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, APRIL 2011, 62, 2, 139—154 doi: 10.2478/v10096-011-0012-0
Introduction
In the Polish sector of the Magura Nappe eleven tectonic
windows were documented (Fig. 1A—C). These windows be-
long to the Grybów Nappe of the Fore-Magura Group of
units (Oszczypko et al. 2008). This group of units, which oc-
cupy the intermediate position between the Silesian and
Magura Nappes (Fig. 1C), contains transitional lithofacies,
which linked the Silesian and Magura Basins (see Książkiewicz
1962; Bieda et al. 1963; Geroch et al. 1967; Koráb & Ďurkovič
1978; Olszewska 1981; Cieszkowski 1992, 2001; Oszczypko-
Clowes & Oszczypko 2004; Oszczypko-Clowes & Ślączka
2006; Oszczypko-Clowes 2008). The Obidowa-Słopnice and
Grybów Nappes occur in the tectonic windows. They are re-
garded as the western and southern prolongation of the Dukla
Nappe (Cieszkowski 2001). These nappes are composed pre-
dominantly of Upper Eocene-Oligocene deposits (Oszczypko-
Clowes & Oszczypko 2004; Oszczypko-Clowes & Ślączka
2006; Oszczypko-Clowes 2008).
The aim of this research was to establish the pecularities of
the lithofacies and to determine the age of the calcareous
nannoplankton of the Świątkowa Wielka Tectonic Window
(SWTW) deposits, but also to plot their correlation with sim-
ilar sediments from adjacent areas (Fig. 1B). On the basis of
up-to-date geological mapping as well as old oil field drill-
ings this work provides a new structural approach to this tec-
tonic window.
Previous studies
In 1888 Uhlig described the dark variety of Menilite shales
as “grybower Menilitschiefer” – already known in East
Slovakia as the Smilno beds (Hauer 1859).
Stratigraphy and tectonics of a tectonic window in the Magura
Nappe (Świątkowa Wielka, Polish Outer Carpathians)
MARTA OSZCZYPKO-CLOWES and NESTOR OSZCZYPKO
Institute of Geological Sciences, Jagiellonian University, Oleandry 2a, 30-063 Kraków, Poland;
marta.oszczypko@.uj.edu.pl; nestor.oszczypko@uj.edu.pl
(Manuscript received March 24, 2010; accepted in revised form October 13, 2010)
Abstract: The Świątkowa Wielka Tectonic Window belongs to the Grybów Nappe of the Fore-Magura Group of units.
This tectonic window is located in the marginal part of the Magura Nappe and is composed of Oligocene – Sub-
Grybów Beds as well as the Grybów Marl Formation. These beds have been correlated with the Oligocene deposits of
other tectonic windows of the Grybów Nappe in Poland. Our research reveals that the Krosno beds’ shally facies, which
occur at the western termination of the Świątkowa Wielka Tectonic Window, belong to the Dukla succession. On the
basis of calcareous nannoplankton analysis, the Grybów Marl Formation as well as the Krosno Beds belong to the
NP23—NP24, and NP24 Zones, respectively. The structure of the Świątkowa Wielka Tectonic Window reveals a multi-
stage evolution of the Magura Nappe overthrust onto their foreland.
Key words: Oligocene, Western Carpathians, Magura, Grybów and Dukla Nappes, duplex structure tectonic windows,
biostratigraphy, calcareous nannoplankton.
Over the period 1930—1932, while carrying out geological
mapping in the Świątkowa Wielka area, Böhm (1933) dis-
covered the Grybów black shales, which were established as
the Cretaceous “Świątkowa facies”, the oldest strata of the
Magura succession. This concept was accepted by Świdziński
(1934, 1947). However, in the early 1950’s, the concept was
questioned by K. Mrozek (see Kozikowski 1956) who, on
the basis of geological mapping, drilling and micropaleonto-
logical data, documented that the “Świątkowa facies” are the
equivalent of Menilite shales and occur in the tectonic win-
dow beneath the Magura Nappe.
The oldest sediments from the Grybów Nappe belong to
the Jaworzynka Beds (Senonian—Paleocene) of the Mszana
Dolna Tectonic Window (Fig. 1B), (see Oszczypko-Clowes
& Oszczypko 2004). The most frequent rocks are Lower to
Upper Eocene green, grey and black shales, with intercala-
tions of medium- and fine-grained glauconitic sandstones,
known as the Hieroglyphic Beds (Sikora 1960; 1970),
Klęczany Beds (Kozikowski 1956) or Sub-Menilite Beds
(Nemčok 1990; Nemčok et al. 1990). Towards the top they
pass into greenish marls, a few meters thick, with an abun-
dance of Globigerina representing the Late Eocene and cor-
responding to the horizon of the Sub-Menilite Globigerina
Marls (SMGM), known from all units of the Outer Car-
pathians (Olszewska 1983; Leszczyński 1996, 1997; Oszczyp-
ko 1996; Oszczypko-Clowes 1998). Early Oligocene is
represented by a series of roughly 150 meters of grey, dark
green, black marls, and marly shales with intercalations of
thin- to medium-bedded, micaceous, laminated sandstones
and several thick-bedded, glauconitic sandstones. These de-
posits were established as the Sub-Grybów Beds by
Kozikowski (1956). These beds pass upwards into Grybów
Shales distinguished by Uhlig (1888) and named as Grybów
Beds by Kozikowski (1956). In 1960 Sikora renamed them
Stratigraphy and tectonics of a tectonic window in the Magura
Nappe (Świątkowa Wielka, Polish Outer Carpathians)
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again as the Grybów Shales. In the highest part of the Gry-
bów Shales there are intercalations of black cherts and also
brownish siliceous marls with cherty lenses. The lower
boundary of the Grybów Shales can be found where grey-
green marls from the Sub-Grybów Beds disappear, and
where a sequence of brown and black marls appear.
