GeolCarp_Vol67_No3_257

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

, DOROTA SALATA

and PATRIK KONEČNÝ

Jagiellonian University, Institute of Geological Sciences, Oleandry 2a, 30-063 Kraków, Poland;

nestor.oszczypko@uj.edu.pl; dorota.salata@uj.edu.pl

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

Pb — cerusite, Th — ThO

, U — UO

, Ca — wollastonite,

Fe — forsterite, S — barite, As — GaAs and REE plus Y

were calibrated on phosphates REEPO

and YPO

, 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

, and Th at

ThMα. An overlap of PbMα with YLγ

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

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

— TiO

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

Tyl14

SiO

[wt%]

37.51

37.62

37.85

37.76

39.86

39.10

38.95

39.38

TiO

0.08

0.22

0.01

0.00

0.14

0.00

20.78

20.85

21.32

21.28

19.02

19.47

19.62

19.46

0.02

0.00

0.01

0.05

0.00

0.12

0.00

0.19

0.25

0.00

0.49

0.46

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

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

99.82

100.00

Numbers of cations calculated on the basis of 12 oxygen atoms
Si [apfu]

3.005

3.009

2.993

3.215

3.168

3.136

3.159

0.005

0.013

0.001

0.000

0.008

0.000

1.962

1.966

1.988

1.808

1.860

1.862

1.840

0.001

0.000

0.001

0.003

0.000

0.008

0.000

0.012

0.015

0.000

0.029

0.027

0.000

1.906

2.425

2.063

2.010

2.188

2.206

1.834

1.868

0.276

0.022

0.363

0.462

0.453

0.487

0.730

0.660

0.101

0.286

0.396

0.342

0.119

0.087

0.300

0.299

0.728

0.272

0.170

0.177

0.080

0.082

0.070

0.078

Total

7.997

7.990

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

0.0

Grossular

23.2

8.7

4.9

5.1

3.0

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

0.1

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

) (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

content

within all monazite populations studied does not exceed

3.5 wt. % for each sample studied, while the difference in the

concentration does not exceed 0.8 wt. %. The difference

in the UO

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

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.

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

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

0.00

0.01

0.00

0.01

0.00

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

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

3.28

3.24

3.16

3.24

3.35

3.36

3.11

3.19

3.31

3.08

3.28

3.15

3.27

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

1.18

1.22

1.21

1.05

1.03

1.11

1.07

1.95

1.83

2.00

2.26

2.10

1.97

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

1.53

1.64

1.58

1.62

1.40

1.29

1.33

1.67

1.68

1.78

1.94

1.83

1.71

0.08

0.11

0.17

0.03

0.02

0.00

0.06

0.10

0.06

0.13

0.15

0.12

0.08

0.95

0.99

1.04

0.77

0.73

0.68

0.78

0.44

0.50

0.63

0.54

0.65

0.57

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

0.33

0.31

0.36

0.35

0.29

0.37

0.28

0.27

0.04

0.03

0.01

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

0.35

0.34

0.39

0.41

0.36

0.44

0.60

0.42

PbO

0.13

0.10

0.16

0.14

0.12

0.15

0.11

0.09

0.12

0.06

0.09

0.10

ThO

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

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

0.14

0.10

0.08

0.11

0.05

0.08

0.09

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

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

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

0.000

0.001

0.003

0.001

0.002

0.000

0.001

0.000

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

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

0.193

0.190

0.185

0.186

0.187

0.198

0.201

0.184

0.190

0.180

0.188

0.181

0.188

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

0.066

0.068

0.067

0.057

0.058

0.063

0.060

0.107

0.100

0.111

0.123

0.115

0.107

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

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

0.004

0.006

0.009

0.002

0.001

0.000

0.003

0.005

0.003

0.007

0.008

0.006

0.004

0.050

0.051

0.054

0.039

0.038

0.036

0.040

0.022

0.025

0.033

0.027

0.033

0.029

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

0.017

0.016

0.018

0.014

0.018

0.014

0.013

0.000

0.002

0.000

0.002

0.000

0.011

0.008

0.011

0.010

0.008

0.009

0.006

0.008

0.001

0.004

0.003

0.002

0.017

0.016

0.019

0.020

0.017

0.022

0.030

0.021

0.000

0.006

0.004

0.007

0.006

0.005

0.007

0.005

0.004

0.005

0.003

0.004

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

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

0.005

0.004

0.006

0.005

0.006

0.004

0.005

0.002

0.003

0.004

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

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

8.052

8.053

8.043

8.045

8.048

8.042

8.054

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

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

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

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

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MICA-SCHIST PEBBLES FROM EOCENE CONGLOMERATES (OUTER CARPATHIANS)

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, 2016, 67, 3, 257–271

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.



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Fig. 7. Monazite age histograms and Pb vs. Th* (wt. %) monazite isochrone diagrams.

267

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, 2016, 67, 3, 257–271

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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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).

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, 2016, 67, 3, 257–271

(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).

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