de ve l op ment and in ver sion of de vo ni an and car bon

Geo log i cal Quar terly, 2007, 51 (3): 231–256

De vel op ment and in ver sion of De vo nian and Car bon if er ous bas ins in the east ern part of the Variscan fore land (Po land)

Marek NARKIEWICZ

Narkiewicz M. (2007) — De vel op ment and in ver sion of De vo nian and Car bon if er ous bas ins in the east ern part of the Variscan fore land(Po land). Geol. Quart., 51 (3): 231–256. Warszawa.

The Pol ish part of the Cen tral Eu ro pean Variscan fore land in cludes sev eral re gional units that dif fer in crustal struc ture and are char ac ter -ized by dis tinct De vo nian to Car bon if er ous sub si dence and depositional his to ries. These units re sponded dif fer ently to palaeostresschanges along the south ern mar gin of the Old Red Con ti nent. Dur ing the De vo nian to Namurian A, ar eas lo cated to the south-west of theTeisseyre-Tornquist Zone (TTZ), in clud ing the Up per Silesian Coal Ba sin, Ma³opolska and £ysogóry–Radom blocks, were in flu encedby stress fields sim i lar to those in the west ward ad ja cent Rheno-Hercynian Zone, whilst the Lublin Ba sin, lo cated to the north-east of theTTZ, shows a sim i lar de vel op ment to the Pripyat–Dniepr–Donets rift sys tem. Af ter the Namurian A, the en tire south ern Pol ish fore landstarted to re spond in a more con sis tent way to the build-up of synorogenic compressional stresses, im ply ing a more uni form de vel op mentof the stress field. Dur ing the Namurian B to early Westphalian D, the Pol ish fore land was dom i nated by north-di rected compressionalstresses em a nat ing from the Southeastern Variscan Belt. Dur ing the late Westphalian and early Stephanian, the en tire fore land un der went compressional de for ma tion and con com i tant ba sin in ver sion un der the in flu ence of stresses prop a gat ing from the Moravian-SilesianFold-and-Thrust Belt. In the Pol ish fore land, the de vel op ment of De vo nian-Car bon if er ous bas ins, as well as the ar chi tec ture of Variscanstruc tures, clearly re flect the re ac ti va tion of pre-ex ist ing crustal dis con ti nu ities, in clud ing spe cif i cally the TTZ, but also other ma jorgeophysically de fined crustal bound aries. In gen eral, thick-skinned tec ton ics con trolled by the in her ited struc tural grain of the base mentpre vailed, whereas struc tural de coup ling, re sult ing in the de vel op ment of mi nor thrusts and re verse fault ing, was of lo cal sig nif i canceonly. The dis tinct struc tural-depositional de vel op ment of the Pomerania re gion re flects its dis tal lo ca tion with re spect to the evolv ingorogen. Orogenic com pres sion in flu enced this area only in di rectly, with the TTZ act ing as a guide for the trans mis sion of transtensionaland transpressional stresses.

Marek Narkiewicz, Pol ish Geo log i cal In sti tute, Rakowiecka 4, PL-00-975 Warszawa, Po land, e-mail: [email protected](re ceived: March 7, 2007; ac cepted: April 6, 2007).

Key words: Variscides, Cen tral Eu rope, fore land bas ins, sub si dence, palaeo ge ogra phy, palaeostress.

INTRODUCTION

While the ex ter nal parts of the Cen tral Eu ro pean Variscanorogen con sist of a stack of fore land-verg ing pre dom i nantlythin-skinned thrust sheets in volv ing thick De vo nian and Car -bon if er ous, partly synorogenic suc ces sions (“VariscanExternides”), time-equiv a lent strata are dis rupted in some partsof the Variscan fore land by base ment-in volv ing intraplatecompressional struc tures (Ziegler, 1990; Ziegler et al., 2002).The bound ary be tween these two fun da men tally dif fer ent de -for ma tion belts is placed along the Variscan (Thrust) Front(e.g. Jubitz et al., 1986), here re ferred to as the VariscanOrogen Bound ary Zone (Fig. 1). This bound ary may co in cidewith dis crete fron tal thrusts (e.g. the Midi and Aachen thrustsof the Ardennes) or with a more dif fuse, wide zone of grad ualfad ing out of folds-and-thrusts (north ern Rhenish area; Behr etal., 1984). In South ern Po land, the Orlova Thrust marks thebound ary be tween the Moravian-Silesian Fold-and-Thrust Belt of the Variscan Orogen and the much less de formed strata of

the Up per Silesian Coal Ba sin in its fore land (Fig. 2). In con -trast, the bound ary be tween the thrusted and folded flysch suc -ces sion of the Fore-Sudetic area and the fore land of North ernand Cen tral Po land is poorly con strained (e.g. Dadlez et al.,1994; Mazur et al., 2006).

The sed i men tary and tec tonic de vel op ment of theMoravian-Silesian seg ment of the Variscan Externides is nowwell-con strained ow ing to stud ies over many years, ex pandedand sum ma rized dur ing the last de cade by Schulmann and Gayer (2000), Hartley and Otava (2001) and ¯aba et al. (2005). Thestruc tural-palaeogeographic po si tion of the Moravian-SilesianBelt within the gen eral frame work of the Cen tral Eu ro peanVariscides is, how ever, still a mat ter of de bate (e.g. Franke and¯elaŸniewicz, 2002), al though con sid er able prog ress has beenmade in plac ing this belt in the con text of the Bo he mian Mas sif,and par tic u larly the Sudetic do main (Mazur et al., 2006). More -over, there is still un cer tainty about the dy namic re la tion ship be -tween the Variscan Orogen and the de for ma tion of its dis tal fore -land ba sin that is lim ited to the NE by the ero sional edge of Car -bon if er ous strata (Fig. 2). The list of un re solved or poorly re -

solved ques tions in cludes pos si ble causal links be tween the dif -fer ent stages in the tec tonic de vel op ment of the orogenic belt and the fore land ba sin, palaeostress pat terns, and the role played bypre-ex ist ing com plex base ment struc ture.

This pa per syn the sizes and in te grates the avail able strati -graphic, palaeogeographic and struc tural data, and pres ents anup dated in ter pre ta tion of the De vo nian to Car bon if er ous evo lu -tion of the Pol ish Variscan fore land as a whole. It partly buildsand ex pands on an ear lier syn the sis by Narkiewicz et al.(1998b) that fo cused on the Pomerania and Lublin ar eas. An at -tempt will be made to iden tify and dis cuss far-field ef fects oftec tonic stresses, that were trans mit ted both from the West -ern-Cen tral Eu ro pean Variscan Orogen as well as from itssouth east ern branch into the fore land of Po land. At ten tion willbe also paid to a mode in which re gional stresses were par ti -tioned by a pat tern of re ac ti vated crustal dis con ti nu ities.

REGIONAL DATABASE

Ear lier re gional strati graphic and tec tonic data was sum ma -rized and re viewed in the mono graphs ed ited by Marek (1983),

¯elichowski (1983a), Raczyñska (1987), Zdanowski and¯akowa (1995), syn thetic pa pers by Po¿aryski (1986),¯elichowski (1987a), Po¿aryski et al. (1992) and Narkiewiczet al. (1998b), and in a car to graphic form by Po¿aryski andDembowski (1983), ¯elichowski and Koz³owski (1983) andPo¿aryski and Karnkowski (1992).

Since the late 1990s new im por tant data and con cepts have been re ported in nu mer ous pub li ca tions. Bu³a and ¯aba(2005) re cently re viewed the struc tural-depositional de vel op -ment of the Up per Silesian Coal Ba sin in the con text of theMoravian-Silesian Fold-and-Thrust Belt. Ear lier, Bu³a et al.(1997) and ̄ aba (1999) doc u mented the Palaeozoic struc tural evo lu tion of the Kraków–Lubliniec Fault Zone. Based onstruc tural field-data, Lamarche et al. (1999, 2003) pre sented a geodynamic in ter pre ta tion of palaeostress pat terns in the Holy Cross Mts. area. Antonowicz et al. (2003; see also Hooper etal., 2002) re in ter preted re flec tion seis mic data from theLublin Area and pro posed a new struc tural model of a pas sivesyncline above a ma jor de tach ment sur face. This in turn trig -gered a dis cus sion on the tec tonic con trols on sub si dence andin ver sion of the Lublin Ba sin (Dadlez, 2003; Narkiewicz,2003; Krzywiec and Narkiewicz, 2003a).

232 Marek Narkiewicz

Fig. 1. Broader re gional con text of the Variscan fore land in Cen tral Eu rope (com piled mainly af ter Po¿aryski and Dembowski, 1983; Ziegler, 1990; Banka et al., 2002)

The trace of the Rheno-Hercynian su ture cor re sponds roughly to that of the Rheic su ture; cross pat tern — el e va tions of the East Eu ro pean Plat form; AM — Armori can Mas sif, HCMts — Holy Cross Moun tains, MP — Moesian Plat form, MSFTB — Moravian-Silesian Fold-and-Thrust Belt, STZ —Sorgenfrei-Tornquist Zone, TTZ — Teisseyre-Tornquist Zone, USCB — Up per Silesian Coal Ba sin, VA — Voronezh Anteclise

Sev eral re cent strati graphic con tri bu tions have a di rectbear ing on the un der stand ing of the Variscan fore land de vel op -ment in Po land. Of par tic u lar im por tance are pa pers dis cuss ingeustatic and tec tonic con trols on the De vo nian and Early Car -bon if er ous depositional sys tems (Narkiewicz, 1988;Szulczewski et al., 1996; Belka et al., 1996; Racki, 1997; Racki and Narkiewicz, 2000). New data on Car bon if er ous sed i mentac cu mu la tion and tec ton ics were re ported by Skompski (1996,1998), Lipiec and Matyja (1998), Waksmundzka (1998, 2005),

Krzemiñski (1999), Lipiec (2001), Jaworowski (2002) and Narkiewicz (2005).

The study pre sented here is based on a com pi la tion, re viewand anal y sis of pub lished and some un pub lished data col lectedby the au thor. For ba sin anal y sis, the time scale of Gradstein etal. (2004) was adopted (Fig. 3). The re sults of ear lier tec tonicsub si dence anal y ses car ried out in dif fer ent re gions byNarkiewicz et al. (1998b), Racki and Narkiewicz, (2000) andNarkiewicz (2005) were amended us ing up dated strati -

Development and inversion of Devonian and Carboniferous basins in the eastern part of the Variscan foreland (Poland) 233

Fig. 2. Sub-Perm ian-Me so zoic map of Po land show ing re gional units of the Variscan fore land (partly based on Po¿aryski and Dembowski, 1983)

BAH — Bielsko-Andrychów High; bro ken TTZ line marks its less firmly con strained segment


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graphic-struc tural ob ser va tions and a con sis tenttime scale (Fig. 4). Fi nally, dis sem i natedpalaeostress data were com piled and com pared. The def i ni tion and out line of re gional struc tural units ispartly based on new in ter pre ta tions of the deepcrustal seis mic sound ing (DSS) data that were ac -quired in the con text of the POLONAISE andCELEBRATION 2000 pro grams (see Guterch andGrad, 2006 for a re cent re view), and partly on ananal y sis of po ten tial field data (Królikowski andPetecki, 1995; Grabowska and Bojdys, 2001;Królikowski, 2006).

