Geological structure of the western part of the Polish Carpathians

GcologiCilI Quarterly, Vol. 40, No.4. 1996, p. 501-520

Zbigniew PAUL. Wojcie<:h R Yt.KO, Adam TOMA$

Geological structure of the western part of the Polish Carpathians

The study area is located between Cicszyn and meridian of Socha Beslddzka. Tile Prccambrilln Ilnd its cover- Palaco1.oic plotrornl deposits -occuninl:; here, ore &lrongly dcfonned Ilnd capped by tile NeogcllC molllS5c. The lnojorp4t1 or tile area isoccupicd by the Ays.::h Carpathians. In the Carpathians, units oftbe MiddlcGroup (Skole.

Sub·Silesian, Klippen, Silesian, Dukla and Gryb6w) as well as tbe Magura unit have been distinguished and

d~ibcd.

Geolo,pClll structure ofllle lower strudural stagC5 haye only been outlined while the flysch. its str.lligmphy and te<:tonic:s. has been discussed in details. The Sl:olc unit occurs in the marginal p4t1 orthc Carpathi:ms, in the region of AndrycllOw and in tectonic windows within the Sub·Silesian and Silesian units. Deposits orthe Sub..silesi:m unit are found at the surface: as twoorthrce discontinuous bands. During the Neogene the unit had been truncated and developllf:\s doubled oreven tripled scales (imbtic:ded folds). The RIOSt external pari of tile Sub..silesian unit occurs (It the front of the Drpathian overthrust as a band extending from Cienyn to the region of AndrychOw.

The more internal part orllle unit is recorded in the: llzit;giel6w and Ustrorl windows. :md the inntrmo5l. southern part is found at the front of the Dukla, Gryb6w and Magum units. The middle clemcll\ of the Sub·Silesian unit might be associated wilh the extcnsion of Ihe Lanckorona-:agocina zone towLU"ds the wc". The Silesian unit i~

divided into te<:lonic sub·units: the lower one - CieS1.yn sub-unit (n~ppc), and the upper _ Godulll sub-unit (nappe). Deulehment which lcad to 5Cparation of the Godula sub-unit as a separate entity tool: place wililin the Upper Cicstyn Shales or $Iightly hisher. The Dukla unit WUUldIO!>as been distinguished between Slemierl and Istcbna. In the eastern part. between $Iemicr\ and Zywicc,thc Dukla unit is thrust oycrthe deposits oftlle Silesi:m unit of the UIlIe Beskid block. In the soulhcm part oflhe iywie<: Basin the di5Cussed unit together with the deposits orille uppetGryb6w unit is thrust over the deposits orthc Cicnyn Silesian sub·uniL So1.Ith of Barania GOT:l MI..

the Dukla unit is thfust ovec tile deposits orthe Silesian Bcskid.

The authors distinguish thedeposilso(the Gryb6w unit between Gilowiccand ISlcbn:a region. 11Jc unil is mainly formed by clayey·marly deposits of the Lowcr Crct:lCCOus·Palaeogcne age. This unit was strongly compressed.

scaled and crushed belwccn the Dukla and Magura units. In exposures, the Gryb6w unit t.,kes II form of isolated scales and tectonic caps. It has also bcc:n idenlilied in numerous te<:tonic windows within the Magura unit. TIlt Magum unit is the highest unit in the discussed TCgion. It is subdivided into threc sub· units. The northern one is the Siary sub·unit and its deposits nrc thrust over the units of the MiddleGroup. The middle one is ROC1.3 sub·unit over which the southern one - Bystriell sub·unit - is thrust.

502 Z. Paul, W. Rylko, A. To~

INTRODUCTION

The s

tudy

area is located between Cieszyn and the meridian of Sucha Bcskidzka.

Its

western and southern borders coincide with Poland'sstale boundary. From geomorp

hologi-

cal poi", of view the majority of the area belongs to the Outer Carpathians but the nonhern and

nonhwestern paris

belong to the fore-Carpathian basins. In the d

iscussed region, the

Carpathians are divided into the Beskids and the Carpathian Foothills.

The Precambrian and its cover -

Palaeozoic platform deposits. occurring

here, are sirongly deformed and capped by the Neogene molasse. The major part of the area is occupied by the Flysch Carpathians. In the Carpathians, units of the Middle Group (Skolc, Sub-Si

lesian, Klippen, Silesian, Dukln and Gryb6w) have been distinguished and described.

Moreover, the

Magura unit

has been distinguished. There, the Siary, Racza and Bystrica s

ub-un

its

have been singled out and characterized.

The discussion of the Quaternary deposits occurring in the study area are beyond the scope of this paper.

R

EVlEW OF PREVIOUS STUDIES

First infonn ation about geological studies in this region originated from

160 years ago

and can be found in papers by Austrian authors.

First cartographic

maps were printed al the end of the last century by W. Szajnocha (1985) and included the following sheets of the Atlas GeologicVlyGalicyi (Geological Atlas of Galicia)

1:75000: Zywiec-

Ujsofy, Bielsko-Biala and Mak6w.

In 1934-1935 the

Mapa Geologiczna Karpat SUlskich (Geological Map of the Silesian Carpathians) was prepared under the initiative of the Sitesia Publishing Commission, Polish Academy of Arts and Letters (J.

Burtan6wna

el al., 1937).

A

dynamic

development of in."estigations in the study area and in

the

neighbouring

terrains went on in the

post-war years. Works by

A. Tokarski (1947) and M. Ksill.zkiewicz

(195

1)

are particularly important. In the 1950s the s

tudies on the structure ofZywiec pari

of the High Beskid MIS. were carr

ied oUlby W.

Sikora and K. Zy

tko (1956, 1960) and by J. Burton, S. Sokolowski (1956). In thcsucccssive years various geological maps of the area

in question were publ

ished. The authors of these maps were:

K. Zytko (

1

966a, b), J. Go- lonkaet al. (1979) and W. Ry

lko,

Z. Paul (1994). Besides the quoted works of a cartographic charac

ter and geological maps, the discussed area was [he subject to othcr studics including:

stratigraphic, tectonic and lithologic ones that resulted in numerous publications, i.a.:

J

. Burtan (

1936, 19680, b), J.

Burtan, S. Sokolowski (1956),

J.

Burtan

el

al. (1959),

J.

Golonka, A. W6jeik

(1978),

L. Koszarski (1985), L. Koszarski, A. Slll.czka (1973), M. Ksill.i.k

iewicz, J. Liszkowa (1972), J. Liszkowa, W. Nowak (1964), W. Nowak (1

959), B. Olszewska (1981), N. Oszczypko, A.

Tom~

(1985), W. Rylko (

1992,1994), W. Rylko

et al. (1992,

1993) and S.

Sokolowski (

1958).

Moreover, a great many papers dealing with the basement of the Flysch Carpathians

were put out, among others by: W.

Heflik, K.

Konior (1 970, 1974),

K.

Konior (1965),

T. Kucinski,

F.

Mitura (1958), W. Moryc (1970,

1

989), W. Nowak (1975), W.

