Analysis of the fault pattern in selected areas of the Polish Outer Carpathians

Geological Quaterly, 1998, 42(3): 263-276

Analysis of the fault pattern in selected areas of the Polish Outer Carpathians

Leonard MASTELLA,

Ewa SZYNKARUK

MMtella L., SzynklLnlk E. (1998) - Analysis of the f:luil pntlCTn in selecled ^IIl'ea5 of the Polish OUler Carpathians. GeoL QU:ltt., 42 (3):

263-276. WlU'Sz.:Iwa.

Fault pallcm was studied in seledcd areas o( the Polish Outer Carpathians. 'The $Iudy was based on the author's own rn:!pping data, I1Idar irl'\aiCS and the Gtolog;col Map of Poland 1:200 000. A dense and regulill' fault pattem is p~nt in nil the studied areas. II consists of two seu off:luhs dipgonal to the strike of the m:lin tectonic structures, DR lIIld Dt.. and P SC( of less common tl1lllSVCfSC faults T. The azimuths of the set T (pulll c:om:spond approxilTl3lely 10 the azimuths of the 01 axis orthe

Da

and

Dt..

system. The azimuths change accordingly 10 the bending orthe CatpathilUllU'C, from ca. 40' in the ^east to ca. 175' in the west. All the fault sets dissect the I'Cgjonai structures and their overthrust plllnC$, which indicalcs IMllne

faullS

formed aller folding and overthrustin. oflhe nllPPCS.

Ltonard MrIS/tll(1, £W(] Sr,yttkor"t 'fJ.S/;lJllt oJGtology, Unil'tniry of Warsow, tw/rki; Wig"/)' 93, 02~ WarSlQwo, Pofami (nctwtd:

26.02.1998: au tpltd: 8.07. 1998).

Key words: C:up:ilhi:lns, conjugate bull sets. faults, f:lult p:lUtnl, photoinlCrpretnlion, r:tdarimages, lectonial.

INTRODUCTION

This study presents an analysis of

the fault

pattern

in

selected areas of

the Polish Outer Carpalhians (Fig. IA). The

fault pattern was studied in the following areas: the eastern part of the Fore-Dukla unit, tectonic windows of Mszana Dolna and Swilltkowa, Silesian nappe

ncar Solina, between

the rivers Skawa and Dunajec and nearZywicc (Fig. 1

B). The

ana

lysis was based on:

-

author's own fie

ld

studies documented at the scale of I: 10 000 and supplemented wi

lh geological interpretation of

air photos at approx

imate scales of 1:17 000 and

1:50000;

- geological interpretation of radar

images at approxi-

male scale of

I: 100000;

- analysis of Geological

Map of Poland 1

:200 000 (sheets laslo, Nowy S"ez, Bielsko-Biala; Fig.

18)

The study was

a part of the projects KBN No. 60099101 and 8W. I

384/10 (bolh led by Doc. Dr. hab. Leonard Mastel·

la).

METHODS

Diverse me

thods were applied. Classical methods of geo-

logical mapping were used in the

field

work, together with structura

l analysis made according to the general suggestions

presenled by W. Jaroszewski (

1

972) and L. Mastella (1988).

The

methods of interpretation of air photos, including the radar ones, was based on the works by

A.

Pszcz6lkowski (

1968), S. Dokt6r, M.

Granicz

ny (1982), M. Graniczny et al.

(1989)

,

S. Ostaficzuk (1978), P. Vergely.

H.

Zadeh-Kabir (1988), D. J

. Sanderson et 01. (1991). Especially useful

were the radar images at a scale 1:100 000 and resolution of ca. 30

m

(S. Dokt6r,

M.

Graniczny,

1982). The masking effect of

vegetation is partly removed on these images (S. Dokt6r, M.

Graniczny, 1 982; P. Vergely, H. Zadeh.Kabir, 1 988; M. Gra-

niczny et 01.,

1989) and Ihe low angle of incidence of

the radar

beam (S. Dokt6r, M. Graniczny,

1 982; M. Graniczny

et aI., 1989) increases the legibility of linear geological elements,

'64

Leonard MaslelJa. EWI Stynkasuk

B

, ,

Materials used in the study:

W

^{M~se'IC 1:2}

0

^Miocene of Carpathian Foredeep ^5tn.ta

r - -

D

I

1

^I Radar pMtognlpM S iluian n.ppe

--"

0

, . ... . ,

. I . "'"" ... D

^{Other 1}e<;lonic Llnits

\

. . . . .

^:

Fig. lAo Gcnerallocotion oflhe study an:a B. Location of the 1m:a5 of detailed invcstigotions

Loka.lizacja obsuru badad

B. Schemat rozmienczenia odcink6w badlwa:ych

includ ing faults (M. Graniczny

ttl

ai., 1989). The direction of

flight

was

parallel to the regional structural strike, so the

legibility of the faults oblique and nonnal to this direction

increased markedly.

The faults oblique and normal to the structural strike were analyzed, as longitudinal faults are indistinguishable from thrusts on air photographs. The analysis included the faults

which were directly mapped in the field, distinguished

^by interpretation of air photos and marked on existing geological maps. The faults manifest themselves in eJCposures by the presence of zones of breccia and cataclasites. folded shales and broken sandstone

beds.

The nature of these faults was established using folds (PI. I. Fig.

to),

fault drag (pl.

n.

^Fig.

II), slickensides. en echelon arrangement of faults and shears within the zones of breccia (pI. n. Fig. 12).

Fault positions were established by photointerpretation where zones of breccia and cataclasites extended on valley slopes as narrow and often dry gullies. and where they were marked on hill crests as steps, gaps or small shifts in ridge axes (see L. Mastella, 1975; L. Mastella tr 01., 1996; L. Mastella, J. Rubinkiewicz, 1998). The interpretation of faults on the radar photos and geological maps involved analysis of their surface traces, their tn uhelon patterns and the displacement of rock series along them - all using the methods tested earlier in the Polish part of the Carpathians (L. Mastella, 1975,

1988; A. Konon, 1996. 1997; J. Rubinkiewicz, 1996).

The fault pattern was represented as (depending on its complexity-seeS. Dokt6r, M.Granicl-n)" 1982; p, Vergel)"

H. Zadeh·Kabir, 1988; D. J. Sanderson et of., 1991): sche-

malic maps based mainly on field studies. directly on the radar images or on maps drawn from them. In a few cases the paHerns are illustrated by rose diagrams only.

Fault azimuths were measured to the nearest I·. Rose diagrams were drawn by grouping measurements into 5·

classes, each representing the sum of the lengths of faults within the azimuth class and shown as percent of the total length of all faults in the area. Azimuth of the centre of each class was then used forcaJculation.

The fauits of the diagonal sets in the whole studied area are mostly right-Iateral-DR (PI. I, Fig. 11) and left·lateral - DL (pI. I, Fig. 10; PI. D. Fig. 12) strike--slip faults, in many cases reactivated as dip-slip faults. Mutual geometrical rela- tionships of the two sets, namely the offsets of some faults along the others and mutual terminations of some faults on the others, as seen in exposures (L. Mastella, 1988) and air photos (S. Dokt6r, M. Graniczny, 1982; L. Masteila, 1988; P. Verge·

Iy, H. Zadeh·Kabir, 1988; D. J. Sanderson etal .• 1991) indi- cate that a large part of the faults were synchronous (during the strike--slip phase ofthe;r development). In such a situation (W. Jaroszewski, 1980) the acute angle between the two sets is twice the shearing angle 29 and it is usually close to 60·

(op. cir, J. Handin et 01., 1963). It can

be

said of such faults (G. Mandl, 1988;T. Engelder, 1989; R. Dadlez, W. Jaroszew·

ski, 1994) that they were fonned in a triaxial field of stresses.

