GeolCarp_Vol69_No1_71

GEOLOGICA CARPATHICA

, FEBRUARY 2018, 69, 1, 71–88

doi: 10.1515/geoca-2018-0005

www.geologicacarpathica.com

Sedimentary processes and architecture of

Upper Cretaceous deep-sea channel deposits:

a case from the Skole Nappe, Polish Outer Carpathians

PIOTR ŁAPCIK

Institute of Geological Sciences, Jagiellonian University, Gronostajowa 3a, 30-063 Kraków, Poland; piotr.lapcik@doctoral.uj.edu.pl

(Manuscript received July 4, 2017; accepted in revised form December 12, 2017)

Abstract: Deep-sea channels are one of the architectonic elements, forming the main conduits for sand and gravel

material in the turbidite depositional systems. Deep-sea channel facies are mostly represented by stacking of thick-

bedded massive sandstones with abundant coarse-grained material, ripped-up clasts, amalgamation and large scale

erosional structures. The Manasterz Quarry of the Ropianka Formation (Upper Cretaceous, Skole Nappe, Carpathians)

contains a succession of at least 31 m of thick-bedded high-density turbidites alternated with clast-rich sandy debrites,

which are interpreted as axial deposits of a deep-sea channel. The section studied includes 5 or 6 storeys with debrite

basal lag deposits covered by amalgamated turbidite fills. The thickness of particular storeys varies from 2.5 to 13 m.

Vertical stacking of similar facies through the whole thickness of the section suggest a hierarchically higher channel-fill

or a channel complex set, with an

aggradation rate higher than its lateral migration. Such channel axis facies cannot

aggrade without simultaneous aggradation of levee confinement, which was distinguished in an associated section located

to the NW from the Manasterz Quarry.

ateral offset of channel axis facies into channel margin or channel levee facies

is estimated at less than 800 m. The Manasterz Quarry section represents mostly the filling and amalgamation stage of

channel formation. The

described channel architectural elements of the Ropianka Formation are located within

the so-called Łańcut Channel Zone, which was previously thought to be Oligocene but may have been present already in

the Late Cretaceous.

Keywords: Carpathians, sedimentary processes, architectural elements, deep-sea channel, massive sandstone, turbidite,

debrite.

Introduction

The architectural elements concept is widely accepted for

analysis of deep-sea depositional environments (Mutti &

Normark 1987). According to this concept, sedimentary

bodies are distinguished as parts of a hierarchically organized

deep-sea fan model. A high variety of architectural elements

are conditioned by material deposited, size and latitudinal

position of depositional system, sea level changes, tectonic

regime and sedimentary processes (e.g., Stow & Mayall 2000;

Mulder 2011; Cossu et al. 2015; Shanmugam 2016). Architec-

tural elements are usually distinguished in very well exposed

depositional systems through analysis of facies associations

(e.g., Gardner et al. 2003; Prélat et al. 2009; Hubbard et al.

2014; Bayliss & Pickering 2015a, b; Pickering et al. 2015).

However, this concept was so far not applied to numerous

formations, including the Ropianka Formation (Turonian–

Paleocene) in the Skole Nappe (Polish Carpathians). This for-

mation, up to 1.6 km thick, contains a succession of deep-sea

deposits with numerous facies associations suggesting occur-

rence of different architectural elements (e.g., Bromowicz

1974; Kotlarczyk 1978, 1988; Łapcik in press), which remain

almost undetermined. Tectonic deformation and poor expo-

sure of the Ropianka Formation make difficulties in correla-

tions of facies and architectural elements over longer distances.

Nonetheless, large outcrops with high contribution of

thick-bedded sandstones give a chance to distinguish such

bodies in some places, for example, in the Słonne section,

where Łapcik (in press) distinguished over 140 m thick lobe

complex.

In this paper, deep-sea channel-fill and its internal architec-

ture are presented in structureless and graded thick-bedded

sandstones from the Manasterz Quarry, in references to asso-

ciated sections. Moreover, depositional processes are inter-

preted on the basis of sedimentary structures and the internal

architecture of the channel-fill.

Geological setting

This study is focused on the Ropianka Formation (after

Kotlarczyk 1978), also known as the Inoceramian Beds (Uhlig

1888), which is referred to sand-rich deposits in the northern

part of the Skole Nappe (also known as the Skyba Nappe).

The formation comprises a succession of turbidity current,

debris flow, slump, pelagic and hemipelagic deposits of the

Turonian–Palaeocene age up to about 1.6 km thick (e.g.,

Kotlarczyk 1978, 1988). The Skole Nappe is the most external

major tectonic unit in the Polish Carpathians (Fig. 1A).

Deposits of the Skole Nappe accumulated in a separate

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sub-basin (e.g., Kotlarczyk 1988), however, some authors

regard part of the Skole Basin as the Carpathian marginal zone

which corresponds to the basin slope (e.g., Jankowski et al.

2012). Sedimentation in the Outer Flysch Carpathians started

in the Late Jurassic. The Carpathians evolved from a rift basin

(since the Late Jurassic) to a remnant foreland basin in the

Oligocene (Golonka et al. 2006; Nemčok et al. 2006; Ślączka

et al. 2006, 2012; Gągała et al. 2012) and ultimately during the

Miocene the basin was folded and thrusted upon the Car-

pathians Foredeep. During the Turonian–Paleocene times, the

sediments of the Skole Basin are thought to have been derived

from the southern part of the Upper Silesia and Małopolska

blocks to the north (Książkiewicz 1962; Bromowicz 1974;

Salata & Uchman 2013) and from the side of the Subsilesian

Ridge (Węglówka Ridge) to the south (Książkiewicz 1962).

The petrographic variety of the source area was repeatedly

mentioned in the literature (e.g., Salata & Uchman 2013;

Salata 2014; Łapcik et al. 2016 and references therein).

Four lithostratigraphic members of the Ropianka Formation

were distinguished based on repeated carbonate-siliciclastic

deposits (Fig. 1B; Kotlarczyk 1978).

Each member (excluding

the Wola Korzeniecka Member) contains carbonate-rich

succession which passes into siliciclastic dominated deposits

towards the top. Moreover, a decreasing contribution of car-

bonate material from the proximal area to the north to the dis-

tal area to the south of the Skole Basin is observed (Kotlarczyk

Fig. 1. Geographical and stratigraphic location of studied area. A — location map of the studied area in the Skole Nappe. Based on Kotlarczyk

(1988) and modifications by Gasiński & Uchman (2009 and references therein); B — location of the Manasterz-Rzeki, Manasterz and

Manasterz Quarry sections with some indicators of the orientation of beds as measured in the field and prediction of spatial distribution of

facies; C — stratigraphic column of the Skole Nappe. Based on Kotlarczyk (1988), Rajchel (1990), Rajchel & Uchman (1998), Ślączka &

Kaminski (1998), with further corrections based on further data by Gedl (1999) and Kotlarczyk et al. (2007). The investigated interval indicated

by „!”. The time scale is after Gradstein et al. (2012). TRSh Mb — Trójca Red Shale Member, VSh — Variegated Shale, ChS Mb — Chmielnik

Striped Sandstone Member.

