GeolCarp_Vol68_No5_479

GEOLOGICA CARPATHICA

, OCTOBER 2017, 68, 5, 479–500

doi: 10.1515/geoca-2017-0031

www.geologicacarpathica.com

Tectono-sedimentary analysis using the anisotropy of

magnetic susceptibility: a study of the terrestrial and

freshwater Neogene of the Orava Basin

MACIEJ ŁOZIŃSKI



, PIOTR ZIÓŁKOWSKI and ANNA WYSOCKA

University of Warsaw, Faculty of Geology, Żwirki i Wigury 93, 02-089 Warszawa, Poland;



maciej.lozinski@student.uw.edu.pl

(Manuscript received February 2, 2017; accepted in revised form June 9, 2017)

Abstract: The Orava Basin is an intramontane depression filled with presumably fine-grained sediments deposited

in river, floodplain, swamp and lake settings. The basin infilling constitutes a crucial record of the neoalpine evolution

of the Inner/Outer Carpathian boundary area since the Neogene, when the Jurassic–Paleogene basement became

consolidated, uplifted and eroded. The combination of sedimentological and structural studies with anisotropy of

magnetic susceptibility (AMS) measurements provided an effective tool for recognition of terrestrial environments and

deformations of the basin infilling. The lithofacies-oriented sampling and statistical approach to the large dataset of AMS

specimens were utilized to define 12 AMS facies based on anisotropy degree (P) and shape (T). The AMS facies allowed

a distinction of sedimentary facies ambiguous for classical methods, especially floodplain and lacustrine sediments, as

well as revealing their various vulnerabilities to tectonic modification of AMS. A spatial analysis of facies showed that

tuffites along with lacustrine and swamp deposits were generally restricted to marginal and southern parts of the basin.

Significant deformations were noticed at basin margins and within two intrabasinal tectonic zones, which indicated the

tectonic activity of the Pieniny Klippen Belt after the Middle Miocene. The large southern area of the basin recorded

consistent N-NE trending compression during basin inversion. This regional tectonic rearrangement resulted in a partial

removal of the southernmost basin deposits and shaped the basin’s present-day extent.

Keywords: Orava–Nowy Targ Basin, Neogene, intramontane basins, basin inversion, facies analysis, anisotropy of

magnetic susceptibility.

Introduction

The anisotropy of magnetic susceptibility method has been

approved for decades as an effective tool in a broad spectrum

of geological applications (e.g., Graham 1954; Hrouda 1982;

Tarling & Hrouda 1993; Parés 2015). Any rock composed of

mineral grains is characterized by a magnetic susceptibility

reflecting the minerals’ contribution to an applied external

magnetic field. This physical feature usually differs with res-

pect to the direction of the field, which is referred to as the

anisotropy of magnetic susceptibility (AMS). For paramag-

netic and diamagnetic grains (such as clay minerals, quartz

and carbonates) the AMS is a result of their specific magne-

tocrystalline anisotropy, whereas ferromagnetic grains (typi-

cally iron oxides and sulphides) may additionally have the

easy direction of magnetization related to the shape and size of

grains (Rees 1965), as well as to intergranular interactions.

The AMS measurement reflects the total effect of all grains in

a specimen and is predominantly studied in a phenomeno-

logical and descriptive way. The result depicts a sediment or

rock preferred grain alignment and is usually interpreted in

terms of bedding orientation and flow directions, as well as

structural lineation and foliation being a result of deformation

(see discussion in Hrouda 1982).

The application of the AMS method in orogeny-related

basins and accretionary prisms predominantly concerns

a structural interpretation of strain directions (e.g., Hrouda &

Potfaj 1993; Parés et al. 1999; Kanamatsu & Herrero-Bervera

2006; Hrouda et al. 2009; Mazzoli et al. 2012) and turbidity

current directions (e.g., Tamaki et al. 2015), while hemi-

pelagic and pelagic sediments are examined for the occurrence

and directions of bottom currents (e.g., Ellwood & Ledbetter

1977; Shor et al. 1984; Joseph et al. 1998; Park et al. 2000;

Baas et al. 2007; Parés et al. 2007). The sedimentological ana-

lysis supported by AMS measurements has also been done in

a variety of sedimentary settings, namely: deep sea fans and

turbidity deposits (von Rad 1970), deep-sea mass transport

deposits (Novak et al. 2014), alluvial fine-grained sediments

(Garcés et al. 1996; Park et al. 2013), pyroclastic density

currents and lahar deposits (Biró et al. 2015; Ort et al. 2015),

as well as glacial sediments (Eyles et al. 1987; Gravenor &

Wong 1987). In this study we aim to analyse fine-grained

freshwater and terrestrial deposits of the Orava Basin (Łoziński

et al. 2015) focusing on both sedimentary and structural aspects

of the AMS results.

The Orava Basin is a Neogene intramontane basin in the

Western Carpathians. The time of the basin’s development

corresponds to the termination of formation of the Outer

480

ŁOZIŃSKI, ZIÓŁKOWSKI and WYSOCKA

GEOLOGICA CARPATHICA

, 2017, 68, 5, 479–500

Jabłonka

Czarny Dunajec

Chochołów

Trstená

Bobrov

Námestovo

Nové Ústie

Stare Bystre

Lipnica Wielka

Lipnica
Mała

Czarny

Dunajec

Chyżny

Oravica

Orava

Cichy

Bystry

Chyżnik

Lipnic

Červený

Syhlec

Czarna

Orawa

Polhoranka

Kovalinec

Krz1

Koz1

Na1

Bo1

Us1

Us2 Us3

Ko1, Ko2

Uh1

UhQ2

By1

By2

By3

Wo1

DW1

CD1

CD2_1,2

CD3_1,2,3

CD4

CD5

Tv1

Je1
Je2i3
Je4

Je9

Je10

LM1

LM2

Ce1

JeQ1

JeQ2

Je6

Je7

Je8

Ce3÷Ce11

JeQ3

JeQ4

JeQ5

Ch2

Ch4

Ch3

Jo1

Jo2

Jo4, Jo5

Jo6

Jo3

Ch1

Chk1

Ku1

Co1

Li1

Li2

Bv1

Bv3

Bv2

Oravica River

section Or*

4 km

49.50°

49.45°

49.40°

49.35°

49.50°

49.45°

49.40°

49.35°

19.60°

19.70°

19.80°

19.90°

19.50°

19.60°

19.70°

19.80°

19.90°

rav

a L

ake

PIE

NIN

Y K

LIPP

EN B

ELT

PODHALE SY

NCLINORIU

CENTRAL CA

RPATHIAN P

ALEOGENE

ORAVA

BASIN

MAGURA NAPPE

(PKB)

PKB

POLAND

CZECH

REP.

SLOVAKIA

HUNGARY

study area

Carpathians thrust-and-fold belt, and submission of the oro-

geny to exposure and erosion (e.g., Jankowski & Margielewski

2014). The Orava Basin comprises the excellent sedimentary

record of the structural and environmental evolution of the

studied region of that time. This involves the transition

from marine to terrestrial sedimentation (Birkenmajer 1954;

Cieszkowski 1995), development of regional strike-slip move-

ments in the Carpathians (Kováč et al. 1993) and the uplift and

erosion of individual blocks of predominantly Paleogene

rocks in the vicinity of the basin (Tokarski et al. 2012;

Jankowski & Margielewski 2014). However, fine-grained

deposits often are macroscopically structureless and since they

lack correlation indicators, they are not easy to interpret.

We expect that the application of the AMS method may signi-

ficantly contribute to knowledge of the basin’s history.

This study is based on the very detailed facies study of

lacustrine, flood plain, alluvial, and swamp settings presented

in Łoziński et al. (2015). The local facies model for the

well-exposed section of the Oravica River has been verified

and adapted in this paper to describe facies within the whole

basin. The problem of the interplay of tectonic and sedimen-

tary factors in determining the AMS fabrics for the moderately

deformed Oravica River section has already been discussed in

a case-study paper of Łoziński et al. (2016). The considerable

variety of the obtained AMS fabrics suggested a possible

recog nition of the AMS facies reflecting the depositional

processes. The aim of this paper is to construct a model for

fine-clastic deposits of the Orava Basin, which hopefully will

be for universal use as well. This study is based on a large data

set of field-collected spatially oriented AMS specimens (1930

specimens from 85 locations, see Appendix) collected with

respect to the recognized lithofacies. The AMS results are

interpreted to reconstruct the facial scheme of the basin and to

depict its deformational style and possible tectonic strain

directions.

Geological setting

The Orava Basin is currently an approximately 35 km long

and 15 km wide intramontane depression straddling the Inner/

Outer Carpathian border (Fig. 1). It is filled with predomi-

nantly terrestrial clastic sediments which overlie preconso-

lidated, folded and partially eroded older units: mostly the

Magura Nappe, Pieniny Klippen Belt, and Podhale Syncli-

norium. The northernmost unit, Magura Nappe, is built up of

Albian/Cenomanian–Miocene sandstones, mudstones, and

marls (Birkenmajer & Oszczypko 1989; Cieszkowski et al.

1989; Cieszkowski 1995; Malata et al. 1996). The Pieniny

Klippen Belt comprises strongly deformed Early Jurassic–

Paleogene limestones, marls, mudstones, calcarenites, and

conglomerates (e.g., Birkenmajer 1960). The southernmost

part of the Orava Basin in underlain by the Podhale

Synclinorium, a folded Lutetian/Bartonian to Egerian part of

the Central Carpathian Paleogene Basin (Gross et al. 1993b;

Olszewska & Wieczorek 1998; Soták 1998a, b; Garecka 2005).

After these units underwent folding and erosion, the W–E-

trending elongated depression was formed. The onset time of

the deposition in the Orava Basin is poorly constrained, ran-

ging from Late Oligocene (Woźny 1976), through Badenian

Fig. 1. The simplified geological map of the Orava Basin and its vicinity. The AMS sampling locations are marked with dots and sample

names. For detailed locations of the Oravica River section samples see Łoziński et al. (2016).

