GeolCarp_Vol67_No4_347

GEOLOGICA CARPATHICA, AUGUST 2016, 67, 4, 347–370

doi: 10.1515/geoca-2016-0022

www.geologicacarpathica.com

Structure and tectonic evolution of the NE segment

of the Polish-Ukrainian Carpathians during the Late

Cenozoic: subsurface cross-sections and palinspastic models

JAN KU MIEREK

and URSZULA BARAN

Faculty of Geology, Geophysics and Environmental Protection, AGH University of Science and Technology; Al. Mickiewicza 30,

30-059 Kraków, Poland; kusm@geol.agh.edu.pl

Polish Oil and Gas Company S.A., Department of Petroleum Deposit Exploration; ul. Kasprzaka 25, 01-224 Warszawa, Poland;

urszulabaran15@gmail.com

(Manuscript received July 1, 2015; accepted in revised form June 7, 2016)

Abstract: The discrepant arrangement of the Carpathian nappes and syntectonic deposits of the Carpathian Foredeep
reveals the oroclinal migration of the subduction direction of the platform margin during the Late Cenozoic. Formation
of the nappes was induced by their detachment from disintegrated segments of the European Platform; the segments
were shortened as a result of their vertical rotation in zones of compressional sutures. It nds expression in local occur-
rence of the backward vergence of folding against the generally forward vergence toward the Carpathian Foredeep.
The precompressional con guration of sedimentation areas of particular nappes was reconstructed with application of
the palinspastic method, on the basis of the hitherto undervalued model which emphasizes the in uence of the subduc-
tion and differentiated morphology of the platform basement on the tectonic evolution of the fold and thrust belt.
Superposition of the palaeogeographic representations and the present geometry of the orogen allows understanding
of the impact of the magnitudes of tectonic displacements on the differentiation of the geological structure in the NE
segment of the Carpathians. The differentiation has inspired different views of Polish and Ukrainian geologists on
structural classi cation and evolution of the frontal thrusts.

Key words: fold and thrust belt, Outer Carpathians, platform cover, interference of subbasins, kinematics of tectonic
movements, Palaeogene, Miocene.

Introduction

The oroclinal arrangement of the Cretaceous–Tertiary
nappes, fringed by younger molasse of the foredeep, is
a dominant feature of the Outer Carpathians (Fig. 1). Their
northeastwards-protruding salient in the vicinity of the
Polish-Ukrainian border distinguishes itself by the north–
south trend of marginal thrusts of the Skole (Skyba)

and

Boryslav-Pokuttya nappes that are highly oblique to the
frontal thrust of the Early–Middle Miocene folded molasses
of the Stebnik (Sambir) Nappe. The bend, named the
Przemy l Sigmoid ( widerski 1952), connects the eastern
part of the Western Carpathians and the western part of the
Eastern Carpathians.

To the west of the Przemy l Sigmoid: (1) the Boryslav-

Pokuttya Nappe pinches out; (2) the thick series of folded
molasse of the Stebnik Nappe is dismembered into disconti-
nuous tectonic slivers at the base and front of the Skole
Nappe, which are correlated with the Stebnik Nappe (Ney
1968), and/or the separated younger (Late Badenian–Early
Sarmatian) Zg obice Unit (Kotlarczyk 1985; Po towicz
2004); (3) undeformed fragments of the posttectonic trans-
gressive cover of the Badenian–Early Sarmatian deposits are
preserved above folded and erosionally truncated outcrops of
the Skole, Subsilesian and Silesian nappes (of the so-called
Middle Group; Nowak 1927); (4) at the front, the folded

molasse — included in the Marginal Group of the Outer Car-
pathians by Polish geologists (Nowak 1927) — in some
zones rests (locally with a sedimentary gap) on flysch depo-
sits, folded with them and termed the “outer flysch”
(Ksi kiewicz 1972).

Tectonostratigraphic identification of the unconformable

occurrence of the Miocene sediments on older flysch
sequences and heterogeneous structural stages of the sub-Ter-
tiary basement is still an under-recognized problem of Outer
Carpathian evolution. It is worth noting that Ukrainian geolo-
gists assign the Sambir and Boryslav-Pokuttya nappes to the
internal folded zone of the Carpathian Foredeep and consider
these nappes to be detached platform covers accreted to the
Outer Carpathian orogenic front during the Early Miocene
(e.g., Gluško 1968).

In the extensive Carpathian bibliography, and against the

background of thorough studies revealing the regularities of
the geological structure and evolution of the Outer Carpathians
(e.g., Gluško 1968; widzi ski 1971; Ksi kiewicz 1972;
Vjalov et al 1981; Kotlarczyk 1988; Picha 2011), there are
remarkably different reconstructions of the pre-orogenic
geometry of the sedimentary subbasins (e.g., Unrug 1979;
Oszczypko & Toma 1985; Ku mierek 1988; Roure et al.
1993; Golonka et al. 2006; Nem ok et al. 2006; G ga a et al.
2012). They reflect different interpretations of the subsurface
structure of the Outer Carpathians and conceptual models for

* names used by Ukrainian geologists are given in parentheses

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the formation of the nappes, in particular their thrusting
directions and the reference lines of palinspastic projections,
which according to the classic assumptions (Kay 1945) have
implied insurmountable difficulties (Khain et al. 1977;
Kruglov et al. 1985).

In addition to providing a better understanding of the geo-

logical structure of the study area, optimization of those
representations is of fundamental importance for the genera-
tion of oil and gas reservoirs in the flysch sequences and gas
reservoirs in the foredeep molasse (Ku mierek et al. 1995,
2001; Picha 1996; Kolodij et al. 2004), discoveries of which
triggered advances in the study of the subsurface structure of
the frontal segment of the Outer Carpathians.

The new cross-sections, models and tectonostratigraphic

correlations illustrating the geological structure of the frontal
zone of the NE segment of the Outer Carpathians and of their
basement — developed by the authors of the presented paper
— are based on reinterpretation of extensive data sets. In par-
ticular, these include: the most recent seismic sections, well
sections and magnetotelluric soundings from the Polish Car-
pathians, as well as publications and geological maps from
the Ukrainian Carpathians (e.g., Shakin et al. 1976; Gluško
& Kruglov et al. 1986; Burov et al. 1986; Jankowski et al.
2004).

The geological cross-sections represent modified frag-

ments of regional traverses constructed by the authors in the
years 2007–2011, in cooperation with Ukrainian geologists,
in the framework of two interdisciplinary research projects.
These were oriented towards assessment of the possibility of
discovering new hydrocarbon reservoirs and utilization of
geothermal waters in the area of the Polish-Ukrainian Outer
Carpathians, between the Wis oka river valley in the Western
Carpathians and the Stryi river valley in the Eastern
Car pathians (Ku mierek et al. 2009; Ku mierek & Baran
2013). Some of those traverses (or their fragments) have
already been published (Ku mierek & Baran 2008; Czopek
et al. 2009; Ma kowski et al. 2009; Ku mierek 2010;

Górecki 2013).

New aspects of the interpretation of the structure in the

study area are provided by the tectonostratigraphic configu-
ration of the sedimentary successions of the Outer

Carpathians and the underlying Ma opolska Block, and by
the detailed cross-section and correlations (constructed on
the basis of compilation of published data and archival well
sections) illustrating the “interfingering” of the Miocene
cover of the flysch nappes with the foredeep deposits.

Other fundamental theses of the paper, which pertain to the

tectonic evolution of the NE segment of the Outer Car-
pathians (over 300 km in length), are based on: palinspastic
reconstructions of the pre-orogenic configuration of the ori-
ginal depositional areas of the nappes; and the tectonic dis-
placements of the nappes during the Oligocene–Middle Mio-
cene along seven traverses (not enclosed here) running from
the Dukla Nappe overthrust to the autochthonous deposits of
the platform slope.

On the basis of arguments presented in papers of one of the

authors (Ku mierek 1988), it was decided to accept a direc-
tion of the palinspastic projection which would be consistent
with the vergence of folds and thrusts. According to this
assumption, which implies the subduction of the original
basement of the sedimentary basins (towards S-SW) as a pro-
cess that triggered the development of the thrusting and
folding, a kinematic model of the Outer Carpathians evolu-
tion during the Late Cenozoic was constructed.

The new representation of the evolution of the NE segment

of the Outer Carpathians can be supported by interpretations
of the tectonics of the slope of the subducted European Plat-
form, which are based on seismic tomography and thermal
modelling (Kone n et al. 2002), and magnetotelluric sound-
ing (Ku mierek 2010).

