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, APRIL 2016, 67, 2, 147—164
doi: 10.1515/geoca-2016-0010
The Upper Cretaceous Ostravice Sandstone in the Polish
sector of the Silesian Nappe, Outer Western Carpathians
MAREK CIESZKOWSKI
1
, ANNA WAŚKOWSKA
2
, JUSTYNA KOWAL-KASPRZYK
1
,
JAN GOLONKA
2
, TADEUSZ SŁOMKA
2
, ANDRZEJ ŚLĄCZKA
1
, PATRYCJA WÓJCIK-TABOL
1
and RAFAŁ CHODYŃ
1
1
Jagiellonian University, Institute of Geological Sciences, Oleandry 2a, 30-376 Kraków, Poland; marek.cieszkowski@uj.edu.pl,
justyna.kowal@uj.edu.pl, andrzej.slaczka@uj.edu.pl, p.wojcik-tabol@uj.edu.pl, rafal.chodyn@uj.edu.pl
2
University of Science and Technology (AGH), Faculty of Geology, Geophysics and Environmental Protection, Al. Mickiewicza 30,
30-059 Kraków, Poland; waskowsk@agh.edu.pl, jgolonka@agh.edu.pl, tslomka@agh.edu.pl
(Manuscript received June 27, 2015; accepted in revised form December 8, 2015)
Abstract: The Ostravice Sandstone Member was identified and described as a lithostratigraphic unit in the Polish part
of the Outer Carpathians. This division occurs in the lowermost part of the Godula Formation, is underlain by varie-
gated deposits of the Mazák Formation or directly by the Barnasiówka and Lhoty formations, and overlain by the
Czernichów Member of the Godula Formation. Domination by thick- and very thick-bedded sandstones, conglomeratic
sandstones and conglomerates rich in calcareous clasts, mostly of the Štramberk-type limestones, is typical for the
Ostravice Sandstone Member. These deposits are widespread between the Moravskoslezské Beskydy Mountains in the
Czech Republic and the Ciężkowice Foothills in Poland. The documentation of the Ostravice Sandstone Member occur-
rence as well as the petrological, sedimentological features, and inventory of the carbonate clasts are presented here.
Key words: Outer Carpathians, Silesian Nappe, Late Cretaceous, Godula Formation, Ostravice Sandstone Member,
lithostratigraphy, sedimentology, carbonate clasts.
Introduction
The Carpathians, one of the most important mountain ranges
of the European Alpides, are divided into the Inner Car-
pathians and the Outer Carpathians domains (e.g.
Książkiewicz 1962, 1965, 1972, 1977; Mahe 1974; Ciesz-
kowski et al. 1985; Ślączka & Kaminski 1998; Golonka et
al. 2005, 2006 and references therein). The Outer Car-
pathians (with the exception of the Pieniny Klippen Belt) are
also called the Flysch Carpathians because they are mainly
composed of the flysch facies (turbidites) and they consist of
a stack of nappes and thrust-sheets. The nappe succession in
the Polish sector of the Outer Carpathians from the highest to
the lowermost ones includes the Magura Nappe, Dukla
Nappe and Foremagura group of nappes, Silesian Nappe,
Subsilesian Nappe, Skole Nappe, and Stebnik and Zgłobice
units (e.g. Książkiewicz 1962, 1965, 1972, 1977; Bieda et al.
1963; Geroch et al. 1967; Koszarski et al. 1974; Cieszkows-
ki et al. 1985; Żytko et al. 1989; Lexa et al. 2000; Ciesz-
kowski 2003; Golonka et al 2005, 2006, 2013a; Ślączka et
al. 2006; Golonka & Waśkowska-Oliwa 2007 and papers
cited therein).
The Silesian Nappe is one of the largest tectonic units of
the Western Outer Carpathians (e.g. Roth & Matějka 1953;
Andrusov 1959; Książkiewicz 1972, 1977; Eliáš 1979;
Ślączka et al. 2006). It is composed of a continuous turbiditic
sequence up to six thousands metres thick or occasionally
more representing the Late Jurassic through to the Early
Miocene (e.g. Cieszkowski 1992; Ślączka & Kaminski 1998;
Ślączka et al. 2006; Picha et al. 2006; Cieszkowski et al.
2012b and papers cited therein). Numerous papers were
devoted to the litho- and biostratigraphy of Cretaceous and
Palaeogene deposits of the sedimentary succession present in
the Silesian Nappe. Some of them proposed formalization of
the Silesian Nappe’s deposits according to the Polish Strati-
graphic Code (Alexandrowicz et al. 1975; Racki &
Narkiewicz 2006). A lithostratigraphy of the Upper Jurassic—
Lower Cretaceous deposits of the Silesian Nappe in the
Western part of the Outer Carpathians was proposed by
a group of Polish and Czech geologists (Golonka et al. 2008).
A proposal for the complete lithostratigraphy of the Upper
Jurassic—Lower Miocene deposits representing the Silesian
Nappe was prepared by Golonka et al. (2013a). These pro-
posals were preceded by field research aimed at better identi-
fication and revision of the formalized lithostratigraphic
units. The research enables the highlighting of some new
facts, including the discovery that the Ostravice Sandstone
described until now only from the Moravskoslezské Beskydy
Mts. in the Czech Republic also occurs in the Polish sector
of the Outer Carpathians (Fig. 1) and forms the lowermost
member of the Godula Formation (Late Cretaceous in age).
Sedimentation of these sandstones in the Silesian Basin
marks the initiation of a new Late Cretaceous—Early Palaeo-
gene stage of development of the Outer Carpathian
domain (cf. Eliáš 2000; Picha et al 2006; Cieszkowski et al.
2009a).
This paper concerns the Ostravice Sandstones. The authors
paid attention to the development, lithostratigraphic posi-
tion, distribution and composition of these sandstones and
their formal lithostratigraphy.
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Ostravice Sandstone Member
Position of the Ostravice Sandstone Member within the
Godula Formation
The Godula Formation is widespread in the Silesian
Nappe in the western part of the West Outer Carpathians in
Poland and the Czech Republic (e.g. Koszarski et al. 1959;
Koszarski & Ślączka 1973; Ślączka 1986; Słomka 1995;
Picha et al. 2006). It is composed of thick-, medium- and
thin-bedded glauconitic sandstones with intercalations of
grey shales. The presence of glauconite in sandstones is
a characteristic feature important for distinguishing the Godula
Formation. In the western part of the occurrence area, it
reaches the impressive thickness of up to 2500 m or even al-
most 3000 m in the Moravskoslezské Beskydy Mts., 2000 m
in the Beskid Śląski (in Czech: Slezské Beskydy) Mts, and
about 1500 m in the Beskid Mały Mts. (Słomka 1995).
North-east of the Beskid Mały Mts. the Godula Formation is
thinning and interfingering with variegated shales of the
Mazák Formation (Picha et al. 2006) (Fig. 2). Further to the
east the thickness decreases to below 1000 m, and mostly
ranges between 200 and 400 m. In the eastern part of the
Polish Outer Carpathians this formation can be partly or
completely replaced by variegated shales of the Mazák For-
mation (“Godula variegated shales”) as in the Bystre thrust
sheet in the Bieszczady Mts. (cf. Ślączka 1959). The Godula
Formation was described firstly in the Silesian part of the
Carpathians as the Godula Beds, which were divided into
three parts: Lower, Middle, and Upper Godula Beds (e.g.
Książkiewicz 1933; Burtanówna et al. 1937; Geroch et al.
1967; Unrug 1969; Burtan 1973; Koszarski & Ślączka 1973;
Nowak 1973; Słomka 1995). In relation to this, Golonka et
al. (2013a) following partly Burtan (1973) and Wójcik et al.
(1996) proposed formal lithostratigraphy for the sedimentary
sequence of the Silesian Nappe and suggested dividing the
Godula Formation into a few lithostratigraphic members.
The lower part of this formation should be divided into the
Ostravice Sandstone Member which consists mainly of
thick-bedded sandstones, and the Czernichów Member rep-
Fig. 1. Geological setting of the Ostravice Sandstone Member in the western sector of the Outer Carpathians (map after Lexa et al. 2000 —
simplified).
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Fig. 2. Lithostratigraphic log of the Late Jurassic—Cretaceous sedimentary succession of the Silesian Nappe exposing the position
of the Ostravice Sandstone Member within the Godula Formation.
resented by fine-grained, thin- and medium-bedded sand-
stones intercalated with black or grey shales. The middle
part, developed as thick-bedded sandstones with thin shaly
intercalations, is called the Skrzyczne Member. The upper
part named the Wisła Member consists of thin- and thick-
bedded sandstones and green shales. Conglomerates in the
upper part, which were called the Malinowska Skała Con-
glomerate Member (Burtan 1973), are widespread in
the Beskid Śląski (Slezské Beskydy) Mts. and the Beskid
Mały Mts. (e.g. Burtan 1973; Książkiewicz 1974; Słomka
1995). The age of the Godula Formation is estimated as the
Turonian—Early Senonian time interval (Nowak 1973; Ciesz-
kowski 1992; Słomka 1995; Ślączka & Kaminski 1998
and references therein), Turonian—Campanian/Maastrichtian
boundary (Skupien & Mohamed 2008). The Godula Forma-
tion is underlain by the variegated shales of the Mazák For-
mation and overlain by the thick-bedded sandstones of the
Istebna Formation.
