The structural position and tectonosedimentary evolution.pdf

Przegl¹d Geologiczny, vol. 52, no. 8/2, 2004

The structural position and tectonosedimentary evolution

of the Polish Outer Carpathians

Nestor Oszczypko*

A b s t r a ct. The sedimentary basins of the Outer Carpathians are regarded as the remnant oceanic basins that were transformed into

the foreland basin. These basins developed between the colliding European continent and the intra-oceanic arcs. In the pre-orogenic

and syn-orogenic evolution of the Carpathian basins the following prominent periods can be established: Middle Jurassic — Early

Cretaceous opening of basins and post-rift subsidence, Late Cretaceous — Palaeocene inversion, Palaeocene to Middle Eocene subsi-

dence, Late Eocene–Early Miocene synorogenic closing of the basins. In the Outer Carpathian sedimentary area the important driving

forces of the tectonic subsidence were syn- and post-rift thermal processes as well as the emplacement of the nappe loads related to the

subduction processes. Similar to the other orogenic belts, the Outer Carpathians were progressively folded towards the continental

margin. This process was initiated at the end of the Palaeocene at the Pieniny Klippen Belt Magura Basin boundary and completed

during Early Burdigalian in the northern part of the Krosno flysch basin.

Key words: rifting, inversion, subsidence, tectono-sedimentary evolution, Outer Western Carpathians

The Polish Carpathians are a part of the great arc of

mountains, which stretches for more than 1300 km from

the Vienna Forest to the Iron Gate on the Danube. In the

west the Carpathians are linked with the Eastern Alps, whi-

le in the east they pass into the Balkan chain (Fig. 1). Tradi-

tionally, the Western Carpathians have always been

subdivided into two distinct ranges. The Inner Carpathians

are the older range and the Outer Carpathians are the youn-

ger (Ksi¹¿kiewicz, 1977). The Pieniny Klippen Belt (PKB)

is situated between the Inner and Outer Carpathians. The

belt is a Neogene suture zone about 600 km long and 1–20

km wide with a strike-slip boundary (Birkenmajer, 1986).

The Outer Carpathians are built up of stacked nappes and

thrust-sheets, which reveal a different lithostratigraphy and

structure (Fig. 2). Traditionally, three groups of nappes

could be distinguished (Ksi¹¿kiewicz, 1977). The Margi-

nal Group consists mainly of folded Miocene rocks, which

are well represented at the front of the Eastern Carpathians,

whereas the Middle Group (Early/Middle Miocene accre-

tionary wedge) consists of several nappes that form the

corn of the Western and Eastern Carpathians. The Magura

Group (Late Oligocene/Early Miocene accretionary wed-

ge) is flatly overthrust onto the middle group which con-

sists of several nappes: the Fore-Magura–Dukla group,

Silesian, Sub-Silesian and Skole units (Fig. 3). In the Outer

Carpathians the main decollement surfaces are located at

different stratigraphic levels. The Magura Nappe was

uprooted from its substratum at the base of the Turo-

nian–Senonian variegated shales (Oszczypko, 1992), whe-

reas the main decollement surfaces of the middle group are

located in the Lower Cretaceous black shales, with the

exception of the Fore-Magura group of units, which were

detached at the Senonian base. All the Outer Carpathian

nappes are flatly overthrust onto the Miocene deposits of

the Carpathian Foredeep (Oszczypko, 1998; Oszczypko &

Tomaœ, 1985). However, along the frontal Carpathian

thrust a narrow zone of folded Miocene (marginal group)

deposits developed (Pouzdøany, Boryslav–Pokuttya, Steb-

nik (Sambir) and Zg³obice units). In Poland these are repre-

sented mainly by the Zg³obice and partially by the Stebnik

units. The detachment levels of the folded Miocene units

are usually connected with the Lower and Middle Miocene

evaporites.

The basement of the Outer Carpathian is the epi-Va-

riscan platform and its cover (Figs 3–4). The depth of the

platform basement, known from boreholes, changes from a

few hundred metres in the marginal part of the foredeep up

to more than 7000 m beneath the Carpathians. The magne-

to-telluric soundings in the Polish Carpathians have reve-

aled a high resistivity horizon, which is connected with the

top of the consolidated-crystalline basement (¯ytko,

1997). The top of magneto-telluric basement reaches a

depth of about 3–5 km in the northern part of the Carpa-

thians, drops to approximately 15–20 km at its deepest

point and then peaks at 8–10 km in the southern part (Figs

5–6). The axis of the magneto-telluric low coincides, more

or less, with the axis of regional gravimetric minimum.

