GEOLOGICA CARPATHICA
, AUGUST 2018, 69, 4, 347–364
doi: 10.1515/geoca-2018-0021
www.geologicacarpathica.com
Depositional architecture of marginal multiple-source
ramp of the Magura Basin (Eocene Flysch formation,
Outer Western Carpathians)
EWA WÓJCIK
, MAGDALENA ZIELIŃSKA, RYSZARD CHYBIORZ and JERZY ŻABA
Faculty of Earth Sciences, University of Silesia in Katowice, Będzińska St. 60, Sosnowiec 41-200, Poland;
ewa.wojcik@us.edu.pl
(Manuscript received July 13, 2017; accepted in revised form May 31, 2018)
Abstract: The Zembrzyce Beds were studied to interpret the environments and facies in the western part of the Siary
Subunit. New sedimentological data were obtained for the reconstruction of the depositional architecture of
the Zembrzyce Beds. Based on detailed facies analysis, 9 facies and 4 facies associations were recognized. The facies
associations represent different architectural elements of a submarine fan, such as: termination of distributary channel
with transition to depositional lobe (distal part of mid-fan /outer fan sub-deposystem), lobes and distal lobes (outer fan
sub-deposystem). According to the classification of Reading & Richards (1994) the fan deposystem can be classified as
mud /sand-rich ramp. This system consists of several elongated lobes that formed synchronously, migrated laterally, and
then retreated or decayed. The depositional system was supplied from the north and north-east. The inner-fan sub-
deposystem was not detected. The sediments were deposited by high- and low-density turbidity currents and hyper-
concentrated density flows sensu Mulder & Alexander (2001) with participation of the depositional background processes
(pelagic settling). The sedimentary conditions of the Zembrzyce Beds during the Late Eocene were controlled by tectonic
movements, the progress of the subduction and the global sea level changes.
Keywords: Outer Carpathians, Siary Subunit, Zembrzyce Beds, depositional architectural elements, Eocene, turbidites.
Introduction
The Zembrzyce Beds occurring in the Magura Unit are typical
member of the Siary Subunit. In the Polish part of the Magura
Unit, the Zembrzyce Beds outcrop in many localities and were
described by: Książkiewicz 1935, 1970, 1974; Burtan et al.
1959; Golonka & Wójcik 1978a, b; Oszczypko & Wójcik 1989;
Ryłko et al. 1992; Paul 1993; Wójcik & Rączkowski 1994;
Oszczypko-Clowes 2001; Chodyń 2002; Leszczyński &
Malata 2002; Gdel & Leszczyński 2005; Cieszkowski et al.
2006; Kopciowski 2007, 2014, 2015; Warchoł 2007; Ryłko &
Paul 2013; Jankowski & Kopciowski 2014; Kopciowski et al.
2014a, b; Nescieruk & Wójcik 2014.
The Zembrzyce Beds (Middle–Late Eocene), also known as
the Zembrzyce Shale Member (Cieszkowski et al. 2006;
Golonka & Waśkowska-Oliwa 2007; Golonka & Waśkowska
2011), consist mostly of massive, marly shales (seldom clayey
shales), mudstones, and marls interbedded by glauconitic
sandstones. The thickness of the Zembrzyce Beds is up to
500 metres (Cieszkowski et al. 2006; Golonka & Waśkowska-
Oliwa 2007). In literature the Zembrzyce Beds are also called
as the Sub-Magura Beds (Paul 1980, 1993; Oszczypko et al.
1999; Chodyń 2002; Oszczypko-Clowes 2001; Ryłko & Paul
2013; Jankowski & Kopciowski 2014; Kopciowski et al.
2014a, b) and this term is used in older publications. What is
more, sedimentological research carried out by various authors
including Golonka & Wójcik 1978a, b; Golonka 1981;
Cieszkowski et. al. 1985, 2006; Oszczypko et al. 2005 in
the area of the Siary Subunit identified its lithological discre-
pancy between the western and eastern part. Initially 3 separate
lithostratigraphic units were distinguished: the Sub-Magura
Beds (Książkiewicz 1935), Magura Sandstones (Paul 1868) or
Magura Beds (Książkiewicz 1966) and Supra-Magura Beds
(Książkiewicz 1966) in the western part. Next Książkiewicz
(1974) included all these 3 units in the Magura Beds and
proposed to change the name: Sub-Magura Beds into
the Zembrzyce Shales and Supra-Magura Beds to Budzów
Shales. In the eastern part of the Siary Subunit, all these sedi-
ments were classified as Magura Beds (Leszczyński & Malata
2002). Koszarski & Koszarski (1985) applied the name of
Wątkowa Sandstones for the Magura Sandstones, and
Bromowicz (1992) for the shaly upper part of the Magura
Beds applied the name of Małastów Shales in the eastern part
of the Siary zone. What is more, Oszczypko et al. (1999),
Oszczypko-Clowes (1999, 2000, 2001) and Malata (2001)
mentioned the units included by Książkiewicz (1974) to
the Magura Beds as the Zembrzyce Beds, the Wątkowa Sand-
stones and the Budzów Beds respectively. Consequently,
the designation of the Zembrzyce Beds is currently used
because of the presence of greyish-green shales for which
the stratotype profile is located near Zembrzyce village.
Opinions and information on the depositional system that
produced the Zembrzyce Beds are still inconsistent and
incomprehensive. Leszczyński & Malata (2002) interpret
the Magura Beds as a ramp deposit that gradually developed
towards the SE and E along the base of the basin slope.
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, 2018, 69, 4, 347–364
Kopciowski (2007) in the eastern part of the Siary Subunit
attributes the Zembrzyce Beds to a point source, mud-rich
submarine fan, which is a continuation of hemipelagic varie-
gated shales sedimentation, but above the calcite compen-
sation depth (CCD) zone. Warchoł (2007) in the same area,
describes the Magura Beds as a system of linearly supplied
ramps. The author also suggests not to divide the Magura Beds
into Zembrzyce Shales (Szymbark Shales), Wątkowa Sand-
stones and Budzów Shales (Małastów Shales), and the exis-
ting tripartite division should be to apply only in exceptional
cases.
The common feature of the theories about the deposition of
the Zembrzyce Beds is that these sediments were deposited by
different mass gravity transport processes and indicate sedi-
mentation in a deep-marine environment.
Up to now research on the Zembrzyce Beds was concerned
primarily with lithology, stratigraphy and tectonics. The lack
of comprehensive sedimentological research on the Zembrzyce
Beds and the ambiguity about the Zembrzyce Beds deposi-
tional system have become the basis for analysis of the facies
and depositional architecture of the Zembrzyce Beds.
This paper presents a depositional model for the Zembrzyce
Beds in the marginal part of the Magura Unit (the Siary
Subunit). Developing the model required the lithological ana-
lysis of the Zembrzyce Beds, bed by bed, and the recon-
struction of the sedimentary basin. The sedimentary material
of the Zembrzyce Beds and the geological history of the Magura
sedimentary basin were the main subjects of the study.
Sedi ment properties, such as lithology, sedimentary structures
and textures, were used to recognize the sedimentation pro-
cesses. Palaeotransport measurements were used to determine
the direc tion of currents transporting clastic material within
the Magura Basin (the Siary Subunit) and to reconstruct
the source areas for the Zembrzyce Beds. Modelling the ele-
ments of the depositional architecture of the Zembrzyce Beds
depended on correlating the lithological features of the sedi-
ments with the deposition mechanisms, palaeotransport direc-
tions and stratigraphy.
The study area is located in the western segment of the Siary
Subunit, to the south of Żywiec, in Jeleśnia village (Fig. 1).
