The Variscan fore land in Po land re vis ited: new data ...

Geo log i cal Quar terly, 2020, 64 (2): 377–401 DOI: http://dx.doi.org/10.7306/gq.1511

The Variscan fore land in Po land re vis ited: new data and new con cepts

Marek NARKIEWICZ1, *

1 Pol ish Geo log i cal In sti tute – Na tional Re search In sti tute, Rakowiecka 4, 00-975 Warszawa, Po land

Narkiewicz, M., 2020. The Variscan fore land in Po land re vis ited: new data and new con cepts. Geo log i cal Quar terly, 64 (2):377–401, doi: 10.7306/gq.1511

As so ci ate Ed i tor: Leszek Marks

An ear lier con cept of the Variscan fore land in Po land (Narkiewicz, 2007) is re con sid ered in the light of new strati graphic, tec -tonic and geo phys i cal ev i dence, pro vid ing new data on De vo nian sed i men ta tion, Car bon if er ous magmatism and the deepcrustal struc ture of SE Po land. Re gional com par i sons with the tec tonic evo lu tion of Cen tral Eu rope and the Black Sea re gionshow that the sub si dence pat tern in the fore land was con trolled by al ter nat ing phases of ac cel er ated con ver gence and tec -tonic stand still along the south ern mar gin of Euramerica. In par tic u lar, the Bretonian (De vo nian/Car bon if er ous) com -pressional de for ma tion re sulted from in ten si fied orogenic con ver gence in the West-Cen tral European Variscides lead ing toclo sure of the Saxo-Thuringian Ba sin and East-Sudetic back-arc ba sin. An other turn ing point in the re gionaltectonosedimentary de vel op ment around the Mississippian–Pennsylvanian bound ary was prob a bly re lated to the ter mi na -tion of terrane col li sion in the Black Sea re gion. Late Penn syl va nian ba sin in ver sion was as so ci ated with a roughly N–S tec -tonic short en ing. This was partly due to dis place ment along pre-ex ist ing base ment dis con ti nu ities com pris ing re ac ti vatedCal edo nian su tures that also pre-de ter mined the Devonian–Carboniferous ba sin bound aries. Con se quently, deeply-rootedtec tonic zones, in clud ing the Kraków-Lubliniec and Holy Cross faults and the Teisseyre-Tornquist Zone, fo cussed max i mumcompressional and transpressional de for ma tion and as so ci ated up lift. Such a con cept of ter mi nal Variscan tectonism,termed here the “de coup led model”, is dis cussed with ref er ence to the re cently pro posed “cou pled model”. The lat ter as -sumes a wide ex tent of the Variscan Orogen, reach ing as far as the mar ginal Radom–Kraœnik Fold-and-Thrust Belt linkedwith the Bo he mian Mas sif through a ma jor basal de tach ment. It is con cluded that the “de coup led model” is more con sis tentwith the doc u mented seis mic and struc tural ev i dence as well as with the pres ent knowl edge of the heterogeneous pre-De vo -nian base ment in south ern Po land.

Key words: Variscides, fore land bas ins, lithospheric mem ory, far-field stress, ba sin in ver sion.

INTRODUCTION

The Variscan fore land in Po land com prises De vo nian andCar bon if er ous bas ins that de vel oped in front of the Variscan ex -ter nal belt at trib uted to the Rhenohercynian Zone (Narkiewicz,2007). Ero sional rem nants of the ba sin-fill form out crops andsubcrops ex tend ing be tween the fron tal part of the orogen in the south and west, and el e vated ar eas of the East Eu ro pean Plat -form in the north-east. They com pose a 100–150 km wide beltin the north ern Pomerania area, nar row ing to <50 km in cen tralPo land and again wid en ing to ~400 km in the SE part of thecoun try (Fig. 1). The Variscan Front is well de fined in Silesiawhere it cor re sponds to the thick-skinned Orlova andMicha³kowice thrusts at the east ern mar gin of theMoravian–Silesian Fold-and-Thrust Belt (Kotas, 1994). Far thernorth and west it is con cealed be neath thick Perm ian–Me so zoic

strata and its ar chi tec ture is hy po thet i cal. Based on ex trap o la -tion from south ern Po land and on re gional anal o gies it is in ter -preted as a sin gle mas ter thrust sim i lar to that in the ArdennesMas sif (Oncken et al., 1999) or to a se ries of thrusts known from the north ern part of the Rhenish Mas sif (Behr et al., 1984). Itscourse is here as sumed af ter the ear lier study (Narkiewicz,2007) based partly on Jubitz et al. (1986) and Po¿aryski andKarnkowski (1992).

In the ear lier pa per (Narkiewicz, 2007) the data then avail -able on the De vo nian and Car bon if er ous of the Variscan fore -land were sum ma rized and dis cussed. Its tectono-sed i men taryde vel op ment was in ter preted within a broader tec tonic andpalaeogeographic frame work of the post-Cal edo nian south ernpas sive mar gin of Euramerica evolv ing into an ac tive mar ginand fi nally trans formed into a con ti nen tal col li sion zone in thelate De vo nian and Car bon if er ous. Since that pub li ca tion, im por -tant new data and in ter pre ta tions have ap peared, which ne ces -si tates sup ple ment ing and re con sid er ing the ear lier re sults.

In par tic u lar, new syn thetic pa pers have been pub lished onthe depositional de vel op ment of the £ysogóry Ba sin(Narkiewicz, 2011a), the Lublin Ba sin (Waksmundzka, 2010;Narkiewicz, 2011b, Narkiewicz et al., 2011a) and on the gen -eral ge ol ogy of SE Po land (Bu³a et al., 2008). New data on the

* E-mail: [email protected]

Received: September 16, 2019; accepted: November 25, 2019; firstpublished online: February 18, 2020

https://gq.pgi.gov.pl/article/view/7453





378 Marek Narkiewicz

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The Variscan fore land in Po land re vis ited: new data and new con cepts 379

age of ig ne ous pro cesses were ob tained for the cratonic base -ment in NE Po land (sum ma rized in Krzemiñska et al., 2017),the Lublin re gion (Pañczyk and Nawrocki, 2015), the HolyCross Mts. (Nawrocki et al., 2013; Krzemiñska and Krzemiñski,2019) and the Up per Silesian Ba sin (Jirásek et al., 2013).

Sev eral re cent stud ies, mostly based on new re flec tion seis -mic data, are de voted to the deep struc ture and tec tonic de vel op -ment of the Lublin Ba sin and ad join ing re gional units (Narkiewiczet al., 2015; Tomaszczyk, 2016; Krzywiec et al., 2017a, b;Tomaszczyk and Jarosiñski, 2017; Kufrasa et al., 2017, 2019).These stud ies de serve par tic u lar at ten tion here as they partlypro pose new or in voke pre vi ous con tro ver sial tec tonic ideas hav -ing broader im pli ca tions for the Variscan Fore land in gen eral(Krzywiec et al., 2017a; Aleksandrowski and Mazur, 2017).These is sues are dis cussed be low within the frame work of newre gional con cepts re gard ing the base ment struc ture of Po landwith par tic u lar em pha sis on the na ture and course of theTeisseyre-Tornquist Zone (TTZ) at the mar gin of the East Eu ro -pean Plat form (Mazur et al., 2015; Narkiewicz et al., 2015;Narkiewicz and Petecki, 2016, 2017, 2019).

TECTONIC AND PALAEOGEOGRAPHICBACKGROUND

Soon af ter the amal gam ation of Baltica–Avalonia andLaurentia into the Euramerica con ti nent in the Late Si lu rian, thenewly formed Cal edo nian Orogen of north ern Eu rope un der -went grav i ta tional col lapse. The dis in te gra tion was ad di tion allystim u lated by back-arc ex ten sion con nected with thesubduction of the Rheic Ocean litho sphere be neath theEuramerican Plate (Ziegler, 1990; Franke, 2000). This pro cesswas prob a bly re spon si ble for the de vel op ment in the Emsian ofa nar row Rhenohercynian Ocean ex tend ing from SW Eng landin the west to Moravia in the east. On the other hand, nar row ingof the Rheic Ocean led to the con ti nen tal col li sion of Gond wanawith Euramerica pre ceded by a north ward drift and De vo nian toEarly Car bon if er ous amal gam ation of smaller Gond wana-de -rived units of the Armori can Terrane As sem blage (Franke et al., 2017). The con ver gence of both con ti nents con tin ued dur ingthe Early Car bon if er ous, and since that time the newly es tab -lished Pangea Supercontinent dis played a con sis tent drift his -tory. The fi nal phase of the oblique dextral col li sion oc curred inthe Late Car bon if er ous, re sult ing in the for ma tion of aHimalaya-type Variscan Orogen of West ern and Cen tral Eu -rope stretch ing from the Ibe rian Mas sif in the west to the Bo he -mian Mas sif in the east. The orogen com prises in its in ner mostpart the Moldanubian Zone (in clud ing the Vosges,Schwarzwald and south ern part of the Bo he mian Mas sif), theTepla–Barrandian Zone in the cen tral part of the Bo he mianMas sif, the Saxothuringian Zone lim ited by the Rheic Su ture tothe north, and the ex ter nal fold-and-thrust belt of theRhenohercynian Zone with the clas sic out crops of theArdennes–Rhenish Mas sif and Harz (Fig. 1).

The Variscan Orogen is con cealed to wards the south-eastbe neath the Al pine–Carpathian belt. Nev er the less, its far thereast ward ex tent is sug gested by prov e nance anal y sis of ex oticclasts in the Carpathian flysch as well as by dat ing of iso latedbase ment out crops in the In ner Carpathians (e.g., Znosko,1992; Gawêda, 2007). The SE part of the orogenic belt can bere con structed in the Black Sea re gion, be tween the Bal kanMoun tains and Rhodopes in the west and the Cau ca sus in theeast (Fig. 2). There, the Moesian Plat form, Is tan bul Zone andScythian Plat form, la belled as the MOIS Block, were in ter preted by Okay and Topuz (2017) as parts of the south ern Euramerica

mar gin com pris ing an ex ter nal belt of the Variscan Orogen andits fore land bas ins. To the south these re gions are jux ta posedby a zone of crys tal line rocks un con form ably over lain by Up perCar bon if er ous to Lower Perm ian molasse de pos its. The belt,termed BASSAC, ex tend ing from the Bal kan Mts. and theRhodopes, Strandja and Sakarya ter ranes to the Cau ca sus,forms the re gional equiv a lent of the Armori can ter ranes inW-Cen tral Eu rope. Tec tonic pro cesses act ing in these beltslikely af fected the in te rior of the EEP and can be de duced fromthe de vel op ment of a large rift sys tem com pris ing the PripyatGraben in the west through the Dnie per–Donets Rift to thePeri-Cas pian De pres sion in the east (PDD sys tem; Stephen -son et al., 2006).

In the De vo nian, the south ern Euramerica mar gin, in clud ing the Pol ish Variscan fore land bas ins, was lo cated in the south -ern hemi sphere in the mon soonal cli mate of the trop i cal zone,grad u ally mi grat ing to wards the equa tor dur ing the Car bon if er -ous (Cocks and Torsvik, 2006; De Vleeschouwer et al., 2012;Golonka and Gawêda, 2012). A global green house cli mate pre -vail ing dur ing most of the De vo nian was char ac ter ized by smalllat i tu di nal gra di ents and the ab sence of larger con ti nen talice-sheets. This fa voured the de vel op ment of ex ten sive car -bon ate plat forms and reefs in the Mid dle De vo nian to Frasnian.Sed i men ta tion, par tic u larly in the tec toni cally sta ble cratonic ar -eas, was largely con trolled by eustatic changes and bi oticevents, in clud ing one of the larg est Phanerozoic mass-ex tinc -tions re lated to the Kellwasser event near theFrasnian–Famennian bound ary (Belka and Narkiewicz, 2008).The Famennian was a pe riod of grad ual tran si tion from green -house to ice house con di tions punc tu ated by sev eral eustaticpulses and as so ci ated black-shale ho ri zons, in ter preted interms of gla cial-inter gla cial cy cles (Sandberg et al., 2002;Brezinski et al., 2008). The most prom i nent of these ep i sodes,the Hangenberg Event near the De vo nian–Car bon if er ousbound ary, was as so ci ated with one of the most se vere bi oticper tur ba tions in the Phanerozoic (e.g., Kai ser et al., 2016).