The age of the youngest sediments of the Grybów Nappe
is generally regarded as Oligocene. The foraminiferal studies
were conducted by Kozikowski (1956), Blaicher (in Sikora
1960, 1970), and Olszewska (1981). According to Olszewska
(1981), the Sub-Grybów Beds (Klęczany and Ropa Window)
as well as the Grybów Shales (Klęczany and Mszana Dolna
Windows) are of Oligocene age.
Biostratigraphical studies based on nannofossils were initi-
ated by Smagowicz (see Burtan et al. 1992; Cieszkowski
1992) in the Klęczany Tectonic Window. She recognized nan-
nofossil associations from the Sub-Grybów Beds, which were
characteristic for latest Eocene—Early Oligocene. More recent-
ly, a detailed calcareous nannoplankton study of the Grybów
Nappe was carried out in Mszana Dolna and also in the
Szczawa Tectonic Windows (Oszczypko-Clowes & Oszczyp-
ko 2004), as well as in the Grybów (Oszczypko-Clowes &
Ślączka 2006) and Ropa (Oszczypko-Clowes 2008) Tectonic
Windows. In the Mszana Dolna Tectonic Window the young-
est deposits were assigned to the NP24 (Krosno Beds of the
Dukla Nappe) and NP23—NP25 (Krosno (Cergowa) Beds of
the Grybów Nappe) Zones. Similar nannoplankton ages were
also established in the Grybów Nappe of the Szczawa Tecton-
ic Window. Zones NP22—NP24 were determined in the Gry-
bów Shales, whereas the Krosno (Cergowa) Beds belong to
Zone NP24 (see Oszczypko-Clowes & Oszczypko 2004). The
Grybów Shales of the Grybów Tectonic Window were as-
signed to Zone NP24, while the Krosno (Cergowa) Beds were
included in Zones NP24—NP25 (Oszczypko-Clowes &
Ślączka 2006). Simultaneously these authors proposed the
Grybów Marl Formation (GMF) as a more appropriate new
name due to its lithological development. In the Ropa Tecton-
ic Window the NP22—NP24 Zone interval was determined in
the GMF, whereas the Krosno Beds belong to Zone NP25
(Oszczypko-Clowes 2008). On the basis of dinoflagellates,
Barski (in Bojanowski 2007b) determined the middle Rupe-
lian age of the Krosno shales of the SWTW.
In the adjacent Dukla Nappe calcareous nannoplankton
studies were, so far, also sporadic and carried out by
Smagowicz (Olszewska & Smagowicz 1977). Foraminiferal
studies were lately conducted by Olszewska (1983). They pro-
Fig. 1. A – Simplified tectonic scheme of the Alpine-Carpathian orogens. B – Tectonic sketch-map of the Outer Western Carpathians (based
on Żytko et al. 1989, simplified). C – Tectonic sketch-map of the Światkowa Wielka Tectonic Window (based on Koszarski & Tokarski
1968, supplemented). Tectonic windows: 1 – Mszana Dolna, 2 – Szczawa, 3 – Klęczany-Pisarzowa, 4 – Grybów, 5 – Ropa, 6 – Uście
Gorlickie, 7 – Świątkowa, 8 – Smilno.
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posed the biostratigraphical scheme of the Upper Cretaceous—
Paleogene deposits from the Dukla Nappe; which was based
on foraminiferal and calcareous nannoplankton investigations.
A detailed stratigraphic study of the Krosno Beds from the
Dukla Nappe in the Mszana Dolna Tectonic Window was car-
ried out by Oszczypko-Clowes & Oszczypko (2004).
In the Fore-Magura, Ždánice-Subsilesian and Pouzdřany
Units of the Czech sector of the Outer Carpathians the Meni-
lite and Krosno lithofacies were studied by Švábenická et al.
(2007).
In the Ukrainian Carpathians the Vezhany Unit of the Mar-
marosh Flysch can be regarded as the equivalent of the Gry-
bów successions of the Outer Western Carpathians
(Oszczypko et al. 2005). In this succession the Dusina marls
have the same age (NP24) and lithofacies development as
the Grybów Marl Formation in Poland.
Geological setting
The Świątkowa Wielka Tectonic Window, up to 1 km
wide and up to 3.5 km long, is located in the Beskid Niski
Range ca. 3—3.5 km southwest from the front of the Magura
Nappe (Fig. 1C). This tectonic window was discovered by
Kozikowski (1956, 1958). The geological mapping of the
surrounding area was carried out by Koszarski & Tokarski
(1968). The Oligocene strata of the Grybów Nappe in this
tectonic window are bound by the Upper Cretaceous—Pale-
ocene Ropianka Formation (Inoceramian Beds), Lower/Mid-
dle Eocene Łabowa Shale Formation (Variegated Shales)
and the Wątkowa Beds (Upper Eocene—Oligocene) of the
Magura Nappe (Koszarski & Tokarski 1968; Kopciowski
2007). Based on geological mapping and drillings, Tokarski
(1965) described the structure of the Świątkowa Wielka Tec-
tonic Window. According to his interpretation, the present
structure of the tectonic window, developed when the Magu-
ra and Grybów Nappes were overthrust onto the eroded Duk-
la Nappe. This was followed by the refolding of the Magura
and Grybów Nappes together.
The Oligocene deposits of the SWTW are strongly de-
formed and are often in an overturned position (Fig. 2).
These deposits belong to the Sub-Grybów Beds, Grybów
Marl Formation (GMF) (see Kozikowski 1956; Koszarski &
Tokarski 1968; Koszarski & Koszarski 1985). The Krosno
Beds occupy a special position with a block of “exotic”
limestones, located at the boundary between the Magura and
Grybów Nappes (see Mastella & Rubinkiewicz 1998; Boja-
nowski 2007a,b).
The studied section is exposed along the Krokowy Stream,
which is a triburaty of the Świerzówki Stream and Wisłoka
River (Fig. 2).