Rylko,

A. TomM (1995), A. SI«czka (I 976a, b), A. Tokarski (1947) and

K. Zytko (1978).

GeoloSicnl structure ofllle westCtll part ofCarpathinns

S03

_ I n l

I CCI-u ,~.-.-~- ,,'

^{, ~ KlippIn /'11}

~--""'~_III

A-A _ _ 1<11

_ 1 1 ... _ ... II) 2 0 1 ' 1 ' I ( l 0 l . . .

Fig. I. Gcologicalskclch oflhe Polish plIn orille Weslctll Cnrpalhi;ms belween Cicilyn aad Sucha Bcskid1.klI Szkic sculugiczny polskicj ~ci K3I'plIl Znchotlnich mi~dzy Cieszyncm n Such:\ IJcskidzk:&

Zapadli$ko prl.Cdkarpackic: 1- ncogcn (miocen); KllI'Jlnty WW"<'tnnc: 2- jcdnOSlkll skolska - kreda-neogcn, 3 - jednOSlka po(jg]:\Ska - kreda-palcogcn, 4 - jcdooslka ~1;jSka - g6rru\ jUnI-paleogcn, S - jcdnoSlIro dukielska - paleogen, 6 - jcdnostka gf}'bowska - dolnn kredn-palcogcn. 7 - jedooslb Irnlgurskll - g6m3 krcd3-paleo~n: 8 - Vomica n:lSunieciD karpackicgo; 9 - &I3nica gl6wnych jcdnoslek IcklOOictnych; 10- wlltniejsz.e uskoki, II-otwory wicnnic#: 12 -slca/ki andrychowskie; 13 - linia przckroju gcologicwego

A possible discovery of hydrocarbon deposits in the Polish and Czech Western Carpa·

thi ans has aroused much interes t for many years. Moreover, Polish Geological Institute made several deep, study boreholes (Fig. 1 ) in the 1 9705. The first borehole was Lodygo==

wice IG 1 (S. Geroch, W. Nowak, 1 974), and the next one- Bystra IG 1 (K. Zytko, 1978).

In 1974-1976 borehole Suc ha IG 1 (A. Slqczka, 1976b), located in the eastern part of the

study area, was made. In the 19805 Petroleu m Drilling Co. continued exploration of the

S04 Z. Paul, W. Rylko. A. Toma~

discussed region. In the vicinity of Lac how ice several boreholes resulted in interesting (oil- or gas-bearing) outcomes associated wilh the basement of the Flysch Carp:llhians. In vest i- gations in this region are going on. A deep borehole Zawoja-I has provided interest ing data on stratigraphy of th e Ca rpathians and their basement Exploration drill ing in the region of 561 that had been stopped in the 1 9505 was resumed in the 19805 an d bore hole S61-8 was made.

GENERAL GEOLOGICAL CHARACfERISTICS OF THE STUDY AREA

The Precambrian-Palaeozoic platform deposits occur in the b<lsement of the weste rn part of the Polish Carpathians. They are capped by the Neogene mo lasse. Above these two structural siages there lies a third one - the Flysch Carpathians. The highest posit ion is occupied by the Quaternary cover.

PRECAMBRIAN BASEMENT

In the triangle of Cieszy n- Andrych6w-Zywiec, the oldest Precambrian deposi ts have been identified by boreholes: Punc6w-l, Ustron IG 3, Bielsko-4 and -5, Andrych6w-3 and -4, t...odygowice IG I, Bystra lG I and Lachowiec-2. In these borcholes, metamorphic rocks be longing to the lower part ofthc cpi-zone and to the meso-zone have been identified . The on ly exception is borehole Andrych6w-3 where igneous rocks represented by d ia llage-oli- vine gabros have been recorded.

PALAEOZOIC DEPOSITS

The oldest Pa l aeozoic depos its are the Cambrian rocks that have been pierced in vicinity of Kt;ty, Andrych6w and probably occur near Lachowice.

The Devonian and Carboniferous deposi ts have been idcntified by drilling in the northern pan o f the study area between Bielsko-Biala and Andryeh6w as well as in south eastern part, in the region of Lachowice.

NEOGENE DEPOSITS

The Precambrian-Palaeozoic baseme nt is capped by the Miocene molasses. Sometimes,

the Miocene sea, as shallow embayments, entered the Carpathians. There, the Neogene

sediments were depos ited. They are known as the Neogene deposits ovcrlying the Carpa-

thians. Based o n the papers by Z. Bula, D. J ura (1983) and W. Moryc (1989) it can be

assumed that between Cieszyn and the meridian of Sueha Beskidzka there occurs a complex

of the Miocene molasse of the maximum thickness over 2600 m. T hese :Ire the L ower

Miocene a nd Badcnian deposits. In Cieszynian Silesia, in the molassedcposits Z. Bula a nd

D. Jura ( 1 983) have distinguished the Zebrzydowiee Formation, Debowiec Format ion with

Za mar Member and the Skawina Fonn ation. In the region between Bielsko-B iala and the

meridian of Sucha Beskidzka, in the Lower Miocene deposits W. Morye (1989) has

Geological structure of the western

pan

of Cnrpalbians 505

distinguished three li thostratigraphic units: Z'lwoja, Sus and Stryszawa Formations. In the latter the Stachor6wka Conglomerate Member (A. ~I<liczka, 1976b) and 8ielsko-Biata Member occur. The Badenian deposits occurring here are

limited

only to the Lower Badenian. in a lithostratigraphic column of the Lower Badenian, W. Moryc has distin- guished (from below): the J ach6wka Formation, the

~bowiec

Formation and the Skawina Formation.

FLYSCH DEPOSITS Of THE CARPATIflANS

The Flysch Carpathians are made upof deposits oftheSkole, Sub-Silesian, Andrych6w Klippen, Dukla, Gryb6w and Magura units.

SKQLEUN

I

T

Deposits of the Skole unit occur in the northwestern pan of the study area, nonh of A

ndrych6w (Fig. I). To this unit L. Koszarski (1

985), K. :Zytko(1985) and K. Zytko et al.

(1988, 1989) include the Palaeogene-Neogene and Cretaceous(?) deposits of so-called outcr flysch that have been described by M. Ksiqikiewicz (1932, 1951). Opinions were expressed (M. Ksi1l.i:kiewicz,

1972; J. Golonka

etal., 1979) that the deposits of this area represent the Sub-Silcsian unit Here, there are (Tab. I) dark flinty Spas Shales; hard, white Zegocina Marls, Variegated Shales, grey sandstones and shales of the Inoceramian Beds (Pisarzowice Beds); dark marls and marly shales of the Frydek type with interca

lations of Szydlowiec.

Rybie and Gorzen Sandstones etc. Above these sandstones occur thick Variegated Shales alternated with thick-bedded

Ci~i:kowice

Sandstones and the Przybradze Beds deve

loped

as grey clayey shales with inserts of thin-

and

medium-bedded limy sandstones with g

lauconite. Theoverl

ying Menil ite Beds are made up of marls and cherts as well as of brown, almost

black, shales with insens

of thin-

and

thick-bedded glauconitic sandstones. The younges

t are the Krosno Beds which comprise mainly thin-bedded sandstones, often crustal

ones, alternated with marly grey shales.