Geological background
The Outer Western Carpathians are composed of sediments
of marine origin. These are mainly alternating sediments of
conglomerates, sandstones, mudstones, and claystones, with
subordinate beds of marls and limestones, which were folded
in the Palaeogene and Neogene and overthrust as nappes to
the north. The Outer Carpathians are made up of a stack of
nappes and thrust sheets showing different lithostratigraphy
and tectonic structures. Generally each Outer Carpathian
nappe represented separate or partly separate sedimentary sub-
basins (e.g., Oszczypko & Ślączka 1985; Nemčok et al. 1989,
2001; Vašíček et al. 1994; Golonka & Krobicki 2001; Golonka
2004; Ślączka et al. 2006; Golonka et al. 2008; Kováč et al.
2017). Within the Outer Carpathian sedimentary basin, there
were ridges, which recorded periods of sinking and uplifting
corresponding to the tectono-stratigraphic stages of the Car-
pathians orogenic regime. Ridges formed the primary source
of clastic material for the Outer Carpathian depositional sys-
tem, and in the inversion phases, the ridges divided the Outer
Carpathian basin into a number of sub-basins (e.g., Oszczypko
1999, 2004). The Zembrzyce Beds were deposited in the Siary
Subunit (northernmost subunit of the Magura Unit), and
the source of the clastic material was the Silesian Cordillera,
situated to the north (Leszczyński & Malata 2002; Oszczypko
et al. 2006; Kopciowski 2007; Warchoł 2007).
The Magura Unit is the largest and the southernmost tec-
tonic unit in the Outer Carpathians. Within the Magura Unit,
the subunits were distinguished based on the differences in
sediments and facies succession. Starting from the south,
the subunits are as follows: the Krynica Subunit, the Bystrica
Subunit, the Rača Subunit, and the Siary Subunit (e.g.,
Książkiewicz 1958; Świdziński 1958; Sikora 1970; Oszczypko
1973; Koszarski et al. 1974; Żelaźniewicz et al. 2011)
(Fig. 1B). However, it must be emphasized that the boundaries
between the subunits are tectonic (faults, overthrusts) and that
they have not been precisely located and defined throughout
the full extent of the Magura Unit (Oszczypko 1973;
Książkiewicz 1977).
Siary Subunit lithostratigraphy
The Siary Subunit consists mostly of Palaeogene sediments
with subordinate Cretaceous deposits (Fig. 1C, D). In the area
of the Polish Outer Carpathians, the Siary Subunit reveals its
facial differentiation between the eastern and western parts
with the border at the Dunajec river. The eastern part’s profile
is dominated by thick-bedded glauconite Magura sandstones
— Wątkowa Member, and the equivalent of the Zembrzyce
Beds are the Szymbark Beds (Kopciowski 1996, 2007;
Leszczński & Malata 2002; Leszczyński et al. 2008; Warchoł
2007). The marly shales and cross-bedded sandstones belon-
ging to the upper part of Magura Beds was called by Bromowicz
(1992) the Małastów Shales and they are the equivalent of
the Budzów Beds characteristic of the western part of the Siary
Subunit. In the western part the Zembrzyce Beds and Budzów
Beds predominate, interbedded by the glauconite Magura
sandstones (Cieszkowski et al. 2006; Warchoł 2007). Further
west, in the territory of Slovakia, the Outer Rača Subunit is
a synonym of Siary Subunit and the equivalent of Zembrzyce,
Magura and Budzów Beds is the Zlín Formation (Middle/Late
Eocene) (Cieszkowski et al. 2006; Teťák 2010; Teťák et al.
2016). Glauconitic sandstones are typical for the Vsetín
Member (Zlín Formation). Intercalations of glauconitic sand-
stones and greywacke Magura type sandstones are typical for
the Babiše Member (Zlín Formation) (Teťák 2010).
The typical Siary Subunit’s lithostratigraphic succession in
the study area starts with the Ropianka Formation (Senonian/
Palaeocene) (Fig. 1D), with medium and thin beds of fine-
grained calcareous sandstones. The sandstones are overlain by
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EOCENE MARGINAL MULTIPLE-SOURCE RAMP OF THE MAGURA BASIN (OUTER WESTERN CARPATHIANS)
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, 2018, 69, 4, 347–364
PL
UA
MD
RO
BG
SRB
BIH
HR
H
SK
CZ
A
1
2
3
4
5
6
7
8
1. Outer Western Carpathians
2. Inner Western Carpathians
3. Outer Eastern Carpathians
4. Inner Eastern Carpathians
5. Southern Carpathians
6. Western Romanian
Carpathians
7. Transylvanian Plateau
8. Serbian Carpathians
A
B
Su
Ru
Bu
Ku
Zakopane
Żywiec
Kraków
Miocene of the Carpathian
Foredeep
Carpathian Foreland
Outer
Western
Carpathians
Western
Inner
Carpathians
CZECHIA
POLAND
SLOVAKIA
B
C
6
Fa
ult
Koszar
aw
a
Sopotnia
W
ielka
Fig. 1. Location of the study area. Explanations: A — Divisions of the Carpathians (after Kováč et al. 1998, simplified); B — Schematic
tectonic map of the Outer Western Carpathians (after Żytko et al. 1988-1989; Oszczypko et al. 2008; Żelaźniewicz et al. 2011; simplified);
C — Geological map of Jeleśnia (after Golonka & Wójcik 1978a; Golonka et al. 1979; modified): 1 — Krosno Beds, 2 — Barutka Marls,
3 — Supra-Magura Beds (Budzów Member — after Golonka 1981; Cieszkowski et al. 2006), 4 — Magura Sandstones (Wątkowa Member
— after Golonka 1981; Cieszkowski et al. 2006), 5 — Sub-Magura Beds (Zembrzyce Beds — after Cieszkowski et al. 2006), 6 — Hieroglyphic
Beds, 7 — Łabowa Shale Formation, 8 — Ciężkowice Sandstones (Skawce Member — after Cieszkowski et al. 2006), 9 — Pasierbiec
Sandstones, 10 — Beloveža Beds (Beloveža Formation — after Oszczypko 1991; Pivko 2002; Oszczypko et al. 2005), 11 — Łącko Formation,
12 — Mutne Member, 13 — Krzyżowa Member, 14 — Jaworzynka Formation — after Oszczypko et al. 2005; Cieszkowski et al. 2006,
15 — Ropianka Formation — after Oszczypko 1991; Pivko 2002, 16 — Cebula Formation — after Pivko 2002, 17 — Cisownica Shales;
Detailed Geological Map on the scale 1:50,000, sheet: a — Nescieruk & Wójcik 2014; b — Ryłko & Paul 1997; c — Burtan et al. 1959;
d — Golonka & Wójcik 1978a; D — Lithostratigraphic profile of the Siary Unit in the Jeleśnia area: number from 3 to 8 and from 12 to 15 see
Fig. 1C (after Burtan et al. 1959; Golonka & Wójcik 1978a; Ryłko & Paul 1997).
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WÓJCIK, ZIELIŃSKA, CHYBIORZ and ŻABA
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marly and sandy-muddy shales (Sikora & Żytko 1959; Golonka
& Wójcik 1978a, b; Golonka 1981). Within the Ropianka
Formation, there are lithosomes of thick-bedded coarse-grained
sandstones from Krzyżowa (Krzyżowa Member, Senonian/
Palaeocene) (Golonka & Wójcik 1978a, b). In the north- western
part of the Siary Subunit, the Ropianka Formation becomes
interfingered with the Jaworzynka Formation of medium
bedded sandstones with interbeds of shale. In the upper part
of the Jaworzynka formation, there are thick-bedded coarse-
grained and gravelly sandstones from Mutne (Mutne Member,
Palaeocene) (Sikora & Żytko 1959; Golonka & Wójcik 1978a, b;
Golonka 1981; Chodyń 2002). Next, the profile consists of
Eocene variegated shales (Łabowa Shale Formation), with
occurrences of coarse or gravelly sandstones (Ciężkowice
Sandstones, Skawce Member, Cieszkowski et al. 2006)
belonging to the early Eocene (e.g., Książkiewicz 1966, 1974).