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1978). Some areas show domination of mass transport depo-

sits typical of slope areas (Burzewski 1966; Bromowicz 1974;

Kotlarczyk 1978, 1988; Dżułyński et al. 1979;

Geroch et al.

1979;

Malata 2001; Jankowski et al. 2012; Łapcik et al. 2016).

Foraminiferid assemblages point to deposition of the Ropianka

Formation in bathyal depths below and above the calcite com-

pensation depth (Uchman et al. 2006). The lithostratigraphy of

the Ropianka Formation is still debated (e.g., Malata 1996;

Jankowski et al. 2012).

Methodology

The fieldwork was based on sedimentological and facies

analysis of sandy dominated thick-bedded deposits. The tex-

ture and primary structure of these deposits were described

during detailed profiling. Grain-size analysis was conducted

in order to determine the depositional processes of the

thick-bedded sandstones and estimate the thickness of amal-

gamated beds. Fifty samples were taken for grain-size and

petrographic analysis which was conducted as described in

Łapcik (

in press

). The samples for grain-size analysis were

collected from 4–5 cm thick layers with different distance

intervals described further in the text. The orientation of the

longer axis of 103 mudstone and marlstone clasts, orientation

of grains and pebbles imbrication and orientation of the axis of

flute casts from the MQ section were measured by mean of

a geological compass in order to determine direction of palaeo-

transport. The last stage of the sedimentological and facies

analysis of the thick-bedded sandstones was distinguishing the

channel elements.

The sections studied

The studied deposits belong to the internally deformed

Husów Thrust Sheet (Wdowiarz 1949), which is the second

thrust sheet from the northern margin of the Carpathians.

The majority of research was focused on sandy deposits in the

well exposed Manasterz Quarry (MQ). Additional sedimento-

logical study was conducted in two associated sections.

Description of the whole Manasterz section is presented below

in the stratigraphic order.

The Manasterz-Rzeki section

The oldest part of the section studied is located in a small

gorge of an unnamed stream, a tributary of the Husówka

Stream at Manasterz-Rzeki (Fig. 1C). The section is repre-

sented by five isolated outcrops containing thin- to thick-

bedded sandstones, siltstones, mudstones and marlstones

(Fig. 2). Beds are dipping to the SW at angles of 40°–50°

(Fig. 1C). The contribution of each facies class in particular

outcrops is presented in Figure 3. Sandstones are quartz-domi-

nated, very fine- to medium-grained, with abundant parallel,

convolute and cross-laminations underlined by carbonized

plant detritus. Medium- and thick-bedded sandstones are

graded or structureless at the basal part. Sole marks are nume-

rous with a high contribution of the trace fossils Ophiomorpha

and Thalassinoides. Some thin-bedded sandstones rich in

plant detritus show chaotic structure, which probably resulted

from bioturbation (the trace fossil Scolicia is present).

Sandstones are alternated with grey mudstones, which often

include thin layers of parallel and cross-laminated siltstones.

The latest lithology is represented by bluish-white marlstones

with sandstone alternations, which are 0.2–1 cm thick.

Abundant bioturbation structures within marlstones are domi-

nated by Planolites and Chondrites.

The Manasterz-Rzeki section begins as thin-bedded flysch

with abundant alternation of marlstones (Fig. 2). Contribution

of marlstones decreases in the middle part of the section with

simultaneous significant increase in medium- and thick-bedded

sandstones (Fig. 3). The top of the section is again represented

by thin-bedded flysch with abundant alternation of marlstones

similar looking to the bottom part of the section. The total

thickness of the Manasterz-Rzeki section is 116 m with

a 28 m-thick middle part showing numerous medium and

thick sandstone beds. The Manasterz-Rzeki section belongs to

the Campanian Wiar Member (Fig. 1B; Kotlarczyk 1978).

The Manasterz section

Higher part of the section crops out in gorges of unnamed

tributaries of the Mleczka River, south of Manasterz-Rzeki,

where beds dip to the W and SW (Fig. 1C). The lower part of

the section is represented by thin-bedded flysch with alterna-

tion of marlstones showing similar appearance to the top and

bottom part of the Manasterz-Rzeki section (Fig. 2). To the top

of the section, the contribution of marlstones decreases with

simultaneous increasing of mudstones (Fig. 2). The higher

part of the section contains a medium- and thick-bedded sand-

stone interval. These sandstones are dominated by fractionally

graded and parallel laminated parts with abundant, clasts of

coal. However, some of the medium- and thick-bedded sand-

stones are structureless at their base. Above the sandy interval,

packages of fine-grained, structureless, muddy sandstones

with clasts of mudstone and marlstone are alternated with up

to tens of centimetres thick, silty and sandy calcareous, struc-

tureless mudstones with dispersed quartz pebbles. This type of

deposit is abundant in the external (northern) part of the Skole

Nappe and they are known as the Węgierka Marl (Baculites

Marl). This unit is included in the Leszczyny Member (upper

Maastrichtian–lower Palaeocene). The Manasterz section is

375 m thick (Fig. 2). Tectonic deformations leave uncertainty

if the thick-bedded sandstone interval in the Manasterz section

corresponds to the similar one in the Manasterz-Rzeki section

(Fig. 1C).

The Manasterz Quarry section

The highest part of the section studied

is exposed in a small

quarry at Manasterz

where beds are inclined to the south-west

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Convolute lamination
Cross-lamination
Parallel lamination
Very thin-bedded
siltstone or sandstone

cs v.f f

Manasterz-Rzeki section

111

110

112

113

114

115

[m]

116

[m]

102

103

104

105

106

142

149

150

151

152

157

158

159

160

173

174

175

331

334

335

336

337

339

370

374

176

cs v.f f

cs v.f f m

Sandstone

Marlstone

Sandy/silty mudstone

Mudstone

Manasterz section

Site 1

Site 2

Site 4

Site 3

Site 5

Site 2

[m]

Fig. 2. Lithological columns of the Ropianka Formation at the Manasterz. Logs refer to the Manasterz-Rzeki and the Manasterz sections.