Taking into consideration the above-mentioned facts, we
can state that the Ostravice Sandstone Member is the lower-
most lithostratigraphic sub-division of the Godula Forma-
tion. From the bottom it borders with the Mazák Formation.
In many places the lower boundary of this member is erosive
and the Ostravice Sandstone Member contacts directly with
the Barnasiówka or even Lhoty formations. It is caused by
the dynamic sedimentation of the sandy and conglomeratic
deposits. From the top the Ostravice Sandstone Member bor-
ders the thin- and medium-bedded sandstone-shaly complex
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of the Czernichów Member. In the Moravskoslezské Besky-
dy Mts. the transition between the Mazák Formation. and
Ostravice Sandstone Member of the Godula Formation can
be gradual and layers of sandstones rich in carbonate clasts
could be interbedded with red shales (cf. Andrusov 1933).
Anyway, the Ostravice Sandstone Member is widespread in
the southern area of occurrence of the Godula Formation.
Name
The Ostravice Sandstone Member name was given after
the Ostravice River in the Moravskoslezské Beskydy Mts.,
Frýdek-Místek District, Ostrava Province, Morava Land,
Western Outer Carpathians, Czech Republic.
Czech name: ostravický pískovec v godulských vrstvách.
Polish name: ogniwo piaskowca ostrawickiego (shortened
name: ogniwo ostrawickie).
Area of occurrence
The Ostravice Sandstone Member is widespread in the
Outer Carpathians in the Silesian Nappe on the territory of
the Czech Republic and Poland over a distance of about
300 km, from the surroundings of Ostravice village to the
surroundings of Gromnik village. Its outcrops were noticed
in the Moravskoslezské Beskydy Mts., Beskid Śląski
(Slezské Beskydy) Mts., Beskid Mały Mts., and Wieliczka,
Wiśnicz, Rożnów, and Ciężkowice foothills (Fig. 1).
Type section
The abandoned quarry called “Mazák Quarry” located in
the Ostravice river valley, on the right bank of the river, near
the tributary of Mazák Creek in Ostravice village (GPS coor-
dinates: 49°32 25.9” N, 18°26 24.8” E), Frýdek-Místek Dis-
trict, Moravskoslezské Beskydy Mts., Czech Outer
Carpathians, Morava Land, Czech Republic (Figs. 1, 3.1—3.5).
Reference section (proposed by authors)
Abandoned quarry in Ustroń-Poniwiec, town of Ustroń,
Akacjowa Str., northern slope of Czantoria Mt., Beskid
Śląski Mts., Cieszyn District, Upper Silesian Province, Po-
land (Figs. 1, 4).
Thickness
The member’s thickness in the type section is about
60—120 m, but in the Moravskoslezské Beskydy Mts. even
a 150—400 m complex of thick bedded sandstones located at
the base of the Godula Formation is included in this division
(Menčík in: Roth et al. 1962). East of the Beskid Mały Mts.
the thickness of the Ostravice Sandstone Member is chan-
geable but in general it decreases.
Dominant lithology
The Ostravice Sandstone Member is characterized by the
dominant occurrence of 0.7—2.0 m thick sandstone layers.
Thicker, amalgamated layers of up to 5 m also occur. The
sandstone is medium- and coarse-grained, often conglome-
ratic (Figs. 3, 4, 5). Layers or lenses of fine conglomerate are
not uncommon. Occasionally coarser conglomerate with
pebbles or clasts of exotic rocks (3—7 cm, occasionally even
up to 30 cm in size) occurs. In some layers limestone clasts
of different sizes are so numerous that the rock takes on
characteristics of sedimentary breccia. The thicker sandstone
layers are usually massive, but in thinner layers parallel lami-
nation occurs. In some cases dish structures can be noticed as
well as flame structures (Fig. 6). The sandstone is more or
less rich in glauconite, which causes its grey-greenish
colour. In some parts of sections the thick-bedded sandstone
deposits are intercalated with medium-bedded, medium- or
fine-grained glauconitic sandstones with more or less clearly
developed sequences of Bouma intervals, very typical
for the facial type of “Godula sandstone”. These are inter-
bedded very rarely with grey-bluish marly or greenish clayey
shales.
The sandstones and conglomerates are composed of mo-
nomineral grains as well as fragments of rocks. Bioclasts
such as fragments of corals, echinoids, crinoids, fragments
of crushed mollusk shells, and calcareous algae are also ob-
servable (Figs. 7.1, 7.2). Detritic material is matted with car-
bonate or carbonate-ferruginous cement.
The grains and pebbles are usually sub-rounded, but some
of them are more or less angular, especially clasts of lime-
stones, which indicates their short transport to the point from
which they flowed in turbidity currents to the deep sedimen-
tary basin. Some fragments of limestones reveal traces of
synsedimentary erosion and redeposition, and they are allo-
dapic limestones consisting of limestone clasts inherent in
detrital, medium- or coarse-grained carbonate matrix of the
same age as clasts.
In general composition, the sandstones described above
are similar to these common within the whole section of the
Godula Formation. However, a fundamental feature that
allows us to easily distinguish the Ostravice Sandstone
Member is the presence of numerous clasts of limestone in
coarse-grained and conglomeratic sandstone. These whitish
clasts, of different dimensions, are explicitly visible against
the dark grey sandstone background (Figs. 3, 4).
The thick-bedded sandstones of the Ostravice Member
contain large olistoliths of older turbiditic deposits known
from the sedimentary succession of the Silesian Nappe.
Their lateral size is from several metres up to 100 m or more,
and thickness 3—10 m or even more. They are clearly visible
only in big outcrops.
History
The Ostravice Sandstone (in Czech: ostravický pískovec)
within the sedimentary succession of the Silesian Nappe was
named and first described by Andrusov (1933) from Moravia
– eastern part of the Czech Republic. Its name is connected
with the name of the Ostravice River (Roth & Andrusov in:
Andrusov & Samuel 1985, page 111) which has source in
the Moravskoslezské Beskydy Mts. and flows through the
nearby city of Ostrava. However, Andrusov (1933) did not
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Fig. 3. Exposures of the Ostravice Sandstone Member and Mazák Formation in the Mazák Quarry, Moravskoslezské Beskydy Mts., Czech
Republic (3.1—3.5). Outcrop in Porąbka, Beskid Mały Mts., Poland (3.6) and the sample of the conglomerate from this locality (3.7).
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Fig. 4. Exposures of the Ostravice Sandstone Member in the Ustroń-Poniwiec Quarry as the proposed neostratotype. 1—2 – thick-bedded
Ostravice Sandstone Member. 3—4 – whitish clasts of limestones explicitly visible against of the dark grey background. 5 – pebble of
limestone in conglomerate.
recently called the Mazák Formation (e.g. Picha et al. 2006;
Golonka et al. 2013a). In Andrusov’s (1933) description on
page 196 we can find that the Ostravice Sandstone is de-
veloped as thick-bedded, 2—4 m thick, light grey or light
greenish, fine- to coarse-grained, silicified glauconitic sand-
stone layers. Between these layers thin intercalations of
strongly glauconitic muddy-sandstones and red clayey
shales appear. Conglomeratic intercalations with frequent
explicitly write whether he named the sandstones after the
Ostravice River or Ostravice village. However, it is apparent
from the text that the second option is correct (cf. “...I call it
Ostravice Sandstone because it has great extent near Ostra-
vice...”). The described sandstone is exposed there in the
quarry located in the Ostravice river valley near the tributary
of Mazák Creek in Ostravice village. In the quarry the
Ostravice Sandstone overlaid the Godula Variegated Shales,
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pebbles of quartz and significant clasts of the Štramberk
Limestone occur in the sandstones.
This characterization has been completed and partly ex-
tended. Matějka & Roth (1949) noted that the Ostravice
Sandstone in the Ostravice river valley occurs within the
Godula Variegated Shales (Beds) and is represented mainly
by thick-bedded sandstone, discontinuous in many places.
Menčík (in: Roth et al. 1962) included to this division
a 150—400 m thick thick-bedded sandstone package occurring
at the base of the Godula Beds in the S and SE surroundings
of Třinec which laterally replaced the shaly Variegated
Godula Beds. Eliáš (1995, 2000) also described the Ostravice
Sandstone from the Outer Carpathians in Moravia and noted
that they formed a prograding sedimentary fan beginning the
new Late Cretaceous evolutionary stage of the Silesian Basin.
Roth & Andrusov (in: Andrusov & Samuel 1985) stated
that the Ostravice Sandstone developed within the sedimen-
tary succession of the Silesian Nappe and forms a lithostrati-
graphic division dominated by sandstones. In many places it
overlays the Variegated Godula Beds, but also replaces them
partly or completely. They described distinctive coarse and
conglomeratic or even brecciated sandstones rich in lime-
stone clasts as well as light glauconitic noncalcareous sand-
stones. The age of the sandstone was estimated as
Cenomanian—Lower Turonian.
Some specimens of macrofossils were found in some
clasts of sediments redeposited into the Ostravice Sandstone.
The ammonite Perisphinctes sp. and remnants of corals
(Andrusov 1933) were noticed in clasts of the Štramberk-
type limestones, while in clasts of the Tešin-Hradište Beds
(recently called Cisownica Member of the Hradište Forma-
tion) Early Cretaceous ammonite fauna was identified
(Foldyna & Šuf 1964).