Stratigraphically, above the Łabowa Formation are the Hiero-
glyphic Beds (Middle/Upper Eocene according to Książ-
kiewicz 1974; Beloveža Beds according to Cieszkowski et al.
2006), composed predominantly of medium and thin bedded
shales with thin-bedded sandstones. The Hieroglyphic Beds
are covered by the Zembrzyce Beds of Middle Eocene–Upper
Eocene age (Cieszkowski et al. 2006). Within the Zembrzyce
Beds, grey and green marly shales and greyish-blue marls
dominate (Książkiewicz 1974; Oszczypko-Clowes 1999, 2001).
The thickness of the shale beds is from 0.5 to 2.5 metres.
Between shales and marls packages, there are medium-bedded
to thick-bedded glauconite sandstones from 20 centimetres to
1 metre thick. The ratio between shales and sandstones is 3:1
in average and it decreases up the profile. The Zembrzyce
Beds are covered by the Magura Sandstones (Late Eocene–
Oligocene, Wątkowa Member, Golonka 1981; Cieszkowski et
al. 2006).
The Siary Subunit profile ends with the Supra-Magura Beds
(Budzów Member by Golonka 1981; Cieszkowski et al. 2006)
of Oligocene age. These are mainly marly shales, sandy-muddy
shales, and spongiolites, with subordinate medium and fine-
grained mica sandstones (Kopciowski 1996; Oszczypko-
Clowes 2001).
The Zembrzyce Beds (Zembrzyce Shale Member), Magura
Sandstones (Wątkowa Sandstone Member), and Supra-Magura
Beds (Budzów Shale Member) belong to the Makowska
Formation according to Cieszkowski et al. (2006).
Tectonics of the study area
Within the study area, the main structural element is the Bystra-
Pewel Wielka anticline (Fig. 1C), which borders the Kiczory-
Bąkowa syncline to the north and the Zagrodzki Groń syncline
to the south (Golonka & Wójcik 1978a, b). The axes of
the anticlines and synclines run in the SW–NE direction.
Transverse dislocations play a major role (Golonka &
Wójcik 1978a, b; Golonka 1981). These are dip-slip and strike-
slip faults. In the study areas the large dip-slip type Głucha–
Jeleśnia fault runs from the north to Slovakia (Golonka &
Wójcik 1978a).
Methods
During the field studies, which were carried out in the natural
exposures of the Sopotnia stream, 11 (in total ca. 76 metres
long, bed by bed) detailed sedimentological logs of the
Zembrzyce Beds were made (Appendix 1 and 2). Logging
included the description of sedimentary structures and tex-
tures, description of colour and thickness of rock layers, HCl
response, dip and strike measurements, and where possible,
palaeotransport direction. The succession sections where
overthrusts were observed were omitted in the interpretation
of the Zembrzyce Beds depositional architecture.
The next step was to distinguish facies based on lithological
features such as: grain size, thickness of beds, character of bed
boundaries, and the average sandstone to mudstone ratio
within the succession. Names of facies were based on facies
codes in classifications of Mutti & Ricci Lucchi (1972, 1975);
Walker & Mutti (1973); Mutti (1979); Pickering et al. (1989);
Ghibaudo (1992) and Słomka (1995). Afterwards, within
facies, subfacies were distinguished based on sedimentary
structures (Table 1). Facies were grouped into facies associa-
tions (Table 2) using the textural and structural differences in
the facies’ vertical distribution.
The samples from Pewel Mała (sample no. 1), Jeleśnia
(sample no. 2) and Pewel Ślemieńska ( samples no. 3a, b)
were collected for micropalaeontological (nannoplankton)
investigations (Fig. 1C). The samples were derived from
olive or olivish-grey, grey and brown mudstones belonging to
the Zembrzyce Beds. The micropalaeontological analysis of
the samples was carried out by Prof. dr. hab. Barbara
Olszewska and Dr. Małgorzata Garecka (2011) from the Polish
Geological Institute — National Research Institute in Cracow.
For the nannoplankton examination all the samples were pre-
pared by the standard smear slide method for light microspore
observations. In addition, published results of microfauna
studies were used (Golonka & Wójcik 1978a; Golonka 1981;
Olszewska 1981; Leszczyński & Malata 2002).
The research permitted reconstruction of the depositional
environment of the Zembrzyce Beds south of the Żywiec and
the creation of a sedimentation model for these sediments.
Results
Facies of Zembrzyce Beds in the study area
Facies 1
Sediments belonging to Facies 1 represent medium to very
thick-bedded gravelly sandstones. Sandstone beds usually
show irregular basal surfaces covered with groove marks and
flute marks (Figs. 2 and 3A). Planar surfaces occur rarely as
well. The beds of this facies show: graded bedding and convo-
lute lamination. Horizontal lamination and wavy lamination
are less common. Facies 1 corresponds to subfacies A2.5,
A2.7, A2.8 of Pickering et al. (1989), facies GyS of Ghibaudo
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ASSOCIATIONS
FACIES
ENVIROMENT OF SEDIMENTATION
I
1, 2, 3, 4, 5, 6
termination of distributary channel passing upward into depositional lobe distal part of mid-fan/outer fan subdeposystem
II
2, 3, 4, 5, 6
muddy-sandy depositional lobe
outer fan subdeposystem
III
8, 9
distal part of depositional lobe (fan fringe lobes)
IV
7, 9
lower fan (fan fringe/basin plain)
(1992), and facies SC of Słomka (1995). Within Facies 1,
three subfacies were distinguished (Table 1). Sediments of
Facies 1 are interpreted as the results of rapid gravel-sand
deposition of high-density turbidity currents from suspension
with transition to traction (Ghibaudo 1992; Słomka 1995), or
from hyperconcentrated density flows (Pickering et al. 1989;
Mulder & Alexander 2001; Lowey 2007), which are
inter mediate between Newtonian fluid flow and Bingham
plastic flow (Nemec 2009).
Facies 2
Facies 2 consists mainly of medium to very thick-bedded
fine-grained sandstones. Within sandstone beds, there are mud
intraclasts as well as coalified plant detritus. The bottom sur-
faces of sandstone beds are planar or irregular (Figs. 2 and 3B).
The sandstones display horizontal lamination, cross lamina-
tion, convolute lamination and sometimes wavy lamination.
Sediments of this facies also display massive structure.
Table 1: Facies and subfacies description of the Zembrzyce Beds.
Table 2: Facies associations of the Zembrzyce Beds.
Facies
Subfacies
FACIES 1
GRAVELLY SANDSTONES
A2.5, A2.7, A2.8 (Pickering et al.1989); GyS (Ghibaudo 1992); SC (Słomka 1995)
1.1 normally graded gravelly sandstones to convolute-laminated sandstones
1.2 normally graded gravelly sandstones to horizontal and/or wavy-laminated and
convolute-laminated sandstones
1.3 normally graded gravelly sandstones
FACIES 2
SANDSTONES
B (Walker & Mutti 1973; Mutti & Ricci Lucchi 1975; Pickering et al. 1989);
C (Mutti 1979); S (Ghibaudo 1992; Słomka 1995)
2.1 massive sandstones
2.2 convolute-laminated sandstones
2.3 cross-laminated sandstones
2.4 horizontal-laminated sandstones
2.5 wavy-laminated sandstones
2.6 massive to horizontal-laminated and/or wavy-laminated and convolute-
laminated sandstones
FACIES 3
THICK-BEDDED TO VERY THICK-BEDDED SANDSTONE-MUDSTONE
COUPLETS
C and D (Walker & Mutti 1973; Mutti & Ricci Lucchi 1975); C2.1 (Pickering et al.