En su ing cli ma tic cool ing dur ing the Early Car bon if er ous ledto an im mense Late Pa leo zoic con ti nen tal gla ci ation whichstarted by the end of the Mis sis sip pian and lasted un til thePerm ian. The as so ci ated glacioeustatic fluc tu a tions were re -spon si ble for the cy clic de po si tion of coal-bear ing de pos its sochar ac ter is tic of the Variscan fore land of Eu rope dur ing most ofthe Penn syl va nian.

PRE-VARISCAN PATTERN OF BASEMENT UNITS

Pre vi ous re sults have shown that base ment struc ture wasone of the main fac tors de ter min ing the bound aries of par tic u lar De vo nian–Car bon if er ous fore land bas ins and con trol ling theirsub si dence de vel op ment (Narkiewicz, 2007). Re cently, thepre-Variscan pat tern of the base ment blocks has been re con -sid ered by Narkiewicz and Petecki (2017). They de fined sev -eral units, briefly de scribed be low, which dif fer in geo phys i calchar ac ter is tics and in the de vel op ment of their Ediacaran to Pa -leo zoic sed i men tary cover.

The in ner part of the Variscan Orogen in Po land has beenas cribed to the Sudetic Do main com pris ing the Sudetesproper, the Fore-Sudetic Block and the base ment of theWolsztyn–Leszno High (Fig. 3). The NE bor der of the lat ter unitis as so ci ated with a lin ear zone of mag netic anom a lies trace -able to the Mid-Ger man Crys tal line High in the W and SW andthus to the Rheic Su ture at the NW mar gin of theSaxothuringian Zone (Franke, 2000; Kro ner et al., 2008). Theeast ern bound ary of the Sudetic Do main runs along the








Moravian–Silesian Su ture be tween the Cen tral Sudetic ter -ranes and the Brunovistulian base ment of the Up per SilesianBlock (see be low). The su ture is a com plex thrust zone in clinedto the WNW, com pris ing the Staré Mìsto Belt and its north erncon tin u a tion in the Fore-Sudetic Block (Jastrzêbski, 2012).

The Up per Silesian Block forms the north ern part of thetri an gle-shaped Brunovistulicum unit neigh bour ing the east ernmar gin of the Bo he mian Mas sif (Dudek, 1980; Bu³a and ¯aba,2005). The base ment of the block is com posed pre dom i nantlyof Neoproterozoic paragneisses and Paleoproterozoic am phi -bo lites (Bu³a and ¯aba, 2005, 2008) accreted dur ing theNeoproterozoic Cadomian Orog eny (Fin ger et al., 2000).

Its west ern part is onlapped by the Moravian–SilesianFold-and-Thrust Belt form ing part of the Variscan ex ter nal(Rhenohercynian) zone with the fron tal thick-skinned OrlovaThrust in the east (Fig. 3). In the east ern part of the block theweakly meta mor phosed Ediacaran flysch is over lain by rel a -tively undeformed Pa leo zoic strata in clud ing the thick De vo nian to Car bon if er ous suc ces sion of the Up per Silesian Ba sin (Bu³aand ̄ aba, 2005; Bu³a et al., 2015). The NE bound ary of the Up -per Silesian Block cor re sponds to the long-lived Kraków– Lub -liniec Fault, in ter preted as a pre-De vo nian accretionary su ture(Bu³a et al., 1997; ¯aba, 1999; Belka et al., 2002).

Fig. 2. Variscan Orogen and its fore land in Cen tral Eu rope and in the Black Sea re gion (based on Okay and Topuz, 2017: fig. 1, mod i fied)

A – Ardennes, IZ – Is tan bul Zone, RM – Rhenish Mas sif, St – Strandja Mas sif, SZ – Sakarya Zone, TTZ –Teisseyre-Tornquist Zone



The Ma³opolska Block ex tends be tween the Up perSilesian and £ysogóry blocks (Fig. 3). Its deep struc ture is in ter -preted as a stack of NE-verg ing thick-skinned thrusts ini tiallyform ing a part of the Neoproterozoic (Cadomian) Orogen at theGond wana mar gin and later de tached as a terrane, anal o gousto Brunovistulicum (Narkiewicz et al., 2011b, 2015). Thepre-De vo nian sed i men tary cover has been in tensely de formed

and even, in the case of the Ediacaran flysch, partly meta mor -phosed (Dadlez et al., 1994; Bu³a et al., 2008). The fi nal fold ingwas as so ci ated with late Cal edo nian terrane ac cre tion aroundthe Si lu rian–De vo nian bound ary (Narkiewicz et al., 2015). TheNE bound ary cor re sponds to the Holy Cross Fault whose SEex ten sion can be traced us ing bore hole and geo phys i cal data(Bu³a et al., 2008; Narkiewicz et al., 2015).

Fig. 3. Re gional units of the Variscan fore land within the sub-Perm ian–Me so zoic map of Po land (based on Po¿aryski and Dembowski, 1983)

BAH – Bielsko–Andrychów High; ESB – East Sudetic Belt; HCMts – Holy Cross Moun tains; ISF – Intra-Sudetic Fault; KLF -Kraków–Lubliniec Fault; SMCE – Stê¿yca–Me³giew Cen tral El e va tion; MSS – Moravian–Silesian Su ture. Tectonostratigraphic ter ranes inthe Sudetes (af ter Aleksandrowski and Mazur, 2002): GSKT – Góry Sowie–K³odzko Terrane; KT – Kaczawa Terrane; LIT – Lusatia–IzeraTerrane; MT – Moldanubian Terrane; SEKT – South-East Karkonosze Terrane; TBT – Teplá–Barrandian Terrane


The £ysogóry Block1 oc cu pies a wedge-shaped area be -tween the Holy Cross Fault and the TTZ (Fig. 3). Its base mentis un known but the re sults of deep seis mic in ves ti ga tions pointto the crust be ing of East Eu ro pean Craton (EEC) type(Narkiewicz et al., 2011b, 2015). At the same time, how ever,the pres ence of a dis tinct Lower Pa leo zoic suc ces sion con sid -er ably dif fer ing from that of the EEC cover sup ports the con cept of a prox i mal allochthonous terrane trans lated along the TTZ.The NW ex ten sion of the £ysogóry Block be neath theWielkopolska Externides belt com poses a hy po thet i calMid-Pol ish Do main dis play ing an at ten u ated EEC-type crust.The De vo nian strata and basal Car bon if er ous rocks are therein ac ces si ble, how ever, be cause of the thick Perm ian– Meso -zoic cover.

The Pom er a nian Block ex tends be tween the TTZ in theNE and the hy po thet i cal crustal dis con ti nu ity (Pom er a nian Su -ture) run ning north-east of the Variscan Front in the south(Narkiewicz and Petecki, 2017). Its base ment is un known butdeep seis mic re frac tion data show its af fin ity to the EEC crust.The De vo nian and Car bon if er ous strata (Matyja, 2006) formwedge-shaped sub-Perm ian–Me so zoic subcrops un con form -ably over ly ing folded Lower Pa leo zoic rocks ex tend ing north- east wards be yond the TTZ as far as the Koszalin–Choj -nice–Tuchola Fault Zone (Fig. 3).

The East Eu ro pean Plat form (EEP) has a cratonic base -ment formed mostly of Paleoproterozoic Fennoscandian crust.It is com posed of SW–NE trending belts accreted par al lel to thesu ture be tween Fennoscandia and Sarmatia (Fig. 1;Krzemiñska et al., 2017). The SW mar gin of the EEP formed asa re sult of Ediacaran rift ing in the fi nal stages of breakup of thesupercontinent Rodinia, which led to the birth of the Baltica con -ti nent cor re spond ing roughly to the pres ent EEP. Thesub-Perm ian–Ce no zoic el e va tions of the EEP base ment in -clude the Scan di na vian Shield, the Mazury-Belarus Antecliseand the Ukrai nian Shield, sep a rated by de pres sions with a rel a -tively undeformed Ediacaran-Lower Pa leo zoic cover (Fig. 3).The De vo nian-Car bon if er ous suc ces sion rests upon Up per Si -lu rian strata ei ther con form ably or with a slight intra-Lochkovianun con formity. An ex cep tion is the nar row zone lo cated be tween the TTZ and the Koszalin–Chojnice–Tuchola Fault Zone men -tioned above (Fig. 3). The north ern part of the Pol ish Bal tic off -shore area com prises De vo nian de pos its of the mar ginal part of the Bal tic Ba sin ex tend ing far ther north-eastwards to wards Lith -u a nia, Latvija and Es to nia (Belka and Narkiewicz, 2008). Its de -vel op ment was mostly con trolled by eustatic fluc tu a tions in thesta ble EEC in te rior, and was barely af fected by Variscan fore -land tectonism.

It is here as sumed that the con tin u ous Baltica crust isbounded to the SW by the Teisseyre-Tornquist Zone (TTZ) –a tec tonic lin ea ment marked by a first-or der mag netic gra di entand a con trast in crustal struc ture vis i ble in seis mic re frac tionand magnetotelluric data, and also doc u mented by a few of thedeep est re flec tion seis mic lines in SE Po land (Narkiewicz et al.,2015; Narkiewicz and Petecki, 2019). The TTZ is in ter preted as the transcurrent zone along which the Pom er a nian and£ysogóry prox i mal ter ranes were de tached from the Tornquistmar gin of Baltica, trans lated dextrally and re-accreted dur ingthe Late Si lu rian–ear li est De vo nian (Dadlez et al., 2005;Narkiewicz et al., 2015). An al ter na tive con cept in fers con ti nu ity of the Paleoproterozoic crust across the TTZ which is in ter -preted as a Meso-Neoproterozoic intraplate su ture (Mazur etal., 2015). Ac cord ing to the pres ent au thor, this hy poth e sis,

based mainly, if not ex clu sively, on the re sults of grav ity mod el -ing, lacks sup port in di rect geo log i cal and geo phys i cal ev i dence (see dis cus sion by Narkiewicz and Petecki, 2016, 2019;Narkiewicz, 2019).

STAGES OF DEVELOPMENT OF THE FORELAND BASINS

The pat tern de scribed above of the base ment units is to alarge ex tent mir rored in the de vel op ment of dis tinct De vo -nian–Car bon if er ous bas ins with con trast ing depositional ar chi -tec tures and sub si dence his to ries. The ba sin bound aries inmany cases co in cide with the tec tonic zones which de limit theun der ly ing crustal blocks. They were re ac ti vated in extensionaland compressional re gimes, partly with a strike-slip com po nent, both dur ing the sub si dence phase and dur ing the later in ver -sion. The lat eral trans la tions were, how ever, very small in scaleby com par i son with the transcurrent Cal edo nian tec ton ics andthere fore the pres ently ob served fore land con fig u ra tion mim icsthe orig i nal palaeogeographic pat tern, only with some mod i fi ca -tion im posed by the late Variscan tectonism (Narkiewicz, 2007;Narkiewicz et al., 2011a; cf. also Szaniawski, 2008 with ref er -ence to the Ma³opolska Block).

