Geo log i cal Quar terly, 2020, 64 (2): 321–341 DOI: http://dx.doi.org/10.7306/gq.1539

Detri tal zir con age data from the con glom er ates in the Upper Silesian and Małopolska blocks, and their im pli cations for the pre-Variscan tec tonic evo lu tion (S Po land)

Ryszard HABRYN1, *, Ewa KRZEMIŃSKA2, Leszek KRZEMIŃSKI2, Marek MARKOWIAK1 and Grzegorz ZIELIŃSKI2

1 Pol ish Geo log i cal In sti tute – Na tional Re search In sti tute, Up per Silesian Branch, Królowej Jadwigi 1, 41-200 Sosnowiec, Po land 2 Pol ish Geo log i cal In sti tute – Na tional Re search In sti tute, Rakowiecka 4, 00-975 Warszawa, Po land

Habryn, R., Krzemińska, E., Krzemiński, L., Markowiak, M., Zieliński, G., 2020. Detri tal zir con age data from the con glom er- ates in the Up per Silesian and Małopolska blocks, and their im pli ca tions for the pre-Variscan tec tonic evo lu tion (S Po land). Geo log i cal Quar terly, 64 (2): 321–341, doi: 10.7306/gq.1539

As so ci ate Ed i tor: Leszek Marks

Detri tal zir con age of the con glom erates from the Up per Silesian (USB) and Małopolska (MB) (S Poland) have been in ves ti - gated to com pare their depo si tion age and pos si ble pro veni ence. The size and poor sort ing of the lithoclasts reflect a short trans por ta tion, with de po si tion close to the sourceland. The Late Ediacaran con glom er ate of the Potrójna IG 1 and Raciechowice 1 boreholes (USB) re veal a good match be tween the ages known from the lo cal base ment explored by bore - holes. De tri tal zir con clus ters in a range of 579–585 Ma and 628–638 Ma and of 707 Ma are con sis tent with the dis tri butions of Cadomian magmatism within the nearest orogenic belt or those identi fied else where within the Brunovistulicum. In case of the con glom er ate de pos ited in the Batowice 2 borehole (MB), the zir con clus ters of 532, 551, 594 and 649 Ma, ac com panied with a pre-Svecofennian group peaked at 2071 Ma, and the lack of Sveconorvegian pop u la tion may doc u ment a tectono-sed i men tary in ter ac tion be tween the Baltica’s south ern margin and the Gondwanan Cadomian and Late Cadomian base ment during Early Paleo zoic time. This con glom erate bed was depos ited later, af ter the Early Ordo vi cian, then dock ing of Małopolska Block – Baltica was proba bly completed.

Key words: Teisseyre-Tornquist Terrane As sem blage, max i mum de po si tion age, prox i mal source, prov e nance, Cadomian orogen, Baltica.

INTRODUCTION (Kodama, 1994; Fer guson et al., 1996) and there fore may have a par tic u lar ap pli ca tion for the prov e nance study of prox i mal sources. The U-Pb de tri tal zir con geo chron ol ogy of sed i ments pro - In gen eral, the con glom er ates, as spe cific im ma ture sed i - vides in for ma tion about the age of clastic com po nents and, in ments, are de pos ited rel atively close to the sourceland and typi - some cases, con strains a depo si tion time of sed i men tary units. cally asso ci ated with re gions of high tec tonic ac tiv ity. The large Iden ti fy ing spe cific age pop u la tions en ables more re gional size of the clasts and their poor sort ing re flect short dis tances of and palaeogeographic com par i sons be tween other units and trans por ta tion. match ing them with poten tial sed i ment-source ar eas. Many of This as pect of detri tal zir con geo chron ol ogy has been ex - the prov enance age de ter mi na tions have been made on zir con plored by sampling con glom er ate de pos its from the Upper grains ex tracted from sand-sized clastic rocks that are trans - Silesia Block and the Małopolska Block. Both blocks are situ - ported usu ally over thou sands of kilo metres (Pell et al., 1997; ated in the area betw een the west ern edge of an cient litho - Sircombe, 1999; Bassett, 2000). However, coarse-grained de - sphere of the East Euro pean Craton (EEC) and the younger pos its, in clud ing con glom er ates, arise as a result of much litho sphere of the Pa leo zoic ter ranes of Cen tral and West ern shorter trans port dis tances, e.g. tens to hun dreds of kilo metres Eu rope (Fig. 1A). At the end of the Neoproterozoic they formed the southern most part of the Teisseyre-Tornquist Terrane As- sem blage (Nawrocki and Poprawa, 2006; Żelaźniewicz et al., 2009), fi nally amalgam ated in Early Paleo zoic time (Buła, 2000; Belka et al., 2002), or as the prox i mal ter ranes de tached from * Corresponding author, e-mail: [email protected] the cratonic mar gin and re-accreted af ter dextral trans la tion Received: August 7, 2019; accepted: March 11, 2020; first (Dadlez et al., 2005). published online: June 15, 2020 322 Ryszard Habryn, Ewa Krzemińska, Leszek Krzemiński, Marek Markowiak and Grzegorz Zieliński

Fig. 1A – the po si tion of the USB as a part of the Brunovistulian Terrane and the MB at the sub-Perm ian-Me so zoic palaeosurface on a tec tonic sketch map of Cen tral Europe (af ter Mazur and Jarosiński, 2006; Nawrocki and Poprawa, 2006); CDF – Cal edonian Defor - ma tion Front, FSS – Fennoscandia-Sarmatia Su ture, GFZ – Grójec Fault Zone, HCF – Holy Cross Fault, KLFZ – Kraków-Lubliniec Fault Zone, VDF – Variscan De for ma tion Front (af ter Pożaryski et al., 1992), WLH – Wolsztyn-Leszno High; the lo ca tions of drill holes are marked by black circles P – Potrójna IG 1, R – Raciechowice 1 (USB), B – Batowice 2 (MB); B – geo logi cal sketch map with out for ma tions younger than Pre cam brian in the area of the Up per Silesian Block and SE part of the Małopolska Block (after Buła and Żaba, 2005; Buła et al., 2015 mod i fied), show ing the lo ca tion of the Potrójna IG 1, Raciechowice 1 and Batowice 2 bore - holes and ad ja cent bore holes reach ing Pre cam brian rocks