Outline of the architecture of the NE segment

of the Carpathians

The fold and thrust belt

The nappes and tectonostratigraphic units of the Outer

Carpathians form a typical fold and thrust belt with a ver-
gence consistently toward the platform margin, except for
structural depressions where upright or hinterland-vergent
folds appear. The documented amplitudes of nappe

Fig. 1. Locations of cross-sections and well penetrations on a simpli ed geological map of the northeastern segment of the Outer Carpathians.
Nappes and allochthonous units (undivided): 1 — Magura; 2 — Dukla (and Porkulets); 3 — Stebnik (Sambir) and Zg obice.
Sedimentary complexes: 4 — upper Oligocene and lower Miocene (Krosno Beds of the Silesian, Subsilesian and Skole (Skyba) nappes;
Polyanytsya and Vorotyshche Beds within the Boryslav-Pokuttya Nappe); 5 — Menilite Beds (lower Oligocene); 6 — Cretaceous and
Eocene (older than the Menilite Beds); 7 — transgressive Miocene outliers on  ysch (a–with small areal extent).
Overthrusts of nappes and units: 8 — Magura;, 9 — Dukla; 10 — Silesian; 11 — Subsilesian; 12 — Skole (Skyba); 13 — Boryslav-
Pokuttya; 14 — Allochthonous Miocene; 15 — minor overthrusts; 16 — faults; 17 — lines of geological cross-sections (a–geological
interpretation based on seismic sections); 18 — lines of regional traverses; 19 — line of correlation (Fig. 7); 20 — line of the longitudinal
geological cross-section (Fig. 10B); 21 — wells along the cross-sections.
Inset A. Location of the study area within the Polish-Ukrainian Carpathians.
Tectonic units of the Polish and Ukrainian Carpathians: I — Carpathian Foredeep, external part (Bilche-Volytsya); II — Stebnik
(Sambir);  III — Boryslav-Pokuttya; IV — Skole (Skyba); V — Subsilesian; VI — Silesian (Krosno); VII — Chornohora; VIII — Dukla;
IX — Porkulets; X — Rakhiv; XI — Magura; XII — Maramuresh Crystalline Massif; XIII — sedimentary cover of the Maramuresh
Massif; XIV — Pieniny Klippen Belt; XV — Podhale Trough; XVI — Transcarpathian Depression; XVII — Tatra Mts.; the study area
marked by the box;
1A — boundary between the Western and Eastern Carpathians.

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overthrusts and the intensity of their folding justify the view
that they are detached from their original basement along the
basal clay-rich complexes of the Lower Cretaceous and
locally Eocene age. Locally, there is also disharmonic folding
above minor subhorizontal detachments.

In the Polish Outer Carpathians, three groups of nappes

can be distinguished (after Nowak 1927) from S to N: the
Magura Group, Middle Group and Marginal Group. In the
borderland between Poland and Ukraine, the Middle Group
is most extensively developed, reaching its greatest width in
the San and Ondava (in Slovakia) river basins.

The frontal zone of the orogen is characterized by a locally

very complicated geological structure. In general, the alloch-
thonous covers formed of flysch deposits of Cretaceous–
Palaeogene age (up to the Early Miocene in synclinoria)
and/or the Miocene molasse (of Early Miocene–Early Sar-
matian age) are thrust over younger or coeval terrestrial and
marine molasse. The autochthonous molasse transgressively
overlies the Meso-Palaeozoic and Precambrian structures of
the platform slope or the partly eroded nappes as the top
parautochthon, locally folded at the front of the orogen.

Tectonostratigraphic relationships between allochthonous

and parautochthonous covers and autochthonous formations
of the Carpathian Foredeep were discussed in numerous
papers and monographs written by Polish and Ukrainian
geologists, such as To wi ski (1956), Ney (1957, 1968),
Gluško (1968), Komorowska-B aszczy ska (1971),
Ksi kiewicz (1972), Samojluk (1976 b), Wdowiarz (1976),
Vjalov et al. (1981), Gluško et al. (1984), Kotlarczyk (1985,
1988), Po towicz (1991, 2004), Lizoon & Zayats (1997),
Oszczypko (2006), Ku mierek & Baran (2008), and Zayats
(2013), on the basis of results of field studies, interpretation
of well sections, and geophysical surveys.

The basement and foreland of the frontal zone of thrusts

The fold and thrust arc of the Outer Carpathians is overlap-

ping the slope of the platform basement. According to
Kone n et al. (2002), at the contact between the Western
and Eastern Carpathians, that slope was offset by an oblique,
SW–NE-trending deep-seated fracture which separated the
Ma opolska Block (Massif) from the basement of the Trans-
carpathian Depression. Within that depression, no deep well
drilled in the Ukrainian Carpathians reached the platform
basement under the Skole Nappe (Zayats 2013).

Within the Ma opolska Block, beneath the nappes, autoch-

thonous formations of different ages, representing the plat-
form basement, were encountered. In the study area, their
most complete section has been preserved between Pilzno
and Rzeszów (Fig. 2A), that is in the area of oblique submer-
gence of the Miechów Trough below the frontal zone of
thrusts which truncated older and older structural stages of
the basement. Its foundation is composed of weakly meta-
morphosed claystones and mudstones, which in the eastern
part of the Ma opolska Block are of Neoproterozoic (Edia-
caran)–Early Cambrian age (Po aryski et al. 1981).

In the western part of the Ma opolska Block, the eroded

top of the basement is overlain by Mesozoic–Palaeozoic for-
mations separated by numerous erosional hiatuses with dif-
ferent spatial and temporal extents. These formations are
disrupted by fault systems (Fig. 2A). In the eastern part of the
Block, long-lasting post-Laramian erosion (Palaeogene–
Early Miocene) over the Le ajsk Massif (Mizerski & Stupka
2005) removed the Mesozoic–Palaeozoic formations. As
a consequence, autochthonous Miocene sediments, over
which the Stebnik Nappe with erosional outliers of epiconti-
nental facies deposits is thrust, rest directly on the Precam-
brian–Lower Cambrian rocks (Fig. 2B).

Deposition of the Miocene molasse sediments took place

in a depression formed at the Carpathian front during Alpine
deformation. The middle Badenian evaporites occurring in
the lower part of the Miocene molasse section represent
a seismic marker that images the structure of the Carpathian
Foredeep, excepting zones of their absence (e.g., the
“Rzeszów Island”, Komorowska-B aszczy ska 1965). Dips
of those deposits generally range from a few to more than ten
degrees and are disturbed over compactional drape structures
of the basement (Krzywiec et al. 2005) or in the foremost part
of the frontal thrusts. In the area between S dziszów and
Rzeszów, in erosional palaeochannels, deposits composed of
the coarse-grained material from the basement occur; they
originated from formations of different ages, from the Pre-
cambrian up to the Upper Jurassic, and are covered with
silty-sandy terrestrial deposits to which Moryc (1995)
ascribed a Palaeogene age.

In comparison with the strongly deformed Proterozoic

rocks, with prevailing dips of 60–90°, the unconformably
overlying Palaeozoic and Mesozoic sequences are rather
low-dipping, with dips from a few to rarely over 20°. The
larger dips are generally in the lower clastic series and are
related to clastic series that drape the eroded basement.
Angular unconformities in the Mesozoic–Palaeozoic cover,
the variable extents and numerous sedimentary gaps com-
prising sometimes whole periods, imply that each series rep-
resents a different structural stage.

The tectonics of the Mesozoic–Palaeozoic structural stages

is dominated by systems of faults, including extensional
faults inverted during the Tertiary, which cut the open

folds (Cisek & Czernicki 1965; Jawor 1970, 1983; Jawor &
Baran 2004; Krzywiec 1997; Krzywiec et al. 2008; Baran &
Jawor 2009).

The morphology of the top of the Ma opolska Block foun-

dation has been most easily recognized in wells and seismic
surveys in the frontal zone of the fold and thrust belt where it
is shallowest. These data have documented the occurrence of
faults with throws reaching several kilometres, as well as the
reduced thicknesses of the autochthonous formations on the
platform slope; for example, they were absent in the Ba-1
well, drilled on an erosional basement high.

Beyond the depth of the drilled wells, important data are

supplied by the magnetotelluric sounding (MT) along several
regional profiles (Czerwi ski & Stefaniuk 2005). In the MT

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profiles, the Precambrian basement is identified as a high-re-
sistivity complex traced over a long depth interval. The top
basement horizon is shallowest (2.0–8.5 km) in the frontal
zone of the orogen and dips beneath the southern

(synclinorial) part of the Skole Nappe where it is offset by
SW- to vertical-dipping fault systems, with throws exceeding
1 km (Fig. 3). According to the geoelectric characteristics
(Stefaniuk & Ku mierek 1986; Stefaniuk 2003), these fault

Fig. 2. Lithostratigraphic scheme of the foreland and basement in the frontal zone of the fold and thrust belt: A — in the Western Carpathians;
B — in the Eastern Carpathians (in the transfrontier zone). 1 — claystone and siltstone, 2 — sandstone, 3 — limestone, 4 — dolomite,
5 — metaargillite and metaaleurolite, 6 — evaporites (salt, gypsum, anhydrite), 7 — erosional outliers of the epicontinental facies (olisto-
liths?), 8 — conglomerate (pebbly mudstone), 9 — stratigraphic discontinuities, 10 — tectonic extents, 11 — stratigraphic boundaries.
M

— middle Miocene: M

2(Ka-Sa)

–Karpatian–Sarmatian; Pg? — Palaeogene; Cr

— Upper Cretaceous: Cr

2(Sa)

–Santonian, Cr

2(Cn)

–Coniacian,

2(T)

–Turonian, Cr

2(C)

–Cenomanian; Cr

— Lower Cretaceous: Cr

1(Be-H)

–Beriasian–Hauterivian; J

3+2

— Middle and Upper Jurasic:

3(Km-T)

–Kimeridgian–Tithonian, J

3(O)

–Oxfordian, J

2(Bj?-Cl)

–Bajocian?–Callovian

;

T — Triassic: T

–Upper Triasic, T

–Middle Triasic,

– Lower Triasic, P?–T

–Permian?–Lower Triasic; C

— Lower Carboniferous: C

1(Wi-N1)

–Wisean–Lower Namurian, C

1(Wi)

–Wisean,

1(T)

–Tournisian; D — Devonian: D

3+2

–Upper and Middle Devonian, D

1(Em)

–Emsian; S — Silurian: S

(Lu1)

–Lower Ludlow, S

(W)

–Wenlock,

(La)

–Llandover; O — Ordovician: O

(Ll-K1)

–Llanvirn–Lower Caradoc, O

(Ar)

–Arenig; € — Cambrian; p€ — Precambrian (Ediacaran).