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at angles of 30–40°. The quarry is 85 m long and up to 12 m

high. The outcrop consists of 31 m of fully sandstone section

where yellowish-orange, graded and structureless, amalga-

mated sandstones are fine- to coarse-grained with locally

abundant dispersed quartz gravel, mudstone and marlstone

cobbles and boulders (Fig. 4). Mudstone clasts are usually

very poor in microfauna, however, some contain abundant

bryozoans. The sandstones are quartz arenites, which contain

minor admixture of siliceous grains, muscovite, sericite, glau-

conite, biotite, feldspar, mica schists, pyrite concretions, gra-

nite, gneiss and coal. A minor contribution of biogenic material

is represented by abraded bivalve shells, siliceous sponge

spicules and agglutinated benthic foraminifer tests. The con-

tribution of accessory components never exceeds a few per-

cent in total. Quartz grains are almost always well rounded.

Polymineralic grains are limited to the largest fractions of

0.25–2 mm. The sandstone contains variable amounts of car-

bonate, silica and clay minerals cement and passes from hard

lithified to almost loose sand. The MQ sandstone facies sig-

nificantly differ from the thick-bedded sandstone intervals

from the Manasterz-Rzeki and Manasterz sections. A detailed

description of the MQ section is presented in “Material

studied”.

In a similar stratigraphic position, to the NW of the quarry,

thin- to medium-bedded sandstones alternated with grey

mudstones are present (Figs. 1C, 2). These deposits are very

similar to these in the lower part of the Manasterz section and

they represent a lateral facies equivalent of the Manasterz

section.

Material studied

The Manasterz Quarry facies

The majority of research was focused on the well exposed

MQ sandy deposits. Sedimentological and facies analyses of

the structureless and graded sandstones allowed to distinguish

two or optionally three facies, descriptions and interpretations

of which are presented below.

Facies 1

The majority of deposits in the MQ section are represented

by fine- to coarse-grained, graded or macroscopically struc-

tureless sandstones with quartz gravel and clasts of mudstone

and marlstone. Their bedding is poorly expressed because of

abundant amalgamation and paucity of sedimentary struc-

tures. The amalgamation surfaces are uneven and marked by

abrupt grain-size changes (Fig. 5A), which tend to decline

laterally in the scale of metres. Some of the sandstones show

crude lamination, which is underlined by parallel orientation

of coarse grains and pebbles and very rare imbrication. Clasts

are similar to mudstones and marlstones from the Manasterz

and Manasterz-Rzeki sections and are mostly oriented parallel

to the bedding (Fig. 5B). Clasts of mudstone are usually

several tens of centimetres long and a few centimetres thick,

whereas, clasts of marlstone are mostly rounded to sub-

rounded and do not exceed 20 cm in diameter. Marlstones

contain abundant Chondrites, Planolites and some

Frequency (%

)

Total thickness Number of beds Total thickness Number of beds Total thickness

Marlstone

Mudstone

Siltstone

Thin-bedded

sandstone

Thick-bedded

sandstone

Medium-bedded

sandstone

Frequency (%

)

Number of beds

Site 1

Site 2

Site 3

Site 4

Site 5

Total

Fig. 3. Facies class abundance in the Manasterz-Rzeki section.

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MAN1 1-18

1 1-6

2 1-8

Area mostly covered

Debrites basal lag deposits #2

Debrites basal lag deposits #3?

Debrites basal lag deposits #5

Debris basal lag

deposits 2 only

Sample statistics:

Mean vector 1.31

ector magnitue (length) 9.14%

n = 69

Debrite

urbidite

Amalgamation zones and scours

Thalassinoides

Ophiomorpha

and

Inverse and normal grading

Mudstone and marlstone cobbles and boulders

otal

n = 103

Statistical data of

measured clasts orientation:

Debrites basal lag deposits #4

Debrites basal lag deposits #6?

Fig. 4.

Interpretation of the

Manasterz Quarry section with distinguishing of the channel elements and statistical data of measured clast orientation.

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unidentified bioturbation structures. Several erosional inci-

sions up to 1.5 m deep and 2.5–6.5 m wide, with margins

inclined at angles from 30° to almost 90° occur within the

massive sandstones. They are filled with sandstone with quartz

pebbles and shell debris. These structures are considered as

mega-flutes. Some of them are filled exclusively with coarse-

grained material, whereas others contain coarse-grained

deposits in the lower part which is covered by medium- to

fine-grained macroscopically structureless sandstone (Fig. 5C).

However, coarse-grained layers can occur in multiple levels in

one mega-flute. Particular coarse-grained layers may show

normal or inverse to normal grading. Most of the mega-flutes

are partly covered by recent debris or they are partly truncated

by recent erosion. Therefore, their total width was impossible

to estimate. Moreover, smaller, several centimetres thick

scours are abundant within the macroscopically structureless

and graded sandstone (Fig. 5A). The measured mean axis of

the scours and grain imbrication indicate N–S and NW–SE

orientations.

In order to determine the depositional process of facies 1

sandstones, two series of samples for grain-size analysis were

collected (Fig. 6). Series MAN1 1–16 was collected in

20–30 cm intervals from 3.8 m thick bottom part of the section

(Fig. 4). This sandstone interval rarely contains small mu d -

stone clasts and amalgamation surfaces, which disappear at

the distance of 1–3 m. Clasts are oriented parallel to the bed-

ding in a discrete horizons. Grain-size analysis showed that

sampled interval contains three fractionally graded amalga-

mated beds with mud content never exceeding 15 % by weight

(Fig. 6). Estimated beds thickness decreases from 180 cm at

the bottom, 80 cm in the middle to 40 cm at the top of the

sampled interval (Fig. 6).

The second series of samples MA1 1–6 was collected in

10 cm intervals, from the middle part of the section, which

include coarse-grained amalgamated sandstone (Fig. 4).

The series starts at the bottom of an abrupt coarsening surface

and includes two such surfaces. The analysis shows presence

of the normal grading at the bottom amalgamation surface and

the inverse to normal grading in the upper one (Fig. 6).

The contribution of mud does not exceed 12 % by weight in

the whole sample series (Fig. 6).

Interpretation: Facies 1 sandstones are interpreted as

deposits of high-density turbidity currents mostly formed by

layer-by-layer incremental deposition (e.g., Lowe 1982;

Talling et al. 2012). Rapid fallout of grains from turbulent sus-

pension suppressed the formation of sedimentary structures

(Lowe 1982), however, grading was preserved. Mathematical

modelling studies of Baas (2004) showed that lack of T

Bouma intervals in the top of structureless sandstones cannot

be explained by abrupt deceleration of density flow only.

Macroscopically structureless and graded sandstone beds at

the MQ have no sign of water escape structures and lamination

in the upper part, they are within grain-size limit for ripple

lamination (< 0.7 mm), show wide grain-size distribution

(Fig. 6), and they do not have bioturbation structures.