Their ac cre tion pro cess and par tic u lar paths of evo lu tion The state of knowl edge for both ar eas is not equiv alent. Even that refer to Late Ediacaran and Early Paleo zoic times are still a in com plete data in di cate a dis tinct palaeo geo graphi cal, fa cies mat ter of debate (Dadlez et al., 1995, 2005; Pha raoh, 1999; and palaeotectonic de vel op ment (Buła, 2000; Buła et al., 2008) Belka et al., 2000, 2002; Nawrocki and Poprawa, 2006; of USB and MB dur ing the Pre cam brian and Early Pa leo zoic. Narkiewicz et al., 2015; Walczak and Belka, 2017). An other The USB is com monly referred to as the ex otic ter ranes with widely discussed is sue re mains an af fin ity of these crustal units. re spect to the EEC (or Baltica). There is no close palaeo - Detri tal zir con age data from the con glom erates in the Up per Silesian and Małopolska blocks, and their im pli ca tions... 323 geographic re la tion of both the do mains dur ing the Early Cam- mian Mas sif from the east (Dudek, 1980; Buła and Żaba, 2005, brian (Nawrocki et al., 2001). Usu ally, USB is in ter preted as Kalvoda et al., 2007). Be sides USB, the BVT in cludes also the hav ing been de rived from the Cadomian mar gin of Gond wana Brno Mas sif (Block), and the Thaya and Slavkov units lo cated or Avalonia and fi nally docked to Baltica before the Early Devo - on the ter ri tory of the Czech Re public, where several types of nian (Belka et al., 2000, 2002; Nawrocki and Poprawa, 2006). granitoids and gneiss es have been doc umented (Friedl et al., In con trast, the MB is in ter preted to be an in te gral part of 2004; Buła and Żaba, 2005, 2008; Kalvoda et al., 2008). The Baltica mar gin, lo cated in the pres ent-day posi tion dur ing the boundary betw een the USB and the Brno Block is de ter mined whole Pa leo zoic (e.g., Dadlez, 2001; Jaworowski and Sikorska, by the Hána Fault de vel oped on pre-Cam brian foun da tions 2006) or sup posed to have been docked to Baltica in the Late (Buła et al., 2008, 2015). The west ern bound ary of the BVT, at Cam brian (Belka et al., 2000, 2002; Valverde-Vaquero et al., the con tact with the Moldanubicum of the Bohe mian Mas sif, is 2000; Winchester et al., 2002; Nawrocki and Poprawa, 2006; marked as the Moravo-Silesian Fault Zone (Buła et al., 2015). Nawrocki et al., 2007) or in the Si lu rian (Pożaryski, 1991; The NE bound ary with the Małopolska Block cor re sponds to Narkiewicz, 2002; Ver ni ers et al., 2008). It is pointed out that the Kraków–Lubliniec Fault (Buła et al., 1997). Thus, the zone is MB dis plays linkages to both the Baltica and Peri-Gond wana in ter preted as a pre-De vo nian accretionary su ture re ac ti vated palaeocontinents (Belka et al., 2002; Nawrocki et al., 2007; dur ing the Variscan orogenic ac tiv ity. Żelaźniewicz et al., 2009). The base ment of BVT, formed dur ing the Cadomian Orog - The ev i dence for the geotectonic or i gin of MB came from eny (Fin ger et al., 2000), is over lain by weakly meta mor phosed palaeomagnetic and iso to pic prov enance stud ies. The early Ediacaran flysch de pos its. The to tal thick ness of the Ediacaran geo chron ol ogi cal anal y ses based on a low num ber of de tri tal to Ce nozoic cover at tains 8 km in the cen tral and north ern parts, mica and zir con mea sure ments from fine-grained sed i ments decreas ing to 2–3 km in the south and 1 km in the east. (Belka et al., 2000, 2002) sup ported by model ages of clastic In the south east ern part of BVT, in the area betw een Brno rocks from the north ern part of MB and their Nd sig natures and Kraków, in clud ing USB, the base ment rocks were iden ti fied (Walczak and Belka, 2017) al low con clud ing on their or i gin from by boreholes. The Pre cam brian and Lower Pa leo zoic rocks of Am a zo nian sources. USB were pen etrat ed by ~450 boreholes, but not uni formly dis- Sig nif i cant ar gu ments were pro vided af ter re-in ves ti ga tion trib uted over the area (Buła and Habryn, 2011; Buła et al., of Cam brian fauna from the Kielce re gion of MB. The or i gin of 2015). The Pre cam brian base ment is rep re sented by three rock Cam brian trilobites have been sub stan tially revised (Żylińska com plexes (Fig. 1B), dif fer ent in terms of the or i gin and age and Masiak, 2007; Żylińska and Szczepanik, 2009; Żylińska, (Buła and Żaba, 2008; Buła et al., 2008, 2015): 2013) and then di rectly cor re lated with the Scan di navian suc - – Neoproterozoic (660–556 Ma) com plex of ig neous and ces sions, stat ing a Bal tic biogeographic af fin ity. Part of the tri - meta mor phic rocks of the Bielsko-Biała Dome, known from lo bite fauna, how ever, in di cates strong sim i lar ity to the West Cieszyn–Żywiec–Bielsko-Biała–Andrychów–Kęty area; Gond wana and Avalonia fau nas. The pres ence of Avalonian – Late Neoproterozoic (Ediacaran) com plex of anchimeta - and West Gondwanan trilobites in the suc ces sion, with the morphic flysch-type deformed siliciclastics, rec ognized in a pro lif er ation of sin gle spe cies over a large area, suggests that nar row belt stretch ing from Goczałkowice through Piotro - the MB mar gin be longed to a re gion with a mixed fauna. This wice–Wysoka–Potrójna to the Lachowice area. led to the conclu sion that MB must have also faced West – Paleoproterozoic (2.0 Ga), east ern most com plex of the Gond wana and Avalonia dur ing the Cam brian ep ochs 2 and 3 Rzeszotary Horst (south of Kraków), be tween Rzeszotary (Żylińska, 2013). and Wiśniowa (Fig. 1B). It is a rel atively nar row, elon gated, In such an am big u ous geo log i cal con text, de tri tal zir con age NNW–SSE-trending struc tural el e ment ex tend ing to the in ves ti ga tions fo cused on clastic ma te rial from eroded prox i mal bound aries of the Kraków-Lubliniec Fault Zone, where sources, and depos ited on mar gins of USB and MB (Fig. 1B) mafic am phi bo lite-type rocks, with in her ited Neoarchean seems to be an ap pro pri ate tool to track the re la tion ship be - protolith of 2.7 Ga age, have been rec og nized by drillings. tween adja cent crustal blocks from the pe riod when both the In the pe riod pre ced ing the de vel opment of the Cam brian blocks might have re mained in depend ent. sed i men tary ba sin, the crys tal line base ment was sub ject to ero - The in crease in U-Pb zir con data sets for crystal line and sion re sult ing in lo cally oc cur ring con glom er ate beds, fill ing tec - sed i men tary source ar eas in the Baltica base ment, USB and tonic trench struc tures on the Late Ediacaran sur face, mostly in MB dur ing the last de cade al lows for more spe cific com par i - the east ern part of USB. These coarse-grained de pos its are sons be tween de tri tal zir con clus ters and po ten tial sed i ment com posed of lithoclasts of plutonic, vol ca nic, with mi nor meta - source rocks than were pre vi ously possi ble. mor phic and sed i men tary clasts, and char ac ter ized by a thick - De tri tal zir con age data from con glom er ates con sist ing of ness rang ing from 4 to >150 m. >100 dates ac quired from each sam ple pro vide in de pend ent The Lower Pa leo zoic that cov ers the east ern part of USB is means to test for a tec tonic re la tion ship to the mar gin of EEC rep re sented by unmetamorphosed Cam brian siliciclastic and (Baltica) and the Precam brian/ Lower Paleo zoic suc ces sion. Or do vi cian siliciclastic-car bon ate rocks. The strati graphic po si - In the light of these advances, a detri tal zir con geo chron ol - tion of the Lower Cam brian, Mid dle Cam brian and Or do vi cian ogy of proxi mal de pos its from the ad ja cent USB ver sus and units is based on acritarch and tri lo bite fauna (Buła and MB, us ing the large-n meth odol ogy, is the main pur pose of this Jachowicz, 1996; Moczydłowska, 1997). A more de tailed de - con tri bu tion. scrip tion of each lithostratigraphic unit was pro vided by Buła et al. (2015). GEOLOGIC SETTING MAŁOPOLSKA BLOCK

