle/Late Eocene this depo-
sition was followed by a short-lasting episode of the basin
deepening (beneath the CCD level) and deposition of varie-
gated shales of the Mniszek Sh. Mb. (Sh.=Shale;
Mb.=Member) (Oszczypko-Clowes 2001; Oszczypko & Osz-
czypko-Clowes 2006). The Late Eocene gradual shallowing
of the basin again enabled the coarse-clastic sedimentation of
the Poprad Sandstone Mb. (Fig. 2). This was followed by
folding and uplifting of the basin after the Late Oligocene/
Early Miocene and prior to the Middle Miocene (Oszczypko
et al. 2005; Oszczypko & Oszczypko-Clowes 2009).
Bodies of exotic conglomerates in the Krynica zone are
rare. Such conglomerates are related to thick-bedded turbi-
Fig. 1. Location of the studied area in: A — the Alpine-Carpathian Pannonian realm and B — within the Magura Nappe in Poland (based
on Żytko et al. 1989).
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dites of the Zarzecze and Magura
formations (Oszczypko 1975; Osz-
czypko et al. 2006). The exotic con-
glomerates of the Jarmuta-Proč
Formation of the Grajcarek Unit,
occurring along the contact zone be-
tween the Magura Nappe and Pieniny
Klippen Belt, occupy a separate po-
sition (Birkenmajer 1977; Birken-
majer & Wieser 1990).
Studied sections
Piwniczna-Mniszek section
The Piwniczna-Mniszek section
belongs to the Krynica facies zone
and is located on the left slope of the
Dunajec Valley (Fig. 1). This profile
belongs to the top part of the Pi-
wniczna Member of the Magura
Formation. The Middle Eocene va-
riegated shales of the Mniszek Shale
Member appear directly above
(Fig. 2).
The exotic rocks occur in the sub-
marine slump bed, up to 2 m thick,
which developed at the top of the
thick-bedded sandstones of the
Magura type. The slump layer is
composed of folded exotic con-
glomerates with detached blocks of
shales and armed claystones, as well
as of sandstones, mudstones and
claystones (Oszczypko et al. 2006).
The studied metamorphic pebbles
usually reach 7 cm across, while
sedimentary pebbles (sandstones
and limestones) are bigger, up to
10 cm. The material of conglo-
merates (Oszczypko et al. 2006) is
represented by: vein-quartz of meta-
morphic origin (37 %), sandstones
(35 %), igneous rocks (14 %), metamorphic rocks (11 %)
and carbonates (3 %).
Zarzecze section
The Zarzecze section, located on the right slope of the
Dunajec River (Fig. 1B), belongs to the Tylicz transitional
facies zone. The exotic beds are displayed at the top of a 170
metres thick packet of thick-bedded turbidite sadstones and
conglomerates of the Mniszek Shale Member of the Magura
Formation (Fig. 2; Oszczypko 1975; Oszczypko et al. 2006;
Oszczypko & Oszczypko-Clowes 2010). The exotic pebbles
are dominated by crystalline rocks (32 %), vine quartz of
metamorphic origin (26 %), flysch sandstones (24 %) and
Mesozoic carbonate rocks (18 %). Among the exotics sedi-
mentary rocks representing the following microfacies were
diagnosed (Oszczypko 1975; Oszczypko et al. 2006): the Ti-
thonian–Berriasian — organodetritc Calpionella limestones,
Globocheta and charty limestones, Radiolarian-Nannoconus
(Valanginian–Hauterivian) and Urgonian limestones (Barre-
mian–Aptian), Spiculla limestones (Albian–Cenomanian),
marls (Maastrichtian–Palaeocene), and Lithotamnium
Palaeocene sandstone (Oszczypko 1975).
Tylicz section
The exposures at Tylicz are situated in the transitional po-
sition (see Tylicz zone after Węcławik 1969; Figs. 1, 2) be-
tween the Bystrica and Krynica facies zones (Mochnacka &
Węcławik 1967). The lower part of this succession is typical
for the Bystrica zone, whereas the upper part belongs to the
Krynica type of facies (Oszczypko & Oszczypko-Clowes
Fig. 2. Lithology and stratigraphy of the sampled sections.
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2010). The Tylicz exotic conglomerates, belonging to the
Mniszek Shale Member of the Magura Formation (Fig. 2),
are exposed on the left bank of the Muszynka River, partly
in the bed rock of the river. The base and the top of the con-
glomerate boundaries are well exposed. The conglomerates
are underlain and overlain by thin-bedded turbidites repre-
sented by grey and dark grey marly mudstone and marly
shales (Fig. 2; see also Olszewska & Oszczypko 2010). The
marly-shaly deposits are intercalated by thin- to medium -
bedded fine-grained sandstones with muddy/marly cement.
The sandstones display the Bouma Tc and conv. divisions.
The conglomerates and thick-bedded sandstones form two
bodies of 150 m and 50 m thick, separated by a 50 m packet
of thin-bedded flysch (Fig. 2). These conglomerates repre-
sent channel infill incised in thin-bedded turbidites. In general,
these coarse-clastic deposits display a fining and thinning -
upward sequence. The basal packet of the conglomerates be-
gins with 2 m thick layer of coarse conglomerates and
boulders, which passes upwards into a 75 m thick layer of
paraconglomerate packet, composed of pebbly mudstones.
This part of the section was deposited by cohesive debris
flow. Higher up in the section the conglomerates pass up-
wards into a 75 m packet of thick-bedded coarse- to very
coarse-grained sandstones, deposited by high-concentrated
density flow. The palaeocurrent measurements suggest
palaeotransport from the SE. The conglomerates are com-
posed of pebbles of 2 do 16 cm in diameter. The biggest peb-
bles are represented by sandstones and limestones. The
material of conglomerates (Olszewska & Oszczypko 2010)
is represented by: carbonates (44 %), igneous and metamor-
phic rocks (26 %), sandstones (26 %) and other (4 %). The
biggest pebbles are spindle-shaped and ellipsoidal, while
smaller ones are dominated by spheroidal and discoidal
shapes. The carbonate pebble population contains fragments
of shallow-water limestones of the Triassic (Anisian), Kim-
meridgian, deep water Upper Tithonian limestones, as well
as the Lower Cretaceous (Urgonian), Upper Cretaceous,
Lower and Upper Palaeocene, and Lower Lutetian (Olszew-
ska & Oszczypko 2010).
Analytical methods
The chemical composition of rock-forming minerals and
monazites from the mica-schist pebbles was studied in
polished carbon-coated thin sections. In total 243 monazite
analyses in 4 samples were made (sample Tyl14-116 analy-
ses in 30 grains; sample Tyl2-48 analyses in 9 grains; sample
Mn1-63 analyses in 23 grains; sample Zar 3-16 analyses in
8 grains). Several spot analyses were made per single mona-
zite grain if possible. The monazites analysed were located
most of all in the matrix and only single grains within biotite
flakes. Minerals were analysed by electron microprobe using
a Cameca SX100 electron microprobe housed at the Dionýz
Štúr State Geological Institute, Bratislava (Slovak Republic).