In spite of re gional, base ment-con trolled dif fer ences therehad been a com mon pat tern dur ing the De vo nian–Car bon if er -ous de vel op ment of par tic u lar bas ins seen both in theirdepositional suc ces sions (Fig. 4) and in the sub si dence his to -ries (Fig. 5). Thus, sev eral suc ces sive stages can be dis tin -guished in the en tire De vo nian–Car bon if er ous ba sin de vel op -ment point ing to ex ter nal re gional con trols on their evo lu tion.These stages will be briefly sum ma rized be low with par tic u larem pha sis on new data and in ter pre ta tions that have ap pearedsince the orig i nal de vel op men tal model was pub lished by theau thor (Narkiewicz, 2007). For more strati graphic and tec tonicde tails the reader is re ferred to the ear lier pa per and to the sum -ma ries by Belka and Narkiewicz (2008), McCann et al. (2008)and Belka et al. (2010).

DEVONIAN BASINS

Over most of the Variscan fore land area var i ous Pro tero zoic and Pa leo zoic rocks are un con form ably over lain by con ti nen taland mar ginal ma rine Pragian or Emsian clastic rocks up to~200 m thick (Fig. 4). Only in the Lublin Sub-ba sin and in the£ysogóry Ba sin did the open ma rine Late Si lu rianshallowing-up wards de po si tion of shaly-car bon ate strata con -tinue up to the Lochkovian, cul mi nat ing in Mid-Lochkovian shal -low-wa ter open- to mar ginal ma rine clastic de po si tion (Fig. 6).These strata are onlapped, prob a bly with a small un con formity,by con ti nen tal al lu vial red beds, as cribed mostly to the Emsianand with caliche lev els, point ing to a gen er ally warm dry cli mate(Mi³aczewski, 1981; Narkiewicz, 2011b). Stra tal thick ness isvari able, from 200 to 1500 m, with large lat eral con trasts due tover ti cal block move ments cre at ing a horst and graben to pog ra -phy (Narkiewicz et al., 2011a).

Around the Early/Mid dle De vo nian bound ary, shal low-ma -rine car bon ate sed i men ta tion de vel oped and pre vailed acrossthe en tire depositional realm, ex cept for nar row nearshoreclastic belts in the Lublin and Pomerania area. Only the£ysogóry Ba sin was char ac ter ized by an ex cep tion ally high pro -


1 In the pre vi ous pa per (Narkiewicz, 2007) the unit was named as the £ysogóry–Radom Block; here the ab bre vi ated ver sion is usedfol low ing Narkiewicz et al. (2011b) and Narkiewicz and Petecki (2017).







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por tion of marly and silty deeper-shelf fa cies. These de pos its,ex ceed ing 1 km in to tal thick ness, re placed car bon ate fa ciesun der con di tions of ac cel er ated sub si dence in the elon gateddepocentre framed by the Holy Cross Fault and the TTZ.

The Late De vo nian was char ac ter ized by the de vel op mentof nearshore, at tached car bon ate plat forms and ramps, as wellas iso lated or ganic build ups and large reef com plexes such asthe Dyminy Reef in the west ern Holy Cross Mts. (Narkiewicz,1988). Deeper parts of the shelf were dom i nated by dark-col -oured marly car bon ates with a pe lagic fauna. Their thick ness isgen er ally un der one ki lo me ter, al though in the Lublin Sub-ba sin it may reach 2.5 km of mostly Famennian de pos its in thedepocentre lo cated be tween the syndepositionally ac tiveKazimierz–Ursynów Fault and the Kock Fault Zone (Narkiewicz et al., 2011a).

Strati graphic anal y ses have shown a con sid er able in flu -ence of eustatic fluc tu a tions on the Mid dle to Up per De vo niandepositional ar chi tec ture (Racki and Narkiewicz, 2000; Belkaand Narkiewicz, 2008; Narkiewicz et al., 2011a). Globaltransgressive events such as the late Emsian sea level rise, theTaghanic Event in the mid-Givetian and the Frasnian trans gres -sions were su per im posed on a de creas ing tec tonic sub si dencerate typ i cal of the ther mal con trac tion of the litho sphere fol low -ing a ma jor (in this case, Emsian) rift ing event.

On the other hand, a De vo nian extensional or transten -sional re gime is in di cated by depositional re cords ofsynsedimentary block tec ton ics and struc tural palaeostressdata along the Kraków–Lubliniec Fault zone (¯aba, 1999) andin the Holy Cross Mts. (sum ma rized by Racki and Narkiewicz,2000; Lamarche et al., 2003). The Holy Cross Fault acted as a


Fig. 5. Stages of the Variscan fore land de vel op ment in Po land com pared with the tec tonic sub si denceevo lu tion dis played as syn thetic curves rep re sen ta tive of par tic u lar bas ins (based mainly on McCann

et al., 1997; Narkiewicz et al., 1998; Narkiewicz, 2005)


ma jor synsedimentary dis con ti nu ity sep a rat ing the more sta bleMa³opolska Ba sin from the faster sub sid ing £ysogóry Ba sin(Narkiewicz, 2011a; Narkiewicz et al., 2015). Also, em place -ment of some mi nor, poorly dated lam pro phyre dykes(Migaszewski, 2002) may have re sulted from the re gional De -vo nian to Early Car bon if er ous ex ten sion.

Tec tonic sub si dence in the cen tral part of the Lublin Sub-ba -sin ac cel er ated al ready in the mid-Frasnian lead ing to an in -

creased sed i men ta tion rate of re stricted car bon ate-sul phate de -pos its (Narkiewicz and Narkiewicz, 2008). This lo cal depocentrebe came even more pro nounced in the early Famennian with theon set of rapid ac cu mu la tion of dark-col oured shaly-car bon atesed i ments of a deeper shelf (Fig. 6). As so ci ated com monsynsedimentary boudinage and sub ma rine slumps were prob a -bly seis mi cally in duced by on go ing tec tonic ac tiv ity of theKazimierz–Ursynów and Kock Fault zones (Narkiewicz, 2011b).

Fig. 6. De vo nian palaeo ge ogra phy of the Variscan fore land in Po land (mod i fied fig. 6 in Narkiewicz, 2007, based on var i ous sources cited in the text)

BF – Bia³opole Fault, SF – Serebryszcze Fault


In the Pom er a nian Ba sin an extensional re gime also pre vailed,with al ter nat ing pulses of dextral and sinistral transtension andtranspression (¯aba and Poprawa, 2006).

LATEST DEVONIAN AND EARLIEST TOURNAISIAN (BRETONIAN) TECTONISM

Con tin u ous sed i men ta tion across the De vo nian–Car bon if -er ous bound ary has been doc u mented so far only lo cally in theHoly Cross Mts. (Malec, 2014) and in the Pom er a nian Ba sin(Matyja et al., 2015). Strati graphic con den sa tion and gapsspan ning the up per most De vo nian and lower part of theTournaisian have been noted in the Kielce area of the HolyCross Mts. (Szulczewski, 1995) and in the Up per Silesian andPom er a nian bas ins (Be³ka, 1985; Matyja and Stempieñ-Sa³ek,1994). A sed i men tary dis con ti nu ity at the base of the Mis sis sip -pian, com monly la belled the Bretonian un con formity, has beenpos tu lated also in the south ern part of the Ma³opolska Ba sin,e.g., by Jawor and Baran (2004) and Moryc (2006). And, ver ti -cal block-move ments near the D–C bound ary in theKraków–Lubliniec Fault zone have been dis cussed by ¯aba(1999).

The most pro nounced late Famennian synsedimentary tec -ton ics have been long known, how ever, from the Lublin Sub-ba -sin (Narkiewicz, 2007). Ver ti cal block move ments and as so ci -ated ero sion lo cally led to re moval of up to 1500 m of De vo nianand Lower Pa leo zoic strata and to a dis tinct Bretonian un con -formity at the base of the Up per Visean. Re cently, seis mic sec -tions doc u mented a pat tern of thick-skinned ver ti cal and steepre verse faults, with a dextral strike-slip com po nent. The dis con -ti nu ities strike NW–SE to SW–NE across the Hrubieszów El e -va tion flank ing the depocentre of the Lublin Sub-ba sin from theNE (Krzywiec et al., 2017a). The faults partly show a pos i tiveflower-struc ture in di cat ing a transpressional re gime (Krzywiec,2007, fig. 4); the same ap plies to the SE ter mi na tion of the Kock Fault Zone (Tomaszczyk and Jarosiñski, 2017). This ma jor dis -con ti nu ity prob a bly orig i nated dur ing Ediacaran rift ing, was re -ac ti vated as a nor mal fault in the Si lu rian, and as a steep re -verse fault in the Late De vo nian–ear li est Car bon if er ous(Tomaszczyk and Jarosiñski, 2017). The re sult ing up lift andero sion of the Hrubieszów El e va tion led to south-west wardsprogradation of mar ginal ma rine clastics, car bon ates andevaporites grad ing into con ti nen tal red beds (Fig. 4; Narkiewicz, 2011b).

POLCRUST-01 seis mic re flec tion data re vealed that overmost of the SE seg ment of the Lublin Ba sin (ex cept for its SWpart) Bretonian de for ma tion was more pro nounced than the late Car bon if er ous in ver sion (see be low). Along the NE flank of theba sin the Serebryszcze2 and Bia³opole faults (Fig. 6) down -throw the base ment top to the SW by ~700 and 400 m, re spec -tively (Narkiewicz et al., 2015). These ap prox i mately ver ti caldis con ti nu ities are as so ci ated with some sec ond ary faults com -pos ing flower-like struc tures sug ges tive of strike-slip de for ma -tion. The nearly hor i zon tal Car bon if er ous base erosionally trun -cates both faults and the en cas ing Frasnian to Si lu rian strata,with only a small in di ca tion of re ac ti va tion of the SerebryszczeFault in the Late Car bon if er ous. Such a pat tern tes ti fies tostrong ver ti cal block move ments pre dat ing the late Car bon if er -ous de for ma tion. A sim i lar ity be tween both faults and the SEter mi na tion of the Kock Fault Zone sug gests that these struc -tures formed a part of the same transpressional zone dur ing the Bretonian tectonism.

TOURNAISIAN TO MIDDLE VISEAN SHELF SEDIMENTATION AND MAGMATISM

Fol low ing the Bretonian block tec ton ics, the shelf sea re -treated en tirely from the Lublin and P³ock sub-bas ins, and partly from the Pom er a nian Ba sin (Fig. 7). The re main ing in un datedarea of the Tournaisian to mid-Visean shelf was dom i nated byterrigenous de pos its up to 1 km thick, com monly with a con sid -er able volcanoclastic ad mix ture. Some fault-con trolled el e va -tions be came sites of intrashelf and nearshore car bon ate plat -forms. In the Pom er a nian Ba sin al lu vial to mar ginal ma rineclastic de pos its grade into dis tal off shore fine-grainedterrigenous fa cies. In the Ma³opolska Ba sin and in the north ernUSB a com mon lithofacies com prised dark-col oured si li ceousshales and siltstones.

Car bon if er ous strata are known from a few bore hole sec -tions in the £ysogóry Ba sin. They com prise a sev eral hun dredmetres-thick suc ces sion of arkosic sand stones in ter ca latedwith siltstones and dark shales with palynomorphs of lateTournaisian to ?early Visean age. Abun dant ad mix ture oftrachytic and rhyolitic volcanoclastic de pos its points to vol ca niccen tres de vel op ing un der con ti nen tal crust ex ten sion.Sedimentological anal y ses doc u ment grav ity flows on a sub ma -rine slope fed by a nar row shal low shelf to the NE (Jaworowski,2002). This nearshore clastic belt prob a bly ex tended along theTTZ thus rim ming the eroded area of the for mer De vo nianLublin Sub-ba sin. In Pomerania the ba sin mar gin par al leled theKoszalin–Chojnice–Tuchola Fault Zone in prox im ity to a re gionof late Tournaisian acidic vol ca nism.