UPPER SILESIAN BLOCK The Małopolska Block repre sents a tec tonic unit of un iden ti - fied age of con sol i da tion, be cause its crys tal line base ment has The Up per Silesian Block forms a north ern part of the com - not been en coun tered. Ac cord ing to some au thors, the MB is in pos ite Brunovistulicum Terrane (BVT) neigh bour ing the Bo he - fact com posed of sev eral sub-units of dif fer ent geo log i cal de - 324 Ryszard Habryn, Ewa Krzemińska, Leszek Krzemiński, Marek Markowiak and Grzegorz Zieliński vel op ments, in clud ing the north ern Kielce Block and southern The im por tant litho logic unit in the upper part of the se - Miechów-Rzeszów Block, while Belka et al. (2000) defined the quence is greywackes (Niewachlów Beds) com posed of sed i - east ern part of MB as the San Block. men tary and vol ca nic rocks de pos ited dur ing the mid-Ludlow In con se quence, the pres ent-day MB has in gen eral a “mo - (Kozłowski et al., 2014). A time frame of vol ca nic and sub - saic” na ture, expressed by the pres ence of block struc tures volcanic ac tiv ity at the end of the Lud low was con firmed by formed by Ediacaran anchimetamorphic rocks sur rounded by diabase dykes of 432 ±2 Ma (Nawrocki et al., 2007) and abun - var i ous rocks of dif fer ent Pa leo zoic ages, as a re sult of dance of volcanogenic zir con grains crystal lized at Variscan faults with high am pli tudes (Buła and Habryn, 2008 425–426 Ma, pre served as xeno crysts in the Kielce tuffs (Krze- and ref er ences therein). mińska and Krzemiński, 2019). In the western most part, the MB is sepa rated from USB by the tec toni cally well-de fined Kraków-Lubliniec Fault Zone (KLFZ), prob ably form ing a part of the prom i nent Ham burg- SUMMARY OF PUBLISHED U-Pb ZIRCON Kraków trans con ti nen tal fault zone (Buła et al., 2008 and ref er - AGE DATA ences therein), KLFZ which con tin ues also into the base ment of the Outer Carpathians to the south-east. From the south, the MB is cov ered by thick Carpathian flysch and lim ited by the Only a few geochron ol ogi cal re ports have been published Peri-Pieniny Zone. Ac cord ing to geo phys i cal in ves ti ga tions, the dur ing last de cades for the Pre cam brian rocks of USB and MB MB base ment may oc cur at depths exceed ing 10 km (Malino - (Compston et al., 1995; Bylina et al., 2000; Żelaźniewicz et al., wski et al., 2005). 2009; Żelaźniewicz and Fan ning, 2020) or their xeno liths rec og - A se quence of rocks rec ognized in MB consists of Late nized be tween youn ger sed i ments (Burda et al., 2019; Gawęda Neoproterozoic (Ediacaran) de pos its cov ered by Lower Or do vi - et al., 2019). Nev er the less, they pro vide a sig nif i cant sup port for cian to Neo gene clastic and car bon ate rocks. At least five un - the in ter pre ta tion of the new out come of de tri tal zir con age data con formi ties, in clud ing Ediacaran/ Cam brian and Cam brian/Or - in both ar eas. do vi cian, have been doc umented in this se quence. The old est The ev i dence of the old est base ment within USB derives rocks of the MB, rec ognized so far, are mainly siltstones and from the unique Rzeszotary Horst (RzH) which is com posed of mudstones, dated by palynological method ol ogy as Ediacaran high-grade migmatized orthoamphibolites and gneiss es. The (Jachowicz-Zdanowska, 2014). They were dis cov ered in the con ven tional U-Pb dat ing of zir cons from the RzH am phi bo lites newly drilled Cianowice 2 bore hole (Habryn et al., 2014). The yielded the upper in ter cept age of 2732 +23/–21Ma (Bylina et Ediacaran sed i ments were covered di rectly by Middle Ju ras sic al., 2000) in ter preted as the age of ig neous protolith, whereas sand stones and con glom er ates. the zir cons from neosomes analysed by SHRIMP pointed to a The Ediacaran clastic rocks, poorly sorted sand stone and prom i nent meta mor phism or/and migmatization at ~2.0 Ga con glom er ate beds with pla nar bases and grad ual, in dis tinct (Żelaźniewicz et al., 2001; Żelaźniewicz and Fan ning, 2020). tops, in di cate turbiditic de po si tion (Żelaźniewicz et al., 2009). The most com mon ev i dences of the ig ne ous ac tiv ity in USB For part of the flysch-type rocks, Ediacaran age was con firmed and adja cent units within BVT are re ferred to Late Neo pro - by acritarchs (Jachowicz-Zdanowska, 2011). There is also a terozoic time (Ta ble 1). The zir con U-Pb dat ing doc umented a tuff hori zon rec og nized at a depth of 1388–1394 m in the Książ re li able age of sev eral granitoid bodies of the Bielsko-Biała Wielki IG 1 borehole (for lo ca tion see Fig. 1B), where a U-Pb Dome (Żelaźniewicz et al., 2009), which crys tal lized at age of 549 ±3 Ma (Compston et al., 1995) clearly sup ports the ~582.7 Ma (Roztropice) and 579 ±2.7 Ma (Kęty-8). Be sides ig - late Ediacaran age of the MB de posi tion. neous rocks, the Neoproterozoic turbiditic succes sions in USB, In the south west ern part of MT, close to the con tact with the fed largely from a for mer ac tive mar gin of the recy cled collisio - USB, the Ediacaran siliciclastic rocks are cov ered un com fort - nal orogen and its hin ter land, pro vided a re cord of de tri tal zir con ably by Or do vi cian-Lower Si lu rian car bon ates and Up per Si lu - ages (Żelaźniewicz et al., 2009). The 90% of all ana lysed grains rian shales (Buła et al., 1997; Buła and Habryn, 2008). (n = 37), sum ma rized from two sam ples, fall in a group of The ex po sures of Cam brian sed i men tary suc ces sion of 680–550 Ma, ac com pa nied by single grains of ~1.5 and MB, com posed of siliciclastic rocks, are known from the north - ~1.9 Ga (Żelaźniewicz et al., 2009). ern part, in the area of Holy Cross Moun tains. The low er most Among data ob tained di rectly from USB, a sim i lar U-Pb zir - part of the Or do vi cian suc ces sion con sists of glauconite-rich con age has been ac quired from an exotic megablock (>100 m) mudstones with abun dant pyroclastic ma te rial (Salwa and known from the West ern Outer Carpathians flysch (Burda et al., Trela, 2019). 2019). These orthogneisses oc curred in Bugaj and Andrychów Sev eral ash beds are pre served be tween the Up per Or do vi - on the bound ary betw een the Silesian and Subsilesian units. cian and Si lu rian dark shales and mudstones of the Holy Cross They crys tal lized at 580.1 ±6.0 Ma and 542 ±21 Ma, re spec - Moun tains (Trela et al., 2018). The Si lu rian suc ces sion of MB tively, and were in ter preted as olistoliths within the Silesian has been com piled from dis con tin uous drill core pro files. It com - Nappe (Burda et al., 2019). Sim i lar crys tal line olistolithswere prises Llandovery, Wen lock and Lud low de pos its cor re lated also col lected from the Outer Carpathian ba sin flysch (Istebna, with a co eval se quence exposed in the Kielce Re gion of the Osielec and Nowe Rybie exotics) cov er ing the east ern pro lon - Holy Cross Moun tains (Ver ni ers et al., 2008 and ref er ence gation of USB (Gawęda et al., 2019). These rocks pro vided di - therein). In the south west ern part of MB (near Kraków), the Si- rectly a re cord of the hid den mag matic/meta mor phic rocks lu rian de pos its are di vided into two parts. The older one is dom i - formed at 566 ±3.1 Ma, 603.7 ±3.8 Ma, 613.3 ±2.6 Ma, and nated by schists. The younger part is com posed of mudstones, 617.5 ±5.2 Ma, most prob ably origi nated from the east ern BVT sand stones and con glom er ates from Łapczyca (Heflik and (USB). Thus, they are inter preted as an ev i dence of a Cado - Konior, 1972; Konior, 1974 and ref er ences therein). The thick - mian crys tal line base ment el e ment. ness of these se ries var ies from 10 m in the Wyciąże 1 bore hole The same type of co eval ig neous ac tiv ity (Ta ble 1) was doc - to over 217.1 m in the Batowice 2 bore hole. These con glom er - umented in the exposed wes tern most part of BVT. Much more ates were re garded as a Mid dle Lud low molasse-type deposit U-Pb zir con ages were ob tained from the west ern part of BVT, of the Cal edonian orogenic pe riod (Łydka et al., 1963). close to the Brno Mas sif (Soejono et al., 2017; Hanžl et al., Detri tal zir con age data from the con glom erates in the Up per Silesian and Małopolska blocks, and their im pli ca tions... 325

Ta ble 1

The ev i dences of ig ne ous ac tiv ity from USB, MB and ad ja cent units

U-Pb age Area Sam ple ID [Ma] Rock type Refer ences Brunovistulian terrane Lody 629 ±6 Żelaźniewicz et al. (2009) Rozt-2 583 ±6 Żelaźniewicz et al. (2009) granodiorite Upper Silesian Block Kety 8 579 ±2.7 Żelaźniewicz et al. (2009) Rocz 558 ±4 Żelaźniewicz et al. (2009) (olistoliths ) Bugaj 580 ±6 granitoid Burda et al. (2019) exotic blocks Andrychów 542 ±1 orthogneiss Burda et al. (2019) Strzelin 600 ±9 Oberc-Dziedzic et al. (2003) Fore-Sudetic Block Velké Vrbno 568 ±9 Gneiss Kröner et al. (2000) Keprnik Dome 570 ±6 Kröner et al. (2000) Ludvikov 684.5 ±0.9 Kröner et al. (2000) orthogneiss Filipovice 612.7 ±1 Kröner et al. (2000) Jehnice 595 ±1 granodiorite Timmerman et al. (2019) Blansko 597 ±2 tonalite Timmerman et al. (2019) Slavkov Unit Lhota 606 ±2 granodiorite Timmerman et al. (2019) Ždanice 601 ±2 Timmerman et al. (2019) diorite Uhřice 594 ±2 Timmerman et al. (2019) Popice 590 ±8 leucogranite Timmerman et al. (2019) Gumping 595 ±1 Fin ger et al. (2000) Thaya Unit DF-B (Derflice) 603 ±3.2 granodiorite Svojtka et al. (2017) DF-C 603 ±5.2 Svojtka et al. (2017) Opalenka 725 ±15 Fin ger et al. (2000) Central Ba sic Belt BM04 733 ±5 metarhyolite Hanžl et al. (2019) BM12-04 728 ±5 Hanžl et al. (2019) BIT-1 584 ±6 Friedl et al. (2004) BTG-1 578 ±7 Friedl et al. (2004) UD2 568 ±3 orthogneiss Soejono et al. (2017) BM12-02 655 ±3 Hanžl et al. (2019) Bittesch gneiss nappe UD3 (Brno) 601 ±3 Hanžl et al. (2019) UD5 (Svratka) 634 ±6 Soejono et al. (2017) SPI1 614 ±10 Friedl et al. (2004) Eggenburg 583 ±11 Fin ger et al. (2000) granodiorite Bittesch 578 ±7 gneiss Friedl et al. (2004) 555 ±12 Teipel et al. (2004) Bayerischer Moldanubian terrane Wald 549 ±7 Teipel et al. (2004) 549 ±6 Teipel et al. (2004) 549 ±3 Compston et al. (1995) Małopolska Block Książ Wielki (578 ±5) tuff Compston et al. (1995) (619 ±4) Compston et al. (1995)