In that case, accoming to the general rules (R. Oadlez, W.

Jaroszewski, 1994), the bisector of the acute angle between the surfaces of faults from both sets was used to detennine the axis of main stress 0"\. The 0"2 direction is detennined by the

Analysis of the fault o(!hc Polish OutcrCarpathians 265

B 00\ ^{/ t}

C<' 1t ^{h M. A} 7 ^URA

~< ^/

\ '\ \,!w;.~ ^,

/ /

0 2 4km

,

/ '

^{/ '}

DUoT-<..q

Legcnd:

~t

. . . 2

0 2 4km

, , ,

Fig. 2A. Faull patlcrn in the Fore-Dukla unit and ils margin between Bnligr6d and Ustrtyki GOrne with rose diagrams of (pulIS in ilS weslem (I), centrol (2) and ea.stern (3) partS and in the Centro/ Carpathian Depn:.ssion (I) and in the Dutla nappe (10 (allcr L Maslcllll, 1995)

I -faullscparotinB the CentruJ ClrpatlUan Depression (uplhrown side) from the Fore-Dukla unit (downthrown side). amlW1 ,bow the direction of dip; 2 - overthrust orthe Dutla unil; the mdius of!hc rose diagrams ~ponds 10 15'110 oflhe totallcngth of fpults in the area represented by the diagrun B. Fault pallcm in the Swilllkowa Ic<:tonie window with I rose diagram o( (aull directions (after L MastcJla and J. Rubinkiewiez, 1998)

The radius of the rose di.a&nms eorresponds 10 20%

Sicf uskokowa w jcdnoslce pn.eddulttclsltiej i jej obtamownnill miedzy Bnligrodem I USlnykami G6mymi z !'OUtami kienmk6w IIskokow w jcj c~i l':lIChodnicj (I), tmdkowcj (2) i wschodniej (3) oral': w ccnlralnej deprtsji kllTpaekiej (I) i p/asttwwinie dukielskiej (II) (wed/ug L Mnstelli, 1995)

1 _ dyslokacja odd;cielaj~n ccntralnll depresj~ karpack~ (sknydlo wiWlCC) od jednoslki przeddukie[skicJ (sknydlo znueone), sln..aIki w5kazujll kierunek upadu; 2 - nllSUnil;Ciejcdnostki dukielsktcj; promiCl\ kola rozet r6wna siQ 15'1> og6lnej dlugoki uskok6w na obszarze, 1. kl6mgo wykonano rowe B. Sief uskokowa w oknie 1clr:loniC1llym Swilllkowej 'Z rozclll ktcrunkow uskok6w (wedluB L Mastelli i J. Rubinkiewieu., 1998)

Promicli kola rout r6wna 5j~ 20'1>

direction oflhe intersection line of the planes of the two fault

sets, and the

0')

is perpendicu

lar to both (op.cit.).

ANALYSIS OF TIlE

FAULT PAlTERN

THE FORB-DUKLA UNIT AND ITS MARGIN

The studied fragment of the Fore·Dukla unit and its im- mediate surrounding extends for

ca. 40

kIn, from

Ustnyki

G6me in the east to Roztoki Dolne near 8aligr6d in the west.

It is I to 6 Jan wide (Fig. 2A). On SW the uni

t is bound by the overthrust of

the Dukla un it built here of

the

Upper Cretaceous t.upk6w and Cisna Beds

C A .

Sl<lczka, 1961; G. Haczewski,

1971; J. Rubinkiewicz, 1996), and

on

the NE by a large inverse fault whose hanging wall consists of the Upper Oli-

gocene

Krosno Beds of the Central Carpathian Depression (A.

SIQczka, K. Zytko,

1978; J. Kusmierek, 1979; L. Mastella, 1995). The Fore·Dukla unit

consists of numerous steeply inclined tectonic slices of various size, aligned NW-SE, in accordance

with the regional strike of the unit (L. Mastella, 1995). They include almost complete sequenceofthe Silesian

unit (A. Slqczka,

1

959), from the Lower Cretaceous

(op. Cit.)

to the Upper Oligocene Passage Beds O.

Kusmi

erek.

1

979).

The obtained cartographic representation shows a regular

pattern of faults (Fig. 2A

) whose position is independent of li

thology

of the affected rock

series

(L. Mastella, 1995).

Individual faults cross through both the slices and the large faults that border the Fore-Dukla unit (L. Mastella

,

1995; I.

Ru

bi

nkiewicz, 1996), and through folds in the Central Carpa·

2"

lMInard Mastella, EwaSzynkaruk

FO .... O ... l.

",,;~...,..

ofMytk.Kv

...

••

Fig. 3. Mohr diagram with shown 29 lUlgles from yanous fragments of the studied ama and T set faults (aftcr R. Dadlez and W. Jaroszewski, 1994), slightly modified

Diagram Mohra z z.aznaezonymi lGitami 29 z rotnych fragment6w badanego obs:zaru omz uskok6w z.espolu T (wedluB R. Dadleza i W. Jaroszewskiego, 1994), nieeo zmicniony

thian Depression. They were thus formed after establishment of the general structural features of the area.

Three sets of fa ults with steep surfaces dominate in the pattern. The directions of two of them (DR and Dd are diagonal

to

the strike of regional units and the third

(T) is

perpendicular to it.

Faults of the DR and DL sets. The directions of the faults efthe DR set (right·lateral) in the western and eastern parts of the studied fragment of th e Fore-Dukla unit are N-S, while those of the DL set (left-lateral) are NE-SW (Fig. 2A, diag- rams 1 and 3). These sets are undoubtedl y conjugate syn- chronous s hears (L. MasteJla, 1995). Thi s is indicated, among others, by the fact tha

t in the middle part, where the azimuths

of the directions of faults DR vary between 7 a nd

IS'

, and of faults DL - 42-S0' they intersect at an angle 20 of ca. 3S".

In the

southern part of the Central Carpathian Depression and in the northe rn part of the Dukla nappe the directions of the DR set are 10" and those of the set DL are 60' (Fig. 2A, diagrams I and II) (J. Rubinkiewicz, 1996. fig. 8).

The 20 angle varies fro m 33' in the northern part of the Dukla unit and in the middle part of the Fore-Dukla unit to ca.

4 6" on its ends. Suc h shears. whose 20 angle is distinctly small er than 60' are called

hybrid shears (p.

L. Hancock, 1985) and they o riginate in a triaxial stress-field when the 0'3 value is negative (Fig. 3;

R

Dadlez, W. Jaroszewsk i,

1994,

fi g. 58), i.e. extension occurs along this axis.

In

the Fore- Oukla

unit

extension occurred by

lateral

expansion of its mostly ductile

layers.

compressed between the sandsto ne complexes of the Dukla unit a nd the Central Carpathian Depression

(L.

Mastella, 1995). Add

itional

extension oc- curred also in the Central Carpathian Depression and the Dukla unit near sigmoidal bends of their contacts with the Fore-Oukla unit (Fig. 2A) (L. Mastella,

1995). The shearing

angle in the southern part of the Central Carpathian Depress- ion is abo ut SO'. This is due to the fact that the faults c ut there through thick-bedded sandston es.

In this lithology

the 20 angle is usually slightly smaller than 60" (G

. Mandl, 1988).

The mean d

irection of

0'1 over the whole studied section of the Fore-Oulda unit, equivalent to the direction of maxi- mum compression, is close to 2S", and in its margins, both in the Central Carpathian Depressio

n and in the Oukla

unit it

reaches 3S"

(Fig. 2A). The 0'3 directions are ca.

lI

S" and ca.

