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, FEBRUARY 2014, 65, 1, 35—54 doi: 10.2478/geoca-2014-0003
Introduction
As part of a program to study the geodynamic of ridges
(Golonka et al. 2005b) within the Outer Carpathians in south-
ern Poland and adjacent countries, we have undertaken a new
study of the Goryczkowiec Sandstone. Generally these sand-
stones are associated with intrabasinal uplifts. Carbonate fa-
cies developed in the upper parts of the ridges while the slopes
were dominated by flysch deposition. The number and config-
uration of the ridges within the Outer Carpathian basins
changed over time. The uplifts were subjects of intense geody-
namic evolution (Golonka et al. 2005b; Cieszkowski et al.
2009a, 2011). The present-day Outer Carpathians were reor-
ganized tectonically by the Miocene Alpine movements, and
the ridges were largely destroyed. Their original existence is
recorded by the sedimentary rocks deposited on uplifted
slopes and within the basins. The Goryczkowiec Sandstone
represents uplift-slope deposits classified recently as part of
the Subsilesian Unit inventory. The available lithological ma-
terial is limited by isolated surface outcrops; nevertheless the
sandstone provides an important and valuable record of the
Paleocene phase of the evolution of the Subsilesian Ridge
within the Outer Carpathian basins. The Goryczkowiec Sand-
stone belongs to the flysch deposits rich in redeposited mate-
rial represented by crystalline rocks as well as by calcareous
fragments, which document paleoenvironmental conditions in
the shallower part of the ridge. The purpose of this paper is to
determine the paleogeographical position of this ridge within
the Outer Carpathian flysch. We also clarify the ambivalence
Paleocene sedimentary record of ridge geodynamics in Outer
Carpathian basins (Subsilesian Unit)
ANNA WAŚKOWSKA
1
, MAREK CIESZKOWSKI
2
, JAN GOLONKA
1
and
JUSTYNA KOWAL-KASPRZYK
2
1
AGH University of Science and Technology, Faculty of Geology, Geophysics and Environmental Protection, Al. Mickiewicza 30,
30-059 Kraków, Poland; waskowsk@agh.edu.pl; jgolonka@agh.edu.pl
2
Jagiellonian University, Institute of Geological Sciences, Oleandry 2a, 30-063 Kraków, Poland;
marek.cieszkowski@uj.edu.pl; justyna.kowal@uj.edu.pl
(Manuscript received March 7, 2013; accepted in revised form October 16, 2013)
Abstract: The stratigraphic position of the Goryczkowiec Sandstone reflects the Paleocene ridge geodynamics in the
Outer Carpathian basins. The Goryczkowiec Sandstone was deposited on the slope of a ridge, known as the Subsilesian
Sedimentary Area that originated during reorganization of the Outer Carpathian realm. A Paleocene age of this sand-
stone, documented clearly by autochthonous foraminiferal and algal assemblages indicates the time of the final forma-
tion of the Subsilesian Ridge. Abundant calcareous material of biogenic origin was transported by turbidity currents
into deeper zones. This material includes fragments of carbonate buildups represented by algae, bryozoans and other
organisms growing in the shallower part of the ridge. The Goryczkowiec Sandstone, previously known as the Szydłowiec
Sandstone, is here redefined as a new lithostratigraphic unit within the Subsilesian Sedimentary Area in the marginal
Outer Carpathians in Poland. The new name clarifies the ambivalence in the lithostratigraphic nomenclature.
Key words: Paleocene, Outer Carpathians, Subsilesian Sedimentary Area, paleoenvironmental study, stratigraphy, red
algae, foraminifera.
in the lithostratigraphic nomenclature investigating the litho-
and chronostratigraphy of the ridge deposits.
Outline of geology of the study area
The Polish Outer Carpathians form a complex structure
built from Upper Jurassic—Neogene flysch deposits that are
strongly imbricated due to thrusting (Limanowski 1905;
Ślączka et al. 2006). The Outer Carpathian nappes are thrust
over the southern part of the North European Platform which
is covered by autochthonous Miocene deposits of the Car-
pathian Foredeep for a distance of at least 70 km. The north-
ern Carpathian nappes became uprooted from the basement
during their overthrusting movement and only their basinal
parts were preserved. The following Outer Carpathian
nappes have been distinguished: the Magura Nappe, Fore-
Magura group of nappes, Silesian, Subsilesian and Skole
Nappes (Fig. 1). The Subsilesian Nappe was distinguished
by Książkiewicz (1951a,b) in the Wadowice area. It under-
lies tectonically the Silesian Nappe. In the western sector of
the Western Carpathians both nappes are thrust over the Mio-
cene molasse of the Carpathian Foredeep and in the eastern
sector they are thrust over the Skole Nappe (Ksiązkiewicz
1972, 1977; Golonka et al. 2005a; Ślączka et al. 2006). The
presence of the Subsilesian Nappe was also confirmed in nu-
merous boreholes beneath the Silesian and the Magura
Nappes (Fig. 2). On the surface it is usually exposed within
tectonic windows, connected with the border zone of the
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Fig. 1. Location of study area on a tectonic sketch-map of the Western Carpathians in Poland (map after Lexa et al. 2000). 1 – Wadowice
area with stratotype locality; 2 – Gościbia Tectonic Window; 3 – Wiśniowa Tectonic Window.
Fig. 2. Cross-section through the Outer Carpathians and their foreland (map after Golonka et al. 2011, modified) (cross-line on Fig. 1).
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Silesian Nappe. In the Western Carpathians, along the thrust
zone of the Magura Nappe over the Silesian Nappe, it forms a
long and discontinuous belt with outcrops of the Subsilesian
rocks, known as the Lanckorona-Żegocina Zone. The zone
consists of small tectonic windows in different configura-
tions. A large tectonic window known as the Wiśniowa Tec-
tonic Window is located south of Kraków, another one in the
west, in the Żywiec area. Between Żywiec and Wadowice,
stone was also observed by Burtan (1974, 1978) in the Sub-
silesian Unit cropping out in the Wiśniowa and Skrzydlna
Tectonic Windows, ESE of Myślenice and in the west in the
Żywiec Tectonic Window (Geroch & Gradziński 1955).
Książkiewicz (1951a,b, 1953, 1972, 1977) also stated that the
Szydłowiec and Gorzeń Sandstones in Wadowice area form a
separate tectonic structure, and called it the Szydłowiec scale
(thrust-sheet), a different tectonic element of the Silesian Unit.
Fig. 3. A, B – tectonic sketch-maps of: A – Sułkowice Area (after Burtan 1966 and Burtan &
Szymakowska 1966, simplified), B – Wiśniowa Tectonic Window (after Burtan 1974, simpli-
fied); C, D – sampled sections.
surface exposures of Subsilesian
deposits disappear (Książkiewicz
1951a,b, 1972, 1977; Geroch &
Gradziński 1955; Burtan 1974,
1978; Cieszkowski et al. 2001;
Leśniak et al. 2001). The position
of the Subsilesian outcrops con-
nected with the northern border of
the Silesian Nappe is uncertain, and
constitutes a subject of discussion.