428.2 — ages ascribed to stratigraphic boundaries [m.y.]: for the Western Carpathians, after the Stratigraphic Table of Poland without the
Carpathian region (2008); for the Miocene (the Eastern Carpathians), after Steininger (1996).

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systems define the hinge of the flexural slope of the platform
basement.

Transverse, oblique-slip faults striking SW–NE (subordi-

nately S–N and SE–NW) and offsetting the pre-Alpine base-
ment, which were identified on the basis of interpretations of
geophysical survey results and remote-sensing analysis (e.g.,
Doktór et al. 1990; Ku mierek 1990), are reflected only indi-
rectly in the tectonics of the allochthonous nappes by changes
in strikes (Ku mierek & Baran 2008; Ku mierek 2010).
Nevertheless, they had an important influence on differentia-
tion of the thickness and structural style of the nappes.

molasse formations in the frontal thrust zones:

interpretative implications

Based on the contributions mentioned in Section “The fold

and thrust belt” and on descriptions and chronostratigraphic
correlations of geological processes contained in the publica-
tions of Gofstein (1964), Ji í ek (1979), Dolenko et al.
(1985), Kruglov et al. (1985), Petryczenko et al. (1994),
Garecka & Olszewska (1997), and Poprawa et al. (2004),
a model of the succession of the flysch and molasse deposits,
tied to the tectonic regime that controlled their development
(Fig. 3), was constructed in order to systematize the litho-
stratigraphic characteristics of formations distinguished in
the geological cross-sections. Chronostratigraphic correla-
tion of the deposits in the transfrontier zone of the Western
and Eastern Carpathians presented a considerable difficulty
in the light of rapid changes in thickness and lithology and
differences in dating, encountered in a number of Polish and
Ukrainian publications, such as Kotlarczyk (1988), Petry-
czenko et al. (1994), and Garecka & Olszewska (1997).

Graphical synthesis of the tectonostratigraphic sequences

in the NE front of the Outer Carpathians (Fig. 3) has revealed
several important relationships. Firstly, expansion of stratal
units toward the platform slope was associated with pinching
out of thick-bedded sandy series and interfingering of typical
deep-marine turbidites with: epiplatform near-shore deposits
during the late Palaeogene (so-called outer flysch in the

Western Outer Carpathians), with evaporitic deposits (in the
Eastern Outer Carpathians) locally with covers of near-shore
conglomerates composed of exotics during the late Miocene;
and then with marine deposits of the younger molasse.
Secondly, the direction of that expansion can be confirmed
by the increasing age of exotics (olistoliths, clasts) origina-
ting from erosion of older and older (toward NE) outcrops of
the platform slope, from Jurassic and Upper Cretaceous
rocks in sections of the Skole Series to the Palaeozoic quar-
tzites and Precambrian phyllites in the early Miocene con-
glomerates (Ney 1968; Vjalov et al. 1981; Kotlarczyk 1988).
Thirdly, intrabasinal synsedimentary uplifts triggered lateral
changes in the thickness and lithofacies of deposits, particu-
larly the extents of individual sedimentary successions, that
impacted the distribution of Tertiary nappes in the Eastern
Carpathians (e.g., Vjalov et al. 1981).

The diversified architecture of the eastern part of the Polish

Carpathians and the western part of the Ukrainian Carpa-
thians reflects the diachronism of the final phases of sedi-
mentation of the flysch and molasse deposits, tectonic defor-
mation, and the post-orogenic inversion of the orogen, in
general manifested by:
• in the western part, transgression of the younger molasse

onto folded and denudated (by subaerial, synkinematic?
erosion; widerski 1952; Ku mierek 1990) rocks of the
Skole Nappe before the Middle Miocene;

• in the eastern part, continuous sedimentation of the ysch–

molasse deposits (locally washed out), thrust and folded in
the nal stages of their deposition (the Middle–Late
Miocene).

Variation of the geological structure along the front

of the NE segment of the Carpathians

Interpretation of the subsurface structure along the
cross-sections

The locations of the transversal geologic cross-sections

with the best documented subsurface structure of the frontal
zone of the orogen in the eastern part of the Western

Fig. 3. Tectonostratigraphic scheme of sedimentary successions in the frontal zone of the fold and thrust belt. Tectonic regime: 1 — sub-
vertical tectonic movements in the basement of sedimentary subbasins, 2 — trend of expansion of Cretaceous–Tertiary sedimentary subba-
sins, 3 — main phases of Tertiary tectonic thrusts, 4 — expansion of continuous deformation, 5 — surfaces of sedimentary discontinuity,
6 — stages of  nal inversion of nappes. Sedimentary megacomplexes: 7 — early  ysch, 8 — clayey-marly Cenomanian–Coniacian depo-
sits (synrift formations?), 9 — turbiditic formations of Senonian–early Palaeocene, 10 — variegated clayey-marly deposits of late Palaeocene–
Eocene, 11 — older sequences of the Menilite-Krosno Series (Oligocene), 12 — a–younger sequences of the Menilite-Krosno Series,
b–Polyanytsya and Vorotyshche Beds, undivided (Eggenburgian–Ottnangian), 13 — Pre-Alpine basement (Precambrian–Meso-Palaeo zoic),
14 — epicontinental (near-shore) deposits of the Skole Series: a–Eocene, b–Oligocene–lower Miocene, 15 — Miocene molasse (undi-
vided): older–Stebnik Beds (Ottnangian–Karpatian, early Badenian?), b–younger (Badenian–early Sarmatian) – Balychi, Skawina
(– Przemy l), Bohorodchany, Tyras (Wieliczka), Chodenice and Grabowiec (Kosiv) Beds, 16 — intraformational conglomerates with frag-
ments of rocks from: a–basement, b– ysch, 17 — evaporites, 18 — erosion of deposits. Chronohorizons: mg — Globigerina (Sheshory)
Marls, wj — Jas o (Holovetsko) Limestones. Characteristic lithofacies: a — Ku mina Sandstones, b — Spas Sandstones, c — Siliceous
Marls, d — thick-bedded Inoceramian (–Stryi) Sandstones, e — Jamna Sandstones, f — Vyhoda Sandstones, g — Hieroglyphic Sandstones,
h — Boryslav Sandstones, i — Kliwa Sandstones, j — Menilite Sandstones, Cherts and Marls, k — Krosno Beds, l — Polyanytsya Beds,
m — evaporites, Vorotyshche Beds (Peri-Carpathian Salt-bearing Formation), n — Sloboda (Dubnik) Conglomerates, o — (younger)
Wieliczka evaporites (–Kalush evaporites, Tyras Beds), p — Dobromil (–Radych) Conglomerates.

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Carpathians (Fig. 4) and the western part of the Eastern Car-
pathians (Fig. 5) are presented in Fig. 1. Their traces were
chosen to make use of the recent seismic reflection lines shot
by Geofizyka — Kraków in the years 1991–2010 (sporadi-
cally, also older ones), running perpendicularly to structural
strikes, and to the locations of deep wells, which were pro-
jected into the planes of the cross-sections.

For construction of the cross-sections, the fundamental cri-

terion was to honour all the data in such a manner that the
interpreted geometry is consistent with surface outcrops,
seismically defined boundaries, well penetrations, and recog-
nized trends of changes in distinct sedimentary formations
(e.g., Ku mierek et al. 1991–1994; Ku mierek et al. 2009).
The considerable improvements in acquisition and proces-
sing of seismic profiles, expressed by their better resolution
and fidelity, was especially important for imaging the com-
plex geometry of overthrusts and nappes, thrust imbricates
and detachment folds which do not manifest themselves in
the near-surface zone (Ku mierek 2010).

In the Ukrainian Carpathians, interpretation of the subsur-

face structure in the northeastern fragment of cross-section VI
(Fig. 5B) has been based on tectonic maps of so-called hori-
zontal cuts at 3000, 5000 and 7000 m b.s.l. (Gluško &
Kruglov 1986), as a consequence of the unavailability of the
source documentation regarding the results of geophysical
surveys and deep wells (Ku mierek et al. 2009).

As illustrated by the enclosed cross-sections (Figs. 4 and

5), the tectonics of the allochthonous cover is most compli-
cated in zones with deeply buried basement, which are
characterized on magnetotelluric data by extreme resistivity
contrasts and their unconformable positions (Ku mierek
2010), which better synthesize the geometry of the resistivity
boundaries, without going into the detailed description con-
tained in the quoted paper. The cover is also characterized by
great changes in thickness of the Oligocene–Lower Miocene
successions (as a result of their syntectonic deposition), with
the tendency to pinch out on structural elevations of the fron-
tal zone of the Skole Nappe.

The thickness of the Skole Nappe decreases toward the

platform margin as a result of the depositional pinch-out of
the Lower Cretaceous sequences and pre-Badenian erosion
(Figs. 1 and 4A, B). The geometry of the sole thrusts (frontal
detachments) of the Skole Nappe and the Marginal Group
units is generally unaffected by the faulted basement geome-
tries (e.g., Wdowiarz 1976).

In the zone of shallow basement, the dips of thrusts are

generally subhorizontal but become slightly steeper over
depressions in the basement (Fig. 5), whereas further land-
ward, their shape becomes complicated within tectonic
sutures located in the foreland of the Silesian nappes as
a result of subsurface wedging of displaced tectonic blocks.

In the Western Carpathians, the anticlinorium of the Skole

Nappe is characterized by imbricate structures with roughly
E–W strikes (Fig. 1). These are thrust over tectonically
altered fragments of the allochthonous molasse of the Mar-
ginal Group (Fig. 4) and locally covered by outliers of the
transgressive younger parautochthonous Miocene molasse
(Fig. 1).