12S", respectively. Both these axes are horizontaJ a

nd the 0'

2 axis is vertical.

Faults of

the T set. The faults of

the transverse set

(f)

are usuaJly readily mappable, wide zones of tec tonic fa ilure (pI.

n, Fig.13). Their nature is in many cases impossible to de

ter-

mine. The verticaJ and horizonta

l component, if they can be

detennined at all. often have variable orientation s, even in a single zone. However, norm al faul ts generally predominate . Faults with azimuths 24-28" predominate in the Fore-Oukla

unit, while those within its margins have azimuths abou

t 3S".

The directions of those faults are nearly

identi

cal with the direction of a" i.e.

they are nearly perpendicular to 0'3,

thus

they seem to be normal faults

(cJ G. Mandl , 1988; R. Dadlez, W. Jaroszewski, 1994) (Fig. 3).

TECTONIC WINDOW OF SWII\TKOWA

A small tectonic win dow occurs near the villageofSwiQI- kowa (Fig. 2B). in whi ch

the Gryb6w

unit crops oul from beneath

the overlying Inoceramian Beds of the Magu

ra unit (M. KsiQzkiewicz, 1972; L. Koszarski,

1985). The Gryb6w

unit comprises a sequence from the Hieroglyphic Beds to the Kros

no Beds (L. Koszars

ki, A. Tokarski, 1968). Large faults of mappable sizes clearly cut through the wi ndow unit as well as through the Mag ura

nappe

(Fig. 2B), hence they are younger than the overthrust of the Magura nappe.

The described faul

t pa

ttern is overprinted by steep faults with di stinct strike-slip component and azimuths ca. 165" (DR

-

right-lateral) and 45" (DL - left-lateral) (L. Mastella, J.

Rubinkiewicz. 1998). The faul ts form a diago nal system of conju gated simultaneous shears with the 20 angle ca. 60" and with the 0'1 axis azimuth of ca. IS

" (op. cit.).

Subordinately occur faults with azimuths ca. 16" (Fig. 2 B). The co

nformity

of !.heir d

irections to the 0'1

direction of the d

iagonal system

make it possible that the fau

lls have the same origin as

the T set faults in the Fore- Oukla uni t, though some smaller ones are feather fau

lts around the DL faults. Most of

the desc

ribed

faults were reactivated as dip-s

lip faults after

the strike-slip phase

(op.cit.).

THE MSZANA DOLNA TECTONtC WINDOW

The tectonic window of Mszana Oolna extends at the most curved fragmen

t of the arcuate Mag

ura unit (Fig. IB).

Many authors

have shown

(H. Kozikowski,

1972; 1.

Burtan.

1974, 1978; 1. Burtan et ai.,

1976, 1978

; L. Maste lla, 1988)

that two tectonic units crop out withi n it. The

lower. fold

ed

and locally broken into tectonic slices Mszana Dolna tectonic

unit (L. Maste

lla,

1988) is built of sandstones and shales of

the Krosno Beds

(J.

Burtan, 1974, 1978; J. Burtan et aI.,

1976,

1978).

It

is overlain by sma ll tectonic caps of the sliced

Gryb6w unit (H. Kozikowski,

1972; L. Mastella. 1988).

Analysis ortlle fault oflhe Polish Outer Crup:nhi':ms 267

2

Fig. 4. Faull pnltem in the Mszana Dolna. tectonic window (rose diagrams 01, 02, 03) and ils margin (after L. Mastclla, 1988), slightly modified BW -the Beskid Wyspowy ovenhrusl (diagrams B I, 82); M - Mogielica ovcnhrust (diagrams M I, M2); the radius orlhe rose represents 15%

Si~ uskokowa w oknie tcktonicmym MSUllly Dolnej (rozety 01. 02, 03) ijego obrnmowaniu (wedlug L. Masielli, 1988), nieco zmieniona BW - skitm Beskidu Wyspowego (rol.cty BI. B2); M - skiba Mogicliey (rozety M I. M2); promierl kola rozet rowna si~ 159&

The fault pattern in the window and its margins was studied in detail in the field (L. MasteIla, 1988) and sup- plemenled with interpretation of air pho(ographs, and radar images (Fig. 4) over an area of ca... 180 km 2. Here also Ihe faults pos(date the overthrusts, as they cut through all (he three tectonic units. The fault pattern eonsist<; moslly of steep faults oblique to the regional tectonic structures (L. Mastella, 1988). Two sets of inilially mike-slip faults dominate (op.cit.): DR - right-lateral and DL - Ieft-Interal ones, both

forming <l conjugate system of synchronous shears. The faults

with azimuths 160-164" (DR) and 44-50' (DL> dominate within the window and in the adjacent part of its margin. The 28 angle is ea. 66" and the azimuth of the 0"1 is 14" (Fig. 4, diagrams 0 1, 02, 03, Bl and 82). Faults with the azimuth 160" dominate in the DR set in the highest parts of the Magura unit and 40" in DL set (Fig. 4, diagrams Ml and M2) at the28 angle about 60" and the azimuth of the 0"1 about 10" (Fig. 9).

This smull difference in the 0"1 azimuths between the window and the basal parts of the Magurn nappe (0"1 - 14") when compared to its higher parts (0"\ - 10") may be due to the

clockwise rotation of the lower parts relative to the higher ones. This is corroborated by transformation of the right-lat- eral faults (DR) into lefl-Iateral ones (L. Mastella, 1988) suggesling in turn (op. cit.) the earlier reported (R. Unrug, 1984; K. Birkenmajer, 1985; C. Tomek, 1988; P. Aleksand- rowski, 1989) clockwise regional rotation.

Most of the discussed faults were reactivated as dip-slip faults, some of them active until now (M. Gruszczynski, L.

Mastella, 1986; L. Mastella, 1988).

CENTRALCARPATHtAN DEPRESSION (AREA OF LESKO)

The analysis of the fault ~attern was made on radar images which cover about 200 km in the Central Carpathian De- pression south-west of Lesko (Fig. 1B). The area is built mainly of thick-bedded sandstones of the Lower Krosno Beds folded into several steep folds oriented NW--SE, locally dis- sected by thrusts (S. Gucik et al., 1979; S. Gucik, A. W6jcik, 1982; A. Slllczka, K. ZYlko, 1978; S. Wdowiarz, 1980, 1985).

Leonard Mastella, Ewe Szynklll1Jk

Fig. SA. Fault pattern (red lines) in we. of Lesko (CelltraJ Carpathian Depression) interpreted from olr-born rudar im:tges and rose diagmms of their orientations Some sandstone series in the Krosno Beds we shown in yellow; the radius ofllle rose represents 2S%

B. Fllult pattern (red Jines) in well ofiywiee interpreted from air-born radar images and the rose diagnun ofllleirorienlations

Some landslone series in the GoduJa Bcd.\ are shown in yellow; the zone of the overthrust orthe Magura nappe is marked in violet; the radius of the rose represents IS ..