Picha et al. (2006) (page 111) mentioned that thick, coarse
turbiditic sandstones and conglomerates representing the
Ostravice Sandstone (sensu Andrusov 1933) interbed varie-
gated pelagic and hemipelagic shaly deposits of the Mazák
Formation (sensu Roth 1980). They noticed that the Mazák
Formation was assigned by Hanzlíková (1973) to the
Cenomanian age. Their figs. 17A and 17B present the
stratigraphy and lithostratigraphic logs of Outer Carpathian
units in the Czech Republic. The Ostravice Sandstone is
marked there as an intercalation within the Mazák Formation.
The deposits of the Ostravice Sandstone Member were not
mentioned in the Polish literature almost to this time, with
the exception of a cursory consideration by Słomka (1995)
who conducted extensive and detailed research into the de-
velopment and sedimentological features of the Godula For-
mation in Poland and the Czech Republic. He studied the
Ostravice Sandstone in its stratotype area in the Moravsko-
slezské Beskydy Mts., and noticed the origin of a submarine
fan formed by these sandstones at the foot of the north-
western slope of the Silesian Ridge in the Late Cenomanian.
The occurrence, lithology, some sedimentological features,
and lithostratigraphic position of the Ostravice Sandstone in
the Polish sector of Silesian Nappe between Ustroń and
Tuchów area were briefly described by Cieszkowski et al.
(2010). Next, the micropalaeontological data from limestone
clasts from the Ostravice Sandstone in Poland were presented
(Cieszkowski et al. 2011; Kowal et al. 2011). These sand-
stones were also mentioned in some publications considering
the existence and origin of olistostromes and olistoliths in
the Outer Carpathians (e.g. Cieszkowski et al. 2009a,
2012a, b). In a paper presenting the geology of the western
part of Polish Outer Carpathians, Golonka et al. (2013a) pro-
posed to recognize the Ostravice Sandstone as the lowermost
member of the Godula Formation.
Though the name “Ostravice
Sandstone” was not used in Polish
geological publications, some ge-
ologists noticed that in the thick-
bedded sandstone at the base of
the Godula Formation in the Be-
skid Śląski Mts. (e.g. Ślączka and
Kaminski
1998;
Cieszkowski
2004; Cieszkowski et al. 2009b)
or in the Beskid Mały Mts.
(Książkiewicz 1951) clasts of
limestones are abundant. Nowak
(1957) in the Beskid Mały Mts.
(river basin of Wielka Puszcza)
from the lower part of the Godula
Beds described conglomerates and
sandstones composed mostly of
quartz and clasts of the Cieszyn
Limestone
(which
constitutes
a distal, allodapic equivalent of
the Štramberk-type limestones).
One of the best outcrops of the
Ostravice Sandstone Member lo-
cated in an abandoned quarry in
Ustroń-Poniwiec was described in
Fig. 5. The thick-bedded deposits of the Ostravice Sandstone Member in the Poniwiec Quarry
(drawing by Marek Cieszkowski).
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Fig. 6. Type I channel sequences in deposits of the Ostravice Sandstone Member in the Ustroń-Poniwiec Quarry section in the Beskid
Śląski Mts. (after Słomka 1995, slightly modified). 1 – grain size: m — mud, s — silt, fs — fine sand, c- coarse sand, g- gravel. Lithology:
2 – shale; 3 – pebbly mudstone; 4 – micritic limestone; 5 – sandstone; 6 – conglomeratic sandstone; 7 – sandy conglomerates;
8 – conglomerates; 9 – thin, ripple-laminated sandstone beds (below 3 cm); 10 – thin, laminated and massive sandstone beds (below
3 cm); 11 – parallel lamination; 12a – wavy lamination; 13 – through cross stratification; 14 – dish structures; 15 – graded bedding;
16 – shale and/or limestone clasts; 17 – flat, even sole; 18– erosional and /or loaded sole. Cycles: 19 – positive cycle; 20 – negative
(compensation) cycle; 21 – palaeocurrents directions.
some geological guidebooks. Ślączka and Kaminski (1998)
described the Lower Senonian (Turonian—Lower Campa-
nian) very thick-bedded sandstones of the lowermost part of
the Godula Beds outcropping there. They pointed out that
the large olistoliths of turbiditic deposits were derived from
the Lower Cretaceous Lhoty Beds within the Godula sand-
stones and noticed that clasts of limestones belong to the dis-
tinctive components of these sandstones. Cieszkowski
(2004) also emphasized these features of deposits visible in
the Poniwiec Quarry. The sedimentological features of the
Godula Formation were studied there by Słomka (1995). He
presented lithological and sedimentological logs of the God-
ula Beds that cropped out in the quarry, and noticed the oc-
currence of limestone clasts in sandy conglomerates.
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Fig. 7. Micrographs of calcareous clasts and bioclasts in sandstones and conglomerates of the Ostravice Sandstone Member: 1 – Echinoid
spin; sample 18. 2 – Red algae Corallinaceae (arrows); sample UP3/3. 3 – Peloidal-bioclastic grainstone; sample OI/1. 4 – Limestone
with peloids, Dasycladales algae fragments (D) and crinoid plate (C); sample OI/6. 5 – Oncoid wackstone; sample O/Po1. 6 – Ooid pack-
stone; sample OII/1. 7 – Numerous poorly rounded limestone clasts (dark clasts); sample OIII/1. 8 – Fragment of limestone with coral;
sample OII/2.
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Cieszkowski at al. (2010) stated that Ostravice Sandstone
occurs in the Ustroń-Poniwiec Quarry, but a more complete
description of it was presented by Golonka et al. (2013b),
who also stated that this quarry can be a good reference sec-
tion for the Ostravice Sandstone Member.
Sedimentation, sedimentological features
Deposits of the Ostravice Sandstone Member from the
Poniwiec Quarry in Ustroń are dominated by conglomeratic
sandstone facies (SC) (Słomka 1995) in which the most
common variety is medium-grained sandstone with up to
30 vol. % of pebble fraction (Fig. 6). The average size of
pebbles does not exceed 3 cm although boulders (up to
30 cm across) were also encountered. Deposits of this mem-
ber form very thick layers (locally over 5 m) with numerous
distinct amalgamation surfaces. The bottoms of the layers
are erosional or deformational whereas the tops are flat or
wavy. The pebble fraction always accumulates close to the
bottoms of the layers. Up the sequence, pebbles can form
thin lenses or streaks (sSC subfacies – bedded conglomeratic
sandstones) or are randomly scattered within the framework
(mSC subfacies – massive conglomeratic sandstones).
The roundness of pebbles is variable but sub-rounded grains
predominate. In some layers, perfect examples of blow-type
and droplet-type structures can be encountered. The con-
glomeratic sandstones facies is accompanied by sandstone
facies (S), which shows very thick or thick layers with flat
bottom surfaces. Blurred load casts are also present. The
sandstone facies (S) includes two subfacies: massive sand-
stones (mS) and massive sandstones with bowl-types struc-
tures (mqS). Medium-bedded sandy conglomerates facies
(CS) and sandstones with mudstones facies (SM) are rather
scarce (Słomka 1995).
In the bottom part of the Ostravice Sandstone Member
succession an olistolith can be observed as a few-metres-
thick sliding wedge of mudstones with sandstones (MS fa-
cies) of the Lhoty Formation jammed within the Ostravice
Sandstone Member (cf. Słomka 1995).
The mining operations carried on in the Obłaziec Quarry
exposed a diverse succession of the Godula Formation
(Fig. 8). In its bottom part several-metres-thick SM facies
(sandstones with mudstones) can be observed. These are
fine-, rarely medium-grained sandstones with graded bed-
ding and parallel lamination. Sandstone beds show flat bot-
tom and top surfaces. Thin interbeds of mudstones, thin to
medium beds of micritic limestones with locally developed,
poorly visible parallel laminations as well as very thin len-
soidal intercalations of cross-laminated sandstones are com-
mon. Up the sequence, we observe very thick- to thick-
bedded conglomeratic sandstones with a total thickness of
nearly 40 metres. The qSC subfacies (conglomeratic sand-
stones with graded bedding) predominates (Słomka 1995),
accompanied by the less frequent gLSC subfacies (conglo-
meratic sandstones with graded bedding transitional to lami-
nated sandstones) and by thick-bedded, medium-grained,
massive sandstones. The conglomeratic sandstones grade
upward into a 4-metres-thick layer of SM facies (sandstones
with mudstones). These are medium- to thick-grained (pebbles
up to 50 cm across) sandstones with graded bedding, fol-
lowed upward by laminated sandstones and less common
diagonally bedded sandstones. Shale interbeds host lensoidal
bodies of very fine-grained sandstones with ripplemarks.
Up the sequence, the amount of shales increases.
Both successions described above represent the bottom
portion of the Godula Formation in the Beskid Śląski Mts.
These are typical channel sequences of the internal fan
(Słomka 1995) developed as: thick and very thick layers of
conglomeratic sandstones (SC facies), and massive sand-
stones (MS facies) accompanied by sandy conglomerates
(CS facies) and sandstones with mudstones (SM facies,
known only from the top part of the sequence). The upward-
decreasing thickness of layers and grain size of sediments
is clearly visible (Shanmugam & Moiola 1988; Słomka
1995).