The oldest Eocene deposits of the Grybów succession
probably belong to the Hieroglyphic Beds known only from
the borehole Sw4 (Fig. 3). Higher up in the succession the
Sub-Grybów Beds occur at least 100 m thick, which are ex-
posed in the middle flow of the Krokowy Stream and pieced
in borehole Sw4 (Fig. 3). The basal portion of the Sub-Gry-
bów Beds is composed of grey and green, thin-bedded marls,
yellowish as weathered, and which probably belong to the
Sub-Menilite Globigerina Marls. These are followed by
grey, greenish, black marls (Fig. 4A) and greenish non-cal-
careous shales with intercalations of thin- to medium-bedded
sandstones (Fig. 4B). The rocks of these Sub-Grybów Beds
pass upwards into the Grybów Marl Formation the most typ-
ical Oligocene sediments of the SWTW, known both from
exposures and all boreholes. These beds up to 200 m thick
are composed of thick-bedded sandstones and marls. In gen-
eral these beds display upward sequences of thickening and
coarsening. The thick-bedded sandstones (80—160 cm) show
Tabc Bouma’s interval; they are coarse- to medium-grained
with large flute casts. The transition from the Sub-Grybów to
the GMF is manifested by a few packets 5—7 m thick of mas-
sive dark grey marls, brown as weathered (Fig. 4C). These
marls are followed by thick packets of grey, dark grey, green
shales and brown Menilite-type shales (Fig. 4D). The middle
part of the formation contains thick-bedded, light coloured,
medium-grained, quartz rich, laminated, sandstones (Fig. 4E)
of the “Kliwa-like sandstone” (see Nemčok et al. 1990), grey
marls and shales with an intercalation of laminated Tylawa-
type limestone (Fig. 4F). In the upper part of the formation
there are also thick-bedded, muscovitic sandstones of the
Cergowa type and thin-bedded sandstones (Fig. 5A,B,E).
These sandstones are subordinately intercalated by dark
grey, platty (Fig. 5C), massive (Fig. 5D) and thin-bedded
marls (Fig. 5E). The massive marls form 3- to 8 m thick
packets. Sometimes these marls are accompanied by thin-
bedded lenses of ferruginous dolomites (siderites). In the up-
per part of the formation the grey shales (Fig. 6A,B) are
intruded by sandstone dykes.
The youngest deposits of the SWTW belong to the Krosno
Beds, exposed in the upper course of the Krokowy Stream, at
the western termination of the tectonic window (Fig. 2).
From the east these beds are separated from the Sub-Grybów
Beds by a thrust fault. These strongly deformed beds, dis-
play a thinning and fining upward sequence and they are
composed of marly mudstones and shales, with a tablet sepa-
rateness (Fig. 6C,D). They often form packets up to several-
dozen meters thick. The sandstone intercalations are usually
thin- and very thin-bedded. In the middle part of the section
the Krosno shales contain beds of tectonically sheared fer-
ruginous dolomites, and beds of laminated limestones up to
35 cm thick (Fig. 6E). In the contact zone between the Kros-
no shales and the variegated shales belonging to the Magura
Nappe, there are well-known blocks of “exotic” limestones
(Koszarski & Koszarski 1985) – GPS position: N 4931
’671,
E 2124
’377. According to Mastella & Rubinkiewicz (1998)
these limestones are of Miocene age. Recently, Bojanowski
(2007a,b) documented that these limestones are a carbonate
build-up and composed of “cold seep-related carbonate in-
traformational breccia” (Fig. 6F).
Calcareous nannofossils
Methods and sample preparation
The field work in the SWTW was carried out between
2003 and 2005. For the purpose of the biostratigraphic re-
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Fig. 2.
Geological
map
of
the
Świątowa
Wielka
Tectonic
Window,
with
lo
cation
of
sampled
sections
(party
after
Koszarki
&
Tokarski
(19
68,
simplified)).
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search, 26 samples were collected from the Krokowy Stream
where a continuous sequence is exposed (Fig. 2).
All the samples were prepared using the standard smear
slide technique for light microscope (LM) observations. The
investigation was carried out under LM-Nikon – Eclipse
E 600 POL, at a magnification of 1000 using parallel and
crossed nicols. Several of the specimens photographed in
LM are illustrated in Fig. 7.
Results
The majority of the examined samples yield moderately
preserved nannofossil assemblages. The relative abundance
of samples is usually medium to low (Fig. 8).
Sub-Grybów Beds. All the samples 51-52/03/N and 62/
03/N, collected from either non-calcareous or slightly calcar-
eous shales and marls were barren of nannofossils (Fig. 8).
The Grybów Marl Formation. There are two distinctive
nannofossil assemblages within the GMF. The first associa-
tion was described from the following samples: 58-61/03/N
(Fig. 2) whereas the other is characteristic for samples 53-57/
03/N and 63-64/03/N.
The nannofossils from samples 58-61/03/N are reasonably
well-preserved, though the assemblages reveal low diversity
and a medium-to-high number of specimens. The assem-
blage is characterized by the presence of Coccolithus eope-
lagicus, Coccolithus pelagicus, Cyclicargolithus floridanus,
Dictyococcites bisectus, Discoaster tanii, Discoaster tanii
nodifer, Isthmolithus recurvus, Lanternithus minutus, Neo-
coccolithes dubius, Reticulofenestra dictyoda, Reticulofenes-
tra ornata, Sphenolithus moriformis, Sphenolithus radians.
The important feature of this assemblage is the abundant
presence of Reticulofenestra ornata.
Samples from 53-57/03/N and 63-64/03/N contain a relative-
ly rich, abundant and well-preserved assemblage. The nannofo-
sil association is characterized by co-occurenec of Coccolithus
eopelagicus, Coccolithus pelagicus, Cyclicargolithus abisectus,
Cyclicargolithus floridanus, Dictyococcites bisectus, Reticu-
lofenestra lockerii, Reticulofenestra minuta, Reticulofenestra
ornata, Sphenolithus dissimilis, Sphenolithus moriformis,
Zygrhablithus bijugatus. The most important species are Cycli-
cargolithus abisectus and Sphenolithus dissimilis.