1989); SM (Ghibaudo 1992; Słomka 1995)
3.1 horizontal to wavy-laminated and cross-laminated sandstone-mudstone couplets
3.2 very thick-bedded massive to wavy-laminated and convolute-laminated
sandstone-mudstone couplets
3.3 convolute-laminated sandstone-mudstone couplets
3.4 thick-bedded massive to wavy-laminated and convolute-laminated sandstone-
mudstone couplets
FACIES 4
THIN-BEDDED TO MEDIUM-BEDDED SANDSTONE-MUDSTONE
COUPLETS
C and D (Walker & Mutti 1973; Mutti & Ricci Lucchi 1975); D1 (Mutti 1979);
C2.2 and C2.3 (Pickering et al. 1989); SM (Ghibaudo 1992; Słomka 1995)
4.1 massive to cross-laminated sandstone-mudstone couplets
4.2 massive sandstone-mudstone couplets
4.3 horizontal-laminated to convolute-laminated sandstone-mudstone couplets
4.4 convolute-laminated sandstone-mudstone couplets
4.5 wavy-laminated to convolute laminated sandstone-mudstone couplets
4.6 massive to convolute- laminated sandstone-mudstone couplets
4.7 horizontal-laminated sandstone-mudstone couplets
4.8 cross-laminated sandstone-mudstone couplets
4.9 wavy-laminated sandstone-mudstone couplets
4.10 massive to horizontal-laminated sandstone-mudstone couplets
FACIES 5
MUDSTONE-SANDSTONE COUPLETS
D (Walker & Mutti 1973); D2 (Mutti & Ricci Lucchi 1975; Mutti 1979);
C2.4 (Pickering et al. 1989); MS (Ghibaudo 1992; Słomka 1995).
5.1 cross-laminated mudstone-sandstone couplets
5.2 massive to horizontal-laminated and wavy-laminated mudstone-sandstone
couplets
5.3 convolute-laminated mudstone-sandstone couplets
5.4 massive to convolute-laminated mudstone-sandstone couplets
5.5 massive mudstone-sandstone couplets
5.6 cross-laminated to convolute-laminated mudstone-sandstone couplets
5.7 horizontal-laminated mudstone-sandstone couplets
FACIES 6
MUDSTONES AND SANDY MUDSTONES WITH MARLS
D2.3 (Pickering et al. 1986, 1989); MT (Ghibaudo 1992; Słomka 1995)
FACIES 7
MUDSTONES AND SANDY MUDSTONES WITH THIN-BEDDED SANDSTONES
FACIES 8
MUDSTONES AND SANDY MUDSTONES WITH IRREGULAR SANDSTONE LAYERS
E (Mutti 1979)
FACIES 9
MUDSTONES AND SANDY MUDSTONES
E2.2 (Pickering et al. 1986, 1989); TM and MT (Ghibaudo 1992); MT (Słomka 1995)
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Facies 2 corresponds to facies B of Walker & Mutti (1973) and
Mutti & Ricci Lucchi (1975); facies B of Pickering et al.
(1989); facies C of Mutti (1979); facies S of Ghibaudo (1992),
and facies S of Słomka (1995) (Table 1). These sediments are
characteristic for the rapid deposition of sandy high-density
turbidity currents with transition to traction (Ghibaudo 1992;
Słomka 1995) or they result from hyperconcentrated density
flows (Pickering et al. 1989; Mulder & Alexander 2001).
Facies 3
Facies 3 consists of sandstone-mudstone couplets, with
sandstones dominating. This facies forms bipartite beds that
comprise a lower sandy division and an upper muddy division.
The sandstone beds are 30–120 cm thick, whereas the thick-
ness of the mudstone beds ranges 15–20 cm. The thick-bedded
and very thick-bedded sandstones are fine-grained and show
planar or sometimes irregular basal surfaces (Figs. 2 and 3C).
Within sandstone beds, there are mud intraclasts as well as
coalified plant detritus. Beds of sandstones are characterized
predominantly by horizontal lamination, cross lamination and
convolute lamination. Some beds are wavy-laminated or
non-laminated. The interbeds of mudstones and sandy mud-
stones are characterized by parallel and wavy laminations.
Facies 3 corresponds to facies C and D of Walker & Mutti
(1973) and Mutti & Ricci Lucchi (1975); subfacies C2.1 of
Pickering et al. (1989); facies SM of Ghibaudo (1992), and
facies SM of Słomka (1995) (Table 1). These sediments are
a result of concentrated density flows (Pickering et al. 1989).
Facies 4
Facies 4 consists of sandstone–mudstone couplets, with
sandstones dominating (Figs. 2 and 3D). The medium and
thin-bedded sandstones are fine-grained. Sandstone beds show
planar or sometimes irregular basal surface. Coalified plant
detritus is observed within sandstones beds. Beds of sand-
stones usually show convolute lamination, cross lamination
and horizontal lamination. Massive structure and horizontal
lamination usually occur in the lower part of beds. Interbeds of
mudstones and sandy mudstones reveal parallel and wavy
laminations. Facies 4 corresponds to facies C and D of Walker
& Mutti (1973) and Mutti & Ricci Lucchi (1975); facies D1 of
Mutti (1979); subfacies C.2.2 and C.2.3 of Pickering et al.
(1989); facies SM of Ghibaudo (1992); and facies SM of
Słomka (1995). Within Facies 4, ten subfacies were distin-
guished (Table 1). Sediments of Facies 4 are interpreted as
a result of deposition of different-density turbidity currents
with rapid transition to traction of very fine-grained material
(Ghibaudo 1992; Słomka1995).
Facies 5
Sediments belonging to Facies 5 represent mudstone–sand-
stone couplets with mudstones dominating (Figs. 2 and 3E).
Beds show irregular or planar basal surfaces. The mudstone
layers are up to about 15–20 cm thick, whereas the thickness
of sandstone beds ranges from 6–12 cm. Mudstones and sandy
mudstones reveal parallel lamination. Sandstones are fine-
grained, with evidence of coalified plant detritus. The com-
monest subfacies are: cross-laminated mudstone–sandstone
couplets, convolute-laminated mudstone–sandstone couplets,
massive mudstone–sandstone couplets, massive to convolute-
laminated mudstone–sandstone couplets, massive to hori-
zontal-laminated and wavy-laminated mudstone–sandstone
couplets, cross-laminated to convolute-laminated mudstone–
sandstone couplets, horizontal-laminated mudstone–sandstone
couplets (Table 1). Facies 5 corresponds to facies D of Walker
& Mutti (1973); subfacies D2 of Mutti & Ricci Lucchi (1975);
subfacies C2.4 of Pickering et al. (1989); subfacies D2 of
Mutti (1979); facies MS of Ghibaudo (1992); and facies MS of
Słomka (1995). Within Facies 5, seven subfacies were distin-
guished (Table 1). Sediments of Facies 5 were formed by rapid
deposition of dilute turbidity currents with transition to trac-
tion, sometimes with reworking of very-fine detrital material
by bottom currents (Słomka 1995), or from low-density tur-
bidity currents (Ghibaudo 1992).
Facies 6
Facies 6 represents grey, greyish-olive, and brownish sandy
mudstones and mudstones with parallel lamination and occa-
sional interbeds of marls (Figs. 2 and 3F). Interbeds of mud-
stones and sandy mudstones reveal parallel laminations.
Facies 6 corresponds to facies D2.3 of Pickering et al. (1986,
1989); facies MT of Ghibaudo (1992); and facies MT of
Słomka (1995) (Table 1). The sediments of Facies 6 are inter-
preted as a result of fine-grained deposition laid down by sus-
pension or by low-density turbidity currents (Ghibaudo 1992;
Słomka 1995).
Facies 7
In facies 7, olive and grey mudstones with parallel lamina-
tion dominate over sandy mudstones. There are also thin-bed-
ded horizontal laminated and massive sandstones (Figs. 2 and
4A). Thin layers of cross-laminated sandstones occur occa-
sionally within facies 7. The mudstones are sandy to different
degrees. The sediments of Facies 7 are interpreted as a result
of deposition from suspension of fine-grained deposits
(Słomka 1995). This sedimentation was sometimes inter-
rupted by deposition from low-density turbidity currents.
