TO POG RAPHY OF THE MA GURA FLOOR THRUST ...asgp.pl/sites/default/files/volumes/78_2_135_149_0.pdfAnnales Societatis Geologorum Poloniae (2008), vol. 78: 135–149. TO POG RAPHY OF

Annales Societatis Geologorum Poloniae (2008), vol. 78: 135–149.

TO POG RA PHY OF THE MA GURA FLOOR THRUSTAND MOR PHO TEC TON ICS OF THE OUTER WEST CAR PA THI ANS

IN PO LAND

Wi told ZUCHIEWICZ 1 & Nestor OSZC ZYPKO 2

1 Fac ulty of Ge ol ogy, Geo phys ics and En vi ron men tal Pro tec tion, AGH Uni ver sity of Sci ence and Tech nol ogy,Al. Mick iewicza 30, 30- 059 Kraków, Po land; e- mail: wi [email protected]

2 In sti tute of Geo logi cal Sci ences, Jagiel lo nian Uni ver sity, Ole an dry 2A, 30- 063 Kraków, Po land;e- mail: nestor.oszc [email protected]

Zuchiewicz, W. & Oszc zypko, N., 2008. To pog ra phy of the Ma gura floor thrust and mor pho tec ton ics of the OuterWest Car pa thi ans in Po land. An nales So cie ta tis Ge olo go rum Po lo niae, 78: 135–149.

Ab stract: Neo tec tonic (Plio cene–Qua ter nary) ele va tions and de pres sions de tected on maps of su ben ve lopesur faces of the to pog ra phy of the Outer West Car pa thi ans of Po land are, to a cer tain ex tent, por trayed on the mapshow ing to pog ra phy of the Ma gura floor thrust, par ticu larly in the west ern seg ment of the study area. The floorthrust of the Ma gura Nappe is highly un even, its po si tion chang ing from 725 m a.s.l. to more than 7,000 m b.s.l.The most promi nent de pres sion is lo cated in the me dial (S of Du na jec and Po prad con flu ence) seg ment of thePol ish Outer Car pa thi ans (2–7 km b.s.l.), and its axis trends NW–SE from the east ern mar gin of the Mszana Dolnatec tonic win dow to the Po prad River val ley. An other, much more shal lower, Jor danów de pres sion (2 km b.s.l.) isto be found NW of the Mszana Dolna tec tonic win dow, shortly north of the Skawa River val ley. Ele vatedstruc tures, in turn, in clude the Mszana Dolna tec tonic win dow, Sól–Skomielna (on the west), and Lima nowa (onthe east) ele va tions of sub par al lel ori en ta tion. Still far ther to the east, a lon gi tu di nal ele va tion ex tend ing be tweenthe Klêc zany–Pisar zowa and Œwi¹tkowa tec tonic win dows is to be seen some 10–15 km south of the Ma gurafron tal thrust. South of this area, the Ma gura floor thrust slopes steeply down to more than 4 km b.s.l. Acom pari son be tween the pat tern of ele vated and sub sided struc tures of the Ma gura floor thrust and su ben ve lopesur faces of dif fer ent or ders shows that in the west ern part of the Pol ish Outer Car pa thi ans the highest- elevatedneo tec tonic struc tures (in the south ern por tion of that area) co in cide with de pres sions of the Ma gura thrust,whereas far ther north a re verse pat tern be comes domi nant: neo tec tonic ele va tions co in cide ei ther with the Ma gurafron tal thrust or with ele va tions of its sur face. This is par ticu larly true for an area com prised be tween 20° and20°30’E me ridi ans. The ori gin of such re la tion ships is dif fi cult to ex plain. We in fer that one of pos si ble fac torscould be Plio cene–Qua ter nary re ac ti va tion of faults cut ting the Ma gura floor thrust, and par ticu larly that one,which ap pears to sepa rate the western- medial seg ment of the Outer Car pa thi ans from their more east ern por tion.

Key words: mor pho tec ton ics, neo tec ton ics, Plio cene–Qua ter nary, Ma gura thrust, Outer Car pa thi ans, Po land.

Manu script re ceived 1 September 2008, ac cepted 9 Octo ber 2008

IN TRO DUC TION

The aim of this pa per is to dis cuss mu tual re la tion shipsbe tween the pat tern of up lifted and sub sided neo tec tonicstruc tures in the Pol ish Outer Car pa thi ans with highlychange able to pog ra phy of floor thrust of the Magura Nappe, the most ex ten sive nappe of that re gion. In the Plio cene andQua ter nary, the Outer Car pa thi ans have been sub ject to dif -fer en tial ver ti cal and rem nant hori zon tal move ments re sult -ing in the for ma tion of sev eral neo tec tonic ele va tions andde pres sions (Kli maszewski, 1966; Zuchiewicz, 1991; Zu-chiewicz et al., 2002). The ap par ent amount of Late Neo -gene–Qua ter nary up lift of the me dial seg ment of the stud ied

area, co in cid ing with the great est width of the Ma guraNappe, has ranged from 150–430 m in the south and 360–900 m in the me dial sec tor, to 180–310 m in the north. Thesize of purely Qua ter nary up lift of the south ern part of theMa gura Nappe has been es ti mated for some 150 m (cf.Zuchiewicz, 1984, 1991).