Krosno Beds. The autochthonous assemblage of 1-10/05/N
samples is characterized by the presence of Coccolithus eope-
lagicus, Coccolithus pelagicus, Cyclicargolithus abisectus,
Cyclicargolithus floridanus, Dictyococcites bisectus, Neococ-
colithes dubius, Reticulofenestra dictyoda, Reticulofenestra
lockerii, Reticulofenestra minuta, Reticulofenestra ornata,
Sphenolithus dissimilis, Sphenolithus moriformis. The most
abundant are Cyclicargolithus abisectus, Cyclicargolithus flori-
danus, Dictyococcites bisectus and Coccolithus pelagicus. The
youngest species determining the age are Cyclicargolithus abi-
sectus and Sphenolithus dissimilis. Additionally, some of the
samples contained Helicosphaera euphratis, Helicosphaera
compacta, Pontosphaera multipora, Pontosphaera plana.
Biostratigraphical interpretation
For the purpose of biostratigraphic analysis the standard
zonation of Martini (1971) was used. In the cases where in-
dex species were not observed it was necessary to use the
secondary index and characteristic species.
Fig. 3. Geological profiles of boreholes (after Nawrocka-Gierat & Wdowiarz 1975, CAGPIG).
Sw1 BOREHOLE
alt. 452.5 m a.s.l.
Sw2 BOREHOLE
alt. 440 m a.s.l.
N 49 31 35,58, E 21 24 53,05
N 49 31 42, 01, E 21 25 05,54
Magura Nappe
Grybów Nappe
0–86
Variegated Shales ( abowa Sh. Fm)
0–74
Grybów Shales
86–101
Inoceramian Beds (Ropianka Fm)
Magura Nappe
101–156
Variegated Shales ( abowa Sh. Fm)
74–108
Variegated Shales ( abowa Sh. Fm)
156–272
Inoceramian Beds (Ropianka Fm)
108–164
Inoceramian Beds (Ropianka Fm)
Grybów Nappe
Dukla Nappe
272–491
Grybów Shales
164–514
Krosno Beds
Dukla Nappe
491–529
Krosno Beds
Sw3 BOREHOLE
Sw4 BOREHOLE
445 m a.s.l.
alt. 440 m a.s.l.
N 49 31 48,41, E 21 25 20,49
N 49 31 45, 19, E 21 25 20,49
Grybów Nappe
Grybów Nappe
0–137
Grybów Shales
0–155
Grybów Shales
Magura Nappe
155–218
Hieroglyphic Beds
137–146
Variegated Shales ( abowa Sh. Fm)
218–252
Sub-Grybów Beds
Grybów Nappe
252–267
Hieroglyphic Beds
146–159
Grybów Shales
Dukla Nappe
Magura Nappe
277–403
Krosno Beds
159–199
Variegated Shales ( abowa Sh. Fm)
199–250
Submarine slump of tectonic breccia
Dukla Nappe
250–512 Krosno
Beds
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Fig. 4. Exposures of the Grybów succession in the Krokowy Stream, Świątkowa Wielka. A – Grey, greenish and black marls of the Sub-Gry-
bów Beds; B – Grey and greenish non-calcareous shales with intercalation of the medium-bedded sandstones of the sub-Grybów Beds – im-
bricated anticline with west-dipping hinge plane; Gybów Marl Formation; C – Dark brown, thick-bedded massive marls of basal portion
of the formation; D – Grey, greenish and brown (Menilite type) shales; E – Thick-bedded, light quartz-rich sandstones, with graded and
parallel lamination; F – Tylawa laminated limestone.
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Fig. 5. Exposures of the Grybów Marl Formation in the Krokowy Stream, Świąkowa Wielka. A – Base of thick-bedded sandstone with
big flute-casts, displaying paleotransport from SE position; B – Medium-bedded, very fine- and fine-grained sandstones with parallel and
convolute laminations; C – Grey platy marls, with dark grey bed at the base; D – Dark grey, thick-bedded massive marls; E – Grey
thin-bedded marls; F – Base of thick-bedded sandstone with big, loaded flute-casts, displaying paleotransport from SE, overturned po-
sition.
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Fig. 6. Exposures of the Grybów and ?Dukla succession in the Krokowy Stream, Świątkowa Wielka. Grybów Marl Formation. A – Dark
grey massive marls-stone with clastic dyke; B – Grey marly shales with intercalations of medium-bedded, fine-grained sandstones; Kros-
no Beds of the Dukla succession; C – Marly shales and marl-stones of the lower portion of the beds of the Dukla succession; D – Strongly
folded overturned marly shales; E – Laminated limestone intercalation; F – Block of brecciated limestones.
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Fig. 7. LM microphotographs of calcareous nannofossils. A – Braarudosphaera bigelowii, Grybów Marl Fm, sample 54/03/N; B – Cycli-
cargolithus abisectus, Grybów Marl Fm, sample 53/03/N; C – Cyclicargolithus abisectus, Grybów Marl Fm, sample 61/03/N; D – Cyclicar-
golithus abisectus, Krosno Beds, sample 1/05/N; E – Cyclicargolithus floridanus, Krosno Beds, sample 10/05/N; F – Dictyococcites bisectus,
Krosno Beds, sample 10/05/N; G – Discoaster sp., Krosno Beds, sample 2/05/N; H – Ericsonia formosa, Grybów Marl Fm, sample 54/03/N;
I – Helicosphaera compacta, Grybów Marl Fm, sample 55/03/N; J – Helicosphaera compacta, Grybów Marl Fm, sample 55/03/N; K – Heli-
cosphaera euphratis, Grybów Marl Fm, sample 55/03/N; L – Helicosphaera euphratis, Krosno Beds, sample 10/05/N; M – Helicosphaera
recta, Grybów Marl Fm, sample 55/03/N; N – Helicosphaera recta, Grybów Marl Fm, sample 55/03/N; O – Isthmohlithus recurvus, Gry-
bów Marl Fm, sample 58/03/N; P – Pontosphaera lateliptica, Grybów Marl Fm, sample 57/03/N; R – Reticulofenestra lockerii, Grybów
Marl Fm, sample 64/03/N; S – Reticulofenestra lockerii, Krosno Beds, sample 7/05/N; T – Reticulofenestra ornata, Grybów Marl Fm, sam-
ple 58/03/N; U – Reticulofenestra ornata, Grybów Marl Fm, sample 60/03/N; W – Reticulofenestra ornata, Grybów Marl Fm, sample 61/03/N;
X – Reticulofenestra umbilica, Krosno Beds, sample 7/05/N; Y – Sphenolithus dissimilis, Krosno Beds, sample 2/05/N; Z – Zygrhablithus
bijugatus, Krosno Beds, sample 10/05/N.