This was documented by the integrated geophysical model-

ling along the Rzeszów–Bardejov geotraverse (Fig. 6).

South of Krosno this gravimetric low is a result of the com-

bined effect of the thick Carpathian nappes, thick Early

Miocene molasses, and possibly the Mesozoic and

Paleogene deposits related to passive margin of the Euro-

pean Platform (Oszczypko, 1998; Oszczypko et al., 1998).

South of the gravimetric minimum and, more or less

parallel to the PKB, a zone of zero values related to of the

Wiese vectors was found in geomagnetic soundings (Jan-

kowski et al., 1982). This zone is connected with a high

conductivity body at a depth of 10–25 km and is located at

the boundary between the North European Plate and the

Central West Carpathian Block (¯ytko, 1997). In the Polish

Carpathians, the depth of the crust-mantle boundary ranges

from 37–40 km at the front of the Carpathians and incre-

ases to 54 km towards the south before peaking along the

PKB to 36–38 km (Fig. 5).

Main structural units and the problem of the SE

prolongation of the Magura Nappe

Since the 1970s the principal structural units of the

Outer Western Carpathians have been well correlated (see

¯ytko et al., 1989; Lexa et al., 2002). From the west of the

Polish state boundary to the Valaške Mezerice area, where

the Silesian Unit disappears, there is a direct continuity of

*Jagiellonian University, Institute of Geological Sciences,

Oleandry 2a, 30-063 Kraków, Poland; nestor@geos.ing.uj.edu.pl

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Przegl¹d Geologiczny, vol. 52, no. 8/2, 2004

[

Kraków

Ostrawa

POLAND

Przemyœl

0 0000km

Brno

Ivanofrankivsk

SLOVAKIA

Kosice

Uzhhorod

Bratislava

HUNGARY

ROMANIA

Barsana

Botizi

Rakhiv

Carpathian foreland

Rakhiv Unit

Carpathian foredeep molasse

Marmarosh Crystalline Massif

Folded Miocene molasse

Magura group of nappes

Borislav–Pokuttya Unit

Pieniny Klippen Belt and other klippes

Skole/Skyba Unit

Tatricum and its sedimentary cover

Sub-Silesian–Zdanice units

Veporicum, Zemplinicum, Hronicum, Gemericum, Meliaticum, Turnaicum and Silicicum

Silesian–Chornohora Unit

Inner Carpathian and Buda Paleogene

Dukla Unit

Neogene Alpine volcanics

Porkulets Unit

Fig. 1. Structural sketch-map of the Northern Carpathians — based on Lexa et al. (2000), Kuzovenko et al. (1996), and Aroldi (2001)

all main structural units (Fig. 1). Further to the SW the

position of the Silesian Unit is occupied by a thin-skinned

Zdanice–Sub-Silesian Unit. At the same time new and

more external, allochthonous tectonic units (Pouzdrany

Unit and then Waschberg zone), have appeared at the front

of Sub-Silesian Unit. The correlation between the structu-

ral units of the middle group in the Polish and Ukrainian

Carpathians has been discussed in detail by ¯ytko (1999).

This particular correlation is more difficult because in the

Ustrzyki Dolne area (Figs 1, 2), close to the Polish/Ukra-

inian boundary, the Sub-Silesian/Silesian overthrust is

overlapped by the Lower Miocene Upper Krosno Beds.

The eastern prolongation of the Sub-Silesian facies is spo-

radically marked by the occurrence of variegated marls

(Rozluch and Holyatyn folds). The southern part of the

Silesian Unit in Poland (i.e., Fore-Dukla Unit and Bystre

thrust sheet) could be correlated with the Chornohora Unit.