STRUCTURAL AND PALAEOGEOGRAPHICFRAMEWORK

The area ad dressed by this pa per ex tends fromthe Variscan Orogen Bound ary to the south west ernmar ginal zone of the East Eu ro pean Plat form (EEP)and com prises the belt of the De vo nian and Car bon -if er ous subcrop and lim ited out crops fromPomerania in the north-west to Cen tral and south -east ern Po land (Fig. 1). The base ment of this areacon sists of the cratonic crust of the EEP to the SWmar gin of which an ar ray of crustal blocks or ter -ranes and a hy po thet i cal Cal edo nian thrust-andfold-belt were accreted, mostly dur ing the EarlyPalaeozoic, form ing the Trans-Eu ro pean Su tureZone (TESZ) (e.g. Winchester et al., 2002; Dadlezet al., 2005; Nawrocki and Poprawa, 2006). Thiszone is sep a rated from the craton by a first-or dercrustal dis con ti nu ity, re ferred to as theTeisseyre-Tornquist Zone (TTZ; Dadlez, 1997).

Ac cord ing to some au thors, the TTZ acted as astrike-slip fault zone with a to tal dis place ment ofthe or der of thou sand kilo metres dur ing De vo nianand Car bon if er ous times (Lewandowski, 1993;Franke and ¯elaŸniewicz, 2002). If so, the pres -ently ob served jux ta po si tion of struc tural unitsform ing the TESZ against the East Eu ro peanCraton (EEC) would not re flect their ac tual spa tialre la tion ships dur ing the time in ter val dis cussed,ren der ing the con sid er ations ad vanced in this pa -per ground less. It is to be stressed, how ever, thatre cent palaeomagnetic data point to sta bil ity of theMa³opolska and prob a bly other TESZ blocks rel a -tive to the EEC from ear li est De vo nian time on -wards (Nawrocki, 2000). More over, it will beshown that, al though the TTZ was tec toni cally ac -tive dur ing the Late Palaeozoic, it did not sig nif i -cantly dis rupt the palaeogeographic con fig u ra tionof the area ad dressed. In other words, based on theavail able data no large-scale dis place ments are re -quired to ex plain the ob served con fig u ra tion ofDe vo nian-Car bon if er ous bas ins and their struc -tural evo lu tion.


Fig. 4. Com par i son of the De vo nian-Car bon if er ous tec tonic sub si dence de vel op -ment of the Up per Silesian Coal Ba sin (USCB), Ma³opolska Block,

£ysogóry–Radom Block, Lublin Ba sin and Pomerania (based mainly on McCann et al., 1997; Narkiewicz et al., 1998b; Narkiewicz, 2005)

Ab bre vi a tions of strati graphic names as in Fig ure 3

The Pol ish part of the Variscan Orogen that crops out in theSudetes Mts. is char ac ter ized by a com plex struc ture that is stillnot fully un der stood. The Sudetes Mts. in clude pos si ble coun -ter parts of the Saxo-Thuringian and Moldanubian zones intheir west ern and cen tral parts, and the Moravian-SilesianFold-and-Thrust Belt in their east ern part (Mazur et al., 2006).The lat ter is con sid ered as a di rect con tin u a tion of theRheno-Hercynian Zone, though the con cept of oroclinal bend -ing around the NW mar gin of the Bo he mian Arc is not ac -cepted by all (e.g. Franke and ¯elaŸniewicz, 2002). The equiv -a lent of the Rheno-Hercynian Su ture is clearly rec og nized inthe east ern Bo he mian-Sudetic out crop area (Staré Mìsto Belt;Mazur et al., 2006). Its north ward and north-west ward trace,shown ten ta tively in Fig ure 2, is here based on the dis tri bu tionof char ac ter is tic “Sudetic crust” as de fined by the re sults of theDSS pro files LT-7, P4 and SUDETES (Dadlez, 2006;Majdañski et al., 2006).

The ex ter nal, Fore-Sudetic part of the orogen is con cealedbe neath thick Perm ian to Ce no zoic sed i men tary suc ces sions. In Fig ure 2 the outer bound ary of the Variscan Orogen is shown in north west ern Po land es sen tially ac cord ing to the in ter pre ta tionof Po¿aryski and Karnkowski (1992) whereas its po si tion inCen tral Po land was adopted from Jubitz et al. (1986; see alsodis cus sion by Dadlez et al., 1994).

The re cently pro posed “pas sive syncline” model for theLublin Ba sin (Hooper et al., 2002; Antonowicz et al., 2003) im -plies that thin-skinned Variscan thrusts had prop a gated from thecur rently as sumed orogen bound ary ca. 200 km east ward (cf.Fig. 2) and that all of south east ern Po land has to be in cluded inthe Variscan Externides. How ever, care ful anal y sis of seis micand well data does not re veal any ev i dence for large-scale de -tach ments in the base ment of the Lublin Ba sin, or for as so ci atedtri an gle zones along its mar gins (Krzywiec and Narkiewicz,2003a, b; Krzywiec, 2007). More over, the broader re gionalframe work of this area is not com pat i ble with “Ap pa la -chian-type” tec ton ics (Narkiewicz, 2003; Dadlez, 2003).

To wards the south, both the Bo he mian part of the VariscanOrogen and its Pol ish-Ukrai nian fore land plunge be neath theCarpathian nappes, thus ren der ing re con struc tions of theVariscan Belt highly hy po thet i cal. Nev er the less, based on theoc cur rence of ex otic clasts in the Carpathian flysch, as well ason iso lated out crops in the In ner Carpathians, it is gen er ally as -sumed that the Variscan orogenic belt ex tended into the areanow oc cu pied by the Carpathians (Ziegler, 1990; Znosko,1992). The orogen con tin ued along the south ern EEC mar ginto wards the Cri mea and Cau ca sus in re la tion ship with thenorth-dip ping Palaeo-Tethys subduction sys tem (Ziegler,1990; Nikishin et al., 1996, 2001).

The Pol ish Variscan fore land ba sin can be sub di vided intothe six struc tural units, namely the Up per Silesian Coal Ba sin,the Ma³opolska and the £ysogóry–Radom blocks, the LublinBa sin, the P³ock Area and Pomerania (Figs. 1 and 2). Theseunits are char ac ter ized by a con trast ing sed i men tary re cord(Fig. 3) and sub si dence pat tern (Fig. 4) that re flect their struc -tural in de pend ence and in ter nal in teg rity dur ing De vo nian andCar bon if er ous times. It will be shown that these dif fer ences aremainly the ef fect of tec tonic ac tiv ity along crustal-scale dis con -ti nu ities cor re spond ing to the ma jor faults or fault zones shownin Fig ures 1 and 2.

UPPER SILESIAN COAL BASIN

The Up per Silesian Coal Ba sin (USCB) oc cu pies the NEcor ner of the Brunovistulicum Block or Terrane, theNeoproterozoic crys tal line base ment of which was con sol i -dated dur ing the Cadomian orogenic cy cle (Fin ger et al., 2000). The der i va tion of this terrane and its ac cre tion his tory are stillprob lem atic (see re cent dis cus sion in Nawrocki and Poprawa,2006). The north ern part of Brunovistulicum is de fined as theUp per Silesian Block (Kotas, 1985; Bu³a and ̄ aba, 2005). The west ern part of Brunovistulicum ex tends be neath theMoravian-Silesian Fold-and-Thrust Belt (Fig. 2) that evolvedin re sponse to Car bon if er ous subduction of the Brunovistulianplate be low the Bo he mian Mas sif unit (e.g. Schulmann andGayer, 2000; re cently sum ma rized by Bu³a and ¯aba, 2005).The Moravian-Silesian Belt over rides the mar gin of the USCBalong a sys tem of thrusts rooted in the base ment 10 km west oftheir pres ent out crop (Fig. 5). The NE bound ary of the USCB is of mixed depositional-ero sional char ac ter, run ning 10–20 kmwest of the Kraków–Lubliniec Fault (Fig. 2). The lat ter is a nar -row tec tonic zone (¯aba, 1999) that sep a rates theBrunovistulicum and Ma³opolska blocks (Bu³a et al., 1997)which dis play con trast ing crustal struc tures (Malinowski et al.,2005). The south ern bound ary of the USCB is ero sional andex tends across the north ern slope of the Bielsko–Andrychówbase ment high that forms part of the Sub-Carpathian Arch(Narkiewicz, 2005).

MA£OPOLSKA BLOCK

The Ma³opolska Block is bounded to the north by theWNW–ESE strik ing Holy Cross Fault that transects thePalaeozoic core of the Holy Cross Mts. Ac cord ing to grav itydata (Królikowski and Petecki, 1995), this fault con verges inits south east ern ex ten sion with the TTZ (Fig. 2). To the south,the Ma³opolska Block plunges deeply be neath the nappes ofthe Pol ish Carpathians and thus be comes in ac ces si ble to bore -holes. The crustal struc ture of the Ma³opolska Block dif fersfrom that of the ad ja cent £ysogóry–Radom Block, al thoughthe Holy Cross Fault is not marked by sharp con trasts in re -frac tion-seis mic P-wave ve loc ity mod els (Malinowski et al.,2005; Guterch and Grad, 2006). The Early Palaeozoic his toryof the Ma³opolska Block is also dis tinct though its re la tion toad ja cent units re mains con tro ver sial (e.g. Nawrocki, 2000;Narkiewicz, 2002).

£YSOGÓRY–RADOM BLOCK

The pre-Perm ian Palaeozoic suc ces sion of the£ysogóry–Radom Block is poorly known from a few bore holesreach ing Mid dle De vo nian and up per most Si lu rian strata be lowMe so zoic cover. The Up per De vo nian and Car bon if er ous ismostly eroded. Con se quently, the der i va tion of this block is sub -ject to con tra dic tory in ter pre ta tions, in clud ing pos tu lated closeBaltica (EEC) af fin i ties and an ex otic terrane or i gin (see dis cus -sion in Dadlez et al., 1994; Belka et al., 2000). The NE bound ary of the £ysogóry–Radom Block is par tic u larly dif fi cult to de fine.Tra di tion ally it has been placed along the Ursynów–Kazimierz



Fig. 5. A — lithostratigraphic frame work of the Up per Silesian Coal Ba sin (stip pled — im por tant sand stone units); B — geo log i cal cross-sec -tion (see Fig. 2 for lo ca tion; af ter Kotas, 1994, 1995)

Cm. — Cam brian, DLCC — De vo nian-Lower Car bon if er ous car bon ates, MF — Malinowice Fm., PS — Paralic Se ries, USS — Up per Silesian Sand stoneSe ries, MS — Mudstone Se ries, Mioc. — Mio cene

Fault that de lim its the Lublin Trough to the SW (Fig. 2; e.g. re -cently Jaworowski and Sikorska, 2006). The lat ter fault, as wellas the Izbica–Zamoœæ Fault, owe, how ever, their pres ent ge om e -try to late Westphalian in ver sion (see be low). Nei ther of thesefaults co in cides with a geophysically doc u mented ma jor crustaldis con ti nu ity (Dadlez, 2001), and their role in con trol ling the de -vel op ment of depocentre, par tic u larly dur ing the Car bon if er ous,is equiv o cal (Narkiewicz, 2003).