In many cases, deposits of mixed
character occur close to rocks be-
longing, according to the litho-
stratigraphic schemes, to the Skole
and Subsilesian Nappes. The
Goryczkowiec (Szydłowiec) Sand-
stone deposits are distinguished as
a lithostratigraphic unit that is char-
acteristic for this zone. We studied
this unit in the Western Car-
pathians, including the Wiśniowa
Tectonic Window and the Lancko-
rona Zone (Figs. 3 and 4), taking
into special consideration the stra-
totype profile located in Wadowice
near Goryczkowiec Hill (Figs. 4
and 5). A similar sandstone unit de-
scribed from the Żywiec Tectonic
Window (Geroch & Gradziński
1955) is now poorly exposed.
Previous studies
“The Szydłowiec bryozoan-litho-
thamnium sandstone” was origi-
nally described by Książkiewicz
(1951a,b) as a sandstone complex
that forms Szydłowiec Hill (recent-
ly renamed Goryczkowiec Hill) lo-
cated in the southern part of the
town of Wadowice, north of Gor-
zeń
Dolny village. Książkiewicz
(1951b) reported that this sand-
stone was also known to Hohe-
negger (1861) and Dunikowski
(1885). Książkiewicz established
the Szydłowiec Sandstone as a new
lithostratigraphic division of the
Subsilesian Series. The bryozoan-
lithothamnium Szydłowiec Sand-
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This idea was adopted by other authors (Nowak 1963). Balcer
& Koszarski (1992, see also Koszarski et al. 1974; Koszarski
1985; Żytko 1985) suggested that the Szydłowiec beds
should be included in the Skole Nappe and emphasized their
similarities to the Inoceramian Beds of the Skole Series.
Cieszkowski et al. (2011, 2012b) presented the first results
of new detailed investigations of the geology of the Wado-
wice area and concluded that so-called “the Szydłowiec
thrust-sheet” has in fact an olistostrome origin. A block con-
sisting of the Goryczkowiec Sandstone is covered by the
Gorzeń beds and underlain by grey shales, representing a
large olistolith in the highest part of the Krosno Formation
section. The various grey and variegated marls also represent
olistoliths within the Krosno Beds matrix, so the position of
Fig. 4. Geological map of the Wadowice area with stratotype locality (map after Nowak 1963; Szymakowska & Żytko 1965, modified).
Fig. 5. Lithological logs of the Goryczkowiec Sandstone.
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the Szydłowiec and Gorzeń Sandstones is analogous to the
olistostrome blocks known as the Andrychów Klippes
(Cieszkowski et al. 2009b, 2011, 2012a,b). While the olis-
tolithic origin of the block located south of Wadowice is
well documented, the positions of similar rocks in the
Wiśniowa and Sułkowice areas are still under investigation.
It is possible that the present sequence of these deposits re-
flects their original position within the Subsilesian Sedimen-
tary Area.
The older papers suggested a Maastrichtian age of this
lithostratigraphic division (Książkiewicz 1951b). Książkie-
wicz cited the micropaleontological investigations of Bieda
(1948), who studied samples of calcareous sandstones from
the type locality. The larger foraminifera that Bieda (1948) ex-
tracted represented the genera Simplorbites and Siderolites
and are known from the Maastrichtian. A Maastrichtian age
was preferred in other papers (Bieda et al. 1963; Geroch et al.
1967), the table listings, however, also suggested a Paleocene
age. Geroch & Gradziński (1955) defined the age of the bryo-
zoan-lithothamnium sandstones in the Żywiec Tectonic
Window as Maastrichtian to Paleocene based on smaller fora-
minifera assemblages that indicated a transitional age between
the Maastrichtian and Paleocene. They noted that the small
foraminiferal assemblages were very similar to those quoted
by Książkiewicz (1956). Burtan (Burtan et al. 1974; Burtan
1978) preferred a Maastrichtian age, indicating that the sedi-
mentation lasted from the Maastrichtian until the end of the
Danian. The Szydłowiec Sandstone was mentioned in the
“Mesozoic” volumes of the “Geology of Poland” (Koszarski
& Ślączka 1973).
The ambivalence in the lithostratigraphic
nomenclature
The name Szydłowiec Sandstone was used in lithostrati-
graphic nomenclature to describe two independent litho-
stratigraphic units, located within two separate geological
realms. One – more popular – is typical of the Holy Cross
Mountains and consists of a Jurassic white sandstone of con-
tinental origin. The second Szydłowiec Sandstone is typical
of the Outer Carpathians, and constitutes thickly-bedded flysch
deposits connected with the Tethys Ocean now located within
the Subsilesian Nappe. These deposits are widespread be-
tween Żywiec and Wiśniowa, and their outcrops are dis-
membered, small, and rare. The Carpathian Szydłowiec
Sandstone contains numerous calcareous clasts, in most cas-
es of biogenic origin (Cieszkowski et al. 2012a; Waśkowska
et al. 2012). Coralline red algae and remnants of bryozoa are
common, together with other fossils typical of shallow ma-
rine environments. The position of this sandstone unit within
the Silesian or Subsilesian lithological profiles is not clear. It
crops out as isolated exposures among deposits characteristic
for the Subsilesian Sedimentary Area.
The formal lithostratigraphic nomenclature of the Outer
Carpathians is still in the process of reorganization according
to stratigraphic code rules (see Alexandrowicz et al. 1975;
Racki & Narkiewicz (Eds.) 2006). The lithostratigraphic
units of the Subsilesian Nappe are not formalized, and the
traditional informal names like the Paleocene Green Shales,
the Szydłowiec Sandstone, the Frydek-type Marls or the
Czerwin Sandstone are still being used in the Polish litera-
ture (e.g. Cieszkowski et al. 2005a; Leśniak et al. 2005;
Ślączka et al. 2006; Waśkowska-Oliwa 2008). The formal-
ization process requires the precise detailed description of
lithology, chronostratigraphy, and well defined formational
boundaries. The lithostratigraphic inventory of the Upper
Cretaceous and Paleogene deposits of the Subsilesian Nappe
is still a subject of discussion (Burtan 1974; Koszarski (Ed.)