GEO LOG I CAL SET TING

The Outer West Car pa thi ans of Po land rep re sent a typi -cal fold- and- thrust belt (Figs 1, 2), which is com posed of anumber of nap pes piled one upon an other dur ing the Mid dle to Late Mio cene (Ksi¹¿kiewicz, 1977).

The Outer Car pa thian flysch belt was formed as an ac -cre tion ary prism dur ing the southward- directed sub duc tionof the Euro pean plate un der AL CAPA (Pesca tore & Œl¹cz-ka, 1984; Tomek & Hall, 1993; Zo ete meijer et al., 1999,and ref er ences therein), re sult ing in the NW- directed short -en ing, fol lowed by ma jor ro ta tion of ei ther the re gionalstress field (Alek sandrowski, 1985; Decker et al., 1997) orthe belt it self (Már ton et al., 1999; Zuchiewicz et al., 2002).This ro ta tion gave rise to the NE- directed short en ing (Dec-ker et al., 1999) and was post dated in Late Neo gene times

by re gional col lapse ac com pa nied by nor mal fault ing (Dec-ker et al., 1997; Zuchiewicz et al., 2002).

The Magura Nappe is the in ner most tec tonic unit of theOuter West ern Carpathians and it is linked with the Rheno-Danubian flysch of the East ern Alps. The old est, Ju ras sic–Lower Cre ta ceous strata are only known from the Grajcarek thrust-sheet in front of the Pieniny Klippen Belt, the south -ern mar gin of the Mszana Dolna tec tonic win dow (Osz-czypko, 2001, Oszczypko et al., 2005a,b), and from the Mo- ravian sec tor of the Magura Nappe (Švabenick« et al., 1997;

136 W. ZUCHIEWICZ & N. OSZCZYPKO

Fig. 1. Tec tonic sketch of the Outer West Carpathians (based on ¯ytko et al., 1989; sim pli fied). Tec tonic win dows: 1 – Mszana Dolna,2 – Szczawa, 3 – Klêczany–Pisarzowa, 4 – Grybów, 5 – Ropa, 6 – Uœcie Gorlickie, 7 – Œwi¹tkowa, 8 – Smilno

Fig. 2. Phys io graphic units of the Pol ish seg ment of the Carpathians show ing place names men tioned in the text (based on Starkel,1991; mod i fied), as well as the zones of Qua ter nary up lift, marked by ab nor mally high river bed gra di ents (mod i fied from Zuchiewicz,1998, 1999)

Œl¹czka et al., 2006). On the ba sis of fa cies dif fer en ti a tionwith re spect to the Palaeogene de pos its, the Magura Nappehas been sub di vided into four fa cies-tec tonic sub units,namely the Krynica, Bystrica, Raèa and Siary sub units (Fig. 1; see also Koszarski et al., 1974).

Stra tig ra phy

The Up per Cre ta ceous de pos its be gin with Ce no ma -nian/ Tu ro nian varie gated, hemipe la gic mud stones with in -ter ca la tions of thin- bedded tur bid ites. In the Raèa and By-strica subunits, sedi men ta tion of varie gated clays was fin -ished at the San to nian/ Cam panian bound ary, whereas inthe Krynica subunit it still con tin ued in the Maas trichtian(Oszc zypko et al., 2005a). The varie gated shales pass up -wards into thin- bedded tur bid ites with spo radic in ter ca la -tions of thick- bedded sand stones. Higher up in the sec tion,some thin- to medium- bedded tur bid ites, up to 50 m thick,ap pear. These tur bid ites con tain nu mer ous, 5–7 cm to 30 cm thick in ter ca la tions of tur biditic lime stones. These de pos itspass up wards into thick- bedded sand stones and con glom er -ates, which are up to 100–400 m thick. The young est strataof this com plex are of Pa laeo cene age. These de pos its areover lain by a 20–50 m thick com plex of varie gated shales of Early to Mid dle Eo cene age. The varie gated shales pass up -wards into thin- bedded tur bid ites, some few hun dred me tres thick (Oszc zypko, 1991; Oszc zypko et al., 1999). In theKrynica, Bystrica and Raèa subunits, the young est de pos itsof the Eo cene to Oli go cene com plex be long to the Ma guraSand stone Fm., which is of ? Early Eo cene to Oli go ceneage. The thick ness of this for ma tion ranges from 1,200–1,400 m in the the Krynica, through 800–2,000 m in the By-strica, to 1,000 – 2000 m in the Raèa subunits (Ksi¹¿kie-wicz, 1971; Golonka & Wójcik, 1978; Birk en ma jer & Osz-czypko, 1989; Oszc zypko, 1991). The Ma gura Fm. is lo -cally over lain by the Glo bi gerina marls (Up per Eocene–Lower Oli go cene), bi tu mi nous shales, and thin- bedded cal -care ous flysch (Up per Oli go cene). In the north ern most partof the Ma gura Nappe (Si ary subunit), the Mid dle/Up per Eo -

cene varie gated shales pass up wards into marls and thin- bedded flysch with in ter ca la tions of Glo bi gerina marls (Up -per Eo cene–Lower Oli go cene), thick- bedded glau co niticsand stones (W¹tkowa Sand stones) of Early Oli go cene age,and fi nally into marls with in ter ca la tions of glau co niticsand stones (Oli go cene; see Oszczypko- Clowes, 2001). Inthe vi cin ity of Nowy S¹cz and close to the Pi en iny Klip penBelt (Fig. 1), the Lower Mio cene flysch strata of the Ma gura Nappe have re cently been dis cov ered (Ci esz kowski, 1992;Oszc zypko et al., 1999; Oszczypko- Clowes, 2001; Osz-czypko and Oszczypko- Clowes, 2002, Oszc zypko et al.,2005b).

