Annales Societatis Geologorum Poloniae (2011), vol. 81: 221–239.

PRECAM BRIAN AND PALAEOZOIC BASE MENT OF THE CARPATHIAN FOREDEEP AND THE ADJA CENT OUTER CARPATHIANS (SE POLAND AND WEST ERN UKRAINE)

Zbigniew BU£A & Ryszard HABRYN

Polish Geolog i cal Insti tute – Nati onal Re search Insti tute, Upper Silesian Branch, Królowej Jadwigi 1, 41-200 Sosnowiec, Poland, e-mails: [email protected], [email protected]

Bu³a, Z. & Habryn, R., 2011. Pre cam brian and Palaeozoic base ment of the Carpathian Foredeep and the ad ja cent Outer Carpathians (SE Poland and west ern Ukraine). Annales Societatis Geologorum Poloniae, 81: 221–239.

Ab stract: In south-east ern Po land and west ern Ukraine, the Outer Carpathian orogen and the Carpathian Foredeep de vel oped in the fore land of the East-Eu ro pean Plat form (Baltica). The area con sists of a number of tec tonic units in cluded in the Trans-Eu ro pean Su ture Zone (TESZ): the £ysogóry–Radom and Ma³opolska blocks in the ter ri tory of Poland, and the Rava Rus’ka Zone, Kokhanivka Zone and Le¿ajsk Massif in the Ukraine. The de vel op ment of the TESZ be gan in the (?Middle) Late Neoproterozoic and was as soci ated with rift ing pro cesses tak ing place along the west ern edge of the East-Eu ro pean Craton (Baltica) dur ing the break-up of the Rodinia/ Pannotia supercontinent. The pas sive mar gin of Baltica evolved into the TESZ during collisional and/or strike-slip movements . In the TESZ (Ma³opolska Block and Le¿ajsk Massif), Ediacaran flysch-type siliciclastics were af fected by weak meta morphism and folding dur ing the Cadomian orog eny. The de vel op ment of Cambrian de posits in the East-Eu ro pean Craton, £ysogóry–Radom Block, north east ern part of the Ma³opolska Block (Kielce Fold Belt) and in the Rava Rus’ka and Kokhanivka zones was as soci ated with the post-rift ther mal subsi dence. Tec tonic move ments (so-called Sandomierz phase), which oc curred prob a bly due to an oblique col li sion of the Ma³opolska Block (in cluded into the pas sive mar gin of Baltica) and the East-Eu ro pean Craton dur ing late Middle Cambrian to Late Cam brian (pos sibly also Early Ordo vi cian) times, re sulted in the fol lowing: (1) de vel opment of strati graphical (?ero sional) gaps in the Middle and Up per Cam brian sec tions of the Lublin–Podlasie slope of the East-Eu ro pean Craton and the Kielce Fold Belt in the Ma³opolska Block; (2) in tense tec tonic sub sidence of the £ysogóry–Radom Block dur ing the de po sition of Mid dle and Up per Cam brian sed i ments; (3) de vel opment of compressional folds in the Lower Cambrian to lower Mid dle Cam brian de posits of the Kielce Fold Belt on the Ma³opolska Block. Ordo vi cian–Si lu rian se ries were de posited in a typi cal flexural foredeep ba sin, in which sub si dence and de po si tion rates ac cel er ated dur ing Late Si lu rian (Lud low–Pridoli) and Early De vo nian (Lochko- vian) times. It is postu lated that the present po sition of the Ma³opolska Block rel a tive to the £ysogóry–Radom Block and East-Eu ro pean Craton re sulted from post-Silu rian dextral movements be tween the Ma³opolska Block and the East-Eu ro pean Craton. De vonian–Car bonif er ous de posits oc cur only in the Ma³opolska Block lo cated in the Variscan fore land. The Mid dle-Late De vo nian and Early Car bon if er ous shal low-ma rine car bon ate plat forms de vel oped un der an extensional re gime. The siliciclastic Up per Visean–Lower Namurian A Culm se ries were de posited in the flex ural Variscan fore land ba sin. Dur ing the Late Namurian A, the Ma³opolska Block was up lifted in re sponse to the build-up of compressional fore land stresses. Dur ing post-Car bon if er ous times, the Pre cam brian and Palaeozoic de posits were sub ject to ero sion and re struc tur ing dur ing the Al pine orog eny.

Key words: base ment, Carpathians, Carpathian Foredeep, East-Eu ro pean Plat form, Trans-Eu ro pean Su ture Zone, south-east ern Po land, west ern Ukraine.

Manu script re ceived 16 February 2011, ac cepted 13 October 2011

IN TRO DUC TION In the flexural Carpathian foreland ba sin and under the The Pre cam brian and Palaeozoic (ex clud ing Perm ian) Outer Carpathians of south-east ern Poland and west ern serie s of this area form part of the Ma³opolska and £yso- Ukraine, deep boreholes provide control on the distri buti on góry–Radom blocks (terranes ) of Poland and the Le¿ajsk of vari able thick nesses of Palaeozoic sed im ents (Cambrian Mas sif and Kokhanivka and Rava Rus’ka zones of the to Car bon if er ous) and the Pre cam brian base ment be neath Ukraine. These tectono-sedi m entar y units form part of the the Permian and Me so zoic se ries (Fig. 1). Palaeozoic de pos - Trans-Euro pean Suture Zone (TESZ) that extends along the its are only exposed in the Holy Cross Mts. area, to the north south-western margin of the East-Euro pean Craton (Bal- of the Carpathian Foredeep. tica), and which are com monly treated as parts of the Pala- 222 Z. BU£A & R. HABRYN , . l a

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eozoic (epi-Variscan) Plat form of cen tral and western Eu - thian to the southeast from Kraków in the di recti on of Smil- rope, also re ferred to as the West-Eu ro pean Plat form (e.g., no in Slovakia. The northeas tern boundary of the Ma³opol- Kruglov & Tsypko, eds, 1988; Mizerski & Stupka, 2005; ska Block, at the contac t with the £ysogóry–Radom Block, Oszczypko et al., 2006). is marked by the Holy Cross Fault, which is well define d in Sed i men tary-di a strophic pro cesses, oc cur ring at dif fer- the Holy Cross Mts. in the area between Kielce and Sando- ent times (from Precam brian to Carbon if er ous) and with mierz (Fig. 1). differ ent inten sit y within each of the above-menti oned tec- Var i ous in ter pre ta tions have been ad vanced for the tonic units, which should be treated as sepa rat e lithospheric south-east ward conti nu a ti on of the Holy Cross Fault (e.g., units, result ed in the observe d differ ence s in their geolog i - Tomczyk, 2000; Modliñski & Szymañski, 2005; Poprawa, cal struc ture. The boundari es be tween these units are 2006b; Narkiewicz, 2007; Narkiewicz et al., 2007) into the marked by re gional, re peat edly re acti vated fault zones, gen - area where Palaeozoic rocks oc cur at large depths be neath er ally of a strike-slip na ture. the Neogene cover of the Carpathian Foredeep and where Lim ited control on the strati graphical posi ti on and li- this area is deli neat ed on the basis of both geophys i cal and thlogical char ac ter is tics of Pre cam brian and Palaeozoic se - geo log i cal in ves ti ga tions. In this pa per we ad here to the ries occur ring in this area render it diffi cult to deci pher the course of the Holy Cross Fault as shown in the geolog i cal and tec tonic devel op m ent of the differ ent units, giving rise to struc tural maps of the Precam brian and Palaeozoic base ment quite sig nif i cant dif fer ences in views con cern ing their pala- of the Outer Carpathians and Carpathian Foredeep (Bu³a & eotectonic and palaeogeographical evolu ti on and the age of Habryn, eds, 2008) and with refer ence to the views of Tom- their con sol i da tion. Dis crep an cies also con cern the course czyk (2000) and Modliñski and Szymañski (2005), suggest - of bound aries be tween the in di vid ual tec tonic units. ing that it runs from Sandomierz towards Lubaczów, where it This paper at tempts to clarify some of the contro ver sie s approache s the border with the Ukraine (Figs 1, 2). regard ing the above-menti oned problem s on the tec tonic In that area of the Ma³opolska Block that coin cide s with po si tion and palaeogeographical and tec tonic de vel op ment the marginal part of the Outer Carpathians and Carpathian of the Pre cam brian and Palaeozoic suc ces sion in the base - Foredeep, Precam brian (Ediacaran) rocks and var ious in ment of the Carpathian Foredeep and in the marginal part of age Palaeozoic depos it s subcrop at the sub-Perm ian–Meso - the Outer Carpathians in SE Poland and west ern Ukraine, zoic or sub-Cainozo ic (Miocene ) uncon form ity (Fig. 2). and to de velop a coher ent model of the geolog i cal struc ture The Palaeozoic sed im ents of this area were re peat edly sub - in the area. For this purpose, publi shed re sults of litho logi c, ject to tectoni c defor m ati on and erosion, result ing in the de - strati graphic, tectoni c and mapping were used and supple - velop m ent of a “mosai c” patter n of horsts upheld by Edia- mented by the result s of lithological, sedi m entar y, petrogra- caran depos it s and older rocks within the Devo nian–C ar- phic and palynological studies on drill cores acquire d from bon if er ous cover se ries (Fig. 2). sev eral bore holes. Of par tic u lar im por tance are the re sults There is a clear vari abil ity in the struc tural style of the of palynological studies carrie d out on rock sam ples previ - Palaeozoic sed im en tary cover of the Ma³opolska Block. In ously con sid ered Precam brian or Early Palaeozoic in age, its north-east ern part adja cent to the Holy Cross Fault Zone, which per mitted to ver ify their strati graphical po si tion encom passing the Kielce region of the Holy Cross Mts. and (Jachowicz-Zdanowska, 2011). the area be tween Sandomierz and Lubaczów, the Palaeo- zoic suc ces sion (rep re sented by the Cam brian, lo cally Or - do vi cian and Si lu rian de pos its and De vo nian–Car bon if er- TECTONIC PO SI TION OF THE PRE- ous rocks of the Kielce re gion – Fig. 2) shows fold or fold- CAM BRIAN AND PALAEOZOIC ROCKS and-block style of the geolog i cal struc ture. A zone of such struc tures observe d in this part of the Ma³opolska Block has In SE Poland, the basem ent of the marginal part of the been disti nguishe d by Bu³a et al. (2008) as a sep arate tec- Outer Carpathians and Carpathian Foredeep is rep re sented tonic unit called the Kielce Fold Belt (Fig. 1). In the re main- by Pre cam brian and Palaeozoic rocks of the south eastern ing area of the Ma³opolska Block, grabens, half-grabens, part of the Ma³opolska Block and the south-west ern part of horsts and half-horsts pre dom i nate, in volv ing Ediacaran the £ysogóry–Radom Block (Fig. 1). and Palaeozoic (Or do vi cian to Car bon if er ous) rocks. A pro- minent struc ture is a vast horst extend ing betwee n Baranów Sandomierski and Przemyœl, com posed of Ediacaran rocks, Ma³opolska Block referred to as the Lower San Anticlinorium or Lower San This unit, which include s the Kielce re gion of the Holy Ele va ti on (Figs 1, 2) (Karnkowski & O³tuszyk, 1968; Cross Mts. (Po¿aryski et al., 1992; Po¿aryski & Tomczyk Po¿aryski & Tomczyk, 1968). 1993), is flanked to the southwest by the Upper Silesian Block (Brunovistulicum), from which it is sepa rat ed by the £ysogóry–Radom Block well-define d Kraków-Lubliniec Fault Zone (Fig. 1; Bu³a et al., 1997; ¯aba, 1999; Bu³a & ¯aba, 2005; Bu³a & Habryn, This unit is flanked to the SW by the Ma³opolska Block eds., 2008), proba bly form ing part of the prom inent Ham - and to the NE by the East-Euro pean Craton. On the margin burg–Kraków trans con ti nen tal fault zone (Brochwicz- of the lat ter the De vo nian–Car bon if er ous Lublin Ba sin de- Lewiñski et al., 1983; Oberc 1993; Bu³a & ¯aba, 2005; veloped that extends into the terri tory of Ukraine as the Bu³a et al., 2008). Accord ing to Pietsch et al. (2010), this L’viv Trough (Fig. 1). The south-western boundary of the fault zone conti nues in the basem ent of the Outer Carpa- Lublin Basin, of which the Lublin Trough forms the axial 224 Z. BU£A & R. HABRYN