1985; Balcer & Koszarski 1992; Waśkowska-Oliwa 2008;
Cieszkowski et al. 2010). Some units are distinguished lo-
cally, without lateral continuity. The deposits are often
strongly tectonically deformed and the natural, sedimentary
boundaries are not well exposed. The individual tectonic
windows have their own lithostratigraphic schemes, con-
structed on the basis of stratigraphic sequence, without for-
malization. The name Szydłowiec Sandstone is in conflict
with lithostratigraphic code, as every lithostratigraphic name
should be unique. Since 1951, when the Carpathian sand-
stones were described, two independent divisions using the
same names have been in use. The Holy Cross Mountains
Szydłowiec Sandstone was defined in 1887 by Siemiradzki,
while the Carpathian one was described in 1951 (Książ-
kiewicz 1951a,b). The law of priority, respected in the natu-
ral sciences, would suggest suppression of the younger
name. The name Carpathian Szydłowiec Sandstone origi-
nates from the hill south of Wadowice, where Książkiewicz
(1951a,b) found and described these deposits exposed in nu-
merous quarries. The name Szydłowiec Hill functioned as an
equivalent to Goryczkowiec Hill before the 2
nd
World War,
but the name later disappeared from the maps and only
Goryczkowiec is now used. We therefore decided to intro-
duce the name Goryczkowiec Sandstone for this litho-
stratigraphic unit to avoid confusion with the Holy Cross
Mountains Szydłowiec Sandstone.
Lithology
Thickly-bedded coarse-grained sandstones, pebbly sand-
stones and fine-pebble conglomerates predominate within
the Goryczkowiec Sandstone (Figs. 5 and 6). The sandstones
have a well-sorted grain framework, while the conglomer-
ates are poorly sorted and contain more cement. In many
cases the sandstones are amalgamated. Occasionally, the
sandstone complexes are intercalated by thin layers of shales
or thin- and medium-bedded shaly sandstone flysch. Medium-
and thickly-bedded coarse sandstones within green calcare-
ous shales were observed in the Wiśniowa and Sułkowice ar-
eas. The lithological development is variable. The thickness
of the thickly-bedded layers oscillates from 0.8—2.5 m and
amalgamated complexes can reach even 5—6 m. A massive
structure dominates within the thickly-bedded sandstone lay-
ers. Parallel or/and cross laminations occur in the upper parts,
and occasionally parallel lamination is observed in the mid-
dle part of the layer. Coarser material in the lower part of
layers is common. In some cases coarse-grained sandstone
passes gradually to fine-pebble conglomerates.
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Grains measuring 2—7 mm occur within fine- and medium-
grained matrix in coarser sandstones, but isolated pebbles reach
up to 11 cm. Grey shaly mudstone clasts that reach up to several
centimeters in length form local levels within the sandstone
layers. Thinly- and medium-bedded sandstone layers (2—35 cm
thick) are fine- and/or medium-grained, occasionally coarser,
Fig. 6. Outcrops of the Goryczkowiec Sandstone: A – thick-bedded sandstones intercalated green shales in Gościbia tectonic window;
B – thick-bedded sandy complex in Wadowice – stratotype Goryczkowiec Hill; C – coarse-grained sandstones in Lipnik section;
D – coal clast in sandstone, Krzyworzeka section; E – sandstone with pebbles, Goryczkowiec Hill; F – organic trace-fossils; G – sand-
stone with coal clasts, Na Padoły stream, Wiśniowa.
fractional, with parallel and cross laminations, sometimes with
concentrations of muscovite that highlight the lamination. Thin-
ly-bedded sandstones are fine- and very fine-grained and cross-
laminated. The presence of glauconite gives the fine-grained
sandstones a greenish colour. Current marks and organic trace-
fossils are observed on the bottoms of sandstone layers.
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The most abundant grain type is quartz, which occurs in a
monocrystalline, polycrystalline and/or stretched metamor-
phic form. Lithoclasts are an important constituent of these
rocks. The volcanic basic rocks, granitoids, gneisses, sand-
stones with quartz and micas, siliceous rocks, mudstones, and
shales can be identified within these lithoclasts (Fig. 7). Single
grains of micas and glauconite occur as secondary compo-
nents. Quartz grains are predominantly angular to subangular;
the roundness of other grains is slightly better. Calcite cement
occurring between the composite grains is usually fairly
coarse-grained, especially in the conglomerates.
In addition to the detrital material, carbonate bioclasts
constitute an important component of the Goryczkowiec
Sandstone (Fig. 8). These rocks are especially rich in frag-
ments of the coralline algae. The fragments are usually
very fine, but single specimens can reach 1 cm in size.
Fragments of bryozoan colonies and echinoderm plates,
Fig. 7. Lithology of the Goryczkowiec Sandstone: A, B – sandstone with light
calcareous clasts; C – pebbly sandstone; D – conglomerate with a big quartz
grain; E – sandstone with quartz grains, clasts of gneisses and sparry cement
(microphotograph, XPL); F – sandstone with quartz grains, as well as glauconite
and fragments of red algae (microphotograph, PPL); G – pebbly sandstone with
quartz grains, bigger clast of volcanic basic rock and sparry cement (microphoto-
graph, XPL).
and in particular echinoid spines belong to the
other frequently occurring bioclasts. Planktonic
and benthic foraminifera, serpulid worms, and
fragments of bivalves are also present. Most of
these bioclasts originated in a shallow marine
environment, especially the coralline algae that
live within the photic zone.
Sandstones are interbedded with noncalcare-
ous green-grey clayey-muddy shales or occa-
sionally marly shales, often with psammite
admixture.
Age of the Goryczkowiec Sandstone
Material and methods
Micropaleontological investigations deter-
mined the age of the Goryczkowiec Sandstone.
These investigations used mainly foraminiferal
assemblages, but also attempted to use the algal
remains that are present in the sandstones as
bioclasts. The micropaleontological samples for
studies of foraminiferal assemblages were taken
from the grey-greenish muddy shales that are
intercalated with the sandstone layers in out-
crops of the Goryczkowiec Sandstone. The type
locality section is located in old abandoned
quarries on the northern slope of the Gorycz-
kowiec (Szydłowiec) Hill south of Wadowice.
The samples were also collected from sections
of the Gościbia creek valley cropping out in the
Jasienica-Sułkowice Tectonic Window, and
from the Krzyworzeka and Lipnik creeks sec-
tions in the Wiśniowa Tectonic Window.
Field samples consisted of muddy shales (about
0.5 kg each). They were prepared using standard
micropaleontological methods using Glauber’s
salt, and washed on small dimension sieve. The
foraminifera were picked from the > 63 µm resi-
due. The amount and quality of micropaleonto-
logical items was variable, and some samples
contain only a small number of specimens. The foraminifera
consist mainly of agglutinated forms. The abundance of accom-
panying calcareous forms was variable in different samples.
Organic remains contained in pieces of carbonate rocks
were studied in thin sections of samples collected from the
sandstones. Fragments of skeletons of calcareous coralline
algae were also useful for estimating the age of the rocks.
Foraminiferal assemblages
The micropaleontological samples studied here are domi-
nated by agglutinated foraminifera (Figs. 9—11; Table 1).
Single specimens of strongly corroded Lenticulina sp. were
found in a sample from the Lipnik section. This state of
preservation of specimens may suggest their redeposition
from shallow parts to deeper zones of the sedimentary basin.