A. Sie(! uskoIcowa (krcski czcrwooe) w rejonie I..c$b (centralna depresja karpaeb), wy;nterpretowana lC zdjl;Cia Jotniczego radarowego i routa ich kierunk6w Kolorem !6ltym zaznaczono niekl6R: kompleby piaskowcowe w o~bie ^WarslW krolnielbkk:h; promleii kola rm:~y rownll si~ 25'ilo

B. Siet tlskokowa <kn:ski cuNone) w rejooie

iywca

wyinlerprelowana zc zdj¢a l(I(niezego ndarowego i rozeta ich kierunk6w

Kolorem t6ttym 7.:Wlaczono nickt6re kompleksy piaskowcowe w ~bie warstW aodulskich, kolorem fioletowym - Slrefo; nasuniecia plas<:cwwiny

~gurskiej; promiert kola rozcty rOwn. $~ IS"

The fault pattern as seen on the radar images is very dense and regular (Fig. SA), in contrast to how it is represented on geological maps. It consists of two sets of steep faults cutting

diagonally through the overthrusts and folds, regardless of their lithology. The faults of the set DR with azimuths ca. IS·

dominate (Fig. SA - rose diagram). They are arranged into

Analysis of the faoll oflhe Polish Outer Carpathians 269

1 / -( )</ \ \ <, -<I \"\;"

^I

\'r,,/v!t~- ^{, \} >").'V / \ (' ^/"

/ I. \ ' \\ \

I " . \ "

f'" \ ^{>.~ /1\\\'1 1(/\1\\\\}

I

~-<;\ 1 I , Y

^{I / /\}

^V J.. ^~/I

^{\ J ..}

, ,,,bt,

fI 1 \\ \,,' 1

' -( ,,"'{ 'CS> /

Lasko \ :\

X\ \ /

I \

/ Af ~

^I

/ I \~"

^I

^{f).; , /} / " ^{, ,}

⁰

^{, 5}

^lOlon

Fig, 6, Skeleh oflOO faolt pattern drawn from interpn::tolion ofradat image with rose diagram.~ in the Magora nappe (diagram 1) and the Silc.sion nappe (diag- ram 2)

The radios oflhe

rose

diagrams n::pn::senls 25%; dashed line lnarics the wne oflhc ovcnhrust ofthc Magur.l nappe

Odrys sled oskokowej, wylnterprelowanej zc ...:dj~cia radarowego,...: rozetami ich kicrunk6w w ob~bic plaszezowiny m.agurskiej (routa 1) i gl~kiej

(rozeta 2) ^<

Promieli kola rozet r6wn:l 5i~ 25%; linill pl'lCrywan~ zaznacwno sU'ef~ nasuni~cia plas!cwwiny magurskiej

three distinct fault zones extending approximately along the valleys of the Oslawa river, Hoczewka stream, and the lower course of the Solinka river (Fig. SA). The fault zone of the Hoczewka and lower Solinka (Fig. SA) extends clearly to the south to the fault cutting across the B ystre tectonic sl ices along the

Jablonki

stream (A. SI'lczka, 1959; L. Mastella, 1995), Similar directions of faults were observed by A. Pszcz6lkow- ski (

1

968). The described fault zones as well as

individual

accompanying faults with the same direction have a compo- nent of right-lateral movement. The faults of the OL set are less numerous and are usually dispersed (Fig. SA). Both sets intersect at an angle close to 50", The described features and regional analogies suggest that both sets are conjugate and synchronous and the O"t azimuth of ca. 40" is si milar to that measured near the southern boundary of the Silesian unit in this part of the Carpathians (Fig. 9).

THE SILESIAN NAPPE BEITWEEN THE DUNAJEC AND SKA WA RIVERS

This area is considered after M. Ksiotzkiewicz (1972) as a structurally uniform domain within the Si

lesian nappe.

The Silesian nappe in this area cons ists of flal, indisti nct folds and

it

is di vided inlO the northern and southern parts by the strongly tectonically sliced Lanckorona-Zegocina zone, ex- tending east-west. The northe rn part is built mainl y of Creta- ceous strata

ranging from the

Lgota Beds through Istebna Beds, whi

le

the southern part

is built mainly

o f Palaeogene strala, ma

inly

the Krosno Beds (M. Ksi'lzkiewicz, 1972). The western boundary is marked by the faull extending along the Skawa river valley. The tectonic styl e of the Silesian nappe changes eastward of the Dunajec river to one of distinct folds (M. Ksi'lzkiewicz, 1972). From the so uth the studied area includes also a fragment of the Magura nappe.

Th e fault pattern, as interpreted from the air photos, main

ly radar images,

is regular all over this area, both in the Silesian nappe and in the adjacent fragmenl of the Magura

nappe. It consists mainly of two sets - the NNW-SSE and the NE-SW ones, diagonal to the slrike of the main regional structures, simil arly as over the whole area described earlier.

Thedi

rections offaults are independent

of the lithology of the dissected rock series.

The analysis of images, supplemented with the author's and A. Konon's (1996, 1997) field studies indicates that also here the described faults had a strike-slip phase in their evolution, as conjugate synchronous shears: NNW -

right-

lateral (DR), NE

-

left- lateral (OL) and were fonned after the formation of the folds and overthrusts in this part of the Outer Carpathians. The post-thrust age of the faults of this type was accepted for the western part of the discussed frag- ment of the Silesian nappe by M. Ksiotzkiewicz (1974) and also partly by P. Aleksandrowski (

1

989).

The area near the Rozn6w rese

rvoir. The

fault pattern was studied here over an area of 140

km

2 in the Silesian nappe east of the Rozn6w reservoir and in the Magura nappe

10

the west of the reservoir (Figs. I B, 6). The directio ns of the two fault sets are nearly identical in both areas - 15G-15S' (DR) and 3G-35' (Ow (Fig. 6, diagrams I and

2).

The

20

angle is about 60", and the azimuth of 0"1

-

about 5' .

The fault pattern consists of uni formly dispersed faults of both sets (Fig. 6). The faulls with NNW strikes though clearly predominating (Fig. 6) are not grouped into d

istinct fault

zones. The fau

lts

marked on Ihe map (1

. Burtan et al., 1976)

do not appear on the radar image. On

ly the meridional

fault east of the Rot n6w reservoir

(op. cit.) is manifested on

the radar image as a concemration of faults of both sets. It can be thus suggested that no significant horizOnlal displacements occurred in this area after the fonnation of the described fault pattern.

The a

rea of My§Ienice. The studied fragment, about 140

km2 in area, ex tends in the southern, strongly folded and

thrusted part of the Silesian nappe near its contac t with the

overthrust of the Magura nappe 0.1. Ksi'lzkiewicz, 1972, fig .

8). The fault pattern consists ofunifonnly dispersed faults of

270 Leonard MasfClt:L, Ewa S~)'nkaruk

A

Myslenice region Wadowice region

Fig. 7. Rose diagrnms of flWlI directions in [he :I~!I. of Myslenice {A} and Wlldowice(B)

The radius ofllle diagrnms A and B n:presenl5 20%

RO:tCty kicruok6w sied uskokowej \II okolie), My~lcnic (Al i Wndowic (B) Promici\ kola rout r6wna si~ 209&

both

sets.

Some of tnem cut the overthrust of the Magura

nappe.

The DR set with the azimuth ca. 156⁰ clearly dominates.

less numerous is the set DI.. oriented at ca. 24° (Fig. 7 A). The 29 angle is ca. 48° and the 0"1 azimuth is ca. O' (Fig. 9), The low value of 20 seems to indicate the presence of east-west extension during the formation of the discussed fault pattern.

The area of Wad ow ice covers about 160 km2 and extends from the river Skawa in the west as far as 16 km to the east (Fig. 18). It includes the Pog6rze Lanckoronskie element- a nat syncline (M. Ksillzkiewicz, 1972) and a fragmcn! of the northern margin of the Magura nappe. The faull pauern con~

sists, similarly as in the area of My~lcniee, of the dominant DR set and less frequent DL faults (Fig. 79). Faults with azimuth ca.

145"

predominate in the

DR

sct, and about

25"

in the DL sel. The 28 angle is ell. 60" and the 0"1 azimuth is ca.

175" (Fig. 9). Also here the discussed Faults cut through both the Silesian and Magura nappes without any change in direc- tion.

The Faull network is uniformly distributed over the area.