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GEOLOGICA CARPATHICA

, 2017, 68, 5, 479–500

(Oszast & Stuchlik 1977), Late Badenian or Sarmatian

(Cieszkowski 1995), to Sarmatian (Nagy et al. 1996).

However, most authors agree about the Middle Miocene age

of the basin’s origin which is based on the widely-studied flora

associations, and corresponds well with the opening time of

the transtensional basins inside the Carpathian orogenic belt

(Kováč et al. 1993). The dominant siliciclastic basin infill has

been probably derived from older eroded units exposed in the

vicinity of the basin (Birkenmajer 1954; Watycha 1976a;

Tokarski et al. 2012). The deposition of conglomerates, sand-

stones, clayey siltstones, claystones, and coals took place in

terrestrial and freshwater environments: alluvial fans, rivers,

flood plains, lakes and swamps (Watycha 1976a; Birkenmajer

1978; Kukulak 1998; Łoziński et al. 2015). The sedimentary

bodies of deposits are laterally and vertically restricted, and

strongly depend on their paleotopographic position. According

to Birkenmajer (1954) and Watycha (1976a), alluvial fans

with coarse clastics have been developed within the basin

margins. Grain size decreased towards the centre of the basin,

where river-associated and stagnant-water deposition took

place within extensive floodplains and swampy areas.

The abundant plant vegetation within the wet areas favoured

preservation of organic matter and initiated brown coal forma-

tion (e.g., Polášek 1959; Oszast & Stuchlik 1977; Kołcon &

Wagner 1991). Lacustrine deposits represent episodic lakes

and no basin-scale reservoir has been recorded during the

basin’s evolution (Watycha 1976a; Łoziński et al. 2015).

The sedimentary environment could have been disrupted by

volcanic ashfall events resulting in tuffite deposition (Beleš

1974; Sikora & Wieser 1974; Kołcon & Wagner 1991;

Łoziński et al. 2015). The topmost deposits of the Quaternary

age (Watycha 1976a; Baumgart-Kotarba et al. 1996) lie often

discordantly above older deposits. Apart from fine clastics,

they also represent large alluvial fans with pebbles and cob-

bles derived from adjacent areas and the Tatra Mts. This

records a major Quaternary uplift of adjacent source areas and

marginal parts of the basin, which could have had a wider extent

in the Neogene (Tokarski et al. 2012; Łoziński et al. 2015).

The depression could have been formed as a pull-apart basin

(e.g., Pospíšil 1990; Baumgart-Kotarba 2001), a releasing-

bend structure along the Pieniny Klippen Belt (Pomianowski

2003), or as a series of tectonic subbasins within the flexure of

the Outer Carpathian arc (Struska 2008).

Methods

This study is based on field sedimentological and tectonic

observations, magnetic measurements on a set of specimens

collected from outcrops, and pre-existing geological data:

detailed geological maps (Watycha 1976b, 1977a, b, c;

Gross et al. 1993a) and documentation of boreholes Czarny

Dunajec-IG1 (Watycha 1971) and OH-1 (Pulec 1976). Field

observations included: all macroscopic sedimentary and

diagenetic structures, grain size, colour, level of consolidation,

presence of tectonic fractures, faults and ductile deformation,

bedding orientation, as well as position in present-day sedi-

mentary environment with special attention to mass move-

ments. The age of the studied deposits considered to be

Neogene in this paper could not be exactly determined.

Instead, the sedimentological criterion has been used: all

fine-clastic sediments which could not be deposited in

a present-day sedimentary environment have been taken into

account.

The sampling process for magnetic measurements was

intended to give a 25-specimen representation of a sediment

mass of a specific lithofacies found in a studied location,

what is referred to here as a “lithofacies-oriented sampling”.

The conventional method of sampling a sedimentary vertical

sequence has been generally neglected here, since a sedimen-

tary environment in terrestrial settings may change within

small distances laterally and vertically. The sampling was con-

ducted using brass samplers hit with a rubber hammer into

a fresh surface of deposits (see the equipment in Łoziński et al.

2016). A cylinder obtained from a sampler has been cut into

standard ø 25.4 mm-wide and 22 mm-tall magnetic specimens.

All specimens have been collected with measured azimuth,

dipping angle and (in most cases) the axial rotation angle of

the sampler. It should be noted that weakly consolidated

deposits could have been altered by the hitting force and

acquired a false tectonic fabric. This has been examined by

applying different sampling azimuths, and then testing the cor-

relation between sampling direction and the AMS ellipsoid

directions. The total specimen dataset includes 1930 speci-

mens (322 specimens have been reused from Łoziński et al.

2015; names with prefix Or-) grouped into 85 statistical sam-

ples representing various lithofacies and localities (Fig. 1).

The specimens collected have been measured for volume

bulk magnetic susceptibility and its anisotropy at field inten-

sity 200 A/m and frequency 976 Hz using a MFK1-FA

kappa bridge with a 3D rotator (AGICO, Czech Republic).

The AMS obtained during measurements is defined as

a second-rank tensor with symmetrical 3×3 matrix repre-

sentation. The ana lysis of AMS is performed using convenient

anisotropy parameters: main axes of anisotropy ellipsoid k1,

k2, and k3 (axis of maximum, intermediate, and minimum

susceptibility accordingly), anisotropy degree P = k1/k3, linea-

tion L = k1/k2, foliation F = k2/k3, and anisotropy shape

T = [2 log(k2)−log(k1)−log(k3)] / [log(k1)−log(k3)]

(Hrouda 1982 and references therein). Multispecimen statis-

tical processing has been done according to mean tensor

calculation defined in Jelínek & Kropáček (1978).

The magnetic mineralogy was assessed by two methods:

the Lowrie test and thermoanalysis, in which the distinctive,

characteristic coercivities and thermomagnetic properties of

the common ferromagnetic minerals have been used. The ana-

lysis of the acquisition curve of isothermal remanent mag-

netization (IRM) combined with subsequent thermal

demag netization of the IRM provided the interpretation of

the ferromagnetic mineral content of a rock (Lowrie 1990).

The 20 specimens were given an isothermal remanence (IRM),

in steps from 0.014 T up to 3 T along Z-axis, using

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ŁOZIŃSKI, ZIÓŁKOWSKI and WYSOCKA

GEOLOGICA CARPATHICA

, 2017, 68, 5, 479–500

magneti zation in a pulse magnetizer MMPM10 (Magnetic

Measurements, Great Britain). After each step the IRM was

measured using a spinner magnetometer JR6A (Agico).

Afterwards, different coercivity fractions of IRM were remag-

netized in successively smaller fields along two orthogonal

directions: 0.4 T along the Y-axis and 0.12 T along the X-axis.

After thermal demagnetization of 8 representative specimens

in a MMTD80A furnace (Magnetic Measurements), each

ortho gonal component of the composite IRM was plotted

separately. These results were supplemented by thermoana-

lysis by measuring bulk susceptibility of 3 specimens during

heating up to 700 °C and cooling down in a KLY3S/CS3

kappabridge (Agico). All magnetic procedures were carried

out at the European Centre for Geological Education (Chęciny,

Poland), except for the thermoanalysis which was carried out

at the Institute of Geophysics, Polish Academy of Sciences

(Warsaw, Poland). The data was acquired using SAFYR6,

REMA6 and SUSTE7 programs (Agico) and processed with

an R statistical software (R Core Team 2015).

Results

Facies model

The sedimentological analysis of this study is based on the

classical concept of lithofacies and facies associations (see

summary in Miall 2000). This practical approach aims at

defining sedimentary units based on macroscopic sediment

description and interpreting them in terms of physical condi-

tions, e.g.: mechanism of sediment transport, current velocity,

settling process, and biogenic activity. The analysis of litho-

facies associations in vertical and lateral extent is a basis for

interpretation of sedimentary environments. This kind of ana-

lysis has already been applied to the 90-m thick diversified

section of the Oravica River in the southern part of the Orava

Basin in Łoziński et al. (2015). For the purpose of this study

a new lithofacies scheme has been constructed for the whole

Orava Basin (Table 1).

The matrix-supported breccia (Gmm) is composed of angu-

lar clasts of older units spread in a predominantly muddy

matrix and lacking any sedimentary structures (Fig. 2). It has

been interpreted as a plastic debris-flow deposit which was

confined to areas of considerable terrain relief, probably

during pre-basinal basement erosion and later, at basin mar-

gins. In turn, the clast-supported conglomerate (Gcm, Fig. 3A)

represents deposits of low sediment concentration flow within

alluvial fans having a large lateral extent. Lithofacies Gh, Sh

Sp, and St depict bedforms deposited in a water current of

different strength and flow regimes usually within a fluvial

channel. Lithofacies Sm occurs typically as a structureless

intercalation within clayey and silty lithofacies CL, Fl, and Fm

(Fig. 2).

The massive clayey siltstone (lithofacies Fm, Fmc, and

Fmm) may reach thickness of several metres, and typically

lacks any sedimentary structures. Similar massive lithofacies

with rhizoliths may be found within present-day river banks

(Fig. 3B), usually overlying alluvial conglomerates (litho-

facies Gh). Fresh non-consolidated muds are well-oxidized

and often rich in organic matter, which makes them conve-

nient for biogenic activity. Faunal bioturbation is followed by

a quickly developing plant vegetation resulting in root biotur-

bation. Additionally, deposited muds being within a vadic

zone, undergo multiple changes in relative humidity. This

process has been recognized to degrade original sedimentary

structure into massive structure due to particle movements

during shrinkage and swelling (Wetzel & Einsele 1991).