In some samples from the Gościbia section, the admixture of
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Fig. 8. Bioclasts of the Goryczkowiec Sandstone (microphotographs): A – sandstone with fragments of red algae (A) and transverse sec-
tion of an echinoid spine (E) (PPL); B – sandstone with echinoderm plates (E) (XPL); C, F, H – red algae (PPL); D – shell (PPL);
E, G – bryozoans (PPL); I, J – benthic foraminifera (PPL).
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Fig. 9. SEM photographs of foraminifera from the Goryczkowiec Sandstone: A, B – Bathysiphon sp.; C – Nothia excelsa (Grzybowski);
D, G –Psammosiphonella discreta (Brady); E, H – Psammosiphonella cylindrica (Glaessner); F – Psammosiphonella sp.; I, J, K – Pla-
centammina placenta (Grzybowski); L – Ammodiscus cretaceus (Reuss); M – Ammodiscus peruvianus Berry; N – Glomospira irregu-
laris (Grzybowski); O – Annectina grzybowskii (Jurkiewicz). P, Q – Glomospira charoides (Jones & Parker); R – Glomospira
gordialis (Jones & Parker). Scale bar = 100 µm.
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Fig. 10. SEM photographs of foraminifera from Goryczkowiec Sandstone: A – Ammobaculites sp.; B – Karrerulina conversa (Grzy-
bowski); C –Hormosina velascoensis (Cushman); D – Haplophragmoides walteri (Grzybowski); E – Ammosphaeroidina pseudopaucilo-
culata (Mjatliuk); F – Paratrochamminoides sp.; G – Paratrochamminoides mitratus (Grzybowski); H – Paratrochamminoides dubius
(Grzybowski); I – Trochamminoides subcoronatus (Grzybowski); J –Remesella varians (Glaessner); K – Dorothia crassa (Marsson);
L, M – Dorothia retusa (Cushman); N – Dorothia sp.; O, P – Spiroplectammina dentata (Alth). Scale bar = 100 µm.
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Fig. 11. SEM photographs of foraminifera from the Goryczkowiec Sandstone: A, B – Kalamopsis grzybowskii (Dylążanka); C, D,
E, G – Rzehakina fissistomata (Grzybowski); F – Rzehakina lata Cushman & Jarvis; H—J – Rzehakina minima Cushman & Renz;
K – Caudammina gigantea (Geroch); L, M, N – Caudammina ovula (Grzybowski); O – Haplophragmoides mjatliukae Maslakova;
P, Q – Recurvoides sp. Scale bar = 100 µm.
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Table 1: Taxonomic list of foraminifera from the Goryczkowiec Sandstone. Continued on the next page.
Szydlowiec (Goryczkowiec) Hill
Gościbia section
K
rzyworzek
a
sect
io
n
Lipnik
valley
Sample number
63/1/05 Sz
18/2/05 Sz
19/1/05 Sz
16/4/05 Sz
17/3/05 Sz
12/ 335 G
13/ 326 G
14/ 331 G
15/ 330 G
16/ 332 G
17/ 329 G
1/ 336 G
10/311 K
4/358 L
5/359 L
Abyssamina quadrata Schnitker & Tjalsma
I
Ammobacuites midwayensis (d’Orbigny)
I
I
Ammobaculites sp.
I
I
Ammodiscus cretaceus
(Reuss)
I II I I I I I
Ammodiscus peruvianus
Berry
I II II I I I I I
Ammodiscus planus
Loeblich
II
II
II I I II
Ammodiscus
sp.
I I I I I I II I II
Ammodiscus tenuissimus
Grzybowski
I II I I I
Ammolagena clavata (Jones
&
Parker)
I I I
Ammosphaeroidina pseudopauciloculata
(Mjatliuk)
II I II II II II II II II V II
Annectina grzybowskii
(Jurkiewicz)
II I I II I I I II
Anomalina sp.
I
Aragonia ouezzanenzis (Rey)
I
Arthrodendron grandis Grzybowski
I I I I I I II
Bathysiphon
div.
sp.
VI
V
V
II
II
II
I II
Caudammina excelsa (Dylążanka)
II II II II II
Caudammina gigantea (Geroch)
I
Caudammina ovula
(Grzybowski)
(chambers)
II I II I I II I I II II II
Caudammina ovuloides
(Grzybowski)
I I II I I II I
Chiloguembelina morsei (Kline)
I
Cribrostomoides subglobosus
(Cushman)
I I II I
Cystammina sveni Gradstein & Kaminski
I
II
Dentalina
div.
sp.
I II I II
Dorothia crassa
(Marsson)
II I I
Dorothia indentata Cushman & Jarvis
I
Dorothia retusa
(Cushman)
II
II II
Dorothia
sp.
I I I I II I II
Ellipsoglandulina conicana Olbertz
I
Ellipsoglandulina obesa Hanzlikova
I
Eponides subcandidulus (Grzybowski)
I
Gavelinella sp.
I
Globanomalina sp.
I
Globobulimina sp.
I
Glomospira charoides (Jones & Parker)
I
II
II
II
II
V
I
II
I
V
II
I
Glomospira diffundens
Cushman
&
Renz
II I I I I I II I
Glomospira glomerata
(Grzybowski)
I I
Glomospira gordialis
(Jones
&
Parker)
I I II II II I II II
Glomospira irregularis
(Grzybowski)
I I
Glomospira serpens
(Grzybowski)
I I I
Guttulina sp.
I
Haplophragmoides mjatliukae (Mas
l
akowa)
I I II I
Haplophragmoides
sp.
I II I
Haplophragmoides walteri (Grzybowski)
I
I
Hormosina sp.
I
II I II
Hormosina velascoensis
(Cushman)
I I II II II I I II II II
Hyperammina sp.
I
Kalamopsis grzybowskii (Dylążanka)
II II I I II II
Karrerulina conversa
(Grzybowski)
I II II II I I II II
Karrerulina horrida
(Mjatliuk)
II I II I I
Karrerulina
sp.
I I II
Lagena sp.
I
Lenticulina sp.
I
Lenticulina velascoensis White
I
Lituotuba lituiformis (Brady)
I
Morozovella sp.
I
Nodosaria sp. and Nodosarella sp.
II
I
Nothia div. sp. (mainly N. excelsa
(Grzybowski)) II V V VI V V V V II V V
Nuttallides truempyi
(Nuttall)
I II
Nuttallinella florealis (White)
I
Osangularia velascoensis (Cushman)
I
Paratrochamminoides div. sp. (e.g. P. irregularis
(White), P. mitratus (Grzybowski), P. dubius
(Grzybowski), P. acervulatus (Grzybowski))
II III III I I II II II II I I II II II I
Placentammina placenta
(Grzybowski)
I I II II I I I I II I
Praesphaerammina gerochii Hanzlikova
I
Psammosiphonella div. sp. (mainly P. cylindrica
(Glaessner), P. discreta (Brady))
I II II V V VI V VI V VI V VI V
Psammospera fusca Schultze
I
ł
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Table 1: Continued.
calcareous benthic forms is much higher, though their pres-
ervation varies. Taking into account these observations and
the taxonomic composition with identified deep-water gen-
era, the calcareous microfauna appear to be an autochtho-
nous component of the foraminiferal assemblages.