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In the studied area the nannofossil association described from
the GMF allow us to determine Zones NP23 and NP24, which
represent the Kiscellian stage in the Central Paratethys Regional
Scheme (Fig. 9). The zone assignment of NP23 is based on the
abundant presence of Reticulofenestra ornata followed by the
last occurrence of Reticulofenestra umbilica, which marks the
upper limit of Zone NP22. According to Nagymarosy &
Voronina (1992) Reticulofenestra ornata is an endemic species,
and its abundant presence is a characteristic event in Zone NP23
of the Paratethys region, only. The FO of Cyclicargolithus abi-
sectus is usually found close to the FO of Sphenolithus cipe-
roensis (zonal marker for the lower boundary of Zone NP24)
and thus can be used to approximate the boundary of NP23 and
NP24 (Martini & Műller 1986). In addition, Sphenolithus dissi-
milis Bukry & Percival was also observed. The FO of these spe-
cies is characteristic for Zone NP24 (see Perch-Nielsen 1985).
Melinte (2005) identified the FO of Cyclicargolithus abi-
sectus towards the lower part of the NP23, well below the
FO of Sphenolithus ciperoensis. However, the absence of
Transversopontis fibula, Orthozygus aureus, Lanternitus
minutus and Chiasmolithus oamaruensis, which has the LO
in the upper part of NP23 (see Melinte 2005) makes it possi-
ble to include the given samples in Zone NP24.
Fig. 8. Calcareous nannofossil distribution in the Oligocene deposits of the SWTW.
Such an age determination is coeval with the results of
Garecka (2008) from the Silesian Nappe. Almost the same
nannofossil associations were described by Švábenická et al.
(2007) from the Fore-Magura, Ždánice-Subsilesian and
Pouzdřany Units of the Czech sector of the Outer Carpathians.
Paleoecology
The described assemblages are characterized by the pres-
ence of both temperate (Dictyococcites bisectus, Cyclicar-
golithus floridanus, Coccolithus pelagicus, Coccolithus
eopelagicus) and typically cold-water taxa such as Isthmo-
lithus recurvus, Reticulofenestra lockerii, Reticulofenestra
ornata (see Wei & Wise 1990; Nagymarosy & Voronina
1992; Oszczypko-Clowes 2001). The latter two species had
their first occurrence in Zone NP23, which probably indi-
cates another drop in the temperature of water masses.
The assemblages are scarce in species of Helicosphaera,
Sphenolithus and Discoaster (Figs. 7, 8). These species are
typical warm water indicators and occur only sporadically.
The distribution of Reticulofenestra ornata, Transversopntis
fibula and Transversopntis latus is limited not only in time
O L I G O C E N E
GRYBÓW NAPPE
DUKLA NAPPE
Tectonic units/lithostratigraphy
SUB-
GRYBÓW
BEDS
GRYBÓW MARL FORMATION
KROSNO BEDS
NP NP NP NP NP NP NP NP NP NP NP NP
NP NP NP NP NP NP
Nannofossils zones
Martini (1971)
24 24 24 24 24 23 23 23 24 24 24 24
24 24 24 24 24 24
Sample number
51/
03/N
52/
03/N
62/
03/N
53/
03/N
54/
03/N
55/
03/N
56/
03/N
57/
03/N
58/
03/N
59/
03/N
60/
03/N
61/
03/N
63/
03/N
64/
03/N
1/
05/N
2/
05/N
3/
05/N
4/
05/N
5/
05/N
6/
05/N
7/
05/N
8/
05/N
9/
05/N
10/
05/N
Braarudosphaera bigelowii
– – –
X X – X – X – – X X X
Coccolithus eopelagicus
– – –
X X X X X – X X – X X – X – X X X X X
Coccolithus pelagicus
– – – X X X X X X – X X – X X – X – X X X X X
Cyclicargolithus abisectus
– – – X X X X X – – X X X – X – X X X X X
Cyclicargolithus floridanus
– – – X X X X X X – X X – X X X – X – X X X X X
Cyclicargolithus luminis
– – – – X
– X
– –
Dictyococcites bisectus
– – – X X X X X X – X X – X X X – X – X X X X X
Discoaster sp.