part, is usuall y identi fied in Poland with the Ursynów-Kazi- glov and Tsypko, eds, (1988) and Stupka (1991) (cf. Mizer- mierz and Izbica–Zamoœæ faults (e.g., Jaworowski & Si- ski & Stupka, 2005). Local ly – in the Verchany–Derzhiv re- korska, 2006; ¯elaŸniewicz et al., 2009). Narkiewicz et al. gion – Or do vi cian and Si lu rian clastic de pos its oc cur (Fig. (2007) suggest , however, that the Nowe Miasto–Radom 2; Kruglov & Tsypko, eds, 1988), which, accord ing to Fault Zone forms the boundary betwee n the £ysogóry– Stupka (1991, 2002), are folded and involved in thrust and Radom Block and Lublin Basin. Accord ing to Narkiewicz re verse faults. et al. (2007), the trend of this fault zone was constra ined by ”the ex istence of a crustal dis con tinu ity in the base ment – the Teysseire–Tornquist Zone (TTZ), equiva lent to the edge Rava Rus’ka Zone of the East Euro pean Plat form”. Within this tec tonic unit, Si lu rian cal car e ous mudstones On the £ysogóry–Radom Block, bore holes provided in - and sandstone s and Lower Devo nian sandstone -shale de- form ati on on Cam brian (mainly Upper and Middle) , Ordo - posit s subcrop at the base-Juras sic uncon form ity (Figs 1, 2; vicia n, Silu ria n and Devo nian de posit s, which show a char- Stupka, 1991, 2002; Mizerski & Stupka, 2005). These rocks acter istic zonal pat tern (Fig. 2). At the top of the Palaeozoic are strongly tectonized, steeply dipping, and involved in un con formity (sub-Ju ras sic and sub-Ter tiary sur face), Cam - folds as suggest ed by Cam brian serie s occur ring in the core brian depos it s subcrop only in the south-west ern part of this of anticlines outli ned by Silu ria n strata (Kruglov & Tsypko, tec tonic unit, ad ja cent to the Holy Cross Fault. Far ther to the eds,, 1988; Stupka, 1991, 2002). Mizerski and Stupka north and northeast, Or do vi cian, Si lu rian and De vo nian se- (2005) did not clearly express their views on the boundary ries subcrop. Drilling data provided no clear evi dence for betwee n the Kokhanivka and Rava-Rus’ka zones. Differ ent the tim ing and na ture of tectoni c defor m ati on of these se - ages of the Palaeozoic de posit s in these units suggest that a ries. A signif i cant role of Caledo nian movem ents and strong fault sepa rat es them, as shown in the geolog i cal map (Fig. folding of the Cam brian depos it s in the £ysogóry–Radom 2). To the northeas t, the Rava Rus’ka Zone borders the Block were postu lat ed by Dadlez et al. (1994). Alter na- L’viv Foredeep (Figs 1, 2) along the regional Rava Rus’ka tively, Mizerski (2000) postu lat es that these defor m ati ons Fault Zone (thrust?). This tectoni c zone is com monly con- involved exclu sive ly block fault ing, and that only during sidered to repre sent both the south-west ern limit of the the Variscan orogeny, Palaeozoic (Cam brian to De vonian) L’viv Foredeep and the south-western edge of the East-Eu- depos it s were proba bly folded as a whole. ro pean Plat form (cf. Mizerski & Stupka, 2005). In the base ment of the Ukrai nian marginal part of the The framework of the geolog i cal struc ture of Precam - Outer Carpathians, the Carpathian Foredeep and in the fore- brian and Palaeozoic succes sion from the Poland/ Ukraine land area three tec tonic units composed of Precam brian and border land, il lustra ted in Figure 2 and de veloped based on mainly Lower Palaeozoic rocks were iden tified. These are, the latest geolog i cal and partly geophys i cal data, shows that from the southwest to the northeas t, the Le¿ajsk Mas sif, the Palaeozoic struc tures of the Kielce Fold Belt (in the Kokhanivka Zone and Rava Rus’ka Zone (Fig. 1; Kruglov north-east ern part of the Ma³opolska Block) and the £yso- & Tsypko, eds, 1988; Stupka, 1991, 1993; Mizerski & góry–Radom Block in the terri tory of Poland are equiva - Stupka, 2005 and refer ence s cited therein). lents of the Ukrai nian Kokhanivka and Rava Rus’ka zones, respec tively (Figs 1 and 2). Le¿ajsk Massif The Le¿ajsk Massif forms the south-east ern conti nu a - tion of the Lower San Horst, mapped in Poland as part of the STRA TIG RA PHY AND LI THOL OGY Ma³opolska Block (Figs 1, 2; Bu³a & Habryn, eds, 2008). OF THE PRE CAM BRIAN AND Although both of them consis t of sim ilar Precam brian silici- PALAEOZOIC DE POS ITS clastic rocks, there are dif fer ent views on their age. The re - sults of palynological and ra dio met ric in ves ti ga tions of Pre- The Pre cam brian cam brian rocks from the Ma³opolska Block suggest that Precam brian rocks of the Ma³opolska Block, com pos- they are Ediacaran in age (¯elaŸniewicz, et al., 2009 and ing the basem ent of the marginal part of the Carpathians and ref er ences therein). On the other hand, Precam brian rocks Carpathian Foredeep in south-east ern Poland, were encoun - of the Le¿ajsk Mas sif were pre vi ously re garded as Riphean tered in sev eral hun dred wells drilled in the area lo cated in age, corre spond ing to the Polesie Serie s devel oped in the west of the Tarnobrzeg–Le¿ajsk–Jaros³aw–Przemyœl line marginal zone of the East-Euro pean Craton; therefore, the (Bu³a & Habryn, eds, 2008). Only short Precam brian sec - Le¿ajsk Massif was consid ered as having been consol i date d tions of differ ent lengths (up to 750 m in the Zalasowa 2 during the Baikalian tectonogenesis (Kruglov & Tsypko, borehole) were exam ined by drilling. These rocks oc cur be- eds, 1988; Stupka, 1993; Mizerski & Stupka, 2005). neath Palaeozoic (Or do vi cian to Perm ian), Me so zoic (Tri - as sic and Ju ras sic) and Mio cene se ries and are rep re sented by weakly metam or phosed (anchimetamorphic) siliciclas- Kokhanivka Zone tics (e.g., Samsonowicz, 1955; G³owacki & Karnkowski, This tec tonic unit, which is sep arated from the Le¿ajsk 1963; Po¿aryski & Tomczyk, 1968; Jawor, 1970; Karn- Mas sif by the Krakovets Fault Zone (thrust?) (Fig. 1), con- kowski, 1977; Moryc & £ydka, 2000; Bu³a & Habryn, eds, sists of de formed Cam brian mudstone-sandstone s (Fig. 2) 2008; ¯elaŸniewicz et al., 2009), consis ting of mudstones, of possi bly lat est Neoproterozoic age, as suggest ed by Kru- sandstone s, sandy gravelstones and polymictic conglom er- PRE CAM BRIAN AND PALAEOZOIC BASE MENT OF THE CARPATHIAN FOREDEEP 225