By con trast, po ten tial field and DSS data doc u ment the ex -is tence of an im por tant crustal bound ary — the TTZ — form -ing a nar row belt run ning from Nowe Miasto in the NW andcon tin u ing to wards SE near Radom and I³¿a (Grabowska andBojdys, 2001; Dadlez, 2006). The Me so zoic ex pres sion of thiszone is the Nowe Miasto-I³¿a Fault doc u mented by e.g.Hakenberg and Œwidrowska (1997) and Po¿aryski (1997).Dur ing the De vo nian to Car bon if er ous the trace of the TTZwas off set by 10–20 km to wards the east, par tic u larly in the SEcor ner of the Radom–£ysogóry Block, as sug gested by MidDe vo nian depositional and sub si dence pat terns (unpubl. data).This tec tonic bound ary is here re ferred to as the NoweMiasto–Radom Fault Zone (Fig. 2).

LUBLIN BASIN

The depocentre of the Lublin Ba sin cor re sponds to theLublin Trough (Fig. 2). The lat ter unit owes its pres ent ge om e -try mainly to the lat est Car bon if er ous in ver sion which led to arel a tive up lift of the SW and NE flanks (see be low). There fore, the pre vi ously used term “Lublin Graben” (¯elichowski, 1972;Narkiewicz et al., 1998a; Narkiewicz, 2003) is here re placedby a more de scrip tive “trough”.

The Lublin Trough is flanked to the south-west by the el e -vated horst-like belt of the Lower and Mid dle De vo niansubcrops (the Radom–Kraœnik High of ¯elichowski, 1972) that is de lim ited by the TTZ and Ursynów–Kazimierz andIzbica–Zamoœæ faults (Fig. 2). The deep-rooted Kock FaultZone de lim its the Lublin Trough to the north-east and is clearly out lined in the grav ity field (Królikowski and Petecki, 1995).Be yond this fault zone, the Pre cam brian base ment of the EastEu ro pean Plat form as cends north-eastwards to depths of lessthan 4 km and has been reached by sev eral deep bore holes.

The NW ter mi na tion of the Lublin Trough is com monlydrawn along the SW–NE strik ing Grójec Fault lo cated south ofWarszawa (e.g. ¯elichowski, 1983). This fault, which co in -cides with a dis tinct gra di ent zone in the grav ity field(Królikowski and Petecki, 1995), con trolled the Perm ian toMe so zoic ba sin de vel op ment and in ver sion (e.g. Dadlez, 1997) and can be traced as a strike-slip fault zone in the Perm ian-Me -so zoic cover (¯elichowski, 1983). On the other hand, the sig -nif i cance of this fault dur ing De vo nian and Car bon if er oustimes is ques tion able since lim ited bore hole con trol pro videsno ev i dence that it af fected the De vo nian and Car bon if er ous fa -cies pat tern (Po¿aryski et al., 1980, 1983; Mi³aczewski, 1983;Mi³aczewski et al., 1983). Con ceiv ably, Late Car bon if er ousdepositional gra di ents may have oc curred across a rather broadSW–NE or W–E trending zone in the area lo cated south ofWarszawa. A W–E strike of this zone is com pat i ble with thecon cepts of Po¿aryski (1986) and Po¿aryski et al. (1992) whoin ter preted a roughly W–E strik ing £uków Fault along the S

flank of the Podlasie De pres sion (Fig. 2). In ear lier pa pers,Po¿aryski et al. (1980, 1983) were un able to trace the GrójecFault on their depth-to-base ment map and ar gued that theLublin Trough ex tended fur ther to the WNW, with a grad ualwest erly de flec tion.

P£OCK AREA

The pre-Perm ian stra tig ra phy of the P³ock Area(¯elichowski, 1987a) is poorly known due to scarce bore holecon trol. Its bound aries with the Lublin Ba sin to the SE (seeabove) and the Pom er a nian area to the NW are only vaguelyde fined. Ac cord ing to ear lier con cepts, the P³ock Area is un der -lain by the sta ble War saw (Warszawa) Block, which forms thewest ern ex ten sion of the el e vated Mazury–BelarussianAnteclise of the EEP (Po¿aryski, 1975; Po¿aryski et al., 1980).The SW bound ary of the P³ock Area co in cides with the TTZ(Fig. 2), the lo ca tion of which is con strained by the DSS linesLT-4, LT-5 and P4 (Dadlez, 2006; Guterch and Grad, 2006).

POMERANIA

In Pomerania, the NE subcrop edge of the De vo nian strataco in cides with the Koszalin–Chojnice–Tuchola Fault Zone that cor re sponds to the Pom er a nian part of the TTZ, as con strainedby DSS data (Fig. 2; Dadlez, 2006; Guterch and Grad, 2006).To the north-east of this line, De vo nian and Car bon if er ous suc -ces sions were eroded, pre sum ably dur ing lat est Car bon i f er -ous–Early Perm ian times, re sult ing in the re moval of themainly prox i mal depositional sys tems of the ba sin mar gin.Based on fa cies pat terns, how ever, it is pos tu lated that De vo -nian and Early Car bon if er ous suc ces sions had orig i nally ex -tended over con sid er able dis tances north-eastwards, in ter mit -tently con nect ing the Pom er a nian depositional area with theBal tic Ba sin (¯elichowski, 1987b). The Kosza -lin–Chojnice–Tuchola Fault Zone is in ter preted as hav ingacted dur ing lat est Car bon if er ous and Early Perm ian times as acrustal-scale strike-slip fault sys tem (op. cit.). The SW bound -ary be tween the Pom er a nian area and the Variscan orogenicfront is poorly de fined ow ing to deep burial of the pre-Perm ianstrata (Dadlez et al., 1994).

STAGES OF BASIN DEVELOPMENT AND INVERSION

Based on the strati graphic re cord of the Pol ish Variscanfore land and an anal y sis of its sub si dence pat terns and mech a -nisms, as sum ma rized in Fig ures 3 and 4, six ma jor stages canbe dis tin guished in the de vel op ment of its De vo nian and Car -bon if er ous sed i men tary bas ins, in clud ing their lat est Car bon if -er ous in ver sion.

DEVONIAN — THERMALLY DRIVEN SUBSIDENCE AND REGIONAL EXTENSION

Fol low ing the end-Si lu rian fi nal su tur ing of the TESZterrane com plex to the mar gin of the EEC, Lower De vo nian


basal clastic rocks up to 200 m thick, onlapping var i ous Pro -tero zoic to Lower Palaeozoic rocks, were de pos ited in much ofthe study area. Only in the £ysogóry–Radom and Lublin re -gions did open ma rine sed i men ta tion con tinue across the Si lu -rian-De vo nian bound ary (Fig. 6). This area was also char ac ter -ized by al most con tin u ous Early De vo nian ac cu mu la tion of

mar ginal ma rine to con ti nen tal clastic de pos its (Figs. 3 and 7)that reached a thick ness of 1200–1500 m. Close to theEarly-Mid De vo nian bound ary, a shal low-wa ter car bon ateplat form was es tab lished across the en tire De vo nian ba sin ex -cept for its mar ginal parts in the Lublin and Pom er a nian ar eas(Fig. 3). The Late De vo nian depositional pat tern com prises


Fig. 6. Palaeogeographic map of the Pol ish Variscan fore land in the De vo nian (based on var i ous sources cited in the text)

VVF — Vladi mir Volynski Fault; other ex pla na tions as in Fig ure 2

shal low-wa ter car bon ate plat forms, reefs and deeper-shelf sys -tems. The thick ness of these car bon ate-marly se quences is gen -er ally close to 1 km ex cept for the Lublin Ba sin where it may at -tain ca. 2.5 km, con sist ing mostly of Up per De vo nian de pos its.On the other hand, the Mid dle De vo nian of the£ysogóry–Radom Block is ex cep tion ally thick (more than1 km) and is mainly com posed of marly de pos its of a shelf ba -sin. No De vo nian has so far been en coun tered in the P³ockArea, ei ther due to non-de po si tion or sub se quent ero sion. It ap -pears plau si ble, how ever, that dur ing the Late De vo nian globalhigh-stand in sea level, that is clearly re flected in ad ja cent re -gions, shal low-ma rine strata were de pos ited also in the P³ockArea, and later eroded in pre-Westphalian times.

Pre vi ous stud ies have dem on strated the role of eustatic con -trols on cy clic de po si tion dur ing the Mid and Late De vo nian(Narkiewicz, 1988; Racki, 1997; Narkiewicz et al., 1998a;Racki and Narkiewicz, 2000; Fig. 7). The pat tern of as ymp tot i -cally de creas ing tec tonic sub si dence (Fig. 4) is typ i cal of ther -mal re lax ation of the litho sphere af ter a rift ing and/or ther malevent (see e.g. Ziegler and Cloetingh, 2004 and the ref er encesgiven therein). On the other hand, field ex am ples of De vo niansyn-sed i men tary fault ing and palaeostress data con sis tentlypoint to a gen er ally extensional re gime.

The tec tonic bound ary be tween the Up per Silesian andMa³opolska blocks shows ev i dence for Late De vo nian to EarlyCar bon if er ous ver ti cal block move ments and as so ci ated bi -modal magmatism un der con di tions of subhorizontal ex ten sion (¯aba, 1999). NNW–SSE-di rected ex ten sion was sug gested by Jarosiñski (2001) and Poprawa et al. (2001) for the Late De vo -nian-Tournaisian in the east ern most, sub-Carpathian part of the Up per Silesian Block. Well-doc u mented transtension pre vailed in the Holy Cross Mts. area dur ing the late Emsian andFamennian while the most pro nounced syn-sed i men taryextensional tec ton ics are trace able in that area dur ing the LateDe vo nian (Szulczewski et al., 1996; Racki and Narkiewicz,2000; Lamarche et al., 2002, 2003; Figs. 6 and 7). Mea sured di -rec tions of a max i mum ex ten sion range in the Holy Cross Mts.from W–E to SW–NE chang ing to N–S (Lamarche et al.,2003). The Holy Cross Fault clearly sep a rated the£ysogóry–Radom Block, char ac ter ized by in creased Lowerand Mid dle De vo nian sub si dence, from the more sta bleMa³opolska Block (Fig. 4).

