www.geologicacarpathica.sk
GEOLOGICA CARPATHICA, FEBRUARY 2010, 61, 1, 39—54 doi: 10.2478/v10096-009-0043-y
Introduction
The Outer Carpathian sedimentary basin complex was sup-
plied with clastics that were derived from external as well as
internal source areas, with the latter being referred to as “cor-
dilleras” (Książkiewicz 1962). Our understanding of the geo-
logical structures controlling the Carpathian source areas is
based on the investigations of sedimentary blocks and “exot-
ic” pebbles that were transported into basinal areas by subma-
rine gravity flows (see Książkiewicz 1962). In the Outer
Carpathian sedimentary basin system the most important in-
ternal source area was the “Silesian Cordillera” that correspond-
ed to the continental Silesian, Andrychów and Marmarosh
Ridges (Książkiewicz 1965; Unrug 1968; Oszczypko 1992,
2006; Golonka et al. 2000; Oszczypko et al. 2005a; Picha et
al. 2006). According to Unrug (1968), the Silesian Ridge “par-
alleled the long axis of the flysch trough” and separated the
northern Silesian Basin from the southern Magura Basin. Iso-
topic ages of “exotic” pebbles shed from the Silesian Ridge
into the Silesian, Dukla and Magura (Rača Subunit) Basins
document a Variscan age of plutonic and metamorphic rocks
(Poprawa et al. 2004). During the Campanian, inversion-relat-
ed uplift of the Silesian Ridge affected the northern part of the
Magura Basin where it was accompanied by the onset of flysch
deposition. By contrast, along the southern margin of the
Magura Basin the onset of flysch deposition occurred at the
Maastrichtian-Paleocene transition as manifested by the con-
glomerates and olistoliths of the Jarmuta and Proč Formations
(Birkenmajer & Oszczypko 1989; Mišík et al. 1991a). The
source areas for these clastics were uplifted exotic blocks, in-
cluding internal elements of the Pieniny Klippen Belt (PKB)
(Książkiewicz 1977; Oszczypko et al. 2005b). This is attribut-
ed to the collision of the Inner Western Carpathian (ALCA-
PA) Block with the Czorsztyn-Oravicum Ridge (Plašienka
2003) and/or the Andrusov Ridge (Birkenmajer 1986, 1988).
During the Early Eocene, a deep-water submarine fan started
to develop in the southern part of the Magura Basin, as evi-
denced by the occurrence of channel-lobe turbidites supplied
from SE sources. The Eocene deposits of the Krynica Zone of
the Magura Basin contain fragments of crystalline rocks, de-
rived from a continental type of crust, and infrequent clasts of
Mesozoic deep and shallow-water limestones. Mišík et al.
(1991b) suggested that this material was derived from “the
basement of the Magura Basin”, but differs from that of the
Czorsztyn-Oravicum Ridge, that was exhumed during the Ear-
ly/Middle Eocene. Alternatively, this clastic material may
have been derived from an Inner Carpathian type source area,
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
the geological position, sedimentary record and structure of the
composition of the Tylicz Conglomerate (Upper Eocene—Oli-
gocene). The special emphasis was given on provenance analy-
ses of sedimentary clast and pebbles and their age and
paleogeographical significance.
The geological position, sedimentary record and composition
of the Tylicz Conglomerate (Late Eocene—Oligocene):
stratigraphical and paleogeographical implications
(Magura Nappe, Polish Outer Carpathians)
BARBARA OLSZEWSKA
1
and NESTOR OSZCZYPKO
2
1
Polish Geological Institute, Carpathian Branch, Skrzatów 1, 31-560 Kraków, Poland; barbara.olszewska@pgi.gov.pl
2
Jagiellonian University, Institute of Geological Sciences, Oleandry 2a, 30-063 Kraków, Poland; nestor.oszczypko@uj.edu.pl
(Manuscript received April 14, 2009; accepted in revised form June 25, 2009)
Abstract: During the Late Cretaceous to Paleogene the Magura Basin was supplied with clastic material from, non-
existing today, source areas situated on the northern and southern margins of the basin. The northern source area is
traditionally connected with Silesian Ridge, whereas the position of the southern one is still under discussion. The
Upper Eocene—Oligocene pebbly mudstones of the Tylicz/Krynica facies zone contain exotic material derived from the
south-Magura source area. The studied pebbles and clasts contain fragments of crystalline rocks, derived from a conti-
nental type of crust, and frequent clasts of Mesozoic to Paleogene deep and shallow-water limestones. Volcanites,
rarely granitoides as well as schists, gneisses, quartzites and cataclasites were found in the group of crystalline exotic
pebbles. The isotopic ages of “exotic” pebbles from the Tylicz section document a Variscan age of plutonic and meta-
morphic rocks. The composition of the Tylicz exotic conglomerates occupied the transitional position between the
Jarmuta/Proč (Maastrichtian—Lower Eocene) and Strihovce (Eocene) exotic pebbles. The provenance of these rocks
could be connected with Eocene exhumation of the SE sector of the Magura Basin basement. Another possibility can be
explain by supply of siliciclastic material from a SE source area (Dacia and Tisza Mega-Units) and carbonate material
from a S source area (ALCAPA Mega-Unit: Central Carpathian Block and Pieniny Klippen Belt).
Key words: Magura Basin, stratigraphy and paleogeography, source areas, exotic rocks.