According to ¯ytko (1999), the SE prolongation of the

Dukla Unit is related to the Porkulets (Burkut) Nappe,

whereas Ukrainian authors (Shakin et al., 1976; Burov et

al., 1986) link the northern boundary of the Dukla Unit to

the Krasnoshora and Svidovets subunits. The southern-

most units of the Ukrainian Carpathians belong to the

Rakhiv and Kamianyj Potik units, which are correlated

with the Ceahleu and Black Flysch units of the Romanian

Eastern Carpathians, respectively. In the Western Outer

Carpathians there are no equivalents of these units. The

Magura Nappe is composed mainly of Upper Cretaceous to

Eocene deposits. The oldest Jurassic–Early Cretaceous

rocks are known from the peri-Pieniny Klippen Belt in

Poland and few localities in Southern Moravia (Birkenme-

jer, 1977; Švabenicka et al., 1997), whereas the youngest

deposits (Early Miocene) have been recently discovered in

the Nowy S¹cz area (Oszczypko et al., 1999; Oszczypko &

Oszczypko-Clowes, 2002). The Magura Nappe is separa-

ted from the PKB by a subvertical Miocene strike-slip

boundary, and flatly thrust at least 50 km towards the north

over its foreland (Figs 2–6). This nappe has been subdivi-

ded into four structural subunits: Krynica, Bystrica, Raèa

and Siary (Fig. 2), which coincide to a large extent with the

corresponding facies zones. On the west the Magura Nappe

is linked with the Rheno–Danubian flysch of the Eastern

Alps. Towards the east this nappe extends to Poland and

runs through Eastern Slovakia before disappearing beneath

the Miocene volcanic rocks, east of Uzhhorod (Trans-Car-

pathian Ukraine).

In the SE part of the Ukrainian and Romanian Carpa-

thians, the zone of the Marmarosh (Maramures) Flysch has

been distinguished (Smirnov, 1973; Sandulescu, 1988;

Aroldi, 2001). Between the Latorica and Shopurka rivers

this zone is bounded from NE by the Marmarosh Klippens

and further to SE by the the Marmarosh Massif, which are

thrust over the Lower Cretaceous flysch of the Rakhiv and

Porkulets units (Fig. 7). In the Marmarosh Flysch zone two

facies-tectonic units have been distinguished: the external

Vezhany, and the internal Monastyrets units (Smirnov,

1973).

The basal part of the Vezhany Unit is built up of oli-

stostrome, up to 100–200 m thick and is composed of Meso-

zoic carbonate rocks, serpentinites, basic volcanites, grani-

toids and metamorphic rocks. The olistostroma is followed

by a 200 m thick sequence of the Upper Albian–Cenoma-

nian grey and dark grey marly mudstones with intercala-

tions of fine-grained, thin-bedded sandstones of the Soimul

781

Przegl¹d Geologiczny, vol. 52, no. 8/2, 2004

19°

20°

21°

22°

Kraków

Rzeszów

POLAND

Cieszyn

Bielsko Bia³a

Przemyœl

¯ywiec

Jas³o

Krosno

Nowy S¹cz

Gorlice

Nowy Targ

Krynica

Zakopane

Bardejov

Malcov

Dolny Kubin

30 km

– Siary S

ubunit

–

Raèa S

ubunit

–

Bystrica S

ubunit

–

Krynica Subunit

crystalline core of the Tatra Mts.

High Tatra and Sub-Tatra units

Podhale Flysch

Pieniny Klippen Belt

Magura Nappe, a – Malcov Formation

Grybów Unit

Dukla Unit

Fore-Magura Unit

Skole Unit

Lower Miocene

Miocene deposits upon the Carpathian

Stebnik (Sambir) Unit

Zg³obice Unit

Miocene of the Carpathian Foredeep

Silesian Unit

Sub-Silesian Unit

andesite

cross-section line

Fig. 2. Geological map of the Polish Carpathians (after ¯ytko et al., 1989 and Lexa et al., 2000 — supplemented)

Formation, around 180 m of the Turonian–Campanian

pelagic red marls of the Puchov type and 30 m of the

Maastrichtian thin-bedded flysch with intercalations of red

shales of the “Jarmuta beds” (Dabagyan et al., 1989). The

upper part of this sequence, 200–300 m thick, is composed

of dark shaly flysch and thick-bedded sandstones of the

Metove Beds (Eocene) with the Upper Eocene variegated

marls at the top (Smirnov, 1973). Higher up in the section

these beds are overlapped by black marls of the Luh Beds.