Facies 8
Facies 8 consists of grey and rarely brown mudstones and
thin-bedded sandy mudstones. Within facies 8, there are very
thin bedded sandstones with wavy and cross lamination.
Sandstone beds show irregular surfaces (Figs. 2 and 4B).
The sediments of this facies correspond to facies E of Mutti
(1979) and they are interpreted as a result of deposition from
suspension of fine-grained deposits (Słomka 1995). This
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FACIES 1
1.1
1.2
1.3
2.1
2.2
2.3
2.4
3.1
M SFSMSC GF
M SF
2.5
2.6
FACIES 2
M SF
3.2
3.3
3.4
FACIES 3
FACIES 4
M SF
4.1
4.2
4.3
4.4
4.5
4.6
4.7
4.8
4.9
4.10
FACIES 5
M SF
5.1
5.2
5.3
5.4
5.5
5.6
5.7
FACIES 6
FACIES 7
FACIES 8
FACIES 9
M SF
M SF
M SF
M SF
Bedding plane:
Rock color:
sharp, planar
sharp, irregular
Marls
Wavy lamination
Cross lamination
Massive
Parallel lamination
yellow
brown
olive
greyish-blue
dark-grey
grey
light-grey
Facies examples
see fig. 3 and 4
Convolute lamination
Plant detritus
Flute marks
Groove marks
Intraclasts
of mudstones/shales
Small biogenic
structures
3A
oliveish-grey
0.5
m
4B
4C
3F
4A
3E
3D
3C
3B
3A
Fig. 2. Facies of the Zembrzyce Beds in the study area: numbers from 1.1 to 5.7 — subfacies (see Table 1).
354
WÓJCIK, ZIELIŃSKA, CHYBIORZ and ŻABA
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sedimentation was sometimes interrupted by deposition from
different-density turbidity currents.
Facies 9
Facies 9 consists of grey, dark grey, greyish-blue and rarely
brown mudstones with thin-bedded sandy mudstones (Figs. 2
and 4C). Interbeds of mudstones and sandy mudstones reveal
parallel laminations. Facies 9 corresponds to facies E2.2 of
Pickering et al. (1986, 1989); facies TM and MT of Ghibaudo
(1992); and facies MT of Słomka (1995). The sediments of
this facies are interpreted as a result of fine-grained deposits
laid down by suspension, or by low-density turbidity currents
(Ghibaoudo 1992; Słomka, 1995).
Fig. 3. Facies examples of the Zembrzyce Beds; A — facies 1 (gravelly sandstones); B — facies 2 (sandstones); C — facies 3 (thick-bedded
to very thick-bedded sandstone-mudstone couplets); D — facies 4 (thin-bedded to medium-bedded sandstone-mudstone couplets);
E — facies 5 (mudstone-sandstone couplets); F — facies 6 (mudstones and sandy mudstones with marls).
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Facies associations of the Zembrzyce Beds in the study area
Based on facies features, four facies associations of the Zem -
brzyce Beds in the Siary Subunit were distinguished (Fig. 5).
The beds of gravelly sandstones and sandstones are deposits
of high-concentrated turbidity currents sensu Lowe (1982), or
concentrated density flows sensu Mulder & Alexander (2001).
The medium and thin-bedded sandstone–mudstone couplets
as well as the mudstone–shale couplets and the beds of graded
shales are deposits of low-concentrated turbidity currents
sensu Lowe (1982), or turbidity currents sensu Mulder &
Alexander (2001), whereas the varicoloured shales and muddy
shales that occur in the top part of the massive shale layers and
which underline sandstone beds are hemipelagites and back-
ground sediments in the entire succession.
Association I — termination of distributary channels/
depositional lobes
This facies association is composed of gravelly sandstones,
sandstone–mudstone couplets, mudstone–sandstone couplets
and occasionally mudstones and sandy mudstones with marl
facies (Facies 1, 2, 3, 4, 5 and occasionally 6) (Table 2).
The estimated proportion of sandstones is from 57 to 71 %,
whereas mudstones make up 29 to 43 %. Deposition of these
sediments took place in the mid part of a sub-marine fan
depositional system. Negative facies sequences (i.e., decrea sing
upward thickness of beds and grain size) occur in the lower part
of the sedimentary succession. However, in the upper part of
the sedimentary succession, the low number of positive facies
sequences (i.e., increasing upward thickness of layers and
grain size) suggest that these sediments represent the distal
part of the mid fan, probably near the final part of distributary
channels passing upward into depositional lobes.
Association II — depositional lobe
In this facies association, mudstone and mudstone–sand-
stone couplets and thin-bedded to medium-bedded sandstone–
mudstone couplets dominate (Facies 4, 5 and 6), with a small
share of thick-bedded sandstone–mudstone couplets and sand-
stones (Facies 2 and 3) (Fig. 5 and Table 2). The estimated
proportion of sandstones is from 40 to 47 %, whereas mud-
stones make up 53 to 60 %. This type of sediment was depo-
sited in the distal (outer) part of the depositional system,
probably within depositional lobes (in their distal part), which
are responsible for the positive facies sequences within the sedi -
mentary succession. Most likely, these are outer fan deposits
passing upward into deposits of muddy or muddy–sandy
depo sitional lobes.
Association III — distal lobes (fan fringe lobes)
Association III comprises mudstones and sandy mud-
stones with intercalations of sandstone bodies with lenti cular
geo metry (Facies 8 and 9) (Fig. 5 and Table 2). The percentage
of sand-size grains ranges from 9 to 20 %, and the percentage
of mud-size grains ranges from 56 to 77 %. Deposition of this
sediment type is typical for the distal (outer) part of a sub-
marine fan depositional system — the fringe lobes.
Association IV — lower fan/basin plain (fan fringe/basin
plain)
Association IV consists of mudstones and sandy mudstones
with intercalations of thin-bedded sandstones (Facies 7 and 9)
(Fig. 5 and Table 2). The estimated proportion of mudstones
Fig. 4. Facies examples of the Zembrzyce Beds; A — facies 7
(mudstones and sandy mudstones with thin-bedded sandstones);
B — facies 8 (mudstones and sandy mudstones with irregular
sandstone layers); C — facies 9 (mudstones and sandy mudstones).
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WÓJCIK, ZIELIŃSKA, CHYBIORZ and ŻABA
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A
ASSOCIATION IV
M SF
1
2
6
7
8
9
10
[m]
ASSOCIATION III
1
2
5
6
7
8
9
10
11
[m]
ASSOCIATION I
M SF SMSC GF
ASSOCIATION II
[m]
0.5
2
3
4
5
8
9
10
11
12
13
[m]
M SF
M SF
1
2
3
4
7
8
9
10
n = 82
n = 41
0
o
0
o
90
o
90
o
180
o
180
o
270
o
270
o
15
15
25%
25%
5
5
B
a
b
Fig. 5. The synthetic characteristic patterns of facies associations based on sedimentological study of the Zembrzyce Beds (A) and palaeo-
transport directions in the Zembrzyce Beds (B): a — based on literature data (Sikora & Żytko 1959), b — measured during field studies and
based on literature data (Wójcik 2013); legend for facies association see Appendix 1 and 2.
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is 69–89 %, whereas sandstones do not exceed 10 %. Depo-
sition of this type of sediment is characteristic for the distal
(outer) part of a sub-marine fan depositional system — the fan
fringe.
Biostratigraphy
In the western part of the Siary Subunit the age of the Zem-
brzyce Beds was determined as Middle–Late Eocene and even
as Middle Eocene–Early Oligocene (Sikora & Żytko 1959;
Golonka & Wójcik 1978a; Chodyń 2002).
Based on our micropalaeontological investigations in
the Jeleśnia area, the age of the Zembrzyce Beds in the study
area was determined as the Late Eocene (zones NP19–20)
(Tables 3 and 4) (Garecka 2011).