Dur ing the Tournaisian to mid-Visean the tec tonic sub si -dence gen er ally de cel er ated, lo cally ap proach ing zero (Fig. 5).The re gional ex ten sion which re turned af ter the Bretoniantectonism fa voured mag matic pro cesses which be came par tic -u larly ac tive near the TTZ around the Tournaisian/Viseanbound ary. Fur ther more, there are some in di ca tions of mi normafic magmatism in the HC Mts. in the form of small lam pro -phyre dykes emplaced prob a bly in the late Tournaisian(Migaszewski, 2002).

The mag matic ac tiv ity was par tic u larly pro nounced in theEEP area in clud ing the Lublin re gion where al ka line bas alts upto 230 m thick de vel oped be tween late Tournaisian and mid-Visean times (Pañczyk and Nawrocki, 2015). Al ka line diabaseand syenite in truded near the P³ock re gion, while sev eral al ka -line plutons are known from NE Po land, in clud ing the gab -bro-syenite Pisz, syenite E³k, and syenite-monzograniteGrajewo in tru sions (Fig. 7). The age of the in tru sive pro cesseshas been es ti mated at 354–338 Ma based on U-Pb iso topes inzir cons (sum ma rized by Krzemiñska et al., 2017). The max i -mum ac tiv ity can be thus cor re lated with the peak of thepyroclastic in put in the up per Tournaisian (Ivorian) of var i ousbas ins (Fig. 4). It is es ti mated that the par ent magma was de -rived from an en riched man tle source that was ac ti vated bylithospheric ex ten sion which ap par ently af fected large parts ofthe south ern Euramerica mar gin.

LATE VISEAN–EARLY SERPUKHOVIAN – PEAK OF THE CARBONIFEROUS TRANSGRESSION

A ma rine clastic shelf per sisted un til the late Visean andearly Serpukhovian in the Pom er a nian and Ma³opolska bas ins,and prob a bly also in the £ysogóry Ba sin (Fig. 8). From the lat terarea the depositional re cord is miss ing, how ever, and only mi -


2 The struc ture was named the Dubienka Fault by Narkiewicz et al. (2015) but most prob a bly it cor re sponds to the Serebryszcze Faultear lier dis tin guished by ¯elichowski (1983 in: ¯elichowski and Koz³owski, eds., 1983).








nor mafic magmatism has been noted in a form of diabasedykes hosted by De vo nian car bon ates in the HC Mts.(Nawrocki et al., 2013). In the south, the wes tern most part of the Up per Silesian car bon ate plat form started to sub side rap idlyaround the Holkerian/Asbian bound ary while its re main ing por -tion un der went up lift, dis in te gra tion into sep a rate blocks andero sion. In the Bielsko–Andrychów High area the ero sion re -moved lo cally at least 500 m of Up per De vo nian and Mis sis sip -pian car bon ates (Narkiewicz, 2005). The ero sional un con -

formity was onlapped eastwards by up per Visean and lowerSerpukhovian clastic de pos its com posed of ma rine shales,siltstones and sand stones up to 1500 m thick. They thin to theeast, with a tran si tion to nearshore and con ti nen tal fa cies in -clud ing a few coal beds. This whole suc ces sion grades west -wards into a thick Moravian–Silesian flysch fa cies sourced by aprograding Variscan accretionary wedge.

The depositional ar chi tec ture of the USB re sulted from theini ti a tion of a flex ural foredeep de vel oped on the de scend ing

Fig. 7. Tournaisian to mid-Visean palaeo ge ogra phy of the Variscan fore land in Po land (mod i fied fig. 8 in Narkiewicz, 2007, based on var i ous sources cited in the text)

Mag matic in tru sions in the East Eu ro pean Craton area (af ter Krzemiñska et al., 2017): E – E³k; G – Grajewo, M – M³awa, O – Olsztynek, P – Pisz, T – Tajno; other explanations as in Figure 6




plate of Brunovistulicum un der the load of a progradingEast-Sudetic orogenic prism, this in ter pre ta tion be ing sup -ported by a “knee-shaped” pat tern of the tec tonic sub si dencecurve (Fig. 5). Such con cept is con sis tent also with a rapideastwards mi gra tion of the ba sin depocentre in the late Visean(Be³ka, 1987), and with the pre dom i nant west ern source for theclastic ma te rial (Gradziñski et al., 2005; Fig. 8).

In the Lublin Sub-ba sin, the Bretonian un con formity wasonlapped dur ing the Asbian to early Brigantian bytransgressive, shal low-ma rine shaly-car bon ate de pos its50–200 m thick. The south west ern ex tent of this shelf or ramp is un clear but, by anal ogy with the pre vi ous de vel op men tal stage,the ba sin prob a bly sloped gently across the TTZ belt intoslightly deeper shelf en vi ron ments of the £ysogóry Ba sin.These were pre sum ably char ac ter ized by de po si tion of hypoxicdark shales, siltstones and quartz arenites with fine-grainedgreywacke in ter ca la tions, typ i cal of the up per Visean of thenorth ern Ma³opolska Ba sin de scribed e.g., by ¯akowa andMigaszewski (1995) and J. Malec (2010, PGI Kielce, per sonalcomm.). The source area for these sed i ments could have beenat least partly linked with the orogenic prism to the west (unpubl. data of L. Krzemiñski, 2010, PGI Warszawa, per sonal comm.).

In the Pom er a nian Ba sin a dis tinct re gres sion in the TTZ beltwas ac com pa nied by clastic fa cies progradation south -westwards, thus sug gest ing tec tonic ac tiv ity in this zone. Ear lierde vel op ing car bon ate plat forms were ter mi nated near theHolkerian–Asbian bound ary, as in the re main ing bas ins (Fig. 4).

MID-LATE SERPUKHOVIAN – EROSION AND PARALIC SEDIMENTATION

Dur ing that stage, cor re spond ing ap prox i mately to the re -gional Namurian A sub di vi sion (with out the up per most part), ama jor change in palaeogeographic pat tern oc curred in the en -tire Variscan fore land in Po land. Ar eas of the Ma³opolska,£ysogóry and Pom er a nian bas ins were up lifted and erodedwhereas the USB and Lublin Sub-ba sin con tin ued to sub sideand ac cu mu late coal-bear ing paralic suc ces sions (Fig. 9).

In the USB the up per Visean ma rine clastic de pos its gradeup wards into paralic de pos its form ing the basal part of an up to8.5 km thick coal-bear ing suc ces sion of the up per most Mis sis -sip pian and Penn syl va nian. The paralic suc ces sion at tainedmax i mum thick ness of 3800 m, pinch ing out eastwards. It iscom posed mainly of cy cli cally bed ded, fine-grained strata de -pos ited in al lu vial plain and in nearshore en vi ron ments (Kêdzior et al., 2007). Sev eral tens of volcanoclastic ho ri zons are rep re -sented ei ther by thin tuffite beds (tonsteins) or thicker (up to15 m) mixed terrigenous-pyroclastic whet stones with re de pos -ited volcanogenic ma te rial (Jirásek et al., 2013). The cen tres ofthis mostly acidic vol ca nism were prob a bly lo cated in the westin a vol ca nic arc as so ci ated with the west wards subduction ofthe Brunovistulian Plate be neath the Cen tral Sudetic ter ranes.

The ac cu mu la tion of the paralic de pos its oc curred dur ing ape riod of in creased tec tonic sub si dence in the foredeep ba sin,which started in the late Visean. The tem po ral pat tern of ac cel -er at ing sub si dence (Fig. 5) in di cates a pro gres sive flex uralbend ing of the Brunovistulicum Plate un der the load of anorogenic prism ad vanc ing from the west. The depositional re -gime was a net re sult of the tec tonic sub si dence rate and therates of sed i ment sup ply from the eroded orogen and from theBielsko–Andrychów High.

In the Lublin Sub-ba sin the open ma rine shaly-car bon atesed i men ta tion was re placed in the early Serpukhovian byparalic cyclothems com posed mostly of terrigenous shal -low-ma rine, deltaic and al lu vial de pos its. Sub or di nate com po -nents are ma rine lime stone in ter ca la tions and thin coal beds.The en tire suc ces sion ranges up to ~600 m near the SW ba sin

mar gin par tic u larly in its cen tral and SE seg ment, while its thick -ness is re duced in the Kock Fault Zone and it com pletelywedges out just east of it. The SW ba sin mar gin was pre sum -ably lo cated be yond the pres ent tec tonic bound ary of the LublinSub-ba sin (= Kazimierz–Ursynów Fault), which cross-cuts bothfa cies and sed i ment-thick ness pat terns. Nev er the less, up perMis sis sip pian to Penn syl va nian strata are un known from the£ysogóry and Ma³opolska re gions which prob a bly were un der -go ing ero sion since early Serpukhovian times. There fore, itseems plau si ble that the SW mar gin of the Lublin Sub-ba sinwas con trolled by the tec tonic ac tiv ity of the TTZ.

The lo ca tion of the ma rine realm re spon si ble for sea in cur -sions in the Lublin Sub-ba sin is poorly con strained. TheSerpukhovian de pos its pinch out to the north and west, whilethey thicken to wards the SE in the Lwów Ba sin. It seems thusprob a ble that the Lublin Sub-ba sin had a ma rine con nec tionwith bas ins along the SE part of the Euramerican ac tive mar gin.

BASHKIRIAN TO MOSCOVIAN – ACTIVE TECTONISM AND CONTINENTAL SEDIMENTATION

The early Bashkirian (= late Namurian A) was a time ofnon-de po si tion and lo cal ero sion over the en tire Variscan fore -land area (Fig. 4). Re cent ra dio met ric ages have con firmed theoc cur rence of mi nor mafic magmatism (lam pro phyres anddiabases) in the Ma³opolska and £ysogóry parts of the HC Mts.(Nawrocki et al., 2013; Krzemiñska and Krzemiñski, 2019).

In the USB the re newed sed i men ta tion was char ac ter ized bya change in depositional en vi ron ment – from paralic to mainly al -lu vial (Fig. 10). Dur ing the mid-Bashkirian (= Namurian B) to themid-Moscovian (= Westphalian C) the main part of a coal-bear -ing suc ces sion up to 4 km thick was de pos ited. Stra tal thick nessis con sid er ably re duced to wards the east ern ba sin mar gin due todepositional pinch ing out of par tic u lar units and the de vel op mentof intraformational ero sion lev els. Fol low ing the wide spreadnon-de po si tion and ero sion in the late Moscovian the re newedcoarse-grained clastic sed i men ta tion of the lat est Moscovian(= Westphalian D) was lim ited to the east ern ba sin mar gin(Fig. 4). Fi nally, af ter an other break in sed i men ta tion, arkosicsand stones and con glom er ates with var ie gated mudstones de -vel oped lo cally, reach ing a max i mum thick ness of 400 m. Thesepost-orogenic con ti nen tal red beds can be cor re lated with sim i larstrata from the Pilsen–Trutnov Ba sin Com plex in the Czech Re -pub lic dated as lat est Kasimovian–early Gzhelian (StephanianB–C; Opluštil et al., 2016).

Par al lel with the re newed sub si dence, the NE mar gin of theUSB was af fected by dextral transpressional de for ma tion – steepeast-verg ing thrusts with ac com pa ny ing sec ond ary folds and re -verse faults strik ing along the Kraków–Lubliniec Fault zone (¯aba,1999). A chain of calc-al ka line granitoid in tru sions north-east of the fault was pre vi ously as cribed to a phase of subhorizontal ex ten -sion and block up lift in the late Namurian and Westphalian (¯aba,1999). The re cent ra dio met ric data, how ever, in di cate a later age,at ap prox i mately the Gzhelian–Asselian bound ary in ter val(¯elaŸniewicz et al., 2008; Mikulski et al., 2019) which sug gestspost-orogenic em place ment.