Com menc ing in the mid-Frasnian, re gional ex ten sion con -trolled strong sub si dence in the Lublin Ba sin, as seen in the de -vel op ment of a dis tinct depocentre (Narkiewicz et al., 1998a).The ge om e try of this depocentre, as out lined by isopachs of thelower Famennian ma rine marly de pos its (Fig. 7), con firmssyn-sed i men tary ac tiv ity along the Ursynów–Kazimierz Faultin the SW and the Kock Fault Zone in the NE. Famennian de -pos its show ev i dence of syn-sed i men tary de for ma tion, such as


Fig. 7. De vo nian-Lower Car bon if er ous stra tig ra phy in the HolyCross Mts. in the con text of the most im por tant eustatic and tec tonicevents (De vo nian part based mainly on Racki and Narkiewicz, 2000,

Car bon if er ous on Szulczewski et al., 1996)

South ern part of the HCMts. cor re sponds to the north ern Ma³opolskaBlock, whereas the £ysogóry area to the north ern £ysogóry–Radom Block; full names of the Mis sis sip pian chronostratigraphic units as in Fig ure 2

slump ing and boudinage (un pub lished core ob ser va tions), both phe nom ena at trib uted here to seis mic ac tiv ity.

For Pomerania, ¯aba and Poprawa (2006) pos tu lated thatMid and Late De vo nian ba sin de vel op ment was con trolled by a two-phase extensional re gime, with the ear lier pulse prob a blybe ing of sinistral transtensional type and the late pulse, af ter adextral transpressional phase, of extensional or dextraltranstensional type.

Con tin u ous ma rine sed i men ta tion across the De vo -nian-Car bon if er ous bound ary is doc u mented only in thesouth ern Holy Cross Mts. (Fig. 7; Malec, 1995). Con densedse quences or non-depositional gaps are rec og nized in theUSCB (Be³ka, 1985) and Pomerania (Matyja and Stempieñ- Sa³ek, 1994). The De vo nian-Lower Car bon if er ous un con -formity is known from bore holes in the south ern part of theMa³opolska Block (Jawor and Baran, 2004), whilst its pres -ence in north ern Pomerania re mains prob lem atic (Dadlez,1978). Ev i dence for block fault ing at trib uted to the Bretoniantec tonic phase has also been re ported for the Kra -ków–Lubliniec Fault (¯aba, 1999).

In the Lublin Ba sin, late Famennian syn-sed i men tary ac tiv ity along the Kock and Vladi mir Volynski faults caused ero sion onthe blocks ad ja cent to the north and lo cal ized de po si tion of thickmar ginal ma rine clastic sed i ments to con ti nen tal red-beds(Fig. 6). Dur ing the Tournaisian to early Viséan an ero sional andnon-depositional re gime pre vailed in the en tire Lublin Ba sin, re -sult ing in the re moval lo cally of up to 1500 m of De vo nian and(in part) Lower Palaeozoic suc ces sions.

TOURNAISIAN TO MID-VISÉAN — MOBILE SHELF AFFECTED BY VOLCANISM

Dur ing Tournaisian to mid-Viséan times, a wide spreadshelf ba sin ex tended from south ern Po land to Pomerania(Fig. 8). Ma rine clastic de po si tion pre vailed whilst car bon ateplat forms de vel oped on el e vated intra-shelf and coastal base -ment blocks (¯elichowski, 1987b; Belka et al., 1996). Clasticde pos its, com monly con tain ing a con sid er able volcaniclasticad mix ture, at tain thick nesses of the or der of sev eral hun dredsup to one thou sand metres. Al lu vial to near-shore ma rineclastic de pos its grade basinwards into fine-grained off shorefa cies (Pomerania); the lat ter are dom i nated by dark si li ceousshales and mudstones on the Ma³opolska Block and in thenorth ern USCB area.

The Car bon if er ous of the £ysogóry–Radom Block isknown only from a few bore holes in a tec tonic graben of theStudzianna–Osta³ów area (Fig. 2). In com plete sec tions com -prise sev eral hun dred metres of in ter ca lated arkosic sand -stones, siltstones and dark shaly mudstones yield ingpalynomorphs of late Tournaisian to (?) ear li est Viséan age(Turnau in: Jaworowski, 2002). Coarser-grained beds con -tain, in ad di tion to re de pos ited shal low-wa ter car bon ates,abun dant trachytic and rhyolitic volcaniclastic ma te rial, sug -ges tive of con ti nen tal ex ten sion (Krzemiñski, 1999).Jaworowski (2002) in ter preted this suc ces sion as com pris inggrav i ta tional mass flow de pos its that were de rived from ashal low shelf to the NE and that ac cu mu lated on a sub ma rineslope. This near-shore clastic belt prob a bly fringed the landarea com pris ing most of the pres ent Lublin re gion (Fig. 8).

Thus, the Tournaisian to early Viséan ba sin mar gin ap pears toco in cide ap prox i mately with the TTZ (Narkiewicz, 2003).Also in the Pomerania the ba sin mar gin ap par ently co in cidedroughly with the Koszalin–Chojnice–Tuchola Fault Zone,and was close to an area of acidic late Tournaisian vol ca nism(Muszyñski et al., 1996; Lipiec, 2001).

Dur ing the Tournaisian to mid-Viséan, tec tonic sub si -dence rates gen er ally de creased and came lo cally to a stand -still or were even re versed in re sponse to Bretonian tec ton ics(Fig. 4). Re gional ex ten sion trig gered wide spread magmatism that was par tic u larly in tense dur ing the late Tournaisian andearly Viséan along the NE ba sin mar gin; more over, it con -trolled depositional pat terns of car bon ate plat forms on el e -vated blocks. On the Ma³opolska Block (S Holy Cross Mts.)and the USCB the re la tion ship be tween vol ca nic ep i sodes and ver ti cal move ments of car bon ate plat forms can be dem on -strated (Be³ka, 1987; Belka et al., 1996). Mag matic ac tiv itywas in tense also in cratonic do mains to the NE of the TTZ, asseen in the oc cur rence of diabase and syenite in tru sions in theP³ock Area (¯elichowski in: Marek, 1983) and of largemafic-al ka line in tru sive bod ies in NE Po land (Fig. 8;Krzemiñska et al., 2006).

LATE VISÉAN — ONSET OF OROGENIC COMPRESSION

Dur ing the late Viséan, Car bon if er ous bas ins at tained theirmax i mum ex tent and en croached on all re gions de scribed ex -cept per haps for the P³ock Area (Fig. 9). A mo bile clastic shelf,typ i cal of the pre ced ing stage, per sisted in Pomerania and onthe Ma³opolska Block and prob a bly also on the£ysogóry–Radom Block. In Pomerania, prograding clastic fa -cies mark a dis tinc tive re gres sion in the area of the TTZ, sug -gest ing syn-sed i men tary tec tonic ac tiv ity along the lat ter. Car -bon ate plat forms that had thrived dur ing the early Viséan wereter mi nated in the south ern USCB and in Pomerania roughly atthe turn of the Holkerian and Asbian (Lipiec and Matyja, 1998;Lipiec, 2001; Narkiewicz, 2005), whereas on the Ma³opolskaBlock their de vel op ment ceased dur ing the early Asbian (Be³ka et al., 1996).

Close to the Holkerian-Asbian bound ary the wes tern mostpart of the USCB car bon ate plat form be gan to sub side rap idlywhilst the re main der of this plat form was up lifted, dis sectedinto blocks and eroded. In the area of the Sub-Carpathian Arch,ero sion lo cally re moved more than 500 m of Lower Car bon if -er ous and Up per De vo nian car bon ates (Narkiewicz, 2005).This ero sional sur face, which dis plays ev i dence ofkarstification, was onlapped and pro gres sively over steppedfrom the west by late Viséan and ear li est Namurian A clasticde pos its that rest with a low-an gu lar un con formity on their sub -strate (Fig. 3). This transgressive se quence con sists in the westof ma rine shales, siltstones and sand stones up to 1500 m thick(Malinowice Fm.; Fig. 5) that thin east ward and grade intonear-shore and con ti nen tal clastic de pos its con tain ing a fewcoal beds (Zalas Fm.; Fig. 5). This se quence grades west wardsinto the Early Car bon if er ous flysch of the Moravian-SilesianBelt, and con se quently it was in ter preted by Kotas (1995) as its dis tal equiv a lent (“flysch as so ci a tion”).

The gen eral late Viséan-ear li est Namurian depositional ar -chi tec ture of the USCB (Fig. 5), com bined with the pat tern of


its sub si dence (Fig. 4), re flect the de vel op ment of a flex uralfore land ba sin on the Brunovistulian lower plate in re sponse toits tec tonic load ing by the Moravian-Silesian orogenic wedge(Bu³a and ̄ aba, 2005). This in ter pre ta tion is com pat i ble with alate Viséan rapid eastwards mi gra tion of the depocentre of thisba sin (Be³ka, 1987) and a gen eral west ern prov e nance of de tri -tal ma te rial (Paszkowski et al., 1995; Œwierczewska, 1995,sum ma rized by Gradziñski et al., 2005).

In the Lublin Ba sin, the late Viséan sed i men tary-tec tonic cy -cle was pre ceded by the ex tru sion of lat er ally dis con tin u ous, lo -cally up to 230 m thick vol ca nic rocks of ba saltic com po si tion

that have yielded K-Ar ages of 339–325 Ma (Depciuch, 1974;Grocholski and Ryka, 1995). Dur ing the Asbian and earlyBrigantian, a late Viséan 50 to 200 m thick car bon ate-clayeyshelf se quence onlapped NE-wards the Bretonian un con formity(Skompski, 1998). Dur ing this time, the Kock Fault Zonemarked the bound ary be tween a more sta ble car bon ate plat forms to its NE, and a more rap idly sub sid ing car bon ate-clayey shelf tothe SW. The SW mar gin of the shelf is es sen tially un known.Rather than cor re spond ing to a dis crete shelf edge, it could haveformed a gen tle slope tran si tional to a slightly deeper en vi ron -ment, char ac ter ized by dark mudstones and quartz arenites with


Fig. 8. Palaeogeographic map of the Pol ish Variscan fore land in the Tournaisian to mid-Viséan (based on var i ous sources cited in the text)

Other ex pla na tions as in Fig ures 2 and 6

greywacke in ter ca la tions, typ i cal of the late Viséan of the HolyCross Mts. (¯akowa and Migaszewski, 1995). A ten ta tive po si -tion of this fa cies tran si tion is shown in Fig ure 9, as sum ing that itwas con trolled by syn-depositional ac tiv ity along the TTZ. Thegen eral late Viséan palaeo ge ogra phy sug gests that clastic ma te -rial oc cur ring on the Ma³opolska Block was de rived from the ris -ing Variscan Orogen in the west. Cor re spond ingly, these de pos -its can be in ter preted as prob a ble dis tal equiv a lents of thesynorogenic flysch, doc u mented in the “Variscan Externides”(e.g. Krzemiñski, 2005).