2019) which is sep arated from USB by the Hána Fault. In gen - zir con col lec tion con tains also two older com ponents of 578 eral, the Cadomian events iden ti fied in the BVT in cluded: meta - ±4.5 Ma (13%) and 619 ±4 Ma (15%), as well as sev eral de tri tal mor phism and plutonism at ~650–620 Ma, wide spread arc-type grains that have con cor dant and sep arate Early Protero zoic granitoid in tru sions at ~590–580 Ma, and late bi modal mag - and Archaean ages. matism at ~560–550 Ma. Re cently, these time frames have The Neoproterozoic rocks of MB are rep re sented mainly by been di rectly con firmed (Soejono et al., 2017) by U-Pb zircon a clastic, flysch-type se ries. In con se quence, only detri tal zir con ages of 634 ±6 Ma from the Svratka Dome, 601 ±3 Ma from the age de ter mi na tion was con ducted (Żelaźniewicz et al., 2009) on Brno Mas sif, and 568 ±3 Ma from the Bíteš orthogneiss (Ta ble fine-grained sed i ments sam pled from the area close to the 1: sam ple UD2). A co eval ig neous rocks protolith for ma tion are Kraków-Lubliniec Fault Zone (five sam ples). Despite the sta tis - known from the Moravian unit (Friedl et al., 2004).Their crys tal - ti cally small num ber of ar chived sin gle grain anal yses (from n = li za tion ages were ob tained at 584 ±6 Ma (Bittesch gneiss), 578 7 to n = 30) from each sam ple, these age data re veal the youn- ±7 Ma and 567 ±6 Ma (Eggenburg metagranite). gest pop ula tion of de tri tal zir cons have ages be tween ~670 and In con trast to the ev i dences from USB, the U-Pb age data of ~570 Ma. Also de tri tal zir con stud ies from the Lower Cam brian the MB rocks still re mains poorly doc umented. In one bore hole, rocks from the north ern part of MB (Kędziorka out crop, Kielce Książ Wielki IG 1, how ever, the zir con U-Pb age de ter mi na tion Re gion) pro vided U-Pb ages of ~540, 557 and 592 Ma, and (Compston et al., 1995) for a tuff layer confirm ed the Ediacaran Pb-Pb ages of ~1.21.37, 1.5 and 2.0–2.1 Ga, 2.5 and 3.0 Ga age of a vol ca nic event at ~549 ±3 Ma (72% of the total). The (Belka et al., 2002). 326 Ryszard Habryn, Ewa Krzemińska, Leszek Krzemiński, Marek Markowiak and Grzegorz Zieliński

SAMPLING con glom er ate – rock sam ples, in clud ing clasts of var i ous sizes up to fine-grained com ponents and ma trix. It was not pos si ble to extract an in di vid ual groups of clasts, and the system atic clasts Sam pling for the de tri tal zir con geo chron ol ogy was per - count ing was not per formed. formed on con glom er ate beds cored in bore holes drilled a long Con glom er ate with clasts of var i ous lithologies, de scribed time ago; hence, the core pro files were incom plete. New inves - below , were col lected from three bore holes: two from USB ti gations of detri tal zir con age were con ducted on whole bulk (Potrójna IG 1 and Raciechowice 1) and one from MB (Batow ice 2) in the area near the bound ary with the USB (Figs. 1B, 2 and 3).

Fig. 2. Cor re la tion of the Ediacaran/Lower Pa leozoic sec tions of the Potrójna IG 1 and Raciechowice 1 boreholes from the Up per Silesian Block, and the Batowice 2 bore hole from the Małopolska Block; in ter vals of sam pled con glom er ates are marked De tri tal zir con age data from the con glom erates in the Up per Silesian and Małopolska blocks, and their im pli ca tions... 327

Fig. 3. Pho to graphs doc u ment ing con glom er ate drill core sam ples and their as sem blages of clasts (see the main text for expla na tions) 328 Ryszard Habryn, Ewa Krzemińska, Leszek Krzemiński, Marek Markowiak and Grzegorz Zieliński

POTRÓJNA IG 1 grey mudstones and greywackes. The clasts are poorly sorted and con tain peb bles in range of 0.2–12 cm. The Potrójna IG 1 borehole rep re sents a nar row area close Be cause of a sig nif i cant strati graphic gap, there is no di rect to the Bielsko-Biała Dome el evated struc ture (Fig. 1B). This el - ev i dence of the age of con glom er ate. His tor i cally, a De vo nian eva tion is formed by Neoproterozoic crystal line rocks, mostly age was con sid ered (Cebulak, 1958), but the rock from granitoids and meta-granitoids (Żelaźniewicz et al., 2009). The Batowice 2 closely resem bles the con glom er ate known from Potrójna IG 1 conglom er ates (Fig. 2), cov ered by non-meta - Łapczyca, which was as signed to the Mid dle Lud low/Up per Si - mor phosed Lower Cam brian sed i ments, were in ter preted as lu rian (Łydka et al., 1963). Eocambrian (Ślączka, 1985) and then as Ediacaran (Buła and All pre sented con glom er ates are poorly sorted, and the Żaba, 2008). The red dish brown con glom er ates oc cur be tween pebbles show a wide range of com po si tion, round ness and a depth of 3466 and 3493.5 m (Fig. 3). Two sam ples from size, and contain var i ous amounts of ma trix that con sists com - depths of 3471–3472 m (Potrójna IG 1 – A) and 3472–3481 m monly of clay- or sand-sized par ti cles or a mixture of clay and (Potrójna IG 1 – B) were taken for de tri tal zir con age in ves ti ga - sand. The frame work grains of con glom er ates are com posed tion. They repre sent in ter vals of ~1 and ~9 m in thick ness, re - mainly of rock frag ments (lithoclasts) rather than of in di vid ual spec tively, but there was no dis cern ible lithological dif fer ence min eral grains. The round ing of the clasts in di cates that they be tween these two sam ples. Thus, a di vi sion was made for were trans ported over some dis tance from their orig i nal source check ing of the results repeat abil ity and as a con trol of the in ter - and they have resided in a high-en ergy envi ron ment for some nal vari abil ity within one con glom er ate layer. Both sam ples time. from the Potrójna IG 1 are rep re sented by oligomictic con glom - er ate com posed mainly of im ma ture sed i men tary and low-grade metasedimentary rocks (Fig. 3). The ma jor com po - ANALYTICAL PROCEDURES nents are frag ments of im ma ture greywacke, ac com pa nied by marls, car bon ates and al tered pyroclastics. They not contain a The sam ples were pro cessed by stan dard meth ods for sep - clasts of ig ne ous rocks. Feld spar grains are very scarce. a rat ing zir cons, in clud ing crush ing, siev ing, heavy liq uid and Frantz isodynamic sep ara tor treat ment, and the fi nal hand-pick - RACIECHOWICE 1 ing. The zir cons to gether with chips of the Temora-2 zircon (206Pb/238U age of 416.8 ±0.3 Ma; Black et al., 2004) and 91500 zir con as a ref er ence for U-con tent (U = 78 ppm, a 207Pb/206Pb The Raciechowice 1 bore hole is lo cated on the Rzeszotary age of 1065.4 ±0.3 Ma; Wiedenbeck et al., 1995) were mounted Horst (Fig. 1B) formed by a complex of Neoarchean- Paleopro - in ep oxy and pol ished un til quasi-cen tral sec tions were rea - te rozoic crystal line rocks. The con glom er ate beds were found ched. Cathodoluminescence (CL) tech nique was used to iden - at depths of 2399–2404 m and 2415–2424 m (Fig. 2) un der tify dis tinct zir con do mains. Lower Ju ras sic de pos its. No Pa leo zoic rocks have been pre - The U-Pb de tri tal zir cons geo chron ol ogy was con ducted by served. De spite the lack of di rect ev i dences, a Late Neo - SHRIMP at the PGI-NRI us ing anal ogous strat egy as described proterozoic age of the con glom er ate was as sumed based on by Wil liams et al. (2009). The anal yses were per formed us ing com par i sons with other depos its within USB (Buła, 2000). The an O-pri mary beam fo cused onto the zir con sur face with an el - avail able core frag ments (Fig. 3) taken from depths of 2404 and lip ti cal spot size in a range of ~20–23 mm. Off-line data pro cess - 2415 m were com piled as one sam ple. The polymictic con glom - ing was ac com plished us ing cus tom ized in-house soft ware er ate con sists of sev eral dif fer ent types of rocks. The peb bles SQUID2. All U-Pb data are shown in Ap pen dix 1*. Anal y ses de rived from meta sedi ments seem to be vir tu ally domi nated, were car ried out on >100 spots in each sam ple, ac quired on the but there are also nu mer ous clasts of vol ca nic or pyroclasti c core of each zir con grain, in a se quence con sist ing of one anal - rocks, and clasts of plutonic rocks and their metamor phic coun - y sis of a Temora-2 ref er ence zir con mea sure ment af ter ev ery ter parts. fourth un known sam ple anal y sis. For de tri tal grains >1000 Ma, the 206Pb/207Pb age is used in BATOWICE 2 the cu mu la tive prob abil ity plot, but for data <1000 Ma, the 206Pb/238U age is pre ferred be cause 206Pb/238U ages are gen er - ally more precise for younger ages, whereas 206Pb/207Pb ages The Batowice 2 bore hole was lo cated in the north ern sub - are more precise for older ages (Gehrels, 2012). urb of Kraków. Drill ing was com pleted in 1958, thus, at the time To de ter mine the max i mum depositional age, the gen eral of cur rent sam pling, the core ma te rial was frag men tary. The meth od ol ogy of Dickinson and Gehrels (2009) has been petrographic descrip tion was pre pared by Cebulak (1958) adopted. The only modi fi ca tion for the youngest clus ter of zir - These coarse grained sed i ment are cov ered by Jurasic strata. cons (n >3) that over lap in age at 2s was the cal cu la tion of con - Un der of in com plete lay ers of the Me so zoic sed i ments (Fig. 2). cordia age in stead of weighted mean age. The con glom er ate bed was drilled at a depth of 330 m, con tin u - More over, as part of the dis cus sion, in or der to com pare ing down to the borehole bot tom (~530 m) with a fewan arkosic and eval uate di rectly the or i gin of de tri tal zir con age, re cords sand stone and greywacke thin layers. The con glom er ate con - from var i ous clastic rocks from the EEC sed i men tary cover sists of multi-col oured peb bles (Fig. 3): plutonic rocks in clud ing were used. al ka line gran ites, peg ma tite ac com pa nied with red quartzi tes, They were col lected from: black sil ica rocks, red-brown acid erup tive rocks (rhyo lite, da - – coarse-grained sand stones and con glom er ates of the Żu - cite, an de site), and some sed i men tary rocks in clud ing shales, ków For ma tion (Pacześna, 2014), com posed of clasts de-