In the Lublin Sub-ba sin the re ac ti va tion of the depocentre inthe mid-Bashkirian (= Namurian B) was as so ci ated with its dis -place ment to the NW. The up per Bashkirian to Moscovian suc -ces sion (Fig. 4), com pris ing sev eral coal-bear ing cyclothems,dis plays a thick ness change from 1500 m in the ax ial part of theNW sec tor to ~600 m in the SE. The depocentre mi gra tion con -tin ued also later, lead ing to en croach ment of sed i men ta tion intothe P³ock Sub-ba sin where Westphalian A to C (D?) clastic de -pos its un con form ably over lie the Si lu rian, at tain ing a thick ness of 1 km and wedg ing out to NE. In the Pom er a nian Ba sin the con ti -nen tal clastic de pos its of the up per Moscovian to Kasimovian




(Westphalian B to Stephanian A–B), up to sev eral hun dredmetres thick, un con form ably onlap var i ous De vo nian and Mis sis -sip pian strata, fill ing the WNW–ESE strik ing grabens.

TERMINAL VARISCAN TECTONICS – LATE PENNSYLVANIAN INVERSION

It is gen er ally ac cepted that at around theWestphalian– Stephanian bound ary (late Moscovian–earlyKasimovian) the Variscan fore land area un der went compres -

sional de for ma tion with an ap prox i mately N–S di rec tion of there sult ing tec tonic short en ing. The pre cise age of these pro -cesses is poorly con strained, be ing de fined as pre-Stephanian(late Moscovian) in the USB and pre-Perm ian in theP³ock–Lublin and Pom er a nian bas ins (Narkiewicz, 2007).

The rigid USB base ment and its Cam brian to Car bon if er ous cover were de formed into broad, faulted syn- and antiforms with a gen eral strike close to E–W, with am pli tudes of the or der of1–2 km (e.g., Kotas, 1994). The mag ni tude of the late Car bon if -er ous up lift and ero sion may be es ti mated as 2–3 km in the cen -tral part of the ba sin and ~1 km in the NE (Belka, 1993). In the

Fig. 8. Late Visean to early Serpukhovian palaeo ge ogra phy of the Variscan fore land in Po land (mod i fied fig. 9 in Narkiewicz, 2007, based on var i ous sources cited in the text)

Other explanations as in Figure 6




Kraków–Lublin Fault zone, af ter an in ferred phase of ex ten siondur ing the late Bashkirian–early Moscovian, the axis of com -pres sion ro tated from ini tially N–S to NNE–SSW and evenNE–SW. The re sult ing dextral transpression led to the for ma -tion of in verse faults, as so ci ated folds and small thrusts (¯aba,1999).

In the Ma³opolska Ba sin area the Variscan com pres sioncaused tec tonic short en ing, the di rec tion of which changedfrom N–S to NNE–SSW (Lamarche et al., 2003). The com pres -sion re sulted in the for ma tion of buckle folds strik ing 110–120°,with a no ta ble south ern vergence, and even partly be ing over -turned as in the case of the well-known Œluchowice Fold ex -

posed in Kielce (Lamarche et al., 2003; Konon, 2006). Limbs ofanticlines are com monly cut by lon gi tu di nal, mostly N-dip pingre verse faults or even small-scale thrusts de vel oped in lesscom pe tent marly Up per De vo nian strata (i.a. Racki andZapaœnik, 1979). Ac cord ing to Lamarche et al. (2003) the lon gi -tu di nal dis con ti nu ities may rep re sent in verted nor mal faults thatde vel oped due to the De vo nian ex ten sion. The Variscan struc -ture of the Ma³opolska Ba sin south of the HC Mts. dis playsfaulted folds with an am pli tude sim i lar to those in the HC Mts.but with a con sid er ably larger wave-length (Jurkiewicz, 1975;Papiernik et al., 2007; Bu³a et al., 2008).

Fig. 9. Mid-late Serpukhovian palaeo ge ogra phy of the Variscan fore land in Po land (mod i fied fig. 10 in Narkiewicz, 2007, based on var i ous sources cited in the text)

Other explanations as in Figure 6


Konon (2007) doc u mented two phases of strike-slip de for -ma tion in the south ern HC Mts. area. Phase I-1, as so ci ated with a late-fold ing or post-fold ing stage, com prised the gen er a tion ofN–S-strik ing dextral, and NE–SW-strik ing sinistral faults(NNE–SSW short en ing). A later phase I-2 en tailed the gen er a -tion or re ac ti va tion of ap prox i mately NW–SE strik ing dextralfaults, in clud ing the Holy Cross Fault (HCF). This ma jor dis lo ca -tion whose right-lat eral strike-slip mode was pro posed byBrochwicz et al. (1983) forms an up to 10 km wide zone ofmostly N-in clined re verse faults. These com pose a com plex

pos i tive flower-struc ture re sult ing from dextral transpression(Po¿aryski et al., 1992; Lamarche et al., 2003), the am pli tude of tec tonic in ver sion and as so ci ated ero sion be ing up to 4 km. The Variscan struc tural style of the south ern part of the £ysogóryBa sin is sim i lar to that in the ad join ing (HC Mts.) part of theMa³opolska Ba sin (Mizerski, 1995; Lamarche et al., 2003).

The re sults of palaeomagnetic stud ies im pose rather widecon straints on the tim ing of the Late Pa leo zoic de for ma tion inthe HC Mts. – from the Visean, when an early fold ing phase oc -curred, to the early Perm ian mark ing the ter mi na tion of the


Fig. 10. Mid-Bashkirian to early Kasimovian palaeo ge ogra phy of the Variscan fore land in Po land (mod i fied fig. 11 in Narkiewicz, 2007, based on var i ous sources cited in the text)

Mea sured di rec tions of late Westphalian com pres sion – af ter Jarosiñski in Narkiewicz et al. (2007), Lamarche et al. (2003) and ¯aba(1999); other explanations as in Figure 6



Variscan tectonism (Lamarche et al., 2003; Szaniawski, 2008).Thus, the de for ma tion could have started near the Visean–Serpukhovian bound ary un der a compressional re gime whichled to up lift and ero sion of the Ma³opolska Ba sin (Fig. 9). Later,prob a bly dur ing the late Penn syl va nian, the main phase of tec -tonic short en ing and as so ci ated de for ma tion oc curred.

The re gional strike of the late Car bon if er ous struc ture of theP³ock–Lublin Ba sin changes from NW–SE in the NW and cen -tral seg ments to NNW-SSE in the south-east (Fig. 3). TheRadom–Kraœnik El e va tion (RKE) is char ac ter ized by the stron -gest de for ma tion and high est in ver sion mag ni tude with not lessthan 3 km of a to tal up lift and as so ci ated ero sion of the Car bon -if er ous and De vo nian strata. The RKE is cut by lon gi tu di nalnearly ver ti cal and steep in verted faults, in sev eral cases form -ing pos i tive flower struc tures sug ges tive of transpression(Krzywiec, 2007: fig. 12, 2009: fig. 9).

Re cently, Krzywiec et al. (2017a) in ter preted the RKE as athin-skinned fold-and-thrust belt with ?Ediacaran to De vo nianstrata de formed into a NNE-vergent stack of thrust units. Thiscon cept, al lud ing to the con tro ver sial model of the LublinSub-ba sin as a piggy-back pas sive syncline (Antonowicz et al.,2003) raises many ques tions, how ever, and will be ad dressedsep a rately in the “Dis cus sion” chap ter be low.

The stron gest Variscan de for ma tion in the Lublin Sub-ba sin is re lated to lon gi tu di nal belts as so ci ated with theStê¿yca–Me³giew Cen tral El e va tion (Narkiewicz et al., 2007)and the Kock Fault Zone (KFZ). The first struc ture is sit u ated inthe ax ial part of the ba sin and com prises a chain of elon gatedanticlines of am pli tude up to 1.5 km flanked by in verse faultsand small thrusts com pos ing pos i tive flower struc tures. Theseare prob a bly aligned above a steep base ment fault, be ing de -tached from its plane by duc tile Si lu rian shales and Frasnianevaporites (Krzywiec, 2007; Narkiewicz et al., 2007).

The KFZ, be ing in ter nally com plex and vari able alongstrike, was de vel oped above the older base ment-rooted dis -con ti nu ity (see above; Tomaszczyk and Jarosiñski, 2017). Fol -low ing the Bretonian up lift, the Hrubieszów El e va tion was onlyslightly re ac ti vated dur ing Late Car bon if er ous tectonism. In thecen tral seg ment of the KFZ the el e va tion formed a rigid but tress for a NE-vergent thrust rooted in Si lu rian shales. Along the fron -tal part of the thrust, ero sion re moved Car bon if er ous and in part De vo nian strata up to 3 km thick while the to tal max i mumdip-slip off set is es ti mated at up to 3.5 km. The lat ter num ber,how ever, may rep re sent a cu mu la tive ef fect of thin-skinnedthrust ing and thick-skinned transpression that may have ac -com pa nied the late stage strike-slip re gime (Tomaszczyk andJarosiñski, 2017).

In ad di tion to these belts, an ex cep tion ally high de gree oftec tonic com plex ity is also noted near the bound ary be tweenthe SE and cen tral seg ments of the ba sin – in the area wherethe re gional strike changes its di rec tion (cf. Fig. 3). In other ar -eas, the seis mic sec tions show some sub or di nate in vertedfaults and mi nor thrusts with small ver ti cal throws, of var i ous but mostly NE vergence. Partly, and in some cases ques tion ably(see the “Dis cus sion” be low), these struc tures ex tend in seis -mic sec tions down to strata-par al lel de tach ment planes in theSi lu rian shaly suc ces sion (Tomaszczyk, 2016; Kufrasa et al.,2017, 2019).

The SE seg ment of the Lublin Sub-ba sin dif fers from its re -main ing part in its NNW–ESE re gional strike (Fig. 3) and, above all, in the mag ni tude of Variscan de for ma tion be ing smaller rel -a tive to that of the Bretonian (ex cept for the SW ba sin mar gin).For ex am ple, the Serebryszcze and Bia³opole faults(Narkiewicz et al., 2015), which can be re garded as the SE ex -ten sion of the KFZ (see above), have a clear Bretonian im print

while their Variscan re ac ti va tion in a strike-slip re gime is ei therab sent (Bia³opole) or mod er ate (Serebryszcze; Narkiewicz etal., 2015). Also, the char ac ter is tic fault-bounded anticlines aremiss ing here as are larger re verse faults and thrusts. Along theNE tec tonic bound ary of the RKE and in the ad join ing part of the Lublin Ba sin, base ment-rooted re verse faults are ac com pa niedby sec ond ary re verse faults and small thin-skinned thrusts witha NE and partly SW vergence (Krzywiec, 2007: fig. 7, 8, 2009:fig. 13; Narkiewicz et al., 2015).

The tec tonic style of the Variscan de for ma tion in the Pom er -a nian Ba sin is poorly known. Based on ob ser va tions of bore -hole cores, a dextral transpressive and thrust re gime was pos -tu lated by ¯aba and Poprawa (2006).

RESPONSE OF THE VARISCAN FORELAND TO OROGENIC PROCESSES

The tectono-sed i men tary evo lu tion of the Variscan fore landin Po land can be ex plained in terms of a re sponse to tec tonicpro cesses tak ing place along the ac tive south ern mar gin ofEuramerica be tween the Early De vo nian and late Penn syl va -nian (Narkiewicz, 2007). In par tic u lar, dur ing the suc ces sivestages of its de vel op ment, the fore land and its con stit u entdepocentres were vari ably af fected by tec tonic forces em a nat -ing from the West ern and Cen tral Eu ro pean Variscan orogeniczone and from its hy po thet i cal ex ten sion to wards the east. Thefor mer in flu ence will be ana lysed by con sid er ing pri mar ily theevo lu tion of the Bo he mian Mas sif (Schulmann and Gayer,2000; Mazur et al., 2006, 2010a). On the other hand, the in flu -ence of the SE branch of the Variscan Belt can be in ferred fromthe tec tonic evo lu tion of the Black Sea re gion (re cently sum ma -rized by Okay and Topuz, 2017), and, in di rectly, from the EEPde vel op ment. With re gard to the lat ter, par tic u lar at ten tion willbe paid to a ma jor late Pa leo zoic tec tonic struc ture – thePripyat–Dnie per–Donets (PDD) rift sys tem (Stephenson et al.,2006). Its de vel op ment is here be lieved to re cord evolv ingfar-field stresses gen er ated in the south (Narkiewicz, 2007).