Petrology
Thin-section investigations from samples taken from de-
posits of the Ostravice Sandstone Member reveal composi-
tion and sedimentary microstructures. Detrital material is
texturally immature. The sizes of grains vary over a wide
extent from 0.2 to 20 mm (extremely up to 10 cm). The ma-
jority of large clasts of the gravel fraction are poorly to well-
rounded, whereas the background (grain size 0.5 mm in
ave-rage) consists of angular grains. The sandy fraction
framework consists of: quartz occurring as singular grains
and polycrystalline aggregates; feldspar, mainly altered
orthoclase, rarer plagioclase; mica (mainly muscovite plus
minor amounts of biotite); glauconite; heavy minerals
(abraded grains and euhedral crystals of rutile, tourmaline,
zircon) (Fig. 9).
Gravel-sized grains appear separately, dispersed by finer
material. There are quartz mono- and polycrystalline and
pieces of rocks (intrusive and extrusive igneous rocks, meta-
morphic schists and gneisses as well as sedimentary rocks,
e.g. sandstones, mudstones, cherts, limestones, and coal).
Matrix occurs in minor amounts within interstitial spaces
between the framework grains. Occasionally it is ferric.
Detritus is cemented by crystalline calcite, which corrodes
grain surfaces.
Granites are phaneritic, medium-grained rocks consisting
of ca. 70 % alkali feldspar, 25 % quartz, and minor amounts
of biotite. The feldspar grains tend to be between 0.5—1 mm
in size on average. They occur generally as colourless anhe-
dral grains. Dusty alteration is visible. Orthoclases damaged
by speckled sericite replacement represent the majority of
feldspars. Only minor amounts of albite have been observed
as discrete twinned grains. The quartz is clear and unaltered
with sweeping extinction under crossed nicols. The quartz
grains tend to be between 1—3 mm in size on average, though
smaller grains are common, often aggregated. The quartz
grains have anhedral habit. There are intergrowths with the
orthoclase grains. The biotite is brown with single cleavage.
It shows subhedral flaky habit. Numerous dark spots in
biotite, called pleochroic haloes, are developed around small
zircon inclusions. Chlorite represents a common product of
biotite alteration.
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Strongly altered basalt reveals an amygdaloidal structure
(Fig. 9). The matrix originally composed of augite, plagio-
clase, and olivine is entirely changed. Olivine is replaced by
serpentine with admixture of iron ores and chalcedony,
which in turn are replaced by carbonates. Vesicles are filled
with chlorite, quartz, chalcedony and calcite.
Another type of extrusive igneous rocks is characterized
by well-developed trachytic structure. Parallel lying feldspar
plates (1 mm length) are embodied in the feebly developed
matrix, consisting of the plagioclase mixed with quartz and
pyroxene (often replaced by chlorite). Hematite occurs as
reddish pigment.
The metamorphic rock assemblage contains quartzite,
schists and gneisses (Fig. 9). Quartzitic rocks reveal grano-
blastic or porphyroblastic structure. The parallel texture is
due to more abundant biotite, dispersed in bands or lenticular
quartz aggregates enveloped by fine-grained quartz. Mica
schists are a medium grained rock of homeoblastic and thin
schistose structure. The rock is composed of quartz, biotite,
and rarer muscovite. Quartz is xenoblastic and usually flat-
tened. Micas are present in thin flakes and parallel aggre-
gates, arranged separately or in layers often wavy deformed.
Sericite-chlorite schists are fine-grained, phyllitic rocks. Por-
phyroblasts of plagioclase are enveloped by chlorite-sericite
or quartz-albite aggregate. Gneisses are medium-grained,
heteroblastic rocks, of intermediate texture between massive
and schistose. Biotite, which does not form continuous layers,
is corroded and intergrown with muscovite. Orthoclase occurs
in somewhat larger grains. Quartz shows cataclasis.
Sedimentary rock clasts are represented by the following
lithotypes: fine-grained, quartzitic sandstones; dark, non-
calcareous mudstones; clayey shales; cherts composed of
chalcedony stuff with recrystallized, circular tests (radiolarian,
sponge) therein; limestones. Sandstones and shales represent
recycled turbiditic deposits.
Carbonate clasts
Fragments of light coloured limestones constitute the most
characteristic component of deposits of the Ostravice Sand-
stone Member (Figs. 3, 4, 7). The carbonate clasts were studied
in detail in thin sections. The analysed clasts are poorly
rounded and measure from less than 1 mm to several centi-
metres, mostly 1—5 mm.
It is possible to recognize such types of limestones as bio-
clastic wackstone, oncoid wackstone, bioclastic-peloid
wackstone and packstone, peloid packstone, peloid-bioclas-
tic grainstone, ooid grainstone, ooid-bioclastic grainstone, li-
thoclastic-bioclastic grainstone. Boundstone microfacies are
difficult to state with regard to the small size of limestone
fragments, but a lot of calcareous clasts that could constitute
fragments of microbial deposits were observed. Fragments
of calcareous sponges and corals are also found, which may
indicate the presence of some reefs formed by these groups
of organisms in the source area. These limestones represent
diversified deposits of the inner carbonate platform, platform
margin, slope of platform, and probably also deeper shelf.
Identified fossils indicate the latest Jurassic—earliest Creta-
ceous (mainly Tithonian-Berriasian) age of the limestones
(Kowal et al. 2011). The most important for the age determi-
nation are calpionellids, most of which are poorly preserved,
but some can be precisely identified: Calpionella alpina
Lorenz (Fig. 10.1), Calpionella elliptica Cadisch (Fig. 10.2),
Crassicollaria parvula Remane (Fig. 10.3), Calpionellopsis
oblonga (Cadisch) (Fig. 10.4), Tintinnopsella carpathica
(Murgeanu et Filipescu) (Fig. 10.5). Foraminifera occurring
in these clasts are mostly typical for the carbonate platform
environments, and are known from the Štramberk-type lime-
stones, as well as from the Cieszyn Limestone Formation
(e.g. Olszewska 2005; Ivanova & Kołodziej 2010). Among
them miliolids are the most common (e.g. Moesiloculina cf.
histri (Neagu) (Fig. 10.6), Ophthalmidium sp., Rumanolocu-
lina sp.), as well as foraminifera of the genus Andersenolina,
especially Andersenolina alpina (Leupold) (Fig. 10.7),
Andersenolina elongata (Leupold) (Fig. 10.8), Anderseno-
lina delphinensis (Arnaud-Vanneau, Boisseau & Darsac)
(Fig. 10.9). Other important foraminiferal taxons recognized
in the thin sections are: Mohlerina basiliensis (Mohler)
(Fig. 10.10), Protopeneroplis ultragranulata (Gorbatchik)
(Fig. 10.11), Troglotella incrustans Wernli & Fookes
(Fig. 10.12), Haghimashella arcuata (Haeusler), Uvigeri-
nammina uvigeriniformis (Seibold & Seibold) (Fig. 10.13),
Fig. 8. Type I channel sequences in deposits of the Ostravice Sand-
stone Member in the Wisła-Obłaziec Quarry section in the Beskid
Śląski Mts. (after Słomka 1995, slightly modified). Explanation like
in Fig. 6.
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and foraminifera of the genera Arenobulimina, Bullopora,
Dobrogelina, Gaudryina, Glomospira, Lenticulina, Melath-
rokerion, Nautiloculina, Neotrocholina, Paleogaudryina,
Reophax, Spirillina, Trocholina, Textularia. In some clasts
calcareous dinoflagellate cysts were noticed: Colomisphaera
minutissima (Colom), Committosphaera ornata (Nowak)
(Fig. 10.14), Cadosina fusca fusca Wanner (Fig. 10.15),
Crustocadosina
semiradiata
semiradiata
(Wanner)
(Fig. 10.16), Colomisphaera sp. In the thin sections, other
microfossils typical for the Upper Jurassic and Lower Creta-
ceous deposits of carbonate platforms and slopes of plat-
forms also appear: Crescentiella morronensis (Crescenti) –
a very common microfossil, recently interpreted as nubecu-
larid foraminifera incrusted by cyanobacteria (Senowbari-
Daryan et al. 2008); Globochaete alpina Lombard –
planktonic green alga; problematic alga Thaumathoporella
parvovesiculifera (Raineri); polychaetes Terebella lapil-
loides Münster; microproblematica Koskinobulina socialis
Cherchi et Schroeder; “Bacinellid” fabric. Fragments of
macrofossils occur in many clasts, especially fragments of
calcareous green algae of the order Dasycladales, bryozoan
colonies, brachiopods, bivalves, calcareous sponges, and
corals. Moreover spines of siliceous sponges, radiolarians,
calcimicrobes, echinoderms elements, shells of gastropods,
and ostracods were noticed.
The age, fossils, and microfacies of the studied limestone
clasts indicate that they correspond to the Upper Jurassic—
Lower Cretaceous exotic limestones, mostly shallow-water,
platform deposits – so-called Štramberk-type limestones,
which commonly occur in deposits of the Outer Carpathians
(see e.g. Książkiewicz 1951; Morycowa 1968; Cieszkowski
1992; Kołodziej 2015) and are compared with the Štramberk
Limestone from Moravia (Czech Republic) (e.g. Eliáš &
Eliášová 1984). Clasts of mudstones, often with calpionel-
lids probably represent deeper facies of the latest Jurassic
and earliest Cretaceous.
Age
The Ostravice Sandstone Member occurs in the lowermost
part of the Godula Formation. The sedimentation of the
Lower Godula Beds started from the Early Turonian (e.g.