Therefore, the laminated top of structureless beds was eroded

or bedforms are too thin to be recognized if duration of flow

was too short within plane bed and ripple stability fields (Baas

2004). Occurrence of amalgamation surfaces, clasts of mud-

stone and marlstone and scours directly indicate strong ero-

sional forces of the flows. Moreover, grain-size analysis

showed that amalgamation surfaces are not restricted only to

macroscopically abrupt grain-size coarsening but also occur

within the structureless part. Therefore, amalgamation sur-

faces are more abundant than Figure 4 shows.

Isolated and laterally discontinuous mega-flutes reflect

complex internal structure of the concentrated density flows

(sensu Mulder & Alexander 2001) responsible for their origin.

Such flows are featured by abrupt lateral transition from ero-

sional through bypass to depositional conditions near the bot-

tom. Fillings of the mega-flutes record a variety of depositional

conditions which are expressed by lateral changes in the tex-

ture and primary structure of sediments (e.g., Leszczyński

1989 and references therein). Coarse-grained flute filling and

coarse-grained amalgamation zones are basal lag deposits,

which represent the thickest material carried by traction near

the bottom (e.g., Dżułyński & Sanders 1962; Lowe 1982;

Postma et al. 1988; Sohn 1997; Strzeboński 2015). Vertical

multiple grain-size coarsening surfaces within some mega-

flutes indicate deposition from an unsteady fluctuating flow or

multiple filling of the flute by different events. Origin from

multistage filling from independent flows is more probable

because particular events would erode the top of the previous

filling and leave lag deposits to underline amalgamation sur-

face. Moreover, particular coarse-grained layers within the

mega-flute fills show normal grading and inverse to normal

grading from one coarse layer to another (Fig. 5C). Inversely

graded coarse-grained amalgamation zones like the one from

the M1 1–6 sampled interval imply deposition from high con-

centrated frictional traction where inversely grading is formed

in the basal layer by shearing and kinematic sieving (Sohn

1997; Cartigny et al. 2013). Sediments deposited from traction

are also confirmed by rare occurrence of coarse grains and

imbrication of pebbles.

One of the features of the high-density turbidites is c

oncen-

tration of clasts in discrete horizons like in some structureless

and graded sandstones in the MQ (Talling et al. 2012).

Clast

ransportation within the high-density turbidity current is

mostly on the rheological boundary between the turbulent

damped bottom part of the flow and the more turbulent top or

highly concentrated, turbulent damped, near bottom layer

driven by turbulence from a more diluted top (e.g., Postma et

al. 1988). M

ost of the elongated mudstone clasts suggest

transportation on top of the highly concentrated bottom part of

the high-density turbidity current, which prevented their

further erosion and allowed them to keep their longitudinal

shape. However, s

ome authors suggest that preservation of

mudstone clasts and their planar concentration to the top of

bed is rather typical of sandy debrites (e.g., Shanmugam 2006;

Strzeboński 2015).

The well-rounded marlstone clasts imply

relatively long traction transportation. Therefore, two impor-

tantly different shapes of clasts of lithologies which are easily

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Fig. 5.

Sediment

ological

features

facies

from

the

Manasterz

Quarry

section.

—

coarse-grained

amalgamation

surface

with

small

scale

scours

within

the

structureless

sandstone

facies

;

—

well-rounded

clasts

bluish-white

marlstone

oriented

parallel

the

bedding

discrete

horizon;

—

lar

scour

within

the

massive

sandstone

facies

filled

with

multiple

levels

oarse-grained layers. Particular coarse-grained layers show normal grading or inverse to normal grading

which correspond to multistage filling of the scour

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abraded suggest two different sources of the material and dif-

ferent distance of transportation. The marlstones clasts sug-

gest erosion in a more proximal slope setting and longer

transportation, whereas, elongated mudstones probably origi-

nated from undercutting of local overbanks.

The relatively small contribution of mud (Fig. 6) probably

corresponds to flow stripping, which caused grain segregation

in the long run confined flows and bypass of muddy dilute

upper part of the stratified density flow (e.g., Piper & Normark

1983; Peakall et al. 2000; Posamentier & Walker 2006;

0.9

0.5

0.6

0.7

0.8

MA 1

1.1

1.2

1.3

1.4

1.5

1.6

1.7

1.8

Mean grain size (φ)

Grains <0.054 mm
by weight (%)

MA 2

0.1

0.2

0.3

0.4

0.5

v.c

v.f

100

0.1

0.2

0.3

0.4

0.5

200

220

240

120

140

160

180

260

280

300

320

340

360

380

400

420

Debrites basal

lag deposits

MAN1 1-18

Channel element turbidite fill

Mean grain size (mm)

Mean grain size (φ)

Mean grain size (mm)

Grains <0.054 mm
by weight (%)

v.c

v.f

Mean grain size (φ)

Mean grain size (mm)

Grains <0.054 mm
by weight (%)

v.c

v.f

Fig. 6. Grain-size trends and mud content in MAN1 1–18, MA 1 1–6 and MA 2 1–8 sample series from the Manasterz Quarry section.

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McHargue et al. 2011). In such a case, sediments of the MQ

should be deposited in the relatively distal area to have enough

time for grain segregation during transportation.

Facies 2

The MQ section contains a few layers of very fine- to

coarse-grained sandstones with abundant large clasts of grey

and reddish-brown mudstone and bluish-white marlstones

(Fig. 7A). The layers are 1–2 m thick and can be traced over

distance up to tens of metres. The boundary between facies 1

and facies 2 is usually reflected by a change in grain-size and

mud content. Nevertheless, some beds of facies 1 seem to pass

into structureless clast-rich sandstone of facies 2 with no sharp

boundary. Angular to sub-rounded clasts represent the same

lithology as in the facies 1. However, marlstones in some

clasts, which are much thicker and poorly bioturbated, litho-

logically resemble the Węgierka Marl (e.g., Burzewski 1966;

Geroch et al. 1979; Fig. 7B). Clasts are mostly oriented with

their longer axis parallel to the bedding with maximum size up

to 150x60 cm. However, those with size up to tens of centi-

metres in diameter dominate. Some clasts contain incised

sand- and gravel-size grains chaotically distributed within the

clasts or filling clastic veins. Matrix is represented by fine- to

coarse-grained sandstone with slightly higher contribution of

mud than in facies 1, which laterally may pass into fine- to

medium-grained, dark, muddy sandstone with abundant small

mudstone clasts and veins and lenses of clean sandstone simi-

lar to facies 1. Chaotic distribution of coarse grains within the

matrix is reflected by their nest or patchy distribution and

lateral changes in their density (Fig. 7C). Fine-grained matrix

contains Thalassinoides and Ophiomorpha preserved as endich-

nial full reliefs. Moreover, some of the trace fossils cross-cut

marlstone clasts and are filled by the matrix (Fig. 7D).