EARLY NAMURIAN A — EROSION AND PARALIC SEDIMENTATION

At the turn of the Early to Late Car bon if er ous thepalaeogeographic set ting of Po land un der went a ma jor re or ga -ni za tion. Whilst dur ing the Namurian A the Ma³opolska,Radom–£ysogóry (?), and Pomerania re gions be came ex posedand sub jected to ero sion, the USCB and the Lublin Ba sin con -tin ued to sub side, as seen in the ac cu mu la tion of paraliccoal-bear ing se quences. In South ern Po land this change may be in ter preted as re flect ing NE-wards mi gra tion and ae rial ex pan -


Fig. 9. Palaeogeographic map of the Pol ish Variscan fore land in the late Viséan (based on var i ous sources cited in the text)

Other ex pla na tions as in Fig ures 2 and 6

sion of the forebulge that had de vel oped dur ing the late Viséanin the east ern USCB (Narkiewicz, 2005). An al ter na tive ex pla -na tion is a broad-scale lithospheric buck ling in re sponse to thebuild-up of col li sion-re lated intraplate compressional stresses(Fig. 10). The lat ter in ter pre ta tion (sug gested by P. A. Ziegler,2007, pers. comm.) seems more prob a ble given the con sid er -able width and oblique ori en ta tion of the up lifted area rel a tiveto the hy po thet i cal orogenic front.

In the USCB, the late Viséan de pos its grade up wards intorhyth mi cally bed ded flu vial and, subordinately, ma rinecoastal-deltaic de pos its of the Paralic Se ries (Gradziñski et al.,

2005). This “coal-bear ing paramolasse” (Kotas, 1994) is up to3500 m thick, thins pro gres sively eastwards and ul ti matelypinches out (Figs. 5 and 10). Ac cu mu la tion of this suc ces sionoc curred dur ing a cy cle of in creased tec tonic sub si dence of theflex ural fore land ba sin that had com menced dur ing the lateViséan and that re flects the pro gres sive evo lu tion of theMoravian-Silesian orogenic wedge. The Namurian Adepositional re gime of the USCB re flects a bal ance be tweensub si dence rates and sed i ment sup ply from the eroded orogenas well as from the Sub-Carpathian Arch (Kotas, 1995). Sed i -men ta tion prob a bly over stepped the Kraków–Lubliniec tec -


presumablemarine connection

isopachs (in metres)alluvial-deltaic(paralic) deposition

300

ORO

GEN

?

?

?

FLYSCH

FLYSCH

?

?

LUBLIN BASIN

UPPER SILESIAN BASIN

500

400

300

20

06

00

1000

14

00

18002200

26003000

14 19o

24 E

o54 N

52

50

0 200 km100

Fig. 10. Palaeogeographic map of the Pol ish Variscan fore land in the early Namurian A (based on var i ous sources cited in the text)

Isopachs in the Lublin Ba sin re fer to the Terebin Fm., in the Up per Silesian Ba sin to the Paralic Se ries (cf. Fig. 5); other ex pla na tions as in Fig ures 2, 6 and 9

tonic line, as in di cated by oc cur rences of Namurian A de pos itsin the SW part of the Ma³opolska Block area re ported by¯akowa and Jurkiewicz (1995) and Jawor and Baran (2004).

In the Lublin Ba sin, the pre dom i nantly clayey-car bon atesuc ces sion gave way dur ing the lat est Viséan to paraliccyclothems com pris ing mostly siliciclastic shal low-ma rine todeltaic and flu vial fa cies con tain ing sub or di nate lime stone andcoal ho ri zons (Skompski, 1998; Waksmundzka, 1998, 2005).This suc ces sion at tains a max i mum thick ness of 600 m near the SW mar gin of the Lublin Trough, par tic u larly in its cen tral andSE seg ment, whereas to wards the NE it thins across the KockFault Zone and wedges out be yond it. The in ferred SW mar ginof the ba sin was prob a bly lo cated be yond the pres ent SW tec -tonic bound ary of the Lublin Trough that ap par ently cross-cutsfa cies and palaeothickness pat terns (¯elichowski andKoz³owski, 1983).

No Up per Car bon if er ous has been en coun tered so far onthe Ma³opolska and £ysogóry-Radom blocks. Un til more datacan be ob tained it is safe to as sume that these ar eas were ex -posed and sub jected to ero sion start ing from the Namurian Atimes. If so, the tec toni cally ac tive SW mar gin of the LublinBa sin may have been con trolled by the TTZ.

The di rec tion of ad vance of ma rine in cur sions from theflex ural Variscan fore land ba sin into the Lublin Ba sin is stillun cer tain. Avail able data sug gest that the Namurian A de pos -its pinch out to wards the west and north (¯elichowski andKoz³owski, 1983). At the same time this suc ces sion be comesthicker to wards the SE where, how ever, it was eroded in theeast ern Lviv area of Ukraine (Fig. 1). Nev er the less, it is con -ceiv able that the Lublin Ba sin was con nected in one way oran other to the fore land flysch ba sin of the South east ernVariscan Orogen.

NAMURIAN B-WESTPHALIAN — CONTINENTALSEDIMENTATION

The end of the Namurian A cor re sponds to a re gional breakin sed i men ta tion (Fig. 3) that ap par ently is not as so ci ated withsig nif i cant tec tonic de for ma tion (Kotas, 1994; Narkiewicz etal., 1998b). This sug gests a still-stand in tec tonic sub si dence oreven a small up lift that is prob a bly su per im posed on an eustaticlowstand in sea level (mid-Car bon if er ous event; Saunders andRamsbottom, 1986). Dur ing the Namurian B the depocentresof the Up per Silesian and Lublin bas ins were re-ac ti vated(Fig. 10), al though with a con sid er able re-ar range ment of sub -si dence pat terns. This may point to struc tural con trols on thelate Namurian A hi a tus.

In the USCB, sed i men ta tion re sumed un der ex clu sivelycon ti nen tal al lu vial con di tions while the depocentre shiftedeastwards (Fig. 5). The main part of the “coal-bear ingorthomolasse” (Kotas, 1994), com pris ing the Namurian B tolower Westphalian C, dis plays prom i nent thick ness gra di ents,pinch ing out of par tic u lar depositional units and the oc cur rence of intra-formational ero sional sur faces to wards the east ern ba -sin mar gin. The up per most part of this suc ces sion is com posedof late Westphalian D coarse-grained de pos its. These are onlyknown from the east ern part of the ba sin where their de po si tionwas pre ceded by a sed i men tary gap com pris ing lateWestphalian C to early Westphalian D. Stephanian red beds of

sub or di nate thick ness un con form ably over lie older Car bon if er -ous rocks, clearly post dat ing ba sin in ver sion.

The sub si dence pat tern dem on strates (Figs. 4 and 5) that the post-Namurian A change in ba sin ar chi tec ture was as so ci atedwith a sec ond orogenic phase and con com i tant thrust-load ingof the west ern mar gin of the Brunovistulian plate. Terrigeneous sed i ments, gen er ally more coarse-grained than dur ing the ear -lier phase, were sup plied from the west but also from the south -ern Sub-Carpathian Arch (Kotas, 1995).

With the Namurian B re sump tion of sub si dence of theUSCB, the NE mar gin of the Up per Silesian Block un der wentstrong dextral transpressional de for ma tion. High-an gle thrust -ing of the west ern wall of the Kraków–Lubliniec Fault zoneover the Ma³opolska Block was as so ci ated with sec ond aryfold ing and re verse-fault ing. This was fol lowed in the lateNamurian and Westphalian by sub-hor i zon tal ex ten sion andblock up lift (¯aba, 1999), ac com pa nied in the Westphalian Bby magmatism that peaked in the em place ment of calc-al ka linegranitoids north-east of the Kraków–Lubliniec Fault (Fig. 11).

The Lublin Ba sin depocentre of the re newed sub si denceshifted dur ing the late Namurian slightly to wards the NE (com -pare isopachs of the Dêblin Fm. in Fig. 11 with those of theTerebin Fm. in Fig. 10). Dur ing the Westphalian thedepocentre was lo cated in the NW part of the Lublin Ba sin andex tended fur ther NW-wards into the P³ock Area (Fig. 11). TheNamurian B to Westphalian C (D?) suc ces sion in cludescoal-bear ing cyclothems com posed of al lu vial clastic de pos itswith an up wards de creas ing pro por tion of deltaic ma rine fa cies. Its thick ness de creases from up to 1500 m in the ax ial NW partof the ba sin to ca. 600 m in SE part (¯elichowski, 1972, 1983;¯elichowski and Koz³owski, 1983; Porzycki, 1984). In theP³ock Area, Westphalian A to C (D?) de pos its rest with a thickbasal con glom er ate con tain ing rhyolitic clasts un con form ablyon the Si lu rian suc ces sion, and con sist of con ti nen tal clasticsuc ces sion up to 1000 m thick that is cor re la tive with the north -west ern Lublin re gion (¯elichowski, 1983, 1995) and wedgesout to the NE. There is no di rect proof of synsedimentary faults ac tiv ity in the Lublin and P³ock ar eas, al though Up per Viséanto Namurian depositional ar chi tec ture strongly sug gests thatthe Kock Fault Zone con trolled sub si dence and sed i men ta tionpat terns (Waskmundzka, 2005; Narkiewicz et al., 2007b). Thisand other cir cum stan tial ev i dence sug gests a pull-apartdepositional-sub si dence re gime (¯elichowski, 1983;Narkiewicz et al., 1998b). Par tic u larly the NW-wards mi gra -tion of the depocenter points to (dextral?) strike-slip move -ments along the TTZ. It is here as sumed that the TTZ boundedthe Lublin Ba sin to the SW.

In Pomerania, Westphalian B to Stephanian A–B con ti nen -tal clastic de pos its un con form ably over lie var i ous Lower Car -bon if er ous and De vo nian rocks (¯elichowski, 1995) and fillWNW-trending grabens in the NW part of the area where theyat tain thick nesses of severals hun dred metres. ¯elichowski(1995) pos tu lated that these grabens formed as pull-apart bas -ins in re sponse to strike-slip move ments along the TTZ.