Nowak 1963; Bieda et al. 1963; Geroch et al. 1967; Koszarski
& Ślączka 1973; Hanzlíková 1973; Menčík et al. 1983;
Słomka 1995; Olszewska 1997 and references therein), only
its eastern part was connected with the early Senonian
(Słomka 1995). The foraminiferal assemblages from the
Ostravice Sandstone Member are usually very poor, but in
some samples they are stratigraphically diagnostic and indi-
cate the Turonian Uvigerinammina jankoi biozone (zone
after Geroch & Nowak 1984; Olszewska 1997). The occur-
rence of the index taxon Uvigerinammina jankoi Majzon in
the Carpathians is estimated to the Turonian—Campanian
range (e.g. Geroch & Nowak 1984; Olszewska 1997 and refe-
rences therein) and is recently observed even in the Cenoma-
nian. The lower boundary of the Ostravice Sandstone Member
is synonymous with the age of the directly underlying the Bar-
nasiówka Radiolarian Shale Formation. Bąk et al. (2001 and
references therein), according to the integrating radiolarian
and foraminiferal data, indicated the earliest Turonian age of
the uppermost part of the Barnasiówka Formation. The
radiolarian assemblages have been classified to the lower
part of the Alievium superbum zone (biozone after
O’Dogherty 1994), while in the foraminiferal assemblages
the first appearance of Uvigerinammina jankoi Majzon was
noticed (Bąk et al., 2001).
The sedimentation of the deposits of the Ostravice Sand-
stone Member probably took place only in the Turonian. The
preliminary results from the poor foraminiferal assemblages
derived from the upper part of this member are not strati-
graphically diagnostic. The occurrence of single specimens
of Uvigerinammina jankoi Majzon is noticed here. On the
basis of micropalaeontological analysis Słomka (1995) sug-
gested the Turonian or possibly Turonian—Coniacian age for
the overlying Middle Godula Beds. Thus, the superposition
of the Lower Godula Beds, containing in their lower part the
Ostravice Sandstone Member, indicates the Turonian age.
This aspect is now being studied in detail.
Studied locations
Moravskoslezské Beskydy Mountains
In the Moravskoslezské Beskydy Mts. the Godula Forma-
tion reaches record thicknesses of up to 2500 m or even more
than 3000 m (Eliáš 1979). It is underlain by the variegated
shales of the Mazák Formation. The Ostravice Sandstone
Member makes up the basal, several dozen metres thick part
of the Godula Formation. The sandstone layers are thick,
usually 2—4 m, intercalated occasionally with thin- or medium-
bedded glauconitic fine-grained sandstones and grey non-
calcareous shales. Sandstones are coarse-grained or
conglomeratic, rich in clasts of limestones, so that they partly
represent a kind of sedimentary breccia. A representative
outcrop of the Mazák Formation and the Ostravice Sand-
stone Member is exposed in the Mazák Quarry in Ostravice
village (Roth 1980). Pieces of magmatic rocks typical for the
teschenite association, black cherts, and clasts of shales tens
of centimetres in size typical for the Lower Cretaceous Hra-
dište Formation, were found within the sandstones. These
clasts include the Early Cretaceous fauna (Foldyna & Šuf
1964) with Lamellaptychus didayi (Coquand), Salfeldiella
cf. guettardi (Raspail), aucellids shells, juvenile forms of
snails, as well as flora Zamites göpperti Schenk, Baiera cf.
cretosa Schenk. Turbidites consisting of thin- and medium-
Fig. 9. Microstructures of coarse-grained sandstones and conglomerates of the Ostravice Sandstone Member. 1—4 – Texturally immature
conglomerate, clasts of gravel fraction are rounded, grains of psammite are angular. Matrix fills up interstitial spaces of the framework.
5—6 – Clast of altered mafic volcanic rock with amygdaloidal structure. 7 – Quartzitic arenite with corrosive carbonate cement.
8 – Clast of trachyte. 9 – Granite exotic. Images under crossed nicols, excluding 6 taken using parallel nicols, transmitted light.
Abbreviations (after Whitney and Evans, 2010): Ab — albite, Bt — biotite, Cb — carbonate minerals, Chl — chlorite, Glt — glauconite,
Kfs — K feldspar, Qz — quartz, Qz — fibrous quartz = chalcedony, Srp — serpentinite.
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Fig. 10. Micrographs of selected microfossils from clasts of the Upper Jurassic and Lower Cretaceous limestones: 1 – Calpionella alpina
Lorenz; sample O/Po2. 2 – Calpionella elliptica Cadisch; sample OIV/1. 3 – Crassicollaria parvula Remane; sample OI/8. 4 – Calpio-
nellopsis oblonga (Cadisch); sample OIV/1. 5 – Tintinnopsella carpathica (Murgeanu & Filipescu); sample OIV/1. 6 – Moesiloculina cf.
histri (Neagu); sample OII/1. 7 – Andersenolina alpina (Leupold); sample OIV/1. 8 – Andersenolina elongata (Leupold); sample O/Br.
9 – Andersenolina delphinensis (Arnaud-Vanneau, Boisseau & Darsac); sample O/Br. 10 – Mohlerina basiliensis (Mohler); sample O/Br.
11 – Protopeneroplis ultragranulata (Gorbatchik); sample O/PoB. 12 – Troglotella incrustans Wernli & Fookes; sample O/Po1.
13 – Uvigerinammina uvigeriniformis (Seibold & Seibold); sample OV/1. 14 – Committosphaera ornata (Nowak); sample OI/5.
15 – Cadosina fusca fusca Wanner; sample O/Po2. 16 – Crustocadosina semiradiata semiradiata (Wanner); sample O/Po2.
The name “Mazák Formation” was taken from the Mazák
Quarry but this quarry is also important as a part of the typical
(stratotype) exposures of the Ostravice Sandstone Member.
Beskid Śląski (Slezské Beskydy) Mountains.
In the Beskid Śląski (Slezské Beskydy) Mts. the Godula
Formation reaches the thickness of up to 2500 m or more.
bedded glauconitic sandstones and grey shales typical for the
Godula Formation occur above the Ostravice Sandstone
Member. In some publications (e.g. Roth 1980; Picha et al
2006) the Ostravice Sandstone was described as a member
within the Mazák Formation, but others claim that this sand-
stone is directly overlaid by shaly-sandstone turbidites typi-
cal for the Godula Formation.
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Here the Godula beds were first described in details by Bur-
tanówna et al. (1937), and then divided into three parts:
Lower, Middle, and Upper Godula beds and included in the
Godula Formation created firstly in the Silesian part of the
Carpathians as the Godula Beds (cf. Unrug 1969; Burtan
1973; Nowak 1973). Golonka et al. (2013a) following Bur-
tan (1973), Wójcik et al. (1996) and Cieszkowski et al.
(2010) proposed a new formal lithostratigraphy of the Godula
Formation with a few lithostratigraphic members (see
above). In the Beskid Śląski (Slezské Beskydy) Mts. the Os-
travice Sandstone Member is exposed in the northern foot-
hills of this mountain range in Nýdek, Ustroń, Brenna, and
the southern suburbs of Bielsko-Biala. It lies directly on the
top of the Lhoty Formation and is covered by the shaly-sand-
stone Czernichów Member. The variegated shales of the
Mazák Formation have not been noticed at its base there.
The Ostravice Sandstone Member is well outcropped in the
Ustroń-Poniwiec abandoned quarry and its surroundings
(Figs 4, 5, 6). Now this position is proposed as a parastrato-
type of the discussed member (Golonka et al. 2013a, b). In
that place coarse-grained and conglomeratic sandstones as
well as conglomerates are rich in clasts of carbonate rocks
dominated by the Štramberk-type limestones. Clast dimen-
sions range from a few millimetres up to several centimetres,
and the largest are more than 20 cm in size (Ślączka & Ka-
minski 1998; Cieszkowski 2004; Cieszkowski at al. 2009a, b).
Large olistoliths of the deposits represented by the Lhoty
and Verovice formations are exposed within the thick- and
very thick-bedded sandstones (Ślączka & Kaminski 1998;
Cieszkowski 2004; Cieszkowski at al. 2009a,b; Golonka et
al. 2013b).
Beskid Mały Mountains
In the Beskid Mały Mts. the Godula Formation is up to
1500 m thick (Słomka 1995) or more in the western part.
The Ostravice Sandstone Member is found in the western
part of this mountain ridge in the basal part of the Godula
Formation. Sedimentation of the Godula Formation began
there with a complex of thick- and very thick-bedded sand-
stones. In some places they overlie variegated shales of the
Mazák Formation. In the eastern part of the Beskid Mały
Mts. the Ostravice Sandstone Member has not been found.
A thin level of variegated shales and a complex of calcitur-
bidites, described by Książkiewicz (1951) as siliceous marls
Turonian—Coniacian in age, called the Kaczyna Marls occurs
there at the base of the Godula Formation (cf. Cieszkowski
et al. 2001, 2003; Uchman & Cieszkowski 2008). Thick-
bedded sandstones without clasts of carbonates occur in the
lower part of the Godula Formation in the section at Rzyki
village overlying a shaly complex several tens of metres
thick. Small outcrops of deposits typical for this member ap-
pear in the Puszcza Wielka stream at Porąbka village
(Fig. 3.6).