The microprobe was calibrated with synthetic and natural
standards: P — apatite, Si — wollastonite, Al — Al
2
O
3
,
Pb — cerusite, Th — ThO
2
, U — UO
2
, Ca — wollastonite,
Fe — forsterite, S — barite, As — GaAs and REE plus Y
were calibrated on phosphates REEPO
4
and YPO
4
, respec-
tively. The microprobe is equipped with large (parabolic)
analysing crystals LLIF and LPET that ensure a few times
higher sensitivity then conventional (planar) ones. Monazite
dating strongly depends on the precise measurement of the
Pb, which reaches only low to trace concentrations in mona-
zites. The measurement method was therefore adjusted for
getting maximum counts especially for Pb. An accelerating
voltage of 15 kV and beam current of 120 nA were applied.
The beam diameter of 3 to7 mm was preferred. The counting
time was 100 s for Pb, 75 s for U and 45 s for both Y and Th.
Pb was measured at PbMα line, U at UMβ
1
, and Th at
ThMα. An overlap of PbMα with YLγ
1
and UMβ with ThMβ
was resolved via empirical correction (Åmli and Griffin
1975).
Before measurement of monazites of unknown age a set of
so-called age standards were measured. A collection of mona-
zite standards include monazites of various ages and compo-
sitions which were dated using SHRIMP: pegmatite from
Madagascar (495 Ma), granite form Veikkola (1825 Ma),
granite from Aalfang, Austria (327 Ma), gneiss-migmatite
from Dürstein/Wachau, Austria (341 Ma), monzogranite
from Nakae, Japan (77 Ma). Age standards provide additional
tests for accuracy of microprobe calibration and measure-
ment conditions. Some more details on the monazite dating
method are given by Konečný et al. (2004). A statistical ap-
proach following Montel et al. (1996) was used to obtain re-
sulting ages from spot microprobe analyses.
Results
Mineral composition of pebbles
The rock pebbles analysed in all localities studied are rep-
resented by mica-schists. The texture and mineral composi-
tion is alike in all samples. The texture of the schists
representing the Tylicz (Tyl2, Tyl14) and Piwniczna -
Mniszek sections (Mn1) is typical monotonous schistose tex-
ture characterized by parallel alignment of fine- to
medium-grained mica flakes (mainly biotite, muscovite) in-
tercalated with quartz, plagioclase feldspar (albite and oligo-
clase), orthoclase and accompanying minerals like garnet,
apatite, monazite, zircon, TiO
2
polymorph (Fig. 3A–C and
E–H), pyrite and xenotime. Muscovite is more abundant than
biotite in the Tyl2 sample, whereas biotite flakes dominate
among micas in the Tyl14 and Mn1 samples. Garnet grains
are scarce in all the mentioned schist pebbles. Garnet grains
follow schistose fabric forming fine anhedral grains of about
50–100 µm across rarely reaching 250 µm (Fig. 3A–C, F).
Apatite occurs as relatively large subhedral or anhedral
grains (up to 200 µm across) occurring mainly in the matrix
and less frequently within biotite flakes (Fig. 3A–B, E–F, H)
or as inclusions in feldspars. Monazite is a typical con-
stituent of the pebbles from the Tylicz and Piwniczna -
Mniszek sections. It occurs in the form of subhedral or
anhedral crystals up to 150 µm long prevailingly in the ma-
trix, rarely hosted by biotite or feldspar (Fig. 3E, G). Zircon,
similarly to monazite, occurs in between quartz or feldspar
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Fig. 3. Microphotographs of the studied mica-schist pebbles. Pictures A–D — plane polarized light; pictures E–H — YAGBSE. Abbrevia-
tions: Ap — apatite; Bt — biotite; Grt — garnet; Mnz — monazite ; Pl — plagioclase feldspar; Qz — quartz; TiO
2
— TiO
2
polymorph;
Zrn — zircon.
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grains or as inclusions in
biotite (Fig. 3B, E, G). The
schist from the Zarzecze sec-
tion (Zar3) is composed of
similar minerals to the peb-
bles from the other localities
studied. Biotite dominates
among micas, accompanied
by quartz and feldspars. Gar-
net grains are much bigger
than those from the Tylicz
and Piwniczna-Mniszek peb-
bles forming porphyroclasts
reaching up to 1mm across.
Mica and garnet yield fea-
tures of deformation showing
a N-S alignment (Fig. 3D).
Garnet grains are partly bro-
ken down and fragmented.
Monazite and apatite are less
frequent than in the Tylicz
and Piwniczna-Mniszek schist
pebbles.
Garnet from pebbles from
the Tylicz and Piwniczna
-
Mniszek sections is not zonal
in terms of main elements.
Almandine molecule prevails
in the garnet in all mica-
schists studied reaching up to
80 mol %. They are accompanied by lesser amounts of py-
rope and spessartine. Pyrope and spessartine in mica schists
from Tylicz (Tyl2) and Piwniczna-Mniszek (Mn1) usually
do not exceed 15 mol % each. The spessartine molecule
amount in sample Tyl14 is slightly elevated in respect to
Mn1 and Ty2 samples reaching up to 26 mol %. The grossu-
lar content in the mica-schists from Tylicz and Piwniczna-
Mniszek is very low, usually not exceeding 5 mol %. The
garnet population from a mica-schist pebble from the
Zarzecze section (sample Zar3) differs in composition com-
pared to other samples studied. The garnet from the Zarzecze
section displays zonality expressed in elevated grossular and
spessartine molecule amounts in the core (up to 23 mol %
and 9 % respectively) at the expense of pyrope and almandine
molecules (Table 1). Garnet chemistry from the mica-schists
of Tylicz and Piwniczna-Mniszek suggests that it was
formed in low P/T metamorphic environment, while the
composition of garnet from Zarzecze implies higher P/T
metamorphic conditions of its formation (Fig. 4).
Monazite composition and age
The contents of Th and U and LREE like La, Ce and Nd
show restricted ranges in all the samples analysed. The Th
content changes in the range of 0.03–0.09 (cations/4oxy-
gens) and U content from 0.004 to 0.010 (cations/4 oxy-
gens). However, the Th and U amounts concentrate mostly
around 0.05±0.02 and 0.007±0.02 cations/4 oxygens respec-
tively (Fig. 5A, B). The La amount oscillates in the range of
0.18–0.23, Ce in the range of 0.38-0.45 and Nd content con-
centrates around 0.17 cations/4 oxygens (Fig. 5C–E). The
REE curve slightly slopes down towards HREE with Eu nega-
tive anomaly visible in most of the monazites analysed
Table 1: Representative analyses of garnet from the pebbles studied. Oxides in [wt. %], molecular
garnet end-members in [mol %].
Fig. 4. Garnet composition in the mica-schists studied and its P/T
conditions of forming (diagram adapted from Win et al. 2007).