The observable stage of biogenic activity is exhibited by

a sublithofacies Fmm (Fig. 3C) being in most cases a rela-

tively young deposit of the Orava Basin. This subdivision of

lithofacies Fm is defined by its weak consolidation, significant

porosity, and abundant root moulds and tubules (Klappa 1980)

emphasized by red oxidation zones. However, these features

may also be achieved by weathering and reworking of older

exhumed deposits. The lithofacies Fm (Fig. 3D) represents

compacted overbank deposit which gained its massive struc-

ture shortly after sedimentation. It lost its biogenic porosity

and gained a typical monotonous bluish-grey colour in

oxygen- deficient conditions after burial. This lithofacies in

an outcrop often exhibits muddy clasts (Fig. 3D) which are

known to be formed on weathered surfaces during repetitive

drying-wetting cycles (Wetzel & Einsele 1991). Rare rhizo-

liths are present in forms of carbonate rhizocretion horizons,

as well as root tubules and petrified root tissues preserved

within siderite concretions (Bojanowski et al. 2016). The pre-

sence of siderite concentrations and siderite cemented hori-

zons defines a sublithofacies Fmc (Fig. 3E) and is interpreted

as a result of anoxic diagenetic condition and bacterial

methanogenesis under a swamp.

The heterolithic sandstone-dominated lithofacies Hs com-

prises an association of sandstone, siltstone and claystone

layers. Grain size usually exhibits gradual change. In some

cases the cyclicity is poorly defined, but the regular Bouma

cycles (Tb–Te) may be present as well. The latter structure

predestines this lithofacies to be interpreted as a low-density

turbidity current deposit. However, in general this lithofacies

may occur in various settings where current flow is ephemeral.

Heterolithic siltstone-dominated deposits (lithofacies Hf,

Fig. 3F) show very subtle laminations and rare ripple cross-

beddings. The erosive capability of the environment must

have been very restricted, and the flow deposition alternated

with a long time of stagnant water settling. Hence, the distal

low-density turbidity current seems the most adequate inter-

pretation. Lithofacies Fl and CL represent mostly deposition

from suspension. Laminated siltstones (lithofacies Fl, Figs. 2,

3G) usually reveal well parting along bedding planes. This is

in contrast to typically massive claystones (CL) where bed-

ding is distinct only due to the admixture of plant detritus.

The organic matter content varies ranging gradually from grey

pure claystones (CL), through black coaly claystones (CCL)

to pure coals (C) (Fig. 3H). The rare freshwater limestone beds

(lithofacies L) usually accompany coal seams. The volcanic

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THE TECTONO-SEDIMENTARY AMS STUDY OF THE NEOGENE FROM THE ORAVA BASIN

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(OrFl)

Gmm

(OrGmm)

30 cm

Facial

code

Lithofacies

Description and interpretation

Interpretation

freshwater limestone

beds up to 30 cm thick; calcitic rock; well-preserved mollusc shells; white, yellow; [4]

authigenic calcite precipitation

tuffite

beds from a few millimetres to 2 m thick; pyroclastic silty and clayey deposit with

admixture of terrigenous fine clastic sediments; massive or laminated, rarely cross-

bedded; white, yellow; green when wet; [1] [2] [4]

ashfall deposition, may be altered by

current

coal

beds typically up to 40 cm thick; lignites from unlithified plant detritus to shiny and

brittle rock; brown to black; [2] [4]

phytogenic accumulation

CCL

coaly claystone

beds typically up to 20 cm thick; claystone abundant in organic matter; brown to

black; [4]

phytogenic accumulation with influx

of siliciclastic material

claystone

beds up to 50 cm; massive structure to weak lamination; subordinately plant detritus

admixture; dark grey, grey or grey-blue; [4]

suspension fallout deposition

laminated or massive

clayey siltstone

varied thicknesses; subtle laminations or massive structure with weak tendency to break

along bedding surfaces; grey to dark grey; [4]

suspension fallout, may be

current-driven

siltstone-dominated

heterolithic deposits

varied thicknesses; normally graded siltstones and claystones; laminated with subordinate

ripple cross-bedding; grey to dark grey; [4]

low-density turbidity currents or

ephemeral ripple bed transport

sandstone-dominated

heterolithic deposits

varied thicknesses; normally graded sandstones, siltstones and rare claystones; laminated

or ripple cross-bedded; occasionally Tb-e Bouma sequences; grey, dark grey or grey-

blue; [4]

low-density turbidity currents or

ephemeral ripple- and plane- bed

transport

massive clayey siltstone varied thicknesses (up to several meters); siltstone and clayey siltstone; predominantly

massive structure, very rare indistinct laminations; locally calcitic concretions; rare

muddy clasts (up to 15 cm) appearing at weathered surface; grey-blue or red; [4]

mud-suspension fallout, may be

current-driven; original structure

overprinted by bioturbation and/or

synsedimentary weathering

Fmc

massive clayey siltstone

with siderite concretions

lithofacies Fm with siderite concentrations, concretions and horizons; grey-blue or red;

[4] [5]

lithofacies Fm influenced by geo-

chemical processes related to soil or

swamp development

Fmm

massive clayey siltstone

and sandstone (mottled)

lithofacies Fm; often sandy; locally single pebbles; weakly consolidated; grey with

orange to red spots around pores of biogenic origin (rhizoliths, Fig. 3B and C)

lithofacies Fm at an initial stage of

diagenesis, altered by young biogenic

activity

massive sandstone

varied thicknesses; usually clayey and silty; fine- and medium- grained; grey or

grey-blue;

grain flow, rapid deposition

horizontally laminated

sandstone

fine- and medium- grained; often abundant plant detritus; rarely muddy intraclasts; grey,

red to brown; [4]

plane-bed flow

Sp, St

planar and trough

cross-bedded sandstone

beds up to 1 m; usually clayey and silty; fine- to coarse- grained; common plant detritus;

rare muddy intraclasts; grey, red to brown; [4]

2D and 3D bedforms (dunes)

horizontally bedded and

imbricated

conglomerates

up to 50 cm thick beds and lenses; indistinct horizontal bedding and imbrication, often

massive; predominantly composed of monomict clasts: sandstones, mudstones, sub-

ordinately limestones, quartzites, crystalline rocks and others; grey, red to brown; [3]

bedload sheets, lag deposits

Gcm

clast-supported

monomict conglomerate

several meters thick; massive; predominantly composed of monomict clasts: sandstones,

mudstones, subordinately limestones, quartzites, crystalline rocks and others; small

amount of sandy or muddy matrix; grey, red to brown; [3] [4]

low sediment concentration flow

Gmm

matrix-supported

breccia

several meters thick; breccia composed of monomict clasts: sandstones and mudstones,

subordinately limestones; sandy and muddy matrix; grey, grey-blue [4]

cohesive debris flow

Table 1: Lithofacies distinguished on the basis of their macroscopic features. Based on Miall (2006) classification, the results of this

study, and: Sikora & Wieser 1974 [1], Kołcon & Wagner 1991 [2], Tokarski et al. 2012 [3], Łoziński et al. 2015 [4] and Bojanowski et

al. 2016 [5].

Fig. 2. Fine clastic lithofacies: massive sandstones (Sm) and laminated siltstones (Fl) overlie with sedimentary contact disorganized breccia

(lithofacies Gmm) of inferred debris-flow origin (Oravica river, for detailed locations see Łoziński et al. 2016). AMS sample names are shown

in brackets.

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activity is recorded by tuffite layers and small intercalations

(lithofacies T), usually strongly chemically weathered.

Levels of structural deformation

In order to regard the various levels of deformation in the

AMS analysis, four levels of structural deformations have

been introduced based on field observations. The weakly con-

solidated category denotes soft deposits lying horizontally,

often mottled and porous due to young bioturbation, and

lacking any tectonic features. The consolidated category does

not have macroscopic pores, and is relatively better compacted

than the first one. These two types prevail in the central part of

the basin. Within the moderately deformed category, an irregu-

lar (or mostly one-directional) sets of joints, as well as normal

faults, have been observed (Tokarski & Zuchiewicz 1998;

Kukulak 1999; Łoziński et al. 2015). The moderately deformed

strata are tilted typically from 5 to 30° and are exposed pre-

dominantly along the southern and south-eastern margin of the

basin (from Nové Ústie to Stare Bystre village) and in the

north (near Lipnica Mała and Lipnica Wielka villages).

The strongly deformed category is used for deposits tilted

strongly (50–90°) and/or revealing ductile deformation. Such

a strong deformation has been observed or suggested by the

AMS results near the Nové Ústie and Bobrov villages, as well

as the Kovalinec, Červený, and Wojcieszacki streams.

Magnetic susceptibility carriers

According to the grain size analysis from the OH-1 borehole

(Pulec 1976), clay- and silt-sized particles usually dominate,

and sand grains are a minor admixture (typically 1÷15 %)

except for sandy intercalations. Sand grains are mainly com-

posed of quartz, pyrite, Fe-carbonates, limonite, apatite, chlo-

rite, garnet, calcite, and muscovite. Ferromagnetic minerals

are rare, but their content may be significant for magnetic

measurements (typically: magnetite 0÷2 % of sandy grains),

especially within Pliocene sediments (up to 7.5 % of sandy

grains have been noticed). Clay minerals comprising 25–55 %

of sediment mass are composed of beidellite, chlorite, illite

and locally subordinate kaolinite (Wiewióra & Wyrwicki

1980; Łoziński et al. 2016). Around 95 % of the specimens

measured in this study have a susceptibility of less than

500×10

-6

SI. Considering the above, paramagnetic minerals

(clay minerals) are expected to control the measured magnetic

susceptibility in most cases.