The foraminiferal assemblages from the stratotype section
of the Goryczkowiec Sandstone on the slope of Goryczkowiec
(Szydłowiec) Hill contain the typical Paleocene taxon Rzeha-
kina fissistomata (Grzybowski) (Fig. 11C,D,E,G). This spe-
cies is typical for the deep-sea flysch deposits, noted from
many deposits of Late Cretaceous-Early Paleogene age. Its to-
tal stratigraphic range was approximated as Maastrichtian-
Paleocene (mostly Paleocene) (Kaminski & Gradstein 2005
and references therein). In the Carpathian region, the species
Rzehakina fissistomata (Grzybowski) occurs exclusively in
the Paleocene, so it is used as an index taxon for regional Car-
pathian biostratigraphic divisions (Geroch & Nowak 1984;
Olszewska 1997). Haplophragmoides mjatliukae (Maslakova)
(Fig. 11O) identified from the Goryczkowiec Sandstone sec-
tion also indicates a Paleocene age. Olszewska (1997) applies
its extent as a supplementary parameter defining the Paleocene
Rzehakina fissistomata Biozone. Additionally, cosmopolitan
forms are found in the assemblages: Maastrichtian—Paleocene
Remesella varians (Glaessner) (Fig. 10J), Glomospira diffun-
dens Cushman & Renz; Senonian—Paleocene Caudammina
gigantea (Geroch) (Fig. 11K), C. ovuloides (Grzybowski), C.
excelsa (Dylążanka), Pseudonodosinella parvula (Huss), Rze-
hakina epigona (Rzehak), R. minima Cushman & Renz
(Fig. 11H,I,J), Dorothia crassa (Marsson) (Fig. 10K), Spiro-
plectammina dentata (Alth) (Fig. 10O,P), as well as Senonian—
Eocene Caudammina ovulum (Grzybowski), Spiroplectammina
spectabilis (Grzybowski), Annectina grzybowski (Jurkiewicz)
(Fig. 9O), Hormosina velascoensis (Cushman) (Fig. 9C). The
composition of foraminiferal assemblages from other locali-
ties in the Sułkowice-Jasienica and Wiśniowa Tectonic Win-
dows is very similar. Spiroplectammina navarroana Cushman,
and Dorothia indentata Cushman & Jarvis (the Senonian-
Paleocene forms) as well as Cystammina sveni Gradstein &
Kaminski (noted in the Early Paleogene) are found in the
Gościbia section. Assemblages of calcareous benthos, rela-
tively rich in taxa as well as the Early Paleocene planktonic
forms including Subbotina triloculinoides (Plummer) occur
there. Benthic calcareous foraminifera are represented by
Ellipsoglandulina, Nuttallides, Eponides, Nodosaria, Gave-
linella and Pullenia. Cretaceous—Paleocene calcareous benthic
species such as Nuttallinella florealis (White), Osangularia
velascoensis (Cushman), Pullenia coryelli White, Ellipsoglan-
dulina obesa Hanzlikova, Aragonia ouezzanenzis (Rey) as
well as Paleocene—Eocene taxa, such as Nuttallides truempyi
(Nuttall) and Abysammina are the most common.
Szydlowiec (Goryczkowiec) Hill
Gościbia section
K
rzyworz
ek
a
sect
io
n
Lipnik
valley
Sample number
63/1/05 Sz
18/2/05 Sz
19/1/05 Sz
16/4/05 Sz
17/3/05 Sz
12/ 335 G
13/ 326 G
14/ 331 G
15/ 330 G
16/ 332 G
17/ 329 G
1/ 336 G
10/311 K
4/358 L
5/359 L
Pseudonodosinella nodulosa
(Brady)
I I I I
Pseudonodosinella parvula (Huss)
I
Pullenia coryelli White
I
Recurvoides div. sp., Thalmannammina subturbinata
(Grzybowski)
V V V II II II II II II I II II V II
Remesella varians
(Glaessner)
I I II I I
Reophax
sp.
I I I
Reophax duplex
Grzybowski
I
Reophax pilulifer Brady
I I I
Rhizammina
sp.
V V II
V I V
Rzehakina epigona
(Rzehak)
I I I I I I II
Rzehakina fissistomata
(Grzybowski)
II I I I II I I II I
Rzehakina minima Cushamn et Renz
II
I
I
Saccammina grzybowskii (Schubert)
II I I II I
Saccammina scabrosa
Mjatliuk
I II I I II I I
Saccammina sp.
I I I I II II
Saracenaria sp.
I
Spiroplectammina navarroana
Cushman
I I II I
Spiroplectammina sp.
I
Spiroplectammina spectabilis
(Grzybowski)
I I II
Spiroplectinella dentata (Alth)
II
Subbotina triloculinoides
(Plummer)
I
Subreophax splendidus (Grzybowski)
I
Subrepohax scalaris (Grzybowski)
I I I
Trochammina globigeriniformis (Jones & Parker)
II
I
I
I
I
Trochammina
sp.
I I I I I I II I
Trochamminoides proteus
(Karrer)
I I
Trochamminoides subcoronatus (Grzybowski)
I
I
I
Trochamminoides variolarius (Grzybowski)
II
II
I
Trochamminopsis altiformis (Cushman & Renz)
I
Specimens (per sample): I — 1–4 specimens; II — 5–9 specimens; III — 10–19 specimens; V — 20–99 specimens; VI — 100 and more.
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The frequency of various species commonly known from
Senonian assemblages, (especially relatively numerous speci-
mens of Caudammina ovulum (Grzybowski) or Caudammina
excelsa (Dylążanka) and Rzehakina) together with the pres-
ence of restricted Paleocene foraminifera can suggest that the
Goryczkowiec Sandstone was formed in the Early Paleocene.
This type of faunal diversity was observed in Paleocene as-
semblages from deposits of the Subsilesian Nappe. The fre-
quency of relatively numerous and taxonomically diversified
agglutinated foraminifers, which survived the extinction
event at the Cretaceous/Paleogene boundary, is typical for
the Lower Paleocene deposits of the Subsilesian Nappe. In the
Upper Paleocene deposits the abundance of tests and their
diversity significantly decreased (Waśkowska-Oliwa 2001,
2004, 2008). Moreover, the frequency of sporadic typically
Cretaceous Caudammina gigantea (Geroch) is noted exclu-
sively from the Early Paleocene (Liszkowa 1959; Sztejn et al.