Tec ton ics

In our tec tonic and mor pho tec tonic con sid era tions weac cept tra di tional shape of the front of the Ma gura Nappe inthe Gorlice area, to gether with £u¿na and Harklowa sa li ents (“pen in su las") (Figs 1,6, 7). This idea has re cently beenques tioned by Jan kowski et al. (2004), who in ter pretedthese sa li ents and “Ma gura ero sional ouliers” near the Jas³oas cha otic com plexes. In other in ter pre ta tions these de pos its are re garded as frag ments of the Fore- Magura tec tonic units (see Oszc zypko et al. , 2008).

The Ma gura Nappe is flatly thrust over its fore landwhich is built up of the Fore- Magura group of units andpartly by the Sile sian Unit (Fig. 1). The am pli tude of theover thrust is up to 50 km (Figs 1, 3, 4), and the post- MiddleBade nian thrust dis place ment is more than 12 km (Osz-czypko & Zuchiewicz, 2000; Oszc zypko, 2001, 2006) Thenorth ern limit of the nappe is an ero sional one, whereas thesouth ern limit co in cides with a strike- slip fault along thenorth ern bound ary of the Pi en iny Klip pen Belt (Figs 3, 4).The thrust de vel oped mainly within the duc tile Up per Cre -ta ceous varie gated shales. The sub- thrust mor phol ogy of the Ma gura fore land is very dis tinc tive (Figs 3–5). The shape of the north ern limit of the Ma gura Nappe and the dis tri bu tionof the tec tonic win dows in side the nappe are con nected with the to pog ra phy of the Ma gura base ment. As a rule, the “em -

MORPHOTECTONICS OF THE OUTER WEST CARPATHIANS 137

Fig. 3. Geo log i cal cross-sec tion through the west ern por tion of the Magura Nappe (based on Oszczypko et al., 2006). For lo ca tion seeFig 1. IC – In ner Carpathians, PKB – Pieniny Klippen Belt, OP 1 – Oravska Polhora 1 bore hole

bay ments” of the mar ginal thrust are re lated to trans ver salbulges in the Ma gura base ment, whereas the sa li ents are lo -cated upon the de pres sions (Oszc zypko, 2001, 2006). At adis tance of 10–15 km south of the north ern limit of thenappe, the zone of tec tonic win dows con nected with the up -lifted Fore- Magura base ment is lo cated (e.g., MszanaDolna, Szczawa, Klêc zany, Grybów, Ropa, Uœcie Gor -lickie, and Œwi¹tkowa tec tonic win dows; cf. Fig. 1). TheMa gura Nappe is sub di vided into four struc tural subunits(slices), namely: the Krynica, Bystrica (Nowy S¹cz), Raèa,and Si ary (Fig. 1). The ? Lower Eo cene to Oli go cene flyschstrata of the Raèa and Krynica subunits build broad, W–Etrend ing syn clines and nar row an ti clines. The south ernlimbs of syn clines are of ten re duced and over turned. In theBystrica subunit, sub- vertical thrust- sheets are com mon.Both the north ern limbs of an ti clines and south ern limbs ofsyn clines are tec toni cally re duced and usu ally over turned.In the Krynica and Raèa subunits the young est (Late Eo -cene–Early Oli go cene), weakly de formed, de pos its of theMa gura Nappe rest ucon forma bly upon the older Eo ceneflysch strata (Figs 3–5).

The Ma gura thrust has de vel oped in sev eral stages. Thefirst epi sode of thrust ing oc curred in Late Oli go cene timeswhen the nappe, to gether with the Grybów Unit, was thrustover the Dukla Unit (Oszczypko- Clowes & Oszc zypko,2004). In the early Bur di ga lian, the fron tal part of Ma guraNappe was thrust north wards onto the ter mi nal Krosnoflysch ba sin. This was also ac com pa nied by the for ma tionof a piggy- back ba sin on the Ma gura Nappe, filled with the

Lower Mio cene sy no ro genic tur bid ites of the Za wada andKremna for ma tions (Oszc zypko, 2006).

The sub se quent epi sodes of thrust ing took place in theOtt nan gian and af ter the mid dle Bade nian. The last epi sode,in clud ing some 12 km of thrust ing, was that which con -trolled the present- day in ter sec tion of the thrust and was re -spon si ble for the strike- slip char ac ter of the con tact be tween the Ma gura Nappe and the Pi en iny Klip pen Belt (cf. Osz-czypko, 1998). The post- Badenian thrust ing has fi nallyshaped the du plex struc ture of the Mszana Dolna tec tonicwin dow (Oszc zypko, 2001; Oszczypko- Clowes & Osz-czypko, 2004), be ing post dated by nor mal fault ing (Osz-czypko & Zuchiewicz, 2000), con trol ling sub si dence of theLate Bade nian–Sar ma tian troughs of the Orava–Nowy Targ and Nowy S¹cz ba sins.