The changes in strikes of the marginal folds and thrusts of

the Skole Nappe in the Przemy l Sigmoid are accompanied
by an intense reorganization of the orogenic front. To the SE
of that zone, the tectonics of the Skole Nappe anticlinorium
is dominated by a system of more closely spaced imbricate
thrusts which separate structural elements of the “skyba”
type, that is with the asymmetric geometry accentuated by
pinchouts of the youngest flysch series, preserved only in
deep synclines (Fig. 5). Also the stratigraphic section of the
Boryslav-Pokuttya Nappe that pinches out laterally into the
Przemy l Sigmoid zone demonstrates the severe thickness
reduction of the flysch deposits (Fig. 5A) in relation to their
prolongation in the Ukrainian Carpathians (Fig. 5B), where
above the structural depression of the pre-Tertiary basement,
flat-lying disharmonic folds were formed.

Isolated erosional outliers of the epiplatform Palaeogene

facies, which are unconformably underlying (with a strati-
graphic gap) the Miocene molasse and were encountered by
several wells (e.g., in the Hu-1 deep well, Fig. 5A), presumably
determine the NE extent of the Palaeogene deposits in the
Skole succession (Ku mierek & Baran 2008). These deposits
have not been found at the bottom of the Stebnik (Sambir)
Nappe in the Ukrainian Carpathians (Fig. 5B) where the
thickness of folded molasse exceeds 5000 m, although their
occurrence cannot be excluded (Burov et al. 1969) at depths
exceeding the ranges of the wells drilled.

In order to elucidate the complicated tectonostratigraphic

relationships between the allochthonous/parautochthonous
cover and the autochthonous series of the Carpathian

Fig. 4. Geological cross-sections (I–IV) through the frontal zone of the Western Carpathians, eastern part. Allochthonous and parautoch-
thonous cover: 1 — parautochthonous molasse (Badenian – early Sarmatian) transgressively overlying folded ysch series,

2 — folded molasse of the Stebnik Nappe (Ottnangian–Karpatian, early Badenian?) and Zg obice Unit (Badenian–early Sarmatian), undi-
vided; Skole Series: 3 — deposits of the Menilite-Krosno Series (Oligocene–early Miocene), 4 — Hieroglyphic Beds and Variegated Shales
(late Palaeocene–Eocene), 5 — Inoceramian Beds (Senonian–early Palaeocene) and Siliceous Marls (Turonian), undivided, 6 — Cretaceous
deposits (Hauterivian–Turonian); Subsilesian Series: 7 — Variegated Shales and Marls (Senonian–Eocene),

8 — Lower Cretaceous (sub-Senonian) deposits; Silesian Series: 9 — Menilite-Krosno Series (Oligocene), 10 — Hieroglyphic Beds, Var-
iegated Shales and Ci kowice Sandstones (late Palaeocene–Eocene), 11 — Istebna Beds (Senonian–early Palaeocene), 12 — Lower Cre-
taceous (sub-Senonian) deposits, Lgota Beds, Ve ovice Beds and Cieszyn Beds. Autochthonous covers: 13 — Badenian – Sarmatian
molasse (undivided), 14 — Mesozoic (undivided), 15 — Meso-Palaeozoic (undivided), 16 — Palaeozoic (undivided), 17 — Precambrian
(Riphean–Vendian, Early Cambrian?). Graphical symbols: 18 — stratigraphic unconformities, 19 — nappe overthrusts,

20 — lower-order thrusts and other faults, 21 — wells: a–in the cross-section plane, b–projected onto the cross-section.

356

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, 2016, 67, 4, 347–370

Foredeep, the authors constructed three selected cross-sec-
tions through the front of the Carpathian overthrust at larger
scales (Fig. 6A, B and C), as well as their detailed correlation
between well penetrations (Fig. 7).

Cross-section A (Fig. 6), located to the west of the Wis oka

river valley (Fig. 1), illustrates the occurrence of the Upper

Badenian deposits in three structural positions (from south to
the north) as:
• the top parautochthon that is overlying (with a strati graphic

gap) the Cenomanian–Palaeocene deposits of the Skole
Series but concordantly folded (?) and thrust together with
them (the G-1 well);

Fig. 5. Subsurface geological cross-sections (V–VI) through the frontal zone of the Eastern Carpathians, western part. Allochthonous and
parautochthonous cover: 1 — parautochthonous molasse ( Radych and Dobromil Conglomerates; late Badenian–early Sarmatian) trans-
gressively overlying folded deposits of the Stebnik and Skyba nappes. Folded molasse of the Stebnik (Sambir) Nappe: 2 — M

–older

(Ottnangian?–Karpatian) Stebnik Beds (M

); 3 — M

–younger (Badenian–lower Sarmatian) Balychi Beds (M

) and Bohorodchany and

Tyras Beds (M

b+t

); 4 — erosional outliers of ysch subfacies of the Skole Series (Palaeogene). Boryslav-Pokuttya Nappe: 5 — Menilite

and Polyanytsya Beds, undivided (Ol–M

), 6 — Vorotysche Beds (Eggenburgian). For remaining explanations see Fig. 4.

Fig. 6. Detailed cross-sections (A, B and C) through the outermost parts of the frontal thrusts. A —  ki Górne–Pogórska Wola (after Jedno-
rowska & Moryc 1967, slightly modi ed);  B — Zalesie–Pobitno (tectonics of  ysch series after Ney 1968, of Miocene molasse after
Komorowska-B aszczy ska (1971), with adaptation); C — Przemy l–Jaksmanice (from Fig. 5A, with more details).
ad A/ Skole Nappe: 1 —  ysch deposits: Variegated Shales (Cenomanian) K

, Siliceous Marls (Turonian) K

, Inoceramian Beds (Seno-

nian–Palaeocene) K

-P

1-2

; parautochthon: 2 — upper Badenian–lower Sarmatian; folded Miocene: 3 — lower Badenian, 4 — evaporites,

5 — upper Badenian–lower Sarmatian; autochthon: 6 — Upper Cretaceous marls and limestones, 7 — lower Badenian, 8 — upper Bade-
nian–lower Sarmatian; 9 — stratigraphic unconformities, 10 — overthrust of the Skole Nappe, 11 — overthrust of folded molasse,
12 — faults, 13 — well penetrations with measured dips of strata.
ad B/ Skole Nappe: 1 — ysch deposits: Spas Shales (Early Cretaceous) K

, Inoceramian Beds (Senonian–Palaeocene) K

-P

1-2

, Hierogly-

phic Beds and Variegated Shales (late Palaeocene–Eocene) P

-E, Menilite-Krosno Series (Oligocene) Ol; parautochthon: 2 — Badenian–

lower Sarmatian; folded Miocene: 3 — upper Badenian, 4 — lower Sarmatian; autochthon: 5 — Precambrian, 6 — Devonian,
7 — Carboniferous, 8 — upper Badenian, 9 — lower Sarmatian. For the remaining symbols, see Fig. A.
ad C/ Stebnik Nappe: 1 — erosional outliers of ysch subfacies of the Skole Series; folded molasse: 2 — Stebnik Beds M

, 3 — Balychi

Beds M

;

— upper Badenian–lower Sarmatian M

2-3

; post-tectonic cover (parautochthon): 5 — Przemy l (Skawina)

Beds M

2-3

, 6 — Radych Conglomerates M

; autochthon: 7 — Precambrian Pcm, 8 — undivided Miocene molasse (M

aut

); 9 — overthrust

of the Stebnik Nappe, 10 — overthrust of the Zg obice Unit, 11 — thrust slices and faults. For the remaining symbols, see Fig. A.

358

KU MIEREK and BARAN

GEOLOGICA CARPATHICA

, 2016, 67, 4, 347–370

• a parautochthonous Miocene fold (at the front of the Skole

Nappe overthrust), thrust over the autochthonous deposits
of the Carpathian Foredeep (the PW-3 well) with the thrust
amplitude on the order of 1 km;

• the subhorizontal autochthon, somewhat tectonically dis-

turbed at depth (the PW-5 well), with basal lower Badenian
deposits overlying (with a stratigraphic gap) the Upper
Cretaceous marls (the G-1 well).
Krzywiec et al. (2014) presented an alternative interpreta-

tion of the geological structure of the thrust front in the
Pogórska Wola area (Fig. 1, cross section A), based on inter-
pretation of a seismic 3D survey. In the southern segment of
the seismic time section (fig. 10 in Krzywiec et al. 2014) —
with the course similar to that of the cross section from our
Fig. 6A — the quoted authors plotted (with a question mark)
a backthrust that suggested a tectonic character of the uncon-
formable position of the Miocene sediments on the Skole
Nappe. Such interpretation conflicts with profiles of the early
Badenian known from numerous wells (e.g., Po towicz
1993), at the base of which there are sandstones and con-
glomerates with fragments of flysch rocks and sedimentary
breccia of these rocks (Rajchel 1988), which indicate a trans-
gressive origin of this surface. It is generally gently sloping,
except for frontal thrusts where it was folded together with
the Skole Nappe (Fig. 6A) during deposition of the Miocene
synorogenic sediments.

Cross-section B (Fig. 6) is located in the eastern part of

so-called Rzeszów Embayment (Fig. 1). The embayment is
built up of the thickest preserved transgressive Miocene

cover, with thicknesses exceeding 1000 m in the Mo-1 well
(Wdowiarz 1976). In cross-section B, the upper and lower
Badenian subhorizontal strata are unconformably overlying
the tightly folded flysch series of the Skole Nappe (of Early
Cretaceous–Oligocene age). In reality, the Badenian deposits
that “drape” the flysch formations (the Po-2 and Po-1 wells)
in the frontal zone were folded together with the transgres-
sional surface during sedimentation of the lower Sarmatian
deposits (the Po-5 well), resulting in overturned Miocene/
flysch fold thrust onto the lower Sarmatian–upper Badenian
autochthonous deposits which in turn unconformably overlie
Devonian rocks (the Po-2 well).