Element/analysis Zar3 core Zar3 rim Mn1 core
Mn1 rim
Tyl2
Tyl2
Tyl14
Tyl14
SiO
2
[wt%]
37.51
37.62
37.85
37.76
39.86
39.10
38.95
39.38
TiO
2
0.08
0.22
0.01
0.00
0.14
0.00
0.00
0.00
Al
2
O
3
20.78
20.85
21.32
21.28
19.02
19.47
19.62
19.46
Cr
2
O
3
0.02
0.00
0.01
0.05
0.00
0.12
0.00
0.19
Fe
2
O
3
0.25
0.00
0.49
0.46
0.00
0.00
0.03
0.00
FeO
28.44
36.20
31.20
30.34
32.43
32.55
27.21
27.84
MnO
4.08
0.32
5.42
6.89
6.63
7.09
10.71
9.72
MgO
0.84
2.40
3.36
2.90
0.99
0.72
2.50
2.50
CaO
8.48
3.17
2.01
2.08
0.93
0.95
0.81
0.91
Total
100.48
100.79
101.68
101.75
100.00
100.00
99.82
100.00
Numbers of cations calculated on the basis of 12 oxygen atoms
Si [apfu]
3.005
3.009
2.993
2.993
3.215
3.168
3.136
3.159
Ti
0.005
0.013
0.001
0.000
0.008
0.000
0.000
0.000
Al
1.962
1.966
1.988
1.988
1.808
1.860
1.862
1.840
Cr
0.001
0.000
0.001
0.003
0.000
0.008
0.000
0.012
Fe
3+
0.015
0.000
0.029
0.027
0.000
0.000
0.000
0.000
Fe
2+
1.906
2.425
2.063
2.010
2.188
2.206
1.834
1.868
Mn
0.276
0.022
0.363
0.462
0.453
0.487
0.730
0.660
Mg
0.101
0.286
0.396
0.342
0.119
0.087
0.300
0.299
Ca
0.728
0.272
0.170
0.177
0.080
0.082
0.070
0.078
Total
7.997
7.990
8.005
8.005
7.872
7.898
7.933
7.915
End-members [mol %]
Almandine
62.9
80.4
68.9
67.2
75.9
76.6
60.6
62.6
Andradite
1.1
0.5
0.7
0.7
0.0
0.0
0.0
0.0
Grossular
23.2
8.7
4.9
5.1
3.0
2.5
2.5
2.2
Pyrope
3.4
9.7
13.2
11.4
4.4
3.1
10.7
10.8
Spessartine
9.3
0.7
12.1
15.4
16.7
17.4
26.1
23.8
Uvarovite
0.1
0.0
0.0
0.1
0.0
0.4
0.0
0.7
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Fig. 5. Frequencies of Rare Earth Elements in monazites from the studied pebbles: A — Th; B — U; C — La; D — Ce; E — Nd;
F — compiled chondrite-normalized REE plots of the monazites analysed (the grey field); the dashed line in the diagram represents REE
plots for spots 1-6 within the grain Tl14-mnz13 shown in Fig. 8 (normalization according to McDonough & Sun 1995).
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(Fig. 5F). Some monazites in sample Tyl2 show enrichment
in Si (up to 1.16 wt. % of SiO
2
) (Table 2). This may be the
effect of cation substitution in monazite structure or of
quartz micro-inclusions present in monazite grains (Pyle et
al. 2001). All of the monazites analysed (Fig. 6) represent
huttonite-cheralite solid solutions (e.g. Spear & Pyle 2002
and references therein). The monazites analysed are generally
compositionally alike. The difference in the ThO
2
content
within all monazite populations studied does not exceed
3.5 wt. % for each sample studied, while the difference in the
UO
2
concentration does not exceed 0.8 wt. %. The difference
in the UO
2
content, considering various spots within a single
monazite grain, is mostly lower than 0.1 wt. %, rarely
reaching about 0.2 wt. %, while variation of ThO
2
within
singular grains may reach up to 2 wt. % (Table 2). Changes
in chemical composition within single grains are irregular or
patchy, but there is no difference between the chondrite nor-
malized REE plots representing various spots in a grain (e.g.,
grain Tyl14-mnz13 in Fig. 5F).
There is no significant difference in the composition and
age of monazites occurring in the matrix or as inclusions
within biotite. The calculated spot ages for the analysed
monazites indicate Variscan Devonian/Carboniferous to Per-
mian time-span. The average ages are very similar for mona-
Table 2: Selected microprobe analyses of monazites from the samples studied. Monazite number (=Mnz No.) refers to monazite grain
analysed; spot number (=spot No.) refers to analytical spot within a grain. Representative analyses within a grain are marked. The data refer
to monazite grains shown in Fig. 8.
Sample label
Tyl2
Tyl14
Mn1
Zar3
Mnz No.
Mnz 2
Mnz 4
Mnz 1
Mnz 13
Mnz 2
Mnz 20
Mnz 3
Mnz 4
Mnz 8
Spot No.
3
4
1
2
1
2
1
4
1
2
4
5
8
15
P
2
O
5
27.79
27.92
27.45
27.52
29.24
27.93
27.42
27.68
28.77
29.18
28.53
29.22
29.11
29.19
SiO
2
0.74
0.75
1.16
0.98
0.22
0.17
0.21
0.38
0.44
0.39
0.50
0.26
0.31
0.27
Al
2
O
3
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.01
0.00
0.00
0.00
0.00
0.01
0.00
La
2
O
3
12.06
12.81
12.01
12.04
12.90
13.41
13.37
13.28
14.27
15.03
13.99
14.51
13.53
14.51
Ce
2
O
3
26.44
27.27
26.23
26.45
26.76
27.76
28.02
26.04
29.20
29.89
27.60
29.68
28.26
29.49
Pr
2
O
3
3.28
3.24
3.16
3.16
3.24
3.35
3.36
3.11
3.19
3.31
3.08
3.28
3.15
3.27
Nd
2
O
3
10.60
10.80
10.34
10.46
11.08
11.31
11.52
11.16
11.72
11.85
11.39
12.16
11.86
11.93
Sm
2
O
3
1.18
1.22
1.22
1.21
1.05
1.03
1.11
1.07
1.95
1.83
2.00
2.26
2.10
1.97
Eu
2
O
3
0.28
0.27
0.26
0.33
0.43
0.32
0.30
0.28
0.11
0.01
0.26
0.24
0.23
Gd
2
O
3
1.53