When an a lyz ing the orogen-fore land re la tion ship, par tic u larim por tance should be at trib uted to the Up per Silesian Ba sin –the foredeep ba sin formed ad ja cent to the ad vanc ingMoravian–Silesian orogenic prism. Start ing from the lateVisean and un til the late Penn syl va nian the USB sed i men taryfill was a sen si tive re corder of orogenic pro cesses. In the re -main ing fore land area the re sponse to orogenic com pres sionalong the Variscan belt was more in di rect and thus more dis put -able.

The extensional re gime pre vail ing in the Pol ish part of thesouth ern Euramerica mar gin dur ing most of the De vo nian canbe ex plained by slab-pull forces re lated to the N-di rectedsubduction of the Rheic oce anic plate. Most prob a bly, theseforces were re spon si ble for the Emsian ini ti a tion of the nar rowRhenohercynian Ocean and its east ward ex ten sion – theback-arc ba sin in the west ern part of the Brunovistulian Plate(Fig. 11; Ziegler, 1990; Franke, 2000; Kalvoda, 2002). Thesame mech a nism may ex plain the de vel op ment of the PDD riftsys tem far ther to the east (Fokin et al., 2001). The Frasnian tec -tonic sub si dence pulse and the Famennian phase of a max i -mum sub si dence in the Lublin Sub-ba sin cor re late with the in -cep tion of rift ing and with the main rift ing stage in the PripyatTrough, re spec tively (Kusznir et al., 1996; Narkiewicz andNarkiewicz, 2008). This sug gests a com mon extensional mech -a nism of the sub si dence ac cel er a tion, con nected prob a bly within ten si fied subduction pro cesses and re lated slab-pull forcesalong the south ern mar gin of Euramerica.






Dur ing most of the De vo nian the fore land evo lu tion ap pears to have been un re lated to the tec tonic re gime of the West andCen tral Sudetic do main. The collisional Eo-Variscan tec ton icsin the Cen tral Sudetes around the Mid dle/Late De vo nianbound ary (Mazur et al., 2006, 2010a) did not res o nate in thecon tem po ra ne ous fore land bas ins. This neg a tive ev i dence may im ply a large dis tance and/or me chan i cal de coup ling be tweenthe Sudetic ter ranes and the Euramerica plate.

The extensional De vo nian re gime was in ter rupted by theBretonian tectonism near the be gin ning of the Car bon if er ous.Par tic u larly strong ver ti cal block move ments in the Lublin Ba sinwere con trolled by a compressional stress re gime with a dextraltranspression com po nent (Tomaszczyk and Jarosiñski, 2017).The Bretonian tectonism may have been re lated to ac cel er atedcollisional pro cesses along the Euramerica mar gin. The clo sureof the Rhenohercynian Ba sin in the Rhenish area started in theLate De vo nian with the old est flysch de pos its (Kulm greywackes) known from the Frasnian (Franke, 2000). In the Sudetic realmthe Famennian was a time of a con ver gence of the west and cen -tral Sudetic ter ranes lead ing to clo sure of the Saxo-Thurin gianBa sin. More or less si mul ta neously, clo sure of the East Sudeticback-arc ba sin started (Mazur et al., 2006, 2010a). These pro -cesses col lec tively tes tify to an in ten si fi ca tion of orogenic col li -sion in the west-cen tral Eu ro pean sec tor of the south ernEuramerica mar gin late in the De vo nian. The compressionalstresses were trans mit ted to the north and east into the fore landarea, lead ing to the Bretonian ver ti cal block move ments con cen -trated along zones of crustal weak ness such as the KLF zone,the TTZ (?) and the Kock Fault Zone. At the same time, ev i dence of Bretonian com pres sion is miss ing from the Pripyat Trough,which sug gests that the in ner parts of the EEP were not af fectedby collisional pro cesses along the south ern Euramerica mar gin,par tic u larly along its Black-Sea sec tor.

Af ter the Bretonian de for ma tion ep i sode, an extensional re -gime and re lated magmatism dom i nated the fore land area dur -ing most of the Tournaisian to mid-Visean. By con trast, in theSudetes, a compressional re gime con tin ued dur ing theTournaisian and early Visean, with on go ing con ver gence ofwest and cen tral Sudetic ter ranes and the de vel op ment of anaccretionary wedge above the Brunovistulian Plate which wasbe ing obliquely subducted west wards (Fig. 11; Schulmann andGayer, 2000; Mazur et al., 2006, 2010a). In the mid-Visean theWest Sudetes were up lifted and sub jected to extensional col -lapse, this be ing ac com pa nied by an in cep tion of granitoidplutonism and ini ti a tion of the pull-apart Intra-Sudetic Ba sin.

In the fore land area the most ac tive ig ne ous pro cesses,known from the late Tournaisian-early Visean of the LublinSub-ba sin (Fig. 7), cor re spond to the lat est stage ofheterochronous mag matic ac tiv ity start ing in the Givetian in thePeri-Cas pian De pres sion in the east, in the early Frasnian of theDonbas area and in the early Famennian to (?) early Tournaisianof the Pripyat Trough in the west. Tec tonic qui es cence in theTournaisian and ear li est Visean in the PDD was fol lowed by lateearly Visean ex ten sion and as so ci ated magmatism. The fore -land ex ten sion was prob a bly due to slab-pull forces trans mit tedfrom the on go ing subduction of the oce anic plate be neath theBlack Sea sec tor of the Euramerica mar gin.

In ten si fied Gond wana–Euramerica col li sion in the lateVisean–early Serpukhovian re sulted in ac cel er atedprogradation of the flysch greywackes in the Rhenisch area and also in the Wielkopolska externides (Ricken et al., 2000; Mazuret al., 2010b). In the West and Cen tral Sudetes, on go ing pro -cesses of granitoid plutonism were ac com pa nied by high-tem -per a ture and low-pres sure meta mor phism and con tin u ing de -vel op ment of the Intra-Sudetic Ba sin. In the East Sudetes the

collisional pro cesses were re flected in in creased rates of up liftand ex hu ma tion of in ter nal Moldanubian units. Be tween 340and 330 Ma the Moravian–Silesian accretionary prism un der -went ver ti cal ex tru sion, ex ten sion and thrust ing onto the east -ern fore land. The old est ev i dence of synorogenic flysch de po si -tion ap peared in the mid-Visean in Moravia (Jirásek et al.,2018), and in the late Visean in the USB. This in di cates thatdur ing that time the USB area was in cor po rated into a foredeepba sin in front of the Moravian–Silesian orogenic wedgeprograding to the NE. This is also re flected in the tec tonic sub si -dence curves, which show a steeper slope in the Asbian, mark -ing the on set of a flex ural re sponse of the Brunovistulian Plateun der the orogenic load (Fig. 5). In the Namurian A (Ser -pukhovian) the cen tral Sudetic mas sif was ap proach ing itspres ent po si tion rel a tive to Brunovistulicum.

Re newed sub si dence in the Lublin Sub-ba sin and re sult ingen croach ment of ma rine trans gres sion were co eval with the on -set of the ac cel er ated sub si dence in the late Visean andSerpukhovian of the Dniepr–Donets Ba sin. This may in di catethat the EEP area was still in flu enced by an extensional re gimewhich con tin ued lon ger than in the west ern-cen tral Eu ro peanseg ment of the Variscan belt. Al ter na tively, the sub si dence was an ef fect of orogenic com pres sion lead ing to lithospheric-scalebuck ling (Nikishin et al., 1996) or of a strike-slip/pull-apart re -gime gen er ated along crustal weak ness zones by compres -sional forces from the south. In the Black Sea re gion the south -ern BASSAC belt was af fected by in tense low pres sure-hightem per a ture meta mor phism and gra nitic plutonism (Okay andTopuz, 2017), com pa ra bly to the West and Cen tral Sudetes.

As a re sult of the early Serpukhovian re gres sion, ero sional or al lu vial-deltaic con di tions pre vailed in the fore land area dur ingthe mid-late Serpukhovian (Fig. 9). This prom i nentpalaeogeographic change has no ob vi ous ex pla na tion in tec -tonic pro cesses ob served in the Bo he mian Mas sif and in thePDD. Prob a bly, in ad di tion to a gen eral ten dency forcompressionally-in duced fore land up lift, the early-mid Serpu -khovian glacioeustatic lowstand (Bishop et al., 2009) may alsohave played a part. In the USB area, flysch suc ces sionsprograded eastwards dur ing flex ural foredeep de vel op ment in di -cat ing an on go ing pro cess of orogenic prism ad vance ment. Thedis tinct Lublin depocentre is here in ter preted in terms of apull-apart re gime (¯elichowski, 1987; Narkiewicz et al., 1998;Narkiewicz, 2007). Dextral strike-slip move ment may have beentrans mit ted by the TTZ from the orogenic com pres sion zone inthe south and was dis trib uted among TTZ-par al lel dis con ti nu ities such as the Kock Fault Zone, the Kazimierz–Ursynów Fault andthe Izbica–Zamoœæ Fault (Figs. 3 and 9).

The late Visean–late Serpukhovian phase of the ac cel er -ated foredeep sub si dence in the USB ended with the ear li estPenn syl va nian gap (early Bashkirian). This ep i sode of wide -spread non-de po si tion and mi nor ero sion (Fig. 4) co in cided with the glacio-eustatic lowstand which may have been su per im -posed on a tec tonic stand still sep a rat ing two phases oforogenic com pres sion. The en su ing re ar range ment of thedepocentres of the USB and P³ock–Lublin Ba sin may havebeen as so ci ated with a change in tec tonic con ver gence pat ternalong the Euramerica mar gin. The last collisional event in theBlack Sea re gion – be tween the accreted BASSAC belt and the MOIS con ti nen tal mar gin – oc curred near the Mis sis sip -pian–Penn syl va nian bound ary, and since that time the newlyes tab lished Euramerican mar gin faced the Palaeotethys ocean in the south (Okay and Topuz, 2017). By con trast, the col li sionbe tween Euramerica and Gond wana con tin ued in theWest-Cen tral Eu ro pean Variscides.






The eastwards mi gra tion of the USB depocentre dur ing themid-Bashkirian to Moscovian rel a tive to its lateVisean–Serpukhovian lo ca tion is con sis tent with the char ac ter -is tic foredeep-ba sin shape of the sub si dence curve (Fig. 5).Both ob ser va tions sug gest re ac ti vated flex ural bend ing of thelower Brunovistulian Plate in re sponse to a suc ces sive phase of the orogenic prism ad vance to wards the NE. The lateMoscovian ero sional/nondepositional ep i sode be fore the endof the Moscovian ba sin de vel op ment may be cor re lated with aphase of mod er ate tec tonic de for ma tion, the “Leonian” tec tonicevent. This is widely noted in the Bo he mian Mas sif area, for in -stance in the Pilsen–Trutnov Ba sin Com plex com pris ing theIntra-Sudetic Ba sin, where it is rep re sented by a gap in sed i -men ta tion last ing ~3.5 Ma (Opluštil et al., 2016).