BASE OF THE MAGURA NAPPE

The map of the base of the Ma gura Nappe (Fig. 6) wascon structed by one of us (N. Oszc zypko) bas ing on 90 welllogs, as well as on the re sults of nu mer ous ex plo ra tionwells. Well- bore data from the west ern part of the nappe are un evenly dis trib uted, most of them com ing from the north -ern, mar ginal part of the nappe that co in cides with the Raèafa cies zone. This ap plies par ticu larly to the Klêc zany–Pisa-rzowa win dow and the Lima nowa area. The re gion com -prised be tween the Raba and So³a riv ers has also beendrilled ex ten sively, whereas the south ern part of the nappe,


Fig. 4. Geo log i cal cross-sec tion through the me dial seg ment of the Magura Nappe (based on Oszczypko, 2006). For lo ca tion see Fig. 1.

namely the Krynica fa cies zone, still re mains to be stud ied.The only well from that area, lo cated near Nowy Targ (Figs1, 2; cf. Paul & Po prawa, 1992), did not pro duce une quivo -cal re sults, al though it did docu ment that the thick ness ofthe Ma gura Nappe ex ceeds here 3.8 km. To the east of theDu na jec River, well- bore data are rela tively scarce, be ingcon cen trated near Gor lice, within the Si ary and north ernpart of Raèa zones. The re main ing fa cies zones be tween theDu na jec–Po prad and Ropa riv ers (south ern Raèa, Bystrica,and Krynica zones) have not been drilled yet.

To the west of the Du na jec River (Figs 3, 6), the Ma -gura Nappe is rela tively steeply thrust over its fore land, i.e.the Sile sian Nappe, and west of the So³a River also over theFore- Magura thrust- sheets. The Grybów Unit builds thebase of the Ma gura Nappe within the Klêc zany–Pisar zowa,Mszana Dolna, and Szczawa tec tonic win dows (Figs 4, 6).The Grybów Unit has also been drilled by nu mer ous wellsnear Lima nowa (cf. Po³towicz, 1985), where it forms threeslices com posed of the Krosno, Menil ite, Grybów, sub- Grybów, and Klêc zany beds. The thick ness of this unitchanges from a few hun dred me tres to a few kilo me tres,whereas shortly south of the Mszana Dolna tec tonic win -dow its thick ness is re duced to some 100 m only. Views onthe ori gin of more outer units are strongly dif fer en ti ated. Itis gen er ally ac cepted that im me di ately be low the GrybówUnit, the Dukla Unit is to be found. The lat ter unit has beende scribed from a few wells (Figs 1, 4). The af fin ity ofLower Cre ta ceous strata, mostly the Lgota beds, drilled by a few wells south of Lima nowa (Fig. 1) is not clear.

In the west ern part of the Outer Car pa thi ans, the to pog -ra phy of the Ma gura ba sal thrust is domi nated by the

Mszana Dolna ele va tion and the Nowy S¹cz and Orawa–Nowy Targ ba sins (Figs 3, 4, 6, 7). The Mszana Dolna ele -va tion ex tends 20 km N–S and 25 km E–W (Figs 1, 6). Thisele va tion con tains two cul mi na tions, which are co in ci dentwith the Mszana Dolna and Szczawa tec tonic win dows. The former shows an iso met ric shape and is ca. 10 km across. Inthe mid dle part of the win dow, strata be long ing to theDukla–Grybów Unit are ex posed at 725 m a.s.l. A small tec -tonic win dow of Szczawa is situ ated on the east ern slope ofthe ele va tion (Figs 1, 6). It is only 1 km across, and in itshighest- elevated part the Grybów Unit de pos its are ex posedat 550 m a.s.l. The Mszana Dolna ele va tion builds a du plexstruc ture. Out side the ele va tion, the Ma gura ba sal thrustdips at ca. 25° in all di rec tions, ex cept to the north. To thesouth, near Nowy Targ, and east (close to Nowy S¹cz), thethrust sur face slopes down to ca. 4 km b.s.l.

The Mszana Dolna ele va tion (Figs 6, 7) is linkedthrough nar row pas sages with two other ele va tions ofSól–Skomielna and Lima nowa. The Sól–Skomielna ele va -tion, ex tend ing across the Oravska Pol hora re gion, is up to 5 km wide and strikes roughly E–W (Fig. 7). The Lima nowaele va tion, in turn, is sepa rated from the Mszana Dolna ele -va tion by a trans ver sal (NNW–SSE) S³opnice–Leœniówkazone of rapid thick ness change, also 5 km wide (Po³towicz,1985). The Klêc zany–Pisar zowa tec tonic win dow builds acul mi na tion of the Lima nowa zone. Strata of the GrybówUnit near Klêc zany are ele vated as high as 500 m a.s.l.