In the Terebla River section, Oligocene (Rupelian) calcare-

ous nanoplankton was recently discovered (Oszczypko &

Oszczypko-Clowes, 2004). The Luh Beds resemble the

Grybów and Dusyno bituminous marls known from the

Fore-Magura units in Poland and Ukraine. In our opinion,

the Vezhany succession could be regarded as an equivalent

of the Jas³o Unit and the North Fore-Magura thrust sheet in

Poland (Oszczypko & Oszczypko-Clowes, 2004).

The Monastyrets Unit is composed of Coniacian–Pala-

eocene calcareous flysch with red shales (Kalyna beds,

Vialov et al., 1988) at the base. These deposits are followed

by thin-bedded flysch and variegated shales of the Shopur-

ka Beds (Lower–Middle Eocene) and thick-bedded Dra-

hovo Sandstones (Middle–Upper Eocene, see Smirnov,

1973; Andreyeva-Grigorovich et al., 1985). From the south

this unit joins the PKB along the sub-vertical fault.

Towards the NE it is thrust over the Vezhany Unit or direc-

tly onto the Rakhiv or Porkulets nappes.

In the Romanian Maramures equivalents of the Mona-

styrets Unit are known as the Leordina and Petrova units

and are composed of Maastrichtian–Chattian deposits

(Aroldi, 2001). South of the Bohdan Foda Fault position of

the Petrova Unit is occupied by the the Wild Flysch Unit.

According to Aroldi (2001) this unit is a SE prolongation

of the Petrova Unit. All these units have been included by

Aroldi (2001) to the Magura Group of units, which are fla-

tly overthrust towards the NE and S onto the Paleoge-

ne–Lower Miocene deposits of the Borsa Beds. Between

the Botiza–?Krichevo Unit (Late Cretaceous–Oligocene)

and the Wild Flysch Unit, the Middle Jurassic–Oligocene

Poiana Botizei Klippens are wedged. These klippes are

regarded by Aroldi (2001) as the SE termination of the

PKB, but according to Bombita et al. (1992) they represent

the intra-Magura klippens (like Hluk Klippe in S Moravia).

O UTER CARPATHIANS

CARPATHIAN FO REDEEP

MAGURA UNIT

SILESIAN UNIT

OP 1

Andrychów 3

Pszczyna 4

Zawoja 1

Sucha IG 1

Potrójna IG 1

Andrychów 2

Sosnowiec IG 1

(km)

PKB

Devonian and

Lower Carboniferous

Upper Carboniferous

Lower Cretaceous–Paleogene

of the Silesian Unit

Upper Cretaceous–Paleocene

of the Sub-Silesian Unit

Lower Badenian–Sarmatian

Upper Miocene

thrust and overthrust

consolidated basement

of the Inner Carpathians

Proterozoic–Lower Paleozoic

of the Bruno-Vistulicum

Triassic

Senonian–Paleocene

boreholes

High Tatra/Sub-Tatra Units

Eocene

IC Inner Carpathians

Lower Palaeozoic

Pieniny Klippen Belt

Lower Miocene

Podhale Flysch

Fig. 3. Geological cross-section (A–B) Orawa-Sosnowiec (after Oszczypko et al., in print)

782

Przegl¹d Geologiczny, vol. 52, no. 8/2, 2004

OUTER

CARPATHI ANS

PKB

MAGURA

NAPPE

MSZANA DOLNA

TECTONIC WINDOW

SILESIAN

UNIT

Krynica Subunit

Bystrica Subunit

Nowy Targ IG1

Obidowa IG1

Porêba Górna IG1

NiedŸwiedŸ IG1

Wiœniowa IG1

8km

Inner Carpathians

High Tatra crystalline basement

and its sedimentary cover (Tatricum)

Upper Cretaceous variegated marls

of the Sub-Silesian Unit

Palaeocene–Eocene

Krosno & Malcov Formations

Sub-Tatricum units (Fatricum)

Waksmund Formation (Lower Miocene)

Eocene and Oligocene

of the Podhale Flysch

Outer Carpathians

Eocene

Upper Miocene post-tectonic cover

Platform basement and Carpathian foredeep

Pieniny Klippen Belt

Eocene variegated shales

Vendian–Lower Cambrian

of the Ma³opolska Massif

Lower Cretaceous

Grybów Unit

Platform carbonate cover

(Meso–Palaeozoic)

Lower/Middle Miocene

Upper Cretaceous–Palaeocene

Menilite shales (Oligocene)