Discussion
The main depositional architectural elements of
the Zembrzyce Beds
The submarine fan deposystem comprises three sub-depo-
systems: inner-fan, mid-fan and outer-fan. The mid-fan
sub-deposystem is the transitional part between the inner-fan
and outer fan. It is characterized by numerous distributary
channels. The outer-fan sub-deposystem is formed beyond
the channel-featured mid-fan sub-deposystem (Zhang et al.
2015).
In the study area only the mid-fan and outer-fan sub-depo-
systems are present. We classified three architectural elements
as terminations of distributary channel-depositional lobes
(distal part of mid-fan/outer fan), depositional lobes and distal
lobes (outer fan).
Termination of distributary channel / lobes
Association I occurs in the lower part of the channel succes-
sion. Association I is an example of sediments belonging to
the termination of a distributary channel with transition to
depositional lobe succession. This association is represented
by gravelly sandstones, sandstones and sandstone–mudstone
couplets or mudstone–sandstone couplets. Association I is
characterized by vertical sediment differentiation. Sediments
that are characterized by the presence of: muddy clasts and
coalified plant detritus, negative facies sequences in the lower
part of sedimentary succession and positive facies sequence in
the upper part of the sedimentary succession. In association I,
in the lower part of the sedimentary succession, thick-bedded
to very thick-bedded channel sandstones and gravelly sand-
stones occur, whereas, in the upper part of the sedimentary
succession usually thin-bedded to medium-bedded sandstones
occur. Sandstone beds are massive, parallel-laminated, cross-
laminated and convolute-laminated. Basal surfaces of beds are
sharp and flat, or locally irregular. Mudstones are parallel-
laminated. Erosional structures at the base of sandstones are
attributed to the erosion by heads of high-velocity turbidity
currents. Mudstone beds of laminated intervals were formed
when distributary channels kept changing their positions
(Zhang et al. 2015).
Lobes
Association II represents muddy-sandy depositional lobes.
Sediments are characterized by the presence of positive facies
sequences. This association mostly consists of sandstone–
mudstone couplets or mudstone–sandstone couplets, but
some times between sandstone–mudstone couplets and
mudstone– sandstone couplets, sandstones and episodically
gravelly sandstones occur. The difference of association I
from association II is that association I is characterized by
the prevalence of sandstone-size grains in relation to mud-
stone-size grains, whereas association II is characterized by
the reverse ratio of the above fractions. Sandstone beds mostly
show parallel surfaces. In laminated intervals, cross lamina-
tion, convolute lamination, horizontal lamination are common.
Sometimes sandstone beds show erosional basal surfaces with
flute casts or tool marks on the base. Sandstones beds are
rarely massive with muddy clasts or with deformation of
the lamina. The occurrence of thick-bedded sandstones and
gravelly sandstones together with the great thickness of beds
of sandstone–mudstone couplets, mudstone–sandstone couplets
and mudstones can represent the residue after channel migra-
tion or fill end distributary channel on depositional lobes.
Association II is characterized by vertical sediment differen-
tiation which can be explained by cutting off and lobe migra-
tion within the sub-marine fan. There were probably elongated
depositional lobes that laterally migrated.
Distal lobes
Association III represents sediments from the fan fringe
lobes. In this facies association, mudstones dominate with
a low percentage of sandstones. The occurrence of sandstone
bodies with lenticular geometry is associated with the migra-
tion of lobes during the Zembrzyce Beds deposition.
Association IV is related to sedimentation located far from a
source area. In this association, mudstones dominate. The
presence of this sediment type is typical of sedimentation in
the most distal part of lobes with the transition to sediments of
fan fringe. In contrast to association III, the greater share of
mudstones represents the transition to more stable sediments
of low-density turbidity currents, and the presence of thin-
layer (thin-bedded) sandstones which represent interfingering
of sediments from the hemipelagic environment with those of
the fan fringe lobes.
Depositional system of the Zembrzyce Beds
Based on the characteristics of the distinguished associa-
tions, it was determined that the Zembrzyce Beds in the study
area were formed within the distal part of the depositional
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system as result of lateral migration of distributary channels
and lobes stacked on top of each other. Also, in the eastern part
of the Siary Subunit (near Gorlice) Kopciowski (2007) defined
the Zembrzyce Beds as sediments that were accumulated as a
result of turbidity currents within the distal part of a mud-rich
submarine fan and the abyssal plain. According to the author,
the following features confirm this statement: sandy low-den-
sity turbidites and muddy turbidites within hemipelagic sedi-
ments; the increase and decrease in layer thickness within
the sedimentary complex, and the extensive distribution and
presence of manganese ores within green shales in the sedi-
mentary basin.
In total, sediment features indicate that the Zembrzyce Beds
were accumulated by different gravity flows in a deep-marine
environment (multiple source, mud/sand-rich ramp according
to Reading & Richards’ 1994 classification). The following
features of the Zembrzyce Beds provide evidence for this
statement: the constant transport direction of clastic sediments
from NE; the simultaneous distribution of high- and low-den-
sity turbidity currents and hyperconcentrated density flows;
the asymmetrical increase and decrease of layer thickness and
well-sorted thick- and very thick-bedded sandstones; the con-
tinuous distribution of the Zembrzyce Beds in the Siary zone.
Similar statements were made by Warchoł (2007), though, his
interpretation refers not only to the Zembrzyce Beds but also
to the overlying deposits considered in common as the Magura
Beds (Zembrzyce Beds and Wątkowa Sand stones — sedi-
ments of distributary channels and depositional lobes domi-
nated by sand and Budzów Shales — sediments of depositional
lobes dominated by mud with the participation of sedimenta-
tion in smaller channels). The continuous cover of sediments
and the linear layout of source area indicate that
the depositional system has common features with those of
a deep-sea ramp and a drape at the base of the slope.
Leszczyński & Malata (2002) were the first to interprete
the whole succession called by them Magura Beds in glauconitic
facies as a submarine ramp deposits. Noteworthy, the almost
exclusively shaly deposits distinguished as the Szymbark
Shales, coeval with the Zembrzyce Beds (Sub-Magura Beds),
described by Leszczyński & Malata (2002), Leszczyński et al.
(2008) near Gorlice, were interpreted mostly as sediments of
muddy turbidity currents (hemiturbidite) and hemipelagites
which were deposited in the form of a cover, in the marginal
part of the Magura Basin.
According to Leszczyński & Malata (2002) the Siary zone
was a basin surrounded by the margins of the Magura basin in
the north and by the northward sloping bottom of the Rača
zone in the south. Its bottom formed a ramp. This ramp may
have extended along the margins of the Magura basin, and on
the west encroached on the Rača zone. Intensive resedimen-
tation of clastic material by different mass gravity flows
took place during sedimentation of the entire succession in
the western part of the Siary zone and points to intensive ero-
sion of the source area. Sedimentary conditions and sedimen-
tation development in the Siary zone, as well as remaining
parts of the Magura Basin were controlled by subduction roll-
back. What is more, the authors claim that diachronism of
the Magura Beds between the western and eastern part of
the Siary Subunit and palaeotransport directions indicated
sedimentation controlling by basin subsidence and migration
of the subsidence centre obliquely to the Siary Subunit from
the west to the east. It drove transpression in the Magura
Basin, which resulted there in accretionary wedge progress
and expanded subsidence in front of the accretionary wedge.
At the same time, the margins of the Magura Basin underwent
uplifting (Leszczyński & Malata 2002).
In the study area during sedimentation of the Zembrzyce
Beds the depositional conditions were controlled by the tecto-
nics as well as the global sea level changes. Tectonic develop-
ment (flexural subsidence) during the Late Eocene influenced
the topography of the basin floor, uplift of source areas and
northward migration of depocentres. Many faults, horst and
grabens have been formed and primary elements of tectonics
have been reactivated. The basin floor was very varied. There
species / samples
Braarudosphaera bigelowii Braarudosphaera
sp.
Chiasmolithus oamaruensis Chiasmolithus
sp.
Clausicoccus subdistichus Coccolithus eopelagicus Coccolithus pelagicus Corannulus germanicus Cribr
ocentrum r
eticulatum
Cyclicar
golithus floridanus
Cribr
ocentrum coenurum
Cribr
ocentrum
sp.
Dictyococcites callidus Discoaster saipanensis Dictyococcites bisectus Discoaster barbadiensis Dictyococcites scrippsae Dictyococcites
sp.
Discoaster tanii Discoaster
sp.
Ericsonia cava Ericsonia formosa Helicosphaera compacta Isthmolithus r
ecurvus
Lanternithus minutus Markalius inversus Neococcolithes minutus Neococcolithes
sp.
Pontosphaera latelliptica Pontosphaera multipora Pontosphaera
sp.
Reticulofenestra hillae Reticulofenestra umbilica Reticulofenestra dictyoda Reticulofenestra
sp.
"small r
eticulofenestrids"
Rhabdosphaera
sp.
Rhabdosphaera tenuis Sphenolithus moriformis Sphenolithus spiniger Sphenolithus moriformis Sphenolithus
sp.
Transversopontis pulcher Thoracosphaera oper
culata
Thoracosphaera heimii Thoracosphaera oper
culata
Thoracosphaera saxea Thoracosphaera
sp.
Zygr
hablithus bijugatus
fragments of cocoliths
Pewel
Mała
1
×
× × × ×
× ×
× × ×
×
×
× × ×
× ×
× × × × ×
× × × ×
× × ×
×
×
Jeleśnia
2
×
×
×
×
× × ×
× × × ×
×
×
× ×
× × × ×
×
× ×
Pewel
Ślemieńska
3a
×
×
×
× × ×
×
×
×
× × ×
×
×
3b × × × ×
× ×
× ×
× × × ×
×
× ×
×
× ×
× ×
× × ×
×
×
× × × ×
Table 3: Distribution of calcareous nannoplankton recorded in the investigated samples (Garecka 2011).
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Braarudosphaera bigelowii
Chiasmolithus oamaruensis
Coccolithus pelagicus
Discoaster barbadiensis
Ericsonia formosa
Dictyococcites callidus
Discoaster saipane
nsis
Lanternithus minutus
Reticulofenestra umbilica
Cribrocentrum reticulatum
Cribrocentrum coenurum
Cyclicargolithus floridanus
Dictyococcites bisectus
Helicosphaera bramlettei
Reticulofenestra hillae
Discoaster tanii
Helicosphaera compacta
Corannulus germanicus
Isthmolithus recurvus
Clausicoccus subdistichus
BIOSTRA
TIGRAPHIC
POSITION OF SAMPLES
NANO ZONES
Varol
(1998)
Martini
(1971)
AGE
TIME
NNTo9-12
NNTo4-6
NNTo1-2
NNTe13-14
NNTe12
NNTe11
NNTe10
NNTe9
NNTe8
NNTe7
NNTe6
NNTe1
NP11
Np16
Np22
Np12
Np17
Np23
Np14
Np13
Np19-20
Np18
Np24
Np15
Np21
Np25
NNTe2-5
NNTo3
NNTo8
NNTo7
CHATTIAN
RUPELIAN
PRIABONIAN
BARTONIAN
LUTETIAN
YPRESIAN
LATE
LATE
EARLY
EARLY
MIDDLE
OLIGOCENE
EOCENE
Table 4: Stratigraphic range of selected species of the calcareous nannoplankton and biostratigraphic position of analysed samples
(Garecka 2011).
were ridges, which were source areas and provided material to
the basin. The ridges were underwater, as well as emerged on
the surface. The features of sediments indicate that the fan
deposystem can be classified as a mud/sand-rich ramp sensu
Reading & Richards (1994). The fan deposystem is characte-
rized by moderate size, 5–75 km long, lobate shape, the slope
gradient 7–35 m/km, moderate and moderate/small size source
area, channel system: multiple leveed channels with meande-
ring to straight platform.
Palaeogeography of Magura Basin during the Zembrzyce
Beds sedimentation
The opening time of the Magura Basin is still under discu s-
sion (Oszczypko 1992; Oszczypko et al. 2015). The Early–
Middle Jurassic opening of the Magura Basin was probably
coeval with the South-Penninic–Piedmont–Ligurian Ocean
opening (Schmid et al. 2005; Oszczypko et al. 2015). The Magura
Basin domain was divided by the Czorsztyn Ridge into the NE
and SE parts. The NE part was occupied by the Magura Basin,
an equivalent of the north-Penninic (Valais) domain, whereas
the SE arm was occupied by the Pieniny Basin, also known as
the Vahicum Oceanic Rift (south Penninic domain) (Oszczypko
1992, 2004). The Magura Basin was limited by the European
shelf to the north and it passed into the Ceahlau–Severin Ocean
towards the SE (Oszczypko et al. 2015).
During the Late Cretaceous–Palaeocene time, the Magura
Basin was modified probably by folding and thrusting pro-
cesses taking place in the Central Carpathians and the Pieniny
Klippen Belt (Plašienka 2014a, b; Oszczypko et al. 2015).
The Magura Basin was transformed into several sub-basins
with different size, bathymetry, floor morphology and tectonic
activity. Particular sub-basins were supplied with clastic mate-
rials derived from intrabasinal source areas and marginal land
parts (Plašienka 2014a, b; Oszczypko et al. 2015). To the north,
the Magura Basin was limited by the Silesian Cordillera.
The problem of the southern margin of the Magura Basin
is still under consideration. In general, it is designated as
the northern boundary of the Pieniny Klippen Belt (Oszczypko
et al. 2015).
During the Palaeocene, the Inner Western Carpathian
Orogenic Wedge reached the southern margin of the Magura
Basin, which caused the subsidence and collapse of the Pieniny
Klippen Belt and southwards shift of the Magura Basin.
The migrating load of the Magura and the Pieniny Klippen
Belt accretionary wedge caused further subsidence and a shift
of depocentres to the north (Oszczypko 2004). In the Middle
Eocene–Late Eocene, the sedimentation in the Magura Basin
was controlled by many processes: (i) tectonic movements,
(ii) the progress of the subduction within the southern margin
of the Magura Basin, (iii) by local sediment supply and (iv) by
the global glacioeustatic fall of sea level (Oszczypko 2004;
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WÓJCIK, ZIELIŃSKA, CHYBIORZ and ŻABA
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Teťák 2008). The Magura Basin floor was segmented by
longitudinal synsedimentary depressions and lifted plains
(Teťák 2008, 2010).
Palaeotransport directions (literature data and data mea-
sured during field studies) as well as the distribution of facies
indicate the Silesian Cordillera as a source of clastic material
from the NE for the Zembrzyce Beds (Figs. 5 and 6). The Siary
sub-basin was limited by slopes of the Silesian Cordillera to
the north (Leszczyński & Malata 2002; Warchoł 2007) (Fig. 6).
The southern margin of the Siary sub-basin was probably
limited by synsedimentary faults separating the Siary domain
from the Rača sub-basin (Teťák 2008, 2010).
In the western part of the Siary sub-basin, increasing thick-
ness of the Zembrzyce Beds sediments was observed, in
contrast to the eastern area. Such diversity was related to
the inclination of the whole Magura Basin axis towards the west
(Fig. 6). The depositional area belonging to the Siary sub-
basin was controlled by the influence of eustatic sea level
Fig. 6. Simplifed model of deposition system of the Zembrzyce Beds (multiple mud/sand-rich ramp) (A) and simplified palaeogeographical
sketch of Magura Basin during Zembrzyce Beds deposition (B) (Late Eocene): FMB(DB?) — Fore-Magura Basin (Dukla Basin?);
SB — Silesian Basin; MB — Magura Basin; M–DB — Magura–Dukla Basin; DB — Dukla Basin; KK — Kuman Ridge (after Książkiewicz
1962; Kopciowski 2007; Warchoł 2007; Teťák 2010; Jankowski et al. 2012; modified)
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EOCENE MARGINAL MULTIPLE-SOURCE RAMP OF THE MAGURA BASIN (OUTER WESTERN CARPATHIANS)
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changes. During sedimentation of the Zembrzyce Beds,
the rela tive sea level was high (highstand systems tract —
maximum transgression), and the CCD was lowered.