The Lima nowa, Mszana Dolna, and Sól–Skomielnabelt of ele va tions is sur rounded on the north and south byde pres sions (Fig. 7). The north ern ones are rep re sented by:Ja worzna (–1,209 m b.s.l.), Jor danów (–2,470 m b.s.l.), and

MOR PHO TEC TON ICS OF THE OUTER WEST CAR PA THI ANS 139

Fig. 5. Geo log i cal cross-sec tion through the east ern por tion of the Magura Nappe (based on Oszczypko et al., 1998; mod i fied). For lo -ca tion see Fig. 1

Bystra (–1,148 m b.s.l.) de pres sions. Be tween the Jor danów and Bystra de pres sions, the trans ver sal Oravska Polhora–Lachowice ele va tion (–230–550 m b.s.l.) oc curs. Par ticu -larly high re lief of the base of Ma gura thrust is to be ob -served be tween the Mszana Dolna ele va tion and Jor danówde pres sion, where the base of the Ma gura Nappe slopes bymore than 3 km at a dis tance of 20 km. The south ern belt of

de pres sions is poorly rec og nized. The only data come fromtwo deep wells (Hanušovce-1, Nowy Targ IG-1), which didnot drilled the en tire Ma gura Nappe (Figs 1, 2). The bore -hole Nowy Targ IG-1 proba bly reached the back- thrust ofthe Ma gura Nappe onto Grajcarek thrust- sheet, at a depth of 3,853 m. It can be con luded that the base of the Ma guraNappe at the con tact with the Pi en iny Klip pen Belt is placed


Fig. 6. To pog ra phy of the Magura floor thrust. Num bers re fer to tec tonic win dows shown in Fig. 1. Dif fer ent shades of grey in di catedis tance be tween the Magura floor thrust and sea level

Fig. 7. El e va tions and de pres sions in the base of the Magura Nappe. Num bers re fer to tec tonic win dows shown in Fig. 1. El e va tions: S– Sól, Sk – Skomielna, OP-La – Oravska Polhora – Lachowice, MD – Mszana Dolna, Li – Limanowa; De pres sions: By – Bystra, J –Jordanów, Ja – Jaworzna; S-L – S³opnice – Leœniówka zone

at ca. –6 km b.s.l. in East ern Slo va kia, and at around –4 kmb.s.l. near Nowy Targ. The prob lem of depth dif fer en tia tionof the base of Ma gura Nappe can only be solved by newseis mic sound ings.

The to pog ra phy of the base of the Ma gura Nappe in flu -ences as well the strike of its fron tal thrust. Ele vated por -tions of the Ma gura Nappe are marked at the sur face by con -cave to wards the south, bay- like curves of the fron tal thrust, whereas the de pres sions are re flected by “pen in su las” ofthis nappe. Such a re la tion ship, how ever, is not so well- marked as in the east ern part of the Outer Car pa thi ans.

To the east of the Du na jec River, the Ma gura Nappe isflatly thrust over its fore land, which is com posed of theSile sian Nappe and Dukla–Grybów Unit (Figs 5–7). Mor -pho logi cal dif fer en tia tion of the base of the Ma gura Nappeis well marked in the strike of its fron tal thrust, form ingchar ac ter is tic “em bay ments” and sa li ents. The “em bay -ments” are re lated to up lifted parts of the fore land, the sa li -ents co in cide with trans ver sal de pres sions. Ele va tion dif fer -ences be tween the “em bay ments” and sa li ents do not ex -ceed 250 m. To the east, the dip of the Ma gura fron tal thrustin creases mark edly, as docu mented by wells drilled nearRopi anka.

Some 10–15 km south of the Ma gura fron tal thrust, abelt of tec tonic win dows lo cated upon a lon gi tu di nal base -ment ele va tion is to be found. This zone, 4–6 km wide, be -gins on the west in the Klêc zany–Pisar zowa win dow, andcon tin ues far ther east through a half- window north of Nowy S¹cz, and the Grybów–Ropa–Uœcie Gor lickie and Œwi¹tko-wa win dows (Figs 1, 6, 7). To the south of the Uœcie Gor -lickie and Œwi¹tkowa tec tonic win dows, the base of the Ma -gura Nappe rap idly slopes down to 4,200 m b.s.l. inSmilno-1 well in Slo va kia. This well has docu mented thatthe po si tion of the Smilno tec tonic win dow is proba bly dif -fer ent from those near Gor lice. South of Gor lice, the tec -tonic win dows are clearly as so ci ated with base ment highs,whereas the Smilno win dow is de tached from its base mentand em bed ded into one of the Ma gura slices. South of Smil-no, the base of the Ma gura Nappe has not been drilled yet.One can sup pose that this base near Pi en iny Klip pen Beltcan be placed at depths rang ing from 7 to 10 km. This hy -pothe sis is con firmed in part by the re sults of the Hanu-šovce-1 well (6,003 m deep) in East ern Slo va kia, whereinthe Pi en iny Klip pen Belt has been drilled through at a depthof 4 km b.s.l., whereas the Ma gura Nappe has not beendrilled down to its base. We in fer, there fore, that also in theSE part of the Ma gura Nappe in Po land, its base is proba blyplaced at depths of 4 to 7 km. In the Nowy S¹cz Ba sin, inturn, where the thick ness of Mio cene mo las ses is up to 600m, the base of the Ma gura Nappe must be lo cated at a depthof at least 3–3.5 km.