Carpathian overthrust

Magura overthrust

other overthrusts

Fig. 4. Geological cross-section (C–D) Nowy Targ IG1—Wiœniowa IG 1

The Marmarosh Flysch of the Eastern Carpathians

(Ukraine ad Romania) revealed several similarities to the

Magura Nappe of the Western Carptahians in Slovakia and

Poland. These nappes occupied the same geotectonic posi-

tion and they are bounded from the north and south by the

Fore-Magura group of units and PKB, respectively. The

Magura and Marmarosh flysch successions revealed the

same basin development trends, palaeocurent direction and

location of source areas. Both these successions revealed a

prominent, northward progradation of the Eocene/Oligoce-

ne thick-bedded muscovitic sandstones (see ¯ytko, 1999).

In the Marmarosh Flysch this is manifested by occur-

rence of the Secu Sandstones (Lutetian–Priabonian) in the

Botiza Unit, Stramtura/Drahovo Sandstones (Priabonian)

in the Petrova/Monastyrets Unit and the Voroniciu Sandsto-

nes (Rupelian–Chattian) in the Leordina Unit (Aroldi, 2001).

According to ¯ytko (1999) the Petrova/Monastyrets,

Botiza and Wild Flysch units of the Marmarosh Flysch

could be the equivalents of the Raèa, Bystrica and Krynica

subunits of the Magura Nappe respectively. Taking into

account facies prolongation of the Petrova/Monastyrets

Unit into the Wild Flysch Unit (Aroldi, 2001) and the lack

of £¹cko Marls in the Botiza Unit, these correlations

should be modified. It appears that there are no equivalents

of the Bystrica succession in the Marmarosh Flysch, and

the Botiza succession better fits the Krynica succession

than that of the Wild Flysch (see Oszczypko & Oszczyp-

ko-Clowes, 2004).

In view of the internal position of the Marmarosh Fly-

schinrelationtotheMarmaroshMassif,aswellasthe

above mentioned similarities between:

1) the Vezhany and Fore-Magura/Jas³o successions,

2) the Monastyrets/Petrova and Raèa and

3) the Botiza and Krynica successions, it is possible to

conclude that the palaeogeographical positions of the Mar-

marosh Massif and the buried Silesian Ridge were almost

the same (see Sandulescu, 1988; Oszczypko, 1992, 1999).

The Evolution of the Outer Carpathian basins

The Outer Carpathians are composed of Late Jurassic

to Early Miocene mainly flysch deposits. The sedimentary

sequences of the main tectonic units differ in the facies

development as well as in the thickness. The thicker sedi-

mentary cover belongs to the Silesian Unit, which varies

from 3000 m, in its western part, to more than 5000 m in the

east. The stratigraphic thickness of the other tectonic units

is distinctively thinner and varies between 3000 and 3800

m in the Skole Unit, around 1000 m in the Sub-Silesian

Unit, 2300–2500 m in the Dukla Unit and 2500–3500 m in

the Magura Nappe (Poprawa et al., 2002a). Taking into

account the distribution of facies, the thickness of the depo-

sits and the palaeocurrent directions (see Ksi¹¿kiewicz,

1962) only the Magura, Silesian and Skole basins could be

considered as independent sedimentary areas (see also

Nemèok et al., 2000). During the Late Cretaceous–Eocene

times, the Sub-Silesian depositional area formed a subma-

rine high dividing the Skole and Silesian basins. The histo-

ry of the Dukla sedimentary area, which played the role of a

transfer zone between the Magura and Silesian basins, was

more complex. According to the reconstructions of Roure

et al. (1993) and Behrman et al. (2000), the Outer Carpa-

thian basins during the Early Oligocene were at least 380

km wide across the Przemyœl–Hanu

783

8km

ovce geotraverse.