SUB·SILESIAN UNIT

Sediments of the Sub-Silesian unit deposited from the Lower Cretaceous (Valanginian)

to

the Lower Miocene (Tab. I). The

lithostraligraphic

column of Ihe unit starlS with the

Cieszyn Shales developed as grey marly shales alternated with thin-bedded sandstones

overlain by the Grodziszcze Beds comprising conglomerales, shales and gaizes. Overlying

are the W

ierzowa Beds which differ from their normal development known from the Eastern

Carpathians. They are black shales with conglomerates and large exotic boulders occurring

in places. Thc Lgota Beds developed

as gaizes or grey shales with radiolarites at Ihe top

(Jasper Beds) occur above the Wierzowa Beds. They are in turn overlain by Variegated

Shales. usually green clayey shales alternated with hard, thin-bedded grey marls. Above the

Variegated Shales with marls there arc Wcgl6wka Marls developed here as soft rcd marls

a

lternated

with Variegated Shales. Sometimes, the

W~gl6wka

Marls arc replaced or

Ta bl c I Slntignpbic cb:>rt of (be werlcrn p:art of Ibe Polisb C:arp:r.lbi:ans

s<"'"

SUe-SILESIAN SILESIAN DUKlA GAVB6w MAGUAAUNIT

UNIT UNIT UNIT UNIT UNIT

w z

,

w

~ -- -- _---- ... - ,-

ShaIu MIll exorlcs

""'-"" - - - - -

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... _~-

w z ~-~ ""'-

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~ §

G",... . . .

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...- - ^....

^{r.I .... o8~}

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_ ....

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V.rle;aled

@ ^{-L :=}

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-

""~ VaMga'e<I

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t-- ""a

^V.t!egoleC

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""~

~

w Vllles!lled

- --

z "" .. _::1 I=-

w

8

Vslleg"'"

~ ^{L- "-}

^S/IaIe$ a n e l _

- ~

I----. /

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^{U!l!*' 1_ 9tds}

~ V ."" - ^,

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^, Uppo,GcxUa_

- ^{.,... ::: ;:;}

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^V~od SI>aIcI

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.... I 1-- -- -- -

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^...

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~ """"""" ... ^/ """""", ""

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^{- - - -}

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"""

Gcological structure of the western pari of Carpathians S07

interlayered with grey or black marls of the Frydek type. Within the grey marls there is a le nticular sandslOne horizon (Rybie, Szydlowiec, Oorzen Sandstones). Grey and black muscovite shal es, distinctly arenaceous, corresponding 10 the Upper lstebna Shales occur above the Wygl6wka Marls. Variegated Sha les rest on the Istebna Shales. In the region of Zywiec, within these shales, there is a compl ex of thin-bedded glauconitic sandstones (Radziechowy Sandstones). Directly above the lstebna Shales there are the Eocene Varie- gated Shales with Globigerina Marls a t the top. They are overtopped with the Menilite and Krosno Beds. The Menilite Beds are developed as clayey shales, sometimes flinty ones, with intercalations of thin-bedded sandstones or cherts, in places. The Krosno Beds are developcd as thin-bedded sandstones passing to grey shales. Sometimes the sandsto ne horizon is sedimentary reduced, and, then, grey shales rest directly on the Menilite Beds.

The Sub-5i1csian unit comprises mainly sha le-marly deposits with small amounts of thin-bedded sandstones. In the boreholes, they have been recognized under a large mass of the Silesian unit. In the northernmost part of the Carpathi ans they occur between Cieszyn and Andrych6w while in the southern part they are found between Dzi ygiel 6w, Ustron and Zywiec. Owing to lithology of the Sub-S ilesian unit and its location, described above, its profile is discontinuous and truncated, and certain members have often been squeezed

OUI

or scoured.

KLIPPEN UNIT

Deposits of the Klippen uni t occur in the region of And ryc h6w (Fig. I) and are represented by mylon ites, granitogne isses (locally), Oxfordian and Tithonian limeston es and various marls from the Campanian to Maastrichtian as well as by IimeslO nes from the Upper Palaeocene to Midd le Eocene. The deposits listed above have been describcd in details by, i.a. M. Ksi<lzkiewicz (1935, 1951, 1965,1968, 1972) and L. Koszarski (1985).

SILESIAN UNIT

Deposits of the Si lesian unit occur in the northern part of the study area and stretch as a wide belt between Cieszyn and Andrych6w region (Fig. I). The seri es is represented by sedimc ntary rocks (Tab. I) from the Upper Jurass ic (filhon ia n) 10 Palaeogene (Oligocene).

In the study area, the Si lesian unit has been subdivided into the Cieszyn sub-uni t and Godula sub-unit. The differentiating feature between the both is the development of the Upper Cretaceous deposits. The deposits of the Lower Cretaccous and Palaeogene are developed alike and their differentiation is insignificant.

The lithostratigraphic column of both the Cieszyn and Godula sub-units starts with the

Cieszyn Limestones. AI the base. these are pelitic, pelitic-detritallimeslones, a nd upwards

- detrital limestones with graded bedding and limy sandstones. Higher up there lie the

Cieszy n Shales. Le. dark grey shales with thin-bedded limy sandstones. Above the lattcr

occur extremely thi ck Grodziszcze Beds. They comprise sandsto nes which nre thi ck-bedded

and coarse-grai ned orconglomcrates with limy cement. Above these beds occur Wierzowa

Beds which are sometimes replaced by black shales with exotics. The overlying Lgola Beds

are developed in the Cieszyn sub-uni t as green and grey. spotty shales with thin-bedded

sandstones while in the Godula sub-unit, they are tri-partite. The lowcr member is formed

508 Z. Palll, W. Rylko. A. To~

by thick- and medium-bedded sandstones, the middJemcmbercomprises

11

shale-sandsto

ne

complex, and the upper member is represented by gaizes, the so-called Mikuszowice Cherts.

In the Cieszyn sub-unit, Variegated Shales with small amounts of

sandstones of

the Godula type rest above the Lgola Beds,

but th e Godula sub-unit is developed as sandstones. The Gociula Sandstones may be divided into three members: (I) thick-bedded sandstones, (2) medium- and thick-bedded sandstones. and (3) thin- and medium-bedded sandstones with

intercalations ofcong[omcrates, the so-called Malinowa Conglomerates. Unfortunately, the

above division into members seems to be inadequate, particularly in the Little Beskid Mts.

where fairly large complexes of grey shales and thin-bedded sandstones occur in

the

distinguished

horizons. In

the Cieszyn sub-unit tne Variegated Shales are overlain by the

Istebna Shales

and by a

rather

thin complex of the

Istebna Sandstones (known as

the

Pralkovice Beds in the Czech). In

the Godula sub-unit, the Upper Godula Beds with the Malinowa Conglomerates gradually pass to the sandstone-conglomerates

Lower

Istebna Beds. On the latter rest thin-bedded sandstones with shales and conglomerate sandstones of the Upper Istebna Beds

. These deposits are covered with the Upper Istebna Shales. In the

Palaeogene part of the lithostratigraphic column, the deposits of both units become

unified and comprise Variegated Shales with a packet of the thick-bedded coarse Ciezko-

wice Sandstones overlain by shales and thin-bedded sandstones of Hieroglyphic Beds, and above by the Menilite Beds with

brown shales, thin-bedded glauconiti

c sandstones and cherts as well as by

the

Krosno Beds developed as thick- and thin-beddcd sandsLOnes gradually passing towards the top

into thin-bedded sandstones and grey

marly shales.