* Supplementary data associated with this article can be found, in the online version, at doi: 10.7306/gq.1539 Detri tal zir con age data from the con glom erates in the Up per Silesian and Małopolska blocks, and their im pli ca tions... 329

rived from eroded crystal line rocks depos ited in gravel-bed tios and the con cordia age at 554.5 ±6 Ma (MSWD = 1.3), that braided river chan nels and on al lu vial fans of the SW slope iden tify the youngest po ten tial proto-source and may suggest of EEC (Pacześna, 2014). They begin the Ediacaran clastic the ear li est pos si ble age of de posi tion as the Late Ediacaran. suc ces sion of the Lublin-Podlasie sed i men tary ba sin. The The age spec trum has an unimodal dis tri bu tion. The dom i nant re sults of detri tal zir con age de ter mi na tions, n = 80 (Ap pen - group with a peak at ~602 Ma repre sent ing ~80% of all grains is dix 2), from a polymictic con glom er ate sam ple taken from Ediacaran (Ta ble 2). There is also a sub-group 13.9% of the Kaplonosy IG 1 borehole (depth 1809 m), re flect a Cryogenian age and two Tonian grains (Fig. 6A). clastic ma te rial sup plied from a rel a tively prox i mal source, most prob ably located on the TTZ mar gin of EEC in east ern POTRÓJNA IG 1 – B: and south east ern Po land; DEPTH 3472–3481 m (USB) – fine-grained sand stone of the Białopole bore hole, depth 2870 m, of the Łopiennik For ma tion, us ing Pb-Pb zir con age The ages of de tri tal zir cons from the sec ond sam ple of data, n = 30, pub lished by Żelaźniewicz et al. (2009). These Potrójna IG 1 bed, range from Mesoproterozoic (1419 ±48 Ma) clastic sed i ments of the Łopiennik Fm. are wide spread in the to Late Ediacaran (549 ±18 Ma). The youngest clus ter is com - cen tral and southw est ern parts of the sedi men tary basin, posed of four grains (Fig. 5B), with a con cordia age at 552 rep re sent ing the low est part of the Edia caran zone of Vendo - ±13 Ma (MSWD = 0.073). The youngest de tri tal ma te rial and taenia–Sabellidites in the cen tral part of the Lublin-Podlasie the dom i nant group of detri tus rep re sented by ~91% of grains is sed i men tary ba sin (Pacześna, 2014). Ediacaran (Fig. 6B). The his to gram (in sert) doc uments at least Due to lack of dat able vol ca nic marker ho ri zons or/and youn- three sub-peaks at ~585, 607 and 614 Ma. The grains older ger cross-cut ting intrusives, diagenetic monazite grains were in - than 650 Ma are rel atively rare. ves ti gated to constrain the age of the diagenetic or/and meta - mor phic events (authigenic grains) or to char ac ter ize the ages of RACIECHOWICE 1: DEPTH 2399–2404 m (USB) de tri tal monazite pre served in the ma trix of conglom er ates. Chem i cal anal y ses of the monazite observed mostly within the ma trix in sam ples from Potrójna A (USB) and Batowice The sam ple from Raciechowice 1 showed a dis tinct spec - (MB) were per formed us ing a Cameca SX 100 elec tron micro- trum of detri tal zir con ages (Fig. 4C), rang ing from sin gle probe equipped with four wave length dispersive spec trom eters Mesoarchean (3145 ±80 Ma) to Late Ediacaran (549 ±32 Ma) (WDS) at the PGI-NRI. ages. It con tains a ma jor con cen tra tion of ages peaked at Monazite chem i cal com po si tion was ana lysed us ing 15 kV ~650 Ma and a mi nor con cen tra tion at ~2600 Ma. The youngest ac cel er at ing volt age, 180 nA beam cur rent, and ~3 mm size clus ter is formed by four grains (Fig. 5C) that yielded a con- beam fo cused on a car bon-coated thin-sec tion. cordia age at 547.5 ±21 Ma (MSWD = 0.006), but a sta tis ti cally More over, chlorite chem i cal com po si tion was ana lysed to dom i nant group (~39% of the anal yses) has a Cryogenian age ob tain the tem per a ture con di tion of this min eral for ma tion, peaked at 650 Ma (Fig. 6C), with a mi nor Ediacaran sub group which may cor re spond to anchimetamorphism tem per a tures. (26.7%). There is also a prom i nent group of Neoarchean grains Tem per a ture was de ter mined us ing solid so lu tion ther mom e - (17%), with peaks form ing wider clus ter around 2600 Ma. ters that uti lize a pos i tive cor re la tion be tween AlIV con tent and tem per a ture based on cal i brated for mu las pro posed by BATOWICE 2: DEPTH 313–530 m (MB) Cathelineau and Nieva (1985) and Cathelineau (1988), and fur - ther mod i fi ca tions of those geothermometres and two fur ther mod i fi ca tions of these geothermometres in which Fe/(Mg+Fe) The age of de tri tal zir cons from the Batowice 2 con glom er ate ra tio in chlorite has been em ployed to cor rect the AlIV quan tity (Fig. 4D) ranges from Paleoproterozoic (2153 ±18 Ma) to Or dovi - (Kranidiotis and MacLean, 1987; Zang and Fyfe, 1995). All cian (474 ±27 Ma). The youngest group consists of only two WDS ana lyt i cal data are shown in Ap pendixes 2 and 3. grains (Fig. 5D) with sim i lar U-Pb ratios, yielding a con cordia age at 482 ±27 Ma (MSWD = 0.14). The youngest sin gle zir con grain (474 ±27 Ma) is con cor dant (the discordancy of +4%). The main RESULTS OF DATING group of ages peaked at ~590 Ma is formed by 42% of grains of Ediacaran age (Fig. 6D). The next pop ula tion with a peak at ~2085 Ma is formed by 27.6% of grains of Paleoproterozoic age. DETRITAL ZIRCON GEOCHRONOLOGY The rest of the zir cons show a Cam brian age (sub-group of 14.6%) and Cryogenian age (sub-group of 9.48%). The num ber of sin gle-grain anal yses per sam ple ranges be - tween 102 and 116. All U-Pb zir con age re sults ob tained in this CHEMICAL GEOCHRONOLOGY study are listed in Ap pen dix 1, but sum mary of data in clud ing OF MONAZITE age char ac ter is tics of each sam ple are pre sented in Ta ble 2. A few re sults with high com mon lead (Pbc >1%) were ex - In con trast to the zir con geo chron ol ogy, the monazite were cluded, but all ac cepted were used to construc t Tera- analysed using grains ex posed in thin-sec tions, thus the sta tis - Wasserburg and Wether ill con cordia di agrams in Fig ure 4A–D. tics of mea sure ments is rel atively low. The monazites from two con glom er ate sam ples from the Potrójna IG 1 – A (USB) and POTRÓJNA IG 1 – A: Batowice 2 (MB) were stud ied. Chem i cal dat ing of monazites DEPTH 3471–3472 m (USB) from the Potrójna sam ple USB (Ap pen dix 2) re vealed a lim ited num ber of small and rel atively homo geneous grains, ~10 to The ages of de tri tal zir cons from the up per most part of the 30 mm in size. They provide only Ediacaran ages be tween 590 Potrójna IG 1 conglom er ate range from Late Paleoproterozoic ±44 Ma and 548 ±62 Ma. (1638 ±17 Ma) to Late Ediacaran (549 ±7 Ma). The youngest About 20 monazite anal y ses from Batowice 2 (MB) doc u - clus ter is formed by six grains (Fig. 5A) with con sis tent U-Pb ra - ment a wider age range be tween 658 ±44 Ma and 476 ±25 Ma. 330 Ryszard Habryn, Ewa Krzemińska, Leszek Krzemiński, Marek Markowiak and Grzegorz Zieliński