Grain-size analysis of clast-rich layers includes samples

MAN1 17–18 from the bottom part and MA2 1–8, which were

collected in 5–10 cm intervals from the middle part of the sec-

tion (Fig. 5). Samples MAN1 17–18 show relatively muddy

(> 25 % of mud content by weight) fine-grained sandstones.

There is an important decrease in mean grain-size and mud

content from facies 1 to facies 2 in the sample series

MAN1 1–18.

Samples MA2 1–8 show alternations of fine- to medium-

grained, graded, clean sandstone and muddy sandstone. Layers

of muddy fine-grained sandstone are discontinuous laterally

and change their thickness from a few to tens of centimetres.

They correspond to matrix with veins and lenses of clean

sandstone described above. Amalgamation surfaces are

present at the bottom of the lower structureless clean sand-

stone and above the fine-grained sandstone and stand as

boundaries between facies 1 and facies 2. Similarly to MAN1

1–18, muddy layers are much finer-grained than in facies 1

clean sandstones.

Orientation of the longer axes of 103 clasts was measured in

different clast-rich layers (Fig. 4). Most of the clasts, which

were accessible for measurement, are concentrated within the

lowermost clast-rich layer. These data do not correlate with

orientation of erosional structures and grain imbrication,

which indicate NW-SE and N-S palaeotransport direction.

Collected data show that majority of clasts are oriented ran-

domly without any specific trend which may indicate palaeo-

flow direction (Fig. 4).

Interpretation: Fine- to coarse-grained, clast-rich, muddy

structureless sandstones of facies 2 are interpreted as debrites.

Numerous, chaotically oriented huge clasts could be trans-

ported only by matrix supported debris flows (e.g., Shanmugam

2006; Strzeboński 2015). Moreover, patchy and nest distribu-

tion of coarse-grains imply poor conditions for grain segre-

gation, which is the feature typical of laminar flow. Each

clast-rich layer represents one or more debrites, which in some

cases tend to abruptly pinch out laterally. Abrupt change in

thickness and pinch-out of clast layers over a distance of

several metres agrees with the spatial shape typical of debrites

(e.g., Amy & Talling 2006). In some case laterally disconti-

nuous muddy type of matrix with veins and lenses of clean

sandstone may represent large eroded muddy boulders, which

were poorly mixed during transportation with sandy matrix of

the previous flow. Moreover, the poor roundness of larger

clasts confirms weak interactions between components during

transportation. Parallel orientation of clasts to the bedding and

occurrence of veins filled by sand- and gravel-size grains

imply matrix internal shear stress during debris flows move-

ment. The occurrence of huge boulders of marlstone typical of

the Węgierka Marl suggests shelf origin of some debrites and

therefore, relatively long distance of transportation. However,

rare occurrence of thin, tens of centimetres long, unfolded

mudstone clasts imply that there were also short-lived slides

with internal shear low enough to prevent clast deformation

and folding. Similarly to facies 1, they may derived from

undercutting of local overbank deposits. The erosional

potential of some debris flows is reflected by uneven bottom

surfaces and incision of debrites into turbiditic sandstone of

facies 1.

Particle-size analysis shows important change in grain-size

and mud contribution from deposits of turbidity currents and

debris flows in both MAN1 and MA2 samples series (Fig. 6).

Some of the debris flows were probably transformed from

concentrated to hyperconcentrated density flows by increasing

contributions of cohesive mud from disintegration of eroded

clasts (Mulder & Alexander 2001), which agrees with the

abundance of clasts and poor boundary between some beds of

facies 1 and 2.

Occurrence of clasts of marlstone cross-cut by bioturbation

structures filled with surrounding matrix implies bioturbation

after deposition of debrites (Fig. 7C). This indicates good

post-depositional environmental oxic conditions for benthic

life. Preferential occurrence of bioturbation structures within

the debrites may result from higher contributions of supplied

nutrients or from periods of decreased sedimentation rate

after deposition of debrites. Nevertheless, lack of biotur-

bation structures at the top of facies 1 beds may result from

erosion.

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Fig. 7.

Sediment

ological

feature

facies

from

the

Manasterz

Quarry

section.

—

clast-rich

sandy

debrite;

—

a huge

boulder

bluish-white

marlstone

similar

the

Węgierka

Marl

the

sandy

debrite

facies

—

sandy

debrite

with

clast

marlstone

cross-cut

bioturbation

structures

filled

with

surrounded

matrix.

White

arrows

show

bioturbation

structures;

—

clast-rich

(c)

sandy

debrite with sharp boundary between coarse-grained (c.m) and fine-grained matrix (f.m).

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Facies 3 or large boulder?

In the lower part of the MQ section, a 1.8 m thick layer of

grey to bluish-white, calcareous mudstone with rare alterna-

tion of < 0.6 cm thick siltstone is present. To the top and bot-

tom, sharp boundary with sandstone of facies 1 is observed.

Laterally, mudstone layer is continuous over a distance of at

least 3 m. Nevertheless, incomplete exposition does not allow

determination of its true lateral size and continuity. The mud-

stone is structureless and it shows no sign of bioturbation.

The siltstone is laminated and rich in plant detritus. It shows

sharp bottom boundaries.

Interpretation: Grey, calcareous mudstones are hemipe-

lagic to pelagic facies typical of basin slope. Laminated silt-

stones are interpreted as deposits of dilute low-density

turbidity currents and correspond to the T

Bouma division,

but their origin from bottom currents cannot be totally

excluded. Uncertain lateral continuation and exceptional

thickness suggest that this mudstone-dominated layer may

represent a large boulder within a debris flow rather than

a cape of thick sandstones from below. Moreover, some tran-

sition from very thick-bedded sandstone to very thick mud-

stones might be expected, but it is absent in the section studied.

Nevertheless, such a mudstone layer may also originate from

an abrupt decrease of activity in the source area, which resulted

in vanishing of sand deposition in the study area.

Manasterz Quarry section as a channel-fill

Deep-sea channels are often thought as prolongation of

deep-sea canyons or gullies, which distribute boulder to clay

size material from upper and middle slope to abyssal plain.

Deep-sea channels show many different forms with two end

members where dominating processes are erosion (incising

channels) or aggradation (constructive channels) respectively

(e.g., Normark 1970; Flood et al. 1991; Hübsher et al. 1997;

Babonneau et al. 2002).

Deep-sea channels are distinguished

as one of the hierarchical elements within deep-water deposi-

tional systems. Stacking of storeys or channel elements form

channel complexes, channel complex sets and channel sys-

tems (Sprague et al. 2002, 2005; Abreu et al. 2003). Channels

are relatively temporary structures, which migrate laterally by

avulsion and lateral accretion. In this paper the MQ section

facies are interpreted as deep-sea channel deposits with fea-

tures and characteristics that are discussed below.