40
OLSZEWSKA and OSZCZYPKO
Previous works
In the southern part of the Magura Nappe (Fig. 1) the “exotic”
conglomerates have been known from many years. They be-
long to coarse-grained deposits of the Szczawnica, Zarzecze
and Magura Formations (Jaksa-Bykowski 1925; Mochnacka
& Węcławik 1967; Wieser 1970; Oszczypko 1975; Oszczypko
et al. 2006). The first detailed description of exotic clasts were
given by Mochnacka & Węcławik (1967), who studied both
crystalline as well as sedimentary pebbles from the Hiero-
glyphic Beds at Tylicz.
A few years later Oszczypko (1975) in the Eocene deposits
of the Beskid Sądecki Range (Krynica Zone) found granitoids,
gneisses, phyllites and quartzites, with a relatively small
amount of basic volcanic rocks and Mesozoic carbonates. In
Eastern Slovakia the Strihovce Sandstone is an equivalent of
the Piwniczna Sandstone Member of the Magura Formation in
Poland. The “exotic” pebbles from these beds have been stud-
ied by Mišík et al. (1991a).
The carbonates are represented by deep-water Jurassic-
Lower Cretaceous sediments as well as fragments of shallow-
water limestones of Triassic (Anisian), Kimmeridgian—Upper
Tithonian, Lower Cretaceous (Urgonian), Upper Cretaceous,
Lower and Upper Paleocene, and Lower Lutetian (Mišík et al.
1991a).
These authors also studied conglomerates of the upper part
of the Strihovce Sandstone which could be regarded as an
equivalent of the Poprad Sandstone Member of the Magura
Formation in Poland (see Oszczypko et al. 2005b). They stud-
ied the Eliasovka, Maly Lipnik 1, Maly Lipnik 2 and Starina
sections located in the ubovnianska Vrchovina. These con-
glomerates are dominated by clastic rocks and milky quartz,
other components occur as an admixture in different amounts:
carbonates 2.4—14.7 %, volcanites 3.4—14.7 %.
The characteristic microfacies of these locations are (Mi-
šík et al. 1991a): the Paleozoic biohermal limestones, Mid-
dle Triassic dolomites, lower-middle Lias, upper Lias and
Dogger, shallow-water Kimmeridgian—Lower Tithonian, pe-
lagic Kimmeridgian—Upper Tithonian, Berriasian—Valangin-
ian, Urgonian limestones (Barremian—Aptian), Upper
Aptian—Lower Albian, Albian—Cenomanian, Senonian deep
Globotruncana, and shallow-water Pseudosiderolites and
Orbitoides limestones, Maastrichtian Omphalocyclus lime-
stones, Paleocene biohermal limestones, and Lower Lutetian
Alveolina-Discocyclina limestones. The Eocene material of
the Krynica Zone is composed of fragments of crystalline
rocks, which are derived from a continental type of crust,
and infrequent clasts of Mesozoic deep and shallow-water
limestones as well as Paleocene/Lower Eocene reef lime-
stones (?Myjava Succession). This suggests a provenance of
clastic material type from the Inner Carpathian source area
located on the SE margin of the basin.
According to Mišík et al. (1991a,b) these exotic rocks of
Eocene deposits from the Krynica Zone differ substantially
from those of the Paleocene/Lower Eocene (Jarmuta and
Proč Formations), dominated by the PKB carbonate clasts
and volcanic clasts derived from the exotic Andrusov Ridge.
According to Mišík et al. (1991b) and Ma ašovský (2002)
the mean rock composition of these conglomerates is as fol-
lows: 76.13 % carbonates, 4.53 % sandstones, 3.18 %
quartzites, 0.6 % metamorphic rocks, 0.25 % milky quartz
and 9.15 % volcanites. According to Mišík et al. (1991b)
Fig. 1. Tectonic sketch of the Outer Western Carpathians (based on Żytko et al. 1989; simplified). Tectonic windows: 1 – Mszana Dolna,
2 – Szczawa, 3 – Klęczany-Pisarzowa, 4 – Grybów, 5 – Ropa, 6 – Uście Gorlickie, 7 – Świątkowa, 8 – Smilno.
41
GEOLOGY, SEDIMENTARY RECORD AND COMPOSITION OF TYLICZ CONGLOMERATE (CARPATHIANS)
these conglomerates are dominated by shallow-water Trias-
sic Alpine limestones (with the exception of Wetterstein
Limestones), pelagic facies of the Carnic-Norian, Czorsztyn
(Dogger) type red limestones, microonkolite limestones with
Saccocoma and Globochaete, shallow-marine Upper Titho-
nian and Berriasian, ?Urgonian sometimes with spineless,
pelagic Albian, and shallow-water Cenomanian, Campanian
and Maastrichtian, biohermal limestones of Paleogene and
not frequent Lower Eocene limestones with Nummulites.
Geological setting
Lithostratigraphy: The studied area is situated in the south-
eastern part of the Magura Nappe, at the boundary of the
Bystrica and Krynica facies zones (Fig. 1). East of the
Muszynka river, between the Krynica and Bystrica Zones
Węcławik (1969) distinguished the transitional Tylicz Zone
(Fig. 2). This author’s investigations in the southern part of
the Low Beskid Range documented profiles, “in the lower
Fig. 2. Geological map of the Tylicz area (based on Oszczypko & Oszczypko-Clowes, in print, supplemented).
42
OLSZEWSKA and OSZCZYPKO
part of which the development of sediments is typical for the
Sącz (Bystrica) Zone, whereas in the upper part it is charac-
teristic of the Krynica Zone”. The Paleogene sequence of the
Tylicz Zone was distinguished as follows: the lower part –
Variegated Shales with Glomospira (Paleocene?—Lower
Eocene), Beloveža Beds (Lower Eocene), Łącko Beds (Lower
Eocene—Middle Eocene); the upper part – Red Shales with
Reticulophragmium (Cyclammina) amplectens (Middle
Eocene), Hieroglyphic Beds with intercalations of polymic-
tic conglomerates (Middle Eocene—Upper Eocene) and
Magura Beds (Upper Eocene). The lower part of the Tylicz
Zone is strongly deformed with presence of overturned folds,
whereas the upper part of sequence displays strata, which
gently dip southwards. This tectonic disconformity was ex-
plained by Węcławik (1969) as a result of the Late Eocene
Illyrian phase, which affected the East Slovak sector of the
Magura Nappe (Leško & Samuel 1968).