1.64
1.58
1.62
1.40
1.29
1.33
1.67
1.68
1.68
1.78
1.94
1.83
1.71
Tb
2
O
3
0.08
0.11
0.17
0.17
0.03
0.02
0.00
0.06
0.10
0.06
0.13
0.15
0.12
0.08
Dy
2
O
3
0.95
0.99
1.04
1.04
0.77
0.73
0.68
0.78
0.44
0.50
0.63
0.54
0.65
0.57
Er
2
O
3
0.84
0.85
0.81
0.79
0.78
0.81
0.68
0.82
0.10
0.06
0.09
0.06
0.13
Tm
2
O
3
0.33
0.31
0.36
0.35
0.29
0.37
0.28
0.27
0.04
0.03
0.01
Yb
2
O
3
0.23
0.15
0.22
0.20
0.16
0.17
0.11
0.17
0.02
0.08
0.07
0.06
0.05
0.05
Lu
2
O
3
0.35
0.34
0.39
0.41
0.36
0.44
0.60
0.42
PbO
0.13
0.10
0.16
0.14
0.14
0.12
0.12
0.15
0.11
0.09
0.12
0.06
0.09
0.10
ThO
2
7.11
5.78
8.34
7.55
6.00
5.36
4.92
6.87
4.90
3.91
5.56
2.89
5.50
3.85
UO
2
0.66
0.53
0.66
0.62
0.90
0.75
0.81
1.41
0.87
0.63
1.07
0.45
0.48
0.41
PbO
0.11
0.09
0.14
0.12
0.13
0.11
0.11
0.14
0.10
0.08
0.11
0.05
0.08
0.09
Y
2
O
3
2.61
2.77
2.89
2.91
2.34
2.03
1.69
2.00
1.41
1.28
1.65
1.74
1.97
1.56
CaO
1.14
0.83
1.00
0.98
1.27
1.11
1.01
1.35
0.98
0.74
1.03
0.65
0.99
0.88
Total
98.45
98.74
99.58
99.03
99.50
98.61
97.66
99.12
100.24
100.74
99.26
100.23
100.43
100.28
Oxygen base
16
16
16
16
16
16
16
16
16
16
16
16
16
16
P
3.803
3.805
3.735
3.760
3.913
3.842
3.817
3.800
3.869
3.890
3.865
3.905
3.892
3.899
Si
0.120
0.121
0.187
0.158
0.036
0.028
0.035
0.061
0.070
0.061
0.081
0.042
0.049
0.043
Al
0.000
0.000
0.000
0.000
0.001
0.003
0.001
0.002
0.000
0.000
0.000
0.001
0.001
0.000
La
0.719
0.761
0.712
0.716
0.752
0.803
0.811
0.794
0.836
0.873
0.826
0.845
0.788
0.844
Ce
1.565
1.607
1.544
1.562
1.549
1.651
1.687
1.546
1.698
1.723
1.617
1.715
1.634
1.703
Pr
0.193
0.190
0.185
0.186
0.187
0.198
0.201
0.184
0.184
0.190
0.180
0.188
0.181
0.188
Nd
0.612
0.621
0.593
0.603
0.625
0.656
0.677
0.647
0.665
0.666
0.651
0.686
0.669
0.672
Sm
0.066
0.068
0.068
0.067
0.057
0.058
0.063
0.060
0.107
0.100
0.111
0.123
0.115
0.107
Eu
0.016
0.015
0.014
0.018
0.023
0.018
0.017
0.016
0.000
0.006
0.001
0.014
0.013
0.012
Gd
0.082
0.087
0.084
0.087
0.073
0.070
0.073
0.090
0.089
0.087
0.094
0.101
0.096
0.089
Tb
0.004
0.006
0.009
0.009
0.002
0.001
0.000
0.003
0.005
0.003
0.007
0.008
0.006
0.004
Dy
0.050
0.051
0.054
0.054
0.039
0.038
0.036
0.040
0.022
0.025
0.033
0.027
0.033
0.029
Er
0.043
0.043
0.041
0.040
0.039
0.041
0.035
0.042
0.005
0.003
0.000
0.004
0.003
0.006
Tm
0.017
0.016
0.018
0.018
0.014
0.018
0.014
0.013
0.000
0.002
0.000
0.000
0.002
0.000
Yb
0.011
0.008
0.011
0.010
0.008
0.009
0.006
0.008
0.001
0.004
0.004
0.003
0.002
0.002
Lu
0.017
0.016
0.019
0.020
0.017
0.022
0.030
0.021
0.000
0.000
0.000
0.000
0.000
0.000
Pb
0.006
0.004
0.007
0.006
0.006
0.005
0.005
0.007
0.005
0.004
0.005
0.003
0.004
0.004
Th
0.262
0.212
0.305
0.277
0.216
0.198
0.184
0.253
0.177
0.140
0.202
0.104
0.198
0.138
U
0.024
0.019
0.024
0.022
0.032
0.027
0.030
0.051
0.031
0.022
0.038
0.016
0.017
0.014
Pb
0.005
0.004
0.006
0.005
0.005
0.005
0.005
0.006
0.004
0.004
0.005
0.002
0.003
0.004
Y
0.224
0.237
0.247
0.250
0.197
0.176
0.148
0.173
0.119
0.107
0.141
0.146
0.166
0.131
Ca
0.197
0.143
0.173
0.169
0.215
0.193
0.178
0.235
0.166
0.125
0.177
0.110
0.167
0.149
Total cath.
8.053
8.050
8.054
8.055
8.032
8.084
8.084
8.052
8.053
8.043
8.045
8.048
8.042
8.054
Th
6.252
5.078
7.326
6.636
5.275
4.711
4.325
6.037
4.302
3.434
4.885
2.539
4.835
3.385
U
0.578
0.463
0.580
0.545
0.790
0.657
0.711
1.241
0.766
0.558
0.939
0.396
0.421
0.357
Pb
0.106
0.080
0.130
0.112
0.118
0.099
0.101
0.128
0.092
0.077
0.106
0.045
0.073
0.082
Y
2.054
2.178
2.278
2.291
1.842
1.601
1.334
1.576
1.110
1.009
1.299
1.366
1.553
1.226
Th*
8.125
6.577
9.210
8.403
7.844
6.847
6.639
10.059
6.788
5.248
7.931
3.819
6.198
4.552
Age (Ma)
292
273
317
299
339
325
341
286
303
331
301
266
265
405
265
MICA-SCHIST PEBBLES FROM EOCENE CONGLOMERATES (OUTER CARPATHIANS)
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zites from all the mica-schists studied oscillating around 300
Ma: 303±4.2 Ma (Tyl2) and 313±3.8 Ma (Tyl14) in Tylicz,
314±4.5 Ma in Piwniczna-Mniszek and 320±11.8 Ma in
Zarzecze (Table 2; Figs. 7, 8). The differences in age calcu-
lated for spots within single grains do not exceed 50 Ma still
oscillating around 300 Ma. Age distribution within single
monazite grains is irregular, showing a patchy pattern
(Table 2; Fig. 8).
Discussion and conclusions
The set of pebbles
The exotic pebbles in the Eocene deposits of the southern
part of the Magura Nappe (Tylicz and Krynica zones) have
been recognized in two stratigraphic positions: 1) in the
Mniszek Shale Member (Middle-Upper Eocene) of the
Magura Formation (Tylicz and Zarzecze sections); 2) in the
Piwniczna-Mniszek section belonging to the Piwniczna
Member of the Magura Fm. (Lower-Middle Eocene).