ates, vari ously coloured, mostly cherry-brownish, grey- ual boreholes that reached Riphean flysch rocks in this part green, ol ive-green or grey, oc ca sion ally ac com pa nied by of the Ukraine. Hence, we do not know the cri teria for dis- tuffite interbeds. These de pos its are char acter ized by rhyth - tinguish ing the rocks in those boreholes. mic sed i men ta tion and graded bed ding, in di cat ing that they In view of the result s of palynological and radio m etric were de posit ed by densit y cur rents and thus are flysch-type studies of the Precam brian flysch in the Ma³opolska Block, sedi m ents. They often exhibi t signs of chloritization and indi cat ing its Ediacaran age (Compston et al., 1995; Moryc sericitization, and lo cally of phyllitization. The rocks are & Jachowicz, 2000; Jachowicz et al., 2002; Jachowicz, char acter ized by a very strong de gree of tec tonic de for ma - 2008; ¯elaŸniewicz et al., 2009), it can be assum ed that sim - tion, com monly dip at 45–90° and include cataclastic rocks ilar Pre cam brian rocks of the Le¿ajsk Mas sif in the Ukraine and tec tonic breccias. (which forms an inte gral part of the Ma³opolska Block) and These rocks used to be consid ered to be Pre cam brian prim aril y those of its prom inent Lower San Horst (Figs (Riphean, Vendian) or Early Cam brian in age (Samsono- 1, 2), are also Ediacaran in age, rather than Riphean as pre- wicz, 1955; G³owacki & Karnkowski, 1963; Po¿aryski & viously assumed. Tomczyk, 1968; Jurkiewicz, 1975; Karnkowski, 1977; ¯elaŸniewicz et al. (2009) postu lat ed that the Ediacaran Kowalski, 1983; Kowalczewski, 1990; Bu³a, 2000; Moryc flysch suc ces sion of the Ma³opolska Block was folded and & £ydka, 2000). Their Neoproterozoic–Ediacaran (Ven- un der went weak and vari able meta mor phism dur ing the dian) age was proved in the Ma³opolska Block, based on Cadomian tectonic move ments at the end of the Ediacaran, palynological studies (acritarchs) from the follow ing bore - as suggest ed by the result s of radio m etric age de ter mina - holes (Fig. 2): Radlna 2, Stawiska 1, Zalasowa 1 (Tarnów tions of detri tal zir cons (U-Pb) from the Ediacaran flysch of region); Lipnica 7, 10, 16, 17 and Tryñcza 2 (Le¿ajsk re - the Ma³opolska Block and of detri tal mica (K-Ar) from gion) (Moryc & Jachowicz, 2000; Jachowicz et al., 2002; Cam brian rocks of the Holy Cross Mts. (Be³ka et al., 2000; Jachowicz, 2008). The Late Pro tero zoic–Ediacaran age of Nawrocki et al., 2007). the sub-Or do vi cian siliciclastics found in the Ksi¹¿ Wielki IG1 borehole (Miechów re gion) was proved by the isoto pic The Palaeozoic anal ysis of zircons (U-Pb method) from tuffite interbeds in these rocks (age 549 ± 3 Ma) (Compston et al., 1995). The Cam brian result s of isoto pic studies (U-Pb SHRIMP II method) of sin- In south-east ern Poland, Cam brian clastic rocks occur gle zircon grains from fossil -dated or presum ed Ediacaran on the north-east ern flank of the Lower San Horst where rocks from the Zalasowa 1, Tulig³owy 38, Cha³upki Dêb- they subcrop at the sub-Miocene or sub-Juras sic uncon - niañskie 1 (Fig. 2), ¯ 141 and BN 58 boreholes show a sig- formity along a belt extend ing from the Holy Cross Mts. nifi cant propor ti on of zircon grains, which grew in parent through Stalowa Wola towards Lubaczów and the border rocks as whole crystal s (or their rims) betwee n 720 and 550 with the Ukraine (Figs 2, 3). Farther to the northeas t, Cam - Ma (¯elaŸniewicz et al., 2009). These data clearly con firm brian rocks are gradu all y onlapped by Ordo vi cia n and Si lu- the Late Ediacaran age of the Ma³opolska Block flysch de - rian rocks (Janów Lubelski–Bi³goraj–Narol region; Figs 2, pos its. 3). In this area, Cam brian rocks were encoun ter ed in more Rocks of unde fine d age, form ing the Le¿ajsk Mas sif in than 300 boreholes . In some of them their strati graphic posi - west ern Ukraine, which are sim ilar to those above de scribed tion was de ter mined based pri maril y on palynological stud- from the Ma³opolska Block, were to date consid ered to be ies (Dziadzio & Jachowicz, 1996; Kowalska et al., 2000; Riphean in age (Fig. 1; Kruglov & Tsypko, eds, 1988; Jaworowski & Sikorska, 2006; Jachowicz-Zdanowska, Stupka, 1993; Mizerski & Stupka, 2005). They show fea- 2011). Re sults present ed in these papers indi cat e that only tures of siliciclastic flysch that ei ther un der went weak epi- fragm ents of the Lower, Middle and Upper Cam brian sec - zonal meta morphism or was subject ed to strong epidiage- tions vary ing in length from a few metres to several hundred netic metam or phic pro cesses. In west ern Ukraine, they were metres (over 650 m in Narol IG2) have been identified in encoun ter ed – ac cording to Stupka (1993) – in about 20 individual boreholes. boreholes, includ ing several wells locat ed in the Chyzhky Drill ing data also in di cate a clear zon ing of the lateral and Mostys’ka re gions near the Ukrainian-Polish border. dis tri bu tion of these de pos its (Kowalska et al., 2000). For Palynological studies on drill cores of pre sumed Rip- insta nce, the oldest , Lower Cam brian rocks oc cur in the hean age in the Chyzhky 1 and 2 boreholes (Jachowicz- south-western zone of the outcrop belt di rectly adja cent to Zdanowska, 2011), yielded the follow ing re sults: the Lower San Horst, while farther to the northeas t, Middle – the Chyzhky 1 secti on repre sent s rocks younger than to Upper Cam brian depos it s subcrop at the sub-Miocene , Palaeozoic; sub-Ju ras sic and sub-Or do vi cian un con formi ties. The Cam - – the Chyzhky 2 secti on consis ts down to 3,600 m of brian series are rep re sented by black, grey or grey-green rocks younger than Palaeozoic, below – (inter val 3885– claystones and mudstones, usuall y sandy, and light grey, 3940 m), grey and greenish mudstones with faint lam ina ti on fine-grained (rarely medium -grained) quartz sandstone s, dipping at 40° were recov ered in four cored inter vals of low com monly interbeded or lam inate d with mudstones and core yield. claystones (heteroliths), oc cur ring in dif fer ent pro por tions. These rocks, which are weakly chloritized and sericiti- There are also rare thin con glomer ate layers. These rocks zed contai n no deter mina ble micro- and macrofossils and con tain a va ri ety of sed i men tary struc tures and nu mer ous are proba bly Precam brian in age. It should be noted that the trace fos sils. Accord ing to Dziadzio and Probulski (1997) geo log i cal lit er a ture pro vides no de tailed data from in di vid- and Jaworowski and Sikorska (2006), Cam brian depos it s of 226 Z. BU£A & R. HABRYN s n o i t c e s - s s o r c

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. g i F PRE CAM BRIAN AND PALAEOZOIC BASE MENT OF THE CARPATHIAN FOREDEEP 227

this area developed on an extensive shelf, dominated by the lower porti ons of the Dobromyl’–Stril’bychi 33 and tides and storms. Dubliany 1 secti ons also negate their Cam brian or Ordo vi - Stra tal dips re corded in the Cam brian sec tions are cian age. Sam ples taken from these rocks contai n palyno- highly variable , from low-angle to steep and even verti cal. morphs, which are charac ter isti c of rocks younger than the Steep dips prevail in the Lower and Middle Cam brian sec - Palaeozoic. Early Cam brian acritarch as semblages have tions, whereas the Upper Cam brian strata of ten lie in a hori - been identi fied by Jachowicz-Zdanowska (2011) in the fol - zon tal po si tion (Kowalska et al., 2000; Jaworowski & lowing bore holes: Korolyn 2 (depth 4,423.0–4,565.0 m), Sikorska, 2006). Fragm entar y data avail able on the Cam - Bortiatyn 1 (depth 3,986.0–4,297.0 m) and Rudky 300 brian depos it s and their vari able stra tal dips make it im pos- (depth 3,176.0–4,501.9 m). sible to deter mine their total thickness (Fig. 4), which prob- It should be noted that the Lower Cam brian rocks, con - ably exceeds 1,000 m in this region. taining acritarchs found in the Bortiatyn 1 borehole, were Cam brian rocks of the study area oc cur within two tec- include d by Drygant (2000) into the lower part of the Bal tic tonic units dis tinguishe d in the sub-Perm ian–Meso zoic Se ries (ten tatively inter preted as Lower Cam brian) and into base ment of south-east ern Poland, i.e. the Kielce Fold Belt the Precam brian–Vendian, whereas in the Rudky 300 bore- cover ing the north-eastern part of the Ma³opolska Block and hole – into the Juras sic , Ordo vi cia n, Cam brian and Ven- the £ysogóry–Radom Block. These tectoni c units extend to dian. In the Verchany 1 bore hole (Figs 2, 5), Jachowicz- the bor der with the Ukraine in the southeas t (Figs 1, 2). Zdanowska (2011) found Late Cam brian acritarch as sem - Drygant (2000) proposed a lithostratigraphic scheme blages in rock sam ples from depths betwee n 1,996.0 and for the Palaeozoic rocks oc curring be neath the marginal 2,056.8 m, whilst the overly ing rocks (1,967.0–1,975.4 m) parts of the Outer Carpathians and Carpathian Foredeep in con tain char ac ter is tic Or do vi cian acritarch as sem blages. By the west ern Ukraine based mainly on lithological cri te ria contra st, Drygant (2000) assigne d in the same borehole de - and the result s of well log anal yses in several boreholes , in- posit s of the depth inter val of 1,961.0–2,104.0 m entirety to cluding: Dobromyl’ Stril’bychi 33, Dubliany 1, Bortiatyn 1, the Ordovician. Chornokuntsi 1, Podilsti 1, and Rudky 300 (Fig. 2), sug- This casts seri ous doubts on the va lidit y of the Palaeo- gest ing the pres ence of Ordo vi cia n and Cam brian rocks. It zoic lithostratigraphic scheme offered by Drygant (2000) should be stressed that these rocks contai n no fossil s in most for this part of the Ukraine. Moreover, it is questi onable that boreholes , and their strati graphic posi ti on has been proved most of the boreholes listed by this author pene tra ted com - on the ba sis of single faunal evi dence or acritarchs found plete Cam brian sec tions of al most equal thicknesse s, cov- only in some of them. ered with a conti nu ous Ordo vi cia n cover, also of nearly Drygant (2000) disti nguishe d Cam brian rocks mostly consta nt thickness. Such an assum pti on is contra dicted by, un der fos sil-free Or do vi cian clastic de pos its. The Cam brian among others, strong varia ti on of the stra tal dip angle ob- succes sion is repre sent ed by mudstones-claystones and served in both the Palaeozoic and Juras sic rocks, as pointed quartz sandstone s (quartzites) that are interbeded in differ ent out by Kruglov and Tsypko, eds, (1988), Stupka (1991) and propor ti ons. These rocks local ly contai n trace fos sils. Dry- Dulub et al. (2003). It is, therefore, expect ed that coeval gant (2000) subdi vided the Cam brian sec tion into three litho- Palaeozoic rocks identi fied in the indi vid ual boreholes vary strati graphic units, namely: the Lower Cambr ian Bal tic Se - in thicknesse s. The above-menti oned boreholes and others ries at taining the thickness of 132 m; the Lower Cam brian descri bed by Drygant (2000), where Cam brian rocks were Berezhtsi Serie s at taining the thickness of 306 m, and the identi fied, are locat ed in the Kokhanivka Zone, which is an Middle to Upper Cam brian Stryvigor Se ries, which does not exten sion of the Kielce Fold Belt in Poland (Figs 1–4). ex ceed 98 m in thick ness. These se ries were pri mar ily sub di - Thus, it should be as sumed that Cam brian depos it s of these vided into 14 second ary lithostratigraphic units ranked as tec tonic units developed under similar sedi m entar y-di a- beds. strophic conditions. The oc cur rence of the complete Cam brian section and the lithostratigraphic scheme, as proposed by Drygant Or do vi cian (2000) for the Ukrai nian Carpathian Foredeep is, however, In the Polish part of the study area, Ordo vi cia n rocks questi oned for several reasons. In most bore holes, Cam - occur in both the Ma³opolska Block and the £ysogóry– brian and Or do vi cian sec tions are ex clu sively dis tin guished Radom Block (Figs 1–5). Ordo vi cia n rocks of the Ma³o- on the ba sis of lithological cri te ria, and there are clastic polska Block do not form a conti nu ous cover, but were pre- rocks that are Palaeozoic and even Ju ras sic in age of sim ilar served in several regions (Figs 3, 5) in tectoni c structure s, lith o logic char ac ter is tics in the in ves ti gated bore holes such as fold, fold-and-block or block struc tures (Bu³a & (Dulub et al., 2003). Dis tin guish ing be tween the dif fer ently Habryn, eds, 2008). Or do vi cian strata un con form ably over- aged and lithologically sim ilar depos it s based exclu sive ly lie Ediacaran or Cambrian series and are in turn over lain by on lithological cri te ria can lead to se ri ous er rors in the as - Si lu rian sed i ments and lo cally by De vo nian, Carbon if er ous, sess ment of their strati graphic posi ti on. Based on palae on - Mesozoic or even Miocene deposits. tol ogic stud ies, Dulub et al. (2003) indi cat e that indeed part In the base ment of the Carpathian Foredeep and the of the sec tion pene tra ted by the Chornokuntsi 1 and marginal part of the Outer Carpathians, Ordo vi cia n depos it s Podil’tsi 1 boreholes is proba bly Juras sic in age rather than of the Ma³opolska Block were pene tra ted by 20 wells loca- Palaeozoic (Cam brian and Or do vi cian), as en vis aged by ted in the follow ing re gions: Busko-Zdrój–D¹browa Tar- Drygant (2000). The result s of palynological studies carrie d nowska (bore holes: Stro¿yska 5, Niwki 3, Lubasz 2, Zalesie out by Jachowicz-Zdanowska (2011) on rock sam ples from 1 and Zgórsko 2); Pilzno–Rzeszów (boreholes : Pilzno 40, 228 Z. BU£A & R. HABRYN