This concept was questioned by Oszczypko (1979) who
suggested that the Tylicz facies zone represents the tectonic
superposition of the Bystrica and Krynica Subunits of the
Magura Nappe. According to him the boundary between these
subunits runs along the contact of the red shales with Reticu-
lophragmium amplectens (Middle—?Upper Eocene) and the
Hieroglyphic Beds (sensu Węcławik), which was regarded by
Oszczypko (1979) as an equivalent of Zarzecze Beds (Lower—
Middle Eocene) of the Krynica Subunit. This was supported
by findings of scarce Lower Eocene calcareous nannoplakton
in these beds. This opinion was accepted by Birkenmajer &
Oszczypko (1989) in the formal stratigraphy of the Krynica
Subunit, as well as the Bystrica Zone (Oszczypko 1991).
During the last years litho- and biostratigrapy of the Beskid
Sądecki (Bystrica, Tylicz and Krynica Zones) have been stud-
ied (Oszczypko et al. 1999, 2005b; Oszczypko-Clowes 2001;
Oszczypko & Zuchiewicz 2007 and Oszczypko & Oszczypko-
Clowes, in print). These studies documented that the youngest
deposits of the Magura Nappe in this facies zone belong to the
Poprad Sandstone Member of the Magura Formation (Oli-
gocene). Aditionally in several sections the flysch Lower
Miocene (NN1—NN2) has been found (Oszczypko et al. 1999,
2005b). The Oligocene age of the Magura Sandstone in the
Orava region was documented by Soták (2006).
According to present-day formal lithostratigraphy the depos-
its of the Tylicz Zone (Fig. 2) belong to following formations:
the Łabowa, Beloveža, Żeleźnikowa and Magura Formations.
The Łabowa Formation (Lower Eocene), up to 100 m
thick, is represented by red shales, in the lower part and thin-
bedded flysch, with intercalations of red shales in the upper
part of the formation. This formation is known only from the
Mochnaczka area (see also Węcławik 1969).
The Beloveža Formation (Lower to Middle Eocene), up
to 250 m thick is composed of a thin-bedded flysch with pre-
dominance of clayey deposits.
The Żeleźnikowa Formation (Middle Eocene), up to
300 m thick, formerly known as the Lower Łącko Beds is
represented by a complex deposits where turbiditic Łącko
marls are set among thin-bedded flysch of the Beloveža type
of lithofacies.
The Magura Formation has been subdivided into the
Maszkowice, Mniszek and Poprad Members.
The Maszkowice Sandstone Member is represented by
60—120 cm, fine- to very coarse-grained, poorly sorted, musco-
vitic sandstones bearing calcareous-muddy cement (Fig. 2,
Fig. 3A,B). These sandstones display Bouma’s Tabc intervals.
The sandstones contain numerous clasts of mudstones, up to
15 cm in diameter, and pass upwards into strongly bioturbated
mudstones, rich in mica flakes and coalified plant debris. The
sandstones are intercalated by soft, dark grey marlstones (5 do
20 cm thick) or sandy/muddy couplets, up to 1 m thick. Thick
to very thick-bedded (50—200 cm), clast-rich granule conglom-
erates, and amalgamated sandstones also occur. The Maszkow-
ice Sandstone Member contains rare packets, up to a few meters
thick, of the Łącko-type marls (Figs. 2, 3B). Thick to very
thick-bedded (50—200 cm), clast-rich granule conglomerates,
and amalgamated sandstones also occur. These strata display
coarsening and thickening upwards sequences, typical of the
channel-lobe turbidite system. In the Tylicz area, the thickness
of the Maszkowice Member reaches 700—800 m. This member
belongs the Middle Eocene calcareous nannoplankton Zone
NP16/17 (see Oszczypko-Clowes, in Oszczypko et al. 1999).
The Mniszek Shale Member (Middle to Upper Eocene) is
composed of thin-bedded strata bearing intercalations of var-
iegated shales with Reticulophragmiun amplectens. The basal
portion of the member is composed of two packets of red
shales (Fig. 2), overlain by grey mudstones with intercalation
of thin-bedded flysch (Fig. 3C). Higher up in section these
thin-bedded turbidites are overlain (Tylicz area) by a lenticu-
lar conglomerate body (Fig. 3D,E) up to 1 km long and up
200—50 thick, with a packet of exotic conglomerates (Moch-
nacka & Węcławik 1967; Węcławik 1969). The thickness of
the Mniszek Shale Member varies between 50—100 m in the
Krynica area up to 250—300 m in the Tylicz area.
The upper-most part of the Tylicz sequence belongs to the
Poprad Sandstone Member (Oligocene) of the Magura Forma-
tion (Fig. 3F). This member is composed of thick-bedded
(0.5—1.0 m), fine- to medium-grained, calcareous sandstones,
sometime intercalated by thin-bedded flysch packets. The
thickness of the Poprad Member reaches at least 600—800 m.
Structure
The studied area belongs to two facies-tectonic subunits:
the Bystrica Subunit in the North, and Krynica Subunit in
the South (Fig. 2). In the Bystrica Subunit the sub-vertical
thrust sheets are common. The Krynica Subunit is character-
ized by the presence of narrow anticlines and broad, W—E
trending synclines, built up of the Piwniczna Sandstone
Member of the Magura Formation.