SUBVULCANITES

The Lower Cretaceous Cieszyn volcanic association is related to the Neocomian deposits of the Silesian unit. These are vein intrusions (sills), extrusions differing

in

thickness and inserts of pyroclastic rocks. Their petrograp

hic composition is variable. Here

occur cieszynits (rarely with tuff and tuffites), picrites. monchignites and basalts. Some of these rocks have been changed by secondary processes.

DUKLA UNIT SENSU LA TO

Initially, th

e authors have distinguished deposits of the Dukla unit between Lekawica,

Gilowice and Slemien (Z. Paul, W. Rylko, 1995). However, subsequent field studi cs allow

to assume

that

these deposits occur also farther to the southwest, between Zywiec and

istebna, as well as

in the region of

Sopotnia (Fig.

I). In the lithostratigraphic column of the

d

iscussed unit

, which used to be considered the Fore-Magma unit, the authors distinguish

(at the surface) Variegated Marls and Shales developed as soft, red, lumpy marls alternated

with green or red shales. In this horizon

,

the thin-bedded glauconitic sandstones occur

sporadically. Above, there is a very thin (only a few metres thick) complex of black and

brown shales with thin-bedded glauconitic sandstones, being an equivalent of the Menilite

Beds in

other units.

The complex in

question is overlain by a complex of thi ck-bedded

muscovite sandstones of the Krosno Beds. A characteristic feature which differentiate them

from the Krosno Beds of the Silesian unit

is, for example. a higher diageneSis and thus

a

hi

gher hardness and more diverse lamination patterns. Above the thick-bedded sandstone

Geological suucturc oftl>c western part of Carpathians

""

complex there occur thin-bedded sandstones and grey shales of the Krosno Beds on which grey shales with exotics rest. The sha les in question are marly with very fine muscovite and with a large variety of exotic rocks.

GR

ys6w

UNIT SENSU LATO

The authors (Z. Pau l, W. Ry lko, 1 995) havedislinguished and described the deposits of the Gryb6w unit in the region ofRychwald-Ryehwaldek, Kamesznica, Istebna and Konia- k6w (Fig. I). In this region, the deposits of the Gryb6w unit used 10 be assigned to the Fore-Magura unit. However, the field studies allow to accept a hypothesis thai thc dcposils of the Gryb6w un it. as in the former case, occur farther southwest, between :lywiec and Poland's wes tern boundary in the reg ion of Istebna and Sopolnia. Yet in contrary to the Dukla un ii, the Gryb6w un it comprises mainly clayey-marly deposits. To the Gryb6w unit, the authors have also assigned the Lower Cretaceous Cieszyn Beds occurring at the sutface in the Sopotnia Mala region.

The lithostratigraphic column of the Gryb6w unit starts with the Cieszyn Beds compris- ing grey, marly shales and thin-bedded sandstones. These beds are sedimentary strongly red uced as it is the case with an the deposits of the Lower Cretaceous age. They resemble the depos its occurring in this unit in Ihe region of Nowy Sqcz where they arc called the Kur6w Cretaceous deposits. The GodulaBeds, normally occurring in the lithostratig raphic column above the deposits of the Lower Cretaceous, arc here substituted by Variegated Shales with marls. biotite beds (Inoceramian Beds) and biotite-feldspar beds. Above, thcre are grey and Variegated Marls and Variegated Shales with thick-bedded and coarse sandstones

ofCi~zkowice

type. A large diversity of grain sizes in these sandstones was the fundamental criterion to dis tinguish them as the Gr6jec Sandstones. These sandstoncs usua lly contain quartz grains differing in colours, fragments of magmatic and metamorphic rocks, and, in some beds, a very abundant fauna ma inly including nummulites and disco- cyclines.

Above, there are the Hieroglyphic Beds, called in this series the Rdzawka Beds or Kleczna Beds, and zoogenic Koniak6w Limestones (t.uzany Limestones) which are also found in Ihe overlying Variegated Shales up to the border with marls of the Barutka Beds.

In the Variegated Shales, besides limestones, thin-bedded limy sandstones, are also found overcrowded with large foramin ifera. Similar sandstone beds can also

be

observed in the Barutka Beds and in the Menilite Beds (Gryb6w Beds). Here, the Barutka Beds arc developed as hard grey or beige marls and as marly shales. They arc alternaled with thin-bedded muscovite sandstones. In th is horizon concretions or even beds of clay-iron- stone often occur. The discussed sequence corresponds to the Sub-Gryb6w Marls.

The Gryb6w-Menilite Beds are represented by brown, almost black, shales sporadica lly

alternated with muscovite-glauconitic sandstones and sometimes with conglomerates con-

taining large foraminifera. These deposits are overlain by a complex of the Krosno Beds

(Cergowa Beds) developed as grey marly shales, thin -bedded sandstones with singular

SIQ Z. Paul, W. Rylko, A. Toma§

layers of medium-bedded muscovite sandstones with large amounts of hieroglyphs both orga nic and mechanic ones.

MAGURAUNIT

A characteristic feature of the Magura unit is its facial differentiation in meridiona l direction that is particularly well expressed in the Palaeoge. ne deposits (Tab. I),

The problem of facial changes in the Magura un it has been dealt with by numerous geologists including. Based on the studies of the authors mentioned above, four facial zones can be distinguished in the Magura unit. Starting from the north these are: Siary, Racza, Bystrica (Sijcz) and Krynica sub-units.

The first three sub-units occur in the study area, The Ropianka Format ion with local members occurs in the lower (Cretaceous-Paleocene) part of the profile.in all these sub-units. The Eocene deposits in the Siary sub-unit (the Outer Racza unit according to W. Siko ra, K. Zytko, 1960) arc represented by Variegated Shales wi th intercalations of the

Ci~zkowice

Sandstones (Lower Eocene-Middle Eocene), capped by marly-shale-sandstone deposits of the Upper Eocene-Oligocene. Here, one distinguishes a thick-bedded complex of glauco nilic Magura Sa ndSlOne s underlain by marly-shales of the Sub-Mag ura Beds (Zembrzyce Beds) and overlain by the Supra-Magura Beds (Budz6w Beds). In the outer- mos t reg ions of the S iary sub-unit the complex of th ick -bedded sandstones often disappears.

The Racza sub-unit is typified by the Belowa Hierog lyphic Beds (the Middle Eocene), underl ain by Variegated Shales and overlain by a thick complex of the thick-bedded muscovite Magura Sandstone.

In the Byslrica sub-unit , in the Middle and panially Upper Eocene, there is a member of the marly or the marly-sandy t.qcko Beds underlain by the Lower Eocene Belowa Beds and by Variegated Shales. Theoverburden ofthet..qcko Beds consists of shales, marls, thin- and medium-bedded Sub-Magura Beds. The lithostratigraphic column ends with the thi ek- bedded, muscovite sandstones differing in thickness.