Ta ble 2

A sum mary of the U-Pb de tri tal zir con age re sults ob tained from conglom er ate sam ples

Area/Block USB USB USB MB Sub area Bielsko-Biała Bielsko-Biała Rzeszotary western most part of MB Sam ple ID Potrójna IG 1 Potrójna IG 1 Raciechowice 1 Batowice 2 Depth in ter val [m] 3471–3472 (A) 3472–3481 (B) 2399–2424 >3000 Num ber of anal y ses n = 108 n = 102 n = 116 n = 114 Youngest grain [Ma] 549 ±7 549 ±18 549 ±32 474 ±27 (% discordancy) (+1%) (–10%) (–10%) (+4%) Range [Ma] 549 ±6 (+1%) 549 ±18 (–10%) 549 ±32(–10%) 474 ± 27 (+4%) (from youngest ac cepted) 1638 ±17 1419 ±48 3145 ±80 2153±18 Age of youngest clus ter 554 ±6.6 552 ±13 547 ±21 482 ±27 (number of grains) (6) (4) (4) (2) Num ber of sub groups 1 1 2–3 2–3 Dom i nated group (peak) 600 602 650 & ~2600 590 & 2085 532 ±10 (17) 585 ±12(17) 550 ±10 (7) Concordia ages of the 579 ±4 (20) 585 ±3 (65) 638 ±8 (43) co her ent groups: 594 ±8 (34) 630 ±4 (31) 628 ±8 (13) 707 ±14 (17) (number of grains) 649 ±12 (17) 2624 ±24 (10) 2071 ±9 (12) Age spec trum % (number of grains) Si lu rian 416–444 Ma – – – – Or do vi cian 444–488 Ma 1.7% (n = 2) Cam brian 485–541 Ma 14.6% (n = 17) Ediacaran 541–635 Ma 80.6% (n = 87) 91.2% (n = 93) 26.7% (n = 31) 42.2% (n = 49) Cryogenian 635–720 Ma 13.9% (n = 15) 4.9% (n = 5) 38.8% (n = 45) 9.48% (n = 11) Tonian 720–1000 Ma 1.85% (n = 2) 0.98% (n = 1) 4.3% (n = 5) – Mesoproterozoic 1000–1600 Ma – 1.96% (n = 2) 1.7% (n = 1) 4.3% (n = 5) Paleoproterozoic 0.92% (n = 1) – 9.48% (n = 11) 27.6% (n = 32) 1600–2500 Ma Archean >2500 Ma – – 17.2% (n = 20) –

DISCUSSION same limit of 548 ±62 Ma of the youngest grains was ob tained af ter a chem i cal study of monazite (sam ple Potrójna IG 1 – A). The age of the youngest zir con clus ters cor re sponds per - AGE OF DEPOSITION fectly to the strati graphic po si tion of coarse-grained clastic beds in USB (Fig. 2), where con glom er ates oc cur lo cally, fill ing de - The re la tion ship be tween the youn gest de tri tal zir con and pres sion struc tures on the eroded Ediacaran sur face (Buła et de posi tion age de pends strongly on the tec tonic set ting of sedi - al., 2015). men tary ba sin (Dickinson and Gehrels, 2009; Cawood et al., An exam ple of pas sive tec tonic set ting is ob served in the 2012; Spencer et al., 2016). Geo chem i cal sig na ture of Edia - Batowice 2 con glom er ate (MB), where the sub si dence de vel op - caran sed i ments in USB (Żelaźniewicz et al., 2009) sug gests ment, ther mal his tory and crustal struc ture (includ ing the Kielce an ac tive tec tonic set ting con trolled by Cadomian orogenic pro - Re gion), point ing to a stable cratonic set ting dur ing Or do vi - cesses, with wide spread in tense magmatism and avail abil ity of cian-Si lu rian time (Narkiewicz, 2002). The pas sive tec tonic set - abun dant near-depositional-age grains, which is crit i cal to the ting is sug gested in de pendently on the basis a geo chem i cal ac cu racy of cal cu lated de po si tion age (Coutts et al., 2019). The stud ies of ma ture quartz sand stones of the Cam brian and Or - ef fec tive in di ca tor of the max i mum de po si tion time seems to be dovi cian sam ple set from MB (Nawrocki et al., 2007). Ma jor and a group of grains n >3 (Dickinson and Gehrels, 2009; Coutts et trace el e ment con tents doc u ment a pas sive con ti nen tal mar gin al., 2019); thus, this method was applied for the USB con glom - by means of the Th-Co-(Zr/10) plots of the Bhatia and Crook er ate, and the clus ter of youngest grains from each con glom er - (1986) dis crim i na tion di a gram. ate sam ple has been com pared. The con cordia ages from the The pas sive tec tonic set ting is char ac ter ized by lack of up per and lower Potrójna IG 1 sam ples at 544 ±6.6 Ma (n = 6) mag matic ac tiv ity. In con se quence, sed i men tary suc ces sions and 552 ±13 Ma (n = 4), re spec tively, and Raciechowice 1 at have no po ten tial rocks that could be a source of near- 547 ±21 Ma (n = 4) con firm the max i mum depositional age of depositional-age zir cons; thus, the youngest grains could to be the con glom er ate unit to be Late Ediacaran (Fig. 5A–C). The tens or hun dreds of mil lions of years older than the real time of Detri tal zir con age data from the con glom erates in the Up per Silesian and Małopolska blocks, and their im pli ca tions... 331

sed i ment ac cu mu la tion (Cawood et al., 2012), be cause the youn gest de tri tal grain clus ter de fines the last ig ne ous ac tiv ity. The con glom er ate sam ple taken from MB (Batowice 2 bore - hole) con tains Lower Pa leo zoic de tri tal ma te rial, in clud ing two Lower Or do vi cian grains (1.7%) ac com pa nied with sev eral Cam brian grains (14.6%), form ing a clus ter at 482 ±27 Ma. The same age range of the youngest de tri tal monazite pop u la tion (476 ±25 Ma) was obtained by in situ chem i cal geo chron ol ogy. These ages pro vided by detri tal zir cons and monazites do not rep re sent the maxi mum de posi tion time, but reflect the age of the youngest ig ne ous rocks that have con trib uted ma te rial to the sed i men tary ba sin in Batowice 2. There is no re cord of vol - ca nic ac tiv ity from the end of the Lud low ~432–425 Ma (Nawrocki et al., 2007; Krzemińska and Krzemiński, 2019).

DETRITAL ZIRCON GROUPS AND POTENTIAL SOURCES OF LITHOCLASTS

UPPER SILESIA BLOCK CONGLOMERATES

Two sam ples from the Potrójna IG 1 con glom er ate con tain mainly pebbles of eroded sed i ments or meta sedi ments (Fig. 3). Thus, de tri tal ma te rial was sup plied con trib uted to the sed i men - tary basin through recy cling of older sed i men tary rocks. A few groups of po ten tial sources (Fig. 7) have been rec og nized. The zir con grains with sim i lar U-Pb isoto pic ra tios cor re spond to the same or coeval source rocks. Most of detri tal zir cons, however, ex hibit os cil la tory zonings that reflect sim i lar mag matic source rocks, which were rap idly rew orked (Fig. 8A, B), and the age pat tern shows an almost unimodal age dis tri bu tion (Fig. 6A, B). In Potrójna IG 1 – A and Potrójna IG 1 – B, the major ity (81% and 91%) of zir con ages fall within one broad Ediacaran range with the peaks at 600 Ma (Fig. 6A) and 602 Ma (Fig. 6B), re- spec tively. This in sig nif i cant dif fer ence re flects a sim ple ten - dency of the ac cu mu la tion of slightly youn ger de tri tal ma te rial in the up per most part of the Potrójna IG 1 con glom er ate bed. The ma jor ity of clasts were sup plied from two Cadomian sources, where the magmatism was cu mu lated at 580–585 and at 627–630 Ma. It sug gests that the protolith may repre sent the same Cadomian orogenic set ting. In such dynamic con di tions, the re cy cling pro cesses may pro ceed im me di ately dur ing a rel - atively short time, which is obvi ous in case of im ma ture greywacke-type depos its. Within a vol ca nic is land-arc set ting, iso lated from con ti nen tal in put (e.g., fore-arc/back-arc), uni - modal pat terns of detri tal zir con ages are prev alent and re flect the main time of magmatic ac tiv ity (Cawood et al., 2012). Sim i lar unimodal de tri tal zir con age spec tra for three sand - stone sam ples with age max ima at 600 or ~650–660 and ~558 Ma (with lack of Pa leo zoic zir cons) are cur rently re ported from Basal Clastics close the Brno area of the west ern part of BVT (Timmerman et al., 2019). A dis tinct age dis tri bu tion was de ci phered from the east ern - most part of USB (Fig. 5C) in the Raciechowice 1 bore hole (Ta - ble 2). The first two clusters (Fig. 7C), cor re spond to the groups iden ti fied in Potrójna, and they were sup plied from rel atively uni- form Cadomian source rocks. The third one, with Cryogennian