– – – X
X
X
– X
– –
Discoaster tanii
– – – X
X
X
– – –
Discoaster tanii nodifer
– – – X
X
X
– – –
Ericsonia fenestrata
– – – X X X X X – – X X – – X X X
Ericsonia formosa
– – – R R R – – – –
Helicosphaera compacta
– – – X X
– – X
– –
Helicosphaera euphratis
– – – X X
– – – – X
Helicosphaera recta
– – – X X
– – – –
Isthmolithus recurvus
– – – X X X X X – X X – X X X – – X X X
Lanternithus minutus
– – – R R R R X – X X – X R – – X X X
Neococcolithes dubius
– – – X X
X
X
– X
– –
Pontosphaera lateliptica
– – – X
– – –
Pontosphaera plana
– – –
– – –
Reticulofenestra dictyoda
– – – X X X X – X X – X – – X X X
Reticulofenestra lockerii
– – – X X – X – X – – X X X
Reticulofenestra minuta
– – – X X X – X X – X X – – X X X
Reticulofenestra ornata
– – – X X X X X X – X X – X X – – X X X
Reticulofenestra umbilica
– – – R – R R – R – – R R R
Sphenolithus dissimilis
– – – – – – –
Sphenolithus moriformis
– – – X X X X X – X X – X X – – X X X
Sphenolithus pseudoradians
– – – X
– X
– – –
Sphenolithus radians
– – – R
R
R R
–
R
R
– R
– –
Transversopontis pulcheroides
– – – X X
– – – –
Zygrhablithus bijugatus
– – – X X X X X X – X X – X X X – X – X X X X X
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Fig. 9. Correlation of Oligocene and Early Miocene stages (Berg-
gren et al. 1995) with Central Paratethys stages (Cicha et al. 1998),
modified.
but also in space (to the Paratethys region). The above-men-
tioned association is strictly characteristic for Zone NP23
(Nagymarosy & Voronina 1992).
So far the species Transversopntis fibula and Transversopntis
latus were not found in the nannofossil association from GMF
from the SWTW. At the same time the assemblages of GMF
are characterized by an abundance of Reticulofenestra ornata
which prove that in the higher part of NP23 there was a dis-
tinct drop in salinity, which led to the development of the
brackish-water environment (see Nagymarosy & Voronina
1992; Krhovský et al. 1992; Oszczypko-Clowes 2001; Soták
et al. 2001; Melinte 2005; Švábenická et al. 2007). This event
is associated with the complete isolation of the Paratethys
(Baldi 1980; Rusu 1988; Rögl 1999) and can be traced in both
the Central (Chert Member and Dynów Marl of Menilite For-
mation in Ždánice-Pouzdřany Unit, see Krhovský 1981a,b;
Krhovský et al. 1992; Soták 2001) and Eastern Paratethys
(Polbinian horizon, see Nagymarosy & Voronina 1992).
Close to the NP23/24 boundary, open-marine, calcareous
nannofossil assemblages have developed again. Zone NP24
is characterized by the presence of rich and highly diversi-
fied assemblages dominated by mid-latitudinal species (Dic-
tyococcites bisectus, Coccolithus eopelagicus, Coccolithus
pelagicus, Cyclicargolithus abisectus, Cyclicargolithus
floridanus).
At the same time the typical low-salinity species of Reticu-
lofenestra ornata are becoming much less abundant. Such
assemblages indicate that, at the turn of NP23/24, the normal
salinity condition in the Grybów Sub-basin was restored and
the connection between the Paratethys and the North Sea as
well as with the Mediterranean region was re-established
(see Baldi 1980; Rusu 1988; Rögl 1999; Popov et al. 2003;
Schulz et al. 2005).
Tectonics
The SWTW (Figs. 2, 10) is located in axial part of the
broad, NWN-SES trending Krępna-Świątkowa Wielka anti-
cline; composed of the Ropianka Formation (Inoceramian
Beds, Late Cretaceous—Paleocene). From the south and north
refolded, broad synclinal zones accompany this anticline.
The moderate inclined limbs of the anticline are composed
of narrow strips of the variegated shales of the Łabowa Shale
Formation (Paleocene—Middle Eocene), while relatively
broad and elongated synclines are filled by thick-bedded
glauconitic sandstones of the Wątkowa Beds (Late Eocene—
Oligocene) and Supra-Magura (Budzów) Beds (Oligocene).
The rocks of Grybów Nappe are arranged in several narrow
NW-SE trending, imbricated folds. The axes of the anticlines
and synclines plunge to the NW and SE (Mastella & Rubin-
kiewicz 1998). The best exposures of the nappe are displayed
in the Krokowy Stream (Fig. 2). The SWS dipping, mainly
overturned beds of the GMF and Sub-Grybów Beds form
small pseudoanticlines and pseudosynclines. These small
structures are incorporated in seven mapped-scale (1 : 10,000)
thrust sheets (slices, see Mastella & Rubinkiewicz 1998). Us-
ing the same scale we mapped a narrow anticline, up to 50 m
wide composed of the Sub-Grybów Beds, while the limbs of
the fold belong to the GMF. The hinge of the anticline dis-
plays a horizontal hinge surface (Fig. 4B). The axes of the an-
ticline (W—E) gently (10°) plunge to the W. The hinge of the
anticline is thrust over the northern overturned limb. The
southern limb of the fold gently dips to the west. Going up ca.
400 m in the Krokowy Stream we cross the hinge of the syn-
cline, inclined (80°) to the SW and overturned (Fig. 5A,F).
The southern limb of the syncline is composed of GMF and
Sub-Grybów Beds. Towards the west we cross the WSW dip-
ping (250°/60°) tectonic contact of the Sub-Grybów Beds with
Krosno shales. The Krosno shales are exposed in the upper
course of the Krokowy Stream for a distance of ca. 500 m.
These beds show very strongly ductile deformation (kind of tec-
tonic mélange), with small folds (axes WSW—ENE, EW—SE
and sub-horizontal hinge surfaces), several shear zones, and
folded boudinaged layers. Sometimes the character of defor-
mation is chaotic (Fig. 6D). In the upper part of exposures the
Krosno shales contain boudines and beds of ferro-dolomitic
limestones, beds of laminated limestones and brecciated car-
bonate-build-up (Bojanowski 2007a,b). These limestones con-
tact with gently south dipping red shales of the Łabowa
Formation.
On the basis of our field and archival drilling data (Fig. 3, see
also Nawrocka-Gierat & Wdowiarz 1975, CGA PIG) two geo-
logical cross-sections, more or less perpendicular to the bound-
ary of the tectonic window, have been constructed (Fig. 10).
These cross-sections illustrate a relationship of the Grybów
Nappe to the Magura Nappe and basement of these units.