Fig. 4. Precam brian and Palaeozoic schematic stratigraphi cal sections of south-eastern Po land and western Ukraine PRE CAM BRIAN AND PALAEOZOIC BASE MENT OF THE CARPATHIAN FOREDEEP 229

Nosówka 1, 2, 5, 6, 7, 8, 9, 12, Podgórze 1, Zagorzyce 1, and Mudstones Mem ber (upper). The Bi³goraj Form ati on is Bêdziemyœl 3 and Hermanowa 1); Tarnogród–Lubaczów over lain by two lat er ally equiv a lent lithostratigraphic units: (boreholes : Wola Obszañska 8, 9, 10, Uszkowce 1, 4 and the Tanew Claystones Form ati on and the Susiec Limestone s Lubaczów 14) (Fig. 5) (Tomczyk, 1963; Kwiatkowski et Form ati on, which is subdi vided into the Psary Limestone al., 1966; Bednarczyk et al., 1968; Moryc, 1974, 1992, Mem ber (lower) and Rebizanty Limestone Member (up - 1996, 2006; Moryc & Nehring-Lefeld, 1997; Kowalska et per). The Tanew Claystones Form ati on is repre sent ed in its al., 2000; Maksym et al., 2003; Bu³a & Habryn, eds, 2008). basal part by a glauconite layer (0.1–3.0 m) or a claystone The stra tig ra phy of the Or do vi cian, rep re sented in these layer with abundant glauconite, and in its upper part by a ar eas by clastic (claystones and siltstones, and rare sand - com plex of claystones and mudstones (up to about 85 m in stones and con glom er ates) and car bon ate (lime stone and thickness). dolo m ite) rocks, was estab li shed on the basis of graptolite, The Susiec Limestone s Form ati on is com posed of cono donts and acritarch de ter mi na tions. In in di vid ual bore- marly limestone s with abundant bioclasts, and marls, lo- holes, evi dence for the strati graphical posi ti on of pene tra ted cally dolomitic, up to 3 m in thickness. Accord ing to Or do vi cian se ries is, how ever, vari able and es sen tially de - Modliñski and Szymañski (2005), the Tanew Claystones pends on the quanti ty of available drill core mate ria l. In Form ati on was de posit ed during the Early to Late Arenig. some bore holes, Or do vi cian sed i ments were iden ti fied ex- The Susiec Limestone s Form ati on, in turn, was de posit ed clusive ly on the ba sis of well logging analy sis . The exist ing during the Late Arenig and Early Llanvirn. These form a- data indi cat e the presence of strati graphic gaps spanning tions are sep arated from the Lower Tremadoc Bi³goraj For - differ ent parts and even the enti re Ordo vi cia n (Fig. 4). mati on by a strati graphic gap spanning the Upper Tre- These data also es tab lish the oc cur rence of lateral litholo- madoc. In the northwest of the region, the Susiec Form ati on gical changes, such as the replacement of carbonates by also spans the lower Lower Arenig, whereas in the south- clastics. east, it rep re sents the Lower and Middle Arenig. A char ac ter is tic fea ture of the Or do vi cian suc ces sion in In this region, the upper porti on of the Ordo vi cia n se- the Ma³opolska Block is the presence of a disti nct, proba bly quence is repre sent ed by 130–180 m thick calcar e ous synchro nous (?Upper Tremadoc–Lower Arenig) glauco- claystones, local ly with benton it e interbeds, and lenses of nitic sandstone of vary ing thickness (from several metres to marly limestones and limestones, re ferred to the Cieszanów 70 m), which occurs at its base. Up in the Ordo vi cia n sec - Limestone s and Claystones Form ati on by Modliñski and tions (Upper Arenig through the Ashgill), there is a re mark- Szymañski (2005). Its lower part consis ts of up to 6 m thick able lithological and fa cies vari abil ity. Car bon ates (sandy marly and organodetritic limestone s, which were disti n - and nod u lar bioclastic limeston es, bioclastic and crys tal line guished as the Osuchy Limestone Mem ber. The stratigra- dolomites) are the prev a lent or sig nif icant lithological com- phical range of this form ati on covers the Upper Llanwirn ponents in the western parts of the Busko- Zdrój–D¹browa and the en tire Caradoc. It rests with a sed im en tary dis con ti- Tarnowska, Pilzno–Rzeszów and Tarnogród–Lubaczów re - nuit y surface on the Tanew Claystones Form ati on or the gions. Clastic rocks (claystones, marly claystones and mud- Susiec Lime stone For ma tion de pos its. This strati graphic stones with graptolites) predom inate in the Ordo vi cia n sec - gap spans the Lower and Middle Llanvirn in the northwest tions of the eastern parts of the Busko-Zdrój–D¹browa Tar- of the region, and the Middle Llanvirn in the southeast. nowska and Pilzno–Rzeszów regions. In the Bi³goraj–Narol area, Or do vi cian sed i men ta tion Ordo vi cia n rocks of the Ma³opolska Block are charac- ends with calcar e ous claystones and mudstones include d by terized by a small, but vari able thick ness, mostly below Modliñski and Szymañski (2005) into the 19–25 m thick 100 m. The greatest thickness is observe d in the south of the Narol Cal care ous Claystones Form ati on of Ashgill age. Pilzno–Rzeszów region in the Hermanowa 1 bore hole – The thickness of the Ordo vi cia n depos it s in the Bi³- 336 m. The only par tially pen etra ted Ordo vi cia n sec tion of goraj–Narol area ranges from 184.6 m (Doliny 1 bore hole) the Pilzno 40 borehole is 140 m thick. The dips of the Ordo - to 380.1 m (Dyle IG1 borehole) , and stratal dips vary be - vicia n strata in the above-menti oned three re gions of the tween 5 and 45°. Present ing the charac ter isti cs of the Ordo - Ma³opolska Block usuall y do not excee d 20°, and are only vi cian de pos its iden ti fied in the Bi³goraj–Narol area, Mo- lo cally steeper in tec tonic de for ma tion zones. dliñski and Szymañski (2005) (vide Drygant et al., 2006) Palaeontologically dated (graptolites, conodonts) Or do - suggest that they show a close palaeogeographical re lati on - vicia n rocks of the £ysogóry–Radom Block have been ship and far-reaching analo gies of the geolog i cal events found in the fol lowing bore holes of the Bi³goraj–Narol re- with Ordo vi cia n depos it s from the £ysogóry region of the gion (Figs 4, 5): Narol IG1 and IG2, Dyle IG1, Kozaki 1, Holy Cross Mts. For this reason, the Bi³goraj–Narol area is Osuchy 1, and Doliny 1 (Modliñski & Szymañski, 2005; included in the Radom–£ysogóry Block. Drygant et al., 2006). The Ordo vi cia n succes sion is under - In the marginal part of the Outer Carpathians and the lain in this area by Upper Cam brian depos it s, and overlai n Carpathian Foredeep in west ern Ukraine, palaeontologi- by Si luria n, Juras sic or Miocene rocks. cally dated Ordo vi cia n rocks were encoun ter ed in only two The Ordo vi cia n sec tion starts with Lower Tremadoc boreholes : Dobromyl’–Stril’bychi 33 and Verchany 1 (Fig. quartz sandstone s, claystones and mudstones (vary ing in 5; Drygant, 2000, Jachowicz-Zdanowska, 2011). thickness from 63 m to about 93 m), include d by Modliñski In the Dobromyl’–Stril’bychi 33 borehole, Ordo vi cia n and Szymañski (2005) into the Bi³goraj Sandstone s and rocks were pene tra ted at a depth of 5,001–5,132 m and con- Claystones Form ati on. This form ati on is subdi vided into the sist of grapto li tic claystones and mudstones, local ly Frampol Sandstone s Mem ber (lower) and Goraj Claystones interbedded and lam inate d by fine-grained quartz sand - 230 Z. BU£A & R. HABRYN