In order to examine magnetic minerals, 8 representative

specimens were chosen from 20 magnetically saturated speci-

mens, which represented various sedimentary environments

(Fig. 4A). The curve of the magnetic susceptibility vs. tempe-

rature (Fig. 4B; see Hrouda et al. 1997; Hrouda 2010) con-

firmed that the dominant component in low-susceptibility

specimen 1 was paramagnetic (78–88 % of susceptibility

inferred from hyperbola fitting), whereas high-susceptibility

specimens 3 and 21 were controlled by ferromagnetic compo-

nent. The results of magnetic saturation (Fig. 4A) showed that

the majority of specimens saturated rapidly in fields up to

0.3 T, except for specimens 1 and 6, which saturated in the

range of 1.5 to 2 T. The demagnetization curves obtained in

the Lowrie test (Fig. 5; Lowrie 1990) showed that the magneti-

zation values for these two specimens were dozens of times

lower, and blocking temperatures of both fractions (soft

THERMAL ANALYSIS

0.00

0.25

0.50

0.75

1.00

100

200

300

400

500

600

susceptibility

(K/K

)

temperature [°C]

SATURATION

0.00

0.25

0.50

0.75

1.00

0.0

0.5

1.0

1.5

2.0

2.5

3.0

peak field intensity [T]

IRM

(M/M

)

2,3,13,17,21,24

COOLING

HEATING

lake

0.4

lithofacies,

environment

NRM

[m A/m]

SIRM

[A/m]

0.1

lake

1.9

4.9

253

[x10 SI]

-6

324

11.1

floodplain

22.0

863

floodplain

0.4

0.2

424

river channel

10.3

22.1

410

floodplain

2.6

2.9

254

lake (fault zone)

45.2

22.1

646

ephemeral lake

8.8

12.0

448

Fmc

Fig. 4. Magnetic surveys of selected eight specimens from various depositional settings (table). A — The progressive acquisition of isothermal

remnant magnetization (IRM). B — Variation of bulk susceptibility during heating and cooling.

486

ŁOZIŃSKI, ZIÓŁKOWSKI and WYSOCKA

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575 °C and hard over 650 °C) were higher than for the others.

The remaining specimens (2, 3, 13, 17, 21, 24) were almost

completely demagnetized at a temperature of approx. 375 °C

(soft fraction) and around 320–375 °C (medium and hard frac-

tion). Complete demagnetization was reached at the tempera-

tures similar to those of specimens 1 and 6. All this indicates

a constant low content of magnetite in

all tested specimens. In specimens

1 and 6 magnetite is the essential

ferromagnetic mineral. In the other

specimens, where the saturation

magneti zation is relatively high, the

main ferromagnetic minerals s.l. are

greigite (see Babinszki et al. 2007;

Roberts et al. 2011; Reinholdsson et

al. 2013) and subordinately mono-

clinic pyrrhotite (see Dekkers 1988;

1989). Magnetic iron sulphides

appeared to exist in all investigated

environments, but their content

strongly varied. The presence of

greigite in high- susceptibility speci-

mens may be interpreted as either

an authi genic chemical precipitation

(possibly supported by microbial

activity) or mineralization by magne-

totactic bacteria. High-susceptibility

specimens were not found in this

study to stand out significantly in

terms of the anisotropy of suscepti-

bility, except for samples collected

within a strongly tectonically affected

zone. Regarding the above, the ferro-

magnetic component of susceptibility

was achieved presumably at the early-

diagenetic stage with no preferred

alignment of easy magnetization

axes.

AMS facies

According to the mineral content

discussed above, most specimens

have a susceptibility controlled by

paramagnetics, predominantly clay

minerals. This allows for interpreta-

tion of the AMS in terms of clay

particles alignment being a result

of sedimentation, compaction, and

tectonic reorientation. The standard

cylinder-shaped specimen having

above 10 cm

used in this study

reflects the total anisotropy of many

clay-, silt- and sand-sized grains, as

well as other components up to a few

millimetres wide, such as flora debris,

muddy clasts, lithoclasts, and small

concretions. It also summarizes the

variability of laminations and small

100

200

300

400

500

600

100

200

300

400

500

600

0.00

0.05

0.10

100

200

300

400

500

600

100

200

300

400

500

600

100

200

300

400

500

600

0.0

0.5

1.0

1.5

2.0

100

200

300

400

500

600

0.000

0.025

0.050

0.075

100

200

300

400

500

600

0.0

2.5

5.0

7.5

100

200

300

400

500

600 °C

A/m

LOWRIE TEST

HARD

MEDIUM

SOFT

Fig. 5. Thermal demagnetization of a three-component IRM [A/m] produced by magnetizing the

sample in 3.0 T along its z-axis (orange), followed by 0.4 T along the y-axis (grey), and finally

0.12 T along the x-axis (blue). For specimen details see Fig. 4A.

487

THE TECTONO-SEDIMENTARY AMS STUDY OF THE NEOGENE FROM THE ORAVA BASIN

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, 2017, 68, 5, 479–500

bioturbations. Sedimentary structures, and other sediment

variables having a size of several centimetres, may be charac-

terized by a set of AMS specimens, referred to as a sample in

this article and consis ting of up to 25 specimens (Fig. 1).

Using this approach Łoziński et al. (2016) have given the basis

for the definition of AMS facies with respect to lithofacies

type in the well-studied Oravica River section (Łoziński et al.

2015). The concept of AMS facies (also AMS fabrics) follows

the idea of the descriptive categorization of observations and

measurements, usually with some genetic interpretation, and

has already been used by other authors (e.g., Garcés et al.

1996; Ort et al. 2015). In this study, AMS facies is defined by

the distribution of anisotropy degree (P) and shape (T) para-

meters (Fig. 6). For the aniso tropy determined by a given clay

mineral composition, the anisotropy degree (P) parameter is

dependent on the clay content and consistency of particle

arrangement. The shape parameter (T) characterizes the type

of particle alignment: T>0 (oblate ellipsoid) denotes preferred

plane-parallel alignment (foliation), whereas T<0 (prolate

ellipsoid) axis-parallel alignment (lineation). For a statistical

description of specimen P and T values within a sample,

median values Pm and Tm (quantile 50 %) and range indi-

cators Pr and Tr (quantile 90 % – quantile 10 %) have been

used. The range of these four values within the studied sam-

ples are given in Table 2.

All 85 AMS samples have been grouped into AMS facies

(bracketed facies codes) with the focus on distinguishing pre-

viously defined lithofacies and levels of structural deforma-

tions (Fig. 7). The consolidated and moderately deformed

categories were combined since they appeared to be undistin-

guishable in AMS fabrics. The most common AMS facies

<Fm> which represents typical massive siltstones (lithofacies

Fm, subordinately Fmm, and Fmc) is characterized by low

anisotropies (Pm from 1.009 to 1.029) and a high shape range

(Tr from 0.40 to 1.43), usually manifested by the presence of

negative T values (prolate fabric) of individual specimens.

This poorly fits the generally accepted sedimentary AMS

fabric which is clearly anisotropic and oblate (e.g., Crimes &

Oldershaw 1967, Tarling & Hrouda 1993). This may be attri-

buted to the wide range of post-sedimentation processes

including sediment drying, wetting, and bioturbation, which

cause movement and reorientation of the sediment particles

and decrease the general anisotropy. The group of samples

with the smallest anisotropies (Pm ≤1.008) has been assigned

to a separate AMS facies <Fm-unc> representing deposits

un- or weakly- consolidated, often porous and subjected to

present-day surface processes (lithofacies Fmm and Fm).

The border between facies <Fm> and <Fm-unc> is arbitrary

and a range of intermediate fabrics are present. The lithofacies

Fm in the tectonically deformed zone of the Červený stream

appears to have reduced anisotropy shape value so that

negative T values predominate (Tm from −0.38 to −0.04,

<Fm-def>). The effect of a presumed horizontal compression

could have overcome the original oblate anisotropy resulting

in prolate fabric. Although the deformational factor is unques-

tionable, the AMS fabric of samples is not clearly triaxial

suggesting that a ductile deformation could have occurred.

The more distinct tectonic fabric is present within the tectonic

zone of the Wojcieszacki stream where k1 axes are well-

grouped and k2 and k3 are scattered. The lithofacies <Fm-rot>

denoting the rotated fabric (k3 rotated from normal to a bed-

ding plane position) has T values predominantly negative

(Tm = − 0.16) and slightly higher anisotropies than facies

<Fm-def>.

The AMS facies <S> represents a sand-dominated litho-

facies (mainly Sh, Sp, and St) having low oblate anisotropies

(Pm from 1.017 to 1.022). Compared to facies <Fm> it has

a rather narrow range of anisotropy shape values (Tr from 0.20

to 0.42) which may be attributed to the current-driven grain

sorting and sedimentation giving the well-clustered AMS

parameters. Additionally, the post-sedimentation processes,

altering the magnetic sedimentary fabric within floodplain

deposits (lithofacies Fm), could have been absent from river-

channel deposits. However, a range of intermediate settings

(e.g., crevasse splays and ephemeral channel deposits) is pos-

sible, so the AMS facies may be ambiguous as well. The other

lithofacies deposited from the current form a continuum of

AMS facies (<Hst>, <Hsl>, and <Fl>) having a clearly oblate

fabric and well-clustered AMS parameters. The heterolithic

lithofacies Hs may occur within various sedimentary settings,

thus it has revealed two different AMS fabrics. The AMS

facies <Hst> (terrestrial) has a wide range of anisotropy degree

(Pr from 0.023 to 0.040) which reflects the changes of the

depo sition mechanism. It could have occurred within the

settings of ephemeral currents, such as flood plains and

ephemeral channels. In contrast, the AMS facies <Hsl> (lacus-

trine) is characterized by a well-grouped anisotropy degree of

values (Pr from 0.011 to 0.014). In this case, the grain size and

depositional mechanism (interpreted as a low-density turbi-

dity current) do not change as much as for <Hst>. While the

sand-dominated heterolithic facies <Hsl> has Pm values from

1.024 to 1.032, the silt- and clay-dominated deposits of litho-

facies Hf, Fl, and CL represented by one AMS facies <Fl>

(lacustrine) have higher anisotropies with Pm ranging from

1.034 to 1.041. The well-clustered AMS parameters, and

clearly oblate anisotropy of <Hsl> and <Fl>, point to a stable

undisturbed deposition favoured in long-lasting lakes, and

thus provide a good environmental indicator. The contrasting

AMS facies <CLt> (terrestrial) displays a wide range of aniso-

tropies (Pr from 0.036 to 0.071), similar to that of facies

<Hst>. The high dispersion of anisotropies may be attributed

to the strong dependence of a short-lasting pond deposition to

environmental fluctuations manifested by the influx of silty

material (low anisotropy) and plant debris (high anisotropy).

In addition, oxygen-deficient conditions in swampy areas

could have favoured precipitation of magnetic minerals

(mainly iron sulphides) which contribute to higher magnetic

susceptibility of facies <CLt> and its anisotropy parameters.