COMMENTS ON TECfONlCS

Three stru ctural stages can be distinguished in the study area. The lower stage consists of the Precambrian-Palaeozoic rocks of the subsided part of the platform which have been recognized in boreholes (La. PUllc6w- I, Ustrori IG 3, Andrych6w-2, lodygowice 1 0 J, BySlra 10 I, Sucha 10 I, Zawoja¥ I, Lachowice-l, ¥ 2, -3, -4, -7). The second stage comprises theNeoge nemolassesofthcAlpine trough recognized in the surface exposures and in many borehole profiles. The third, allochthonous zone comprises the Flysch Carpath ia ns

repre~

sented by the deposits of the Skole, Sub-Silesian and Klippen (Andrych6w Klippen), Si lesian, Dukl a, Gryb6w and Magura units (Fig. 2),

The platfonn deposits at the margin of the Carpathian overthrust (in the region of

Cieszyn- Bielsko-Biala-Andrych6w) are thick (often not pierced) Upper Carboniferous

rocks of the southe rn slope of the Upper Silesian Coal Basin beneath which the older

deposits gradually emerge southwards; these arc the Lower Carboniferous (Biclsko-2),

Upper Devonian (Bielsko-3), and middle Lower Devonian and presumably Cambrian

. - -ov~fhrusf of ~ Ftrsch CdrpJfhi:lns (1) ./ overthrust of the milin fecfrJni, units (3)

~ imbricilted fau/ding

!21

S-2 boreholes Bielsko !4J

Fig. 2. Geological CI"OS$-scction between Zlalna and Bielsko-Biala

I -eonsolid~led b:tsement; II - platform basement; 1lI - Neogene deposits; Flysch Carp~lhi~ns: IV - Middle Group: IVa - Sub-Silesian unit, IVb - Silesian unit (IVbl - Cieuyn Silesian sub-unit, IVln - Godula Silesian sub-unit), lYe - Dukla unit, IVd - GrybOw unit; V - Magura unit: Va - Siary sllb-unit. Vb-Racza sub-unit. Vc - Byslrica sub-unit

Przckr6j geologiczny ~dzy Zlatn~a Bie!skiem-BiaJ~

1- padIou skonsotidowane; 11- padiou platfonno-...-e: 1lI - utwory neogenu: Karpaty ms~owe: IV - grupa tredniajednostek: IVa - jednostka pod~h,ska, IVb- jednostka O~.(IVbI -podjcdnostka~llISkacieszytiska.lVb2 - podjednostka 'I~ka godulska), IVc- jednostkagrybowska. IVd - jednostbdukielska; V - jednostka magurita: Va - podjednostka Siar. Vb - podjednOSlka raczahska. Vc -podjednostka bysuzyeka

512 Z. Paul, W. Ry!ko, A. Toma$'

(Bielsko.,-4) deposits. South of the USlrOll- Bielsko-Biala

line crystalline basements repre-

sented by the so-called Ci eszyn plate ^(A. Kotas. 1982; N. Oszczypko et al., 1 989;

W. Potaryski

, P.

Karnkowski,

1

992) has been recognized by boreholes l.odygowice

IG I

and Bystra IG

1.

Based on the results of seismic studies. borehole Bystra IG 1 and magnetotelluric studies (W. Rytko, A. Toma§, 1995) one can presume that farther sou

th-

ward the border line of the Palaeozoic deposits is a longitudinal fault or a system of faults ofENE-WSW direction. This fault is recorded ca.

11

km south of borehole Lodygowice IG

I,

between

Pietrzykowice

and Lipowa. South of it the basement is down faulted by ca.

1 550 m.

The direct overburden of the Precambrian-Palaeozoic deposits is the molasse Miocene of the Carpathian Foredeep. The Miocene deposits at the Carpathian margin (Bielsko-Biala

region,

Andrych6w

region -

borehole

K~ty

8) were partially folded

together with the

Sub-Silesian unit (W. Nowak, 1959).

In

the remaining part of the Carpathian Foredeep (Cieszyn-Andrych6w region

),

as well as deep beneath the Carpathians, the Miocene is

undisturbed by folding, but, at most, cut by faults.

The Flysch Carpathians form a next

s

tructural elemen

t

and comprise: the Skole.

Sub-Silesian, Klippen, Silesian, Dukla, Gryb6w and Magura units. Accordi

ng

to M. Ksi<'l- zkiewicz (1972) the first six. units form the so-called Middle Group of flysch nappes.

Following the opinion of M. Ksiqzkiewicz the Middle Group might be considered a

huge

nappe from which stem secondary nappes (listed above).

SKOLEUNIT

Within the present-day framework (K. Zytko et a/., 1988, 1989), the Skole unit occ

urs

in the marginal part of the Carpathians, in the region of Andrych6w and in tectonic windows within the Sub-S

ilesian and Silesian units. In

the region of Andrych6w, to the Skole has been assigned, among others, the Palaeogene outer flysch. Following the opinions of K.

Zylko (

1

985) and L. Koszarski (1985), the Frydek succession might also be included to the Skole unit in

the discussed region. Here, the flysch deposits of the Upper Cretaceous and

Palaeocene arc developed

locally (e.g. Szydlowiec,

Rybie Beds etc.) and

show

a certai

n

simi larity to

the Ropianka Beds.

SUB-SILESIAN UNIT

Deposits of the Sub-Silesian unit occur at the surface as two or three disco

ntinuous

bands. During the Neogene the unit had been truncated and developed as doubled or even tripled sca

l

es (imbricated folds)

. The most external part of

the Sub-Silesian unit occurs at the front of the Carpathian overthrust as a band extendin g from Cieszyn to the region of Andryc

h6w (Fig. I). The more internal parts of

the unit are recorded in the Dzi!;giel6w and Ustron windows. and the innermost, southern part is found at the front of the Dukla, Gryb6w and Magura

units

and appears at the surface in the Zywiec

tectonic window. There, it is present as

intensely folded NE sca les. The middle eleme nt of the Sub-Silesian unit might be assoc

iated

with the extension of the Lanckorona- Zegocina zone towards the west.

The southern band of the Sub-Silesian unit stretches in the southern part of

the Silesian

unit. The Sub-Silesia

n unit has been best recognized in theZywiec tectonic window. There,

Geological $truclurc of the western part of Carpathians

513

the Valanginian Ihrough Oligocene

(1.

Burtan, 1 96&1) depos its occur. They are intensely folded and arranged in scales trendin g north-south. In genera!, the Sub-Silesian unit is tectonically compressed and defonned very strongly owing to its lithology (mai nl y marly and shaly rocks).

KL.tPPEN UNIT

Oneofthe most interesting features in the Western Beskids is the occurrence of isolated klippen in the region of Andrych6w. According to M. Ksit\zkiewic1. (1972) the klippen occ ur up on the deposits of the Sub-Silesian unit, at the base of the Silesian unit. He claimed that such a position showed that the Silesian unit, while thrusting north towards, encountered a ridge built of crystalline and Jurassic rocks, covered with the Senonian and Palaeogene deposits. One should assume that the ridge could have been a fragment of a cordillera separating the Sub-Silesian basin from the Silesian one. L. Koszarski (1990) sugges ts th at the klippen arc olistostrome. The latter originated either from a cordillera separa ting the Sub-Si lesian unit from the Skole unit or from the margin of the Carpathian geosyncline lying farther to the nonh.

SILESIAN UNIT

Owing to the development of the Godula Member and to dishannonic folding, the Si lesian un it divided into two tectonic sub-units: the [owerone - Cieszyn sub-unit (nappe), and the upper - Godula sub-unit (nappe) (ef M. Ksi<lzkiewicz, 1972). Detachment whic h lead to separation of the Godula unit as a separate entity took place within the upperC ieszyn Shales or slightly higher.