Cross-section C (Fig. 6), located on the eastern side of the

Przemy l Sigmoid, represents the style of the geological
structure of the Eastern Carpathians (Fig. 1A). This cross-
section is an enlarged fragment of section V (Fig. 5A) and
illustrates the geological interpretation of the northern part of
the seismic section 2-13-94 K (originally scaled to 1:50,000),
adapted from Ku mierek & Baran (2008). The visualization
aims at presenting the “internal structure” of the Stebnik
Nappe and its relation to the overthrust nappes, the tectonics
of the Carpathian Foredeep, and the structural situation of
so-called “deep-seated flysch elements” (Ney 1968) that in
fact represent erosional outliers of flysch deposits in the
epiplatform facies (after Ku mierek & Baran 2008) which
rest at the base of the Stebnik molasse. Those outliers,
encountered by the Ja-10, Ja-25 and Hu-1 wells (in the
cross-section plane), are bounded by a surface of the Early
Miocene erosion. In the seismic image, they are expressed

Fig. 7. Correlation of “ ysch elements” in sections of the allochthonous Miocene in the frontal zone of the Polish Carpathians (eastern part).
Allochthon of the Skole and Boryslav-Pokuttya nappes: 1 — Inoceramian Beds (Late Cretaceous–Palaeocene);
subfacies of the Skole Series: 2 — Polyanytsya Beds (early Miocene), 3 — Menilite Beds (Oligocene), 4 — Variegated Shales (Eocene),
5 — Inoceramian Beds (Late Cretaceous–Palaeocene); allochthonous and posttectonic Miocene: 6 — Zg obice cover (late Badenian–
early Sarmatian), 7 — Stebnik cover (Ottnangian–Karpatian); autochthon: 8 — Precambrian, 9 — Devonian, 10 — Miocene (Badenian–
early Sarmatian); 11 — transverse zones of deep-seated faults (J–R, –P), 12 — overthrust of the Skole Nappe, 13 — overthrust of the
Boryslav-Pokuttya Nappe, 14 — overthrust of the Stebnik Nappe, 15 — overthrust of the Zg obice Unit, 16 — stratigraphic unconformities,
17 — symbols of well penetrations.

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GEOLOGICA CARPATHICA

, 2016, 67, 4, 347–370

by: decline of the reflector continuity; angular discordance;
and different dynamics of their record in relation to the over-
lying molasses.

The flysch elements within the allochthonous Miocene

cover were penetrated in different structural positions,

delineated by stratigraphic discontinuities or overthrusts
(Fig. 7), in the following forms:
• in the western zone, as eroded folds of the front of the

Skole Nappe overlain by the transgressive cover of the
Badenian–lower Sarmatian deposits and sometimes thrust
over folded deposits of that same cover (see 6B, Po-1
well), which is distinguished as the allochthonous Zg obice
Unit (Kotlarczyk 1988, Po towicz 2004);

• in the central part, as erosional outliers of the Cretaceous–

Palaeocene, unconformably overlain by deposits of the
lower Miocene (Eggenburgian?, Ottnangian–lower Bade-
nian), distinguished as the allochthonous Stebnik Nappe
(Unit) (Kotlarczyk 1988, Po towicz 2004), and locally
underlain by folded outliers of the Zg obice Unit (in the
Al-6 and Prz-117 wells);

• in the eastern part (the Eastern Carpathians), as the

youn gest sequence of ysch deposits (Eocene–lower Mio-
cene) at the bottom of the overthrust Upper Cretaceous de-
posits belonging to the Boryslav-Pokuttya Nappe

(the Prz-10 well?), and as erosional outliers uncon formably
overlain by the Stebnik molasse, thrust together with them
over the autochthonous deposits of the Carpathian Fore-
deep (the Prz-4 and Ja-10 wells) (Ku mierek &

Baran 2008).

The palinspastic image of the tectonic evolution

Reconstruction criteria for the palinspastic framework

The image of the precompressional configuration of the

subbasins in the NE segment of the Outer Carpathians during
the Late Tertiary was obtained through palinspastic projec-
tion of the following folded and thrust surfaces of:
• the base of the Menilite-Krosno Series (Oligocene) in

cross-sections of the Silesian, Subsilesian, Skole and
Boryslav-Pokuttya nappes, which is correlated with the
stratigraphic horizon of the Globigerina Marls (Sheshory
Marls), approximately 34 Ma BP;

• the base of the Balychi Beds in cross-sections through

the Stebnik Nappe, approximately 16 Ma BP (after Garec-
ka & Olszewska 1997), assuming that it determines the
boun

dary between the Early and Middle Miocene

(Gradstein et al. 2004), although in older papers those
beds were dated as Karpatian (Ney 1968; Petryczenko et
al. 1994).
The authors assumed the relative reference line for the pal-

inspastic projection to be the trace that connects the points of
intersection of the base of the Oligocene deposits with the
Dukla Overthrust surface, which were marked in 7 regional

cross-sections (traverses I, III-VIII, Fig. 1), not included in
this paper. They were chosen from a larger set of traverses,
constructed by the authors and originally scaled to 1:50,000
or 1:100,000 (Ku mierek et al. 2009; Górecki 2013) in such
a way that their traces are perpendicular to fold strikes and
evenly distributed in the reconstructed part of the Outer
Carpathians (Fig. 1). Some of the segments (NE) are coinci-
dent with traces of the geological cross-sections (Fig. 4A, C, D
and Fig. 5A) and the generalized structural models of the tra-
verses IV and V were previously published (Ku mierek
2010, figs. 7 and 8).

The cross-sections that illustrate the subsurface geological

structure of the Ukrainian Carpathians along traverses VI
(the NE part), VII and VIII (Ku mierek et al. 2009) were con-
structed on the basis of geological maps (Shakin et al. 1976;
Gluško & Kruglov et al. 1986; Burov et al. 1986; Jankowski
et al. 2004; Kuzovienko et al. 2004) and publications (Danysh
1973; Gluško et al. 1984; Kolodij et al. 2004).

In order to reconstruct the configurations of the subbasins

(Figs. 8 and 9), the lengths of stratigraphic boundaries were
measured with an opisometer (in the cross-sections), ascri-
bing them to particular nappes (tectonofacies units). The
lengths of the straightened lines in directions consistent with
their general vergence determined the original widths of
sedi mentation zones of particular nappes in the traces of the
traverses.

Potential inaccuracies in constructing the palinspastic

framework of the subbasins may arise from:
• neglecting the in uence of the varied bathymetry (subsi-

dence of the bottom) on the reduction of widths of sedi-
mentation zones;

• assuming (a priori) that the age of structural offsets

(thrusts, imbrications of folds, faults) was younger than the
time of: (a) deposition of the guiding lithostratigraphic
boundaries; and (b) formation of the subsurface line of the
Dukla Thrust intersection with the basal surface of the Oli-
gocene strata.
The second of these may include a potential error (on the

order of several hundred metres to a few kilometres) in the
eastern part of the Dukla Thrust, where synsedimentary tec-
tonic movements in the foreland occurred as early as the
early Oligocene (e.g., Ku mierek & Baran 2013), possibly
involving also the Dukla Nappe after the deposition of the
Globigerina Marls (Fig. 3). The time of the initial shortening
of the Krosno lithofacies deposits in the sedimentation zone
of the Silesian nappes as early as the early Oligocene has
been suggested by results of balancing cross-sections
(Ku mierek 2010, fig. 6A). It can also be confirmed by data
from the literature, which were compiled by Nem ok et al.
(2006, table 1).

Selection of the subsurface edge of the Dukla Thrust as the

relative reference line for the palinspastic projection —
taking account of its coincidence with the line of zero values
of the Wiese vector — enables indirect tying of the Outer
Carpathian cover to the potential zone of their collision with
the Inner Carpathian zones (Figs. 8 and 9).

362

KU MIEREK and BARAN

GEOLOGICA CARPATHICA

, 2016, 67, 4, 347–370

• in the Western Carpathians, 35.8–49.6 km
for the sedimentary cover and 54.6–78.1 km
for the consolidated basement;
• in the Eastern Carpathians, 55.3–74.2 km
and 68.9–92.1 km, respectively.

The above ranges of values suggest dis-

memberment of the subducted platform
slope into lithosphere blocks with variable
directions and magnitude of displacement.

Interference of the allochthonous and
parautochthonous covers in the Outer

Figure 9 is a palinspastic model of the tec-

tonic evolution from the middle Miocene to
Quaternary. It shows the extent of sedimen-
tation zones of the allochthonous and
parauto chthonous Miocene molasse and the
locations of frontal thrusts of the Skole and
Boryslav-Pokuttya nappes at the end of the
early Miocene, preceding the final inversion
of the orogen (Fig. 3). During this interval,
differences between the Western and Eastern
Carpathians became marked.

The strikes of subbasins of the Marginal

Group in the Eastern Carpathians follow the
system of NW–SE oriented deep-seated
faults that affect the SW slope of the East
European Platform (Samojluk 1976a),
namely the Tornquist-Teisseyre Zone (Picha
2011). Oblique interference of the T-T zone
with the deep-seated fractures of the West
European Platform manifests itself by mini-
mum values of the gravity field (Zayats
2013) in the NE segment of the Outer
Carpathians.