This restoration does not include the Silesian Ridge, at

least 20–50 km wide (see Unrug, 1968), located between

the Magura and Silesian depositional areas. This suggests

Przegl¹d Geologiczny, vol. 52, no. 8/2, 2004

INNER

CARPATHIANS

PKB

SLOVAKIA POLAND

OUTER CARPATHIANS

Krynica

Nowy S¹cz

Bochnia

MAGURA

NAPPE

R-1

LG-1

WN-2

WN-1

L-22

Z-1

I-1

PD-2

D-1

C-1

(km)

100 °

200 °

300 °

400 °

500 °

20 km

Podhale flysch

Pieniny Klippen

Belt

Dukla and

Grybów units

Mesozoic

high resistivity basement

(after ¯ytko, 1997)

boreholes

Fatricum

Krynica subunit

of Magura Nappe

Sub-Silesian

and Silesian units

Palaeozoic

low-resistivity horizon

(after ¯ytko, 1997)

CO ascension

Tatricum

Bystrica subunit

of Magura Nappe

Badenian

and Sarmatian

upper crust

400 °

isotherms

Moho

Vahicum

Siary and Raca subunits

of Magura Nappe

Palaeogene and

Lower Miocene

lower crust

faults and

overthrusts

Krynica dislocation

upper trench

Fig. 5. Geological cross-section (E–F) Krynica–Bochnia (after Oszczypko & Zuber, 2002 — suplemented)

that the entire width of the Outer Carpathian domain rea-

ched at least 500 km.

Traditional opinions suggest that the Magura and Sile-

sian basins were situated parallel to each other (see

Ksi¹¿kiewicz, 1962; Unrug, 1968, 1979; Birkenmajer,

1986). This view was recently questioned by Nemèok et al.

(2000) who placed the Magura depositional area as the

south-western neighbour of the Silesian depositional area,

whereas the present-day position of these units is a result of

the Miocene eastwards escape of the Magura Nappe. This

model does not fit the facies distribution in the Polish Outer

Carpathians (Bieda et al., 1963), palaeocurent measure-

ments, nor the transitional position of the Dukla suc-

cession, between the Magura and Silesian basins.

The sedimentary succession of the Outer Carpathians

(Table 1) reveals three different megasequences of depo-

sits, reflecting the main stages of the basins development

(Poprawa et al., 2002a). The first (long lasting) and third

(relatively short) periods were characterized by the unifica-

tion of sedimentary conditions, whereas the intermediate

periods were characterized by a maximal differentiation of

sedimentary conditions.

longation towards the east (Oszczypko, 1992; Golonka et

al., 2000, 2003). This oceanic domain was divided by the

submerged Czorsztyn Ridge into the NE and SE arms. The

Czorsztyn Ridge and the Inner Carpathian domain were

separated by the SE arm of the Pieniny Ocean, known also

as the Vahicum Oceanic Rift (south Penninic domain),

whereas NE arm was occupied by the Magura deep-sea

basin situated south of the European shelf, an equivalent of

the north-Penninic (Valais) domain (see also, Plasienka,

2003). This stage of the Magura Basin evolution is rather

speculative, because the Magura Nappe was uprooted

roughly at the base of the Upper Cretaceous sequence. The

Jurassic–Lower Cretaceous deposits of the Magura Basin

were probably represented by deep water, condensed pela-

gic limestones and radiolarites. At the end of the Jurassic in

the southern part of the European shelf, the palaeorifts

were floored by a thinned continental crust (Birkenmajer,

1988; Sandulescu, 1988). This rifted European margin was

incorporated into the Outer Carpathian Basin (Skole,

Sub-Silesian/Silesian basins). The rifting process was

accompanied by a volcanic activity (teschenite sills, dykes,

and local pillow lavas), which persisted up to the end of

Hauterivian (Luciñska-Anczkiewicz et al., 2002; Grabow-

ski et al., 2004). This part of the rifted continental margin

probably extended in the Eastern Carpathian (basic effu-

sives —Tithonian–Hauterivian), see Lashkevich et al.

(1995) of the “Black Flysch”, Kamyany Potic, and Rakhiv

beds) as well as to the Southern Carpathian (Sandulescu,

1988). During the initial stage of development, the Silesian

Basin was filled with calcareous flysch followed by silicic-

lastic flysch and pelagic shales. The Early Cretace-

ous–Cenomanian deposition took place during relatively

Middle Jurassic–Early Cretaceous opening of basins

and post-rift subsidence (125–150 My)

The Outer Carpathian basins can be regarded as rem-

nant ocean basins, which developed between the colliding

European continent and the intra-oceanic arcs (Oszczypko,

1999). The Early/Middle Jurassic opening of the Magura

Basin was probably coeval with the timing of the

Ligurian–Penninic Ocean opening and its supposed pro-

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