To sum ma rise, the floor thrust of the Ma gura Nappe ishighly un even, its po si tion chang ing from 725 m a.s.l. tomore than 7,000 m b.s.l. (Figs 6, 7). The most promi nent de -pres sion is lo cated in the me dial seg ment of the Pol ish Outer Car pa thi ans (2–7 km b.s.l.), and its axis trends NW–SEfrom the east ern mar gin of the Mszana Dolna tec tonic win -dow to the Po prad River val ley. An other, much more shal -lower, Jor danów de pres sion (2 km b.s.l.) is to be found NWof the Mszana Dolna tec tonic win dow, shortly north of the

Skawa River val ley. Ele vated struc tures, in turn, in clude the Mszana Dolna tec tonic win dow, Sól–Skomielna (on thewest), and Lima nowa (on the east) ele va tions of sub par al lelori en ta tion. Still far ther to the east, a lon gi tu di nal ele va tionex tend ing be tween the Klêc zany–Pisar zowa and Œwi¹tkowa tec tonic win dows is to be seen some 10–15 km south of theMa gura fron tal thrust. South of this area, the Ma gura floorthrust slopes steeply down to more than 4 km b.s.l.

MORPHOTECTONIC PAT TERNOF THE OUTER CARPATHIANS

The stud ies fo cus ing on de for ma tion of pla na tion sur -faces of Late Mio cene, Early and Late Plio cene and EarlyQua ter nary age, as well as Qua ter nary flu vial ter races havemade it pos si ble to dis tin guish a number of ele vated andsub sided struc tures of rela tively small widths (15–20 km)and sub par al lel ar range ment with re spect to the strike ofprin ci pal thrusts and im bri cated folds. These struc turesproba bly origi nated due to Plio- Quaternary re laxa tion ofhori zon tal move ments within the flysch nap pes, lead ing tothe steep en ing of fron tal thrusts and open fold ing above ter -mi nal thrust planes (cf. Zuchiewicz, 1998; Zuchiewicz etal., 2002). The maxi mum size of Qua ter nary up lift has beenfrom 150 m in the Be skid S¹decki Mts. to 50–100 m in theother re gions (Zuchiewicz, 1984, 1995), whereas the over -all, mini mum am pli tude of post- tectonic up lift dur ing thepast 10 to 11 mil lion years has been cal cu lated for some1 km in the West Be skidy Mts. to 260–360 m in the Car pa -thian Foot hills (Oszc zypko, 1996; Zuchiewicz et al., 2002).The dis tri bu tion of Bou guer grav ity anoma lies points togen er ally non- isostatic pro cesses caus ing this up lift, rang -ing from 250 m to 550 m (Zo ete meijer et al., 1999).

The rates of re cent ver ti cal crus tal mo tions in the Pol ish Outer Car pa thi ans range be tween 0 mm/yr in the west ernand me dial seg ments to ca. +1 mm/yr in the east (Wyrzy-kowski, 1985), while those in the Pi en iny Klip pen Belt donot ex ceed 0.5 mm/yr (cf. Czar necki, 2004). The re sults ofre cent GPS cam paigns (Hefty, 2007) as well as bore holebreak out analy ses (Ja ro si ñski, 1998, 2005) point, in turn, toNNE- directed hori zon tal mo tions through out the area.

Dif fer en ti ated val ues of mor phomet ric pa rame ters char -ac ter iz ing the present- day to pog ra phy pro vide in di rect evi -dence in fa vour of di ver si fied neo tec tonic ten den cies.Analy sis of river- bed gra di ents, Hor to nian in di ces, hyp so -met ric curves and hyp so met ric in te grals, drain age ba sinasym me try, val ley floor width to val ley height ra tios, moun -tain front sinu os ity, and other pa rame ters proved help ful iniden ti fi ca tion of up lifted and sub sided zones in the Pol ishseg ment of the Outer Car pa thi ans (cf. Zuchiewicz, 1995,1999; and ref er ences therein).

In 1965, Kli maszewski pub lished a map show ing gen -er al ized to pog ra phy of the Outer Car pa thian drain age pat -tern by plot ting con tours of the main river val ley bot toms.This pat tern sug gested dif fer en ti ated Plio cene–Qua ter naryup lift of the Outer West Car pa thi ans, since the ele va tions ofval ley bot toms rose from 200 m a.s.l. in the foot hills area up to 400–500 m a.s.l. in the Be skidy Mts. A simi lar tech niquewas ap plied by Jahn (1992) to the East Car pa thi ans.



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An other car tomet ric ap proach to mor pho logi cal mani -fes ta tions of young tec tonic ac tiv ity is rep re sented by con -struc tion of en ve lope and su ben ve lope maps (Dury, 1951;Fi lo so fov, 1960; Pan ne koek, 1967; R¹czkowski et al.,1984; Kel ler & Pin ter, 1996; and ref er ences therein). Theformer por tray the high est ele va tions of ter rain, the lat ter re -con struct the level to which the streams have eroded by con -nect ing points of equal ele va tion be tween the streams. A se -ries of such su ben ve lope maps pro duced for drain age net -works, clas si fied ac cord ing to the Horton- Strahler hi er ar chy and called base- level sur face maps, makes it pos si ble tocom pute maps of re sidu als be tween in di vid ual sur faces ofdif fer ent or ders and to hy pothe size about ei ther up lift orsub si dence ten den cies, in di cated by dense or sparse pat ternof iso bases and in creased or de creased re lief por trayed onre sid ual maps (cf. R¹czkowski et al., 1984; Zuchiewicz &Oaks, 1993). Re li able in ter pre ta tion of such maps, how ever, is im pos si ble with out knowl edge about the number and ageof geo mor phic cy cles that af fected the study area. There -fore, both en ve lope and su ben ve lope maps should com ple -ment tra di tional geo mor phic map ping (see, for in stance, ar -gu ments listed by Starkel, 1985).