The Cieszyn Silesia n sub-unit occurs mainly between the Olu and Sola rivers, and its smaller fragments have been found in the western, southern and southeastern margin of the :Zywiec window. Moreover, the isolated tecLOniccaps resting on the Sub-Silesian unit, have bee n spotted in several locations in the Zywiec Basin (Fig. I). The authors presume that in the western and southwestern part of the Zywiec window there are two partial Cieszyn sub-units: the 1 0werCieszyn sub-unit and the upper one. The lower unit (at the contact wi th the Sub-Si lesian unit of the Zywiec window) is located more to the east, the upper unit reSIS on th e lower one in thecontaci zone with the Godula Silesian sub-unit oftheSi lcsian Beskid block. The discussed sub-uni ts oceur as intensely disturbed scales. The lower Cieszyn sub-un it is built of Lower and Uppcr Creltlceous deposits. In this sub-unit, within the Cieszyn-Grodz iszcze Beds, the presence of the Lower Callovian olistolite of the detrital limestone (klippen from Wna) has been stated. The upper Cieszyn sub-unit is built of the deposits rang ing in age from the Uppcr (or Lower) Cretaceous to the Palaeogene.

Following the approach of M. Ksi;p:kiewicz ( 1 972), the Godula Silesian sub-unit is

clearly de limited from its foreland. The transverse, NW-5E faults divide this sub-unit into

three blocks: lablonkovsky Beskid (in the Czech), Silesian Beskid and Little Beskid

(Fig. I). The Si lesian Beskid block forms a four-sided body whose northern and eastern

margins are uplifted. From the south the Dukla, Gryb6w and Magura units are thrust over

the block. From th e west the Jablonkovsky Beskid is thrust over the Si lesian Beskid.

"4

^Z. Paul, W. Ry!k.o. A. Torn:lt

The Silesian Beskid block

is dissected by

several transverse faults with downthrown eastern sides. Along the eastern margin of the block there is a great NNW-SSE fault which separates the Silesian Bcskid block from

the

Litlle Beskid block (Fig. 1). The blocks in question were displaced along the fault line and rotated. In the northern part orlhe fault the older members of the Silesian Beskid block arc in contact with the Krosno Beds of the Little Beskid block (Fig. I). Thus, the Little Bcskid block is downlhrown with respect to the Silesian Beskid block

. Farther south, along the same fault,

the Cretaceous members of the Silesian Beskid block arc in contact with the deposits of the Cieszyn sub-un

it and of the

Sub-Silcsian unit in the Zywiec window (Fig. I). There, the arrangement is reverse, the block of the Silesian Beskid is downthrown and the area of the :lywicc tectonic window is uplifted. The discussed fault is then a pivotal fault (eJ M. Ksi'likiewicz, 1972).

The Little Beskid block (Fig.

I) is a monocline dipping southward. In this direction, the

younger and younger members of the Godula Series, including the Palaeogene members, appear at the surface. Within the discussed block there are also larger transverse N-S faults.

Particularly important is the fault zone along the Sola river that, in the southern part, forms

the eastern border of the Zywiec lectonic window.

DUKLA UNIT SENSU UtTO

The Dukla unit has been distinguished by Z. Paul and W. Rylko (1995) between Slemicri and Istebna. In the eastern part, between Slemieti and Zywiec, the Dukla unit is thrust over the deposi

tsoftheSilcsian unitoftheLittle Beskid block. In thesoulhern part of the Zywiec

Basin the d

iscussed unit together with the deposits of

the upper, Gryb6w unit is thrust over the Cieszyn Silesian sub-unit. South of Barania G6ra MI., the Dukla unit is

thrust over the

deposits of the Silesian Beskid (Fig. I).

The Dukla unit occurring at the surface is represented here by a thick complex o

f the

Palaeogene depos

its. Thickdeposits

of the Krosno Beds predominate.

!

n borehole BystraJG I (K. Zylko,

1

978), at the depth of 2240--2890 m, there is a complex of the Krosno Beds classified by A. Tokarski (1947), K. Zytko (1978), as so-called lurasz6w scale whic

h, in

tum, belongs to the Godula Silesian sub-unit. In our opinion, the discussed complex might represent the Duk

la unit (Fig. 2) that is in agreement with thl.':

views orK. Zytko (19600, b) and

R. Vnrog (1969) who have assigned the Jurasz6w scale to the Sub-Magura unit.

Deposits of the Dukla

unit are likely to occur in the Sopotnia Mala

tectonic window where the discussed unit is represented by thl.': Krosno Beds. Farther to the south, the deposits of the DukIa uni

t detected in

the logs of the boreholes in vicinity of S61 occur under the overthrust of the G

ryb6w and Magura units.

GRys6w UNIT SENSU UlTO

The authors of this paper distinguish the deposits of the Gryb6w unit be

tween Gilowice

and Istebna region. The unit is mainly formed by the clayey-marly deposits of

the Lower

Cretaceous-Palaeogene age. Owing to the character of the deposits, the unit was strongly

compressed, scaled and crushed between the Dukla and the Magura units. In exposures, the

Gryb6w unit takes a fonn of isolated scales and tectonic caps resting on the deposits of the

Geological struClllro orthc WCSlcm part or Carpathi:ms

'"

Dukla and Silesian units (Fig.

I).

Moreover, it has been identified in numerous tectonic windows within in the Magura unit, e.g., in Rychwatd and Sopotnia Mala.

MAGURA UNIT

The Magura unit is the hig hest unit in the discussed region (Fig. I). As it has been emphasized in the section on stratigraphy, three facia l zones with defi ned stratigraphic profiles might be distinguished in Polish territories: Siary, Racza and Bystrica zones. As results from the detailed studies by J. Burtan, S. Sokolowski (1956), W. Sikora, K. Zytko (l960),1. Golonka, A. W6jcik (1978). W. Rylko eeaL (1992, 1993), W. Rylko (1992, 1 994) the contacts between the listed zones are tectonic. Following the approach of W. Sikora, K . Zylko (1960) and

L.

Koszarski et aL ( 1 974), three sub-units might be d istinguished.

The northernmost is Siary sub-unit (unit A according 10 W. S ikora, K. Zylko, 1960).

The Magura unit, or speaking more precisely. the deposits of the Siary sub-unit are thrusted over th e units of the Middle Group. An abruptly increasing width of the Siary sub-u nit towards north-cast is a striking feature. In the region ofMil6wka it reaches about 5 km while farther NE, in the region of Sopotnia Mala - ca. 6 lan, and finally ncar Zywiec-Jele§nia line - even I

!

km.

The Racza sub-unit thrusting over the Siary sub-unit is located more to the south. Near S61 . the line of thrusting is latitudinal while farther to the east it takes a SW-NE direction and then ncar Sopotnia regions its primary orientation. East of Zywiec-Jelclnia line the overthrust is again SW-NEoriented. The analysis of the width of the Siary sub-unit and of the geometrical patte rn of the overthrust of the Racza sub-unit indicate that the thrusting of the laller on the Siary sub-unit is 4.5 Ian at ZwardOll-Mil6wka line, ca. 5.5 Ion at Mil6w·

ka-5opotnia line and ca. 1 0 km at MiI6wka- lele§nia line.