Channel characteristics of the Manasterz Quarry section

The MQ section shows the following features typical of

deep-sea channel facies: high sand-to-mud ratio, occurrence

of thick structureless and graded sandstones with paucity of

sedimentary structures, a relatively high contribution of coarse

material, numerous amalgamation surfaces, abundant scours

and rip-up clasts and basal lag deposits (e.g., Mutti & Normark

1987; Shanmugam & Moiola 1988;

Mayall et al. 2006;

McHargue et al. 2011; Hubbard et al. 2014). Facies

comparison in the same basin is a useful tool for distin guishing

between particular facies of deep-sea channels (McHargue et

al. 2011). The MQ section shows an extremely high sand-to-

mud ratio in comparison to other outcrops of the Ropianka

Formation (e.g., Bromowicz 1974; Kotlarczyk 1978). In the

close vicinity of the study area, only a few small isolated out-

crops with facies similar to the MQ section are available

(Salata & Uchman 2013; Łapcik et al. 2016). This may sug-

gest that deposits in the MQ section are related to a channel

axis depositional environment.

An important feature of deep-sea channels is the lateral tran-

sition from channel axis to channel margin and channel-levee

facies (e.g., Campion et al. 2000; Sprague et al. 2002, 2005;

Gardner et al. 2003;

Mayall et al. 2006;

McHargue et al. 2011;

Hubbard et al. 2014).

Usually, the transition from channel axis

to channel margin facies occurs at a distance of a few hundreds

of metres (e.g., Shanmugam & Moiola 1988; Bruhn & Walker

1997; Campion et al. 2000; McHargue et al. 2011; Hubbard et

al. 2014). The MQ thick-bedded sandstones are estimated to

totally pinch-out to the NW at a distance of no more than

800 m (Fig. 1C). The outcrops which occupy similar strati-

graphic positions to the MQ sandstones are dominated by thin-

and medium-bedded sandstones alternated with mudstones

and siltstones (Fig. 2). This facies change suggests a lateral

offset of channel facies, which passes into channel margin or

channel levee facies. In the close vicinity to the SE, facies

similar to the MQ section are unknown (Gucik et al. 1980).

Therefore, thick-bedded sandstones probably pinch-out late-

rally at a distance of tens to hundreds of metres. The total

width of the Manasterz Quarry channel should not exceed

a few hundreds of metres.

Formation and filling of the Manasterz Quarry channel

Deep-sea c

hannels can be filled by turbidites, debrites,

slumps and hemipelagic deposits with different contributions

of these components but with a generally decreasing quantity

of mass transport deposits downcurrent (e.g., Shanmugam &

Moiola 1988; Dakin et al. 2013; Bayliss & Pickering 2015a).

Channel incision is mostly attributed to erosion by previous

high-density turbidity currents or the current responsible for

channel filling. However, some of them can be created during

bypass of debris flows when erosion can reach tens of metres

(e.g., Dakin et al. 2013).

The MQ channel is filled with mixed

deposits of high-density turbidity currents and debris flows.

Numerous amalgamation surfaces and alternations of turbi-

dites and debrites imply a multistage process of filling charac-

terized by repetitive transitions from deposition with a basal

lag through erosion of the lag and to channel filling with domi-

nation of structureless and graded sandstones (e.g., Clark &

Pickering 1996; Gardner et al. 2003). Thickness of the MQ

channel reaches at least 31 m and is in range of channel-fill

thickness (e.g., Sprague et al. 2005;

Mayall et al. 2006;

McHargue et al. 2011; Hubbard et al. 2014). The lowest

hierarchical architectural element in channel settings are

storeys or channel elements with thicknesses usually does not

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exceeding 5 m (Sprague et al. 2002). The internal architecture

of the MQ section allowed to distinguish storeys with two

basic elements, which repeatedly occur within the section.

The first basic element includes debrites of facies 2, which

correspond to basal lag deposits at the bottom of a particular

storey (e.g., Mayall et al. 2006). Occurrence of these deposits

determines the boundary between different storeys located at

their base. Facies 1 represents storey-fill, deposited after sedi-

mentation of debrite basal lag deposits. The MQ section con-

sists of five storey-fills alternating with three debrite basal lag

deposits (Figs. 4, 8). It is uncertain if the channel element

turbidite fill 5 represents two different elements separated by

poorly exposed debrite or one very thick storey-fill (Figs. 4, 8).

Thickness of particular storey varies from 2.5 m to 8 m or up

to 13 m if the channel element 5 represents one channel

element (Fig. 4). The thickness of particular debrite basal lag

deposits is much thinner and reaches 1–2 m. The cover of the

bottom part of the section does not allow us to distinguish the

basal lag deposits of the first storey. Alternatively, debrites

may represent event deposits, which randomly interrupted

turbidite sedimentation during formation of the channel-fill.

However, multiple repetition of 1) deposition of debrite lag

deposits, 2) erosion of debrite lag deposits and 3) deposition of

high-density turbidites supports the first alternative.

Thick-bedded structureless and graded sandstone facies and

their vertical stacking suggest that the MQ section may repre-

sent an area near the thickest part of the channel where the

coarsest material is stacked. Moreover, vertical stacking of

couplets of facies 1 and facies 2 suggests affiliation to a larger

channel-fill or a channel complex set with an aggradation rate

higher than its lateral migration. Such channel facies cannot

aggrade without simultaneous aggradation of levee confine-

ment (McHargue et al. 2011). Hence, interpretation of the out-

crops in the similar stratigraphic position to the NW as channel

margin or channel levee is most probable (Figs. 1C, 2).

Channel formation can be subdivided into three stages: 1)

erosion and bypass when large scale erosional surfaces up to

tens of metres are formed and capped by lag deposits, 2) chan-

nel fill when the coarsest material is repeatedly deposited and

eroded with simultaneous sediment spill outside the channel,

and 3) abandonment when the finest material caps and sepa-

rates two channel elements (e.g., Clark & Pickering 1996;

Gardner et al. 2003; Mayall et al. 2006; Labourdette et al.

2008; Dakin et al. 2013; Bayliss & Pickering 2015a, b).

Abundant amalgamation and small scale erosion, relatively

low contribution of lag deposits and domination of deposits of

collapsing flows imply that the MQ deposits represent the

channel fill stage. According to McHargue et al. (2011), early

filling and amalgamation of a channel begins after stabiliza-

tion of the equilibrium profile by the previous erosional stage.

Despite lower energy of the flows during the filling stage,

erosion is still prominent, especially near the channel axis.

Moreover, occurrence of clast-rich debrites is common during

the early amalgamation stage (McHargue et al. 2011).

Most of

the models assume that the last stage of the channel formation

is abandonment recorded by sedimentation of thin-bedded

deposits. Lack of fining and thinning upward trend in the MQ

section may derive from poor exposure where all deposits

represent only a small part of a larger channel complex set.