Kopciowski (2007) indicates that high similarity of sediments
in the Siary Subunit and Dukla Subunit allow us to suppose
that the sedimentation of depositional systems was related to
the same sub-basin occurring within the Carpathian Basin.
Both areas were subjected to the same source areas controlled
by relative sea-level changes (Kopciowski 2007). Similar
statements were written by Oszczypko et al. (2015), since
the Late Cretaceous to the Late Eocene, both the Dukla and
Magura sub-basins were characterized by the same deposi-
tional pattern (Inoceramian facies, Beloveža and Zlín
formations).
Conclusions
1. In the study area, four main facies associations and nine
lithofacies were identified and interpreted. The submarine
fan deposystem comprises two subdeposystems of mid-fan
and outer-fan. We classified three architectural elements:
termination of distributary channel-depositional lobe (distal
part of mid-fan/outer fan), depositional lobe and distal
lobes (outer fan).
2. The sediments of the studied succession were deposited by
high- and low-density turbidity currents and hyperconcen-
trated density flows sensu Mulder & Alexander (2001) with
trace participation of sediments of depositional background
(pelagites and hemipelagites).
3. The western part of the Siary Subunit is characterized by
a multiple source, mud/sand rich ramp sensu Reading &
Richards (1994).
4. The Zembrzyce Beds are sediments of the distal (outer)
part of the depositional system: sediments of distributary
channel terminations with transition to depositional lobes,
sediments of migrating muddy-sandy depositional lobes,
sediments of the fan fringe lobes and sediments from
the fan fringe/basin plain. This system consisted of several
elongated lobes stacked on top of each other that were
active at the same time. The lobes migrated laterally and
retreated or decayed. The massive and coarse-grained,
thick-bedded sediments were formed in the central part of
the lobe, whereas thin-bedded sediments represent the retreat
of the lobes. The hemipelagic sediments represent the far
distal part of the lobes and sediments that mixed with
the abyssal plain sediments.
5. The Zembrzyce Beds were deposited above the CCD
(Uchman et al. 2006).
6. The sediments of the Zembrzyce Beds were related proba-
bly to a high-stand system tract (Kopciowski 2007).
7. The sedimentary conditions and sedimentation develop-
ment of the Zembrzyce Beds were controlled by tectonic
movements, the progress of the subduction to the south and
by the global sea level changes (cf. Leszczyński & Malata
2002; Oszczypko 2004; Teťák 2008).
8. The examined samples from the Zembrzyce Beds have
shown that the sampled beds are of Late Eocene (zones
NP19–20).
Acknowledgements: Our thanks go to the Reviewers and
Editor of the Geologica Carpathica for comments. This research
was supported by Statutory Funds, University of Silesia,
Poland no. ZFIN00000040, el. PSP 1S-0416-001-1-01-05 and
PSP 1S-0416-001-1-01-01 “Study of geological processes and
structures as well as natural resources and geoenvironmental
risks”. The microfauna studies were supported by a grant
from the Ministry of Science and Higher Education, Poland
no. MNiSW 0689/B/P01/2010/39 “Siliciclastic sedimentation
of the Palaeogene of the Magura Nappe south of the Żywiec”
under the management of Prof. dr hab. Antoni Wójcik from
the Polish Geological Institute — National Research Institute
in Cracow. Thanks are due to Prof. dr hab. Antoni Wójcik
(Polish Geological Institute-National Research Institute in
Cracow) for his support and to Prof. dr hab. Barbara Olszewska
(Polish Geological Institute — National Research Institute in
Cracow) and Dr Małgorzata Garecka (Polish Geological Insti-
tute — National Research Institute in Cracow) for microfauna
work.
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i
EOCENE MARGINAL MULTIPLE-SOURCE RAMP OF THE MAGURA BASIN (OUTER WESTERN CARPATHIANS)
GEOLOGICA CARPATHICA
, 2018, 69, 4, 347–364
def
SECTION 1
8
9
8.5
9.5
14
17
17.5
19
19.5
20
0.5
1
1.5
2
14.5
15
15.5
16
16.5
20.5
21
21.5
22
[m]
M SF SM SC GF
M SF SM SC GF
M SF SM SC GF
3A
23
23,5
24
3C
3E
brown
light-olive
light greyish-olive
Deformation
Bedding plane:
Rock color:
sharp, planar
sharp, irregular
Marls
Wavy lamination
Cross lamination
Massive
Parallel lamination
yellow
brownish-grey
olive
oliveish-grey
greyish-blue
dark-grey
grey
light-grey
Convolute lamination
Plant detritus
Positive (a) and negative (b)
facies sequence
Flute marks
Groove marks
Intraclasts
of mudstones/shales
Small biogenic structures
a
b
def
Facies examples
see
ig . 3 and 4
F
s
3A
Supplement
Appendix 1: Detailed sedimentological sections of the Zembrzyce Beds (see Appendix 2).
ii
WÓJCIK, ZIELIŃSKA, CHYBIORZ and ŻABA
GEOLOGICA CARPATHICA
, 2018, 69, 4, 347–364
M SF SM SC GF
M SF SM SC GF
M SF SM SC GF
0.5
1
1.5
2
[m]
0.5
1
1.5
2
2.5
3
3.5
4
4.5
5
5.5
6
6.5
[m]
SECTION 4
SECTION 3
5
SECTION 2
2.5
3
3.5
4
7
7.5
8
8.5
[m]
0.5
1
1.5
2
4.5
5.5
6
6.5
M SF SM SC GF
M SF SM SC GF
3F
3D
Appendix 1 (continued)
iii
EOCENE MARGINAL MULTIPLE-SOURCE RAMP OF THE MAGURA BASIN (OUTER WESTERN CARPATHIANS)
GEOLOGICA CARPATHICA
, 2018, 69, 4, 347–364
2.5
3
3.5
4
4.5
3
3.5
4
4.5
5
0.5
1
1.5
2
5
5.5
6
6.5
[m]
SECTION 6
0.5
1
1.5
2.5
[m]
SECTION 7
M SF SM SC GF
M SF
M SF
M SF
M SF SM SC GF
0.5
1
1.5
2
2.5
3
3.5
4
4.5
5
5.5
6
6.5
7
SECTION 5
7.5
[m]
M SF SM SC
3B
Appendix 1 (continued)
iv
WÓJCIK, ZIELIŃSKA, CHYBIORZ and ŻABA
GEOLOGICA CARPATHICA
, 2018, 69, 4, 347–364
SECTION 9
SECTION 10
SECTION 11
[m]
[m]
[m]
0.5
1
1.5
2
2.5
3
3.5
4
4.5
5
5.5
0.5
1
1.5
2
2.5
2.5
2
1.5
1
0.5
M SF
M SF
M SF
M SF
6
def
2.5
3
3.5
4
7
7.5
8
8.5
[m]
SECTION 8
0.5
1
1.5
2
4,5
5
5.5
6
6.5
M SF
M SF
4C
4B
4A
Appendix 1 (continued)
v
EOCENE MARGINAL MULTIPLE-SOURCE RAMP OF THE MAGURA BASIN (OUTER WESTERN CARPATHIANS)
GEOLOGICA CARPATHICA
, 2018, 69, 4, 347–364
Appendix 2: Location of the detailed sedimentlogical sections and facies associations in the study area (source Orthophotomap 2009: License
No. DIO.DFT.DSI.7211.18428.2014_PL_N for the University of Silesia in Katowice).