The Bystrica sub-unit thrusts over the Racza sub-unit. In the region of Wi elk a Racza- Rycerzowa Wielka, the Bystrica sub-unit is tectonically depressed when compared with its eastern part. From the region ofSobI6wka- Ujsoly, the sub-unit is tectonically uplifted.

~his

uplift continues to the cast towards the region of Mutne in Slovak Ora va. In the discussed region. the northern border of the uplifted Bystrica sub-unit runs to the south ofPilsko Mt.

Farther to the eas t, the Bystrica sub-unit appears (in Poland) ncar Glinne Pass and runs to the north (region of KorbieI6w). East of Korbiel6w the line of its overthrust follows latitudinally and between Beskid and Jaworzy na MIS. enters again Slovakia. O n the eastern slopes of Jaworzyna Mt. the uplifted Bystriea sub-unit is cut off by a large transverse (NW-SW) fault along lele§n ia-G lucha- Oravska Polhora line. In the NE side of this fault the deposits of the Bystrica sub-unit are displaced south-east by ca. 8 km, towards the region located north-cast of RabCice. Here the front of the Bystrica sub-unit is SW-NE oriented and the sub-unit runs towards lhe Polish boundary to the region located south ofBabia G6ra Ml.

Odd1.ial Karp~cJd

Pruistwowcgo rnS!~lutu Gco[ogicznego Krakow. ul. Sknat6w r

Received: 9.06.1996

TrulISlufed by Tere5a Mrozek

'16

^{Z Paul, W}. Rylko. A. Torna§

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OLSZEWSKA B. (1981) _ On some assemblages of small fomminifers oflhe window series ofSopoinia Mala, MS7.ano Onlna. S=WD and Klc:c'Lally (in Polish with English summary). Biut. InSI. G001" 331, p. 141-162.

OSZCZYPKO N., TOMAS A, (1985)- Tectonieevolution or margin:l\ part of the Polish Flysch Carpathians in the Middlc Miocene. Kwart. Gco!., 29, p. 109-12g, no. I.

OSz.c-L:YPKON., ZAJI\C R .. GARLICKA I., MENCIK E .. DVOAKJ., MA TElOVSKA O. (1989)- Genlogical map of the substrlllum of the Westcrn OuterCarpalhians and their foreland. In: Geological otlas of Ihc Weslcrn Outer Carpathians and their foreland. Pwlstw. Inst. Geol. W;:US7.awa.

PAUL Z, RYt.KO W. (l995) - Problemjcdnostek grupy ~redniej no poIudniowym 7.apleczu Beskidu Malego.

Posicdl.. Nauk. Pmlstw.lnst. Geo!., 51(3), p. 86-87.

PAULZ., RYt.KO

w ..

TOMAS A. (1996)- Wptyw tektoniki skonsolidowanego podlota Krupa! na rozkfocl mas fliszowyeh w polskiej ~ci Karpat Zaehodnieh. Pn. Gcol" 44. p. 489-494. no. 5.

POZARYSKI W., KARNKOWSKI P. (1m) - Mapa tekloniczna Polski wepoce waryscyjskicj I: I 000 000.

Pwlstw.lnst. Geol. Warszawa.

RYt.KO W. (1992) - Litostratigruphy of Maguro-nappc sediments in tile soulh-easl pari ofthc Bcskid Zywiceki Mts (Extcrnal Carpathians) (in Polish with EngliSh sUIl1/Tl;ll)'). Biul. Pans!w. [1151. Geo!., 368, p. 37-64.

RYLKO w. (1994) - The tcctoniC$ oflhe Maguro unit in the south.eastem part of Ikskid Zywiecki (the Outer Carpathians) (in Polish with English summary). 8iul. Paristw. Insl. Geot., 369, p. 31-48.

RYt.KO W., PAUL Z. (1994) - Mapa GcologicV1a Polski 1;200000, ark. Cics7.yn (B - Mapo Bcz Utwor6w Czwurton:r:<Iowych). P:mStw. Inst. Geol. Wmozawa.

RYLKO W., TOMAS A. (1995) - Morphology of the consolidated basement of the Polish Carpathians in the light ofmagnclolel1urie do."l\o. Goo!. Quart" 39, p. 1-16, no. I.

RYt.KO W., ZYTKO K., RI\CZKOWSKI W. (1992)-Obj~nieniadoS1:czeg6lowej Mapy Geologicznej Polski 1 :50 000, ark. C1,.3dea-Ujsoly. p:mstw. Inst. Gcol. Warszawa.

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SIKORA W., ZYTKO K. (1956)- Stlllligraphy oflhe Magurascries in the Wysoki Bcskid (High 8cskid) on the ZywiC1: sheet (in Polish with English summary). Pn:. Geol" 4, p. 469-471, no. 10.

SIKORA W., ZYTKO K. (1960)- Geologyofthc Bcskid Wysoki RangcsouthofZywicc (WC$tCln Carpathians) (in Polish with English summ:uy). Biut. Inst. Gent., 141. p. 61-204.

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J -n .

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ZYlKO K. (1978)- Profil orworu badawC2.Cgo Syslr.J. [G -I (Karp;styZachodnie). Kwart. Geo!., 22, p. 943-945, no. 4.

ZYTKO K. (1985) - Some problems of ageodynamic model of the Nonhem Qupnthians. Kwilrt. Geo!.. 29, p.

85-108, no. I.

ZYTKO K. cd. (1966a) - Szc«g6towa Mapa Gcologiczna Polski (bet utworow etwartoncdbwych) 1:50000, Region Karpat i Pnedg6rza, Zeszyt I. Inst. Geo!. Warszawa.

ZYTKO K. cd. (1966b) ~ Szczeg6l0wa Mapa Geologiezna Polski (bel. utwonlw czwartom,dowych) 1:50000, Region Karpat i Pn:edg6n:a, Zeszyl2. Inst. Gcol, Wa!Szawa.

SI' ^{Z. Paul, W. Rytko, A. TorrW}

iYTKQ K. (under colillbor.uion) ZAJAC R" GUC!K So, compiled by; RYt.KO W" OSZCZ¥PKO N., GAR·

UCKA I., NEMCOK 1.. ELIAS M" MEN-elK [i., DVORAK S., STRANIK Z. O. (1988) - Map ortcc[nnie clements oflhe Western OUlcrCnrpolhi:ms and their foreland without Quaternary fonualions. In: Gcological Atlas ortlle Western Outer Carpalhians and their foreland. Pru'istw. Insl. Geol. Wars1.llWa.

ZYTKO K., GUCIK S., RYLKO W., OSZCZYPKO N .. ZAJ.A,C R.o GARLICKA l.. NEMCOK J., ELIAS M., MEN(':IK 11. DVORAKJ., STRANIKZ., RAKUS M., MATtJOVSKA O. (1989)- Gcological mapoflile Western Outer Carpathians and their foreland without Qu~tcmary formmions. In: Geologicnl IIllas of the Western OutcrCarpalhinns and their foreland. Pafistw. Inst. Geol. Warszawa.