1984; Waśkowska-Oliwa 2008). The taxon Chiloguembelina
morsei (Kline), which occurs in the Early Paleocene (Olsson
et al. 1999) was identified in one sample that also contained
planktonic Subbotina triloculinoides (Plummer).
The recently collected micropaleontological material indi-
cates an undisputed Paleocene age for the Goryczkowiec
Sandstone, based mainly on the taxonomic composition of
the agglutinated foraminiferal assemblages, the preserved
calcareous forms, and algal material from thin sections. A
Paleocene age was determined based on the total range of
commonly occurring species, in particular Rzehakina fissis-
tomata (Grzybowski) and Haplophragmoides mjatliukae
Maslakova, as well as the coexisting Senonian—Paleocene
and Paleocene—Eocene agglutinated, calcareous benthic, and
planktonic species. The foraminiferal assemblages have been
assigned to the Rzehakina fissistomata Biozone (zone after
Olszewska 1997), and in particular to the earlier Early Paleo-
cene part of that zone. Other papers dealing with the micro-
paleontological stratigraphy contain age estimates based on
the state of knowledge that existed sixty years ago. This ma-
terial requires reevaluation. The modern sedimentological
models of the Outer Carpathian Flysch emphasize resedimen-
tation of the shallow water older rocks from ridges into the
younger deposits formed within deep-water basins. The larger
foraminifera as well as other calcareous organic remnants
were redeposited by gravity flows together with siliciclastic
material from the shelf or upper basin slope (cf. Książkiewicz
1956). The flysch deposits are never older than their younger
components. The age determination based on examination of
small foraminifera assemblages from shales that consist of
muddy or clayey material deposited mainly by free suspen-
sion is more reliable. The autochthonous microfauna recently
evaluated do not contain any index species of Maastrichtian
age within the Goryczkowiec Sandstone deposits.
Lithostratigraphic position
The upper boundary of the Goryczkowiec Sandstone is
well documented in the type locality south of Wadowice as
well as in the reference section in Wiśniowa and Sułkowice
(Figs. 3 and 4). The thin- and medium-bedded quartzitic sand-
stones intercalated by green shales cover the Goryczkowiec
Sandstone in the area between Goryczkowiec Hill and
Gorzeń village. The green shales contain micropaleontologi-
cal assemblages documenting a Paleocene age (e.g. Balcer &
Koszarski 1992; Cieszkowski & Waśkowska-Oliwa 2002).
The sandstones are greenish in colour. They contain a consid-
erable amount of glauconite and also carbonate clasts. These
flysch deposits covering the Goryczkowiec Sandstone were
named the Gorzeń Sandstone by Książkiewicz (1951a,b). The
name is derived from the nearby Gorzeń village. Burtan
(1974, 1978) found similar deposits in the Wiśniowa area and
named them the Czerwin Sandstone. They are represented by
green shales with thin- and medium-bedded sandstones con-
taining calcareous clasts (most of them have biogenic origin)
and glauconite. They are the equivalent of the Gorzeń Sand-
stone defined by Książkiewicz (1951a,b).
The lower boundary of the Goryczkowiec Sandstone in the
Wadowice area is not so clear due to the olistostrome charac-
ter of the rocks. In most cases, grey and grey-green shales with
very sporadic intercalations of thin-bedded calcareous sand-
stones constitute the lower part of the large olistolith just be-
low the Goryczkowiec Sandstone. A similar sequence is well
documented in the reference sections in the Sułkowice and
Wiśniowa areas. The shales contain foraminiferal assemblages
with Rzehakina fissistomata (Grzybowski) documenting a Pa-
leocene age (Waśkowska-Oliwa 2002). The above described
complex separates the Goryczkowiec Sandstone from the Cre-
taceous Frydek-type marls. The traditional lithostratigraphic
scheme of the Subsilesian Unit (see e.g. Waśkowska-Oliwa
2005, 2008; Ślączka et al. 2006 and references therein) in
which the Goryczkowiec (Szydłowiec) Sandstone covers the
Frydek marls is no longer valid.
Similar clastic rocks are known from the Subsilesian Unit in
the Outer Carpathians in the Czech Republic. They are usually
called Stráž-type Sandstone (type locality Choryňská Stráž
Hill near Choryně). Elias (1988) also distinguished the Lower
Paleocene Klokočov Beds at the top of the Frydek Formation,
without giving, however, any detailed diagnostic characters
that would help to distinguish the Klokočov and Stráž-type
Sandstones. All calcareous biodetritic (algal) sandstones and
conglomerates within the Czech Republic are called the Stráž-
type Sandstone and are marked accordingly on the geological
maps from the 1960s until now, indicating a rock type (in par-
ticular petrography) rather than a well-defined lithostratigraphic
unit. The field survey in the Czech Republic indicated later-
ally equivalent facies (variegated, grey and black grey shales,
biodetritic sandstones etc.) in the Subsilesian Unit are just lat-
erally passing facies (Menčík et al. 1983). The Goryczkowiec
Sandstone would perhaps fit into the Czech lithostratigraphic
scheme as a member within the Frýdlant Formation (Picha et
al. 2006). This new lithostratigraphic scheme requires further
consideration in cooperation with Czech geologists.
Paleogeography and paleoenvironment
The Outer Carpathian realm originated during Jurassic
times as two separate paleogeographical units: the Alpine
Tethys and the Protosilesian Basin (Hsü 1975; Książkiewicz
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1977; Golonka et al. 2005a,b, 2006, 2011; Waśkowska et al.
2009). The Paleogene paleogeography of the Outer Car-
pathians reflects the series of continental break-ups, rifts and
collisions (e.g. Golonka et al. 2009; Golonka 2011) (Fig. 12).
Each basin had a specific type of clastic deposits, and sedi-
mentation commenced at different times (Bieda et al. 1963;
Ślączka et al. 2006). The Magura Basin originated as part of
the Alpine Tethys created during Mesozoic times between
the Tethyan terranes and Eurasia. The other Outer Car-
pathian basins developed in the process of rifting and frag-
mentation of the European platform. During the Cretaceous
compression the Magura Basin joined the Outer Carpathian
realm. Within this realm in the foreland of the folded Inner
Carpathians area, several basins divided by ridges and un-
derwater swells became distinctly separated. In the Paleo-
gene the movement of Adria and ALCAPA terranes resulted
in gradual closing of the flysch basins and development of
an accretionary prism. The ridges dividing the flysch basins
in the Outer Carpathians became more distinguished provid-
ing favourable conditions for development of shallow banks
with carbonate platform sedimentation.
The Late Cretaceous—Paleocene orogenic processes in the
northern Outer Carpathians produced an enormous amount
of the clastic material that started to fill the Carpathian ba-
sins. The material was derived from the northern and south-
ern margins as well as from the inner ridges and elevated
areas. The Silesian Ridge separated the Magura and Silesian
basins. The Marmarosh Ridge was the extension of the Sile-
sian Ridge (Bąk & Wolska 2005). It was also the alimenta-
tion center for detrital material during the Paleocene.