The 4th- order su ben ve lope (base- level) map, origi nallycon structed at the scale of 1:100,000, shows sev eral ar eas of high iso base con cen tra tion, in clud ing the up lifted Be skid¯ywiecki, Ta tra, Pi en iny, Gorce, Be skid S¹decki, and Bie-szczady Mts. (Figs 2, 8). Broadly- spaced iso bases within in -tra mon tane de pres sions are in dica tive of sub sid ing ten den -cies. The 5th- order map, in turn, dis plays two re gions ofcon trast ing iso base pat tern (Fig. 9). In the west ern area iso -bases of 250 to 850 m a.s.l. run close to one an other; theeast ern area is char ac ter ized by low iso base den sity andlower ele va tions (200–700 m a.s.l.). Slightly higher ele va -tions (650–750 m a.s.l.) oc cur only in the ax ial part of theBi eszc zady Mts. The 6th- order map shows a dis tinct bound -ary be tween the West and East Car pa thi ans (Fig. 10). In thewest ern part, a south ern re gion en cir cled by the 550 m a.s.l.iso base, is well pro nounced. Far ther to the north, base- levelval ues di min ish to 250 m a.s.l. Iso bases are broadly spacedwithin the in tra mon tane de pres sions of ¯ywiec and NowyS¹cz. The gen eral E–W trend ing pat tern of iso bases is dis -turbed by “de pres sions” as so ci ated with trans ver sal, deeply- cut val leys of So³a (NNE–SSW), Du na jec (NNE– SSW),and San (NW–SE) riv ers.

Base- level sur faces of dif fer ent or ders are very dif fi cult to date: in many cases they rep re sent dif fer ent frag ments ofa ma ture land scape, formed dur ing dif fer ent time- spans(like, for in stance, up per val ley reaches within wa ter shedar eas), al though be ing as signed to one base- level sur face.One can only in fer that the 6th- order su ben ve lope (base-le-vel) map por trays, roughly, the Late Mio cene/Early Plioce-ne to pog ra phy of the stud ied area (cf. R¹czkowski et al.,1984). Dif fer ences among base- level maps of dif fer ent or -ders ap pear to re flect both litho logi cal con trol and youngtectonic pro cesses. The up lifted re gions are marked on maps of re sidu als as lon gi tu di nal ele va tions (Be skid ¯ywiecki,Ta tra, Be skid S¹decki, S³onne Mts.) or block/dome- like up -lifts (Gorce Mts., west ern Bi eszc zady Mts., Be skid Œl¹skiMts.).

Sum ming up, the hitherto- published geo mor pho logi cal

maps of the Pol ish Car pa thi ans fea ture a few lon gi tu di nalele vated ar eas (Starkel, 1980; R¹czkowski et al., 1984;Zuchiewicz, 1995). More promi nent sub sid ing struc turesare lo cated along the So³a River course, in the Orava–Nowy Targ Ba sin, in the Jas³o–Sa nok De pres sion, and fol low ingthe lower course of the San River val ley in the east ern por -tion of the Outer Car pa thi ans.

MORPHOTECTONIC STRUC TURESVER SUS MAGURA FLOOR THRUST

The present- day dif fer en ti ated mor phol ogy of the Ma -gura Nappe floor thrust strongly con trasts with very regu lar, SE deep en ing, Mid dle/Late Mio cene floor thrust of the Pol -ish Outer Car pa thi ans (see Oszc zypko & To maœ, 1985;Behrmann et al., 2000). In the west ern part of the OuterWest Car pa thi ans, the base of the Ma gura Nappe dis playsstrongly dif fer en ti ated and thrust upon ramp- flat mor phol -ogy of the base ment (cf. Nemèok et al., 2000). The nappe isun der lain here by a strongly re duced in thick ness equiva lent of the Dukla Unit, which, in its more east ern part, is rep re -sented by rela tively thick rock com plex of un dif fer en ti ated,smooth top sur face (Behrmann et al., 2000). This sug gestsmulti- stage de vel op ment of the Ma gura Nappe floor thrust.The pro cess of over thrust ing was ini ti ated dur ing the LateOli go cene when the front of the Ma gura Nappe reached, un -der sub ma rine con di tions, the Dukla–Grybów sedi men taryarea (Oszczypko- Clowes & Oszc zypko, 2004). Dur ing theEg gen bur gian, the front of the Ma gura Nappe reached thesouth ern part of the Sile sian Ba sin (Oszc zypko et al., 1999;Oszc zypko & Oszczypko- Clowes, 2002).