The thick-bedded sandstones and conglomerates of the
Mniszek Shale Member, uppermost part of the Piwniczna
Member of the Magura Formation are located above the
Middle-Upper Eocene variegated shales of Cyclammina am
-
plectens Grzybowski. These are deposits of channel facies
with relatively high contents of the Mesozoic carbonate peb-
bles from 18 % in the Zarzecze section (in the west) to 44 %
at Tylicz (in the east) and similar content pebbles of flysch
sandstones (about 26 %). The content of crystalline rocks
ranges from ca 26 % to 32 % in the Tylicz and Zarzecze sec-
tions respectively. The population of pebbles at Tylicz is rich
in medium grade metamorphic rocks such as fine-grained
gneisses and schists and very poor in igneous rocks, while
a striking feature of the conglomerates at Zarzecze is the
high content of vein quartz. The composition of carbonate
material and microfossil assemblages of the Tylicz and
Zarzecze conglomerates (Middle–Late Eocene) indicates
similarity to both the Jarmuta/Proč and Strihovce exotic peb-
bles (Oszczypko & Olszewska 2010).
The exotic conglomerates of the Piwniczna-Mniszek sec-
tion belonging to the Piwniczna Member of the Magura Fm.
are located beneath the horizon of variegated shales with Cy
-
clammina amplectens Grzybowski. These conglomerates are
rich in vein quartz (37 %), flysch clasts (35 %), crystalline
clasts (25 %) and poor in carbonate clasts (3 %). The exotic
conglomerates of the Piwniczna Sandstone Mb. (Middle/
Lower Eocene) of the Magura Fm. are an equivalent of con-
glomerates of the lower part of the Strihovce Sandstone (see
Nemčok 1990a,b; Mišík et al. 1991). These conglomerates
are rich in granitoids, medium-grade metamorphic gneisses
and schists, phyllites and quartzites, with a relatively small
amount of felsic volcanic rocks and Mesozoic carbonates
(Oszczypko 1975; Mišík et al. 1991; Oszczypko et al. 2006).
Metamorphic rocks found in all sampled conglomerates
are similar to each other and correspond to medium grade
Fig. 6. Substitution diagrams for the monazites analysed.
266
OSZCZYPKO, SALATA
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Fig. 7. Monazite age histograms and Pb vs. Th* (wt. %) monazite isochrone diagrams.
267
MICA-SCHIST PEBBLES FROM EOCENE CONGLOMERATES (OUTER CARPATHIANS)
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metamorphic conditions of epidote-amphibolite or amphibo-
lite facies. Similar results as for garnet composition and
metamorphic conditions of its forming were obtained on the
basis of numerous analyses of detrital garnets found in the
Jarmuta (Maastrichtian-Palaeocene) and Szczawnica (Palaeo-
cene-Lower Eocene) Formations (Salata 2004; Oszczypko
& Salata 2005).
Monazite age remarks
According to Spear & Pyle (2002 and references therein)
a low and restricted range of Th content oscillating around
0.05, U content up to 0.01 and also La, Ce and Nd averaging
around 0.20, 0.43 and 0.17 cations/4 oxygens respectively
Fig. 8. Microphotographs showing representative monazites analysed with distribution of calculated ages. SEM BSE.
are typical for monazites formed in metamorphic conditions.
Additionally, the REE patterns of metamorphic monazites
slope down towards HREE (e.g. Catlos et al. 2002; Spear &
Pyle 2000 and references therein). Therefore, the Variscan
ages of the monazites analysed are interpreted as docu-
menting metamorphic processes in the source area. There is
no evidence of a rejuvenation younger then the Variscan
orogeny reflected in the calculated ages. The irregular age
distribution within single grains may reflect different phases
of metamorphic processes influencing trace element compo-
sition in the monazites analysed. The compositional patchy
pattern could be caused by several processes that include
overgrowth, regrowth, intergrowth, replacement and recrys-
tallization during metamorphic events (e.g. Zhu & O’Nions
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OSZCZYPKO, SALATA
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1999). The currently obtained ages correspond well to earlier
radiometric ages obtained from mica dating and CHIME
dating of monazite in a metamorphic rock pebble from
Tylicz (Poprawa et al. 2004, 2005).
Possible sources
The plutonic rocks in the Tylicz conglomerate represent
volcanic-arc granites and syn-collisional granites of S-type,
which are well known from the Western Carpathians (e.g.,
Petrík et al. 1994; Broska & Uher 2001; Broska & Petrík
2015). Such granites were also described as protoliths for
Carpathian orthogneisses found as pebbles in Palaeocene
flysch in the Dukla Nappe (Bąk & Wolska 2005). According
to Pitcher (1982) and Broska and Uher (2001) S-type granites
are orogenic granites connected with continental collision.
They can be accompanied by regional metamorphic rocks
(Pitcher 1982). The Western Carpathian I- and S-type grani-
toids display monazite ages of ~350 Ma and ~340 Ma (Bros-
ka & Petrík 2015 and references therein). Unfortunately, the
very small (up to 2 cm across maximum) granitic pebbles
found in the studied sections did not contain monazites to
compare the dating. Variscan metamorphism, although docu-
mented in the Tatric (~310 Ma) and Veporic (~340–350 Ma)
metamorphic units, is not widespread in the Western Car-
pathian domains as mainly Alpine recrystallization events
are recorded in the area (e.g., Janák 1994; Dallmeyer et al.
1996; Janák & Plašienka 1999; Janák et al. 2001 and
references therein). The dates established for the Western
Carpathian igneous and metamorphic rocks suit the time-
span established for the dated mica-schist pebbles studied
here. However, there are some facts that exclude Western
Carpathian crystalline massifs from the possible source areas
for the studied conglomerates. They are: i) the total lack of
sedimentary rocks, derived from the PKB and instead the
presence of shallow-water limestone of the Urgonian facies,
typical for the Median Dacides of the Dacia Mega Unit;
ii) the palaeotransport directions measured in the sampled
deposits indicate location of the source massif(s) in the
south-east termination of the Magura Basin, while the small
dimensions of the mica-schist pebbles suggest a rather distal
source in relation to their deposition place in the Magura
Basin and/or their re-deposition. The similar mineral compo-
sition and consistent monazite age distribution and
palaeocurrent directions of deposits suggest provenance of
the mica-schists studied from the same source area. The dif-
ferent garnet composition between schists from Tylicz,
Piwniczna-Mniszek (low- to medium grade) and Zarzecze
(high-grade) may reflect the origin of the pebbles from
various parts of an inhomogeneous metamorphic body of the
source area.
Both crystalline and sedimentary rock pebbles are charac-
terized by good roundness, typical for river channel sand and
marine coastal abrasion. These pebbles could be re-deposited
in coastal embankments or as channel facies of submarine
cones.
The exotic conglomerates are located directly below
(Piwniczna/Mniszek section) and above (Tylicz and Zarzecze
sections) the variegated shales of the Mniszek Sh. Mb, mani-
festing vertical movements of the Magura Basin basement.
These movements were accompanied by seismic shocks,
which triggered gravity-driven debris flows and submarine
slumps moving forward into the deepest parts of the basin
(Einsele 2002).