The AMS facies <CCL> represents an organic matter-

abundant clayey lithofacies CCL, with the highest degree of

observed anisotropy (Pm up to 1.078). The tectonically

deformed AMS facies <CLt-def>, <Hsl-def>, <Fm-def> and

488

ŁOZIŃSKI, ZIÓŁKOWSKI and WYSOCKA

GEOLOGICA CARPATHICA

, 2017, 68, 5, 479–500

<Fm-rot> exhibit lower shape Tm values than their mode-

rately deformed equivalents <CLt>, <Hsl> and <Fm>.

The prolate shapes are common especially within <Fm-def>

and <Fm-rot>, so the tectonic overprint appears to be strongly

lithofacies-dependent.

Facies associations

The lithofacies associations and their succession supported

by AMS facies analysis lead to the definition of general facies

associations and allow for the interpretation of the

100 200 300 600 1000 2000

−1

1.00

1.04

1.08

1.12

n=189

100 200 300 600 1000 2000

−1

1.00

1.04

1.08

1.12

n=119

−1

1.00

1.04

1.08

1.12

100 200 300 600 1000 2000

n=25

100 200 300 600 1000 2000

−1

1.00

1.04

1.08

1.12

n=60

100 200 300 600 1000 2000

−1

1.00

1.04

1.08

1.12

n=25

100 200 300 600 1000 2000

−1

1.00

1.04

1.08

1.12

n=48

[x10 SI]

-6

−1

1.00

1.04

1.08

1.12

n=85

100 200 300 600 1000 2000

−1

1.00

1.04

1.08

1.12

n=128

100 200 300 6001000 2000

−1

1.00

1.04

1.08

1.12

n=700

100 200 300 600 1000 2000

−1

1.00

1.04

1.08

1.12

n=93

−1

1.00

1.04

1.08

1.12

n=106

100 200 300 600 1000 2000

−1

1.00

1.04

1.08

1.12

n=161

weakly consolidated

consolidated & moderately deformed

strongly deformed

<Fm-unc>

<CLt>

<CCL>

<S>

<Hst>

<Fm-def>

<Fm>

<Fm-rot>

<CLt-def>

<Hsl-def>

<Hsl>

<Fl>

swamp

river channel

lacustrine

(heterolithic)

floodplain

lacustrine

(heterolithic)

floodplain

ephemeral

lake

ephemeral

lake

floodplain/

river channel

floodplain

Fig. 6. The characteristics of AMS facies defined with respect to lithofacies type, inferred depositional environment and degree of deformation:

mean susceptibility histograms (Km) and plots of anisotropy shape (T) towards anisotropy degree (P). The name of each group designates

the lithofacies determining the AMS fabrics: CLt — claystone (terrestrial), CCL — coaly claystone, Fm - massive siltstone, Hst and

Hsl — heterolithic deposits (terrestrial and lacustrine), S — massive and horizontally/trough cross-bedded sandstones, Fl — laminated

siltstones and claystones. The degree of deformation other than consolidated & moderately deformed is denoted with: unc (weakly consoli-

dated, undeformed, very low anisotropies P), def (tectonically induced particle reorientation; reduced shape parameter T), and rot (strong

particle reorientation; partial rotation of k3 from bedding plane). Number of specimens are denoted with n.

489

THE TECTONO-SEDIMENTARY AMS STUDY OF THE NEOGENE FROM THE ORAVA BASIN

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lake

erosion of
basement

sedimentation

river

lithoclasts

sand, silt,
lithoclasts,
muddy intraclasts,
organic matter (bioturbation),
siderite concretions

silt,
clay aggregates

swamp

flood plain

lithofacies

Gmm

C, CCL, CL, L

Gh, Sh, Sp, St, Hs

Fm, Hs, Sh, Sm

Hs, Hf, Fl, CL

AMS facies

processes

debris-flow
plastic mass

movements

phytogenic

accumulation

suspension

fallout deposition

current deposition

suspension fallout and current

deposition

bioturbation
weathering due to drying, wetting,

and pelitoclast formation

low density turbidity currents

and suspension fallout
deposition

weak bioturbation

hillslope

sedimentary environment (Table 3, Fig. 8). Tuffites being

a separate facies (FA-I) have been noticed mostly near the

southern margin of the basin (Bystry stream — e.g., Sikora &

Wieser 1974; Czarny Dunajec river; Oravica river — Łoziński

et al. 2015) and locally in the northern margin (Lipnica Mała

village — Kołcon and Wagner 1991; and the Bobrov village

vicinity — Beleš 1974). The lacustrine facies association

(FA-II) is designated by mostly fine-grained laminated litho-

facies Hf and Fl. The AMS facies <Hsl> and <Fl> provide

a proper proxy in the case of indistinct sedimentary structures.

These deposits crop out in the southern part of the basin only

(Fig. 8) and represent stable lacustrine sedimentary conditions

AMS facies code

Lithofacies equivalent

Deformation

(median)

(range)

(median)

(range)

<Fm-unc>

Fm, Fmm, Fmc

weak

1.006÷1.008

0.003÷0.012

0.28 ÷ 0.68

0.38÷1.06

<Fm>

moderate

1.009÷1.029

0.004÷0.029

0.03 ÷0.81

0.40÷1.43

<Fm-def>

strong

1.006÷1.012

0.004÷0.010

-0.38 ÷ -0.04

0.45÷0.84

<Fm-rot>

k2-k3 rotation

1.022

0.017

-0.16

0.62

(low)

(high)

<S>

Sh, Sp, St, Hs, Fm (sandy)

weak, moderate

1.017 ÷ 1.022

0.007÷0.019

0.51 ÷ 0.86

0.20÷0.42

(low)

(high)

<Hst>

weak, moderate

1.023÷1.030

0.023÷0.040

0.64 ÷ 0.89

0.19÷0.29

(high)

<Hsl>

weak, moderate

1.024÷1.032

0.011÷0.014

0.70 ÷ 0.77

0.15÷0.31

<Hsl-def>

strong

1.031

0.016

0.56

0.41

(low)

<Fl>

Hf, Fl, CL

weak, moderate

1.034÷1.041

0.012÷0.017

0.61 ÷ 0.94

0.10÷0.29

<CLt>

CL, Fm (clayey)

weak, moderate

1.034÷1.067

0.036÷0.071

0.70 ÷ 0.91

0.24÷0.61

<CLt-def>

strong

1.032÷1.039

0.031÷0.033

0.48 ÷ 0.71

0.33÷0.78

(average)

(high)

<CCL>

CCL

weak, moderate

1.051÷1.078

0.029÷0.032

0.79 ÷ 0.83

0.17÷0.24

(high)

−

chaotic ellipsoid directions

Table 2: Statistical characteristics of the AMS facies: median and range values of anisotropy degree P and anisotropy shape T (see text for

explanations). Unique features of individual facies are marked in bold.

Fig. 7. Model of lateral diversification of sedimentary processes, lithofacies and AMS facies. Siliciclastic material derived from the eroded

basement reaches the terrestrial settings of the basin having the form of sand and silt grains, and lithoclasts, or is reworked as muddy intraclasts.

Muds on flood plains are subjected to synsedimentary weathering and bioturbation. Only fine, well-sorted grains and clay particles are brought

into the lake setting and settle from low-density currents and suspension fallout. The AMS facies support the environmental interpretation, and

especially help to distinguish between terrestrial and lacustrine settings (e.g., ambiguous lithofacies CL and Hs).

490

ŁOZIŃSKI, ZIÓŁKOWSKI and WYSOCKA

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over a long period. The swamp facies association (FA-III)

typically inferred from abundant organic matter (CCL, C)

associated with fine-grained deposits (CL, Fm) have a larger

extent than the latter. The areas of low clastic input, often

with stagnant water, favoured phytogenic accumulation and

organic matter preservation in oxygen-deficient conditions

(Bojanowski et al. 2016). The organic detritus content is

marked well by a high grade of magnetic anisotropy. Within

this facies association freshwater limestones may be found

(Łoziński et al. 2015), but they were encountered only in the

southernmost outcrops (Nové Ústie village, Oravica and

Jelešńa rivers). The associations mentioned above are spatially

exclusive with the weakly consolidated floodplain facies asso-

ciation (FA-IV). This one represents floodplain lithofacies

Fm and Fmm cropping out in rather flat areas of the basin.

The AMS usually reveals clearly horizontal sedimentary fabric.

Deposits often exhibit considerable porosity and are affected

by present-day bioturbation. Considering the above, this facies

association is presumed to be the youngest of the basin sedi-

mentary sequence and therefore determines the extent of the

greatest modern subsidence. The consolidated equivalent for

FA-IV is the floodplain facies association (FA-V), which is the

most common in the Orava Basin. The massive lithofacies Fm

and its low magnetic anisotropy suggest that the original struc-

ture has been lost due to synsedimentary weathering including

the wetting-drying process and bioturbation (Wetzel & Einsele

1991). The finest organic detritus have been almost totally

wiped out which points to well oxidizing conditions within

exposed mudflats. In contrast, the fluvial channel facies asso-

ciation (FA-VI) comprises distinctly bedded sandstones and

conglomerates. The AMS fabric is oblate with well-clustered

anisotropy parameters. Fluvial channel deposits are not very

common, but they appear throughout the whole basin.