A small concentration of the NNW-SSE oriented faullS.

visible along the Skawa river coincides with the large fault known here (M. KsiOlikiewicz. 1972). A much more distinct

w

_N

20 20

NNW-SSE oriented fault zone is formed by the faults of

DR

set concentrated along the Cedron stream.

TfIE AREA OF tYWIEC

The area extends over ca. 200 km2 (Fig. IB) in the Silesian and Magurn nappes. The fault pattern consists of the

DR

faults with azimuths

140--1 55"

and

Dt.

faults with azimuths

25- 30"

(Fig. SB). The 20 angle is between

55

and

65".

The O"t azimuth is ca. 175" (Fig. 9). While both sets are uniformly distributed. the less numerous DL faults form two fault zones with azimuths ca.

30".

The more distinct of them lies on the

~astern side of the iywiec reservoir and the second. more dispcrsed one is near Kocoti (Fig. 58). The faults clearly cut through the Magura nappe overthrust, maintaining the same direction in the Silesian and Magura nappes (Fig. 58).

ANAl. YSIS OFTIiE FAULT PATTERN ON GEOLOGICAL MAPS 1:200000

The analysis of the fault pallcrn revealed by field studies and interpretation of air photographs and radar images were supplemented with the analysis offaults shown on geological maps 1:200 000. shcets Jaslo (P. Nescieruk et aI., 1992), Nowy Sqcz

(1.

Burtan et aL, 1981) and Bielsko-8iala (J. Golonka et al., 1978). The striking feature of the fault pattern in this area is the clear domination of steep faults of one set with widely changing (within

30")

orientations (op.cit.) Thc faults of this set that are identified in the field form usually wide zones of tectonic disruption. cataclasites and breccias, similarly as Ihe T sel faults in the Central Carpathian Depress~

ion (PI. n, Fig.

1 3).

These are usually oblique slip-faults in which the direction of movement along the fault plane changes even along one fault. Similarly as earlier described faults in the Central Carpathian Depression. these faults were found by W. Zuchiewicz Dnd A. Henkiel (1993) to be approxi~

mately perpendicular to the strike of the regional tectonic structures (J. Golonka et al .• 1978; J. Burtan et al., 1981; P.

Nescieruk et al .•

1992).

Their azimuths. as was noted by S.

E

Sheet Bielsko~Biala Sheet Nowy Sqcz Sheet Jaslo, western part

Sheet Jaslo, middle part

Sheet Jaslo, eastern part

Fig. 8. Rose di:\inlffiS oftransversc raults T drawn nfter gcologieat maps 1:200 000, shI;:(:ts Bidsko-Biala, Now)' Stlez and Jaslo Numbers on the lower left ~idcs of tile dingrtnns indicate pcrcc:ntilge values of tile diilgrnm rndiu5

Rozely uskok6w POPl7.Cc1.nych zespolu T wykonnne nll podstDwie map geologitVlych w skali 1:200 000, nrk. Biclsko-Billla, Nowy SQCz; i J:JSlo Liczby z; Icwcj doJncj slrony T01..c1 OUlOCUjtl WllJt~ procento\Yll promienia

Analysis ofthc fault of the Polish Outer Carpathians 271

/

"'\.. /)V~"'C.

~'I·" r J " " v

Lr-, } I ^cr.

^{(D. OJ}

~'k'/ _, I

Baligr6d

I

D D D

Miocene Slfata of Carpathian Foredeep Silesian nappe

Other lc<:10nie units

I ^{cr. rn o ,}

^50km

I i ^{, . ,}

US1'lyki

·06tt1e

.,

Fig. 9. Schematic map ofli1e study 8ll:a with Gl ues determined for the DR and Dt, raull system (solid lines) and ~or the T faults (dnshcd lines) Scoomatyczna mapaobszaru bada6 z wyznacronyrni osiami 0"1 z systemu uskok6w DR i Dt,(kreski ei~gle) i z zespolu uskok6w T (kreski przerywane)

Ookt6r and M. Graniczny (1982) approximately correspond to the described 0"1 of OR and OL sets. This additionally confirms that these are T set faults. Their origin should be thus the same as of the faults of this set in the Fore-Oukla unit and its margin. Taking into account the evolution of the stress field in various parts of the Polish Carpathians (p. Aleksandrowski, 1989; L. Mastella, 1975, 1988) one may suppose that these faults are the youngest and have been fonned during the post-orogenic uplift of the Carpathians under conditions of vanishing submeridional compression.

The faults of the DR and 0L sets on the studied maps are not numerous. but they almost always correspond to the faults detected in the field and on the radar images.

THE FAULT PATTERN AND JOINTS

The directions of the fault pattern described above largely correspond to the directions of the two conjugate sets of joints (01 and D2) and the T set (L. Mastella

et af .•

1997; W.

Zuchicwicz.

1 997a. b)

observed by us and reported by other authors (M. Ksi<lzkiewicz. 1968; P. Aleksandrowski, 1989;

W. Zuchiewicz, A. Henkiel. 1993; L. Mastella et aJ.,

1997;

W. Zuchiewicz.

1997a, b).

These sets change their orientation from the east to the west, maintaining stable position with respect to the regional fold structures. The 0\ and ~ joint sets display a tendency to left- and right-lateral displacement along them, respectively (L. Mastella

et ai.,

1997). As in the case of DL and OR faults, the 28 angle of 0\ and D2joint sets is about 60' (W. Zuchiewicz, A. Henkiel, 1993; L. Mas- lella

et ai.,

1997). The analogy is so close that in the areas of My§lenice. Fore-Oukla zone and in its southern margin the 28angle is lower than the dominant one and is

30-48'

for the OL and OR faults as well as the joint sets OJ and 02, as it is

shown by the author's observations. The joints there are hybrid shears fonned at negative values of 03. This constata- tion has far-reaching consequences. It indicates that the faults (OL and OR) and joints 0] and 02. regardless of the age of the host rocks. appeared in nearly the same time, after the over- thrusting of nappes and fonnation of the fault that separates the Fore-Dukla unit from the Central Carpathian Depression.

As is suggested by the use of the method ofO. J. Sanderson el al. (1991) the formation of the OL and OR faults was facilitated by mechanical weakening of the terrane by the slightly earlier fonnedjoints 0\ and~.

Also the directions and origin of the faults of T set and transverse joints (L. Mastella

et ai.,

1997; W. Zuchiewicz.

1 997b; w.

Zuchiewicz, A. Henkiel. 1993) seem to be the same.

SUMMARY

The results of the field studies and air photo interprelation.

especially radar images, indicate that a dense pattern of steep faults is present in the studied fragment of the Polish Outer Carpathians. It consists mainly of two sets, DR and OL of faulls diagonal to the strike of major regional structures and of a less dense set T of faults transverse to these structures.

The DR and OL faults are mostly strike-slip faults reacti- vated as dip-slip faults. In the strike-slip faults the OR faults were right-lateral and the OL ones - left-lateral. Their azi- muths display a regional variation: DR - from about 10' in the east to about ISO' in the west, and DL - from 60 10 25'. respectively. The results of the structural analysis indicate that Ihey fonn a system of conjugate simultaneous shears wi.th

272 Leonard Masleita, Ewa Szynkaruk

dominant 20

angle of about

60', Locally the value of this angle is smaller. In the Fore-Dukla unit and its direct vicinity it is about 35° and in the My§lenice area near the overthrust of the Magura nappe on the Silesian nappe - about 48", In both cases this is probably the result

of extension

in the

direction of strike of the regio nal structures during the forma-

tion of the described faults.