The sole thrust of the Grybów Nappe was reached at a depth
of 74 m (Sw2 borehole) through to 491 m (Sw1 borehole),
which’s 366 m a.s.l. and 38.5 m b.s.l., while the top of the
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Fig. 10. Geological cross-sections through the Świątkowa Wielka Tectonic Window.
Dukla Nappe was pierced at a depth of 164 m (Sw2) to 491 m
(Sw1), 276 m a.s.l. to 38.5 m b.s.l. (Figs. 3, 10). Between the
Grybów Nappe and Dukla Nappe the 62—90 m block of the
Magura Nappe was found in boreholes Sw2 and Sw3 (Figs. 3,
10). The pierced beds belong to variegated shales (Łabowa
Shale Formation) and the Ropianka Formation of the Magura
Nappe. In borehole Sw3 inside the variegated shales, a 13 m
thick block of GMF was found. In this borehole beneath the
lower portion of the variegated shales and above the top of the
upper Krosno Beds of the Dukla Nappe, a 51 m packet of “fos-
sil slump” was drilled (Tokarski 1965). At same time in the
borehole Sw4 the mentioned block of the Magura Nappe is re-
placed by Hieroglyphic and Sub-Grybów Beds probably both
belonging to the Grybów Nappe.
The analysis of the cross-section (Fig. 8) anabled new
structural interpretation of the SWTW window:
1. The Grybów Nappe of the SWTW and Magura Nappe of
the northern part of the winow are flatly overthrust upon the
Grybów and Magura Nappes of the southern part of SWTW.
2. The very strongly deformed Krosno shales exposed in
the upper course of the Krokowy Stream and edged between
the Magura Nappe and Sub-Grybów Beds of the Grybów
Nappe are in the “out of sequence” position.
3. The brecciated rocks of the “fossil slump” (Figs. 3, 10)
edged between the Variegated Shales of the Magura Nappe and
Upper Krosno Beds of the Dukla Nappe in the boreholes Sw3,
probably represent a detached fragment of the Dukla Nappe.
4. The present-day structure of the SWTW is a result of the
retro-thrust of the Magura and Grybów Nappes towards the
south. The amplitude of this ovethrust is at least 1.5 km.
Disscusion
In the following tectonic windows (Grybów Nappe, Mszana
Dolna, Szczawa, Grybów, Ropa and Świątkowa Wielka) we
found the Oligocene strata belonging to the Sub-Grybów
Beds, Grybów Marl Formation (GMF) and Krosno Beds
(Fig. 11). All these strata occur above the Sub-Menilite Globi-
gerina Marls. The oldest strata represented by Hieroglyphic
Beds were probably pierced in the Sw4 borehole in the
Światkowa Wielka (Gierat-Nawrocka & Wdowiarz 1975).
The lower part of the Grybów succession, belonging to the
Sub-Grybów Beds, is dominated by non-calcareous grey and
greenish mudstones and shales, with packets of the black and
brown Menilite-type shales.
The most typical deposits of the tectonic windows belong to
the GMF. This formation is composed of dark grey, black and
dark brown muddy marls. In the lower part of the formation
the marls with intercalations of thin- to medium-bedded tur-
bidite sandstones are present, while the upper part is dominat-
ed by thick-massive marl and thick-bedded Cergowa-type
sandstones. Subordinately, this formation contains lenses or
beds of the ferruginous dolomitic limestones (Fig. 11). In the
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Szczawa, Grybów and Ropa Tectonic Windows the thickness
of the formation is up 200 m, while in the SWTW and Smilno
Tectonic Windows (see Nemčok et al. 1990) the thickness os-
cillated around 100 m (Fig. 10). The lower boundary of the
formation is transitional, while the upper boundary is repre-
sented by a horizon of silicites (horstones) (Fig. 11) with dif-
fernt thicknesses, varying from 10 cm in Szczawa up to 10 m
on the Smilno site (see Nemčok et al. 1990). In the Ropa sites
the horstone horizon is replaced by black siliceous marls
(Oszczypko-Clowes 2008). The upper part of the succession is
occupied by shally facies of the Krosno Beds at least 100 m
thick. The Grybów succession correlate well with the succes-
sion of the Smilno Tectonic Window in Eastern Slovakia
(Fig. 11, see also Nemčok 1990; Nemčok et al. 1990).
In the Smilno Beds, which can be regarded as the equiva-
lent of the Grybów Marl Formation, Nemčok et al. (1990)
described the thick-bedded “Kliwa” sandstones. This type of
non-calcareous, quartz rich sandstone can be correlated with
the same sandstones from the lower part of the GMF and
Sub-Grybów Beds in the western part of the Światkowa
Wielka section (Fig. 11).
The Rupelian sequences of the Grybów succession (Sub-
Grybów and GMF) of the SWTW as well as the correlative
deposits of the other tectonic window of the Polish sector of
the Magura Nappe were deposited during the TA4 supercy-
cle (Haq et al. 1988), resulting in a gradual rise of the rela-
tive sea level. The climatic and sequence-stratigraphy
changes in the Central Carpathian Paleogene Basin during
this supercycle have been defined by Soták et al. (2001).
These changes can also be applicable to the depositional en-
viroments of the Menillite and Krosno Beds in the Outer
Carpathian sedimentary area. The transgressive stage (TST)
of the supercycle in the Grybów Sub-basin was probably
marked by the deposition of menilite shales with green-inter-
clations (Fig. 4A—D) of Sub-Grybów Beds and the basal por-
tion of the GMF with the begining of the reticulofenestrides
bloom. The highstand system tract (HST), with massive
mud-rich marly megaturbiditic beds is typical for the main
portion of GMF with the chert and siliceous marls at the top.
The TB1 lowstand wedge (LSW) (see Soták et al. 2001) is
marked by the beginning of the deposition of the shally
Krosno Beds (Fig. 1) (NP24—NP25) zone.