The exact position of the source area for the investigated
exotic pebbles is speculative. However, the obtained data
suggest recycling and erosion during the Middle Late Eocene
to Oligocene an older accretionary wedge and deposition of
detritus from the SE prolongation of the Marmarosh Massif
located at the south-eastern boundary of the Magura Basin
(Lashkievitsch et al. 1995). The supply of carbonate and si-
liciclastic material from a SE source area (part of the Dacia
Mega Unit) was suggested by Oszczypko and Oszczypko-
Clowes (2009) as well as by Oszczypko et al. (2005, 2015).
The latter solution can be also deduced from the Oligocene?/
Early Miocene (Fig. 9) pre-orogenic palaeogeographic resto-
ration of the Alpine-Carpathian-Panonian realms (Usta-
szewski et al. 2008).
Currently, the eastern termination of the Magura Nappe is
situated in the Eastern Carpathians, along the boundary be-
tween Ukraine and Romania (Fig. 1). In this place the Magura
Nappe (Monastyrets and Pertrova subunits) is a few km
wide, and it is limited to the north by the Median Dacides
and its sedimentary cover and from the south by the Pieniny
Klippen Belt, Neogene volcanic belt and the Miocene deposits
of the Pannonian Basin (Aroldi 2001; Schmid et al. 2008;
Oszczypko et al. 2005, 2015).
The possible supply to the Magura Basin from the Marma-
rosh Massif is indicated by palaeotransport measurements.
There are also the similarities between the Jurassic and Lower
Cretaceous carbonate microfacies of the Marmarosh Massif
and Marmarosh Klippens with the Eocene microfacies exotic
pebbles from the Krynica Zone of the Magura Nappe
and Pieniny Klippen Belt in Poland and Eastern Slovakia
Fig. 9. Reconstruction of the geotectonic situation in the Alps,
Carpathians and Dinarides domains in the Early Miocene (based on
Ustaszewski et al. 2008 and references therein).
269
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(Mochnacka & Węcławik 1967; Oszczypko 1975; Mišík
et al. 1991a, b; Olszewska & Oszczypko 2010).
The Crystalline Mesozoic Zone of the East Carpathians
belongs to Median Dacides (Săndulescu 1984) and is com-
posed of the Bucovinian nappe stack, which is of Cretaceous
age. In the Ukrainian sector the Marmarosh crystalline mas-
sif is an eastern prolongation of the Median Dacide (Ślaczka
et al. 2006). This massif displays a nappe structure and is
overthrust upon the Black Flysch or Rachiv units. The Mar-
marosh Massif is composed of Pre-Cambrian gneisses,
Palaeozoic metamorphic schists, Carboniferous/Permian
coal shales, conglomerates, tuffs, lavas, as well as Mesozoic
limestones and breccias (Kruglov & Cypko 1988).
The set of Variscan metamorphic rocks within Eastern
(Romanian) Carpathian basement includes very low to low-
and medium-grade metamorphic mica-schists, quartz biotite
paragneisses, amphibolites metamorphosed under green-
schist to almandine-amphibolite facies (see Balintoni 2010
in Miclăuş et al. 2010). Variscan ages are the most common
in basement rocks of the Eastern Carpathians and Apuseni
Mountains. The ages are well established on the basis of ra-
diometric K-Ar and Ar-Ar dating of muscovite and biotite
concentrates as well as monazite (e.g. Dallmeyer et al. 1999;
Strutinski et al. 2006; Gröger et al. 2013; Săbău & Negules-
cu 2014 and references therein). The established Variscan
time span of the metamorphic events encloses within
370–251 Ma (see e.g. Strutinski et al. 2006) with a distinct
plateau of ages grouping around 300±20 Ma. It is worth
noting that the area of the East Carpathians is situated out-
side the Alpine metamorphic zone, thus Alpine metamor phic
rejuvenation is not strongly developed there. However, the
rejuvenation overprints Alpine ages in the rocks of the Apuse-
ni Mountains (see e.g. Dallmeyer et al. 1999; Strutinski et al.
2006). The Variscan time-span established for the metamor-
phic micas in the east Carpathians closely agrees with the
currently obtained data for the Magura Nappe mica-schist
pebbles. Moreover, since the monazites dated do not show
Alpine ages it may be supposed that the pebbles studied de-
rive mainly from the East Carpathian domain of the Dacia
Mega Unit rather than from the more southern parts of it.
The idea is supported by the garnet composition indicating
a mainly low grade of metamorphism of the pebbles studied
(Fig. 4).
Acknowledgements: The authors express their thanks to
prof. Monika Kusiak (Institute of Geological Sciences, Polish
Academy of Sciences, Warsaw) and an anonymous reviewer
for their valuable remarks on the manuscript. We are also
grateful to the Editorial Board of Geologica Carpathica for
comments which helped to improve the paper. This paper
was financed by the DS fund of the Jagiellonian University
and by the Polish Ministry of Science and Higher Education
(grant nr 2 P04D 002 28).
References
Amli R. & Griffin W. 1975: Microprobe analysis of REE minerals
using empirical correction factors. Am. Mineral. 60, 599–606.
Aroldi C. 2001: The Pienides in Maramureš. Cluj University Press,
1–156.
Balintoni I. 2010: The Crystalline-Mesozoic Zone of the East Car-
pathians. A review. In: Iancu O. G. & Kovacs M. (Eds.): RO1
— Ore deposits and other classic localities in the Eastern Car-
pathians: From metamorphics to volcanics. Field trip guide.
20
th
Meeting of the International Mineralogical Association
Budapest. Acta Mineral. Petrogr., Field Guide Series 19,
1–55.
Bąk K. & Wolska A. 2005: Exotic orthogneiss pebbles from
Palaeocene flysch of the Dukla Nappe (Outer Eastern Car-
pathians, Poland). Geol. Carpath. 56, 3, 205–221.
Birkenmajer K. 1977: Jurassic and Cretaceous lithostratigraphic
units of the Pieniny Klippen Belt, Carpathians. Stud. Geol.
Polon. 45, 1–159.
Birkenmajer K. & Oszczypko N. 1989: Cretaceous and Palaeogene
lithostratigraphic units of the Magura Nappe, Krynica Subunit,
Carpathians. Ann. Soc. Geol. Pol. 59, 145–181.
Birkenmajer K. & Wieser T., 1990: Exotic rock fragments from Up-
per Cretaceous deposits near Jaworki, Pieniny Klippen Belt,
Carpathians, Poland. Stud. Geol. Polon. 97, 7–67 (in Polish).
Broska I. & Uher P. 2001: Whole-rock chemistry and genetic ty-
pology of the West-Carpathian Variscan granites. Geol. Car-
path. 52, 2, 79–90.
Broska I. & Petrík I. 2015: Variscan thrusting in I- and S-type gra -
nitic rocks of the Tribeč Mountains, Western Carpathians (Slo-
vakia): evidence from mineral compositions and monazite
dating. Geol. Carpath. 66, 6, 455–471.
Catlos E.J. Gilley L.D. & Harrison T.M. 2002: Interpretation of
monazite ages obtained via in situ analysis. Chem. Geol. 188,
193–215.