Rożnów Foothills
In the Rożnów Foothills, the Ostravice Sandstone Member
was noticed in Czchów and its surroundings in the southern
limb of the Czchów Anticline. The Godula Formation is up
to 800 m or more thick there (Cieszkowski 1992). Its base
consists of a several tens of metres thick complex of the Os-
travice Sandstone Member Sandstones rich in carbonate
clasts. The biggest clasts reach up to 10 cm or even occa-
sionally 15 cm. Thin- or medium-bedded shaly-sandstone
turbidites are developed above the Ostravice Sandstone
Member. In the uppermost part of the section thick-bedded,
coarse-grained or conglomeratic sandstones that steeply pass
into the thick-bedded sandstones of the Istebna Formation
arrive. The Godula Formation is underlain by red shales of
the Mazák Formation. Red or variegated shales form occa-
sionally thin intercalations within the Godula Formation.
The sandstones of the discussed member were used in the
Middle Ages to build some Gothic buildings in Czchów
town. It is possible to see them in the walls of the defensive
tower, which is located on a small hill composed of the Os-
travice Sandstone, and the walls of the Gothic church in the
town centre. Clasts of the Štramberk-type limestones from
a few millimetres up to 12 cm, as well as separate algal frag-
ments, pieces of corrals or echinoids can be seen in the sand-
stones used in walls. Part of the market is also paved with
slabs of these sandstones. It is interesting that the presence of
deposits from the Ostravice Sandstone Member in Czchów
was first noticed in the walls, and following these findings,
the authors (Waśkowska and Cieszkowski) started looking
for them in the field.
Ciężkowice Foothill
The easternmost locality of the Ostravice Sandstone Mem-
ber was noticed east of the Biała Dunajcowa River. The
sandstone crops out here in the core of the Rzepienniki Anti-
cline in the surroundings of Gromnik village and in the
Brzanka-Liwocz Anicline in the surroundings of Ryglice vil-
lage. The cores of these anticlines are composed of deposits
of the Mazák and Godula formations and limbs of the Istebna,
Ciężkowice, Hieroglyphic, and Krosno formations. The
Godula Formation is developed here as thin- and medium-
bedded glauconitic sandstones and grey shales passing up
the section to the medium- and thick-bedded sandstones and
shales. At the top of the section, thick-bedded, coarse-
grained, and conglomeratic sandstones occur. They are
somewhat similar to the Istebna sandstone facies, but with
noticeable amounts of glauconite. Thick-bedded, conglome-
ratic sandstones of the Ostravice Sandstone Member rich in
carbonate clasts occur at the base of this complex. The Godula
Formation is underlain by red shales of the Mazák Forma-
tion, but interbeddings of variegated shales also occur within
the middle part and top of the section. The thickness of the
Godula Formation in the Rzepienniki Anticline is estimated
as 200—250 m and in Brzanka—Liwocz up to 400 m.
Discussion
The Ostravice Sandstone has been known as a lithostrati-
graphic unit of the Silesian Nappe since 1933 (Andrusov
1933), and later was commonly used by Czech geologists in
the area of the Moravskoslezské Beskydy Mts., the West Outer
Carpathians in the Czech Republic (e.g. Matějka & Roth
1949; Roth et al. 1962; Andrusov & Samuel 1985; Eliáš
162
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1995, 2000; Picha et al. 2006 and papers cited therein).
When describing this division, the author paid special atten-
tion to its lithological development and clearly noticeable in-
dividuality among the other Upper Cretaceous deposits of
the Silesian Nappe. Then the Ostravice Sandstone was clas-
sified as a facies within the Mazák Formation (Roth 1980;
Menčík et al. 1983).
The Ostravice Sandstone also occurs in the Polish sector
of the Outer Carpathians and belongs to the same lithosome
as that known from the Moravskoslezské Beskydy Mts. The
lithostratigraphic position, age, lithology, mineral composi-
tion, and sedimentological features of these deposits are the
same in the Czech Republic and Poland. Their lithological
features clearly distinguish this unit from the other sand-
stones of the Godula Formation. This observation was ini-
tially provided by Słomka (1995). Field investigations found
that this lithotype is widespread in the Polish sector of the
Outer Carpathians ad its outcrops continue eastward from the
Beskid Śląski (Slezské Beskydy) Mts. through the Beskid
Mały Mts., Wieliczka and Rożnów Foothills, several kilo-
metres east of the Biała River. Therefore, this unit has re-
gional range. Thanks to its unique diagnostic lithological
features, the Ostravice Sandstone is easy to distinguish and
map out. These thick-bedded sandstone deposits represent
a characteristic sandstone lithotype rich in carbonate rocks
clasts mainly of the Štramberk-type. They form the sand-
stone complex in the lowermost part of the Godula Forma-
tion with well-defined upper and lower limits. Clearly
visible diagnostic features are well-marked in both the verti-
cal and lateral directions within the Ostravice Sandstone sup-
porting the previous observations distinguishing it as
a separate lithostratigraphic unit within the Godula Formation.
Therefore, the present authors propose treating this lithologi-
cal unit as a lithostratigraphic member within the Godula
Formation. The definition and description of the proposed
member fit the rules described in the Stratigraphic Codes
(Alexandrowicz et al. 1975; Racki & Narkiewicz 2006).
The structure of the Ostravice Sandstone Member litho-
some formed by its lithostratigraphic position, petrographic
composition, and sedimentological features is important for
understanding the history of sedimentation within the Sile-
sian Basin as well as for reconstruction of the Silesian Ridge,
which was destroyed during the orogenic process in the West
Outer Carpathians. The changes of sedimentary regime,
which contributed to the origin of the Ostravice Sandstone
Member and the entire Godula Formation, began a new stage
in the Cretaceous evolution of the Carpathian basins. The
geotectonic reorganization of the Outer Carpathian basins
took place at the beginning of the Late Cretaceous. The Sile-
sian Basin sensu stricto was separated during this reorgani-
zation from the widespread proto-Silesian Basin, which
existed at least from the Late Jurassic.
Conclusions
The deposits described in the Czech Republic as the Os-
travice Sandstone of the Silesian Nappe continue eastward to
the Polish sector of the Outer Carpathians.
The authors distinguish these deposits as a lithostrati-
graphic member – the Ostravice Sandstone Member of the
Godula Formation. This member is developed in the lower-
most part of the Godula Formation. The bottom of the
Ostravice Member borders the variegated shales of the
Mazák Formation, and at the top it is overlain by the
Czernichów Member of the Godula Formation.
The Ostravice Sandstone Member is developed as thick-
bedded sandstones and conglomerates. The sandstones are
composed of quartz, glauconite, feldspar, muscovite, as well
as lithoclasts of magmatic, metamorphic and sedimentary
rocks. The presence of numerous carbonate clasts represented
mainly by the Uppermost Jurassic-Lowest Cretaceous
Štramberk-type limestones is a characteristic feature which
clearly distinguishes this member.
In general, the age of the Ostravice Sandstone Member is
estimated as Turonian.
The discussed member is widespread in the Moravsko-
slezské Beskydy Mts. in the West Outer Carpathians in the
Czech Republic and continues eastward through to the
Beskid Śląski (Slezské Beskydy) Mts. and Beskid Mały
Mts., as well as the Wieliczka, Wiśnicz, Rożnów,
Ciężkowice foothills in Poland.
Acknowledgements: Thanks are addressed to Barbara
Olszewska for helpful discussion about microfossils, as well
as to reviewers — Jacek Rajchel, Miroslav Bubík and Petr
Skupien for constructive comments on the manuscript. This
research has been financially supported by Ministry of Science
and Higher Education/National Centre of Sciences grant
no. NN307 249733, and AGH grant no. 11.11.140.173.
References
Alexandrowicz W., Birkenmajer K., Burchart J., Cieśliński S.,
Dadlez R., Kutek J., Nowak W., Orłowski S., Szulczewski M.
& Teller L. 1975: Principles of Polish stratigraphical classifi-
cation, terminology and nomenclature. Instr. i metody badań
geol. 33, 1—63 (in Polish).
Andrusov D. 1933: Brief information on geology of Moravian-Silesian
Carpathians. Věst. Stát. Geol. Úst. ČSR 9, 194—199 (in Czech).
Andrusov D. 1959. Geology of Czechoslovakian Carpathians. II.
Vyd. SAV, Bratislava, 1—375 (in Slovak with German and Rus-
sian summary).
Andrusov D. & Samuel O. (Eds) 1985: Stratigraphic dictionary of
the Western Carpathians. Part 2 L—Z. GÚDŠ, Bratislava,
1—359 (in Slovak).
Bąk K., Bąk M. & Paul Z. 2001: Barnasiówka Radiolarian Shale
Formation – a new lithostratigraphic unit in the Upper Ceno-
manian—lowermost Turonian of the Polish Outer Carpathians
(Silesian Series). Ann. Soc. Geol. Pol. 71, 2, 75—103.
Bieda F., Geroch S., Koszarski L., Książkiewicz M. & Żytko K.
1963: Stratigraphie des Carpathes externes polonaises. Bull.
Inst. Geol. 181, 5—174.
Burtan J. 1973: Explanation to detailed geological map of Poland
1:50,000. Wisła Sheet. PIG, Warszawa, 1—37.
Burtanówna J., Konior K. & Książkiewicz M. 1937: Carte
geologique des Karpates de Silesie. PAU, Wyd. Śląskie,
Kraków, 1—104 (in Polish with French summary).