stones (Drygant, 2000). Based on graptolites, these rocks In the Ma³opolska Block, the extent of Ordo vi cia n sedi - were include d into the Lower, Middle and lower Upper Or- ments par tially over laps the ex tent of Si lu rian de pos its (Figs dovi cia n (from the Tremadoc through lower Caradoc). For 3, 5). Palaeontologically dated (by graptolites and acrit- this sec tion, Drygant (2000) (vide Drygant et al., 2006) es- archs) Silu ria n rocks were found beneat h Devo nian, Carbo- tabli shed the Stril’bychi Se ries, subdi vided (from the bot - niferous, Tri as sic, Ju ras sic and Mio cene for ma tions in sev- tom) into the Verchany, Vyrva, Nahuievychi and Skelivka eral wells locat ed in the fol lowing re gions: Busko Zdrój– beds. D¹browa Tarnowska (Stro¿yska 5, Niwki 3, Mêdrzechów 1 The Ordo vi cia n sec tion of the Dobromyl’–Stril’bychi 33 and Lubasz 2 bore holes); Pilzno–Rzeszów (Zawada 8K, borehole was de fined by Drygant (2000) as the stratotype for Czarna Pilzno 3, ¯ukowice 38, Pilzno 40, Zagorzyce 1 and west ern Ukraine. Palaeontologically bar ren Or do vi cian rocks 6, Nawsie 1 and Hermanowa 1 bore holes); and Tarnogród– from other boreholes , menti oned in the chapter on the Cam - Lubaczów (Uszkowice 1, Wola Obszañska 6, 8 and 10) brian rocks, were disti nguishe d by Drygant (2000) in re lati on (Fig. 5) (Tomczyk, 1963; Bednarczyk et al., 1968; Moryc, to this stratotype sec tion. However, it should be noted that 1974, 1992, 1996, 2006; Moryc & Nehring-Lefeld, 1997; Ordo vi cia n rocks of the Dobromyl’– Stril’bychi 33 borehole Kowalska et al., 2000; Maksym et al., 2003; Bu³a & were treated, ac cord ing to ear lier views (Drygant, 2000 and Habryn, eds, 2008). ref er ences therein), as a detached block within the Outer Car- In this area, the Si luria n is repre sent ed by mudstones pathian flysch units. Drygant (2000), assum ing their auto- and claystones, of ten marly, with graptolites, that lo cally chthonous (“root”) posi ti on in this bore hole and suggest ing a con tain in ter ca la tions of fine-grained quartz sand stones, oc- Cam brian age for the under ly ing rocks, did not provide credi - casional limestone lenses and interlayers of radiolarites and ble ev i dence for his hy poth e sis. tuffogenic rocks. Biostratigraphic studies indi cat e the oc- Result s of palynological studies carrie d out by Jacho- currence of strati graphic gaps in the top and basal parts of wicz-Zdanowska (2011) on sam ples of sub-Ordo vi cia n the Si lu rian sec tions (Fig. 4). Si lu rian rocks rep re sent ing the base ment rocks from the Dobromyl’–Stril’bychi 33 bore- upper Llandovery occur only to the south of the Pilzno– hole in di cate that they are youn ger than the Palaeozoic. This Rzeszów re gion (Hermanowa 1 and Nawsie 1 boreholes ). In shows – as previ ously assum ed – an allochthonous posi ti on its northern part and in the Busko Zdrój–D¹browa Tar- of the Ordo vi cia n rocks in this borehole. There fore, the sec- nowska and Tarnogród–Lubaczów regions, Silu ria n sedi - tion cannot be a stratotype for the Ordo vi cia n rocks that oc - menta ti on started in Wenlock or only in Early Ludlow times cupy an autochthonous posi ti on in the Palaeozoic sec tions (e.g., Niwki Stro¿yska 5 and 3 boreholes). throughout western Ukraine. In the light of the forego ing In the Ma³opolska Block, no Pridoli depos it s have been con sid er ations, the lithostratigraphic scheme of Or do vi cian proved so far, presum ably due to end-Silu ria n and Early De- rocks in this area, as proposed by Drygant (2000), re quires a vonian erosion. As a re sult, Silu ria n rocks of variable thick- revi sion based on more com plete palaeontological evi - nesses are pre served only lo cally as sum marized in the fol - dence. Pres ently, it is dif fi cult to jus tify the au thor’s view lowing re gions: Busko Zdrój–D¹browa Tarnowska – 36– that, in the basem ent of the marginal part of the Outer 264.3 m; Pilzno–Rzeszów – 28–206 m; and Tarnogród– Carpathians and the Carpathian Foredeep of the Ukraine, Lubaczów – 7.5–165 m. Stra tal dips of Silu ria n depos it s there is a massive (conti nu ous) cover of Ordo vi cia n clastic com monly range from a few to betwee n ten and twenty de- rocks ranging in thickness be tween 30 and 130 m, which grees, rarely exceeding 30°. rests conform ably on Cam brian depos it s and is unconfor- In the £ysogóry–Radom Block, Si luria n serie s subcrop mably overlain by Jurassic deposits, as shown in Fig. 5. the basal Ju ras sic and Ter tiary un con formities in a belt ex - Or do vi cian (and pos si bly Si lu rian) rocks, which were tending from the Janów Lubelski region, through Narol to- origi nall y de posit ed in the Kokhanivka Zone in the Ukraine, wards the border with the Ukraine (Figs 2, 5 ) where the were proba bly eroded – as it is the case in the Ma³opolska were pene tra ted in several boreholes , includ ing Narol IG1 Block of Poland – proba bly prior to the Juras sic transgres - and IG2 and Dyle IG1. A parti al secti on of the Silu ria n suc- sion. In the Kokhanivka Zone erosiona l proces ses reached ces sion was drilled, among others, in the Potok IG1 bore - the Cam brian. The Verchany 1 borehole (Fig. 2; Drygant, hole (Figs 3, 4; Modliñski et al., 1993; Tomczyk, 2000; 2000; Jachowicz-Zdanowska, 2011), which pene tra ted Bu³a & Habryn, eds, 2008). The lowest part of the Silu ria n about 30 m of Ordo vi cia n mudstones and sandstone s sec tion is repre sent ed here by about 50 m thick black bitu - interbedded with fine-grained quartz sandstone s (overly ing minous claystones with num erous graptolites proving their the Up per Cam brian and un der ly ing the Ju ras sic), proves Llandovery age. The Wenlock is repre sent ed by 50–70 m that Ordo vi cia n depos it s were local ly preserve d in this tec- thick dark claystones with graptolites, lo cally con tain ing tonic unit. In the Rava Rus’ka Zone, palaeontologically bar - limestone lenses. The lower part of the Ludlow secti on is ren Ordo vi cia n claystone-mudstone depos it s were found in com posed mainly of grap to lit ic claystones, con tain ing lime- the Ivano-Frankivs’k 1 bore hole be low Si luria n at a depth stone lenses or interbeds of marly limestone s, tuffites and of 3,592–3,693 m (after Drygant, 2000). bentonites. Its upper part is dom inate d by mudstones, sandy mudstones and fine-grained sandstone s, which becom e Si lu rian more im portant up sec tion. The Ludlow suc ces sion is 580– Sim i lar to Or do vi cian strata, Si lu rian se ries are only lo - 620 m thick. The lower part of the Pridoli suc ces sion is cally devel oped in the basem ent of the Outer Carpathians com posed of claystones and mudstones, whereas its upper and Carpathian Foredeep and on the Ma³opolska and £yso- part is dom inate d by claystones with limestone lenses, con - góry–Radom Blocks of Poland (Figs 2–5). taining graptolites. The Pridoli depos it s, preserve d under PRE CAM BRIAN AND PALAEOZOIC BASE MENT OF THE CARPATHIAN FOREDEEP 231

Juras sic rocks, attai n a thickness of over 400 m (Narol IG1 fies to lo cally re stricted marin e con di tions. The Givetian and Potok IG1 boreholes ); in the Narol IG2 borehole it is sec tion consis ts of dolomites and limestone s, predom inantl y 112 m. The stratigraphically most complete Silu rian sec tion stromatoporoidal ones. The Famennian is repre sent ed by of the great est thickness (1,094.5 m) was encoun ter ed in the de tri tal and nod u lar, bi tu mi nous and marly lime stones. Narol IG1 borehole. The Potok IG1 borehole encoun ter ed Rhyth mic de po si tion of clayey-marly or cal car e ous-de tri tal an 832.5 m thick Si luria n sec tion while the Dyle IG1 bore- sedi m ents dom inate d in the Famennian. The thickness of hole pene tra ted 200 m of Silu ria n sedi m ents. In these bore- the Mid dle and Up per De vo nian car bon ates, pre served in holes the stratal dip of the Silurian deposits varies between a this part of the Ma³opolska Block under the Carbon if er ous few and about 40°. succession, varies greatly from 87 m to over 1,000 m. Beneath the Carpathian Foredeep of the west ern Ukra- No Devo nian de posit s are encoun ter ed in the Dêbica re - ine, Silu ria n sedi m ents were found under Juras sic or Lower gion and farther northwards as far as D¹browa Tarnowska, Devo nian de posit s in the Rava Rus’ka Zone (Figs 2, 4, 5; where the Car bon if er ous (Visean) rests un con form ably on Kruglov & Tsypko, eds, 1988; Stupka, 1991, 2002; Dry- Si lu rian, Or do vi cian or Ediacaran rocks. gant, 2000). Si luria n sec tions, poorly dated by fossil s, were This suggest s that this re gion formed a high during the among others encoun ter ed in the Rava Rus’ka 1 and Ivano- De vo nian and pos si bly Early Carbon if er ous times, re ferred Frankivs’k 1 boreholes (Fig. 5). In the lat ter, Silu ria n strata to as the “Dêbica Pen in sula” (Zaj¹c, 1987) or the “Mêdrze- oc cur be tween Lower De vo nian and Or do vi cian sed i ments chów–Brzozów Land” (Narkiewicz et al., 1998b). at a depth of 3,148–3,592 m (Drygant, 2000) and consis t of In the £ysogóry–Radom Block and along the margin of marly claystones interbedded with marly or clayey lime - the East-Eu ro pean Plat form, the Lower De vo nian sed i ments stones, rarely with mudstones and fine-grained sandstone s, were pen e trated be low the Ju ras sic se ries be tween Sando- attri buted by Drygant (2000) to the upper Llandovery, Wen- mierz and Kraœnik by the follow ing bore holes: Rachów 1, lock, Ludlow and Pridoli. There are no data on the thickness Stró¿a IG1, and Zakrzew IG2 and IG3 (Fig. 2; Mi³aczewski, distri buti on of Silu ria n rocks in the Rava Rus’ka Zone. 1981; Po¿aryski & Tomczyk, 1993; Tomczyk, 2000). Their Strong tectoni c defor m ati on of the Palaeozoic succes sion in thicknesse s vary betwee n 170 m to over 1,400 m. In the this tectoni c unit (dip angles from 70 to 90°) is suggest ed by boundary area betwee n the Radom–£ysogóry Block and the Kruglov and Tsypko, eds, (1988) and Stupka (1991, 2002) East-Euro pean Plat form (at the edge of which the Devo - (vide Mizerski & Stupka, 2005). nian–Car bon if er ous Lublin Ba sin de vel oped), the fol low ing three Lower Devo nian lithostratigraphic units are recog - De vo nian nized (Mi³aczewski, 1981; Narkiewicz et al., 1998a, 2007): Devo nian serie s, occur ring in the basem ent of the mar- – Sycyna Form ati on – dark-grey claystones and mud- ginal part of the Carpathians and Carpathian Foredeep of stones with rare limestone interbeds, in ter preted as deeper south-east ern Poland, were exam ined by wells in the west- shelf depos it s of the lower Lower Lochkovian age; ern part of the Ma³opolska Block (Figs 2, 3). Lower Devo - – Czarnolas Form ati on – dark-grey claystones, mudsto- nian sedi m ents subcropping Juras sic serie s occur in the nes and fine-grained quartz sandstone s, depos it ed in a shal - northern part of the Carpathian Foredeep on the £ysogóry– low-marine near-shore zone, at tributed to the upper Lower Radom Block (north of Sandomierz) and at the edge of the Lochkovian; East-Euro pean Plat form in the Kraœnik re gion (Fig. 2). Sim - – Zwoleñ Form ati on – fine-grained sandstone s and i larly, Lower De vo nian se ries subcropping Ju ras sic sed i - mostly mottl ed claystones and mudstones, rarely accom pa- ments, occur beneat h the Ukrai nian Carpathian Foredeep in nied by conglom erate lay ers with quartz pebbles . These are the Rava Rus’ka Zone and at the edge of the East-Euro pean allu vial depos it s (Old Red facie s) of the Late Lochkovian to Platform in the Ivano-Frankivs’k region (Fig. 2). end-Emsian age. In the west ern part of the Ma³opolska Block, west of the Sim ilar Lower De vonian rocks, in terms of li thol ogy Lower San horst struc ture (Figs 2, 3), Devo nian serie s were and facie s types, oc cur in the Rava Rus’ka Zone and along encoun ter ed in over 40 boreholes in the marginal part of the the south-western edge of the East-Euro pean Plat form in the Carpathians and Carpathian Foredeep (Jawor, 1970; Ukraine. They are as signed to two lithostratigraphic units, Jurkiewicz & ¯akowa, 1972; Kicu³a & ¯akowa, 1972; namely the Tyver Serie s (Lochkovian–lower m ost Pragian) Zaj¹c, 1981, 1984; Moryc, 1987, 1992, 1996, 2006; Bu³a & and the Dnister Se ries (upper Pragian–?Lower Eifelian) Habryn, eds, 2008) where they occur beneat h Carbon if er - (Drygant, 2000). Equiva lent lithostratigraphic units were ous, Meso zoic and Terti ary depos it s and rest uncon form - en coun tered be low the Ju ras sic suc ces sion in the Rava ably on Ediacaran, Ordo vi cia n and Silurian rocks. Rus’ka Zone in the Rava Rus’ka 1 (depth 1,225–2,587 m) The lower part of the Devo nian secti ons is repre sent ed and Ivano-Frankivs’k 1 (depth 880–3,148 m) boreholes by Emsian clastic rocks (Old Red fa cies). These are usu ally (after Drygant, 2000). mottl ed quartz sandstone s (quartzites), mudstones and clay- The Lower Devo nian serie s of the East-Euro pean Plat - stones. The propor ti on of these rock types varies in the indi - form, Radom–£ysogóry Block and Rava Rus’ka Zone over- vidual Lower Devo nian secti ons, the thickness of which lie Si luria n depos it s conform ably and in depositional conti - ranges betwee n 15 m and 150 m. nu ity. The Middle and Upper Devo nian succes sion is repre - sented by carbon ate s. Dolomites, accom panied by dolomitic Car bon if er ous limeston es, and lo cally marls and limeston es domi nate in Car bon if er ous rocks, oc cur ring be neath the mar ginal the Eifelian. The occur rence of anhydrite and gypsum tes ti - part of the Outer Carpathians and Carpathian Foredeep, 232 Z. BU£A & R. HABRYN