In the P³ock–Lublin Ba sin the ap par ent con trol of mi grat ingdepocentre ge om e try by par al lel lon gi tu di nal faults sug gests apull-apart re gime re lated to a (dextral?) strike-slip move mentalong the TTZ (¯elichowski, 1987; Narkiewicz et al., 1998). Onthe other hand, the tec tonic ac tiv ity of the Kock Fault Zone

(KFZ), par tic u larly well-doc u mented for the Namurian, is re -flected in re duced sed i ment thick ness on the more sta bleHrubieszów El e va tion con trast ing with the depocentre ad join ing it to the SW (Waksmundzka, 2010). Sim i larly, the lo caldepocentres in the Pom er a nian Ba sin may had been formed ina pull-apart re gime re lated to strike-slip ac tiv ity along the TTZ(¯elichowski, 1987). As dur ing the late Visean–late Serpu -khovian stage, the strike-slip dis place ment along the TTZ mayhave been the ef fect of compressional stress trans mit ted fromthe south ern orogenic belt where tec tonic short en ing con tin uedaf ter the mid-Car bon if er ous collisional event (Okay and Topuz,2017). This in ter pre ta tion is con sis tent with the dextraltranspressional de for ma tion ob served along the Kraków–Lub -liniec Fault (¯aba, 1999).

Near the Moscovian–Kasimovian bound ary the last ep i -sodes of tec tonic short en ing oc curred in the West ern and Cen -tral Eu ro pean Variscides dur ing the ter mi nal events of con ti nen -tal col li sion. By the end of the Moscovian the West and Cen tralSudetes were fi nally moulded in an embayment of the


Fig. 11. Cor re la tion of the Variscan fore land de vel op men tal stages with the De vo nian–Car bon if er ous tec tonic and mag maticpro cesses in the Sudetes and Pripyat–Dnieper–Donets (PDD) rift sys tem (com piled from var i ous sources cited in the text)


Euramerica mar gin west of Brunovistulicum. Dur ing the fi nalphase of this pro cess the Variscan Internides moved obliquelynortheastwards along the Moravian–Silesian su ture zone, while N–S to NE–SW-di rected tec tonic short en ing af fected the en tirefore land area. In the in ter nal parts of the EEP, par tic u larly in thePDD belt, ev i dence of compressional de for ma tion is miss ing.This points to a de ci sive role of Gondwana–Euramerica col li -sion pro cesses in the west-cen tral Eu ro pean seg ment of theVariscan orogenic belt for the end-Car bon if er ous de for ma tionin the fore land area, while the Black Sea seg ment was prob a blyless ac tive at that time.

DISCUSSION

Re cently, the style and mag ni tude of Variscan tectonism inSE Po land have been re in ter preted by Krzywiec et al. (2017a,b) and in fur ther pub li ca tions by Mazur et al. (2018), Kufrasa etal. (2017, 2019), which in turn in spired a new ap proach to there gional sub di vi sion of Variscan Po land (Aleksandrowski andMazur, 2017). The con cepts pro posed in these pub li ca tions re -fer to the idea of the Lublin Sub-ba sin be ing a pas sive synclinebounded by zones of du plexes along the RKE and KFZ, andthrust northeastwards in a piggy-back fash ion (Antonowicz etal., 2003; Antonowicz and Iwanowska, 2004). This idea, draw -ing on anal o gies with the Ap pa la chian Orogen, as sumed the lo -ca tion of the Variscan orogenic front along the KFZ and im pliedits cou pling with the in ter nal parts of the orogen by means of amas ter de tach ment. Af ter its pro posal, it be came a sub ject of alively dis cus sion and was con tested in sev eral pa pers (Dadlez,2003, Krzywiec and Narkiewicz, 2003; Narkiewicz, 2003;Krzywiec, 2009). The con cept, fur ther de vel oped by Krzywiec et al. (2017a) based on new seis mic data, is here re ferred to asthe “cou pled model” of the Variscan fore land, in op po si tion tothe “de coup led model” sup ported by the pres ent au thor(Narkiewicz, 2007, this pa per; Fig. 12A). In the “de coup ledmodel” the orogenic front runs much closer to the VariscanInternides (Fig. 3). The Variscan fore land as de fined here un -der went the fi nal Late Car bon if er ous de for ma tion due toorogenic com pres sion trans mit ted from the orogen in the south, partly through ma jor crustal-scale subvertical fault zones strik -ing roughly NW–SE. The lat ter in cluded the KLF, HCF and TTZ, around which the most-de formed compressional andtranspressional struc tures are cen tered (Narkiewicz, 2007).

A key el e ment of the re cent ver sion of the “cou pled model”is the in ter pre ta tion of the RKE as a thin-skinned fold-and-thrust belt emplaced onto the mar gin of the EEC, based mainly on theseis mic re flec tion PL-5100 and 5000 pro files (Krzywiec et al.,2017a; see the lo ca tion in Fig. 3). This belt, com pris ing an up to12 km thick stack of NNE-vergent thrusts com posed of the?Ediacaran to De vo nian strata, is sup posed to ex tend from theGrójec Fault in the NW, and to wards the SE to Ukraine(Fig. 12B). Con se quently, the RKE rep re sents an orogenic front where a deep-rooted de tach ment rises up to the pre-Perm -ian–Me so zoic un con formity. The thrusts form ing the RKE con -verge to the SW into a basal de tach ment near the base of theEdiacaran strata. To the east the mas ter thrust as cends to abase of Si lu rian shales form ing a com plex tri an gle zone due to a but tress ing ef fect of the EEC base ment slope.

Krzywiec et al. (2017a) con cluded that their seis mic data donot im age any base ment-rooted subvertical dis con ti nu ities re -lated to the RKE or TTZ as in ter preted by Narkiewicz et al.(2015). On the con trary, they sug gested that the £ysogóry andMa³opolska blocks were thrust onto the East Eu ro pean cratonmar gin. In the sub se quent pa per Krzywiec et al. (2017b: fig. 3)re in ter preted the POLCRUST-01 pro file, plac ing the mas terthrust above the EEP base ment in the RKE and far ther to the

SW be yond the HCF(cf. Narkiewicz et al., 2015). The same po -si tion of the main basal de tach ment is shown by Mazur et al.(2018: fig. 7) in their in ter pre ta tion of the re gional SW–NEcross-sec tion ex tend ing from the HC Mts. to the KFZ. Ac cord -ing to their con cept, the stack of thrusts un der ly ing the RKE and most of the £ysogóry Block merges to the SW be neath the HCMts. into a sin gle de tach ment plane above the crys tal line base -ment top.

At the out set of the fol low ing dis cus sion, there should bestressed the dif fer ence be tween the doc u men ta tion of thetranscurrent model of the TTZ and ERK-re lated de for ma tion(Narkiewicz et al., 2015) on one hand, and the ev i dence sup -port ing the ri val hy poth e sis by Krzywiec et al. (2017a) on theother. In the first pub li ca tion the in ter pre ta tion is doc u mentedwith a seis mic re cord show ing re flec tions re lated to the ar chi -tec ture of the base ment and its sed i men tary-vol ca nic cover. On the other hand, the va lid ity of the seis mic in ter pre ta tion of thethin-skinned thrust-and-fold belt by Krzywiec et al. (2017a:fig. 5) is hard to as sess as they show only line draw ings of theirdeep seis mic lines PL-5000 and PL-5100, not pro vid ing anuninterpreted seis mic re cord. Two shal low com mer cial sec tions il lus trated by these au thors (their fig. 6) show vaguely im agedseis mic re flec tors with an in ter pre ta tional over lay that ren dersany in de pend ent ver i fi ca tion dif fi cult (by con trast with e.g. seis -

Fig. 12. Sche matic sketches show ing com par i son of tec toniccon cepts of the Variscan fore land in Po land: (A) ac cord ing toNarkiewicz (2007, this pa per) and (B) ac cord ing to Krzywiec(2017a, b) and Mazur et al. (2018)

HCF – Holy Cross Fault, HCMts. – Paleozoic core of the HolyCross Moun tains, KFZ – Kock Fault Zone, OBT –

Orlova–Boguszowice Thrust




mic ma te rial from the same area ear lier il lus trated and in ter -preted dif fer ently by Krzywiec, 2009: fig. 13). Clues to such ver i -fi ca tion are of fered by the pro file PL-5100 re pro cessed byMalinowski (2016), show ing that the crys tal line base ment top ispoorly trace able be yond the TTZ (Narkiewicz and Petecki,2019). On the other hand, Kufrasa et al. (2017) stress the poorqual ity of seis mic im ag ing in the com mer cial pro files cross ingthe RKE-Lublin Ba sin bound ary where their tec tonic in ter pre ta -tions of stacked thrusts are of a “con cep tual char ac ter”. No ta -bly, this res er va tion dis ap pears in the later ver sion of the pa per(Kufrasa et al., 2019).

Krzywiec et al. (2017b) re in ter preted the POLCRUST-01line in the spirit of their fold-and-thrust RKE model. They dis -carded the in ter pre ta tion of the ver ti cal TTZ dis con ti nu ity byNarkiewicz et al. (2015) mainly based on the re sults of mod el ing the seis mic re cord of a par al lel (un named) com mer cialcross-sec tion. Ac cord ing to these au thors the dis con ti nu ity ofthe base ment top is a seis mic ar ti fact caused by a lat eral con -trast in sed i ment den sity. A closer look at their mod el ing re sults(Narkiewicz and Petecki, 2019) shows, how ever, that these are: (1) based on a ques tion able tec tonic in ter pre ta tion of the“model cross-sec tion”, and (2) scarcely com pa ra ble to the orig i -nal seis mic re cord as pro vided by Narkiewicz et al. (2015). Insum mary, the doc u men ta tion pre sented so far by Krzywiec etal. (2017a, b) is un sat is fac tory, and their hy poth e sis of the“Radom–Kraœnik Fold-and-Thrust Belt” – if valid – must awaitfu ture con fir ma tion by more data, or at least a better doc u men -ta tion of pre vi ous ev i dence.

One may claim, how ever, that even if the pres ence of anRKE fold-and-thrust belt and as so ci ated Variscan Front isques tion able, there is still much ev i dence for compressional de -for ma tion in the area dis cussed, in clud ing the Lublin Sub-ba sinit self. More over, compressional struc tures, thrusts in cluded,may have been po ten tially con strained by zones of el e vatedbase ment form ing a back stop, as con ceived by Krzywiec et al.(2017a). Con sid er ing the above ar gu ments in a broader re -gional con text of the Variscan fore land it is clear that in fact themost de formed belts are as so ci ated with ma jor long-livedcrustal dis con ti nu ities: the Kraków–Lubliniec Fault (KLF), HCF,TTZ (and as so ci ated RKE) and KFZ. The “back stop model” isplau si ble in the case of lim ited thrust ing in the KFZ belt, as so ci -ated with a dis tinct base ment step (Tomaszczyk andJarosiñski, 2017). On the other hand, it seems to be in con sis -tent with the con cept of a base ment top slop ing grad u ally at alow an gle across the RKE, as as sumed by Krzywiec et al.(2017a, b) and Mazur et al. (2018).

The Lublin Sub-ba sin is re garded as a pas sive synclineboth by Antonowicz et al. (2003) and Krzywiec et al. (2017a) al -though the lat ter au thors cast doubt on its piggy-back dis place -ment and pre fer to ex plain its ge om e try as re sult ing from bothflanks be ing up turned by tri an gle zones (pas sive-roof du -plexes). Ac cord ing to the pres ent au thor the post-in ver sion ge -om e try of the ba sin may in deed be con ceived as a pas sivesynform flanked by transpressionally el e vated RKE and KFZzones, and not by purely compressional du plexes.