Dallmeyer R.D., Pan D.I., Neubauer F. & Erdmer P. 1999: Tectono-
thermal evolution of the Apuseni Mountains, Romania: resolu-
tion of Variscan versus Alpine events with 40Ar/39Ar ages.
J. Geol. 107, 329–352.
Einsele G. 2002. Sedimentary basins. Second edition. Springer,
1–792.
Gröger H.G, Matthias T., Fügenshuh B. & Schmid S.M. 2013:
Thermal history of the Maramures area (Northern Romania)
constrained by zircon fission track analysis:Cretaceous meta-
morphism and Late Cretaceous toPaleocene exhumation.
Geol. Carpath. 64, 5, 383–398.
Janák M. 1994: Variscan uplift of the crystalline basement, Tatra
Mts., central Western Carpathians: Evidence from
40
Ar/
39
Ar
laser probe dating of biotite and P-T-t paths. Geol. Carpath.
45, 293–300.
Janák M. & Plašienka D. 1999: Deciphering Alpine and Pre-Alpine
metamorphism in the Western Carpathians: an overview. Geol.
Carpath., Spec. Iss., 50, 105–107.
Janák M., Plašienka D., Frey M., Cosca M., Schmidt Th., Lupták B.
& Méres Š. 2001: Cretaceous evolution of a metamorphic core
complex, the Veporic unit, Western Carpathians (Slovakia):
P-T conditions and in situ
40
Ar/
39
Ar UV laser probe dating of
metapelites. J. Metamorph. Geol. 19, 197–216.
Jaksa-Bykowski C. 1925: Contribution to petrographic characteris -
tic of the Magura flysch in the area of Krościenko on the
Dunajec river. Archive of the Mineralogical Lab of the Scien
-
tific Warsaw Society 1, 123–130 (in Polish).
Konečný P., Siman P., Holický I., Janák M. & Kollárová V. 2004:
Method of monazite dating by means of the microprobe.
Miner. Slov. 36, 225–235.
Kruglov S.S. & Cypko A.K. 1988: Tectonics of Ukraine. Nedra
Publishers, Moscow, 1–253 (in Russian).
Książkiewicz M. (Ed.) 1962: Geological Atlas of Poland. Strati-
graphical-facies issues. Cretaceous and Lower Tertiary in Polish
Outer Carpathians. Geological Institute, Warsaw (in Polish).
270
OSZCZYPKO, SALATA
and KONEČNÝ
GEOLOGICA CARPATHICA
, 2016, 67, 3, 257–271
Lashkievitsch Z.M., Medvedev A.P. & Krupskiy Y.Z. 1995: Tec-
tonomagnetic evolution of Carpathians (in Russian). Naukova
Dumka, Kiev, 1–113.
Miclăuş C., Baciu D.S. & Iancu O.G. (Eds) 2010: The crystalline-
mesozoic zone of the East Carpathians. A review. In: Excur-
sion guide of the International Symposium: Geology of
Natural Systems — Geo Iaşi 2010, September 1–4, 2010, Iaşi,
Romania, 14–21.
Mišík M., Sýkora M. & Jablonský J. 1991a: The Strihovce Con-
glomerate and South-Magura Cordillera. Zapadné Karpaty,
ser. geol. 14, 7–72 (in Slovak).
Mišík M., Sýkora M., Mock R. & Jablonský J. 1991b: Paleogene
Proč Conglomerates of the Klippen belt in the Western Car-
pathians, material from Neopieninic Exotic Ridge. Acta Geol.
Geogr. Univ. Carol., Geol. 46, 1–101.
Mochnacka K. & Węcławik S. 1967: Paleogene exotic rocks in the
Paleogene of the Magura Nappe near Tylicz. Sprawozdania
z Posiedzeń Komisji PAN Kraków XI/2, 805–808 (in Polish).
Montel J.M., Foret S., Veschambre M., Nicollet Ch. & Provost A.
1996: Electron microprobe dating of monazite. Chem. Geol.
131, 37–53.
Nemčok J. 1990a: Geological Map of Pieniny, Ľubovnianska Vr -
chovina Highland and Čergov Mts. Geologický Ústav
D. Štúra. Bratislava.
Nemčok J. 1990b: Explanations to the Geological Map of Pieniny,
Ľubovnianska Vrchovina Highland and Čergov Mts. Geol.
Ústav D. Štúra. Bratislava, 1–131.
Olszewska B. & Oszczypko N. 2010: Geological position, sedimen-
tary record and composition of the Tylicz Conglomerate (Late
Eocene-Oligocene): stratigraphical and paleogeographical im-
plications (Magura Nappe, Polish Outer Carpathians). Geol.
Carpath. 61, 1, 39–54.
Oszczypko N. 1975: Exotic rocks in the Palaeogene of the Magura
nappe between Dunajec and Poprad rivers, Carpathians,
Poland. Ann. Soc. Geol. Pol. 45, 3–4, 403–431 (in Polish).
Oszczypko N. 1992: Late Cretaceous through Paleogene evolution
of Magura Basin. Geol. Carpath. 43, 6, 333–338.
Oszczypko N. & Oszczypko-Clowes M. 2006.Evolution of the
Magura Basin. In: Oszczypko N., Uchman A. & Malata E.
(Eds.): Paleotectonic evolution of the Outer Carpathian and
PieninyKlippen Basins. Inst. Nauk Geol. Uniw. Jagiell.,
Kraków, 132–164. (in Polish).
Oszczypko N. & Oszczypko-Clowes M. 2009: Stages in Magura
Basin: a case study of the Polish sector (Western Carpathians).
Geodyn. Acta 22, 1–3, 83–100.
Oszczypko N. & Oszczypko-Clowes M. 2010: Lithostratigraphy
and biostratigraphy of the Palaeogene to Lower Miocene de-
posits of the Beskid Sadecki Range (Magura Nappe, Western
Flysch Carpathians, Poland). Acta Geol. Pol. 60, 3, 317–348.
Oszczypko N. & Salata D. 2005: Provenance analyses of the Late
Cretaceous-Palaeocene deposits of the Magura Basin (Polish
Western Carpathians) — evidence from a study of the heavy
minerals. Acta Geol. Pol. 55, 237–267.
Oszczypko N. & Zuber A. 2002: Geological and isotopic evidence
of diagenetic waters in the Polish Flysch Carpathians. Geol.
Carpath. 53, 4, 257–268.
Oszczypko N., Dudziak J. & Malata E. 1990: Stratigraphy of the
Cretaceous through Palaeogene deposits of the Magura Nappe
in the Beskid Sądecki Range, Polish Outer Carpathians. Stud.
Geol. Pol. 47, 109–181 (in Polish).
Oszczypko N., Oszczypko-Clowes M., Golonka J. & Krobicki M.
2005: Position of the Marmarosh Flysch (Eastern Carpathians)
and its relation to the Magura Nappe (Western Carpathians).
Acta Geol. Hung. 48, 3, 259–282.
Oszczypko N., Oszczypko-Clowes M., Golonka J. & Marko F.