It may be concluded that the system of DR and DL faults originated in a triaxial field of stresses in which only locally 0'3 attained small negative values. The calculated direction of

com pression, corresponding to the axis of the main stress (0'1),

varies regionally from aOOu140' in the east (except the Fore- Dukla unit strongly dissected by thrusts, where 0"1 = 25°) through about O· in the central part 10 aboul 175· in me western end of the studied section of the Western Outer Carpathians (F;g.9).

The pattern ofT set faults consists mainly of faults trans- versal to the regional structures, so that faults with azimuths 35· dominate in the east and 165·-in the west (Fig. 8). Their directions correspond approximately to the crl directions of the DR and DI.. fault system (Figs. 8, 9). This seems to indicate the T faults fonned under a significant extension over the whole area in the direction perpendicular to then vanishing compression of the stage of the DR and DL fault fonnation. Therefore the system of DR and 01.. is older than the T faults.

Both, the DR and DL faults and the T faults cut through the regional structures in the Silesian, Oulda and Magura nappes and the zones of their overthrusts. This indicates that the discussed pattern of faults formed already after folding

and thrusting of the nappes. The regular pattern of faults and the stability of its directions in all tectonic units in the area indicate that they are primary faults, formed in the regionally homogeneous stress field (R. Freund, 1974). It also indicates the lack of major horizontal movements in this part of the Carpathians after their formation.

Thedirections ofthedescribed fault pattern coincides well with the pattern of joints oblique and perpendicular to the regional structures. A1so the value of the 20 angle and its regional variation in the fault pattern and joint pattern are the same. This may indicate nearly simultaneous origin of the joints and faults.

The review of papers by other authors (N. Oszczypko, A.

Toma§, 1985; M. Cieszkowski et aI., 1992) may suggest that the DR and 01.. fault system originated in the early Sannatian when the Magura nappe was finally pushed (M. Cieszkowski et

al.,

1988). It was probably only from that time when the joints of shearing system (OL and DR - L. Maslella et

al.,

1997) began to appear. The T faults (and probably also the T joints) should be attributed to post-orogenic uplift of the studied area which, according to M. Cieszkowski et aJ.

(1992), should be referred to the end of Neogene Period.

Acknowledgements The authors thank Doc. Dr. hab.

Marek Graniczny and his team, for providing access to the radar images and assistance in their interpretation. We also thank Dr. Marek Jarosiiiski for his discussion and critical remarks on the draft of this text.

TranS/aled by GrugOrt Haclewski

REFERENCES

AI..EKSANDROWS KI P. (t 989) - Structural geology ofthc Magurn Nappe in the Mt. BabiaG6rn region, Weslcrn Outer Carpathians (in Polish with English summary). Stud. Geol. Pol" 46.

B IRKENMAJER K. (1985)- Majorstrike-slip faults of the Pieniny Klippen Belt and the Tertiary rotation of the Carpathians. PubLlnsl. Geoph. Pol.

Acad. Sci" A-16 (175), p. IOJ-115.

BURTAN J. (1974)-Sz,ug6l0wa mapageologiczo3 Polski 1:50000, nrk.

MSl!Nln Dolna. InSI. Ceol. WlIl'szawn,

BURTAN 1. (1978) - Obja§nienin do s=g6lowej m:lpy geologiczneJ Polski 1:50000, nrk. MS7Jl11a Dolna. Insl. Geol. W3lOZ3wa.

BURTAN J .. PAUL Z., WATYCHA L. (1976) - Szczeg6lowa mapa geologicznaPolski 1:50000, nrk. Mszana G6ma. Insl. Gcol. WlII'Szawa BURTAN 1., PAULZ., WATYCHA L. (1978)-Obja.<nieniado s=g610-

wcj mapy geologiczoej Polski 1:50000, ark. MSlnOa G6malnst. Geol.

Warszawa.

BURTAN J., GOLONKA 1., OSZCZYPKO N., PAUL

z.,

SLA,CZKA A.

(1981) - Mapa geologicznll Polski 1:200 000, ork. Nowy S1\Cl., tnsl.

Geol. Warszawa.

CIESZKOWSKI M., GONERA M., OSZCZYPKO N., SLI;ZAK J., ZU- CHIEWICZ W. (1988) - Litoostrntigruphy and age of Up pcI' Miocene deposits at Iwkowa, Polish West Carpathians. Bull. Pol. Acad. Sci., Earth Sci" 36, p. 309-329, no. 3-4.

CtESZKOWSKI M., OSZCZYPKO N., ZUCHIEWICZ w. (1992) - Tcktonika .frodkowcj cz;ki plauczowiny magumkiej. Prz.cw. LXIII Zjazdu Pol. Tow. Geol. w Koninkach, p. 20-30.

OAOLEZ R., 1AROSZEWSKt W. (1994) - Tektonika PWN. Warszawa.

DOKT6R S .. GRANICZNY M. (1982) - Geological interprelation of satcllite and ",dar imagery of the eastern part of the Curpnthinns (in

Polish with English summary). Kwart. ^Ceo!., 26, p. 229-243, no. I.

ENGELDER T. (1989) - Joints:U'ld shear fractures in rock. In: Fracture mechaniC5 of rock (cd. B. K. Atkinson), p. 27-65. Acad. Press. London.

FREUND R. (1974) - Kinematics of trnnsforrn nnd trnnscurrent faults.

TcctonophysiC5, 88, p. 291-312.

GOLONKA J .. BORYSt..A WSKI A., PAULZ .. RYl:..KOW. (l978)- Mapa geologiczoa Polski I :200000, ark. Bielsko-Bialn.lnst. GeoL Waruawa.

GRANICZNY M .. DOKT6R S .. KIBITLEWSKI S .. MARSZCZEK T.

(1989) - Kompleksowe badanill. teledctckcyjne. gcofizyczoe i hydro- geologiezoe din potrzeb geotennii na obsz.arzc PodhaJa. Tcchn. Poszuk.

Ceol., 1/89, p. 9-15.

GRUSZCZYNSKI M., MASTELLA L. (1986) - CalCare(lUS tufas in the

~ of the Mszana Dolna tectonic window (in PoIiM with English summary). Ann. Soc. Geol. Pol., 56, p. 111-131, no. 1-2.

GUCIK S., W61CIK A. (1982)- Obja.fnienia do mapy geologiczoej Polski w shU 1:200 000, ark. Pn:emy~t, Kalnik6w. Insl. Geol. Warszawa GUCIK S., PAUL Z., SLACZKA A .. ZYTKO K. (1979) - Mapa geologia-

na Polski 1:200 000, ark. Przemy~l, Kalnik6w. Insi. Geol. WarsUlWIl.

HACZEWSKI G. (1971)-Geologicnl slructure Oflhc Dukla unit's front in tile vicinity of Ustn:yki G6me (in Polish with English summary). ZeS:t.

Nauk. AGH. 292:. p. 85-91, no. 14.

HANCOCK P. L. (1985) - BritUe microtectonies: principles and praclice.

Jour. Stmct. Geol .. 7, p. 437-457.

Analysis of the (aull of the Polish Outer Carpathians 273

HANDIN J., HAGER R. V., FRIEDMAN M., FEATHER J. N. (1963)- Experimental deformation o(sedimcntary rocks under confining press- ure: pore pressure test. Bull_ Am_ Ass. Pelrol. Geol., 47, p. 717-755.

JAROSZEWSKI W. (l972) - Mesoscopic structural criteria of tectonics of n'on-orogenic areas: an example from the nOM-eastern Mesozoic margin of the Swil;tokrzyskie Mountains (in Polish with English summary).

Stud. GeoJ. Pol., 38.

JAROSZEWSKI W_ (1980) - Tektonika uskok6w i fald6w. Wyd. Geol.

Warsmwa.

KONON A. (1996) - Tectonics ofLapicrt Mt. (Beskid Wyspowy, southern Poland) (in Polish with English summary). Pn. Qo:ol" 44, p. 1195--1198, no. 12.