The Bystrica and Krynica Subunits are bounded by the
NW—SE trending sub-vertical Krynica Fault (Świdziński
1972; Oszczypko et al. 1999; Oszczypko & Zuchiewicz
2007; Oszczypko & Oszczypko-Clowes, in print). East of
the Muszynka river (Tylicz transitional facies zone), this
fault is located inside the Magura Formation.
The Bystrica and Krynica Subunits are cut by the several
NE—SW trending transversal faults. On of them, which sepa-
rates the Bytrica and Krynica Subunits from the Tylicz tran-
sitional zone, runs along the Muszynka river (Fig. 2).
43
GEOLOGY, SEDIMENTARY RECORD AND COMPOSITION OF TYLICZ CONGLOMERATE (CARPATHIANS)
Fig. 3. Typical exposures of the upper part of the Tylicz Succession. A – Thick-bedded poorly cemented sandstones of the Maszkowice Sand-
stone Member (Middle Eocene). Muszynka river east of Tylicz; B – Łącko Marls of the Maszkowice Sandstone Mb. Muszynka river east of
Tylicz; C – Grey marly mudstones and very thin-bedded sandstones, at the top of the red shales with Reticulophragmium amplectens. The
lower portion of Mniszek Shale Mb (Late Eocene—Oligocene). Muszynka river at Tylicz; D – Tylicz Conglomerate, Muszynka river at
Tylicz; E – Small anticline, thin-bedded flysch of the Mniszek Shale Mb at the top of the Tylicz Conglomerate. Muszynka river south of
Tylicz; F – Thick-bedded sandstones with big muddy clasts of the Poprad Sandstone Mb (Oligocene), Muszynka river south of Tylicz.
44
OLSZEWSKA and OSZCZYPKO
Studied section
The Tylicz Conglomerate section is located on the left bank
of the Muszyna river, partly in the bed rock of the river (Fig. 2).
The base and top of the conglomerate body are well exposed.
The conglomerates are underlain and overlain by the thin-bed-
ded turbidites represented by grey and dark grey marly mud-
stone and marly shales (Fig. 4A, Fig. 3C—D). After weathering
these mudstones and claystones became green with rusty coat-
ings. The marly-shaly deposits are intercalated by thin- to medi-
um-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
150 m and 50 m thick, separated by 50 m packet of thin-bedded
flysch (Fig. 4A). These conglomerates represent the channel in-
fill incised in thin-bedded turbidites. In general these coarse
clastic deposits display the fining and thining-upwards sequenc-
es. The basal packet of conglomerates begins with 2 m thick-
layer of coarse conglomerates and boulders (Fig. 4A, Fig. 5A),
which pass upwards into 75 m thick layer of paraconglomerate
packet composed of pebbly mudstones. This part of the section
was deposited by cohesive debris flow (Fig. 4A, Fig. 5B—E).
Higher up in the section the conglomerates pass upwards into
75 m packet of thick-bedded coarse- to very coarse-grained
sandstones, deposited by high-concentrated density flow. The
paleocurrent measurements suggest paleotransport from the SE.
Sampling
During the field work in 2004—2005 we exploited (Fig. 4A)
172 pebbles in diameter 2.2 do 16 cm. The biggest pebbles
(13.1 to16 cm) belong to sandstone and limestones respective-
ly. For statistical purposes we divided the pebbles into four
classes (Fig. 4B): carbonates (44.44 %), crystalline (25.93 %),
sandstones (25.93 %) and other (3.70 %). Strong domination
of sedimentary rocks (carbonates and sandstones – 70.37 % )
suggest that sedimentary supply was coming from erosion of
sedimentary rocks of the accretionary wedges. On the Zingg’s
diagram (Fig. 4C) the biggest pebbles are spindle-shaped and
ellipsoidal, while the smaller are dominated by spheroidal and
discoidal pebbles.
Micropaleontological part
Material and methods
This contribution presents the results of the micropaleon-
tological study of the 41 exotic pebbles of carbonate rocks
collected by one of the authors (N. Oszczypko) from the de-
scribed strata.
Thin sections were examined under the Labophot 2-pol
Nikon polarizing microscope. The photos of microfossils
were taken with the aid of the Nikon photomicrographic at-
tachment Microflex HFX-DX. Microfacies identification is
based on Dunham’s revised classification (Wright 1992) and
the classification of mixed siliciclastic and carbonate rocks
by Mount (1985). Microfossil study enclosed foraminifers
(systematics based essentially on Loeblich & Tappan 1988),
calpionellids (systematics based on Makareva 1982), calcar-
eous cysts of dinoflagellata (systematics based on Řehánek
& Cecca 1993). Additionally some other significant micro-
fossils have also been reported.
Results
The results of micropaleontological investigations are pre-
sented in stratigraphical order from the oldest to the young-
est on the basis of identified microfossils.
Fig. 4. A – Lithostratigraphical profile of the Mniszek Mb of the
Magura Formation at Tylicz facies zone; B – Composition of peb-
bles; C – Zingg’s diagram.
45
GEOLOGY, SEDIMENTARY RECORD AND COMPOSITION OF TYLICZ CONGLOMERATE (CARPATHIANS)
Fig. 5. Tylicz conglomerates. Muszynka river south of the Tylicz. A – Basal portion of conglomerates; B—D – Pebble mudstones of the
basal portion of Tylicz Conglomerate.
46
OLSZEWSKA and OSZCZYPKO
Triassic
Triassic pelagic sediments (sample 27) are represented by
“filaments-globochaete” microfacies (Fig. 6A) with rare no-
dosariids (e.g. Nodosaria cf. rossica Miklucho Maklay)
(Fig. 6B).