were encoun ter ed in the Ma³opolska Block only (Figs 2–4). Pres ent in for ma tion on the geo log i cal struc ture of the Like the Devo nian rocks, they occur in the west ern part of Pre cam brian and Palaeozoic suc ces sion in this area of the this tectoni c unit (west of the Lower San Horst). In the TESZ and the margin of the East-Euro pean Plat form does Outer Carpathians and Carpathian Foredeep, Carbon if er ous not per mit to es tabli sh dis crete boundari es be tween the dif- rocks have been reporte d from over 60 boreholes under the ferent tectoni c units that are presum ably bounded by re- Perm ian, Me so zoic and Ter tiary for ma tions. They com- gional or super-re gional fault zones. Their course has been monly overli e Devo nian rocks, whereas in the D¹browa deli neat ed with vary ing ac curacy (Fig. 1) in the geolog i cal Tarnowska–Dêbica–Rzeszów region they rest direct ly upon map (Fig. 2), depend ing on the avail abil ity of geophys i cal Si lu rian, Or do vi cian or Ediacaran rocks. The fol low ing and geolog i cal control on the Precam brian and Palaeozoic three Carbon if er ous lithostratigraphic units have been iden- structure of different parts of the study area. ti fied by Moryc (1987, 1992, 1996, 2006) and Jawor and The problem s of palaeoge ogra phy and tec tonic pro- Baran (2004): cesses affect ing the devel op m ent of the south-western edge – Car bon ate-Clastic Complex ”A“ , at trib uted to the of the East-Euro pean Craton and tectoni c blocks (terranes ) Upper Tournaisian, com posed of red and grey-green, vari - involved in the form ati on of the TESZ during Neoprotero- ously grained sandstone s, local ly conglom erati c, and varie - zoic and Early Palaeozoic times (espe cially Ma³opolska gated claystones and mudstones, contai ning interbeds of Block and Brunovistulicum) have been sum mariz ed by Ma- car bon ates , mainly pelitic dolomites, marly claystones and linowski et al. (2005), Jaworowski and Sikorska (2006), pelitic limestone s. Depos it s of this com plex oc cur only in a Nawrocki and Poprawa (2006), Poprawa (2006a, b), Nar- narrow strip along the west ern, northern and east ern margin kiewicz (2007), Nawrocki et al. (2007) and ¯elaŸniewicz et of the so-called ”Dêbica Pen in sula“ (Zaj¹c, 1981) or the al. (2009). These authors express ed in general a consis tent ”Mêdrzechów–Brzozów Land“ (Narkiewicz et al., 1998b), opinion that the devel op m ent of the TESZ be gan in (?Mid - where pre-De vo nian se ries are di rectly over lain by Visean dle) Late Neoproterozoic times and was as so ciated with rift- depos it s. The thickness of the complex attains 76 m; ing proces ses taking place along the western edge of the – Car bon ate Complex ”B“, also re ferred to as the ”Car - East-Euro pean Craton during the breakup of the Precam - bonif er ous Limestone “, is early Visean in age and overli es brian Rodinia/Pannotia supercontinent (vide Golonka 2009, com plex “A” in depositional conti nuit y. It is repre sent ed by Golonka et al. 2009). Accord ing to Poprawa (2006a), the crys tal line, cryptocrystalline and micritic limeston es and rift ing proces s led to ”the devel op m ent of Baltica passive dolomites. The limestone s contai n thin inter cala ti ons of var- margin, which evolved into the TESZ during Palaeozoic iegate d claystones or mudstones. These de posit s are much collisions and/or strike-slip movements”. more wide spread than those of com plex ”A“. They were re - De po si tion of siliciclastic rocks of the Polesie For ma- moved by ero sion over a large area. In places where they are tion, overly ing the Palaeo- or Mesoproterozoic crystal line over lain by youn ger Car bon if er ous clastics (be low de- base ment, is re lated to an early rifting phase on the south- scribed complex ”C“), they range in thicknesses between west ern slope of the East-Euro pean Craton. These rocks 80 m and 590 m; were de posit ed about 770–700 Ma ago (?Early-Middle – Clastic (terrigenous) Com plex ”C”, which spans the Neoproter ozoic ) (Poprawa, 2006a). The main rift ing event ?Middle Visean through Lower Namurian (lower Namurian in this part of the East-Euro pean Craton is proved by the de- A), is com posed of claystones, grey mudstones and fine-to vel op ment of widesprea d ba saltic traps, in clud ing those medium-grained sand stones (Culm facies). These clastics known from south-east ern Poland and west ern Ukraine attai n in this part of the Ma³opolska Block thicknesse s of up (Nikishin et al., 1996). The related S³awatycze For mation to 500 m. (repre sent ed in its bot tom porti on by coarse-clastic allu vial de pos its, con glom er ates and coarse-grained sand stones, and in its upper porti on by volcanogenic rocks – basalt s inter- PALAEO GE OGRA PHY AND TEC TONIC bedded with tuffs and agglom erate s) is the record of this EVO LU TION OF THE PRE CAM BRIAN event in the Lublin–Podlasie region (Poprawa & Paczeœna, AND PALAEOZOIC 2002; Paczeœna & Poprawa, 2005). Based on ra diom etric data, the age of these rocks was esti mated at about 650–550 In south-east ern Poland and west ern Ukraine, the Outer Ma (Nawrocki & Poprawa, 2006; Poprawa, 2006a). Carpathians and Carpathian Foredeep de veloped on the The ba salt lavas and volcaniclastic rocks of the S³awa- margin of the East-Euro pean Plat form (Baltica) and the ad - tycze For mation and Ediacaran clastic de pos its of the Bia³o- jacent £ysogóry–Radom and Ma³opolska blocks in Poland pole and Siematycze form ati ons, whose depocentres devel - and the Rava Rus’ka Zone, Kokhanivka Zone and Le¿ajsk oped proba bly under an extensional regim e, are consid ered Mas sif in the Ukraine (Figs 1, 2). These units, togethe r with by Poprawa and Paczeœna (2002) and Poprawa (2006a) as the Brunovistulicum that adjoins the Ma³opolska Block in Late Proter ozoic synrift de posit s of the Lublin–Podlasie Ba- the southwest (Fig. 1), form parts of the Trans-Euro pean sin. However, the upper m ost Ediacaran rocks of the Lublin Suture Zone (TESZ). The evolu ti on of this zone during Pro- and the W³odawa for mati ons in the Lublin–Podlasie Ba sin tero zoic and Palaeozoic times is in many respects still not record, accord ing to Poprawa and Paczeœna (2002), repre - fully re solved, owing to lim ited control on its Palaeozoic suc- sent the tran si tion from the syn-rift to the post-rift phase. ces sions and the lack of data on the base ment struc ture of the The Ediacaran se ries, rep re sented by weakly metam or - indi vid ual tectoni c units (Fig. 4; Dadlez, 2006; Nawrocki & phosed (anchimetamorphic) and strongly tec toni cally de- Poprawa, 2006; Jaworowski & Sikorska, 2006). formed flysch-like siliciclastics, oc cur in the TESZ in the PRE CAM BRIAN AND PALAEOZOIC BASE MENT OF THE CARPATHIAN FOREDEEP 233

Ma³opolska Block (¯elaŸniewicz et al., 2009). Litholo- caran rocks (Fig. 4). It is very unli kely that Cam brian sedi- gically simi lar rocks of the Le¿ajsk Mas sif lo cated in the ments were depos ited in this area and were completely ero- Ukraine, which forms undoubt edly an inte gral part of the ded during a rela ti vely short time prior to the Ordovician. Ma³opolska Block (Figs 1, 2), should be consid ered to be of Accord ing to Jaworowski and Sikorska (2006), the the same age. Ac cord ing to ¯elaŸniewicz et al. (2009), these Middle and Upper Cam brian rocks of the £ysogóry–Radom rocks were folded and under went weak meta morphism at tec tonic unit and the Lower and Middle Cam brian depos it s the Ediacaran/Cam brian transi ti on during the Cadomian on the west ern margin of the East-Euro pean Plat form form orogeny and repre sent the outer part of the Cadomian part of a siliciclastic pas sive margin prism that devel oped on orogenic belt. a broad shelf dom inate d by tides and storms. These authors Refrac tion seis mic data pre sented by Malinowski et al. assum ed that the £ysogóry–Radom unit formed the proxi - (2005) from the profil e CEL 02 point out the fol lowing: mal part of the Cam brian passive margin of the East-Euro - – wave propa ga ti on veloc it y Vp within the crust of the pean Craton, while the Kielce Zone (Kielce Fold Belt) in - Ma³opolska and £ysogóry blocks is al most identi cal to that cluded in the Ma³opolska Block was situ ated in its dis tal within the crust of the south-west ern edge of the East-Euro - part. Jaworowski and Sikorska (2006) claimed that a char- pean Plat form in the Lublin–Podlasie region; acter istic feature in the Cambrian palaeogeographical re- – Ediacaran flysch de posit s of the Ma³opolska Block cord of the Holy Cross Mts. is the presence of narrow zones are under lai n by rocks charac ter ized by low wave propa ga - of sand de posi ti on, which are sepa rat ed by areas dom inate d tion ve loc ity, which are in ter preted as Neoproterozoic meta - by sandstone -mudstone heteroliths, mudstones and clay- sedi ments rep re sent ing a rift suc ces sion of a pas sive margin stones. Accord ing to these authors, the zones of sand depo - sub se quently in cor po rated into the TESZ. siti on corre spond to shallows locat ed on the ele vate d edges Based on these data, Malinowski et al. (2005) and ¯ela- of tilted blocks con trolled by large-scale nor mal listric Ÿniewicz et al. (2009) conside r the £ysogóry–Radom and faults. These faults were es pe cially active dur ing the Edia- Ma³opolska blocks as the most south-westerl y parts of the caran breakup of the Rodinia supercontinent. As a re sult of East-Eu ro pean Craton (Baltica), which, since the Late Edia- relat ed tensiona l fault ing in the £ysogóry–Radom unit and caran, oc cu pied a sim i lar po si tion as to day. How ever, they the Ma³opolska Block, the margin of the East-Euro pean do not exclude strike-slip movem ents during the Phanero- Craton subside d (Jaworowski & Sikorska, 2006). The £yso- zoic along the faults that bounded the indi vid ual tectoni c góry–Radom and Ma³opolska blocks were, however, not units of the TESZ. sepa rat ed from Baltica during the breakup of the Rodinia An al ter nati ve view on the posi ti on of the Ma³opolska superconti nent, but were an inte gral part of its passive mar- Block rel ative to Baltica dur ing the Ediacaran was ad vanced gin. Thus, de for ma tion of Cam brian sed i ments oc cur ring by Nawrocki and Poprawa (2006) and Poprawa (2006a), during the Middle Cam brian and at the Late Cam brian/Or- who assum ed that its present posi ti on with respec t to the do vi cian tran si tion may be re lated to the re ac ti va tion of ro- East-Eu ro pean Craton was not rep re sen ta tive for Neoprote- ta tional move ments on pre-ex ist ing nor mal listric faults in rozoic times. The rati onale for this hypoth e sis was the great response to strike-slip movements (Jaworowski & Sikorska, con trast be tween the lith o logic-fa cies de vel op ment of Neo- 2006; Nawrocki & Poprawa, 2006). proter ozoic (Ediacaran) rocks in the Ma³opolska Block and Poprawa and Paczeœna (2002), Paczeœna and Poprawa those observe d along the margin of the East-Euro pean (2005), and Poprawa (2006a) suggest ed that the Cam brian Craton in the Lublin–Podlasie Ba sin. In addi ti on, the Ma³o- and Early Or do vi cian sed i men ta tion on the Baltica pas sive polska Block rocks are intens ely tec toni cally deform ed and margin in the area of the Lublin–Podlasie, £ysogóry–Ra- weakly meta morphosed due to Cadomian orogenic pro- dom and Ma³opolska blocks (Kielce Fold Belt) was con- cesses, whilst coeval rocks of the Lublin–Podlasie Ba sin trolled by post-rift therm al subsi dence , typi cal of both pas- show no signs of meta morphism and compressional defor - sive margins and rift basins. The upper Middle- Upper Cam - mati on. There fore, these authors assum ed that the Ma³o- brian and Lower Ordo vi cia n sec tions of the Lublin– polska Block was docked to the East-Euro pean Craton dur- Podlasie slope and the Kielce Fold Belt of the Ma³opolska ing the Cam brian in re sponse to convergence processes and Block contai n strati graphic gaps. Nawrocki and Poprawa strike-slip movements. (2006) and Poprawa (2006a) suggest ed that these gaps de - The Cam brian rocks oc cur on the south-west ern slope veloped during the docking of the Ma³opolska Block of the East-Euro pean Plat form, in the £ysogóry–Radom (treated as a prox im al terrane) to Baltica. Ac cre tion of tec- Block, in the north-east ern part of the Ma³opolska Block tonic units at the end of the Middle Cam brian and during the (Kielce Fold Belt), and in the Rava Rus’ka and Kokhanivka Late Cam brian is thought to involve their oblique conver - zones (Figs 1, 2). Accord ing to our inter preta ti on, the lack gence that might have been relat ed to the sinistral rota ti on of of Cam brian depos it s in the western part of the Ma³opolska Baltica. Poprawa (2006a, b) suggest ed that, in the latest Block (west and south of the Kielce Fold Belt) and in the Cam brian, the Ma³opolska Block was locat ed farther to the Le¿ajsk Massif (Figs 2–4) is due to the upli ft during Cado- southeast with respect to its present location. mian tec tonic move ments. As a re sult, this part of the Ma³o- A model of oblique col li sion of the Ma³opolska Block polska Block and the Le¿ajsk Mas sif proba bly formed with Baltica dur ing the pe riod of late Mid dle Cam brian emer gent ar eas dur ing the Cam brian. This hy poth e sis is through Late Cam brian (and possi bly Early Ordo vi cia n), supporte d by the fact that in the west ern part of the Ma³o- postu lat ed by Nawrocki and Poprawa (2006) and Poprawa polska Block (west and south of the Lower San Horst struc- (2006a, b), perm its to explai n the de velop m ent of compre- ture) Or do vi cian and youn ger se ries di rectly over lie Edia- ssional fold structure s in the Lower and lower Middle Cam - 234 Z. BU£A & R. HABRYN