Carbonate detritus was transported to the north into the Sile-
sian Basin and to the south into the Magura Basin. The Sub-
silesian uplifted area was located between the Silesian and
Skole Basins. The shallow banks with the carbonate plat-
form sedimentation developed on this ridge. Carbonate detri-
tus was transported to the surrounding slopes and basins
contributing to the development of accretionary prism de-
posits. The Goryczkowiec Sandstone belongs to these depos-
its. It represents the coarse-grained type of flysch dominated
by psammite-psephitic deposits separated by shale complexes.
These rocks were deposited on the slope of the Subsilesian
uplifted area (Figs. 12 and 13). The allogenic material,
present within sandstones and conglomerates was transported
from the shallower parts on the slopes. The petrographic in-
ventory is diversified representing crystalline as well as sedi-
mentary rocks. During the maximal stage of ridge uplift the
basement was eroded, providing crystalline rocks belonging
originally to the North European Platform. Proterozoic, Ven-
Fig. 12. Palinspastic cross-section showing the Outer Carpathian basins during the Paleocene. Abbreviations: FC – Fore-Magura Ridge,
Fm – Fore-Magura Basin, Si – Silesian Basin, SK – Skole Basin, SC – Silesian Ridge, SS – Subsilesian Ridge, SR – Subsilesian
Sedimentary Area (after Waśkowska et al. 2009).
Fig. 13. Paleogeography of the Outer Carpathian basins during the Late
Cretaceous. Abbreviations: BG – Bucovinian-Getic, Co – Cor-
nohora, Porkulec, Audia, Teleajen, Du – Dukla, FC – Fore-Magura
Ridge (cordillera), Fm – Fore-Magura Basin, Gr – Grybów Basin,
Mg – Magura Basin, Mn – Manin Basin, SI – Silesian Basin,
SK – Skole Basin, SC – Silesian Ridge (cordillera), SS – Subsile-
sian Ridge, Zl – Zlatna (after Golonka et al. 2011, modified).
dian (Cadomian), Early Paleozoic (Caledonian), Late Paleo-
zoic (Hercynian) fragments can be distinguished within the
folded and metamorphosed basement of this plate (Golonka
et al. 2004, 2006; Ślączka et al. 2006).
The sedimentary fragments are represented mainly by car-
bonates, the clastic rocks are not so frequent. The carbonate
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clasts occur within medium-thick layers of the Goryczkowiec
Sandstone. They also dominate the flysch layer constituting
the allodapic limestone. Originally they were deposited
within the sublittoral, mainly reefal facies. The uplifted part
of the ridge was surrounded by shallow water, probably a
narrow shelf locally dominated by coralline algae; other reef
species are not so frequent. In smaller amounts there were
bryozoans, brachiopods and foraminifers. The patchy distri-
bution of these bioclasts is confirmed by the local occurrence
of redeposited organic limestones within the siliciclastic ma-
terial. The algal material is quite similar in all the Carpathian
Paleocene carbonates. Numerous calcareous red algae have
been found in Paleocene flysch and olistostrome deposits
within all the Outer Carpathian subbasins (e.g. Cieszkowski
et al. 2005b; Golonka et al. 2005a; Ślączka et al. 2006). The
calcareous algae play a major role in ecological and paleo-
geographical reconstructions, as they are only derived from
shallow and littoral zones. The character of algal assemblages
closely follows the facies paleoenvironment. These paleoen-
vironments include reefs, patch reefs, reef talus, shallow wa-
ter platforms, lagoons, and others.
In older works several algal genera (Lithothamnium,
Lithophyllum, Mesophylum, Arhaeolithothamnium, Paleo-
thamnium, Ethelia among the others) were distinguished in
the so-called Lithothamnium limestones and sandstones
within the Outer Carpathian Flysch (Golonka 1974). Recently
fossil red algae species are often considered artificial (e.g.
Rasser & Piller 1999; Rasser 2000) and the algal material re-
quires reevaluation. Nevertheless, the strong development of
the Corallinaceae family occurred during Paleocene (Thane-
tian) times (Perrin 2002). The Corallinaceae and Squamari-
aceae algae artificial species assemblages also known from
the Goryczkowiec Sandstone include Paleothamnium iorii
Maslov, Lithothamnium abrardi Lemoine, L. andrusowi
Lemoine, L. contraversum Lemoine, L. densum Lemoine, L.
quadrangulum Lemoine, Lithophyllum carpathicum Lemoine,
Ethelia alba Pfender, and Distichoplax bisserialis (Dietrich).
These assemblages are similar within olistoliths and organo-
detritical sandstones within the Paleocene formations of all
Outer Carpathian and Pieniny Klippen Belt units. They are
not known from the Cretaceous deposits.
The algae occurring in flysch sediments indicate the exist-
ence of intrabasinal ridges and carbonate platforms along the
basin margins. The abundance of algae in flysch deposits in-
dicates the time of geotectonic activity, development of rifted
basins and/or closing of flysch basins. Well-preserved reefs
are known from the olistolithic limestones found in Eastern
and Western Slovakia (e.g. Kambühel Kalk, see Köhler et al.
1993; Köhler & Buček 2005) the Haligovce and Velký Lip-
nik olistolithic limestones (e.g. Cieszkowski et al. 2004;
Köhler & Buček 2005; Krobicki et al. 2005; Cieszkowski et
al. 2009a), which provide excellent example of coral-algal
reefal facies. These limestones were also found as olistoliths
within the fore-arc flysch deposits of the Žilina Formation.
The fore-arc Złatne (Klape, Myjava) Basin was formed dur-
ing Late Cretacaeous times as a result of subduction of the
southern part of the Alpine Tethys (Cieszkowski et al.
2009a). The huge Mesozoic Haligovce Klippen olistoliths
and Paleocene limestone reefs blocks were sliding during
Paleocene—Eocene times as repetitive events during the for-
mation of the Złatne accretionary prism.
During Paleocene time narrow carbonate platforms origi-
nated, in some places full of coral-algal reefs, which are now
known as Kambühel-type limestones (see Köhler et al. 1993;
Köhler & Buček 2005 and references therein).
The organogenic limestones are formed by Scleractinia cor-
als together with numerous red algae from the Corallinaceae
family Corallinaceae, Melobesiideae subfamily, algae (genera
Lithothamnium, Lithophyllum, Arhaeolithothamnium, Paleo-
thamnium, Ethelia), bryozoans, sponges, brachiopods, gastro-
pods and foraminifera.