KONON A. (1997) - Tectonics of the Sniernica Massif and its foreland (Beskid Wyspowy, Magura Nappe, southern Poland) (in Polish with English summary). Pn. Gco!.. 45, p. 1001-1007, no. 10(1).

KOSZARSKI L. (1985) - ~ology of the Middle Carpathian and the Cnrpathian Foredeep. XIII Congress C!I1patho·Balkan ~o!. Ass,,3, stop 51, p. 213.

KOSZARSKI L., TOKARSKI A. (1968) - Szczcg610wa mapa geologicZlUl Polski 1:50000, ark. Osiek. Wydanie tymczasowc. [nst. Geo!. Warsza-

w.

KOZIKOWSKI H. (1972) - Metltod of selecting the areas forcxpJorations on tile example of tile geological structures of the tectonical window in Mszana Doilla (Central Carpathians) (in Polish with English summary).

Geof. Geo!. Naft., 11-12, p. 191-192.

KSIA.ZKIEWICZ M. (1968) - Observalions of jointing in the nysch Car- pathians (in Polish with English summary). Roc!.. Po!. Tow. Goo!., 38, p. 335-384, no. 2-3.

KSII\ZKIEWICZ M. (1972) - Budowa geologic-"na Polski, 4 - Tektonika, part 3 - KDrpaty. [nst. ~ol. Warszawa.

KSII\ZKIEWICZ M. (1974) - Szczeg610wa mapa gcologiczna Polski 1:50000, ark. Sucha Beskidzka, wraz z objaAnieniami. Inst. Geo!.

Wa.rs1.awa.

KUSM[EREK J. (1979) - Gl1Ivitlllioolil deform31ions and backward over- thrusts with reference to deep structures and petrolcum prospectS of tile Dukla unit in the Bie>lC7;1dy Mountains (in Polish with English sum·

mary). Pt. Geo!. Komis. Nauk. Geo!. PAN Krak" 114.

MANDLG. (1988) -M~chanics oftcctonic faultiog. Deve[op. Struc!. GeoL E[sevier. Amsterdam.

MASTELLA L. (1915)- Aysch tcctonics in thc~nstern part of tile Podllale Basin (Carpathions, Poland) (in Polish with English summary). Rocz.

Pol. Tow. Geo1., 45. p. 361-40[, no. 3-4.

MASTELLA L. (1988) - Structure and evolution of Mszana Oolno tcctonic window. Out~r Carpathians, Poland (in Polish with English summary).

Ano. Soc. Geo1. Po1., 58, p. 53--173, no. 1-2.

MASTELLA L. (1995) - Mapa tcktoniczno j~dnostki przeddukie[skiej, wrnz z obj~nicniarni. Projektlmdawc;t;y KBN no. 600999101.

MASTELLA L., RUB[NKIEWICZJ. (1998) - Dup[cx structures withio the Swi'ltkowa Wielkllt~Clonic window (Beskid Niski MIS" West~m Car- pathians, Poland): structural annlysis and phOlointerprctation. Goo!.

Quart" 42, p. [73-lg2, no. 2.

MASTELLA L., KONON A., MARDAL T. (1996) - Tectonics of the Podhalc Flysch, Bialka River Valley, soulhern Poland (in Polish with English summary). Pn; Gcol .. 44, p. 1189-1194, no. 12.

MASTELLA L., ZUCH[EWICZ W., TOKARSKI A. K., RUBINKIEWICZ J., LEONOWICZ P., SZCZ.E:SNY R. (t997) - Application of joint antllysis for palCQstress l'e<:onstroctions in structurally complicated set-

lings: case study from Silesian nappe, Outer Carplllllians (Poland) (ex- fcnded abstl1lct). Prz. Geo!., 45, p. 1064--1066, no. 10(2).

NESCIERUK P .. PAUL Z., RvtKO W., SZYMAKOWSKA P., W6JCIK A., ZYTKO K. (1992)-MapageologicVll1Polski 1 :2oo000,art. Jaslo.

Inst. ~o!. Warszawa.

OSTAFlCZUK S. (1978) - Fotogeologia, rotointerpretacja i fOlogl1lmetria gcologiczna. Insl. ~ol. Warszawa.

OSZCZYPKO N .. TOMAS A. (1985) - Tectonic evolution of marginnl part of the Polish F1ysh Carpillhians in the Middle Miocene. Kwart.

G~ol., 29, p. 109-128, no. I.

PSZCZ6t.KOWSKI A. (1968) - Aeri:tl plloto interpretation of fold struc- tures in the sOUlhem part of the Central Carpathian depression (Polish nyscll Carpathians) (in Polish with English summary). Acta Owl. Pol., 18. p. 847-862, no. 4.

RUBINKIEWICZ J. (1996) - Tectonics of the Dukla Ovenhntst Zone in the western part of Bieszcllldy (SE Poland) (in Polish with English summary). Pn. Gool,,44,p. 1199-1204. no. 12.

SANDERSON D. J., CHINN C .. BENTHAM 1. (1991) - Landsat linea- ments and structural control of mincl1llizntion. In: Development ofltCw muhi-disciplioary tcchniques for mln~ral exploration in several areas of

west~m Iberian P~ninsula (cds. P. Gumiel, C. Anton·Pacheco, R. Cam- pos), p. 87-109.lnsl. Techno!. G~oMln. Espana. Madrit.

SLACZKA A. (1959) - SlClItigraphy of the Bystre scale (Middle Carpa- thians) (in Polish with Englisll summary). Biut. Inst. Gool., 131, p.

203-286.

SLA.CZKA A. (1961) - Pmblemy poIudniowego obrzeunia cenlCll[nego synklioorium omz jcdnostld dukielskiej. Przew. XXXIV Zjazdu Pol.

Tow. GcoJ., p. 37-48.

SLA.CZKA A .• ZYTKO K. (1978)-Mapa geo[ogiczna Polski 1:200 000.

ark. t.upk6w. Inst. Geo!. Warsuwa.

TOMEK C. (1988) - Geophysical investigation of the Alpioc-Carpatllian Are. In: Evolution of tile nonhem margin of Tethys: the results oflGCP Project 198, p.167-199.

UNRUG R. (1984) - Geodynamic evolution orthe Carpatllinns. Ann. Soc.

GeoL Pol., 52. p. 39-66, no. 1-4.

VERGEL Y P., ZADEH·KABIR H. (1988) - Etude par photo-interprtt31ion compartede 13 rigion dc Langeti~re Lcs Vans (Languedoc septentrional, Frnnce): utiHS31ion des photographies reriennes, des images parsoteJitcs et des images radar. Bull. Soc. ~ol. Fmnce, 4, p. 303-314, no. 2.

WDOWIARZ S. (1980) - The geo[ogical structure of the Centra[ Carpa- thian Synclinorium in tile Rajskie-Zachoczewie (in Polish witll English summary). Biu!. Inst. ~ol., 326, p. 5-24.

WDOWIARZ S. (198j) - On some aspects of geological structure and oil and gns accumulillion oftheCenlCll1 Cnrpathion Synclinorium in Poland (in Polish with English summary). Biul. Inst. Ow[., 350, p. 5-52.

ZUCH[EWICZ W. (19970)-Rcorientation of the stress fic[d in the Polish Outer Carpathians in the Hgllt of joint pattern analysis (in Polisll with English summary). frI.. ~0L. 45, p. 105-109. no. I.

ZUCH[BW[CZ W. (1997b)-Distribution of jointing within Magurn Noppe;

West Carp31hians, Poland, in the light of statistical analysis (in Polish with English summary). Pn .. Geo!.. 45, p. 634-638, no. 6.