LATE WESTPHALIAN-EARLY STEPHANIAN INVERSION

Dur ing the late Westphalian D and early Stephanian(“Asturian tec tonic phase”) the en tire area of the Pol ish


Variscan fore land was sub jected to strong com pres sion(Fig. 11). The age of the re sult ing struc tures is best con strainedin the USCB where an an gu lar un con formity be tween theWestphalian D and an in def i nite part of the Stephanian is ob -served (Fig. 5). In the Lublin Ba sin, de formed Westphalian C(?D) strata are un con form ably over lain by Perm ian and youn -ger de pos its, whereas in Pomerania the un con formity oc curs

be tween the Stephanian A–B and ?up per Stephanian-low er -most Perm ian de pos its (¯elichowski, 1987b).

At the west ern mar gin of the USCB, the Orlova and re latedthrusts tes tify to E-di rected com pres sion with a dextralstrike-slip com po nent (Bogacz and Krokowski, 1981). Themain part of this ba sin, ad ja cent to the E, is char ac ter ized bygen tle fold ing with su per im posed W–E trending faults of


Fig. 11. Palaeogeographic map of the Pol ish Variscan fore land in the Namurian B to Westphalian

Mea sured di rec tions of late Westphalian–early Stephanian com pres sion af ter Jarosiñski in Narkiewicz et al. (2007b), Lamarche et al. (2003) and ¯aba(1999); SMCE — Stê¿yca-Me³giew Cen tral El e va tion; other ex pla na tions as in Fig ures 2, 6 and 9

mixed dip-slip and dextral strike-slip char ac ter (Kotas, 1985,1994; Fig. 5). These Variscan struc tures dis play am pli tudes upto 2000 m and gen er ally fol low the E–W di rected struc turalgrain of the Pro tero zoic base ment (Bu³a and ¯aba, 2005). Co -eval dextral transpressional de for ma tion af fected the NE mar -gin of the Up per Silesian Block, al though their mag ni tude wassmaller than dur ing the ear lier post-Namurian A phase (Bu³aand ¯aba, 1997; ¯aba, 1999). Whereas Kotas (1985) and Bu³aand ¯aba (2005) pos tu lated N-di rected com pres sion, the hor i -zon tal compressional stress axis changed ac cord ing to ¯aba(1999) from N–S to NE–SW at the turn of the Westphalian tothe Stephanian (Fig. 11). The re lated up lift and ero sion of thewest ern part of the USCB is es ti mated to amount to ca. 3–4 km, based on ex trap o lated sed i ment thick nesses from the east(Fig. 5). For the NE and cen tral parts of this ba sin Belka (1993)es ti mated the mag ni tude of ero sional unroofing at 1200 m and2000–3000 m, re spec tively.

In the intraplate do main of SE Po land, late Variscan de for -ma tion re sulted in the de vel op ment of faulted folds with vary -ing am pli tudes and wave lengths (Fig. 12). In the Holy CrossMts., such struc tures strike ap prox i mately nor mal to the N–S to NNE–SSW di rec tion of the Variscan short en ing (Lamarche etal., 2003). The most in tense de for ma tion, with am pli tudes ofup to 4 km is as so ci ated with the Holy Cross Fault Zone and in -volves a pos i tive flower-like ar ray of sec ond-or der faults sug -ges tive of transpressional or i gin (Po¿aryski, 1990; Po¿aryskiand Tomczyk, 1993; Lamarche et al., 2003). Mizerski (1995)and Lamarche et al. (2003) stressed the sim i lar ity of theVariscan struc tural de vel op ment in both parts of the HolyCross Mts., thus im ply ing a com mon re sponse of theMa³opolska and Radom–£ysogóry blocks to the evo lu tion ofthe palaeostress field. As post-Viséan strata have not been en -coun tered so far on the Ma³opolska Block, its Variscan de for -ma tion was and still is com monly at trib uted to the “Sudetic tec -tonic phase” at the turn of the Viséan to the Namurian (e.g.Zdanowski, 1995; Jawor and Baran, 2004). How ever, con sis -tent pat terns of compressional stress field tra jec to ries in the en -tire SE Pol ish Variscan fore land (Fig. 11) are sug ges tive of thecom mon deformational phase which af fected this area dur ingthe lat est Westphalian to early Stephanian.

The cross-sec tion of the Lublin Trough re veals the con fig u -ra tion of a trun cated broad syncline, the up lifted flanks ofwhich are as so ci ated with the deep-seated Ursy -nów– Kazimierz and Izbica–Zamoœæ faults, and the Kock Fault Zone (Fig. 12). The Ursynów–Kazimierz Fault shows ev i dence for its pre-Perm ian transpressional re ac ti va tion that was ac -com pa nied by strong up lift of the south west ern block that isbounded to the SW by the Nowe Miasto–Radom Fault Zone.Seis mic data re veal that this block, which is com posed of de -formed De vo nian strata and un con form ably over lain by Perm -ian-Me so zoic sed i ments, is transected by NW–SE strik ingfaults (Krzywiec, 2007). It prob a bly rep re sents a (sinistral?)transpressional in ver sion zone across which about 3 km ofstrata were eroded.

In the SE, the Izbica–Zamoœæ Fault has a re verse throw ofca. 1 km (¯elichowski, 1972) whereas in the NE the KockFault Zone is a com plex nar row zone of re verse fault ing andfold ing, lo cally in volv ing thin-skinned de coup ling at the level

of the Lower Palaeozoic shaly suc ces sion (Krzywiec andNarkiewicz, 2003a, b; Krzywiec, 2007).

In ter nally, the Lublin Trough is dis sected by a sys tem ofroughly NW–SE strik ing, both SW and NE dip ping re versefaults with as so ci ated anticlines, in ter preted as pos i tive flowerstruc tures (Po¿aryski and Tomczyk, 1993). The most prom i -nent of these is the Stê¿yca–Me³giew Cen tral El e va tion(Fig. 12), prob a bly a deeply rooted struc ture that was mod i fiedin its cen tral seg ment by de tach ment at the mid-Frasnianevaporitic ho ri zon (Narkiewicz et al., 2007). The an ti cli nalstruc tures show ev i dence of ro ta tion of the com pres sion stressaxis from SSW–NNE to WSW–ENE with a cor re spond ingchange from north east-di rected thrust ing to sinistraltranspression (Jarosiñski, 2004, unpubl. re port; Narkiewicz etal., 2007). In the cen tral seg ment of the Lublin Trough, post-in -ver sion ero sion re moved lo cally up to 1600 m of the Car bon if -er ous strata, whilst east of the Kock Fault Zone 500 m or lessstrata were eroded.

Gen er ally speak ing, in ar eas to the NE of the USCB thestron gest compressional de for ma tion and the larg est mag ni -tudes of in ver sion are con fined to nar row fault zones, in clud ingthe Kraków–Lubliniec and Holy Cross faults, as well as to thema jor lon gi tu di nal faults of the Lublin Ba sin area. Struc turesthat evolved along all of these dis con ti nu ities, which partlyform the bound aries be tween crustal blocks, dis play astrike-slip com po nent and are thick-skinned. The sense of thestrike-slip dis place ment along the dif fer ent faults may, how -ever, dif fer (com pare e.g. the Kraków–Lubliniec Fault and theLublin Ba sin; Fig. 11).

In Pomerania, the style of late Variscan de for ma tion ispoorly known and is here ten ta tively at trib uted to strike-slipmove ments along the TTZ (¯elichowski, 1987b). Based onmesostructures ob served in cores, ¯aba and Poprawa (2006)pos tu lated two Late Car bon if er ous-Early Perm ian phases ofdextral transpression and thrust ing that are sep a rated by atranstensional phase.

REACTIVATION OF OLDER CRUSTALDISCONTINUITIES

Data pre sented in this pa per show that the “mem ory of thelitho sphere” (Cloetingh et al., 2005) played an im por tant rolein the de vel op ment and in ver sion of De vo nian and Car bon if -er ous sed i men tary bas ins in the Pol ish Variscan fore land. This per tains spe cif i cally to the re peated re ac ti va tion of pre-ex ist -ing crustal dis con ti nu ities cor re spond ing to the bound ariesbe tween prob a ble Cal edo nian ter ranes, such as theKraków–Lubliniec and Holy Cross faults, as well as to theSW mar gin of the EEC that co in cides with theTeisseyre-Tornquist Zone.

The Kraków–Lubliniec Fault was par tic u larly ac tive dur ing the Car bon if er ous when it fo cused transtensional and mostlydextral transpressional de for ma tion, as clearly doc u mented byex cel lent mesostructural anal y ses (¯aba, 1999). In volve mentof the deeper crust and prob a bly of the man tle is ev i denced bybi modal magmatism, in clud ing the em place ment of gran itesdur ing the Westphalian. This crustal dis con ti nu ity af fected ba -



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sin evo lu tion by con trol ling the lo ca tion of fa cies gra di ents dur -ing the Early Car bon if er ous and the depositional mar gin in theLate Car bon if er ous.

The Holy Cross Fault sep a rated two ar eas of dif fer ing De -vo nian depositional and sub si dence de vel op ment, with the£ysogóry–Radom Block dis play ing in creased mo bil ity, par tic -u larly in the Mid dle De vo nian. Dur ing the Late Car bon if er ousphase of fore land com pres sion, the Holy Cross Fault acted as atranspressional zone char ac ter ized by sig nif i cant in ver sion am -pli tudes (Lamarche et al., 2003). Palaeogeographic re con struc -tions by Belka et al. (1996) sug gest that WNW–ESE strik ingfault-con trolled base ment highs gov erned the de vel op ment ofEarly Car bon if er ous car bon ate plat forms in the Ma³opolskaarea (Fig. 8).

The TTZ is here in ter preted as hav ing strongly in flu encedthe ar chi tec ture of the De vo nian to Early Car bon if er ous strata inPomerania, with ar eas of in ter mit tent up lift and ero sion lo catedon the EEP (Figs. 8–11). It is likely that the ba sin mar gin wascon trolled by an ar ray of down-step ping blocks along the cratonmar gin rather than by a sin gle fault. The late Tournaisian vol ca -nism in Pomerania ap pears to be as so ci ated with ac tiv ity alongin land part of this fault sys tem. Dur ing the Westphalian the TTZand re lated WNW trending faults were re spon si ble for de vel op -ment of transtensional grabens that in the mid-Stephanian werede formed un der a transpressional re gime.

The SE sec tor of the TTZ in volves the NoweMiasto–Radom Fault Zone and its SE ex ten sion con verg ingwith the Holy Cross Fault (Fig. 2). Dur ing the Mid De vo nianthis part of the TTZ clearly sep a rated the more mo bile blockin SW from the sta ble area in NE. The sub se quent his tory ofthis fault is hy po thet i cal and is here mostly based on in ter po -la tions be tween the Lublin Trough in the NE and the poorlycon strained evo lu tion of the £ysogóry–Radom Block. Itseems, how ever, con ceiv able that this fault con trolled re -gional sub si dence and fa cies gra di ents also dur ing the Car -bon if er ous (Figs. 8–11).