The differentiation of subbasin configura-

tions between the Eastern and Western Car-
pathians during the Middle Miocene is mani-
fested in their structural position and the
width and magnitude of subhorizontal dis-
placements of the sedimentary cover and its
basement (Fig. 9). The difference of extreme
values of tectonic displacement of the sedi-
mentary cover exceeding 25 km (e.g., in the
traverses III and VII, Fig. 9) supports the
thesis that the folding and thrusting were
diachronous along the front of the orogen
toward the SE (Ji í ek 1979), which means
that in the eastern traverses (VII and VIII,
Fig. 1) the final stage could have ended over
2 Ma later. The undeformed transgressive
Badenian molasse on the folded nappes of
the Middle Group in the Western Carpathians
shows that the final phase of contraction in

Table 1: Measured parameters of the magnitude of subhorizontal tectonic displace-
ments of the allochthonous cover and its consolidated basement (CB) in regional geo-
logical traverses through the NE Outer Carpathians in the Late Tertiary

Number of traverse

NAPPES

AND STRUCTURAL

– F

CIES UNITS OF

THE OUTER CARP

HIANS

Silesian Nappe

(Krosno zone)

Subsilesian Nappe

(Unit)

Skole / Skiba

Nappe

Boryslav-Pokuttya

Nappe

Stebnik / Sambir Nappe

and Zg

obice Unit

The whole traverse

Sedimentary cover

edimentary cover

Width of the sedimentation zone

[km]

Present-day width of outcrops

[km]

Magnitude of shortening

[km]

Percentage of shortening

[%]

Magnitude of displacement

[km]

Width of the sedimentation zone

[km]

Present-day width of outcrops

[km]

Magnitude of shortening

[km]

Percentage of shortening

[%]

Magnitude of displacement

[km]

Width of the sedimentation zone

[km]

Present-day width of outcrops

[km]

Magnitude of shortening

[km]

Percentage of shortening

[%]

Magnitude of displacement

[km]

Width of the sedimentation zone

[km]

Present-day width of outcrops

[km]

Magnitude of shortening

[km]

Percentage of shortening

[%]

Magnitude of displacement

[km]

Width of the sedimentation zone

[km]

Present-day width of outcrops

[km]

Magnitude of shortening

[km]

Percentage of shortening

[%]

Magnitude of displacement

[km]

Width of the sedimentation zone

[km]

Magnitude of shortening

[km]

Percentage of shortening

[%]

Magnitude of displacement

[km]

12345

123451234512345123451345

E S

E R N C

R P

H I

N S

69,0

37,4

31,6

45,8

34,4

>2,5

0,7

>1,8

>9,5

22,0

19,6

>2,4

>0,9

>10,7

2,1

0,7

1,4

66,7

14,0

>95,6

37,2

>39,9

68,6

III

58,1

31,3

26,8

46,1

33,7

8,5

5,1

3,4

14,2

53,8

31,1

22,7

44,2

37,1

2,2

0,8

1,4

63,6

7,0

122,6

54,2

44,3

92,0

60,3

28,9

31,4

52,1

35,6

2,5

0,7

1,8

9,5

53,9

36,8

17,1

31,7

19,7

2,4

0,6

1,8

75,0

9,1

119,1

52,1

43,7

73,5

E R N C

R P

H I

N S

51,4

23,9

27,5

53,5

32,4

5,2

1,4

3,8

73,0

7,4

60,5

32,2

28,3

46,8

29,2

7,9

1,4

6,5

82,3

9,2

22,3

12,4

9,9

44,4

15,8

147,3

76,0

51,6

94,0

52,2

26,8

25,4

48,7

31,2

5,7

1,1

4,6

80,7

7,3

46,2

19,8

26,4

57,1

28,3

12,7

2,8

9,9

52,0

15,2

37,0

19,7

17,3

46,7

20,0

153,8

83,6

54,4

105,3

VII

58,9

27,4

31,5

53,5

36,3

4,8

1,6

3,2

66,6

8,0

49,9

26,1

23,8

47,7

28,0

24,9

7,8

17,1

68,7

26,2

49,2

21,8

27,4

55,7

31,3

187,7

103,0

54,9

129,8

VIII

61,8

32,8

29,0

46,9

37,9

73,0

35,4

37,6

51,5

38,2

29,1

5,8

23,3

80,0

33,9

42,1

21,2

20,9

49,6

21,5

206,0

110,8

53,4

131,5

2,3

according to cross-sections

, III, I (Po

towicz 2004; Figs. 6 and 9)

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this area was no younger than the early Sarmatian, and it
probably took place in subaerial conditions associated with
the “cannibalism” of older deposits (Ku mierek 1990).

In basement uplifts of the Western Carpathians (Fig. 4), the

magnitude of shortening of the sedimentation zone of the
allochthonous molasse was controlled primarily by the mag-
nitude of slip on the detachments. In the Eastern Carpathians,
however, it was dominated by development of continuous
deformation as seen in cross-sections of the Boryslav-
Pokuttya and Stebnik nappes (Figs. 5B and 9, Table 1 —
columns 3 and 5).

The maximum extent of transgression of the Miocene

molasse onto the flysch nappes (Fig. 9) was reconstructed on
the basis of unpublished data from Urbaniak (in: Ku mierek
1986) and of Ku mierek et al. (1991-1994), as well as publi-
cations of Po towicz (1993). Because this molasse forms the
parautochthonous cover, its extent was reflected in the recent
topography of the orogen, not the magnitude of tectonic dis-
placements in the marginal zone of the Western Carpathians,
which were dominated by thrusts in the base of the flysch
(Fig. 9, Table 1 — column 5). The authors also plotted the
extent of the younger and older folded molasse, thrust over
the younger, autochthonous molasse of the Carpathian Fore-
deep. The minimum southern (southwestern) extent of their
occurrence was determined by interpolation of well data and/
or interpretation of the geometry of overthrusts in the planes
of the traverses.

A synthesis of the palinspastic reconstruction of the tec-

tonic evolution in the NE segment of the Outer Carpathians
during the Late Tertiary is illustrated by the sums of the
parameters calculated for whole traverses (Table 1). The
ranges of values emphasize differences between the Western
Carpathians and Eastern Carpathians, respectively in:
• the reconstructed widths of sedimentation zones: 95.6–

122.6 km and 147.3–206.0 km;

• the magnitude of shortening: 37.2–54.2 km and 76.0–

110.8 km;

• the percentage of shortening: 39.9–44.3 % and 51.6–

54.9 %;

• the magnitude of basement displacements: 68.6–92.0 and

94.0–131.5 km.
The broad interval of geological time for the tectonic evo-

lution during the Late Tertiary (34–12 Ma) for the whole seg-
ment of the Outer Carpathians located to the NE of the Dukla
Overthrust, implies low average shortening rates, for
example, 3.11–5.98 km/Ma for subhorizontal displacements
of the basement. Nevertheless, when taking into account
migrations (in time and space) of the folding and thrusting,
real rates of shortening could be several times higher, for
example, during the Late Oligocene–Early Miocene for the
Middle Group nappes and during the Middle Miocene for the
Marginal Group; for example, in the traverse VII it could
exceed 10 km/Ma (Fig. 9).

The tectonic activity of the front of the Polish Outer Car-

pathians during the Pliocene–Quaternary involved relatively
minor thin-skinned deformation (Zuchiewicz 2001). There

were also long-wave oscillatory uplifts (Gofstein 1964;
Ku mierek et al. 1985), induced by the isostatic effects of
“erosional unloading”. Nevertheless, recent measurements
on drill cores have revealed compressional stress (Jarosi ski
2006), with the principal compressive stress subhorizontal
and deviated a few to more than ten degrees from the inter-
preted displacement directions ascribed to the traces of the
traverses (Fig. 9A).

The kinematic model of the orogenesis

To illustrate the model of the orogenesis of the frontal zone

of the Outer Carpathians, successive stages of the tectonic
evolution were reconstructed in geological cross-
section V (Fig. 5A) through the Przemy l Sigmoid (Fig. 1).
The stages, in millions of years (I–IV in Fig. 10), were scaled
using the magnitude of the subhorizontal tectonic displace-
ments (Figs. 8 and 9) and the vertical component of tectonic
movement of the Skole Nappe, namely subsidence of the
base Oligocene in stage II, and with the amount of syntec-
tonic erosion in stage III and the postinversional erosion in
stage IIIa, which were interpolated on the basis of recon-
structed maps (after Ku mierek et al. 1995).

Having (for the Skole Nappe) the quantified values of the

subhorizontal and vertical components of tectonic move-
ment, the authors made a diagram of the rate and directions
of the tectonic movements (resultant vectors, Fig. 10A) in the
plane of the cross-section. The diagram shows, for succes-
sive stages of the evolution, both the change in the rate of
movement and the oscillation of the movement vectors. It is
suggested that in the early Oligocene (stage I-II), the palaeo-
tectonics of the subbasins reflected the disintegration of the
platform slope into blocks with variable subsidence and even
local uplift due to block rotation, with the initial subduction
taking place in the zone of the Subsilesian Swell (to SW of
the cross-section). The increase in the rate of tectonic dis-
placement in stage II-III, with the subhorizontal component
still dominant, records the major phase of the subduction pro-
cess during the Late Oligocene–Early Miocene, which mani-
fests itself by the formation of thrust nappe and synsedimen-
tary folds together with subaerial erosion of their uppermost
parts (model II and Fig. 3). At the same time, the synclino-
rium of the Skole Nappe, located over the zone of the “sub-
surface wedging” of crustal blocks (model IV), was charac-
terized by a higher degree of tectonic subsidence and
continuous, more asymmetric deformation (Fig. 5A) in com-
parison with the anticlinorium (as shown by the different
lengths and directions of the vectors s II-III and a II-III in
Fig. 10A).