brian de pos its of the Kielce Fold Belt in the Ma³opolska Lochkovian marine depos it s (Malec, 2006, Koz³owski, Block. Defor m ati on of these rocks and stratigraphi cal gaps 2008). They are sepa rat ed from the uncon form ably overly - observe d in this area in the upper Middle- Upper Cam brian ing Emsian rocks by a stratigraphi cal gap spanning the Pra- suc ces sion were as so ciated with the so-called Sandomierz gian (and maybe also the upper Lochkovian). In both the tectonic phase (e.g., Kowalczewski et al., 2006). Bi³goraj–Narol region and the £ysogóry region, the thick- Strong tec tonic sub si dence dur ing de po si tion of the Mid - ness of the Ludlow and Pridoli depos it s is several times dle-Upper Cam brian and Lower Ordo vi cia n (Lower Trema- greater than that of the older Silurian rocks. docian) serie s of the £ysogóry–Radom Block is – accord ing Sub si dence anal y ses of the Si lu rian–Or do vi cian sec tion to Poprawa (2006a) – the result of flexural bending of the in the Lublin–Podlasie Ba sin (Poprawa, 2006b) indi cat e crust in this block in response to its tectoni c loading by the from the ?Middle- Late Ordo vi cia n onward a gradual in - Ma³opolska Block during its Middle and Late Cam brian crease in sub si dence and de po si tion rate cul mi nat ing in the docking to Baltica. How ever, Poprawa (2006a) did not ex- Ludlow and Pridoli. Like in the £ysogóry Radom Block, clude a possi bil ity that the £ysogóry–Radom Block was at there is depositional conti nuit y betwee n the Silu ria n and that time not yet firmly welded to Baltica as ev iden ced by Lower De vo nian (Lochkovian) se ries. The Si lu rian/De vo - “zones ac tivated in the late his tory of this part of the TESZ”. nian transi ti on depos it s of the L’viv Foredeep and Rava As there is no tectoni c uncon form ity betwee n the Ordo - Rus’ka Zone show sim ilar feature s to those observe d in the vicia n and Si luria n sequence s in the Ma³opolska Block, Lublin–Podlasie Basin and the £ysogóry–Radom Block £ysogóry–Radom Block and on the southern slope of Bal- (Kruglov & Tsypko, eds, 1988; Drygant, 2000). tica (Lublin–Podlasie region), they are include d in a single Pro cesses con trol ling the Mid dle Or do vi cian to Late Si- tectono-strati graphic unit. Or do vi cian se ries are char ac ter - lu rian/Early De vo nian sub si dence and sed i men ta tion on the ized by a great lithological and fa cies vari abil ity, which is south-western margin of Baltica and on the Ma³opolska and parti cu lar ly evi dent in the Ma³opolska Block, where car- £ysogóry–Radom blocks were asso ci ate d with the de velop - bon ate plat form fa cies are re placed lat er ally by grap to lit ic ment of the Caledo nian orogen (Poprawa, 2006b). This shale fa cies (basinal facies) (Trela, 2006; Bu³a & Habryn, orogen extends from the Arcti c-North Atlan ti c dom ain, the eds, 2008). Scandian col lision zone be tween Laurentia-Green land and Strati graphical gaps evi dent in the Lower and lower Baltica, through northern Germ any into Poland where it Middle Ordo vi cia n (Tremadoc–Arenig) secti ons of the area marks the col li sion zone betwee n the Gondwana-de rived un der con sid er ation re flect tec tonic move ments that started East-Avalonia terrane and the south-western margin of in the Middle and Late Cam brian and conti nued even in the Baltica (Ziegler & DÀzes, 2006; Pha raoh et al., 2006; Early Or do vi cian. These Late Cam brian–Or do vi cian tec- Golonka, 2009). Devel op m ent of the North Germ an-Pol ish tonic movem ents led to the upli ft and erosion of older rocks Caledonides was asso ci ate d with the subsi dence of a broad in the Ma³opolska Block and the conti nental slope of Bal- flexural foreland ba sin on the western margin of Baltica, tica. Strati graphical gaps observe d at the Ordo vi cia n/Si lu- com mencing in Silu ria n times (Nawrocki & Poprawa, 2006, rian boundary proba bly relat e to a global eustatic sea-level Šliaupa et al., 2006). drop (Poprawa, 2006b; Trela, 2006). The Si luria n clastic Poprawa et al. (1997), Narkiewicz (2002) and Poprawa suc ces sion is clearly dom i nated by grap to lit ic shales. Char - (2006b) suggest that the Ordo vi cia n and Si luria n tec tonic acter isti c for these basins is the Ludlow episode of large- subsi dence of the Ma³opolska and £ysogóry–Radom blocks scale coarse-grained clastic supply. (de fined for the Holy Cross Mts. area only) was simi lar to In the Ma³opolska Block, Si lu rian sed i men ta tion came the Or do vi cian–Si lu rian ba sin de vel oped along the west ern to its end proba bly during the Ludlow (e.g., Narkiewicz, margin of Baltica, es pe cially the Lublin–Podlasie Ba sin, 2002; Malec, 2006; Poprawa, 2006b; Bu³a & Habryn, eds, and it was driven by load-induced flexural defle cti on of the 2008; Koz³owski, 2008). The Ludlow or older depos it s are litho sphere. The Or do vi cian–Si lu rian sub si dence curves, overlai n in this area by either Lower De vonian (Emsian, deter mined for these basins (Narkiewicz, 2002; Poprawa, Old Red facies) clastics or Mid dle De vo nian car bon ates and 2006b), show the char acter istic ”knee“ shape that is attrib - lo cally by post-De vo nian rocks. The an gu lar un con formity uted to the deflexion of a foreland plate under the weight of betwee n the Devo nian and Silu ria n (amounting 10–15 de- an encroac hing orogenic wedge, as seen, for insta nce, in the grees) in di cate the Cal edo nian de for ma tions on the Ma³o- Carpathian Foredeep (Oszczypko, 2006). polska Block (¯aba, 1999). The dis conti nu ous, patchy dis- In the area under consid er ati on, the Upper Si luria n tri bu tion of Or do vi cian and Si lu rian de pos its in this block (Ludlow–Pri doli) and Lower Devo nian (Lochkovian) se ries (Fig. 5) shows that they were subject ed, even before the re flect a sub stan tial increase in the tec tonic sub sidence and Emsian or Middle Devo nian, to intens e erosion that in depo si ti on rate. No Upper Si luria n (Pridoli) and Lower De - places reached the older rocks (Bu³a & Habryn, eds, 2008). vonian (Lochkovian–Pragian) sedi m ents have been found In the Bi³goraj–Narol region of the £ysogóry–Radom on the Ma³opolska Block. It suggest s that this block occu - Block, vari ably thick Si lu rian sec tions, in clud ing Pridoli pied at that time a differ ent palaeogeographic posi ti on with and Ludlow rocks, occur beneat h the Juras sic cover. Their respec t to the £ysogóry–Radom Block and the Baltica mar- thick nesses are many times greater than those of the older gin than it presentl y does. The post-Si luria n dextral dis- Silu ria n stages (Narol IG1 and Ruda Lubycka 1 boreholes ; placem ent of the Ma³opolska Block (or the Ma³opolska and Modliñski et al., 1993; Tomczyk, 2000). £ysogóry–Radom blocks) rel ati ve to the East-Euro pean In the £ysogóry re gion of the Holy Cross Mts., Pridoli Craton is pos tulat ed by, e.g., Lewandowski (1993), Dadlez ma rine de pos its pass with out a sed i men tary break into et al. (1994), Narkiewicz (2002) and Poprawa (2006b). The PRE CAM BRIAN AND PALAEOZOIC BASE MENT OF THE CARPATHIAN FOREDEEP 235