ZUCHIEWICZ W .. HENKIEL A. (1993) -Orientacja p6inokenozoicmych

nap~!ctltc!::lonicUlycll II' ~wietle analizy pomiar6w sp-:katl ciosowych w SE ~ci K.arpat Polskich. Aon. Univ. M. Curic-Sklodowska, Lublin.

PolQllia, XLVIII, 23 B, p. 311-348.

ANALIZA SIECI USKOKOWEJ WYBRANYCH OBSZAROW Z POLSKlEj'CZIlSCI KARPAT ZEWNF;TRZNYCH

Streszczenic

Oprncowanie dotyczy sicd uskokowej na wybranych obsml1lcll polskiej

c~ci Karpatzcwnetrlnych (fig. I A). Anali~oparto no wlnsnych badaniach terenowych, ioterpretacji zdje~ lotniczych, ^II' tym rndarowych, oraz maJNIcll geoJogicznych (fig. I B). Poslugiwano sil; metodami klllSycznymi, u;t;upcloio-- nymi anali74 stroklUraln~ (tab!. I. fig. 10, I I; tabL II, fig. 12). Stwierdwno,

tc na badanym ~ZDrl.C wystepujc ~ta i regulama sic~ stromych uskok6w.

Sklada 5il; ona gl6wnie z dwOch zespol6w: DR i Dt. - uskok6w skofnych do rozciQglo~ci stroktur regional nych - i zespolu T - popn.cclJlego do tych stroktur (fig. 2, 4-7). Wszystkie one wykazuj~ regionalnll zmienno~ azymu- t6w: DR - od okolo to' na wschodzie do okolo ISO· na zachod1.ie, DL-

274 Leonard Mastella. Ewa S1.ynkaruk

odpowicdnio oil okolo 60'00 okolo 25", Ieh kierunki 511 niculetne ad litologii prlCCinanych pncz nic kompleks6w skalnych. Uskoki DR i Dt.S4 uskokami pnesuwczymi: OR-prowos~lnymi, a IlL -lewosk~tnymL Twol'Ul one system gcieC' sp~wnych r6wnoczcsnych 0 dominujilC;ym kllcie 29 okolo 60', Lokalnic, w jednostce prz.cddukielskicj i jtj p6tnocnym obramowaniu omz w rejonie My~lcnic kilt ten jest znacznic mniejszy - 35-48" i uskoki nabicrajll charakteru ~i¢ hybrydowych. Powstaly onc W lr6josiowym polu nap~tell.. w kt6rym. w wyniku rozcill&nnia zgodncgo zpnebicgicm scruktur regionalnych, G3 przyjmowalll lokalnie wartoU ujernnq (fig. 3). Oblielony kierullek kompresji (odpowiodajllcy Gl) zmien;n sie regio/Ullnic od okolo 40"

nn wschodzie do okolo 175' na 1.8chodzie (fig. 9), Sic!! uskok6w T sk/adasi.;

gl6wnie z dutych uskok6w poprzecznych do rozcillglOOci Slruklllrregional- nych Illk, U w t'l¢ci wschodniej dominujll uskoki 0 :lZynlucie okolo 35', a wzachodniej okolo 165' (fig. 8). Ich 8Zymuty pokrywaj(lsie z kierunkami 0'1 (fig. 9). Wynikaloby Z !ego. te uskoki T powslawaiy przy wysfl;pujqcymjui

na calym obszarze rozci(lgnniu proslopadlym do kierunku zanikajQCCj jut kompn:sji zeillpu powslawania uskok6w DR I DL_ W lej syltJacji uskoki te Sli stllfSlCod uskok6w T. Zar6wno uskoki DR i Dt., jak i T pnecinajll regional ne struklllry w plaszczowinic ~llISkicj, dukiclskiej i magurskiej oraz nnsuni~ia Iyeh jednostck. Wskazujc 10, te ollUlwiana sic!! uskok6w powslaia jut po sfaldowaniu i nasunicciu tyeh plnszczowin.

AnaHzuj~c proce innych autorOw (N. OS7.czypko, A. Tomaf, 1985; M.

Cicszkowski i in., 1992), moina wnioskowa(!, te system uskok6w DR i

Dt.

powstal we wczesnym sarmacie, kiedy to nastllpilo dopchnieeie plaszczowi- ny magurskicj (M. Cicszkowski i in., 1988). Prnwdopodobnie dopiero od lego czasu ucze1y ujawnia!! sic spekllnia ciosowc liyslemu ~ci~iowego {Dt. i DR - L. Mastclla i in .• 1991}_ Nlll.omiast uskoki T (a upewne i cios

n

wi4Zll!!

nn1ciy zpootorogenicznYnl wypietrzanicm badanegoobszaru, co zgodnic zc zdaniem M. Cieszkowskiego i in. (1992) willU!! naleiy Ie schylkiem neoge-

".

EXPLANA TrONS OF PLATES

PLATE I

Fig. 10. Strike-slip left-lateral fault with a fault drag. Azimuth orthe plane is shown next to Ihe f~uh linc: strike and dip of strota n.re also shown.

The arrows show the direction of strike-slip movement. Tectonic window of Msuna Dolna. Exposure of the Krosno Bcds in the Konina river between Nicdtwicdt lind Konina

Uskok pnesuwczy lewoskretny z prl.)'uskokowym 1.a1"aldowanicm.

Przy lin;; uslcoku zaz.naczono jego IIZyntut, a przy warstwach ieh bieg i upad. Slrzalki wsk!i;r;ujll v.vrot ruehu p~suwezcgo. Okno tektoni- C7J1e MS1.any Dolncj. Odsloniccie WlU'Stw kroo:nicnskich w korycie I"t.eki Konina miedZY wsiami Niediwiedt i Konina

Fig. 11. Small ell echeloll low·angle fnults and fault-drag ne:u':I right-lateral strike-~lip fault. Fon:-Dukln unit - Bystn: slice. ruposum of the Cicszyn Beds in the lablonka stn!am al Jablonka village

Drobne uskoki kulisowe niskok:J.lowe i podgieda warstw przy usko- ku pri.CSuwezym prawoskretnym. lednoslka prLCddukic:lska - Iuska

Systmgo. Odsloni~ie watSlw cies;r;ynskich w poIoku Jablonka we wsi Jablonka

PLATE II

Fig. 12. Breccia with ell echelo7ljoints in the ;r;om: of a lefi-Iatcrul strike-slip fault. Central Carpathinn Depression_ mposureoflhe Olryt sandsto- nes in the Stcinica river

Brckcjn ;r; ku!isowymi spekaniami w strefie uskoku przesuwczcgo lewoskretncgo. Centralna deprcsja karpacka. Odsloni~cie piaskow- c6w 1. Otrytu w korycie I"t.eki Sictnicy

Fig. 13. Faull zone. Central Carp;Jthwn Depression_ Exposure ofthc middle part ofille Krosno Beds in the Sotinka river at Suk

SIn:fa uskokowa. Ccnlralna depresja karpacka. Odslonil<Cie ~rodko­

wej cz;;ki warstw krotnienskich dotnyth w korycieneki Sotinka we wsi Buk

GeoI. Qu:u1., 1998,42 (3) PLATE I

Fig. 10

Fig. II

Leonard MASTELLA, Ewa SZYNKARUK - Analysis ortlle rault pallem in selected

=

^of tile Polish OuterCarpathions

PLATE I[ GeoI.Quart.,1998,42(3)

O ,5m

Ma·12

Ma. 13

Leonard MASTElLA, Ewa SZYNKARUK - AnoJysis of the fault p~Hem in selccted wellS of the PoHslI OuterDrpnlhinns