Dur ing the Mid dle Mio cene thrust ing, a large SW–NEtrend ing du plex struc ture be gan to de velop at the front ofthe Ma gura Nappe against its fore land (cf. Roca et al., 1995; Behrmann et al., 2000). This du plex zone, marked by a zone of tec tonic win dows within the Ma gura Nappe, is com posed of im bri cated horses of the Grybów Unit, de vel oped be -tween two thrust sur faces: the floor thrust sur face formedalong the fron tal ramp of the Dukla Unit, and the roof thrustsur face re lated to the Ma gura Nappe (Oszczypko- Clowes & Oszc zypko, 2004). The same mecha nism of the Ma guraNappe thrust ing was sug gested by Mas tella and Rubinkie-wicz (1998) in the Œwi¹tkowa tec tonic win dow. The lastepi sode of pro gres sive thrust ing (about 10–15 km) of theMa gura Nappe to wards the north took place dur ing the LateMio cene (Late Bade nian /Sar ma tian, 9–10 Ma), where thehinge zone of the du plex struc ture was pushed by the frontof the Ma gura Nappe (see Ci esz kowski et al., 1988; Osz-czypko, 1998). These move ments proba bly re sulted in thede vel op ment of a sin is tral, tran spres sional strike- slip- faultzone along the front of the Ma gura Nappe in its NW part(cf. Nemèok et al., 2000).

In the West Car pa thi ans, ele vated mor pho tec tonicstructures re con structed ow ing to analy sis of geo mor phicin di ces, like: ab nor mally high river bed gra di ents or val leyfloor width- valley height ra tios, ap pear to cor re late with thezone of tec tonic win dows, i.e. ele vated struc tures at the base of the Ma gura thrust. This is also true for an area situ atedeast of the Du na jec River, par ticu larly in a re gion placedeast of Gor lice (Figs 2, 7), al though to a mi nor ex tent.



Fig. 11. Cross-sec tions through base-level (subenvelope) sur faces of dif fer ent or ders ver sus to pog ra phy of the Magura floor thrust

On the other hand, a com pari son be tween the pat tern ofele vated and sub sided struc tures of the Ma gura floor thrustand su ben ve lope su faces of dif fer ent or ders shows that inthe west ern part of the Pol ish Outer Car pa thi ans (Fig. 11)the highest- elevated neo tec tonic struc tures (in the south ernpor tion of that area) co in cide with de pres sions of the Ma -gura thrust, whereas far ther north a re verse pat tern be comesdomi nant: neo tec tonic ele va tions co in cide ei ther with theMa gura fron tal thrust or with ele va tions of its sur face. Thisis par ticu larly true for an area com prised be tween 20° and20°30’E me ridi ans. Moreo ver, the strongly up lifted re gionin this part of the Outer Car pa thi ans, i.e. the Gorce Mts., issitu ated shortly south of the main ele va tion of the Ma gurafloor thrust, rep re sented by the Mszana Dolna tec tonic win -dow. Far ther to the east, no clear re la tion ship be tween thedis cussed sur faces can be seen, ex cept for that the high estorogen- parallel neo tec tonic struc tures ap pear to co in cidewith the great est thick nesses of the Ma gura Nappe (Figs 6,7, 11).

CON CLU SIONS

The ori gin of above- discussed re la tion ships is dif fi cultto ex plain. We in fer that one of pos si ble fac tors could bePlio cene–Qua ter nary re ac ti va tion of faults cut ting the Ma -gura floor thrust, as well as the ba sal thrust of the Outer Car -pa thi ans, and par ticu larly that which ap pears to sepa rate thewestern- medial seg ment of the Outer Car pa thi ans from themore east ern por tion. This zone, proba bly mark ing thebound ary be tween the Up per Sile sian and Ma³opol skablocks in the Car pa thian base ment and roughly co in ci dentwith the Du na jec fault (cf. Birk en ma jer, 1979; Jure wicz etal., 2007), strikes NW–SE be tween Lima nowa and the Po -prad River val ley, di vid ing re gions show ing con trast ing pat -tern of both su ben ve lope sur faces and the Ma gura floorthrust. A simi lar con clu sion has been pro posed by Zuchie-wicz et al. (2002) when ana lys ing mor phomet ric pa rame ters of up lifted neo tec tonic struc tures in the west ern and east ernpor tions of the Outer West Car pa thi ans, whose en eche lonar range ment is dif fer ent on ei ther side of a re ac ti vated,proba bly dex tral deep fault zone lo cated be neath the over -thrust nap pes. The zone in ques tion is called some times theKraków–Lubliniec fault zone (¯aba, 1999), be ing re spon si -ble for en tirely dif fer ent struc tural style of the Up per Sile -sian and Ma³opol ska blocks un der ly ing the over thrust Car -pa thi ans, and which has been re ac ti vated in late Cai no zoictimes, up to the Holo cene (cf. Jure wicz et al., 2007).

Ac knowl edge ments

We would like to ex press our grat i tude to Profs. MarekCieszkowski and Jan Golonka for their crit i cal com ments, whichim proved this pa per. The pa per was fi nanced from stat u tory funds(pro ject 11.11.140.560) of the Fac ulty of Ge ol ogy, Geo phys icsand En vi ron men tal Pro tec tion, AGH Uni ver sity of Sci ence andTech nol ogy (to WZ), and by the Pol ish Min is try of Sci ence andHigh Ed u ca tion (Grant 1997/PO1/2006) to (NO).

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