2005: Oligocene–Lower Miocene sequences of the Pieniny
Klippen Belt and adjacent Magura Nappe between Jarabina
and the Poprad River (East Slovakia and South Poland) —
their tectonic position and paleogeographic implications. Geol.
Quarterly 49, 4, 379–402.
Oszczypko N., Oszczypko-Clowes M. & Salata D. 2006: Exotic
rocks of the Krynica Zone (MaguraNappe) an their paleogeo-
graphic significance. Geologia 32, 1, 21–45. (in Polish).
Oszczypko N., Ślączka A., Oszczypko-Clowes A. & Olszewska B.
2015: Where was the Magura Ocean. Acta Geolo. Polon. 65,
3, 319–344.
Oszczypko-Clowes M. 2001: The nannofossils biostratigraphy of
the youngest deposits of the Magura Nappe (East the Skawa
river, Polish flysch Carpathians) and their palaeenvironmental
conditions. Ann. Soc. Geol. Pol. 71, 139–188.
Oszczypko-Clowes M., Soták J., Oszczypko N. & Šurka J. 2013:
Biostratigraphic revision of the Magura Unit in the Horná Ora-
va region (Slovakia): constraints for Oligomiocene formations.
In: Broska I. & Tomašových A. (Eds.): Geological evolution
of the Western Carpathians: new ideas in the field of inter-re-
gional correlations. GEEWEC 2013, Smolenice. Geological
Institute SAS, Bratislava, 66–67.
Petrík I., Broska I. & Uher P. 1994: Evolution of the West Car-
pathian granite magmatism: source rock, geotectonic setting
and relation to the Variscan structure. Geol. Carpath. 45,
283–291.
Pitcher W.S. 1982: Granite type and tectonic environment. In: Hsu
K.J. (Ed.): Mountain building processes. Academic Press,
London, 19–40.
Plašienka D. 2000: Paleotectonic controls and tentative palinspastic
restoration of the Carpathian realm during the Mesozoic. Slo
-
vak Geol. Mag. 6, 2–3, 200–204.
Poprawa P., Malata T., Pécskay Z., Banaś M., Skulich J., Paszows-
ki M. & Kusiak M. 2004: Geochronology of crystalline base-
ment of the Western Outer Carpathians sediment source areas
- preliminary data. Miner. Soc. Pol. — Special Papers, 24,
329–332.
Poprawa P., Kusiak M.A., Malata T., Paszkowski M., Pécskay Z.
& Skulich J. 2005: Th–U–Pb chemical dating of monazite and
K/Ar dating of mica combined: preliminary study of “exotic”
crystalline clasts from the Western Outer Carpathian flysch
(Poland). Miner. Soc. Pol. — Special Papers, 25, 345–351.
Pyle J.M., Spear S.F., Rudnick R.L. & McDonough W.F. 2001:
Monazite-xenotime-garnet equilibrium in metapelites and new
monazite-garnet thermometer. J. Petrol. 42, 11, 2083–2107.
Salata D. 2004: Detrital garnets from the Upper Cretaceous-
Palaeocene sandstones of the Polish part of the Magura nappe
and the Pieniny Klippen Belt: chemical constraints. Ann. Soc.
Geol. Pol. 74, 351–364.
Săbău G. & Negulescu E. 2014: Inheritance, Variscan tectonometa-
morphic evolution and Permian to Mesozoic rejuvenations in
the metamorphic basement complexes of the Romanian Car-
pathians revealed by monazite microprobe geochronology
EGU General Assembly 2014, Geophys. Res. Abs. 16,
EGU2014-4324-2.
Săndulescu M. 1984: Geotectonics of Romania. Ed. Tehnica,
Bucharest, 1–450 (in Romanian).
Ślączka A., Kruglov S., Golonka J., Oszczypko N. & Popadyuk I.
2006: Geology and hydrocarbon resources of the Outer Car-
pathians, Poland, Slovakia, and Ukraine: General Geology. In:
Golonka J. & Picha F.J. (Eds.): The Carpathians and their fore-
land: Geology and hydrocarbon resources. AAPG Memoir 84,
221–258.
Schmid S.M., Bernoulli D., Fügenschuh B., Matenco L., Schuster
R., Schefer S., Tischler M.& Ustaszewski K. 2008: The
Alpine- Carpathian-Dinaridic orogenic system: correlation and
evolution of tectonic units. Swiss J. Geosci. 101, 139–183.
271
MICA-SCHIST PEBBLES FROM EOCENE CONGLOMERATES (OUTER CARPATHIANS)
GEOLOGICA CARPATHICA
, 2016, 67, 3, 257–271
Spear F.S. & Pyle J.M. 2002: Apatite, monazite, and xenotine in
metamorphic rocks. In: Kohn M.L., Rakovan J. & Hughes J.M.
(Eds.): Phosphates - geochemical, geobiological, and materials
importance. Rev. Mineral. Geochem. 48, 293–336.
Strutinski C., Puşte A. & Stan R. 2006: The metamorphic basement
of Romanian Carpathians: a discussion of K-Ar and 40Ar/
39Ar ages. Studia Universitatis Babeş-Bolyai, Geologia 51,
1–2, 15–21.
Unrug R. 1968: Kordyliera śląska jako obszar źródłowy materiału
klastycznego piaskowców fliszowych Beskidu Śląskiego i
Beskidu Wysokiego (Polskie Karpaty Zachodnie). Ann. Soc.
Geol. Pol. 38, 81-164. (In Polish with English Sumary).
Ustaszewski K., Schmid S., Fügenshuh B., Tischler M., Kissling E.
& Spakman W. 2008: A map-view restoration of the Alpine-
Carpathian-Dinaridic system for the Early Miocene. Swiss J.
Geosci. 101, Supp. Issue, 273–294.
Węcławik S. 1969: The geological structure of the MaguraNappe be-
tween Uście Gorlickie and Tylicz, Carpathians (Lower Beskid).
Prace Geol., PAN, Oddz. w Krakowie 59, 1–96 (in Polish).
Wieser T. 1970: Exotic rocks from the deposits of the Magura
nappe. Bulletin IG 235, 123–161.
Win K.S., Takeuchi M. & Tokiwa T. 2007: Changes in detrital gar-
net assemblages related to transpressive uplifting associated
with strike-slip faulting: an example from the Cretaceous Sys-
tem in Kii Peninsula, southwest Japan. Sediment. Geol. 201,
412–431.
Zhu X.K. & O’Nions R.K. 1999: Zonation of monazite in meta-
morphic rocks and its implications for high temperature ther-
mochronology: a case study from the Lewisian terrain. Earth
Planet. Sci. Lett. 171, 209–220.
Żytko K., Gucik S., Ryłko W., Oszczypko N., Zając R., Garlicka I.,
Nemčok J., Eliáš M., Menčik E. & Stránik Z. 1989: Map of the
tectonic elements of the Western Outer Carpathians and their
foreland. In: Poprawa D. & Nemčok J. (Eds): Geological atlas
of the Western Outer Carpathians and their foreland. PIG
Warszawa, GUDS Bratislava, UUG Praha.