The dif fer ence in tec tonic style be tween the SE and NWseg ments of the ba sin (see the sec tion above on the ter mi nalVariscan tec ton ics) may be re lated to an in her ited pat tern ofcrustal dis con ti nu ities, par tic u larly the TTZ. It may be no ticedthat the lat ter zone and the Izbica–Zamoœæ fault change strike

by bend ing west wards near the cen tral seg ment of the ba sin(Fig. 12A). Thus, as sum ing an over all N–S di rec tion of re gionalVariscan com pres sion, it is to be ex pected that along pre-ex ist -ing WNW–ESE strik ing faults the compressional com po nent ofde for ma tion will be more pro nounced. In con trast, in the SEseg ment, the NNW–SSE strik ing struc tural grain of the base -ment will im part a strike-slip or transpressional de for ma tion inthe sed i men tary cover, rather than a purely compressional one.In deed, it may be ob served that the mag ni tude of thrust ing at -tains its max i mum in the cen tral seg ment of the ba sin(Tomaszczyk, 2016; Tomaszczyk and Jarosiñski, 2017), aspre dicted above. At the same time the scale of re verse-fault ingand thrust ing is much smaller in the SE seg ment (Kufrasa et al., 2017, 2019), even smaller than that of the ear lier Bretonian de -for ma tion.

An im por tant ques tion re lated to the “cou pled model” is theal leged mas ter de tach ment link ing the in ter nal orogen (Bo he -mian Mas sif) with the Radom–Krasnik Fold-and-Thrust Belt(Krzywiec et al., 2017a). Such a struc ture was in voked al readyby Lamarche et al. (2003) who spec u lated on dysharmonic de -for ma tion of the De vo nian–Car bon if er ous strata in the HC Mts.,re lated to a basal de tach ment. Nev er the less, such a struc turehas not been doc u mented so far, its pres ence be ing doubt ful on the fol low ing grounds:

(1) dur ing the late Variscan de for ma tions the base ment ofthe Variscan fore land be tween the Moravian-Silesianbelt and the EEP was highly het er o ge neous as were theover ly ing De vo nian sed i ments (Narkiewicz, 2007; seeabove, the chap ter on base ment units); it is thus highlyim prob a ble that they could serve as a re gional de tach -ment ho ri zon;

(2) the base ment is ap par ently down thrown to the NE of the KLF (e.g., ̄ aba, 1999) thus ex clud ing its role as a back -stop for NE-vergent thrusts; also, in the case of the HCFand TTZ, the “back stop ge om e try” of the base ment topis not ob vi ous;

(3) a pre dom i nant SW-vergence of the HCF is in com pat i ble with the op po site vergence of the al leged fore landthrusts of the RKE and would re quire the as sump tion(and doc u men ta tion) of a backthrust, thus lead ing to anoverly com pli cated tec tonic model of the HC Mts.

Krzywiec et al. (2017a) briefly dis cussed the prob lem of thetrans fer of tec tonic short en ing from the in ner parts of the orogen (Bo he mian Mas sif) to the RKE belt and Lublin Ba sin. Theystressed the sig nif i cance of a mas ter basal de tach ment but also con sid ered the pos si ble role of dextral strike-slip move mentsalong the Odra and Kraków–Lubliniec faults in gen er at ing a lo -cal ized short en ing in the RKE zone (Fig. 12B). While dextralstrike-slip move ments re lated to north ward com pres sion mayhave been re spon si ble for the transpressive de for ma tionsalong the KLF, the re la tion ship of a dis place ment along thisfault to the RKE de for ma tion seems doubt ful. The role of theTTZ and as so ci ated faults in trans fer ring the compressionalstresses to the RKE and par al lel faults to the NE is here re -garded as much more plau si ble.

The “cou pled model” of the Variscan fore land/orogen hasbeen promptly ap plied in the pub li ca tion by Aleksandrowski and Mazur (2017)3 as a part of their pro voc a tive whole sale re vi sionof the tec ton ics of ex tra-Carpathian and ex tra-Sudetic Po land.Only the part of their ideas that re fer to Variscan tec ton ics will be


3 This short paper is aimed at explaining the controversial "new tectonic solutions" introduced in the atlas edited by Nawrocki and Becker(2017). It may be parenthetically noted that such thorough revision of concepts well-grounded in the Polish regional geology certainly wouldrequire more clear definition of the new regional units proposed, not to mention their better substantiation. It should be also based on acomprehensive review and discussion of previous results, and not only on selected publications.





briefly dis cussed be low. Aleksandrowski and Mazur (2017)con sid er ably ex pand the in ter pre ta tions by Krzywiec et al.(2017a, b) by in clud ing their Radom–Kraœnik Fold-and-ThrustBelt into the much wider con cept of a Holy Cross– Ra -dom–Lublin Fold-and-Thrust Belt. Con se quently, they fol low an ear lier idea (Antonowicz et al., 2003), shift ing the VariscanFront to the east as far as the KFZ. The in clu sion of the HC Mts.to the Variscan orogen ap pears to be based on a se lec tive his -tor i cal dis cus sion sup ple mented by some vague state mentsabout a “quite in tensely folded” zone and there fore be long ing to“the mar ginal zone of a vast Variscan Orogen”. The USB andmost of the Ma³opolska Ba sin is in cluded within the “Up perSilesian–Ma³opolska Intramontane Ba sin” but nei ther jus ti fi ca -tion of its bound aries nor any in for ma tion on its de vel op ment(age of sed i men tary fill? sed i ment source ar eas? sub si dencepat tern?) are given by the au thors. Most of the HolyCross–Radom–Lublin Fold-and-Thrust Belt, ex cept for theLublin Sub-ba sin (as de fined here) is la belled on the at tachedmap (Aleksandrowski and Mazur, 2017: fig. 1) as the “pre-Car -bon if er ous base ment of intramontane and foredeep bas ins af -fected by a Variscan fold and thrust de for ma tion”. From thecited pa per it is not clear, how ever, if an intramontane orforedeep ba sin is meant in this par tic u lar case, what con sti tutedits ba sin fill and when it was formed.

Con clud ing the above dis cus sion, the “de coup led model” ofthe fi nal Variscan fore land de for ma tion is here re garded asbetter sub stan ti ated than the newly pro posed “cou pled model”which ap pears to be based mainly on in ad e quately doc u -mented seis mic ma te rial. The idea of transpressional de for ma -tion re lated to ma jor fault zones seems more plau si ble, be ingsup ported by well-doc u mented seis mic data and struc tural ob -ser va tions from out crops and bore holes (see sec tion above onter mi nal Variscan tec ton ics). More over, the lat ter model is more con sis tent with our knowl edge of the struc ture and de vel op ment of the Variscan fore land bas ins and their base ment, pro vided inthis ar ti cle and in its pre de ces sor (Narkiewicz, 2007). The re -gional sub di vi sion of the Variscan struc tures in SE Po land pro -posed by Aleksandrowicz and Mazur (2017) not only un crit i cally in cor po rates and ex pands the “cou pled model”, but makes iteven more ques tion able by mul ti ply ing in ad e quately de fined re -gional units, like var i ous con fig u ra tions of fold and thrust beltsand intramontane/foredeep bas ins.

CONCLUSIONS

The pres ent study sup ports the ear lier con clu sions as to therole played by the pre-ex ist ing base ment struc ture (re de finedby Narkiewicz and Petecki, 2017) dur ing the de vel op ment of the De vo nian and Car bon if er ous bas ins of the Variscan fore land inPo land (Narkiewicz, 2007). In par tic u lar, re-ac ti vated Cal edo -nian su tures and older crustal-scale fault zones in the EEP con -trolled the ge om e try of depocentres and de ter mined zones ofthe Bretonian (De vo nian/Car bon if er ous) and late Penn syl va -nian compressional de for ma tion.

Sub si dence was cre ated by forces prop a gated from the ac -tive south ern mar gin of Euramerica. An in di rect ef fect of thefar-field stress led to ex ten sion dur ing most of the De vo nian and Mis sis sip pian through slab-pull forces, and to com pres sion dur -ing the Bretonian tectonism and late Penn syl va nian in ver sion,due to collisional events. Only in the case of the USB can the di -rect ef fect of the ad vanc ing orogenic Moravian–Silesian prismcre at ing a typ i cal foredeep-ba sin sub si dence be dem on strated.

Periodization of the fore land de vel op ment re flects suc ces -sive tec tonic pro cesses along the south ern ac tive mar gin, mainly ac cel er ated con ver gence and tec tonic stand still, with a morepro nounced role of eustatic events par tic u larly dur ing the De vo -nian and near the Mis sis sip pian–Penn syl va nian bound ary. Com -par i son with the tec tonic evo lu tion of the Bo he mian Mas sifshows that Eo-Variscan terrane con ver gence near the Mid-LateDe vo nian bound ary was not re flected in the fore land, thus sug -gest ing a lack of cou pling be tween the Sudetic ter ranes and thePol ish sec tor of the Euramerica plate. On the other hand, theBretonian compressional de for ma tion in the fore land may belinked with in ten si fied orogenic con ver gence in the West-Cen tralEu ro pean Variscides lead ing to a clo sure of the Saxo-Thuringian Ba sin and East-Sudetic back-arc ba sin. A wide spread strati -graphic gap and en su ing re ar range ment of depocentres near the Mis sis sip pian-Penn syl va nian bound ary may have been as so ci -ated with ter mi na tion of the terrane col li sion in the Black Sea re -gion and on go ing con ti nen tal col li sion in the West-Cen tral Eu ro -pean Variscides (Okay and Topuz, 2017).

Late Penn syl va nian ba sin in ver sion and as so ci ated N–E toSW–NE tec tonic short en ing took place dur ing the fi nal ep i -sodes of con ti nen tal col li sion in the south. The fold ing and fault -ing of the fore land ba sin-fill was most in tense along the for merba sin bound aries. These were pre-de ter mined by oldersubvertical crustal-scale dis con ti nu ities act ing as me chan i callyweaker zones dur ing both the sub si dence and in ver sionphases. The zones, in clud ing the KLF, HCF, TTZ and KFZ, pre -de ter mined lo cal iza tion of belts of ex cep tion ally strongcompressional de for ma tion with a strike-slip com po nent, in -clud ing in verse fault ing and small-scale thrust ing. They alsodis play the high est am pli tude of in ver sion and pre-Perm -ian– Mesozoic ero sion. The tec toni cally el e vated ba sin mar ginscre ated, par tic u larly in the case of the Lublin Sub-ba sin, a char -ac ter is tic synformal struc ture. Such a con cept, termed here the“de coup led model”, as sumes trans mis sion of compressionalstresses from the orogen through dis place ment along the TTZand other tec tonic zones fo cus ing in tense, mostly transpressive de for ma tion. At the same time the re main ing ba sin fill wasmuch more weakly de formed into buckle folds and su per im -posed in verse to oblique-slip and strike-slip faults.

This crit i cal re view and dis cus sion of the new seis mic datare gard ing the deep struc ture and sed i men tary cover tec ton icsof SE Po land al lows us to con clude that the hy poth e sis of theRadom–Kraœnik Fold-and-Thrust Belt (Krzywiec et al., 2017a)as an ex ter nal part of the Variscan Orogen seems in ad e quatelysub stan ti ated. The new seis mic data doc u ment compressionalde for ma tion, in clud ing small thrusts in the RKE and LublinSub-ba sin (Tomaszczyk, 2016; Tomaszczyk and Jarosiñski,2017; Kufrasa et al., 2017, 2019). How ever, the “cou pledmodel” of the Variscan fore land, as sum ing a link be tween theBo he mian Mas sif and the RKE through a ma jor hor i zon tal de -tach ment, ap pears ques tion able. Even more doubt ful are im pli -ca tions of this model for the tec tonic sub di vi sion of the Variscanstruc ture in Po land pro posed by Aleksandrowski and Mazur(2017).

Ac knowl edge ments. The jour nal re view ers, S. Opluštil(Charles Uni ver sity in Prague) and S. Skompski (War saw Uni -ver sity) are thanked for their valu able re marks and sug ges -tions. Fund ing of the pres ent work was pro vided by the Pol ishGeo log i cal In sti tute-NRI stat u tory funds (pro ject no.61.2905.1801.00.0). J. Turczynowicz is ac knowl edged for com -puter draw ing of some fig ures.






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