Fig. 11. Correlation logs of the Grybów succession. Profile of the Smilno Tectonic Window after Nemčok (1990) and Nemčok et al.
(1990). Abreviations: TL – Tylawa Limestone, JL – Jasło Limestone.
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The SWTW developed during multi-stage evolution
(Fig. 10). This process was probably initiated during the lat-
est Oligocene when the Magura Nappe was thrusted onto the
Fore-Magura (Dukla and Grybów) sedimentary area. The
overthrusting was probably realized under the submarine
condition (see Oszczypko-Clowes & Oszczypko 2004). As a
result the Magura Nappe, at least 2.5—3 km thick, loaded and
sealed under compacted clayey-sandy deposits of the Grybów
succession and shally upper Krosno Beds of the Dukla
Nappe. This caused the appearance of an over pressured (see
Oszczypko-Clowes & Oszczypko 2004; Bojanowski 2007b)
zone along the contact between the Magura, Grybów and the
Dukla Nappes. This zone, represented by the Krosno shally
facies, was affected by a fracturing and frictional sliding and
formation of tectono-sedimentary breccia. This type of brec-
cia is also known from the Mszana Dolna Tectonic Window,
as well as from deep boreholes Smilno 2 and Zborov 1 in the
E Slovakia sector of the Magura Nappe (Leško et al. 1987).
The successive Magura Nappe overthrusting during the Mid-
dle Miocene (Oszczypko 2006; Oszczypko-Clowes et al.
2009) against the Grybów and Dukla Nappes was formed as
a classical contractional inter-thrust duplex between the
Magura and Dukla Nappes (Mastella & Rubinkiewicz 1998)
with several, refolded horses. In the SWTW the latest over-
thrust movement is documented by the retro-sharing of the
Magura and Grybów Nappe of the northern limb of the win-
dow over the Magura Nappe of the southern none. This was
probably connected with the exhumation of the upper Krosno
Beds breccia from the top of the Dukla Nappe to the
Krokowy Stream. This event probably took place during the
latest post Sarmatian thrust movements in the Northern
Outer Carpathian (see also Mastella & Rubinkiewicz 1998;
Oszczypko-Clowes et al. 2009). The post nappe collapse of
the Magura Nappe was accompanied by the development of
the normal transversal faults (Figs. 2, 10A—B).
The present-day structure of the SWTW is related to the
culmination of the basement of the Magura and Dukla stack
of nappes.
To the east of the Dunajec River, the Magura Nappe is
flatly overthrust upon its foreland (Fig. 1B). The undulation
of the base of the Magura Nappe is well marked in the fron-
tal thrust, forming characteristic “embayments” and “peninsu-
las” (Zuchiewicz & Oszczypko 2008). The first refers to the
uplifted parts of the foreland and the second coincides with
transversal depressions, but differences between the “embay-
ments” and “peninsulas” do not exceed 250 m. Some 10—15 km
south of the Magura frontal thrust, a belt of tectonic windows
located upon a longitudinal basement elevation is to be found.
This zone, 1—6 km wide, begins on the west in the Klęczany-
Pisarzowa Window, and continues farther east through a half-
window north of Nowy Sącz, and the Grybów-Ropa-Uście
Gorlickie and Świątkowa and Kotoń Windows (Fig. 1). To the
south of the Uście Gorlickie and Świątkowa Tectonic Win-
dows, the base of the Magura Nappe rapidly slopes down to ca.
3300 m b.s.l. in Zborov-1 (ca. 2 km S of window) 4200 m b.s.l.
in Smilno-1 (ca. 3 km W of window) well in Slovakia (Leško et
al. 1987). This suggests that the Smilno Tectonic Window, like
the Świątkowa Wielka one, is probably detached from its base-
ment and embedded into the Magura thrust-sheets.
Conclusions
1. The studied section of the Świątkowa Wielka Tectonic
Window is composed of the Dukla and Grybów Nappes. The
Dukla Nappe is represented by shaly facies of the Krosno
Beds, while the Sub-Grybów Beds and Grybów Marl Forma-
tion belong to the Grybów Sub-Nappe. We found the same
tectonic sequence in the Mszana Dolna Tectonic Window.
2. In the Mszana Dolna and Świątkowa Wielka Tectonic
Windows the age of the Krosno Beds of the Dukla Nappe
has been determined as NP24.
3. The typical Oligocene sequence of the Grybów Sub-
Nappe is composed of Sub-Grybów Beds, Grybów Marl For-
mation and Krosno Beds with the exception of the
Świątkowa Wielka Tectonic Window.
4. The youngest deposits of the Grybów Sub-Nappe succes-
sion in the Świątkowa Wielka Tectonic Window belong to the
Grybów Marl Formation and represent Zones NP23—NP24.
The same results were obtained from the same deposits in the
Mszana Dolna Tectonic Window. In the Grybów and Ropa
Tectonic Windows the youngest age (Zone NP25) was deter-
mined in the Krosno Beds.
5. The abundance pattern and the species diversity of nan-
noplankton assemblages reflect temperate to coldish temper-
atures in the surface water of the Grybów Basin.
6. At the base of the Magura Nappe in the Mszana Dolna
and Świątkowa Wielka Tectonic Windows the chaotic rocks
of the breccia type were recognized.
7. In the case of the Świątkowa Wielka Tectonic Window
these brecciated rocks probably represent a detached frag-
ment of the Dukla Nappe, exhumed during the retro-thrust
movement of the Magura Nappe towards the south. The am-
plitude of this ovethrust is at least 1.5 km.
Acknowledgments: The authors express their thanks to Drs.
M.C. Melinte, M. Cieszkowski and J. Soták for their con-
structive comments, which improved this paper. Thanks are
extended to Drs. W. Ryłko and W. Rączkowski who gave us
access to archival drilling data. Special thanks to Dr. David
Clowes for English editing of our manuscript. The research
was financed by Jagiellonian University – DS/ING 808.
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