The typical Paleocene sandstones with algal reef material
were described from numerous locations in the Outer Car-
pathian nappes. The eastern part of the Silesian Ridge was
made up mainly of sedimentary rocks, a source for the mature,
siliciclastic material. This part of the ridge was surrounded by
shallow water, probably narrow shelf locally dominated by
Lithothamnium, but other reef species were absent. There
were smaller numbers of bryozoans, brachiopods and fora-
minifera. Patchy distribution of these faunas is confirmed by
local occurrence of redeposited organic limestones within
siliciclastic material. The best known rocks containing the
redeposited shallow carbonates are the Skalnik Limestone
(Ślączka & Walton 1992) and exotic-bearing shales from
Bukowiec and Roztoki (Ślączka 1961; Golonka et al. 2005a,b;
Bąk & Wolska 2005). The Skalnik Limestone is a megatur-
bidite within the Oligocene bituminous fish-shales (Menilite
beds) from the western part of the Dukla Basin and its adja-
cent foreland. It shows changes from the NW towards the SE
in structures and contents of bioclasts. Its proximal part is
composed of graded and laminated limestones, towards the
SE amount of quartz grains increases and the Skalnik Lime-
stone eventually passes into calcareous sandstones. Every-
where the calcareous algae Lithothamnium is predominant,
with smaller amounts of bryozoans and foraminifera. The
more proximal part also contains fragments of echinoderms,
brachiopods, ostracods and Balanidae. The Czerwin Sand-
stone known from outcrops in the Wiśniowa Tectonic Win-
dow east of Wadowice (Burtan 1974, 1978; Cieszkowski et
al. 2001) also belongs to the Paleocene sandstones with algal
reef material. They contain numerous calcareous clasts. Lo-
cally, these clasts prevail and were described as allodapic
limestones with Lithothamnium (Cieszkowski et al. 2009b).
Carbonate material with coralline red algae was also found
within sandstones typical for the Silesian Basin in the Upper
Istebna Beds and the Ciężkowice Sandstone (Leszczyński
1978), especially its local facies known as the Melsztyn Sand-
stone (Cieszkowski et al. 2010). The Bircza Sandstone depos-
ited in the eastern part of the Skole Basin contains a
Lithothamnium-limestone bed, which is a typical example of
the limestone formed by material that originated on the shal-
low-water margin of the North European Platform and was
redeposited in the Carpathian flysch. The Bircza Sandstone
was deposited on the northern margin of the Skole Basin,
while the Goryczkowiec Sandstone was deposited on its
southern margin within the Subsilesian Sedimentary Area,
mainly in a reef talus paleoenvironment (Fig. 12). The Sub-
silesian Ridge (Golonka et al. 2005b, 2011), which separated
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the Silesian and Skole Basins, was the main provider of detri-
tal material during the Paleocene (Golonka et al. 2004). It was
the source of carbonate material to the Goryczkowiec Sand-
stone, which represents a huge olistolith on the border of the
Subsilesian Unit. The carbonate sediments with coralline red
algae are well preserved in the area of Adrychow, in the Tar-
ganice and Pańska Góra olistoliths. They represent more prox-
imal facies of reef talus, compared with the Goryczkowiec
sediments. The paleogeographical position of the Gorycz-
kowiec Sandstone confirms the Paleocene age of this litho-
stratigraphic unit.
Agglutinated forms predominate in the autochthonous as-
semblages of foraminifera. Foraminifera that agglutinated
grains with carbonate cement also occur within these assem-
blages (e.g. Dorothia, Remessella). A typical admixture of
calcareous forms within the foraminiferal assemblages of
mainly benthic forms, representing a deep-sea bathyal paleo-
environment, is around 2—10 %, occasionally reaching 20 %
(Geroch & Gradziński 1955; Waśkowska-Oliwa 2005). The
taxonomic composition of the calcareous benthos is diversi-
fied. Planktonic foraminifera are occasional, usually not sur-
passing 1 %. This composition of microfauna confirms the
deep-sea conditions of sedimentation in this part of the Sub-
silesian Sedimentary Area, where the Goryczkowiec Sand-
stone was deposited, most likely at a depth between the CCD
and lysocline (Waśkowska-Oliwa 2005). Coarse-grained sus-
pension-feeding foraminifera with massive test walls pre-
dominate, for example, Rhabdammina – a genus typical for
the high-energy turbiditic paleoenvironments. Other mor-
photypes, epifaunal to shallow and deep sea infaunal, are
well developed. The presence of diverse morphotypes sug-
gests good conditions for the development of foraminifera
with respect to organic matter as well as good oxygenation
of the bottom water and the surface of the sediment. In the
deep basinal zones, organic life was apparently the richest,
and the foraminifera were accompanied by macrofauna that
produced diversified trace fossils preserved on the bottoms
of sandstone layers and within the shales.
The Miocene tectonic movements within the Outer Car-
pathian accretionary prism caused final folding flysch de-
posits and created several imbricate nappes. The Subsilesian
Ridge deposits were partially included in the Subsilesian
Nappe, the ridge’s basement rocks and part of its deposits
form olistostromes and exotic pebbles within the upper part
of the Menilite-Krosno flysch and the following Lower Mio-
cene Molasse deposits (Cieszkowski et al. 2009a). The olis-
toliths, slid down into the basin situated in front of the
Silesian Nappe from the Subsilesian Ridge during Late Oli-
gocene or Early Miocene times.
Conclusions
The proximal flysch units from the marginal Outer Car-
pathians containing the Paleocene bryozoan-coralline algae
sandstones reflect the geodynamics of the ridges within the
Outer Carpathians. The Goryczkowiec Sandstone was de-
posited on the slope of an uplifted intrabasinal structure
known as the Subsilesian Sedimentary Area, at depths be-
tween the CCD and lysocline. Lithological investigations re-
vealed abundant calcareous material of biogenic origin rep-
resenting reef and its talus, containing red algae and
bryozoans as the leading organic group. This material was
transported by turbidity currents into deeper zones.
A Paleocene age for the Goryczkowiec Sandstone is docu-
mented on the basis of the autochthonous foraminiferal as-
semblages from shale intercalations and algae identified in
the thin sections.
The larger foraminifera, which suggested a Late Creta-
ceous (Maastrichtian) age are the allochthonous component,
redeposited by turbidity currents from eroded parts of the
Subsilesian Ridge. The Goryczkowiec Sandstone is under-
lain by Paleocene grey shales and covered by the Gorzeń and
Czerwin Sandstones.
We revise and redefine here the lithostratigraphic position
of the Goryczkowiec Sandstone, but further work needs to
be carried out in cooperation with Czech geologists leading
to the formalization of the Goryczkowiec and Gorzeń Sand-
stones as members within the Frýdlant Formation.
Acknowledgments: This research has been financially sup-
ported by AGH University of Science and Technology in
Krakow Grant No. 11.11.140.173. and Grant MNiSW/NCN
No. N N307 249733. We thank Miroslav Bubík (ČGS) for
helpful discussions. Mike Kaminski (KFUPM) and Ján Soták
(GI SAS) are thanked for reviewing the manuscript.
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