lat ter – refer ring to the conclu sions of Nawrocki (2000) who lar to that of the Variscan externides, i.e. in the Rhenohercy- pointed out the lack of palaeomagnetic evi dence for the nian Zone and the Moravo-Silesian fold-and-thrust belt. post-Silu ria n displac em ent of the Ma³opolska Block with The Mid dle-Up per De vo nian shal low-ma rine car bon ate respec t to the East-Euro pean Craton – suggest ed small-scale plat form depos it s of the Ma³opolska Block were depos it ed dis place ments, which were within the limits of methodical under an extensional regim e, local ly in conti nuit y with error and the palaeomagnetic resolution. lithologically sim i lar Lower Car bon if er ous fa cies. A re - The role of the Caledo nian di astro phism in shaping the mark able change in sed i men ta tion, in ter preted by Narkie- struc ture of the Or do vi cian–Si lu rian suc ces sion in this area wicz (2007) as re sult ing from orogenic com pression and is un clear (vide Mizerski & Stupka, 2005). The post-Lud- erosion of the Variscan orogenic wedge, provided the Late low upli ft of the Ma³opolska Block result ed in intens e ero- Visean and Early Namurian A de po si tion of the siliciclastic sion of the Ordo vi cia n–Silu ria n rocks. These rocks, oc cur- Culm facie s on the Ma³opolska Block. In the Late Namurian ring local ly in the southwest of the block (Fig. 5), form a A, the Ma³opolska Block was uplifted, probably as a result patter n of block-faulted struc tures. However, in the Kielce of south-to-north directed orogenic stress. Fold Belt that forms part of the Ma³opolska Block, they oc- In post-Car bon if er ous times, the Pre cam brian and cur within fold or fold-and-fault block struc tures. The reso - Palaeozoic rocks oc curring presentl y in the basem ent of the lu tion of the Or do vi cian and Si lu rian suc ces sion in the Outer Carpathians and Carpathian Foredeep were sub jected £ysogóry–Radom Block (in the Bi³goraj–Narol region) and re peat edly to ero sion dur ing Late Car bon if er ous–Perm ian, Rava Rus’ka Zone is, however, too poor to reli ably define Me so zoic and Caino zo ic times. The geo log i cal struc ture of their struc tural style. Folded style of the suc ces sion in the these rocks changed as a result of the devel op m ent and in- Rava Rus’ka Zone is at tributed by Kruglov and Tsypko, eds version of the Me sozoic basin and Alpine tectoni c move- (1988) to Caledo nian movem ents. It is, however, unknown ments leading to the form ati on of the Outer Carpathian to what extend this area was overprinted by Variscan defor- orogen and the Carpathian Foredeep (Golonka et al., 2000, mations (Fig. 1). 2006; Oszczypko et al., 2006; Kuœmierek, 2010). This re - The De vo nian–Car bon if er ous car bon ate and clastic struc tur ing was as so ci ated pri mar ily with ei ther re ac ti va tion rocks, repre sent ing the Variscan tectono-stratigraphi c unit, of older (Variscan and pre-Variscan) fault zones or the for- occur in the west ern part of the Ma³opolska Block only mati on of new (post-Variscan) faults, displac ing Pre cam - (Figs 2–4). Narkiewicz (2007) as sumed a much greater brian and Palaeozoic rocks in the study area (e.g., Bu³a & orig i nal ex tent of the De vo nian (from Mid dle De vo nian) Habryn, eds, 2008). and Carbon if er ous (up to Upper Namurian A) sequence s and postu lat ed that they occurred alm ost throughout the en- tire Ma³opolska Block, except in its southern part that CON CLU SIONS formed land in De vonian times (Mêdrzechów–Brzozów land; Narkiewicz et al., 1998b). The present lack of these In south-east ern Poland and west ern Ukraine, the Outer De vo nian and Car bon if er ous sed i ments in the north-east ern Carpathian orogen and its foredeep devel oped on the mar- part of the Ma³opolska Block is attri buted by Narkiewicz gin of the East-Eu ro pean Plat form (Baltica). The area con - (2007) to Permo-Car bonif er ous(? ) erosion. It should be also sists of a num ber of tectoni c units, includ ing the £ysogóry– noted that he assum ed a differ ent course of the Holy Cross Radom Block and Ma³opolska Block in Poland, and the Fault, marking the boundary betwee n the Ma³opolska and Rava Rus’ka Zone, Kokhanivka Zone and Le¿ajsk Massif £ysogóry–Radom blocks, from that adopted in the present in the Ukraine (Fig. 1). These tectoni c units, locat ed within work. the Trans-Euro pean Suture Zone (TESZ), are com posed of Accord ing to Narkiewicz (2007), this fault merges in the Pre cam brian and Palaeozoic (Cam brian to Car bon if er - the area north of Lubaczów with the Nowe Miasto–Radom ous) rocks and are sepa rat ed by regional fault zones (Fig. 2). Fault Zone that conti nues from the northeas t and repre sent s In the study area, fragm entar y con trol on Palaeozoic the south-western border of the East-Euro pean Craton. In sec tions and the lack of data on the struc ture of the Precam - this context , the Ma³opolska Block is bordered to the north brian base ment in some of these tec tonic units (Fig. 4) in- by the £ysogóry–Radom Block, and to the northeas t – di - hib its a com pre hen sive and un am big u ous as sess ment of the rectly by the East-Euro pean Craton. Narkiewicz (2007) pro- Late Pre cam brian and Palaeozoic evo lu tion of the TESZ. vides no justi fica ti on for the adopted version of the Holy Devel op m ent of the TESZ be gan in the Late Proter o - Cross Fault trend. At pres ent, it is dif fi cult to de ter mine and zoic rift ing proces ses along the pres ent-day west ern margin to jus tify the de vel op ment of the De vo nian–Car bon if er ous of the East-Euro pean Craton (Baltica) during the breakup of succes sion in south-east ern Poland and west ern Ukraine, in the Rodinia/Pannotia supercontinent (e.g., Poprawa & Pa- the area sit uate d southwest of the East-European Craton. czeœna, 2002, Malinowski et al., 2005; Nawrocki & Po- Narkiewicz (2007) include s the Ma³opolska Block into prawa, 2006; Poprawa, 2006a; Golonka, 2009; Golonka et a mo saic of crustal blocks lo cated in the Variscan fore land. al., 2009; ¯elaŸniewicz et al., 2009). The rift ing cul minate d These blocks, sepa rat ed by deep-rooted and re peat edly re- in the ear liest Cambr ian de vel op ment of the Baltica pas sive acti vated fault zones, react ed dif ferentl y to changing litho- margin, which include s the £ysogóry–Radom and Ma³o- spheric stress pat tern in De vo nian and Car bon if er ous times. polska blocks, where the Earth’s crust is char acter ized by In accor dance with the Narkiewicz’s (2007) view, De vo - sim ilar geophys i cal feature s as the crust in the south-west- nian and Car bonif er ous depos it s (up to Namurian A) of the ern edge of the East-Euro pean Craton in the Lublin– Ma³opolska Block ac cum ulat ed under the stress field sim i- Podlasie segm ent (Malinowski et al., 2005; ¯elaŸniewicz et 236 Z. BU£A & R. HABRYN

al., 2009). The com plete record of the rifting phases and no Upper Si luria n (Pridoli) and Lower De vonian (Loch- post-rift Neoproterozoic and Early Palaeozoic (Cam brian kovian) rocks. This suggest s that the block occu pied a dif- and Early Ordo vi cia n) therm al subsi dence of the basin was ferent palaeogeographic posi ti on at that time in rela ti on to re cog nised only in the geo log i cally well-ex plored Lublin– the East-Euro pean Craton: to the £ysogóry–Radom Block Podlasie slope of the East-Euro pean Platform (Poprawa & and Rava Rus’ka Zone. There fore, its post-Si luria n dextral Paczeœna, 2002; Poprawa, 2006a). movem ent rela ti ve to the East-Euro pean Craton is inferred In the Ma³opolska Block and its inte gral part, the (Lewandowski, 1993; Dadlez et al., 1994; Narkiewicz, Le¿ajsk Mas sif (Figs 1, 2), there oc cur Ediacaran flysch- 2002; Poprawa, 2006b). like siliciclastics that un der went weak metamor phism and The De vo nian–Car bon if er ous car bon ate and clastic fold de form ati on at the Ediacaran/Cam brian transi ti on as a rocks of the Variscan struc tural com plex oc cur in the west - result of Cadomian tectoni c movem ents. They repre sent the ern part of the Ma³opolska Block only (Fig. 2). The posi ti on outer part of the Cadomian orogenic belt (¯elaŸniewicz et of the Ma³opolska Block within the Variscan foreland area al., 2009). In terms of lithological and facie s devel op m ent, sug gests that the De vo nian–Car bon if er ous de po si tion oc- meta mor phic trans for ma tions and the na ture of tec tonic de- curred un der the in flu ence of a stress field that was simi lar form ati on, they differ from the coeval plat form depos it s ob- to that observe d in the Variscan externides, i.e. in the Rhe- served in the south-west ern edge of the East-European nohercynian Zone and Moravo-Silesian fold-and-thrust belt Platform. (Narkiewicz, 2007). The Middle- Upper Devo nian and Sig nif i cant dif fer ences in the palaeogeographical and Lower Car bon if er ous shal low-ma rine car bon ate plat form tec tonic devel op m ent of the Ediacaran rocks betwee n the depos it s devel oped in an extensional re gime, while the de- Ma³opolska Block and the East-Euro pean Craton show that po si tion of the Culm siliciclastic rocks (Late Visean–Early the posi ti on they presentl y occupy rela ti ve to each other is Namurian A) occurred under orogenic com pression. In the not repre sen ta ti ve of Neoproterozoic times (Nawrocki & Late Namurian A, the Ma³opolska Block was uplifted as a Poprawa, 2006; Poprawa, 2006a). result of orogenic stresses. The de velop m ent of Cam brian depos it s in the East-Eu - Dur ing post-Car bon if er ous times, Pre cam brian and ropean Craton, the £ysogóry–Radom Block, the north-east- Palaeozoic de pos its of the base ment of the Outer Carpa- ern part of the Ma³opolska Block (Poprawa, 2006a) and in thians and Carpathian Foredeep were sub ject in this area to the Rava Rus’ka and Kokhanivka zones is asso ci ate d with ero sional pro cesses and re struc tur ing dur ing Al pine oro- the post-rift therm al subsidence. genic movem ents (Golonka et al., 2000, 2006; Oszczypko Strati graphical (?erosiona l) gaps observe d in the Mid - et al., 2006; Kuœmierek, 2010). dle and Upper Cam brian sec tions in the Lublin–Podlasie slope of the East-Euro pean Craton and in the Kielce Fold Belt (Ma³opolska Block) as well as compressional fold Ac knowl edge ments struc tures found in the Lower Cam brian and lower Middle This study was under taken as the re search pro ject No Cambr ian de pos its of the Kielce Fold Belt formed as a re sult UKRAINA/193/2006 of the Minis try of Sci ence and Higher Ed u - of tec tonic move ments (so-called Sandomierz tectonic cation carried out at the AGH Univer sity of Science and Tech nol- phase), proba bly caused by an oblique col li sion of the ogy and Pol ish Geo log i cal In sti tute – Na tional Re search In sti tute Ma³opolska Block and the East-Euro pean Craton during the and was fi nanced from the sci en tific fund of 2007–2010. period spanning the late Middle to Late Cam brian (maybe also the Early Ordo vi cia n) (Nawrocki & Poprawa, 2006; Poprawa, 2006a). 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