Zbignicw PAUL, Wojciech RYLKO. Adam TOMAS

BUDOWA GEOLQGICZNA ZACHODN1EJ CZ"~Cl KARPA T rOLSKICH

Slres:t.czenie

Omawiany len:n leiy rni~dzy CieS7.ynem a poludnikicm Suchej Be~l:idzkiej. Granic~ =hodniq i poludniowil sumowi gmniea pmislw;). l'od Wlgh.dem gCQmorFQlogic7.nym wi~l:s~ obsznru 10 Karpaly zewn.;tnnc. P61noena i p6lnocno-1.Dchodnia clJW§~ Icrenu naldy do kOllin podkarpackich. Karp"ly w Qmawinnym rejonic d1jel:j sie na Bcskidy i Pog6r7.e.

W ySlepujiltu prel:ambryjskQ-palcoznicznc III wory platfonnowe, sitnie 1.aangatowane teklonicznie. pnykfyte molosowymi IIlworami neogerlskimi. Poludniowll Cl~~ terenu zajmuj;! Karpaly niszowc. W Qbn;bie Karpa!

wyr6tniono i opisano jednostki grupy ~redniej (skolskq, pod~l;jSkll, skalkowq, ~1'lSkq, dukielskll i grybowskll) omz jednOSlkc magursl:4, w kt6n:j wydziclono i scharnk\eryzowano podjcdnostki: Siar. rac~nskq i bystnyckq.

Budowa doJnych piCler pl7.cdslawiona zostala w og6lnym 1.arySie. Sl.erzej JlQ!r.lklOwano slmtygmfic i Icktonikc pietro m$ZOwcgQ. Karpaly fliszowc budlljll utwory jednOSlki skolskiej, pod~lljSkiej, skalek alllJrycho- wskich. jednostki ~lljSkiej, dukielskicj i grybowskicj .rellSlI 1(1111 oraz magur!i.kiej. Stmtygrofle opisanych serii w skondcnsowancj fomlie pr/.edslawia lab. I.

Jednostkaskolska wystepuje w brm'.I1cj czck:i Karpat w rejonic Andrychowa ora~ w oknach lc.klonicll1ych jcdnoslki pod~l:&Skiej i ~tilskiej. \II rc:jonie Andrychowa zalic-mno do niej m.in. palcogcrlski Ilis1.1.cwn~tnny_

Utwory jcdnostki pO<Ulqskicj wysl~puj~ nn powicrl.chni w fonnie dw6ch lub lrloL-ch nicci~glych pas6w. W

na.~ic ocogcnsldej prt.ebudowy Icgo Ohs7.aTU nasl~pilo jcj zerwanie i podwojcnic tub nawel potrojenie. N::Ijb~rdziej 7.ewn~ln:na cz¢C jednostki pod~J(lSkicj znnjdujc si~ U czotn ntlSuniccia karpackicgo w poslaci pas:! bicgn'ICCgo od okoJic Cieszyna po rejon Andrychown. Banbiej wcwn~tn.najej czl;!<:jcsl n:jcstrnwana w oknach D7j~gielowa i USlronia, a najbardldcj wcwnctrzna, potudniowa.. 7.11a1u"lla ~i~ II cwln jednnslck dukiclskiej, grybowskicj i mngur!i.kiej. Srodkowy e1cmenljednostki pod~lllskicj rnot.l1n wiq~ ~ pned!ureniem na UlCh6d strery lnnckornn- sko-1.egncinskicj.

Jednostka ~Iqskll, dzicki rnzwojowi ogniwa godulskiego i dyshalmonijoclIJu sfaldownniu sic, :u6inicowala si~ na dwa clcmcnty IckIOnic"LOC: dolny - podjcdnOSlk.; (plOS7.nowinc) cit:.SZynskq om~ g6my - podjcdnOSlkc (plaS1.C7.owin~) godulsk~. Odklucic. kl60: doprowaclzito dQ usumoduelnicniu si~ jcdnostki gotlulskiej. odbylo si~

ulbo w obn;bie g6mych lupk6w ciCS7.yrlskich, a1bo niceo wyfej.

JcdnG.'ilk~ dukie/skl! umu lata wyr6tniono micdzy Slcmicnicrn a Istebn". W c7.¢~ci wschodnicj. mi,.dzy Slcmicnicm a Zywcemjcdnoslka la ntlSuwa si~ nn ulwory jednostki Jl~skicj bloku Bcskidll Malogo. natorniast w poludninwcj C"~ci KOltiny Zywieckicj, wraz z ulworami wy"lszejjednOSlki - grybowskicj. najednOSlk,. tlqska cieszy(isk~. Na poludnie od Baranicj G6ry jcdnostb dukidska nasuniClajesl na Iltwory bloku Beskidu Sl~kicgo.

Jcdnostka dukiclskll, wyst~pujllca na powier~chni,je.sl rcpn:zen\owana pn:ez mill~.szy kompleks IllworOw palco- gcnu. Dominujll w nim dutej mil\l.Sz.o§ci ulwory w3rslw kro§nierlskich.

Utwory jcdnostki grybowskicj UIISU la/a wydzidollQ mil,ldzy Gilowicami a rcjoncm [stcbncj. Zbudowana jcsi w pr/.ewadzc ~ utwordw ilaslo-margHstych dolnokrcdowo-pnlcogetlskich. Zc wzgl~du n:r. char.r.k.tcr osad6w jcdnOSlka tazostalasHnie sprasowana, zillskowana i rnl1arta mi~dzy jcdnostk.qdukicJsk" i magursk". W odstonie- cinch powier/.l1iowych wysl~pujc OIla w Fomlie i7.otowanych lusck i C7.apek Icklollicznych le1..ljcych na ulwor.JCh

GCQlogiCliI structure of the western part of CnrpathiDIIs

'I'

jcdnostki dukielskiej i gl~kiej. Stwierdzono j:j rowniet w 1ic7.nych oknach tektonicznych w obro:blc jednostki rnagurskiej, "P, II' Rychwald~ie j w SopOlni Male;,

Jednostka rnllgurska jest najwyu,ZQ jednoslkll ornawianego rejonu. Roulziela s~ ona nil Iny podjcdnostki.

Najbard1jej p6lnocn~jest podjednOSlka Siar, kl6ra nasuwa si~ no.jednostki grupy j~niej. W przebiegu podjed·

nostki SiM udena ttybki wzrost szcrokojci lej strefy II' kicrunku SW i NE. Analiu s7.eroko~d podjednoSlki Siar i geomeltyC7.nego obnlZU linii nasuni~a podjednoslki mc:trulskiej wskazuje, te nasuniccie lej OSlalniej nil strefc Siar wynosi na linii Zwardoft-Mil6wko. okolo 4,5 km. nil linii Mil6wka-Sopotnia okolo 5,5 km, a na linii Mil6wka-Jeletnia nawct okolo 10 km. Najbardziej poludniowll podjednostlq, osl:llnill w granicach panstwa,jest podjednostlm bystrzycl::a nasuwaj~1I sic nil podjcdllOstk(: r.te;m,iskll. W rejooie Wielkkj Rac-q-Ryccnowcj Wielkicj podjednostka bystnycka jest obni1.ona leklonicznie w slosunku do czeki wschodnicj. Od rejonu Sob16wki-Ujsol6w rozpoc-tyna si~ jcj ICklOniC7.1lC wyniesienic. kt6re kontynuujc si~ ku wschodowi po rejon Mulncgo na Slowaclcicj Orawlc.