Model IIIa (Fig. 10) illustrates the amount of the postinver-

sion erosion, as shown by the vertical component of the vec-
tor III-IV which has a positive value in Fig. 10A. The subver-
tical trajectory of the vector represents the superposition of
the decline of compression with the isostatic uplift of the
orogen during Miocene–Quaternary times (Fig. 3).

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The propagation of the tectonic deformations as a result of

the subduction of the platform slope is reflected by the con-
sistent vergence of the overthrusts, which is characteristic of
this process. They juxtaposed the imbricated “skybas” in the
section of the Skole Nappe with the Boryslav-Pokuttya and
Stebnik nappes at its base. The degree of the tectonic inter-
ference between the flysch and the flysch and molasse covers
was illustrated (Fig. 10, model IV) to accentuate the analogy
with the palinspastic projection (Fig. 9).

In light of the oroclinal geometry of the deformed sedi-

mentary covers (Figs. 8 and 9), the convergent directions of
the subhorizontal tectonic displacements inevitably resulted
in compression also along the strikes of folds. This is illus-
trated, for example, by the longitudinal cross-sections in the
form of thrust faults (Fig. 10B) which “shorten” the deformed
surfaces. Their occurrence is a strong argument supporting

the proposed model of the orogenesis of the fold and

thrust belt.

Summary and discussion of results

1. The arc of the Outer Carpathians, created by thrusting

and folding, overlies faulted segments of the European Plat-
form lithosphere, bounded to the SW by the collision zone
with altered, thinned lithosphere of a mantle diapir (Kone n
et al. 2002). The lithosphere underlies the Carpathian
Internides and back-arc basins, and that zone is identified
with zero values of the Wiese vector (Jankowski et al. 1979).
The basement of sedimentary basins of the Outer Carpathians
was successively shortened during the Late Tertiary along
deep-seated faults (Ku mierek 2010) during its subduction

Fig. 10. Kinematic model of the tectonic evolution of the nappes of the Outer Carpathians in the Przemy l Sigmoid zone. I–IV — Sections
that image successive stages of the tectonic evolution: I — width of sedimentation zone of the Skole Nappe (Sk) and Boryslav-Pokuttya
Nappe (B-P) during deposition of the chronohorizon of Globigerina (Sheshory) Marls; Ps — Subsilesian Nappe: 1 — start of the palinspa-
stic framework correlated with the intersections of the base of the Menilite Beds with the basal thrust of the Subsilesian Nappe, 2 — points
documenting the widths of sedimentation zones; II — as above, during deposition of the chronohorizon of Jas o (Holovetsko) Limestones:
3 — hypothetical sea level, 4 — hypsometry of the base of the Menilite Beds (Oligocene) and location of probable synsedimentary disloca-
tions, 5 — probable zones of subaerial erosion, 6 — probable location of synsedimentary uplifts of the basement, 7 — interpolated magni-
tude and direction of tectonic displacements of points correlated with location of overthrusts (in the stage II–III), F

sub

–interpolated

sedimentation zone of the Skole succession deposits, in the near-shore (epicontinental) subfacies; III — as above, during deposition of the
base of Badenian deposits, 16.0 Ma (younger molasse), correlated with the beginning of sedimentation of the Balychi Beds; estimated
amount of erosion: 8 — syntectonic erosion, 9 — postinversion (terrestrial) erosion in the stage III–IV; IV — present-day tectonic model
(according to Fig. 5A): 10 — vertical projections of nappe covers (extents of interference), 11 — geometry of chronostratigraphic bounda-
ries: a–base of Oligocene, b–base of Badenian, 12 — traces of nappe overthrusts and minor thrusts, 13 — erosional outliers of ysch
deposits of the Skole succession in the epicontinental subfacies, 14 — top of the consolidated basement (Precambrian) and faults that offset it,
15 — well sections: a–in the cross-section plane, b–projected onto the cross-section; “x”–deep-seated fracture skirting the southern extent
of the platform type? basement; extents of synclinorium (s) and anticlinorium (a) of the Skole Nappe.
Inset A: 16 — diagram showing rates and directions of tectonic movements in successive stages of evolution of the Skole Nappe in the Late
Tertiary; for the stage II–III, measured separately for a ( anticlinorium) and s (synclinorium) of the Skole Nappe;
Inset B: Tectonic sketch of the longitudinal geologic cross-section P through the internal synclinorium of the Skole Nappe (the cross-section
line is in Figs. 1 and 9). 17 — overthrusts of nappes: a–Subsilesian, b–Skole, 18 — thrust faults that offset the base of the Oligocene.

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(together with gravitational? subsidence) including original
uplifts in the basement which separate the West Carpathian
subbasins (Ksi kiewicz 1965). Convergence of the conti-
nental plates of the lithosphere was compensated in the colli-
sion zone by diapiric uprise of the mantle (Kone n et
al. 2002).

2. Thrusts and folds of the sedimentary cover, detached

from the subducted basement blocks, propagated toward the
frontal zone of the Outer Carpathians and were subjected to
telescopic shortening. The variable geometry of the zone was
influenced by the pre-orogenic morphology of the basement
of the sedimentary basins, including transverse oblique-slip
fractures. The strike of the outer compressional suture that
delineates the extent of the flexural platform slope in the area
of the Polish Carpathians — the geoelectric signature of
which was different in nature from the remobilized basement
of the Externides in their central and southern parts

(Stefaniuk et al. 2009, fig. 6; Ku mierek 2010) — correlates
(in the first approximation) with the axis of the gravitational
minimum.

3. The sedimentary cover detached from its basement is

charac terized by distinct styles of: tectonic deformations
(particularly the relatively weak syntectonic successions);
the morphology of sedimentary basins; the sediment thick-
nesses and lithologies; and the geometry and amplitude of
thrusts (Ku mierek & Ney 1988). These have been illustrated
by subsurface cross-sections through the frontal zone of the
NE segment of the Outer Carpathians (Figs. 4, 5 and 6). In
zones of shallow basement, the structural style of the alloch-
thonous cover is dominated by thrust imbricates detached on
sole thrusts, with the geometry becoming more complicated
in the zone of the outer compressional suture. The style and
consistent vergence of the thrust faults record their compres-
sional origin (e.g., Wdowiarz 1976; Ksi kiewicz 1972).

4. The influence of deep-seated faults in the basement,

which terminate upward beneath the sole thrusts (e.g.,
Ku mierek & Baran 2008), manifests itself by changes in
strike and modifications of the tectonics of the allochthonous
cover, and particularly by their discrepancy in the Przemy l
Sigmoid zone, associated with the NW margin of the Trans-
carpathian Depression in the basement. The western part of
the Eastern Outer Carpathians, which overlies that depres-
sion, is characterized by an increasing thickness of the nappes
and of the whole lithosphere (Dérerová et al. 2006) and
a thorough reorganization of the frontal zone of the orogen.
This includes the system of imbricate thrusts that separate
structural elements of the “skyba” type (Fig. 5), as well as the
sedimentary continuity of flysch — molasse successions
with their horizontal interfingering with the Stebnik molasse
and autochthonous foredeep molasse (Petryczenko et al.
1994), apart from local stratigraphic gaps (washouts) and
thrusts that offset the lithostratigraphic boundaries.

5. The tectonostratigraphic identification of depositional

systems in the zone of frontal thrusts (Figs 2, 5, 6 and 7) is
a basic source of information necessary for deciphering the
Tertiary evolution of the Outer Carpathians (e.g., Krzywiec

2006) and it implies their direct connection with the architec-
ture of the platform margin.

6. Profiles of the Miocene sedimentary successions of the

frontal cover in the Western Outer Carpathians, thrust onto
the Ma opolska Block basement, are generally discontinuous
on account of their deposition during subduction of the plat-
form slope. The direction of subduction varied obliquely
rela tive to the strikes of the nappes (Ji í ek 1979; Ellouz &
Roca 1994; Ku mierek 1996), which is why the tectono-
stratigraphic relationships of the Miocene successions with
Cretaceous–Palaeogene (flysch) formations and younger (or
coeval) autochthonous molasse are complicated (Figs. 2, 3, 6
and 7). As a consequence, the Miocene deposits occur in
various tectonostratigraphic positions (Figs. 6 and 7):
• the oldest of them form the upper members of the Krosno

Beds of the ysch succession, preserved, for example, in
the synclinorium of the Skole Nappe (Kotlarczyk 1988);

• the younger ones (and coeval ones) transgressively overlay

(with a stratigraphic gap increasing toward the NW?) the
epicontinental ysch facies but are thrusted and folded
with them; for example, the ysch cores of the Bochnia
folds (Tortonian, Ksi kiewicz 1972) and so-called “ ysch
elements” of the Stebnik succession in the Przemy l Sig-
moid zone (Ku mierek & Baran 2008);

• the youngest ones (early Badenian–early Sarmatian) trans-

gressively overlie the nappes of the Middle Group; in the
frontal thrust zones they form synsedimentary folds and
thrusts — locally with underlying ysch strata
(Komorowska-B aszczy ska 1971) – distinguished as the
Zg obice Unit (Kotlarczyk 1985) and thrust onto the
younger (or coeval) autochthonous molasse (late Bade-
nian–middle/late Sarmatian) of the Carpathian Foredeep
(Ney 1968; Por bski & Oszczypko 1999).
Attempts have been made to link the occurrence of the epi-

continental flysch-type lithofacies at the bottom of the Mio-
cene molasse, or patches of such lithofacies that are inter-
stratified with them, with the concept of gravity flows (Po to-
wicz 2004, Oszczypko et al. 2008); but such an option has no
justification in the compressional style of the frontal zone of
the orogen (e.g., Florek et al. 2004) or in its pre-Badenian
morphology. Instead, the gravity sliding could comprise the
zone of the epicontinental flysch facies, which covered the
platform slope that was uplifted before the middle Miocene.