The alluvial fan facies association (FA-VII) comprises large

VIII

III

V V

III

II V

VIII

III

VII

VIII

III

VII

III

VIII

III

VII

III

4 km

49.50°

49.45°

49.40°

49.35°

49.50°

49.45°

49.40°

49.35°

19.60°

19.90°

19.50°

19.60°

19.70°

19.80°

19.90°

19.50°

19.70°

19.80°

floodplain (weakly co

nsolidated

)

flo

odp

lain,

swa

mp, la

ke, tuffit

floo

dpla

in, s

wam

p, al

luvia

l fan

, tu

ffite

Facies associations

Dominant lithofacies

Minor lithofacies

Dominant AMS facies

Interpretation

FA-I

−

tuffites

FA-II

Hs, Hf, Fl, CL

long-lasting lake

FA-III

C, CCL, CL

Fm, L

swamp

FA-IV

Fm, Fmm

floodplain, weak consolidation or weathered

FA-V

Fmc, Hs, Sh, Sm

floodplain

FA-VI

Sh, Sp, St

Gh, Hs

sand-dominated fluvial channel

FA-VII

Gcm

Sh, Sp, St, Sm

−

gravel-dominated alluvial fan

FA-VIII

Gmm

hillslope deposits (colluvium)

Fig. 8. Facies map of the exposed Neogene infill of the Orava Basin. Floodplain and fluvial channel deposits are widespread throughout

the whole area of the basin while others are spatially restricted. The individually exposed parts of the basin are probably of a different age.

The areas with abundant swamp and lake deposits as well as tuffites are interpreted as the oldest part of the basin infilling. At that time

the basin could have spread further to the south (Skorušina foothills area). For facies association codes see Table 3.

Table 3: Facies associations and their interpretation.

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THE TECTONO-SEDIMENTARY AMS STUDY OF THE NEOGENE FROM THE ORAVA BASIN

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bodies of conglomerates. They are exposed only on the eastern

and northern margins of the basin, pointing to the location of

paleosources of clastic supply and probably the synsedimen-

tary tectonic activity. The lithofacies Gmm (FA-VIII) is inter-

preted as the slope debris-flow deposits with random AMS

ellipsoid directions (Łoziński et al. 2016). It appears only on

contact between the lowermost basin deposits and the older

basement (Czarny Dunajec River, Oravica River, Orava Lake

dam vicinity and Lipnica Wielka village), and probably corres-

ponds to the onset of sedimentation when the paleorelief of the

basin area had not been flattened yet.

Structural interpretation of AMS

The AMS fabric and ellipsoid axes direction constitute

an excellent tool for structural analysis, especially at the early

deformation stage (see discussion in Parés 2015). To ensure

that the acquired AMS directions have not been induced by

sampling forces (e.g., Copons et al. 1997; Shimono et al.

2014), different directions of hammering have been adopted

within one sample, usually covering the range of azimuths

60 ÷120° wide. The k1 axes directions normal to various direc-

tions of sampling have revealed the artificially-induced ellip-

soids (Fig. 9A and B) within samples Bo1, Chk1, JeQ3, Ku1,

and UhQ2. This points to their weak consolidation and the

lack of tectonic compression which should be much more

effective than the hammering force transferred by the sampler

walls’ friction. Four of these samples with horizontal and sub-

horizontal k1–k2 plane orientations (tilted up to 12°, Fig. 10)

presumably represent the youngest studied deposits located in

the northern part of the basin. The k1 and k2 axes are mixed

(Fig. 9D) or may be grouped indistinctly (Fig. 9C and E),

which corresponds to generally sedimentary fabric. Some

specimens do not pass the anisotropy tests (neither F12 nor

F23, at the 99 % probability level; Jelínek 1977). In the

extreme, 12 isotropic specimens (out of 25) within the sample

Krz1 (lithofacies Fm) have been excluded from direction ana-

lysis and the remaining specimens represent indistinct hori-

zontal bedding (Fig. 9C). The area of Lipnica Wielka and

Lipnica Mała villages near the northern basin margin stands

out for having a clearly triaxial AMS fabric and bedding tilted

above 15°. However, the most numerous tectonic features are

present in the southern part of the basin (Fig. 10). The AMS

ellipsoid axes are predominantly triaxial or indistinctly triaxial

(Fig. 9F and G), whereas sedimentary fabric is virtually

absent. The bedding is commonly tilted above 10° and can be

vertical within the zones affected tectonically. The Bobrov–

Jelešńa zone has been identified from the vertical k1–k2 plane

of AMS ellipsoids within sample Bv1 (Figs. 1 and 9H). Further

investigation has confirmed a strongly inclined bedding plane

(e.g., sample Bv3) with a strike of 102°. This direction trend is

accurately continued on the other side of the Orava Lake by

the valley of the Jelešńa River suggesting that the river may

follow a tectonic lineament. The zone is accompanied by

slightly inclined deposits (sample JO3 and JO6) with explicit

triaxial AMS fabric with k1 oriented 120° and suggesting

(together with samples Bv1 and Bv3) the NNE-trending

strongest compression. The strong deformation manifested by

joints, faults and a fold has been observed on the southern

shore of the Orava Lake, near the Nové Ústie village. The AMS

measurements have confirmed a variety of bedding orientation

from gently inclined (sample Us1 and Us3) to nearly vertical

(sample Us2), and k1 trending from 105° down to 70° (respec-

tively). A similar trend of k1 axis has been found for the

sample JO1 (k1 at 98°), from the eastern part of the Orava

Lake shore (Fig. 10). This area has been affected by mass

movements, which could have resulted in east-trending steeply

inclined bedding, measured conventionally and from the AMS

k1–k2 plane for sample JO2 (Fig. 9F). Samples JO4 and JO5

collected at the top of the landslide scarp are unaffected and

thus provide reliable k1 directions following the discussed

trend (128° and 106° respectively).

The claystones and siltstones (lithofacies CL and Fm) inter-

bedded with fractured coals cropping out in Kovalinec and the

Uhliská streams are gently tilted and locally faulted. The sam-

ple Ko2 has been interpreted as deformed claystone (AMS

facies <CLt-def>) due to the decreased shape parameter T

compared to undeformed claystones (Fig. 6) and a significant

dispersion of the AMS ellipsoid directions (Fig. 9I) unusual

for this lithofacies. Similarly, the sample Uh1 provides very

poor axes grouping making the k1 direction unreliable. They

have probably undergone a ductile deformation, which is addi-

tionally suggested by fluctuations of lamination observed on

weathered surfaces. The neighbouring sample UhQ2 has been

affected by sampling and is probably a younger, weakly

consolidated deposit.

The Oravica and Jelešńa sections located at the southern

border of the basin both represent moderately deformed

(faulted and fractured) deposits, usually with triaxial AMS

fabrics. The directions of k1 are trending at 85° in Oravica

(Łoziński et al. 2016) and 108° in Jelešńa (Fig. 9G) and seem

to follow the local direction of the exposed contact of the

Neogene with the older basement. The strongly deformed

zone of Červený stream located north of the Oravica and

Jelešńa sections has been identified from numerous faults and

vertical or steep bedding planes striking at azimuth of 60° and

confirmed by the AMS k1–k2 planes (samples Ce9 and Ce10,

Fig. 11A). Most outcrops represent massive lithofacies Fm, so

the AMS measurements of 11 samples have been done to trace

the extent and the character of this zone. It has turned out that

samples (JeQ2, Ce3, and Ce4) collected north of the vertically

bedded outcrop (and north of 60°-trending line following the

stream valley) are gently dipping in the same direction

(305/21÷24) and have W–E trending k1 axes. The samples

south of this outcrop are either unusually south-eastward tilted

25÷50° (Ce6 and Ce11) or represent the AMS fabric domi-

nated by prolate shapes (Ce7, Je11; Figs. 9J, 11C). The latter

may represent massive lithofacies Fm with originally very

weak oblate anisotropy, therefore easily undergoing deforma-

tion to become prolate. The ductile deformation observed in

claystones and siltstones (Fig. 11B) could have also affected

samples Ce7 and Je11 resulting in prolate shapes. Similarly to

492

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180

270

180

270

180

270

180

270

180

270

180

270

180

270

180

270

180

270

180

270

180

270

180

270

sampling

direction

sampling

directions

sampling-induced

axes

grouping

Bo1

<Fm-unc>

subhorizontal

sedimentary

fabric

CO1
<Fm>

Bo1

<Fm-unc>

poorly defined

horizontal

k1-k2 plane

and axes

grouping

Krz1

<Fm-unc>

poorly grouped

axes

JeQ4

<S>

indistinct triaxial

JO2

<Fm>

poorly grouped axes

of clearly oblate

fabric

Ko2

<CL-def>

triaxial

vertical bedding

Bv1

<Fl>

triaxial

Je9

<Fl>

nearly uniaxial (k1)

fabric

Ce7

<Fm-def>

k2 & k3 mixing

vertical bedding

Wo1

<Fm-rot>

chaotic axes directions

JeQ3

vertical direction

north

sampling-induced

axes

grouping

specimen

coordinates

geographic

coordinates

k1 (maximum)

k2 (intermediate)

k3 (minimum)

Principal axes of AMS ellipsoid for specimen and mean tensor (respectively):

Fig. 9. The lower hemisphere’s equal-area projection of the specimen AMS ellipsoid axes within individual samples. The effect of sample-

induced axes grouping may be verified by applying a multi-directional sampling. The projection in a specimen coordinate system (A) reveals

k1 clustering in a position normal to the direction of sampling (A and B). The variety of axes clustering depending on the deformation type and

primary anisotropy degree are presented in a geographic coordinate system in Figs. B–L (see text for explanations). The sample name and AMS

facies (in brackets) are given in the left upper corner of each plot.

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4 km

49.50°

49.45°

49.40°

49.35°

49.50°

49.45°

49.40°

49.35°

19.60°

19.70°

19.80°

19.90°

19.50°

19.60°

19.70°

19.80°

19.90°

19.50°

Červený zone

Bobrov-

Jelešń

a zone

Wojcieszacki

zone

Kovalinec zone

Nové Ústie

zone

triaxial

AMS axes and bedding

poorly grouped

indistinct triaxial

sedimentary

fabric

poor sedimentary

fabric or affected
by sampling

horizontal k1-k2 plane

indistinct horizontal k1-k2 plane

inclined k1-k2 plane

vertical k1-k2 plane

bedding plane

vertical bedding plane

zones of strong

deformation

areas moderately

deformed

compression

samples in the north of the tectonically affected area, the sam-

ples Ce6 and Ce11 have a W–E trending k1 axes giving the

N–S the main compression axis. This combined with the

general 60°-trend of the whole deformational zone indicates

a probable sinistral strike-slip fault zone.