The Lublin Ba sin was dis sected by an ar ray of faults thatroughly par al lel the TTZ and that were transpressionally re ac ti -vated dur ing the lat est Westphalian. On the other hand,syn-sed i men tary ac tiv ity along these faults ap pears to vary intime and space. The Ursynów–Kazimierz Fault and the KockFault Zone con trolled Late De vo nian sub si dence pat terns(Fig. 6). The Kock Fault Zone was again ac tive dur ing the lateFamennian-ear li est Tournaisian Bretonian block move mentsand af fected also depositional sys tems dur ing the late Viséanand Namurian. More over, the fault sys tems of the Lublin areaap pear to be as so ci ated with mid-Viséan mag matic ac tiv ity(Fig. 8). Con ceiv ably the ar ray of craton-mar gin par al lel faults of the Lublin area rep re sents re ac ti vated hy po thet i cal base ment dis con ti nu ities that could had de vel oped to gether with the TTZdur ing the Neoproterozoic break-up of Rodinia (cf. Nawrockiand Poprawa, 2006).

BROADER REGIONAL CONTROLS — DISCUSSION

The evo lu tion of the Pol ish Variscan fore land re flects ingen eral terms the main stages of the De vo nian to Car bon if er -

ous struc tural-sed i men tary de vel op ment of the south ern mar gin of the Old Red Con ti nent that was con trolled by the col li sion ofGond wana-de rived microplates and ul ti mately of Gond wana(Ziegler, 1989, 1990). Sev eral as pects of the evo lu tion of thePol ish Variscan fore land closely match that of theRheno-Hercynian Zone in Ger many and Bel gium (e.g. Frankeet al., 1978; Franke, 2000, 2006):

1. An extensional re gime dur ing the De vo nian and EarlyCar bon if er ous (pre-late Viséan), the de vel op ment of a car bon -ate-siliciclastic mar ginal shelf, and in tense mag matic ac tiv itydur ing the Tournaisian and early Viséan.

2. In ten si fy ing syn-orogenic com pres sion dur ing the lateViséan and early Namurian A (“Sudetic phase”), and the de vel -op ment of Culm-equiv a lent flysch and paralic molasse in theUSCB.

3. Grad ual tran si tion from paralic de po si tion dur ing theNamurian to Westphalian coal-bear ing molasse sed i men ta tion.

4. Ter mi nal Variscan de for ma tion at the turn of theWestphalian and Stephanian (“Asturian phase”).

There are how ever some as pects of the Pol ish fore land evo -lu tion that do not readily fit into the geodynamic sce nario of theRheno-Hercynian Zone. These will be ad dressed in the fol low -ing dis cus sion.

DEVONIAN-EARLY (MID) VISÉAN EXTENSION

The be gin ning of De vo nian sed i men ta tion over large parts of Po land can be at trib uted to ini tial back-arc rift ing pre ced ing the Emsian on set of sea-floor spread ing in theRheno-Hercynian do main (Ziegler, 1990; Franke, 2000). This event is also rec og nized in the Moravian-Silesian area wheresyn-rift sed i men ta tion and vol ca nism started dur ing theEmsian (Schulmann and Gayer, 2000; Kalvoda, 2002). There gional ther mal sub si dence re lated to these events ap pears tohave con trolled also the De vo nian evo lu tion of the Pol ishVariscan fore land.

Phases of strong ex ten sion af fected the Lublin Ba sin inmid-Frasnian and in Famennian times. The mid-Frasnian eventis only weakly ex pressed in the Rheno-Hercynian Zone, butcor re sponds to the ini tial rift ing stage of thePripyat–Dniepr–Donets Graben (Narkiewicz et al., 1998b). Al -though ex act strati graphic cor re la tions have not yet been es tab -lished, it is likely that the Up per Frasnian Rechitsian toEvlanian ho ri zons in the Pripyat Graben, mark ing its earlysyn-rift phase (Kusznir et al., 1996), cor re spond to the on set ofac cel er ated sub si dence of the Lublin Ba sin (Narkiewicz et al.,1998a; unpubl. data). In both bas ins the ini ti a tion of sub si dence is marked by ma rine evaporites (much thin ner in the Lublinarea), and in both the max i mum sub si dence was at tained dur ing the Famennian. The lack of syn-rift vol ca nism in the Lublin Ba -sin is, how ever, a sig nif i cant dif fer ence that is con sis tent withits smaller sub si dence rates and con se quently weaker crustalex ten sion as com pared to the Pripyat–Dniepr–Donets Graben(Po¿aryski, 1986).

The compressional (?) Bretonian pulse is re flected in theLublin Ba sin by block tec ton ics of con sid er able mag ni tudewhilst in the Pripyat Graben it may be ten ta tively re lated merely to the ter mi na tion of the Late De vo nian rift ing stage.


The extensional re ac ti va tion of the Dniepr–Donets–Donbassys tem in the late early Viséan was as so ci ated with ex tru sivemag matic phe nom ena (Stephenson et al., 2006) — sim i lar as in the con tem po ra ne ous Lublin Ba sin. The mid-Viséanmagmatism of the Lublin Area is con sis tent with the gen eralpat tern of diachronous oc cur rence of rift-re lated mag matic ac -tiv ity in the south ern parts of the EEC, peak ing dur ing theGivetian in the Peri-Cas pian De pres sion, in the early Frasnianin the Donbas area, in the late Famennian-early Tournaisian inthe Pripyat Graben, and fi nally, mid-Viséan in the Lublin Ba sin (Wil son and Lyashkevich, 1996; Stovba et al., 1996;Narkiewicz et al., 1998b; Fokin et al., 2001). This cor re spondswith west wards prop a ga tion of rift ing ac tiv ity in the south ernEEC do main that was con trolled by a com mon palaeostress re -gime dom i nated by NW–SE to N–S di rected prin ci pal hor i zon -tal extensional stress tra jec to ries (Fokin et al. 2001).

Kusznir et al. (1996) con sid ered two al ter na tive mech a -nisms of the Pripyat Graben rift ing: (1) plume-in duced up lift,and (2) re mote plate-bound ary stress com bined with lo calplume up lift stress. The co eval rift ing/extensional event in thePripyat Graben and in the Lublin Ba sin ar eas within the frame -work of the con sis tent de vel op ment of the en tire Pripyat toDonbas sys tem points to wide re gional con trols re spon si ble forthe com mon stress-field evo lu tion, and thus fa vours the sec ondmech a nism. At the same time, wide spread and pro longedmagmatism sug gests that ther mal in sta bil ity at the base of thelitho sphere had a con sid er able re gional and tem po ral range and is there fore dif fi cult to ex plain in terms of a sin gle man tleplume (cf. Stephenson et al., 2006).

LATE VISÉAN-EARLY NAMURIAN A

In re sponse to in creas ing collisional cou pling of the OldRed Con ti nent and Gond wana, compressional stresses built upwithin the Variscan do main at the tran si tion to the late Viséan(Ziegler, 1990). Late Viséan clo sure of the Rheno-Hercynianback-arc ocean, as pos tu lated by Ziegler (1990), was ac com pa -nied by the de vel op ment of the flex ural Rheno-Hercynian fore -land ba sin and the ac cu mu la tion of the flysch-type “KulmGrauwacke” that prograded rap idly to wards the fore land(Franke et al., 1978; Ricken et al., 2000).

Fol low ing clo sure of the Moravian-Silesian Ba sin, dextraloblique subduction of the Brunovistulian plate un der the Cen tralSudetic orogenic wedge com menced in the late Tournaisian(Schulmann and Gayer, 2000; Mazur et al., 2006). Al thoughear li est greywackes are re corded dur ing the Tournaisian, rapidflysch progradation started dur ing the early Viséan and ac cel er -ated in the late Viséan (Kumpera and Martinec, 1995; Hartleyand Otava, 2001). This can be re lated to in creased up lift and ex -hu ma tion rates of the Moldanubian in ter nal parts of the orogen.Be tween 340–330 Ma (Holkerian-Asbian) the accretionarywedge un der went ver ti cal ex tru sion with as so ci ated ex ten sionand eastwards thrust ing to wards the fore land (Schulmann andGayer, 2000). Ac cord ing to Franke and ̄ elaŸniewicz (2002) thepres ent-day jux ta po si tion of the Cen tral Sudetes and theBrunovistulian Block was es sen tially achieved by ca. 325 Ma(roughly the Viséan-Namurian bound ary). A sim i lar sce nario isin ter preted for the Pol ish part of the Moravian-Silesian Belt beltby ¯aba et al. (2005).

In the USCB, the ear li est equiv a lents of the syn-orogenicCulm suc ces sion are late Viséan in age, con firm ing that only by this time this area be came in cor po rated into a flex ural fore landba sin in front of the NE-wards ad vanc ing orogen. De vel op -ment of the dis tal flysch was pre dated by a dis tinct ep i sode ofup lift and ero sion of the SE part of the USCB, prob a bly re flect -ing syn-collisional compressional fore land de for ma tion. Thisel e vated area was pro gres sively onlapped by up per Viséan andlower Namurian A de pos its to wards the east, dur ing the mainphase of flysch de po si tion in the Moravian-Silesian belt(Kumpera and Martinec, 1995; Schulmann and Gayer, 2000).

It is note wor thy that ma jor late Viséan and early Namuriancrustal short en ing in the Variscan Orogen is not re flected in any sig nif i cant compressional de for ma tion in its fore land. Gen er -ally, an extensional re gime pre vailed prob a bly un til the end ofthe Viséan through out the Ma³opolska and pre sum ably the£ysogóry–Radom Block. In the Lublin area, mid- to lateViséan ex ten sion was par tic u larly pro nounced as in di cated byba saltic magmatism fol lowed by re newed sub si dence. Thisagrees with the ear lier con cepts by ¯elichowski (1987a, b) ofthe TTZ act ing as a transtensional zone bound ing the LublinBa sin to the SW, and at the same time con trol ling the NE ero -sional edge of the Pom er a nian depositional area.

These events are con tem po ra ne ous with the ac cel er atedlate Viséan to Serpukhovian (=Namurian A) sub si dence ofthe Dniepr–Donets rift sys tem (Dvorjanin et al., 1996; Stovba et al., 1996). The ev i dence of late Viséan to Namurian A ex -ten sion in the south ern parts of the EEC may sug gest that theback-arc extensional sys tem was ac tive lon ger in the south -east ern part of the Old Red Con ti nent than in theRheno-Hercynian Zone of west ern Eu rope. Al ter na tively,Nikishin et al. (1996) and Fokin et al. (2001) pro posed thatthe ac cel er ated late Viséan-Namurian A sub si dence of theDniepr–Donets Graben was con trolled by col li sion-re latedcompressional forces trans mit ted from the south ern con ti nentmar gin (their Scythian Orogen).