Fig. 4. Tera-Wasserburg con cordia dia grams of all accepted ages of de tri tal zir con grains from con glom er ate sam pled in the Potrójna IG 1, Raciechowice 1 and Batowice 2 bore holes

Uncer tain ties are shown at the 2s level 332 Ryszard Habryn, Ewa Krzemińska, Leszek Krzemiński, Marek Markowiak and Grzegorz Zieliński

zir con ages in a range of 740–704 Ma, prob ably reflect a more dis tal equiv alent of the Cen tral Ba sic Belt (CBB) with mafic and fel sic volcanites in a range of 733 ±5 Ma – 728 ±5 Ma (Hanžl et al., 2019). The CBB was in ter preted as a dis mem bered ophiolite with both plutonic and vol ca nic mem bers. Apart from meta-tuffs of metadiabases, dykes of meta-rhyo lite 725 ±15 Ma and meta-dolerite are most abundant in the east ern part of CBB (Fin ger et al., 2000). The last prom i nent group is formed by Neoarchean grains (17%) which most prob ably reflect ero sion of the rocks found in the Paleoproterozoic Rzeszotary Horst (RzH), where some zir - cons yielded 207Pb/206Pb ages in a range of 2.5–2.7 Ga (Bylina et al., 2000; Żelaźniewicz and Fan ning, 2020). A few old est de - tri tal zir cons (Fig. 8C) show a banded zon ing, which is com mon for crystal li za tion from a mafic melt. The age spec tra de ci phered in the Raciechowice con glom - er ate are com pat i ble with those iden ti fied in fine-grained sed i - ments from the Cadomian Orogen in the NE Bo he mian Mas sif (Linnemann et al., 2014), where the West Af ri can prov enance was con sid ered. This gen eral sug ges tion may also have im pli - ca tions for the enig matic or i gin of the RzH as an exotic com po - nent hosted in the ju ve nile Cadomian struc ture of USB. The com pi la tion of age data (Ta ble 1) from sev eral units within BVT, in clud ing the Brno Block of 600.9 ±2.8 Ma, Svratka Dome of 634 ±6 Ma, Thaya Unit of 603.3 ±5.2 Ma, and Slavkov Unit of 575 ±2 Ma, with granitoids emplaced at 606 ±2 Ma – 590 ±8 Ma (Friedl et al., 2004; Soejono et al., 2017 and ref er ences therein; Svojtka et al., 2017; Timmerman et al., 2019), sup - ported by mag matic ages obtained from the hid den area of the Bielsko-Biała Dome (Fig. 1B), in Roztropice at 582.7 ±6 Ma and Kęty-8 at 579 ±2.7 Ma (Żelaźniewicz et al., 2009), shows the main pulses of ig neous ac tiv ity (Fig. 9) within the com pos ite BVT. These stages well match to the age of clastic com po nents de ci phered from the Potrójna and Raciechowice 1 con glom er - ates, con firm ing that nearly all mate rial was sup plied from denu - dation of the lo cal Cadomian source rocks.

MAŁOPOLSKA BLOCK CONGLOMERATE

The clastic ma te rial in the Batowice 2 con glom er ate rep re - sents eroded plutonic and vol ca nic rocks or their meta-equiv a - lents. The youngest zir con group is com posed of two Lower Or - dovi cian grains (1.7%). Their form, lim ited amount, and age of 482 ±27 Ma (Fig. 8D, grain 103.1) sug gest pyroclastic or i gin. The traces of Or dovi cian to Si lu rian vol ca nic pulses are wide - spread in MB of the Holy Cross Moun tains (Trela et al., 2018) and rep re sented by ben ton ite ho ri zons with pyroclastic ma te rial derived by winds from Avalo nian vol ca noes. The dis tri bu tion of pyroclastic flow in MB dur ing Late Or do vi cian time was strongly con trolled by SE trade winds (Trela et al., 2017). The prov e nance of dom i nant pebblesderived from po ten - tially proxi mal crys tal line rocks seems to be more com plex to deci pher, be cause base ment rocks of MB re main un known. The or i gin of MB and its re la tion ship to the adja cent blocks is a sub ject of ongo ing de bate (Belka et al., 2000; Valverde- Vaquero et al., 2000; Narkiewicz, 2002; Żelaźniewicz et al., 2009; Narkiewicz et al., 2011; Walczak and Belka, 2017). The

Fig. 5. Wetherill con cordia di a grams for the youngest de tri tal zir con grains (n >3) that overlap in age at 2s

A – Potrójna IG 1– A, B – Potrójna IG 1 – B, C – Raciechowice 1, D – Batowice 2 Detri tal zir con age data from the con glom erates in the Up per Silesian and Małopolska blocks, and their im pli ca tions... 333

proxim ity of MB and Baltica dur ing Cam brian time was con cluded on the ba sis of sim i lar ity of palaeomagnetic poles of MB ver sus EEC (Nawrocki et al., 2007). The close re la tion ships to Amazonia were re ported on the basis of Nd data of de tri tal sed i ments com bined with de tri tal zir con ages (Belka, 2000; Walczak and Belka, 2017). Thus, it was ac cepted that, dur ing Cam brian time, MB was sup plied with clastic mate rial from (I) Am a zo nian sources, be ing also pro gres sively sourced from (II) the Baltica Svecofennian crust since the Mid dle Cam brian (Walczak and Belka, 2017). The link ages from MB to Baltica and West Gond - wana were con sid ered af ter re-eval u a tion of Cam - brian tri lo bite fauna from MB (Żylińska and Szcze - panik, 2009; Żylińska, 2013). In con se quence, the accrectionary his tory of MB con strained on these fau - nal re cords, com pleted by detri tal mica sig na tures (Belka et al., 2000), point out that MB and Baltica were still not con nected in the Early Cambrian, but a lim ited mi gra tion of fau nal spe cies was pos si ble. In the Mid- Cam brian, the dis tance be came smaller. Thus, the fau nal re cord has been in te grated and fine-grained clastic ma te rial from Baltica was suc cess fully supplied to MB (Belka et al., 2000). At the end of the Ediacaran, the NW mar gin of Baltica changed its tec tonic re gime from extensional to ac tive mar gin (Timanian Orog - eny). Later, in Mid dle Cam brian to Mid dle Or dovi cian times, the Baltica un der went a sub stan tial ro ta tion of ~120°, with a max i mum rate in Late Cam brian and Early Or do vi cian times (Cocks and Torsvik, 2005). Af ter the Late Or dovi cian, when the Batowice conglometare was de pos ited (the youngest de tri tal grain of 482 Ma), the MB mar gin must have been closer to the Baltica mar gin, but since Neoproterozoic time, Amazonia had been grad ually sepa rated from Baltica (Johansson, 2009). Be cause both blocks were pre vi ously closely com bined to at least 0.8 G, the main crust for ma tion stages rec ognized in Amazonia per - fectly match the stages known from ad equate belts of Baltica (Johansson, 2009). One of the hypoth esis as sumes that MB must have docked to the Fennoscandian seg ment of Baltica, along the TTZ mar gin, be ing af ter wards prob - ably alw ays located near its pres ent po si tion (Belka et al., 2002). As sig nif i cant ev i dence the age of ~2.0 Ga known from Kędziorka, MB (Belka et al., 2002) or from Wymyślona 2037–2079 Ma (Valverde-Vaquero et al., 2000) are in di cated. In both cases the de tri tal ma te rial was prob ably supplied from the Svecofennian part of Baltica up to in the Mid dle Cam brian (Walczak and Belka, 2017). The detri tal zir cons in a range 2.1–2.0 Ga, ob - served in the Batowice con glom er ate (Fig. 10A), but

Fig. 6. The com par i son of de tri tal zir con age spec tra from con glom er ate sam ples, show ing the dis tri bu tion of dom i nant grains The curves are proba bil ity plots ac com panied with his to- grams, con strained on 206Pb/238U ages up to 1000 Ma and 206Pb/207Pb ages if the 206Pb/238U ages are older than 1000 Ma; the num ber of detri tal zir con grains ana lysed is shown on the left; the scale of verti cal and hor i zon tal axes is nor - mal ized 334 Ryszard Habryn, Ewa Krzemińska, Leszek Krzemiński, Marek Markowiak and Grzegorz Zieliński