The outcrops of the Czarny Dunajec river valley exhibit

moderately deformed to undeformed deposits slightly tilted

(up to 16°) towards the north and north-west. The k1 direc-

tions change from the parallel to the basin margin (sample

CD1), through W–E trending (samples CD2_1 and CD2_2)

towards ESE-trending (samples CD4, and CD5). The north-

(sample By2) and northwestward (By1 and By3) tilt and k1

axes oriented W–E have also been noted in the Bystry stream

section.

The extreme deformation has been observed in the neigh-

bouring Wojcieszacki stream. The observed vertical bedding

of the coal seam has been confirmed by predominantly verti-

cally oriented k1–k2 plane of the AMS ellipsoid (Fig. 9K)

within siltstones and claystones (lithofacies Fm and subordi-

nately CL). However, a few k3 directions are mixed with k2

directions creating a picture of transitional ellipsoid orienta-

tions towards the totally tectonic fabric, characterized by pro-

late shapes and axis k3 directed along the strongest compression

rather than normal to bedding plane (AMS facies <Fm-rot>).

The variety of AMS fabrics ends with samples OrGmm,

JeQ3, and LM2 (Fig. 9L), which have chaotic axis directions,

but maintaining the anisotropy shape and degree parameters

typical for their lithofacies. These have been interpreted as

deposits affected by ductile mass movements keeping the

original sediment structure at the scale of millimetres, but

moving and rotating fragments at the scale of several

centimetres.

Discussion

Lithofacies and tectonic deformations in AMS measurements

The AMS facial model presented in this paper is based on

the distribution of anisotropy degree and shape parameters

within a sample represented by four variables: Pm, Pr, Tm and

Tr. Traditionally, the prolate shapes (Tm<0) have been indica-

tive of grain orientation being either tectonic or current-driven

(e.g., Crimes & Oldershaw 1967). This study has confirmed

that deformations diminish the anisotropy shape parameter,

although the AMS fabrics vary strongly with respect to litho-

facies (Fig. 6). The lithofacies Fm appears to be most vulne-

rable to deformational overprint. Specimens from this

lithofacies may acquire partially prolate shapes due to sam-

pling forces and weak deformations (AMS facies <Fm-unc>

and <Fm>), while other lithofacies remain oblate even within

tectonic zones. This vulnerability may be attributed to low

original anisotropy gained presumably in a range of early

post-depositional processes experienced by exposed fresh

muds. This shows that the precise estimation of the degree of

deformation is ambiguous if the sedimentary factor is

unknown. However, it seems that some lithofacies may still be

identified using AMS parameters only (Fig. 6).

The directions of the AMS have been interpreted as tectonic

rather than sedimentary. Maximum and intermediate axes are

Fig. 10. The structural aspects of the mean AMS tensor axes orientation and their interpretation in terms of bedding and 2-dimensional

direction of the strongest compression.

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(Ce7)

CCL

(Ce9)

(Ce10)

bedding

150/50

bedding

150/90

fault 26/53

fault 285/75

fault 94/66

30 cm

4 cm

30 cm

either mixed (mostly in the northern part of the basin) or

represent a remarkably constant basinal trend (southern part of

the basin), unusual for a fluvial-dominated environment

characterized by fluctuating transport directions. This may be

due to clay minerals contributing significantly to the magnetic

anisotropy, which have probably been deposited as muddy

clasts not favouring the current’s direction. Also, the classical

interpretation of sedimentary grain imbrication (e.g., Rees

1961; Crimes & Oldershaw 1967; Hamilton 1967; Rees &

Woodall 1975) could not have been applied because it requires

comparison of magnetic foliation with a bedding plane that

was often undetermined or uncertain.

Considerable variations of the AMS parameters with respect

to lithofacies indicate the significance of lithofacies-oriented

sampling, a statistical approach and large datasets of measure-

ments. The measured AMS of a specimen quantifies the

alignment of sediment particles at a scale of millimetres

(specimen-scale), while the homogeneity of the sediment over

tens of centimetres (sample-scale) may be obtained from

a multispecimen representation of each lithofacies. These two

scales may be considered in terms of a time span needed to

deposit a given thickness of sediment. The specimen-scale

result represents a relatively short time of sedimentation and

characterizes a settling mechanism, mineral composition and

grain sorting. Accordingly, the sample-scale result shows the

stability of sedimentary conditions over a long time with the

exception for beds deposited quickly in one depositional event

(e.g., AMS facies <S>). In fine-grained deposits the homo-

geneity has been noticed within the AMS facies <Hsl> and

<Fl> being interpreted as deposits from lakes (lithofacies CL,

Fl, Hf, and Hs), where the sedimentary environment enables

long-term undisturbed sedimentation. It appears that all typi-

cally current-driven sediments (AMS facies <S> and <Hsl>)

show good clustering of P and T parameters (low Pr and Tr).

The stronger the current, the lower the anisotropy degree

(Pm), probably due to the lower content of anisotropic clay

minerals. This observation is contrary to deep-sea sediments

affected by bottom currents where a stronger current is thought

to align ferromagnetic grains more effectively (Ellwood &

Ledbetter 1977; Joseph et al. 1998). In contrast, inhomo-

geneous AMS facies <Hst>, <CLt>, and <CCL> indicate the

sedimentary conditions undergoing fluctuations or being

affected by special sedimentary events (e.g., floods). These

conditions are met within a river setting, especially within

ephemeral channels, local ponds, and overbanks where cre-

vasse splay is deposited (lithofacies Hs and CL). Swamp

depo sition may also be easily affected by water table change

or by siliciclastic influx during floods (lithofacies CL and

CCL). The AMS characteristics of a sample are found at this

point to be a useful tool in distinguishing between lacustrine

Fig. 11. Tectonic deformations within the Neogene fine clastics of the Orava Basin. AMS sample names are shown in brackets. A — Strongly

inclined to vertical position of claystones (lithofacies CL) and sandstone-dominated heterolithic deposits (lithofacies Hs) indicates a significant

deformation zone. Deposits are strongly compacted and faulted (Červený Stream). B — Ductile deformation resulted in irregular contact of

coaly claystones (lithofacies CCL) and clayey siltstones (lithofacies Fm) (Červený Stream). C — Massive siltstones (lithofacies Fm) exhibit

neither sedimentary, nor tectonic structures which have been inferred from the AMS measurements.

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and terrestrial settings of ambiguous lithofacies Hs and CL.

The separate group is represented by the AMS facies <Fm>

usually having low anisotropy (Pm) and low shape (Tm)

values. This has been attributed to post-depositional

weathering (drying, wetting, and bioturbation) presumably

destroying the original sedimentary structure (Wetzel &

Einsele 1991).

The evolution of the Orava Basin

The facial scheme for the Orava Basin shows the spatial dif-

ferentiation of facies associations (Fig. 8). Different sedimen-

tary conditions could have taken place in the north and south

during the basin’s development, but it can also be the case of

stronger erosion in the south uncovering the older part of the

sedimentary sequence. The conglomerate alluvial fan facies

(Gcm) is a good premise for the proximity of a highland hilly

area and thus it indicates the zones of basin paleomargins.

These facies have been noted at the northernmost part of the

basin near Lipnica Mała village and near the eastern margin,

especially building up of the large Domański Wierch cone

(Tokarski et al. 2012, 2016). The gravelly facies (except for

Gmm) are missing in the western part and primarily all along

the present-day southern basin margin (Fig. 8). On the other

hand, the lacustrine facies are found only in the southern basin

area and the transport direction measured in the Oravica River

section (Łoziński et al. 2015) being towards S and SW points

to a subsidence centre in the area of the present-day Skorušina

foothills. The uplift of Paleogene rocks in this area makes the

Orava Basin inversion in the south very probable, as has

already been suggested by other researchers (Nagy et al. 1996;

Tokarski et al. 2012; Łoziński et al. 2015). This is further sup-

ported by the contemporary hilly terrain morphology in the

area south of the line of the Bobrov–Chyżne–Chochołów

villages. The age of the southernmost deposits is weakly con-

strained, but it has been estimated to be Sarmatian in the vici-

nity of Nové Ústie (Nagy et al. 1996). The palynological

investigation of Neogene deposits (Oszast & Stuchlik 1977)

has shown a progressive climate shift from warm and humid to

temperate and dry, which can be associated with the termina-

tion of the Middle Miocene Climatic Optimum (Zachos et al.

2001) towards the cool climate in the Quaternary. Favourable

conditions for peat development could have existed in the

Middle Miocene, and may be linked with the abundant coal

seams in the southern part of the basin and in the lower part of

the basin filling (borehole Czarny Dunajec-IG1; Watycha

1971). This area of the basin is also characterized by locally

occurring siderite concretions related to swamps (Bojanowski

et al. 2016), freshwater limestones, and tuffite intercalations

probably related to the Sarmatian stage of volcanic activity in

the Western Carpathians (Vass et al. 1988). These lithologies

are absent in the northern part of the basin (Fig. 8) where the

upper part of the basin sequence crops out. The inversion

process also has regional implications. The Skorušina and

Gubałówka foothills were proposed by Watycha (1976a) as

a barrier which blocked material supply from the Tatra Mts in

the Neogene. However, the inferred lack of such a barrier in

the Sarmatian along with the absence of this material in the

basin suggests that the Tatra Mts might not have been exposed

enough yet although they were already uplifted (Śmigielski et

al. 2016).

The deformation inferred from the AMS measurements

provides a picture of a predominantly N to NE trending stron-

gest compression axis in the south part of the basin (Fig. 10).