NAMURIAN B-WESTPHALIAN C

Ac cord ing to Schulmann and Gayer (2000), theMoravian-Silesian accretionary wedge un der went con tin u ousNE-di rected dextral transpression af ter its em place ment on theBrunovistulian fore land around 330 Ma, ac com pa nied by mod -er ate short en ing un til ca. 310 Ma (Westphalian C). This is inagree ment with the ob ser va tions from the Pol ish part of theMoravian-Silesian Belt as well as from the USCB where a thick con ti nen tal molasse-type se quence ac cu mu lated dur ing the sec -ond phase of the foredeep sub si dence. It is rather in trigu ingthat pro nounced dextral transpressional de for ma tion oc curredalong the NE mar gin of the USCB af ter the Namurian A andnot ear lier dur ing the pre ced ing orogenic phase. Con ceiv ablythis may be at trib uted to the build-up of north-di rectedcompressional stresses that were ex erted by the SE VariscanOrogen on the Pol ish fore land where they in ter fered with theNE di rected compressional stresses em a nat ing from theMoravian-Silesian Belt. This stress re gime may have been alsore spon si ble for the up lift of the Ma³opolska and£ysogóry–Radom blocks, as well as for the dextral strike-slipre ac ti va tion of the TTZ and as so ci ated fault sys tems that con -


trolled the sub si dence of the Lublin Ba sin. The lat ter ba sin was pre sum ably con nected with prox i malfore land bas ins of the SE Variscan Belt. From theNamurian B on wards the Lublin and P³ock ar eas,lo cated on the mar ginal parts of the EEC, started tode velop in con cert with the re main ing part of thePol ish Variscan fore land. This in di cates that thewest ern and prob a bly also the south ern EEC mar gin be came by that time dom i nated by a uni formpalaeostress field and con sis tently re sponded tofar-field com pres sion em a nat ing north wards fromthe SE Variscan Orogen. The in ferred dextral senseof the Late Car bon if er ous strike-slip move mentsalong the TTZ is con sis tent with the co-eval dextraltranstension at its NW pro lon ga tion, i.e. in the areaad ja cent to the STZ (Fig. 1; Thybo, 1997).

END WESTPHALIAN-EARLY STEPHANIANINVERSION

The fi nal compressional de for ma tion of theVariscan fore land oc curred in its dif fer ent partsroughly si mul ta neously at the Westphal -ian-Stephanian tran si tion, though the strati graphicres o lu tion of this event is vari able. Palaeostress datain di cate that dur ing this time-span the tra jec to ries of prin ci pal compressional hor i zon tal stress axes ro -tated on a re gional scale from nearly N–S toNE–SW. In all the re gional units an a lyzed, thestrike of re sult ing struc tures re flects the re ac ti va tionof pre-ex ist ing crustal dis con ti nu ities. Their com montranspressional over print is re lated to their oblique ori en ta tionwith re spect to the pre vail ing compressional stress tra jec to ries.Ob served per mu ta tions in the sense of transpression are prob a -bly re lated to vari a tions in the strike of re ac ti vated base mentdis con ti nu ities.

Whereas the NE di rected com pres sion is con sis tent withthe trans port di rec tion of the Moravian-SilesianFold-and-Thrust-Belt (Schul mann and Gayer, 2000), the ear -lier north-di rected com pres sion points to stresses em a nat ingfrom the SE Variscan Orogen. It is note wor thy that in theMoravian-Silesian Belt dextral late-stage transpression de vel -oped pro gres sively dur ing the Namurian B to end Westphalianin ter val (Schulmann and Gayer, 2000), whilst the dis tal fore -land ap pears to re cord a sin gle, ap par ently short de for ma tionphase at the Westphalian-Stephanian tran si tion.

Ac cord ing to the in ter pre ta tion pro posed in this pa per thestress field of the Pol ish Variscan fore land was dom i nated dur -ing the late Namurian and early Westphalian by north erly di -rected compressional stresses prop a gat ing from the SEVariscan Orogen. Ev i dence of the Variscan orogenic de vel op -ment south of the EEC, in the pres ent Black Sea area, was re -cently sum ma rized by Okay et al. (2006). They in cluded theMoesian Plat form and west wards con tig u ous Is tan bul Zoneinto the mar ginal part of the Old Red Con ti nent, de fin ing at thesame time the south-ad ja cent Strandja Mas sif and SakaryaZone as a sep a rate Mid Palaeozoic microplate of a Gondwananor i gin (Fig. 13). The Strandja–Sakarya arch accreted dur ing the Late Car bon if er ous across the Intra-Pontide su ture, prob a ble

con tin u a tion of the Rheic su ture. The age of orogenic de for ma -tion is rather poorly con strained in the Is tan bul Zone (Late Car -bon if er ous-Early Perm ian) whereas it is con fined to theNamurian in the Sakarya Zone (Okay et al., 2006). The in ter -preted north erly di rected com pres sion dur ing the Late Car bon -if er ous evo lu tion of the Pol ish Variscan fore land may be thuscon ceived as a far-field ef fect of the co eval col li sion of theStrandja–Sakarya arch with the south ern mar gin of Old RedCon ti nent (cf. Fig. 13). The lat ter may also ex plain the de vel op -ment of dextral strike-slip move ments along the TTZ with re -sult ing Late Car bon if er ous de vel op ment of the Lublin andPom er a nian bas ins in a pull-apart re gime.

Dur ing the fi nal orogenic phase, NE-di rected stresses re -lated to the dextrally NE-wards con verg ing Moravian-SilesianBelt pre vailed. It is pos tu lated that, com menc ing in the lateViséan, the Bo he mian Arc was moulded by the ar cu ateRheno-Hercynian–Moravian-Silesian embayment of the Pom -er a nian and Fore-Sudetic mar gin of the ORC, in volv ing the de -vel op ment of the dextral transpressional Moravian-SilesianBelt. It ap pears, how ever that it was not un til the lateWestphalian that collisional stresses pro jected from this beltbe came dom i nant in the SE Pol ish fore land.

Franke and ¯elaŸniewicz (2002) ar gued against oroclinalbend ing of the Bo he mian Arc. They pos tu lated a com plex sce -nario of late Viséan dextral strike-slip dis place ment of the or der of 1000 km along the Moldanubian Thrust (cor re spond ing tothe Moravian-Silesian Thrust Zone; Fig. 2) that was fol lowedby sim i lar dis place ments along the TTZ be fore the Stephanian.In view of the data pre sented here, this model can not be sup -


Fig. 13. Late Car bon if er ous palaeogeographic con text of the Variscan Orogen ofWest ern and Cen tral Eu rope and its hy po thet i cal east ern ex ten sion along the

north west ern Palaeo-Tethys mar gin (af ter Okay et al., 2006, mod i fied)

Out line of Po land is shown for a better com par i son with Fig ures 1 and 2; IS —Intra-Pontide Su ture; PDD — Pripyat–Dniepr–Donets–Donbas rift sys tem

ported, as there is no ev i dence for such enor mous shear ing nei -ther along the EEC mar gin nor per pen dic u lar to it. Fur ther -more, palaeomagnetic data do not sup port dis place ment ofsuch mag ni tudes (Nawrocki, 2000). More over, this model ap -par ently does not take into ac count the mag ni tude of Early Car -bon if er ous short en ing across the Moravian-Silesian Belt andfails to ex plain how and where the pos tu lated shear dis place -ments are ac com mo dated within the EEC.

CONCLUSIONS

1. The sed i men tary and struc tural re cord of the dif fer entcrustal blocks that con sti tute the Pol ish Variscan fore land re -flects their re sponse to chang ing stress pat terns dur ing the De -vo nian and Car bon if er ous. From De vo nian to Namurian Atimes the evo lu tion of ar eas lo cated SW of the TTZ, in clud ingthe Up per Silesian Coal Ba sin and the Ma³opolska and£ysogóry–Radom blocks, was gov erned by a stress field thatwas akin to that of the west wards con tig u ous Rheno-Hercynian Zone. By con trast, the evo lu tion of ar eas lo cated to the NE ofthe TTZ, in clud ing the Lublin Ba sin, was then gov erned by thestress field that pre vailed on the south ern parts of the EEC, con -trol ling i.a. the de vel op ment of the Pripyat–Dniepr–Donets riftsys tem (as no ticed al ready by Po¿aryski, 1986).

2. Af ter the Namurian A, the en tire south ern Pol ish fore -land started to re spond in a con sis tent way to the build-up ofsyn-orogenic compressional intraplate stresses, thus im ply ing a gen er ally uni form stress field.

3. From Namurian B to early Westphalian times the south -ern Pol ish fore land was mainly con trolled by N-di rectedcompressional stresses em a nat ing from the south east ernVariscan Orogen, de vel op ing along the Intra-Pontide su turesouth of Moesian Plat form and Is tan bul Zone. Dur ing that timethe USCB un der went a sec ond phase of flex ural foredeep de -

vel op ment in front of the NE-wards ad vanc ingMoravian-Silesian Belt.

4. Dur ing the late Westphalian and early Stephanian the en -tire area of the Pol ish Variscan fore land was sub jected tocompressional stresses chang ing from N- to NE-di rected com -pres sion. The lat ter em a nated from the Bo he mian orocline andin duced wide spread ba sin in ver sion. This par tic u larly strongcompressional event marked the end of the Variscan Orog enythat was fol lowed by a wrench-in duced Stephanian-earlyPerm ian tectono-mag matic cy cle (Ziegler, 1990).

5. The De vo nian to Car bon if er ous evo lu tion of theVariscan fore land of Po land re flects the re peated re ac ti va tionof pre-ex ist ing crustal dis con ti nu ities, such as the TTZ, the bound aries be tween the Up per Silesian, Ma³opolska and£ysogóry–Radom blocks and the fault sys tems within the mar -ginal parts of the EEC in the Lublin Ba sin. In gen eral,thick-skinned tec ton ics con trolled by the in her ited struc turalgrain pre vailed dur ing the Westphalian-Stephanian in ver sionof the Pol ish Variscan fore land. Thin-skinned struc tural de -coup ling in volv ing the de vel op ment of mi nor thrusts and re -verse fault ing was of lo cal sig nif i cance.

6. The De vo nian-Car bon if er ous evo lu tion of Pomerania re -sem bles in many re spects that of the Rügen area (cf. McCann,1999a, b) and pre sum ably owes its dis tinct struc -tural-depositional de vel op ment to a dis tal po si tion with re spectto the evolv ing orogen. Late stage de for ma tion of this area wasmainly con trolled by transtensional and transpressional stresses trans mit ted through the TTZ.

Ac knowl edg ments. I wish to ex tend my thanks to P. A.Ziegler for his thor ough re view of the ear lier ver sion of thispa per and for many valu able com ments. I am grate ful to R.Dadlez, P. Krzywiec and M. Jarosiñski for dis cus sions onvar i ous as pects of tec tonic de vel op ment of the Pol ishVariscan fore land.

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