Cieszkowski M. 1992: Michalczowa zone: a new unit of Fore-
Magura zone, Outer Carpathians, South Poland. Kwart. AGH
163
U. CRETACEOUS OSTRAVICE SDST IN SILESIAN NAPPE, OUTER W. CARPATHIANS
G
G
G
G
GEOL
EOL
EOL
EOL
EOLOGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPATHICA
THICA
THICA
THICA
THICA, 2016, 67, 2, 147—164
Geol. 18, 1—2, 1—125 (in Polish with English summary).
Cieszkowski M. 2003: The Outer Carpathians Thrustbelt. In:
Golonka J. & Lewandowski M. (Eds.): Geology, Geophysics,
Geothermics and Deep Structure of the West Carpathians and
their Basement. Part 3. International Workshop, Zakopane, Po-
land, 2003. Publ. of the Inst. of Geophysics, Polish Academy of
Sciences, Warszawa, Monographic vol. M-28, 363, 107—110.
Cieszkowski M. 2004: Stop 3. Ustroń, abandoned quarry. Field trip.
The 11-th Meeting of the Petrology Group of the Mineralogical
Society of Poland. Ustroń, October 14—27, 2004. Mineral. Soc.
Pol., Spec. Pap. 24, 427—428.
Cieszkowski M., Ślączka A. & Wdowiarz S. 1985: New data on struc-
ture of the Flysch Carpathians. Przegl. Geol. 33, 6, 313—333.
Cieszkowski M., Gedl E., Ślączka A. & Uchman A. 2001: Stop C2
– Rzyki village. In: Cieszkowski M. & Ślączka A. (Eds.):
Silesian & Subsilesian units. 12th Meeting of the Association
of European Geological Societies & LXXII Zjazd Polskiego
Towarzystwa Geologicznego, Field Trip Guide. PGI, Kraków,
115—118.
Cieszkowski M., Gedl E. & Uchman A. 2003: Field Trip Western
Carpathians: Kraków—Lanckorona Castle—Inwałd—Roczyny—
Rzyki—Kraków, Stop 3. Zagórnik-Rzyki villages. In: Ber A. &
Alexandrowicz Z. (Eds): Geological Heritage Concept, Con-
servation and Protection Policy in Central Europe – Interna-
tional Conference, Cracow, Poland, October 3—4, 2003.
Abstracts and Field Trip Guide-Book. PGI, Warszawa, 86—91.
Cieszkowski M., Golonka J., Krobicki M., Ślączka A., Waśkowska
A. & Wendorff M. 2009a: Olistoliths within the Silesian Series
and their connections with evolutionary stages of the Silesian
Basin. Kwart. AGH Geol. 35, 2/1, 13—21 (in Polish with En-
glish summary).
Cieszkowski M., Golonka J., Krobicki M., Ślączka A., Oszczypko
N., Waśkowska A. & Wendorff M. 2009b: The Northern Car-
pathian plate tectonic evolutionary stages and origin of olis-
tolithes and olistostromes. Geodin. Acta 22, 1—3, 101—126.
Cieszkowski M., Golonka J., Kowal J., Mika M. & Waśkowska A.
2010: Ostravice Sandstones in Poland (Outer West Car-
pathians, Silesian Nappe). ESSE-WECA Conference, Bratisla-
va, December 2—3. Miner. Slovaca 42, 4, 508.
Cieszkowki M., Kowal J. & Olszewska B. 2011: Limestone clasts
from the Upper Cretaceous Sandstones of Silesian Series
(Western Outer Carpathians, Poland) – micropaleontological
case study. In: Boorova D. (Ed.): 12. Česko-Slovensko-Po ská
Paleontologická Konferencia, Bratislava 20.—21. októbra 2011.
Zborník
príspevkov.
Konferencie—Sympózia—Semináre,
ŠGÚDŠ, Bratislava, 88—89.
Cieszkowski M., Golonka J., Kowal J., Ślączka A., Waśkowska A.
& Wendorff M. 2012a: Early Cretaceous dark shale olistholits
and Upper Jurassic—Early Cretaceous carbonate clasts as indi-
cators of activity of the Silesian Basin’s southern margin (Outer
Carpathians, Poland). In: 29
th
IAS Meeting of Sedimentology,
Schladming, Austria, 10
th
—13
th
September 2012, Abstract
book, 415.
Cieszkowski M., Golonka J., Ślączka A. & Waśkowska A. 2012b:
Role of the olistostromes and olistoliths in tectonostratigraphic
evolution of the Silesian Basin in the Outer West Carpathians.
Tectonophysics 568—569, 248—265.
Eliáš M. 1979: Facies and paleogeography of the Silesian unit in the
western part of the Czechoslovak flysch Carpathians. Věst.
Ústř. Úst. Geol. 54, 6, 327—339.
Eliáš M. 1995: Sedimentology of the Mazák Beds and the Ostravice
Sandstone (Godula Beds). Zprávy o geol. výzkumech v roce
1994, ČGS 44—45 (in Czech).
Eliáš M. 2000: Relation between Pustevny Sandstone and Mali-
novska Skala Sandstone (Godula Formation) in the Beskydy
Mts. Geol. výzkumy na Moravě a ve Slezsku v roce 1999 7,
64—66 (in Czech with English abstract).
Eliáš M. & Eliášová H. 1984: Facies and palaeogeography of the
Jurassic in the western part of the Outer Flysch Carpathians in
Czechoslovakia. Sbor. Gel. Vd, Geol. 39, 105—170.
Foldyna J. & Šuf J. 1964: A note about conglomerates in the fossil
pothole of the Ostravice layers. Sbor. Věd. Prací Vys. Školy
Báň. Ostrava 10, 1—2, 185—189 (in Czech).
Geroch S. & Nowak W. 1984: Proposal of zonation for the late Ti-
thonian-late Eocene, based upon arenaceous foraminifera from
the outer Carpathians, Poland. In: Oertli H.J. (Ed.):
Benthos’83: 2nd Symposium International Sur Les Foraminifères
Benthiques: Pau (France), 11—15/4/1983. Elf Aquitaine,
225—239.
Geroch S., Jednorowska A., Książkiewicz M. & Liszkowa J. 1967:
Stratigraphy based upon microfauna in the Western Polish
Carpathians. Biul. Inst. Geol. 211, 2, 185—282.
Golonka J. & Waśkowska-Oliwa A. 2007: Stratigraphy of the Polish
Flysch Carpathians between Bielsko-Biała and Nowy Targ.
Kwart. AGH Geol. 33, 4/1, 5—28 (in Polish with English sum-
mary).
Golonka J., Krobicki M., Matyszkiewicz J., Olszewska B., Ślączka
A. & Słomka T. 2005: Geodynamics of ridges and develop-
ment of carbonate platform within the Carpathian realm in Po-
land. Slovak Geol. Mag. 11, 5—16.
Golonka J., Gahagan L., Krobicki M., Marko F., Oszczypko N. &
Ślączka A. 2006: Plate Tectonic Evolution and Paleogeography
of the Circum-Carpathian Region. In: Golonka J. & Picha F.
(Eds.): The Carpathians and their foreland: Geology and hy-
drocarbon resources. AAPG Memoir 84, 11—46.
Golonka J., Vašíček Z., Skupien P., Waśkowska-Oliwa A., Krobic-
ki M., Cieszkowski M., Ślączka A. & Słomka T. 2008: Lito-
stratygraphy of the Upper Jurassic and Lower Creataceous
deposits of the western part of the Outer Carpathians (discus-
sion proposition). Geologia 34, 3/1, 9—31.
Golonka J., Ślączka A., Waśkowska A., Krobicki M. & Cieszkowski
M. 2013a: Geology of western part of the Outer Carpathians.
In: Krobicki M. & Feldman-Olszewska A. (Eds): Abstrakty re-
feratów i posterów. Przewodnik do wycieczek. V Polska Kon-
ferencja Sedymentologiczna POKOS 5’2013. Głębokomorska
sedymentacja fliszowa, Sedymentologiczne aspekty historii
basenów karpackich. Żywiec, 16—19.05.2013. PGI-NRI,
Warszawa, 11—62 (in Polish).
Golonka J., Cieszkowski M. & Słomka T. 2013b: Poniwiec. In:
Krobicki M. & Feldman-Olszewska A. (Eds): Abstrakty refe-
ratów i posterów. Przewodnik do wycieczek. V Polska Konfe-
rencja Sedymentologiczna POKOS 5’2013. Głębokomorska
sedymentacja fliszowa, Sedymentologiczne aspekty historii
basenów karpackich. Żywiec, 16—19.05.2013. PGI-NRI,
Warszawa, 341—345 (in Polish).
Hanzlíková E. 1973: Foraminifers of the variegated Godula Mem-
ber in Moravia (Cenomanian—Turonian). Sbor. Geol. Věd, Pa-
leont. 15, 119—184.
Ivanova D. & Kołodziej B. 2010: Late Jurassic-Early Cretaceous
foraminifera from Štramberk-type limestones, Polish Outer
Carpathians. Stud. Univ. Babes-Bolyai, Ser. Geol. 55, 2, 3—31.
Kołodziej B. 2015: Geological context and age of the Štramberk-
type limestones from the Polish Outer Carpathians: an over-
view. Neues Jahr. Geol. Paläont. Abhand. 276, 2, 173—179.