The local deviations may be attributed to faulting and the

impact of basin marginal zones. The recorded stress may

depict the tectonic regime of either the basin opening or its

inversion, but the tectonic AMS fabric appearing predomi-

nantly within the uplifted southern area makes the second

hypothesis more probable. Moreover, Mattei et al. (1997) sug-

gested that the magnetic lineation (k1 direction) parallel to dip

direction of bedding (perpendicular to normal faults) is

characteristic for tilted bedding in an extensional regime,

while lineation perpendicular to dip direction denotes a shor-

tening in the folded strata. In the southern part of the Orava

Basin the magnetic lineation has a prevailing WNW–ESE

trend, which, compared with a similar trend of southern

basin-bounding faults (Pomianowski 2003, Fig. 12) and bed-

ding tilted northward, suggests that the inversion could have

taken place in a N to NE-trending compressional regime,

resulting in a gradual uplifting of the southernmost part of the

basin. In this sense, the present-day basin geometry may be

treated as an asymmetrical or half- graben (Pospíšil 1993 in

Gross et al. 1993b), which seems to be a common trend in

other intramontane basins, such as the Nowy Targ Basin

and Turiec Basin (Pomianowski 2003; Kováč et al. 2011).

The acqui red direction of compression is in accordance

with the NE- and NNE-trend inferred from fractured clasts

(Tokarski & Zuchiewicz 1998), although this direction could

have been rotated (Baumgart-Kotarba et al. 2004; Tokarski et

al. 2016). The uplift has been accommodated at the basin mar-

gins by dip-slip and strike-slip movements (Fig. 12) probably

along regional reactivated strike-slip fault zones (e.g., Myjava

Fault, also referred to as Orava Fault; Bac-Moszaszwili

1993; Baumgart-Kotarba et al. 2004). The intrabasinal fault

zones, Bobrov–Jelešńa and Červený (introduced previously as

topo lineaments, e.g. Łój et al. 2007), could have had a signi-

ficant dip-slip component together with a strike-slip move-

ment of a second-order with respect to regional faults.

The inferred extent of the basin inversion is limited in the

north approximately by the Chochołów–Chyżne–Bobrov–

Vavrečka line.

The Orava Basin represents an important element of the

Carpathian structural domain recording the neo-Alpine stage

of deformation. Its southern part has shown a considerable

tectonic contribution to the magnetic fabric, partly due to

weak compaction and cementation of sediments. In turn, the

rocks of the Skorušina foothills adjacent to the Orava Basin

have revealed sedimentary or weakly deformed AMS fabric

resulting from NW–SE shortening (Hrouda & Potfaj 1993).

Such a trend corresponds well with NE-trending magnetic

lineations within the neighbouring area of the Magura Unit

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representing relatively weakly deformed rocks and interpreted

as a tectonically passive element during folding and thrusting

(Hrouda et al. 2009; Márton et al. 2009). These results from

older units and the obtained N to NE trending compression in

the Orava Basin point to a major shift of the directions of

regional stress field during the Neogene. According to many

authors (e.g., Aleksandrowski 1985; Pešková et al. 2009) this

change could have taken place in the Early/Middle Miocene.

However, it was also suggested that the basin uplift, which

could have occurred after the tectonic regime change, has

continued since the Late Pliocene/Early Quaternary until the

present-day (Baumgart-Kotarba 1996; Nagy et al. 1996;

Tokarski et al. 2012). The direction of strongest compression

suggested in this paper is supported by the similar NNE-

trending contemporary thin-skin compressional regime resul-

ting from movement of the ALCAPA unit (Jarosiński 1998;

Zuchiewicz et al. 2002).

Conclusions

• A detailed scheme of 17 lithofacies representing predomi-

nantly fine-clastic deposits has been defined for the whole

area of the Orava Basin.

• Median and range values of anisotropy degree (P) and shape

(T) within individual sampled locations have been used to

distinguish 12 AMS facies with respect to the sedimentary

environment and deformation intensity. The magnetic

method proved to be very effective in analysing weakly

deformed fine-clastic terrestrial deposits often lacking

macroscopic sedimentary features.

• Mapping of the basin area using lithofacies and AMS

facies allowed us to mark the extent of the basin inversion.

The result supports the hypothesis of a significantly larger

basin extent in the south followed by an uplift and

a complete removal of deposits in the area of the present-day

Skorušina foothills.

• AMS measurements enabled us to identify two intrabasinal

fault zones: Bobrov–Jelešńa and Červený. The latter points

to the reactivation of faults related to the Pieniny Klippen

Belt in the basement after basin sedimentation.

• The structural framework for the inversion is comprised of

the regional NE-trending strike-slip fault zones together

with the secondary transverse faults (e.g., Bobrov–Jelešńa

and Červený) dividing the basin infilling into independently

uplifted blocks.

• AMS ellipsoid directions obtained from the uplifted southern

part of the basin show that the inversion has undergone

compression in the NNE-trending thin-skin presumably

related to the northward advance of the ALCAPA plate.

Acknowledgements: The study was financed by the National

Science Centre (NCN) grant no. 2011/01/B/ST10/07591.

The authors are pleased to offer special thanks to Prof. František

Hrouda, Dr. Alexander Nagy and Dr. Petr Pruner (reviewers),

Prof. Andreas Wetzel, Dr. Michal Šujan, Radosław Wasiluk and

Katarzyna Dudzisz who have greatly contributed to this research

with their advice, discussions, and archived data collection.

49.50°

49.45°

49.40°

49.35°

49.50°

49.45°

49.40°

19.50°

19.60°

19.70°

19.80°

19.90°

19.50°

19.60°

19.70°

19.80°

area

of basin

uplift

area

of subsidenc

(PKB in the basement)

Bobrov-Jele

šńa zone

Červený zone

4 km

regional fault zones

intrabasinal faults

areas of inferred basin uplift

Structural interpretation

depression-bounding faults

(gravimetric survey)

direction of compression

Fig. 12. Interpretation of the Orava Basin structural framework during its inversion. The basin is divided by strike-slip NE-trending fault zones

into independent blocks cut by secondary-order intrabasinal faults and deformation zones (observed). The southern central part of the basin

could have undergone an uplift in the NNE-trending compression regime. The arrangement of western and eastern marginal parts is determined

by strike-slip zones and the movement of surrounding structural blocks. Depression-bounding faults after Pomianowski (2003).

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Sample name

# of

spec.

GPS

N 49°

GPS

E 19°

Lithofacies
code

AMS facies

Bo1

.46883

.71867

CL/Fm

Fm-unc

Bv1

.41923

.56145

Fm/Fl/CL

Bv2

.42451

.57049

Fmm

Fm-unc

Bv3

.41946

.56247

CL/Fm

By1

.39662

.88565

By2

.39819

.88749

Fm/Sm

By3

.39758

.88610

CL/Sm

CD1

.37584

.81073

Fm,Sh

CD2_1

.37717

.81087

Fm,Sm

CD2_2

.37717

.81087

CL,Fm

Hst

CD3_1

.38307

.80904

CD3_2

.38307

.80904

Hst

CD3_3

.38307

.80904

Hst

CD4

.38675

.80839

CD5

.39218

.81226

Ce1

.38256

.72894

Fm,CL

Ce3

.38294

.73601

Fm,CL

Ce4

.38470

.74141

CL,Fm

Ce5

.38468

.74194

Fm-def

Ce6

.38216

.73372

Fm-def

Ce7

.38340

.73830

Fm-def

Ce8

.38521

.74612

Fm,CL

Hst

Ce9

.38280

.73607

Fl,Hs

Hsl-def

Ce10

.38280

.73607

CL/Fl

Ce11

.38387

.74011

Fm,Sm

Fm-def

Ch1d

.43898

.64153

Ch1g

.43898

.64153

Fmm

Ch2

.42245

.67547

Ch3

.42924

.65929

Fm/Sm

Ch4

.41773

.70163

Sm,CL

Fm-unc

Chk1

.44452

.67485

Fmm

Fm-unc

CO1

.45813

.65983

Fm/Sm

DW1

.41326

.88376

Fm,CCL

CCL

Je1

.36620

.75947

Je2

.36620

.75947

Je3

.36620

.75947

Hsl

Je4

.36659

.75791

CL/Fm

Je5

.40444

.67208

Je6

.38550

.72012

Fm/Sm

Je7

.38795

.71724

Fm/Sm

Je8

.39075

.71085

Je9

.36646

.75752

Je10

.37799

.73299

Fm/CL

Fm-def

Sample name

# of

spec.

GPS

N 49°

GPS

E 19°

Lithofacies
code

AMS facies

JeQ1

.38313

.72669

Fm/Sm

Fm-unc

JeQ2

.38292

.73191

Fm/CL

JeQ3

.41092

.64495

Fm/Sm

Fm-unc

JeQ4

.40800

.66499

Sm/Fmm

JO1

.39997

.59163

Fm/Fl

Hsl

JO2

.40173

.59268

Sm/Fm

JO3

.41771

.59506

Fmc

JO4

.40431

.59484

JO5

.40431

.59484

JO6

.41076

.59050

Hsl

Ko1

.37320

.62711

CLt-def

Ko2

.37324

.62712

CLt-def

Koz1

.45038

.56984

Fm-unc

Krz1

.45337

.60597

Fm-unc

Ku1

.45390

.67206

Fmm

Fm-unc

Li1

.46707

.64145

Li2

.47581

.63460

Fm/Sm

LM1

.48864

.65739

CCL,CL

CLt

LM2

.48842

.66577

Na1

.42027

.49771

Fm/CCL

OrCCL

.36638

.69957

CCL

OrCL

.36528

.70538

CLt

OrCL_1

.36558

.70529

OrCL2

.36638

.69957

CLt

OrFl

.36542

.70542

OrFl2

.36560

.69844

OrFm

.36638

.69957

OrFm_3

.36575

.69759

OrFm_4

.36591

.69973

OrGmm

.36515

.70531

Gmm

OrHf_2

.36583

.70545

OrHs

.36560

.69844

Hsl

OrHs_3

.36575

.69759

Hsl

OrHs_5

.36576

.69949

Hst

OrSt

.36639

.70533

Tv1

.37539

.75807

Uh1

.37240

.63042

CL,Fm

UhQ2

.37235

.63242

Fmm

Us1

.38334

.57671

CLt

Us2

.38351

.57823

Us3

.38434

.57971

CL,Fm

CLt-def

Wo1

.39956

.85846

Fm,CL

Fm-rot

Appendix

Dataset of all studied samples: