GeolCarp_Vol67_No2_147

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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

, ANNA WAŚKOWSKA

, JUSTYNA KOWAL-KASPRZYK

JAN GOLONKA

, TADEUSZ SŁOMKA

, ANDRZEJ ŚLĄCZKA

, PATRYCJA WÓJCIK-TABOL

and RAFAŁ CHODYŃ

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

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. 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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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

(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.

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