Koszarski J., Sikora W. & Wdowiarz S. 1974: The flysch Car-
pathians. In: Mahe M. (Ed.): Tectonics of the Carpathian-Bal-
kan Regions. ŠGÚDŠ, Bratislava, 180—197.
Koszarski L., Nowak W. & Żytko K. 1959: Notes on the age of the
Godula Beds (Carpathians Flysch) (preliminary report).
Kwart. Geol. 3, 1, 127—151 (in Polish with English summary).
Koszarski L. & Ślączka A. 1973: Cretaceous: Outer (Flysch) Car-
pathians. In: Sokołowski S. (Ed.): Geology of Poland, 1(2).
164
CIESZKOWSKI et al.
G
G
G
G
GEOL
EOL
EOL
EOL
EOLOGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPA
OGICA CARPATHICA
THICA
THICA
THICA
THICA, 2016, 67, 2, 147—164
Wyd. Geol., Warszawa, 647—660 (in Polish).
Kowal J., Cieszkowski M. & Olszewska B. 2011: Micropaleonto-
logical data of limestone clasts from the Upper Cretaceous Os-
travice
Sandstones
(Silesian
Nappe,
Western
Outer
Carpathians, Poland). In: Bąk M., Kaminski M.A. &
Waśkowska A. (Eds): Integrating Microfossil Records from
the Oceans and Epicontinental Seas. 8th Micropaleontological
Workshop MIKRO 2011 and Annual TMS Foram/Nanno-
plankton Group Meeting. Kraków, 27.06—30.06. 2011. AGH,
UJ. Grzybowski Found. Spec. Publ. 17, 102—103.
Książkiewicz M. 1933: Beitrag zur Kenntnis der mittleren Kreide
der Godula-Decke in den West-Karpaten. Rocz. Pol. Tow.
Geol. 9, 88—95 (in Polish with German summary).
Książkiewicz M. 1951: Explanations to the General Geological Map
of Poland 1:50,000, Wadowice Sheet. Wyd. Geol., Warszawa,
1—283 (in Polish).
Książkiewicz M. (Ed.) 1962: Geological atlas of Poland. Strati-
graphic and facial problems. Cretaceous and early Tertiary in
the Polish External Carpathians. Fasc. 13. Inst. Geol., Warszawa.
Książkiewicz M. 1965: Les cordilleres dans les mers cretaces et
paléogènes des Carpathes du Nord. Bull. Soc. Géol. France 7,
75—97.
Książkiewicz M. 1972: Geology of Poland. Vol. 4. Part 3. Car-
pathians. Wyd. Geol., Warszawa, 1—228 (in Polish).
Książkiewicz M. 1974: Detailed Geological Map of Poland
1:50,000. Sucha Beskidzka Sheet. Wyd. Geol., Warszawa (in
Polish).
Książkiewicz M. 1977: The tectonics of the Carpathians. In:
Pożaryski W. (Ed.): Geology of Poland. Vol. IV. Tectonics.
Wyd. Geol., Warszawa, 476—620.
Lexa J., Bezák V., Elečko M., Mello J., Polák M., Potfaj M. &
Vozár J. (Eds.) 2000: Geological map of the Western Car-
pathians and adjacent areas, 1:500,000. Ministry of Environ-
ment of the Slovak Repub., GSSR, Bratislava.
Mahe M. (Ed.) 1974: Tectonics of the Carpathian-Balkan Regions.
Explanations to the Tectonic Map of the Carpathian-Balkan
Regions and their Foreland. ŠGÚDŠ, Bratislava, 1—455.
Matějka A. & Roth Z. 1949: Compte rendu des levés géologiques
exécutés dans les envirous de Rožnov (Moravie orientale).
Věst. Ústř. Úst. Geol. 24. 125—130.
Menčík E. et al. 1983: Geology of the Moravskoslezské Beskydy
Mountains and Podbeskydská Pahorkatina Hilly Country.
ÚÚG, Praha, 1—304 (in Czech, with English summary).
Morycowa E. 1968: Sur les calcaires exotique a Madréporaires dans
les Lac Rożnów (Carpathes polonaises de Flysch). Ann. Soc.
Geol. Pol. 38. 19—32 (in Polish with French summary).
Nowak W. 1957: The Silesian series in the basin of the river Wielka
Puszcza (Beskid Mały, Western Carpathians). Kwart. Geol. 1,
3—4, 513—540 (in Polish with English summary).
Nowak W. 1963: The Globotruncana at the lower part of the lower
Godula sandstones in Ustroń, Śląsk Cieszyński. Kwart. Geol.
7, 4, 714—715 (in Polish with English summary).
Nowak W. 1973: Outer (Flysch) Carpathians. In: Sokołowski S.
(Ed.): Geology of Poland. Part I. Vol. 2. Mesozoic. Wyd.
Geol., Warszawa, 389—408, 464—469.
O’Dogherty L. 1994: Biochronology and paleontology of mid-Cre-
taceous radiolarians from Northern Apennines (Italy) and
Betic Cordillera (Spain). Mém. Géol. 21, 1—415.
Olszewska B. 1997: Foraminiferal biostratigraphy of the Polish
Outer Carpathians: a record of basin geohistory. Ann. Soc.
Geol. Pol. 67, 2—3, 325—337.
Olszewska B. 2005: Microfossils of the Cieszyn Beds (Silesian
Unit, Polish Outer Carpathians) – a thin section study. PGI
Spec. Pap. 19, 1—58.
Picha F.J., Stranik Z. & Krejčí O. 2006: Geology and Hydrocarbon
Resources of the Outer Western Carpathians and Their Fore-
land, Czech Republic. In: Golonka J. & Picha F.J. (Eds): Car-
pathians and Their Foreland: Geology and Hydrocarbon Re-
sources. AAPG Memoir 84, 49—175.
Racki G. & Narkiewicz M. (Eds.) 2006: Polish principles of stra-
tigraphy. PIG, Warszawa, 1—77 (in Polish).
Roth Z. et al. 1962: Explanation to the Synoptic Geological Map of
ČSSR 1:200,000, M-34-XIX, Ostrava. ÚÚG, Praha, 1—292 (in
Czech).
Roth Z. 1980: The stratigraphy of the Godula Group of the Moravsko-
slezske Beskydy Mountains in the light of deep boreholes.
Věst. Ústř. Úst. Geol. 55, 2, 75—84 (in Czech with English
summary).
Roth Z. & Matějka A. 1953: The pelosiderites of the Moravosile-
sian Beskydy, their historical importance, geological occur-
rence, petrographical and chemical nature, and their origin.
Geotechnika 16, 1—110 (in Czech with English summary).
Senowbari-Daryan B., Bucur I.I., Schlagintweit F., Săsăran E. &
Matyszkiewicz J. 2008: Crescentiella, a new name for “Tubi-
phytes” morronensis CRESCENTI, 1969: an enigmatic Juras-
sic—Cretaceous microfossil. Geol. Croat. 61, 2—3, 185—214.
Shanmugam G. & Moiola R.J. 1988: Submarine fans: characteris-
tics, models, classification, and reservoir potential. Earth Sci.
Rev. 24, 6, 383—428.
Skupien P. & Mohamed O. 2008: Campanian to maastrichtian pa-
lynofacies and dinoflagellate cysts of the Silesian Unit, Outer
Western Carpathians, Czech Republic. Bull. Geosci. 83, 2,
207—224.
Słomka T. 1995: Deep-marine siliciclastic sedimentation of the
Godula Beds, Carpathians. Prace Geol. PAN, Kraków 139,
1—132 (in Polish with English extend summary).
Ślączka A. 1959: Stratigraphy of the Silesian series of the Bystre
slice (to the South of Baligród). Biul. Inst. Geol. 131, 202—260
(in Polish with English summary).
Ślączka A. (Ed.) 1986: Atlas of paleotransport of detrital sediments
in the Carpathian-Balkan Mountain System. Part II: Cenoma-
nian-Senonian. Hung. Geol. Inst., Budapest.
Ślączka A. & Kaminski M.A. 1998: A guidebook to excursions in
the Polish Flysch Carpathians. Grzybowski Found. Spec. Publ.
6, 1—171.
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.
Uchman A. & Cieszkowski M. 2008: Stop 2 – Rzyki – Siliceous
Marl and lowermost part of the Godula Beds: ichnology of the
calcareous turbidites. Post-Congress field trip B – the Car-
pathian Flysch. In: Pieńkowski G. & Uchman A. (Eds): Ichno-
logical sites of Poland, the Holly Cross Mountains and the
Carpathian Flysch. The Pre-Congres and Post-Congres Field
Trip Guide Book. The Second International Congress of Ich-
nology, Cracow, Poland, August 29—September 8, 2008. PGI,
104—109.
Unrug R. (Ed.) 1969: Geological guidebook to the western Flysch
Carpathians. Wyd. Geol., Warszawa, 1—260 (in Polish).
Wójcik A., Kopciowski R., Malata T., Marciniec P. & Nescieruk P.
1996: Proposition of the division of lithostratigrapthic units of
the Polish Outer Carpathians. In: Przewodnik 57 Zjazdu Pol.
Tow. Geol., Szczyrk, 6—9 czerwca 1996. PTG, Kraków,
209—215 (in Polish).
Żytko K., Zając R., Gucik S., Ryłko W., Oszczypko N., Garlicka I.,
Nemčok J., Eliáš M., Menčík E. & Stráník 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. PIG, Warszawa.