Alternatively, the presence of a nearby strongly developed

levee, may also preclude development of fining and thinning

upward trends (Shanmugam & Moiola 1988). Such a levee

may be represented by previously mentioned facies in the

similar stratigraphic position to the NW of the MQ. It is pos-

sible to speculate that highly amalgamated deposits forming

architecture of the MQ channel correspond probably to abun-

dant avulsion and low aggradation of secondary (inner) over-

bank on the scale of channel elements (Deptuck et al. 2003;

Posamentier & Kolla 2003; McHargue et al. 2011).

Location of the Manasterz channel in the Skole Basin

Abundance of mass movement and sediment gravity flow

deposits with extrabasinal material and distribution of marl-

stone facies suggest that sedimentation of the most external

part of the Ropianka Formation took place on the middle or

lower basin slope or close to the base of the slope (e.g.,

Burzewski 1966; Bromowicz 1974; Kotlarczyk 1978, 1988;

Jankowski et al. 2012; Łapcik et al. 2016).

Analysis of heavy

minerals from the Ropianka Formation showed that its depo-

sits derive from an immature passive margin setting (Salata &

Uchman 2013).

The MQ section represents an area of abun-

dant erosion and abrupt waning flows, which correspond to

hydraulic jump of the flow. The channel-lobe transitional zone

is considered as a site of abundant hydraulic jump with com-

mon scouring and erosional structures (e.g., Mutti & Normark

1987; Wynn et al. 2002, Gardner et al. 2003). However, the

channel-lobe transitional zone usually includes traction struc-

tures (often large scale), which are absent at the MQ (e.g.,

Mutti & Normark 1987; Wynn et al. 2002). High contribution

of large intrabasinal rip-up clasts in the MQ section suggests

strong erosional forces in the previous flow stage. Hence, the

MQ channel is probably incised into mudstone- and marl-

stone-rich deposits of the Skole Basin slope or such clasts

derived from undercutting of the channel levees. The

occur-

rence of extrabasinal, shallow water material in the MQ

deposits suggests a strong relationship with the Skole Basin

shelf. Carbonate mud and shell debris were redeposited into

offshore and afterwards slope areas probably by lowering of

the storm wave base. Such material suggests a relationship

with canyons or gullies which captured it after redeposition by

storm events from more proximal areas.

Previously postulated simultaneous aggradation of over-

bank deposits and channel-fill is strongly related to contribu-

tion of overspilled mud from turbidity currents and with

proximal-to-distal position of the channel. The height of

levees can reach hundreds of metres and decreases downcur-

rent with decreasing amounts of the fine-grained cohesive

material which stabilize levee banks (Damuth & Flood 1985).

The

low contribution of mud within deposits of high-density

turbidity current in the MQ section suggests spillover and

bypass of more muddy parts of the flow. Further evidence for

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strong bypass is the almost complete

lack of o

rganic detritus and coal debris

in the MQ section. Such material is

often an important component of

thick-bedded sandstones in the

Ropianka Formation (e.g., Kotlarczyk

& Śliwowa 1963; Łapcik et al. 2016;

Łapcik in press). It is unlikely that these

deposits are related to another source

area than sandstones from the lower

part of the section (Manasterz-Rzeki)

because such material is known from

even younger deposits (e.g., Kotlarczyk

& Śliwowa 1963). Therefore, the most

probable scenario is bypass of organic

detritus and coal, which was deposited

in a more distal area, for example, in

the lobe-like deposition of the Słonne

section (Łapcik in press).

Hence, the

MQ channel should be situated in rela-

tively proximal area on the lower slope

or near base of the slope. According to

Gardner et al. (2003), the MQ section

shows features of the fill stage of

a channel situated in the lower slope or

base of the slope. This also stands in

agreement with the proximal location

of the MQ section within the second

thrust sheet from the northern

Carpathian margin.

Palaeotransport directions and

sinuo sity of the Manasterz Channel

Deposits of the Ropianka Formation

show directions of the palaeotransport

from NW, N and NE with dominance of

the NW direction in the vicinity of

the study area (Książkiewicz 1962;

Bromowicz 1974). The palaeotransport

data from the MQ include only mea-

surements of scour orientation and

grain imbrication within the structure-

less and graded sandstones, which indi-

cate transportation from the NW.

Nevertheless, directions of transport in

a deep-sea channel may be variable and

are rarely unidirectional. Spatial distri-

bution and orientation of long belts of

thick-bedded sandstone facies in the

external part of the Ropianka Formation

is consistent with the presented data

and also point to the NW–SE axis

(Gucik et al. 1980). All these data are

premises for deposition of thick-bed-

ded sandstone facies in the vicinity of

Fig. 8.

The

Manasterz

Quarry

section

with

distinguished

channel

elements.

—

the

Manasterz

Quarry

with

distinguished

channel

elements.

—

top

the

Manasterz

Quarry

with

distinguished

channel elements.

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the study area longitudinal to the slope of the Skole Basin.

Most of these facies suggest a strong relationship with the

Łańcut Channel Zone proposed by Kotlarczyk & Leśniak

(1990) for the Oligocene deposits (see also Salata & Uchman

2012, 2013). It seems that this channel zone was already active

during the Late Cretaceous.

The previously mentioned lateral offset of the facies from

the channel axis to the channel margin or channel levee from

the MQ section to the Manasterz section allows speculation

about sinuosity of the studied channel. Otherwise, axial or

off-axial channel facies would be continued to the NW in the

Manasterz section. Hence, the channel facies outcropping in

the MQ should change their orientation to the N or the W to

evade the Manasterz channel levee facies. Nevertheless, the

MQ section does not appear to have lateral accretion packages

that have been described in

other meandering channel-fill

deposits (e.g., Bouma & Coleman 1985; Mutti & Normark

1991; Abreu et al. 2003; Janocko et al. 2013). Unfortunately,

covering of the area, tectonic def

ormations and inclination of

beds does not allow tracking of the channel facies.

Interpetation of the Manasterz-Rzeki and Manasterz facies

Bottom and top parts of the Manasterz-Rzeki and the

Manasterz section

The bottom and top parts of the Manasterz-Rzeki section

show many similarities to the bottom part of the Manasterz

section (Fig. 2). Thin- to medium-bedded sandstones and

marlstones with abundant parallel, cross and convolute lami-

nations probably correspond to channel levee or inter-channel

deposits.

The

decreasing contribution of marlstones in the bot-

tom part of the Manasterz section suggests that this interval is

situated above the second marlstone-rich interval of the

Manasterz-Rzeki section (Figs. 1C, 2).

