GeolCarp_Vol69_No4_347

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)

GEOLOGICA CARPATHICA

, 2018, 69, 4, 347–364

SRB

BIH

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

Zakopane

Żywiec

Kraków

Miocene of the Carpathian

Foredeep

Carpathian Foreland

Outer

Western

Carpathians

Western

Inner

Carpathians

CZECHIA

POLAND

SLOVAKIA

ult

Koszar

Sopotnia

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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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

1, 2, 3, 4, 5, 6

termination of distributary channel passing upward into depositional lobe distal part of mid-fan/outer fan subdeposystem

2, 3, 4, 5, 6

muddy-sandy depositional lobe

outer fan subdeposystem

III

8, 9

distal part of depositional lobe (fan fringe lobes)

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

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

oliveish-grey

0.5

Fig. 2. Facies of the Zembrzyce Beds in the study area: numbers from 1.1 to 5.7 — subfacies (see Table 1).

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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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ASSOCIATION IV

M SF

[m]

ASSOCIATION III

[m]

ASSOCIATION I

M SF SMSC GF

ASSOCIATION II

[m]

0.5

[m]

M SF

n = 82

n = 41

180

270

25%

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

× × × ×

× ×

× × ×

× ×

× × × × ×

× × × ×

× × ×

Jeleśnia

× × ×

× × × ×

× ×

× × × ×

× ×

Pewel

Ślemieńska

× × ×

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

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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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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def

SECTION 1

8.5

9.5

17.5

19.5

0.5

1.5

14.5

15.5

16.5

20.5

21.5

[m]

M SF SM SC GF

23,5

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

def

Facies examples

see

ig . 3 and 4

Supplement

Appendix 1: Detailed sedimentological sections of the Zembrzyce Beds (see Appendix 2).

iii

EOCENE MARGINAL MULTIPLE-SOURCE RAMP OF THE MAGURA BASIN (OUTER WESTERN CARPATHIANS)

GEOLOGICA CARPATHICA

, 2018, 69, 4, 347–364

2.5

3.5

4.5

3.5

4.5

0.5

1.5

5.5

6.5

[m]

SECTION 6

0.5

1.5

2.5

[m]

SECTION 7

M SF SM SC GF

M SF

M SF SM SC GF

0.5

1.5

2.5

3.5

4.5

5.5

6.5

SECTION 5

7.5
[m]

M SF SM SC

Appendix 1 (continued)

WÓJCIK, ZIELIŃSKA, CHYBIORZ and ŻABA

GEOLOGICA CARPATHICA

, 2018, 69, 4, 347–364

SECTION 9

SECTION 10

SECTION 11

[m]

0.5

1.5

2.5

3.5

4.5

5.5

0.5

1.5

2.5

1.5

0.5

M SF

def

2.5

3.5

7.5

8.5

[m]

SECTION 8

0.5

1.5

4,5

5.5

6.5

M SF

Appendix 1 (continued)