7. The gradual reduction of thickness and decreasing age

of the autochthonous Miocene molasse toward the zone of
the outer suture in the basement — which was cut by sole
thrusts that propagated synchronously with deposition of the
uppermost members (Figs. 4 and 5) — undermine the re -
liability of interpretations that suggest occurrence of alloch-
thonous molasse on the southern side of the suture (e.g.,
Nem ok et al. 2006), which had been linked with presence of
an internal basin of the Carpathian Foredeep, currently reach-
ing up to the upper San river basin (?, Ney et al. 1974).

8. The tectonic evolution of the central-outer belt of the

Outer Carpathians during the Late Tertiary — palinspasti-
cally reconstructed to two time intervals (Figs. 8 and 9,

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Table 1) — was characterized by the variable arrangement of
sedimentation zones of the frontal nappes, which appeared as
early as in the early Miocene (Fig. 8), and by the increasing
magnitude of subduction of the platform slope, which was
accompanied by growth of the accretionary prism with
increasing thickness of the deformed Miocene molasse. The
convergent subduction direction of the basement blocks
induced a conformable direction of the tectonic transport of
the deformed sedimentary cover — namely toward the SW in
the palaeogeographic projection — however, as a result of
thrust propagation (detached from basement), moving in the
opposite direction shown by the vergence of thrusts and
folds. The magnitude of the movements is scaled by values
of the horizontal component of subducting segments of the
basement; shortening of the segments was increasing with
their vertical rotation that triggered gravitational
subsidence.

9. Potential inaccuracies in images of the palinspastic

framework of the precompressional configuration of the sub-
basins in Figures 8 and 9 (apart from those mentioned in
chapter “Reconstruction criteria for the palinspastic frame-
work”) can be attributed to dating of the tectonic deformation
stages in view of the diachronism of folding and thrus ting
movements and the time of initiation of backthrust faul ting in
internal zones of synclinoria.

10. Application of the traditional (opposite) procedure of

palinspastic reconstruction (Kay 1945) — locating the basins
of the Outer Carpathians in the area of the Pannonian mantle
diapir (e.g., Unrug 1979) — requires an unacceptable distor-
tion of their geometry because of the oroclinal nature of the
fold and thrust arc (Khain et al. 1977; Kruglov et al. 1985)
documented by detailed analysis of the palinspastic projec-
tion (Ku mierek 1988). The opposite kinematic model for the
formation of the accretionary wedge, deformed at the front of
the ALCAPA terrane and moving to the N or NE (e.g.,
Nem ok et al. 2006) implies the controversial original loca-
tion of the Carpathian sedimentary basins.

11. Application of the cross-section balancing technique

for imaging the tectonic evolution of the fold and thrust belt
during the Late Tertiary is complicated by the syntectonic
character of deposition of the youngest sediments, associated
with processes of their deposition and synkinematic erosion,
which requires quantification of anisopachous primary thick-
nesses through reconstruction of the magnitude of erosion
(Ku mierek et al. 1995; Ku mierek 2010, fig. 6). This
problem has often been neglected, and this has had an impact
on the reliability of the presented models (e.g., Nem ok et al.
2006). Cross-sections balanced without balancing of the
highly variable thicknesses of synorogenic sediments
revealing a diachronous pattern of lithofacies boundaries
should not be a basis for drawing the tectogenetic conclu-
sions, in particular based on a kinematic model of only single
traverse (e.g., G ga a et al. 2012).

12. The above problem can be overcome through applica-

tion of the palinspastic method, which allows precise ima-
ging of the precompressional configuration of sedimentation

areas and magnitudes of reduction of their original widths,
under the following conditions:
• exact interpretation of the tectonics of folds and thrusts of

isochronous boundaries in a few cross sections perpen-
dicular to strikes of the folds;

• application of an appropriate reference line of the palaeo-

geographic model and a proper direction of “unfolding”,
and compensation of the horizontal component of ampli-
tudes in planes of discontinuous dislocations formed after
sedimentation of marker stratigraphic horizons.
13. Marked influence on modification of the tectonic style

and stratigraphic inventory of nappes was exerted by trans-
verse zones of deep-seated strike-slip faults, which were dis-
tinguished in Figures 8 and 9 from an undoubtedly more
extensive set of transverse faults (Ku mierek 2010) because
they manifested themselves by changes in strikes of marginal
flysch and molasse subbasins.

14. Discriminating between ductile deformations and brit-

tle deformations, exposed by G ga a et al. (2012), is of sig-
nificance when analysing the disharmonious setting of local
structures. In the regional context, however, the tectonic style
disharmony is more dependent on location of sediments sub-
jected to deformation, and on pinching out of thick series of
synorogenic deposits in zones of basement depression, in
sections of which compressional structures are often asso-
ciated by gravitational deformations with disharmonious
tectonics (Ku mierek 1979), improperly located in the recent
geological map of the Outer Carpathians (Jankowski et

al. 2004).

15. The kinematic model of the orogenesis (Fig. 10), con-

strained by the horizontal and vertical components of tec-
tonic movements, depicts the variable rates and directions in
successive stages of the evolution, with its initial phase in the
early Oligocene (Fig. 10A). Zones of disruption and “subsur-
face wedging” (Roure et al. 1990) of tectonic blocks of the
platform slope were characterized by a greater intensity of
deformation, and the decline of the shortening was accompa-
nied by the isostatic uplift. The convergent direction of
movement in relation to the oroclinal geometry of the subba-
sins also induced strike-parallel shortening (Fig. 10B).

16. The differentiation of the geological structure of the

Western and Eastern Outer Carpathians — reflected by the
different arrangement of the nappes and Miocene parautoch-
thonous covers (Fig. 9) — was influenced by rotation of sub-
ducting lithospheric blocks resulting from the convergent
displacement (with collateral transpressional? interfingering;
Ku mierek 1990) and by the magnitude of the subduction
and the basement relief. As distinct from the uplifted
Ma opolska Block beneath the Western Outer Carpathians,
the western part of the Eastern Outer Carpathians is superim-
posed on the Transcarpathian Depression in the basement,
which separated the Western Carpathian and Transylvanian
mantle diapirs (Naumenko 1984). The influence of the
advanced subduction of the basement in that part of the Outer
Carpathians is manifested by the occurrence of Neogene vol-
canics in the hinterland, accompanied by a detached and

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sunken lithospheric slab (Kone n et al. 2002). The differen-
tiation of the evolution from NW to SE of the central-outer
belt of the Outer Carpathians during the Late Tertiary

(34–12 Ma) is reflected by the large variation of measured
parameters (Table 1):
•  the total width of sedimentation zones: 95.6–206.0 km
•  the magnitude of shortening: 37.2–110.8 km
•  the percentage of shortening: 39.9–54.9 %
•  the magnitude of basement displacement: 68.6–131.5 km
•  the average shortening rate: 3.11–5.98 km/m.y. (with the

maximum value in the late Oligocene–early Miocene,
probably exceeding 10 km/m.y. in the traverse VII).
The parameters above are different from the ones deter-

mined by balancing of one traverse with a different sub-
surface interpretation and conceptual kinematic model
(Behrmann et al. 2000; G ga a et al. 2012). The recon structed
width of the sedimentation zone and the magnitude of

the basement displacements in the plane of that traverse
(Table 1, traverse V) are relatively smaller than the values
given by Roure et al. (1993) based on a hypothesis of a maxi-
mum dimension of the subthrust basement (Roure et al. 1994,
fig. 11).

When comparing the above parameters we should keep in

mind that the data in Table 1 and images in Figs. 8 and 9 are
scaling only the subhorizontal component of tectonic dis-
placement, unlike balanced cross-sections which sum up the
values of both components of the displacement.

The significant differences in the structure of the frontal

zone of the Western and Eastern Outer Carpathians, which
have evoked different criteria for their classification by
Polish and Ukrainian geologists, do not undermine the homo-
geneous model of the orogenesis for the whole NE segment
of the Outer Carpathians.

Acknowledgements: The paper was prepared within the
framework of the research project ShaleCarp in the program
Blue Gas II,  nanced by the National Centre for Research
and Development (BG2/ShaleCarp/14). The regional geo-
logical traverses, illustrating the subsurface geological struc-
ture of the transfrontier zone of the Polish and Ukrainian
Outer Carpathians, which are not included in the presented
paper (except for their modi ed fragments) but nevertheless
were used for reconstruction of the palinspastic models, were
prepared within the framework of the Polish-Ukrainian
research projects no. PB/PUPW/6/2005 and no. 646/N from
Ukraine/2010/0,  nanced by the Ministry of Science and
Higher Education of the Republic of Poland. Their construc-
tion was possible thanks to the  nal reports of wells and
archival seismic sections being made available by the Polish
Oil and Gas Company S.A. and Polish Geological Institute
— National Research Institute. The seismic sections were
reprocessed by the AGH-UST research team under the super-
vision of Dr Tomasz Ma kowski. We gratefully acknowledge
Prof. Walery Omalczenko and Dr Krystyna Zayats for con-
sultation on the interpretation of the cross-sections through
the Ukrainian Carpathians. We are grateful to MSc Julian

Krach for the English translation as well as Prof. Szczepan
Por bski and PhD Mark G. Rowan for thorough editorial
remarks preceding submission of the manuscript to the
Editor.

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