Such marlstones are

widely distributed in the Ropianka Formation in the whole

marginal part of the Skole Nappe (e.g., Kotlarczyk 1978,

1988; Leszczyński et al. 1995). The marlstones are considered

as calciturbidites with their source area situated in the shelf

surrounding the Skole Basin. They were deposited by low-den-

sity turbidity currents in the marginal part of the Skole Basin,

which probably corresponds to the basin slope and base of the

slope. However, marlstone clasts from the MQ derive from

erosion of marlstones form the older part of the Ropianka

Formation. After partly lithification they, were ripped up by

high-density turbidity currents and redeposited into a more

distal area.

Thick-bedded sandstones occur in the Manasterz-Rzeki and

Manasterz sections. Stacking of thick-bedded, structureless

and graded sandstones often with parallel laminated top alter-

nating with thin- and medium-bedded laminated sandstones

suggest channel or depositional lobe facies. However, the

thickness and sand-to-mud ratio of these intervals together

with sparse amalgamation and scours suggest some distance

from the axis of such bodies in comparison to the MQ section.

Both sections represent progradation and aggradation of some

sand-rich body. Decreasing contribution of marlstones with

simultaneous increase in thick-bedded sandstones (Fig. 3)

may imply: 1) decreasing activity in the carbonate source area,

2) progradation of a sand body which temporarily became

an obstacle for calciturbidites, or 3) increasing activity in the

siliciclastic source area, sediments from which diluted the car-

bonate sedimentation. The relative proximity of these deposits

can be referred to the marginal position of the study area in the

Skole Nappe (second thrust sheet from the Carpathians mar-

gin). Tectonic deformations of the study area do not allow

certain correlation between the sections studied. It is not clear

whether the two thick-bedded intervals of the Manasterz-

Rzeki and Manasterz sections represent the same sand body or

two different sand bodies. The main difference between these

thick-bedded sandstones is abundance of coal debris in the

Manasterz section. However, this is too weak a premise to

exclude any alternative. If the two intervals represent different

bodies, the interval with decreasing contribution of marlstones

at the bottom of the Manasterz section may correspond to the

lateral offset of channel or lobe facies of the Manasterz-Rzeki

section, and the upper part of the Manasterz-Rzeki section

may correspond to channel abandonment facies or channel

levee facies.

These speculations also imply on

lateral migra-

tion of sandy bodies at the distance of hundreds of metres

derived probably from avulsion (Fig. 1C).

The Węgierka Marl

The Węgierka Marl is widely known from the Ropianka

Formation in the external part of the Skole Nappe and is

mostly represented by packages of fine-grained, muddy sand-

stones with mudstone and marlstone clasts, up to tens of centi-

metres thick, and sandy calcareous mudstones with dispersed

quartz pebbles and clasts of marlstone. Moreover, huge marl-

stone olistoliths are also known (Burzewski 1966; Kotlarczyk

1978, 1988; Geroch et al. 1979). Such deposits mostly repre-

sent slumps and debris flows originating in the middle to

lower slope setting. Their abundance and spatial distribution

suggest their classification as mass transport deposits com-

plex, which influenced the basin floor morphology. Mass

transport deposits often occur at the bottom of channels and

channel complexes (Clark & Pickering 1996; Mayall et al.

2006; Bayliss & Pickering 2015a). In the study area, the

Węgierka Marl facies are located at the bottom of the MQ

channel facies. Hence, the Manasterz Quarry channel complex

was formed on its floor with abundant debrites which could

stand as confinement of the initial channel zone. In the

Leszczyny Member, the Węgierka Marl and thick-bedded

sandstones often alternate (e.g., Burzewski 1966; Bromowicz

1974; Kotlarczyk 1978, 1988; Geroch et al. 1979) but it is not

clear if massive sandstones of the MQ section are situated only

at the top of the Węgierka Marl, or if they also border with

them laterally and/or are capped by them. Some of the debrites

in the MQ section contain huge boulders of marlstone very

similar to the Węgierka Marl. This suggests that mass trans-

port of the Węgierka Marl deposits also filled some channels

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GEOLOGICA CARPATHICA

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and that the channel filling is influenced by sea-level changes

or short tectonic activities, which may trigger deposition of the

Węgierka Marl mass transport deposits complex (Burzewski

1966; Geroch et al. 1979). Incision of the channels reflects

direct changes in the slope equilibrium profile and may

additionally suggest sea-level changes (e.g., Kneller 2003).

The whole composite Manasterz section represents transition

from lobe or channel off-axis facies alternating with inter-channel

or overbank deposits of the Wiar Member to the MQ channel

axis facies incised into the Węgierka Marl mass transport

deposits complex of the Leszczyny Member.

Conclusions

1. Sandstones of the Manasterz Quarry represent channel axial

or near axial facies with abundant amalgamation, coarse lag

deposits, intra- and extrabasinal material. The studied

section is dominated by deposits of high density turbidity

currents (facies 1) with a smaller contribution of debrites

(facies 2).

2. The Manasterz Quarry section represents channel-fill with

total thickness of 31 m and width up to several hundreds of

metres. The channel includes 5–6 storeys with debrite basal

lag deposits at the bottom of storeys capped by channel tur-

bidite fill. The basal lag deposits are 1–2 m thick, whereas

the turbidite channel are 1.5–11.5 m thick. The channel-fill

was formed by repeated deposition and amalgamation of

turbidites and debrites.

3. Strong bypass, occurrence of lag deposits with material

deri ving from shallower zones and location relatively close

to the northern margin of the Skole Basin suggest slope or

base of slope setting of the Manasterz Quarry channel.

The Manasterz Quarry deposits correspond to channel fill

and amalgamation stage (Gardner et al. 2003; McHargue et

al. 2011).

4. The section to the NE of the Manasterz Quarry represents

levee or inter-channel deposits related to the Manasterz

Quarry channel-fill. Its similar stratigraphic position and

occurrence on the path of the palaeoflow direction of the

Manasterz Quarry section are premises for sinuosity of

the Manasterz Quarry channel.

5. The whole composite Manasterz section represents a transi-

tion from lobe off-axis or channel off-axis facies alternated

with inter-channel or overbank deposits of the Wiar Member

(lower Campanian–lower Maastrichtian) to the Manasterz

Quarry channel axis facies incised into the Węgierka Marl

mass transport deposits complex of the Leszczyny Member

(lower Maastrichtian–lower Palaeocene).

6. The

described channel architectural elements of the Ropianka

Formation are located within the so-called Łańcut Channel

Zone, which was previously proposed for the Oligocene

sediments but may already be present in the Late Cretaceous.

Acknowledgements: This study was supported by the Jagiel-

lonian University DS funds. Thanks to W. Nemec (Bergen) for

discussion. Special thanks to A. Uchman (Kraków) for discus-

sion and improvements of the paper and for sharing of photo-

graphs of the Manasterz Quarry section from the period before

this study began. The author is greatful to reviewers Piotr

Strzeboński and unknown reviewer for their constructive

comments.

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