Shallow-water sediments of the same age (sample A) are
represented by floatstone-packstone with numerous fragments
of crinoids, bivalves, brachiopods, serpulids and ostracods.
Rare foraminifers such as Nodosaria cf. variocamerata Coro-
neou & Trofimova (Fig. 6C) are known from the Carnian of
Bulgaria and the Western Carpathians (Salaj et al. 1983; Tri-
fonova 1994).
Middle Jurassic
Middle Jurassic rich foraminiferal assemblage was identi-
fied in partly recrystallized packstone (sample 28). The as-
semblage was composed of: Protomarssonella osowiensis
(Bielecka & Styk) (Fig. 6E), Verneuilinoides cf. sibiricus
(Mjatliuk) (Fig. 6D), Paleomiliolina occulta Antonova
(Fig. 6H,I), Redmondoides lugeoni (Septfontaine) (Fig. 6J),
Protopeneroplis striata Weynschenk (Fig. 6G), Spirillina cf.
liassina Terquem, Bosniella croatica (Gušić) (Fig. 6F).
Fragments of crinoids and snails accompanied foraminifers.
The first two species cited suggest a Callovian age for the
assemblage.
Late Callovian—earliest Oxfordian
The peloidal packstone, probably of the Late Callovian—
earliest Oxfordian age, contained a poor microfossil assem-
blage composed of foraminifers: Conoglobigerina cf.
bathoniana (Pazdro) (Fig. 6K), Spirillina tenuissima (Güm-
bel), Nodosaria sp.; calcareous dinocysts: Orthopithonella
sp. (Fig. 6L), chlorophycean Globochaete alpina Lombard
and ostracods.
Tithonian
The Tithonian microfossilss were represented by several
distinct assemblages.
The Early Tithonian radiolarian-wackestone, (sample d)
besides numerous radiolarians, contained calcareous cysts of
dinoflagellata with the zonal marker Parastomiosphaera
malmica (Borza) (Fig. 7A). The index species was accompa-
nied by: Comittosphaera pulla (Borza) (Fig. 7B), Colo-
misphaera lapidosa (Vogler), Carpistomiosphaera cf.
borzai (Nagy). The chlorophycean species Globochaete alpi-
na Lombard was also present.
Younger sediments are represented by wackestone of the
Middle/Late Tithonian calpionellid Praetintinnopsella an-
drusovi Zone (samples 16,G,H). The index species
(Fig. 7C,D) was accompanied by another calcareous di-
nocyst Comittosphaera pulla (Borza) and radiolarians.
To the Late Tithonian (Zone Intermedia) were assigned as-
semblages (samples 4,20,h) containing Crassicollaria inter-
media (Durand Delga), Calpionella alpina Lorenz (Fig. 7E),
Calpionella grandalpina Nagy (Fig. 7F) and Tintinnopsella
carpathica (Murgeanu & Filipescu) (Fig. 7H). The calcareous
dinocysts: Colomisphaera carpathica (Borza) (Fig. 7G), Ca-
dosina fusca Wanner and radiolarians occur rarely.
Cretaceous
Berriasian
A typical shallow-water Berriasian assemblage was found
in the microbial grainstone (sample 30). The assemblage was
composed of foraminifers: Paleogaudryina bukoviensis
(Cushman & Glazewski), Rumanoloculina mitchurini (Dain),
Quinqueloculina stellata Matsieva & Temirbekova (Fig. 7J),
Protopeneroplis ultragranulata (Gorbatchik) (Fig. 7I),
Melathrokerion spirialis Gorbatchik, Andersenolina alpina
(Leupold), Neotrocholina molesta (Gorbatchik) (Fig. 7K),
Dobrogelina ovidi Neagu (Fig. 7L). Other characteristic mi-
crofossils include the calcareous algae (Salpingoporella sp.),
Thaumatoporella parvovesiculifera Rainieri and calcimicrobes
of the group “Porostromata”.
Valanginian—Hauterivian
Calpionellid assemblages with Tintinnopsella carpathica
(Murgeanu & Filipescu) and Tintinnopsella longa (Colom)
(Fig. 8E) found in dark wackestones (samples i,j,58) proba-
bly belong to the Tintinnopsella carpathica Zone. In the
Carpathians the zone represents the interval late Early Valan-
ginian-Hauterivian (Reháková 1995).
The assemblage (sample 6) composed of Colomisphaera
heliosphaera (Vogler) (Fig. 8A), Stomiosphaera wanneri
Borza (Fig. 8B) and Hedbergella sp. (Fig. 8C) may be of the
same age.
Barremian—Aptian
Shallow-water carbonate platform microfossils of the Ur-
gonian-type were found in samples 39, 42 and L1E1. Fora-
miniferal assemblage contained characteristic orbitolinid
species Palorbitolina lenticularis (Blumenbach) (Fig. 8G)
as well as: Dorothia praeoxycona Moullade (Fig. 8F), Everticy-
clammina hedbergi (Maync), Glomospira urgoniana Arnaud
Vanneau (Fig. 8H), Bolivinopsis labeosa Arnaud Vanneau
(Fig. 8D), Charentia cuvilieri Neumann (Fig. 8K), Ru-
manoloculina pseudominima (Bartenstein & Kovatcheva)
(Fig. 8I), Trocholina paucigranulata Moullade (Fig. 8J),
Arenobulimina sp. A significant part of assemblages was
made up of calcareous algae (Dasycladales), microproblem-
atics (Baccinella irregularis Radoičić) and calcimicrobes
(“Porostromata”).
Paleogene
Paleocene
The foraminiferal-algal-bryozoan packstone of sample
No. 67 was tentatively assigned to the Paleocene. The fora-
miniferal assemblage included: Haddonia heissigi Hagn
(Fig. 9H), Lobatula lobatula (Walker & Jacob) (Fig. 9A),
47
GEOLOGY, SEDIMENTARY RECORD AND COMPOSITION OF TYLICZ CONGLOMERATE (CARPATHIANS)
Fig. 6. Microphographs of the Triassic to Oxfordian foraminifers. A – “filaments-Globochaete” microfacies, sample 27, Triassic; B – No-
dosaria cf. rossica Miklucho Maklay, longitudinal section, sample 27, Triassic; C – Nodosaria cf. variocamerata Coroneou & Trofimova,
fragment of longitudinal section, sample A, Triassic; D – Verneuilinoides cf. sibiricus (Mjatliuk), axial section, sample 28, Middle Jurassic;
E – Protomarssonella osowiensis (Bielecka & Styk), longitudinal section, sample 28, Middle Jurassic; F – Bosniella croatica (Gušić), axial
section, sample 28, Middle Jurassic; G – Protopeneroplis striata Weynschenk, equatorial section, sample 28, Middle Jurassic; H – Paleo-
miliolina occulta Antonova, transversal section, sample 28, Middle Jurassic; I – Paleomiliolina occulta Antonova, longitudinal section,
sample 28, Middle Jurassic; J – Redmondoides lugeoni (Septfontaine), axial section, sample 28, Middle Jurassic; K – Conoglobigerina
cf. bathoniana (Pazdro), longitudinal section, sample 12, Late Callovian-earliest Oxfordian; L – Orthopithonella sp., sample 12, Late
Callovian-earliest Oxfordian.
48
OLSZEWSKA and OSZCZYPKO
Fig. 7. Microphotographs of the Tithonian to Berriasian foraminifers. A – Parastomiosphaera malmica (Borza), sample d, Early Titho-
nian; B – Comittosphaera pulla (Borza), sample d, Early Tithonian; C – Praetintinnopsella andrusovi Borza, longitudinal section, sample H,
Middle/Late Tithonian; D – Praetintinnopsella andrusovi Borza, transversal section, sample H, Middle/Late Tithonian; E – Calpionella
alpina Lorenz, longitudinal section, sample 4, Late Tithonian; F – Calpionella grandalpina Nagy, longitudinal section, sample 20, Late
Tithonian; G – Colomisphaera carpathica (Borza), sample 4, Late Tithonian; H – Tintinnopsella carpathica (Murgeanu & Filipescu), longi-
tudinal section, sample 4, Late Tithonian; I – Protopeneroplis ultragranulata (Gorbatchik), axial section, sample 30, Berriasian; J – Quin-
queloculina stellata Matsieva & Temirbekova, transversal section, sample 30, Berriasian; K – Neotrocholina molesta (Gorbatchik), axial
section, sample 30, Berriasian; L – Dobrogelina ovidi Neagu, sample 30, oblique section, sample 30, Berriasian.
49
GEOLOGY, SEDIMENTARY RECORD AND COMPOSITION OF TYLICZ CONGLOMERATE (CARPATHIANS)
Fig. 8. Microphotographs of the Valanginian-Hauterivian to Aptian foraminifers. A – Colomisphaera heliosphaera (Vogler), sample 6, Val-
anginian-Hauterivian; B – Stomiosphaera wanneri Borza, sample 6, Valanginian-Hauterivian; C – Hedbergella sp., axial section, sample 6,
Valanginian-Hauterivian; D – Bolivinopsis labeosa Arnaud-Vanneau, longitudinal section, sample 42, Barremian-Aptian; E – Tintinnopsel-
la longa (Colom), longitudinal section, sample 58, Valanginian-Hauterivian; F – Dorothia praeoxycona Moullade, oblique section, sam-
ple L1E1, Early Aptian; G – Palorbitolina lenticularis (Blumenbach), subaxial section, sample L1E1, Early Aptian; H – Glomospira ur-
goniana Arnaud Vanneau, oblique section, sample L1E1, Early Aptian; I – Rumanoloculina pseudominima (Bartenstein & Kovatcheva),
transversal section, sample 39, Barremian—Aptian; J – Trocholina paucigranulata Moullade, axial section , sample 42, Barremian—Aptian;
K – Charentia cuvilieri Neumann, oblique section, sample L1E1, Early Aptian.
50
OLSZEWSKA and OSZCZYPKO
Fig. 9. Microphotographs of the Paleocene to Oligocene foraminifers. A – Lobatula lobatula (Walker & Jacob), transversal section, sam-
ple 67, Paleocene; B – Pararotalia lithothamnica (Uhlig), oblique section, sample 68, Middle-Late Eocene; C – Eorupertia cristata
(Gümbel), axial section, sample 68, Middle-Late Eocene; D – Turborotalia cerroazulensis (Cole), oblique section, sample 68, Middle-
Late Eocene; E – Globigerina cf. eocaena (Gümbel), axial section, sample 68, Middle-Late Eocene; F – Discocyclina chudeaui
(Schlumberger), axial section, sample 68, Middle-Late Eocene; G – Discocyclina sella (d’Archiac), subaxial section, sample 68, Middle—
Late Eocene; H – Haddonia heissigi Hagn, vertical section, sample 67, Paleocene; I – Tenuitella sp., axial section, sample E, Oligocene.
J – Cibicides sp., oblique section, sample E, Oligocene; K – Chiloguembelina sp., transversal section, sample E, Oligocene.
51
GEOLOGY, SEDIMENTARY RECORD AND COMPOSITION OF TYLICZ CONGLOMERATE (CARPATHIANS)
Quinqueloculina cf. hexacostata Le Calvez, Planorbulina
cretae Marsson. The characteristic algal species include
Polistrata alba (Pfender), Neogoniolithon sp. and stroma-
tolitic structures.
Eocene
Algal-bryozoan rudstone with foraminifers indicating the
Middle—Late Eocene age was found in sample No. 68. The
foraminiferal assemblage contained large and small foramin-
ifers, characteristic for open shelf carbonate environment:
Discocyclina sella (d’Archiac) (Fig. 9G), Discocyclina
chudeaui (Schlumberger) (Fig. 9F), Marssonella cf. lodoen-
sis Israelsky, Eorupertia cristata (Gümbel) (Fig. 9C),
Pararotalia lithothamnica (Uhlig) (Fig. 9B), Mississippina
binkhorsti Reuss, Cibicides praeventratumidus Mjatliuk,
Globigerina cf. eocaena (Gümbel) (Fig. 9E), Turborotalia
cerroazulensis (Cole) (Fig. 9D). The foraminifers were ac-
companied by numerous fragments of Lithothamnium sp.
and bryozoans.
Oligocene
Brownish mudstones with organic matter and pyrite con-
cretions (samples E, F, f) yielded rare and very small sections
of foraminifers usually observed in thin plates from the Lower
Oligocene sediments (Olszewska 1997a,b). Representatives of
the following genera have been identified: Tenuitella sp.
(Fig. 9I), Globigerina sp., Chiloguembelina sp. (Fig. 9K),
Cibicides sp. (Fig. 9J) and ?Virgulinella sp.
Discussion
Microfossils and the age of examined pebbles show that
generally they follow the same stratigraphical and paleoenvi-
ronmental trends discovered by study of exotic pebbles from
other localities in the Outer Carpathians. Previous research
(Malata et al. 2006), revealed that the most common carbonate
exotics in the Outer Carpathians represent the Middle Triassic,
Middle—Upper Jurassic, and Middle Eocene. Rocks of other
ages (Devonian, Early Cretaceous, Paleocene) occur more
rarely. Pebbles of pelagic origin occur more frequently in in-
ternal parts of the Outer Carpathians (Pieniny Klippen Belt,
Magura and Fore-Magura Nappes). They generally represent
deposits of major regional transgressions. In external parts of
the Outer Carpathians (Skole, Silesian Nappes) pebbles of
neritic origin predominate.
Triassic
The Triassic pelagic assemblage closely resembles the ba-
sinal “filament-Globochaete” microfacies described from the
Reifling Limestone Formation of the Central Western Car-
pathians (Masaryk et al. 1993). The formation is characteris-
tic of the Middle Triassic of the Choč Nappe of the Tatra
Mountains.
Packstone-floatstone with numerous fragments of macro-
fossils, to the certain extent, resembles assemblages of shal-
low intraplatform facies of the Zámostie Formation of the
same nappe.
Similar types of Middle Triassic exotic pebbles was recog-
nized (B. Olszewska) in the Upper Cretaceous gravelstone of
the Sromowce Formation of the Pieniny Klippen Belt.
Middle Jurassic
Identification of the Middle Jurassic (?Callovian) shallow-
water carbonate type foraminiferal assemblage supports the
view of considerable extension of carbonate platforms dur-
ing this period (Bassoullet 1997; Velić 2007). The species
Protomarssonella osowiensis (Bielecka & Styk) and Bosniella
croatica (Gušić) were also observed in exotic pebbles from
the Sromowce gravelstone (Pieniny Klippen Belt). Identifi-
cation of the latter species in the Middle Jurassic sediments
on the Cracow-Wieluń Upland indicates unrestricted connec-
tion between epicontinental basins and the Tethyan carbonate
sedimentation areas.
Late Jurassic
Sediments of the early part of the epoch (Oxfordian—Kim-
meridgian) are poorly represented. They may be absent from
the area or their soft lithology (e.g. mudstone) facilitated ero-
sion. On the contrary Tithonian carbonate pebbles are fre-
quent and numerous, suggesting considerable expansion of
sediments of this age. The presence of common in the Car-
patho-Balkan region calpionellides and calcareous dinocyst
index species (Reháková 1995, 2000) supports the suggestion.
Cretaceous (Berriasian)
The characteristic Berriasian assemblage belongs to the
carbonate shallow-water biota of the Northern Tethyan shelf.
It was found not only in the Western and Eastern Car-
pathians (Bucur 1988; Vašíček et al. 1994; Olszewska 2005)
but also in the Eastern Alps (Gawlick et al. 2005), Moesian
Platform (Ivanova et al. 2008) and Crimea (Krajewski &
Olszewska 2007). The same assemblage was encountered on
the southern edge of the Western European Platform as well
(Olszewska 1999, 2001; Gutowski et al. 2005).
Valanginian—Hauterivian. Argillaceous limestones of this
age coincide with the Valanginian world wide transgression
that brought pelagic organisms such as calpionellids, calcar-
eous dinocysts and planktonic foraminifers and changed the
type of sedimentation from carbonate to siliciclastic (Lini et
al. 1992). The discussed microfossil assemblage of the exotic
pebbles may be compared to assemblages of the same age
found in the Polish Outer Carpathians flysch sequence
(Olszewska 2005).
Barremian—Aptian. The Urgonian-type foraminiferal as-
semblage contains taxa known from the Urgonian sediments
of the Tatra Mts (Lefeld 1968; Vašíček et al. 1994) and many
other European sites of Barremian-Aptian carbonate sedi-
mentation (Arnaud-Vanneau 1980). Similar but very rich Ur-
gonian-type foraminifers occurred in exotic pebbles from the
Upper Cretaceous—Paleogene flysch sediments of the Pieniny
Klippen Belt (Krobicki & Olszewska 2005).
52
OLSZEWSKA and OSZCZYPKO
Paleogene (Paleocene)
The foraminiferal-algal-bryozoan assemblage resembles
those typical for the “in situ” carbonate deposits of the
Pańska Góra locality within the so-called “Andrychów
Klippes” in the north-western part of the Outer Carpathians
and in the Slovak part of the Pieniny Klippen Belt (Scheib-
ner 1968; Krobicki et al. 2004; Köhler & Buček 2005). Similar
assemblages were found in pebbles of allodapic limestones in
Babica Clays of the Polish Outer Carpathians (Rajchel &
Myszkowska 1998).
Eocene
A rich shallow-water microfossil assemblage encountered
during the research represents widespread Middle-early Late
Eocene carbonate platform associations common on the north-
ern Tethyan shelf. In the Outer Carpathians those associations
are found in carbonate sediments known as “the Łużna/Ko-
niaków limestone” which occur as exotic pebbles in the Oli-
gocene Menilite and lower Krosno Beds. The only area where
those sediments are “in situ” are the northern slopes of Tatra
Mts and there they are known as “the Nummulitic Eocene”
(Olszewska & Wieczorek 1998 ). According to Arni’s sedi-
mentological model (Arni 1965) both types predominantly
represent an open shelf environment because of numerous dis-
cocyclinids and the presence of planktonic foraminifers.
Oligocene
The general paucity of microfossils in the Oligocene—Lower
Miocene sedimentary sequence of Carpathians is also reflect-
ed in thin section assemblages. They are composed of only a
few characteristic forms, predominantly planktonic foramini-
fers of the genera: Globigerina, Tenuitella, Chiloguembelina.
Benthic microfossils are rare because of dysaerobic conditions
at the bottom of basins unfavourable for life and preservation.
Conclusions
In the Paleogene deposits of the southern part of the
Magura Nappe (Krynica Zone) the exotic pebbles have been
recognized in two stratigraphical position:
a) In the thick-bedded sandstones of Zarzecze Formation
– the Krynica Sandstone Member (Lower/Middle Eocene)
and the Piwniczna Sandstone Member (Lower/Middle
Eocene) of the Magura Formation and its equivalent the lower
part of the Strihovce Sandstone (Čerhova Sandstone, Middle
Eocene, see Nemčok 1990a,b). These conglomerates are rich
granitoids, gneisses, phyllites and quartzites, with a relative-
ly small amount of basic volcanic rocks and Mesozoic car-
bonates (Oszczypko 1975; Mišík et al. 1991a; Oszczypko et
al. 2006). The later pebbles are represented by deep-water
Jurassic-Lower Cretaceous sediments as well as fragments of
shallow-water limestones of the Triassic (Anisian), Kim-
meridgian—Upper Tithonian, Lower Cretaceous (Urgonian),
Upper Cretaceous, Lower and Upper Paleocene, and Lower
Lutetian (Mišík et al. 1991a).
b) In the thick-bedded sandstones and conglomerates of
the Poprad Member (Upper Eocene-Oligocene) of the Magura
Formation (see the Tylicz Conglomerate, this issue) and the
upper part of the Strihovce Sandstone Mišík et al. (1991a)
(see also lower Malcov Beds-Strihov Beds (Middle/Upper
Eocene; Nemčok 1990a,b). These conglomerates contain
variable amounts of carbonate pebbles, with up to 44 % in
the Tylicz section. This population is dominated by Mesozoic
shallow-water limestones, with subordinate amounts of the
deep-water clasts. The oldest pebbles belong to the Late
Paleozoic, the youngest to the Late Eocene and Oligocene.
The composition of carbonate material and microfossil as-
semblages of the Tylicz Conglomerate (Late Eocene—Oli-
gocene) indicates similarity to both the Jarmuta/Proč and
Strihovce exotic pebbles. In contrast the amounts of the
sandstone clasts is relatively high in both the Tylicz and the
Strihovce sandstones, 25.93 % and 44.0 % respectively, and
very low in the Jarmuta and Proč Formations (3.18 % see
Mišík et al. 1991b and Ma ašovský 2002). This suggests ero-
sion of the older accretionary wedge during the Late Eocene
to Oligocene deposition in the southern part of the Magura
Basin. The other possibility can be explained by supply of
siliciclastic material from a SE source area (Dacia and Tisza
Mega-Units) and carbonate material from S source area
(ALCAPA Mega-Unit: Central Carpathian Block and Pieniny
Klippen Belt). This solution can be deduced from Oli-
gocene?/Early Miocene paleogeographical restoration (see
Fig. 6, Ustaszewski et al. 2008).
The stratigraphical position (above variegated shales with
Reticulophragmium amplectens) and composition of exotic
pebbles of the Tylicz Conglomerate is the same as the Hervatov
Conglomerate located south of Bardejov (see Nemčok
1990a,b). According to this author these paraconglomerates
were deposited by the debris flow and contain blocks and
cobbles of Mesozoic carbonates up 5 m in diameter as well
as crystalline and sandstone pebbles, whereas muddy-sandy
matrix the “Lamellibranchiata” macrofauna were found (see
also Świdziński 1961).
Acknowledgment: The authors express their thanks to Prof.
D. Reháková and Prof. I. Bucur for their constructive com-
ments, which improved this paper. Thanks are extended to
Dr. M. Oszczypko-Clowes for preparation of computer
drawings. This paper was financed by the Polish Ministry of
Sciences and Higher Education (Grant No. 307 025 31/1997
(to NO)).
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