Fig. 7. Con cordia di a grams show ing well-de fined de tri tal zir con clus ters that may cor re spond to the age of po ten tial source rocks

A – Potrójna IG1, B – Raciechowice 1, C – Batowice 2, in clud ing old est com po nents

de scribed also in Cam brian sand stone of MB (Belka et al., the fine-grained sed i ments, where a long dis tance trans port is 2002), could not have come from a Svecofeninan source, be- nec es sary, a num ber of pos si bil i ties for prev enance in ter pre ta - cause the time of ac tiv ity of this orog eny (Korja et al., 2006) was tion. The con glom er ates as coarse-grained de pos its are a re - spanned be tween 1.9 and 1.8 Ga (1.92–1.88, 1.87–1.84, sult of short trans port, e.g. tens to hun dreds of kilo metres, thus 1.87–1.79, and 1.79–1.77 Ga). Thus, the popu la tion of 2.1–2.0 re flect mostly prox i mal sources. Ga re flects un doubt edly an older source. Such a pre-Sveco - As an ex am ple of a prox i mal de po si tion nearby source area fennian crust was pres ent only in north ern Fin land or in the the con glom er ate from Kaplonosy IG 1 at a depth of 1809 m Sarmatian part of Baltica and in the Volga Ural Block. In case of (Ap pen dix 1) is pre sented. This coarse-grained clastic rock was De tri tal zir con age data from the con glom erates in the Up per Silesian and Małopolska blocks, and their im pli ca tions... 335

Fig. 8. Cathodoluminescence (CL) im ages of the col lec tion of pol ished zir con grains in ep oxy mount; images show ing ana lysed detri tal zir con grains from conglom er ates of A – Potrójna IG 1 – A, B – Potrójna IG 1 – B, C – Raciechowice 1, D – Batowice 2

The age and ID of anal ysis are shown (for more details see Appen dix 1); the CL im ages were acquired in the same mag ni fi ca tion, bright ness and con trast con di tions to com pare the in ternal fea tures of in di vid ual grains and sam ples 336 Ryszard Habryn, Ewa Krzemińska, Leszek Krzemiński, Marek Markowiak and Grzegorz Zieliński

Fig. 9. The com par i son of de tri tal zir con ages ob tained as main clus ters ob tained from conglom er ates of the Up per Silesia and Małopolska blocks (this study) and their po ten tial sources The U-Pb zir con con cordia age com pi la tion in cludes a Cadomian orogenic im prints in the Moldanubian Zone; moreover a proxi mal source rocks from the com pos ite Brunovistulia Terrane, includ ing the Up per Silesian and Brno blocks, Thaya, Slavkov and Strzelin units and volcanogenic re cord known from the Małopolska Block and from Baltica rep resented by Volyn-Orsha Aulacogen vol ca nic ac tiv ity; ages ob- tained from xeno liths and olistoliths of the Outer Carpatian flysch are plot ted sep arately. Detri tal age re cord marked by dia mond, in con trast to mag matic ages marked by square; data for compar i son are taken from: Compston et al. (1995); Oberc-Dziedzic et al. (2003); Teipel et al. (2004); Linnemann et al. (2007); Żelaźniewicz et al. (2009), Shumlyanskyy et al. (2016), Soejono et al. (2017); Svojtka et al. (2017); Poprawa et al. (2018); Hajná et al. (2018); Burda et al. (2019); Gawęda et al. (2019); Timmerman et al. (2019) de pos ited in Meso/Neoproterozoic time di rectly on the eroded Lewandowski (1993) and Nawrocki et al. (2004, 2007). There - base ment of the Baltica pas sive mar gin near the Fenno - fore, the clastic ma te rial with pre-Svecofennian Paleopro tero - scandia -Sarmatia su ture. The dom i nant de tri tal zir cons peaked zoic (2.1–2.0 Ga) sig nature, wide spread in the SW Sarmatian at ~1535 Ma were de liv ered from AMCG or/and rapakivi-type edge, may strengthen this hypoth esis. In this model, the MB rocks (Fig. 10C), which are wide spread in the Mazury Com plex. was de vel oped near the pres ent-day south ern mar gin of Baltica A mi nor Sveconennian group at ~1818 Ma may reflect an ero - and has been dextrally re lo cated along the TTZ edge of Baltica. sion event of the Svecofennian part of base ment, in clud ing the The ab sence of the ~1.0–1.2 Ga (Sveconorwegian) com po - near est Mazowsze Do main (Krzemińska, 2010). Almost the nent in Batowice 2, which is known only from south ern Scan di - same age pat tern with a prom i nent rapakivi-de rived sig nal (Fig. na via, re af firms this in ter pre ta tion. 10D) was rec og nized in the up per most Ediacaran fine-grained An other prom i nent group is the pop u la tion (Fig. 7) of Up per sand stone from Białopole IG 1 (Żelaźniewicz et al., 2009) south Ediacaran/Early Cam brian de tri tus formed by grains in a range of Kaplonosy IG 1 (Fig. 1A). These sim i lar i ties sug gest that the of 534–506 Ma, which yielded a concordia age at 532 ±10 Ma. source area re mained more or less un changed over that time. In gen eral, dur ing a time span of 570–530 Ma, a num ber of im - In case of the Batowice 2 con glom er ate, the clasts must por tant mani fes ta tions of ac tiv ity are widely noted as PanAfri - have been de rived from a def i nitely distinct area, or dif fer ent can, Bra zil ian, Baikalian, Timanian and Cadomian oro genies. Baltica’s mar gin, be cause the grains of 1.5 and 1.8 Ga are rel a - Thus, an im por tant pop ula tion with a max i mum at 532 ±10 Ma tively rare (Fig. 10), in con trast to a sig nif i cant zir con clus ter of can be con sid ered as a Late Cadomian sig nature and in put of pre-Svecofennian grains of ~2.1–2.0 Ma. The poten tial Paleo - eroded prox i mal Cadomian crust. Ig ne ous rocks of this age re - proterozoic 2.1–2.0 Ga source rocks are known from the flect a late stage of con ti nen tal arc magmatism along the north - Sarmatian seg ment of EEC (Shumlyanskyy et al., 2015). They ern mar gin of Gond wana and the on set of rift ing and wide - in clude gran ites of the Zhytomyr and Osnitsk com plexes (north - spread magmatism (~530–500 Ma) that led to the open ing of west ern part of Sarmatia) and o the Orekhiv-Pavlograd, Krivyy the Rheic Ocean (Linnemann et al., 2008). Rih and Golovanivsk sub-do mains of the Ukrai nian Shield, A Gondwanan or i gin of the MB was con cluded pre vi ously where the con ti nen tal crust was formed dur ing two orogenic from de tri tal micas and zir con ages from Cam brian sed i ments events at ~2100–2050 Ma and 2000–1950 Ma (Shumlyanskyy and Cam brian brachi o pods (Belka et al., 2002; Winchester et et al., 2015). There is also the East-Sarmatian Orogen that al., 2002). In a palaeoreconstruction proposed by Nawrocki et formed through the col li sion be tween Sarmatia and Volgo - al. (2004), the MB was consid ered as a part of the Cadomian -Uralia at ~2.1–2.0 Ga (Terentiev et al., 2016). Dock ing of MB belt lo cated near the pres ent-day south east ern mar gin of at the south ern, Sarmatian mar gin of Baltica was pro posed by Baltica, which must have been trans ferred to its pres ent po si - Detri tal zir con age data from the con glom erates in the Up per Silesian and Małopolska blocks, and their im pli ca tions... 337

Fig. 10. The compar i son using: A – schematic loca tion of the Fennoscandia, Sarmatia and Volgo-Uralia blocks within the Baltica palaeocontinent (af ter Gorbatschev and Bogdanova, 1993); B – main crust for ma tion events from the Am a zon Craton (ac cord ing to Nance and Murphy, 1996); C – de tri tal age spec trum of the Kaplonosy con glom er ate (Żukow Fm.), which re flects the age of eroded base ment near the TTZ Baltica mar gin; D – de tri tal age spec trum of Up per Ediacaran fine-grained sed i ments from Białopole, re flect ing the age of de tri tus near the TTZ Baltica magin, data from Żelaźniewicz et al. (2009); E – detri tal zir con age spectrum charac ter is tic for the Batowice 2 conglom er ate (MB); F – compi la tion of detri tal age data collected from Late Ediacaran fine-grained sed iments from the Małopolska Block margin, samples: Tuligłowy, Chałupki Dębiańskie, BN58, Zalasowa and Żarki, (data taken from Żelaźniewicz et al., 2009) tion in lat est Ediacaran to Late Cam brian times. There fore, a tectono-sed i men tary in ter ac tions be tween both the blocks than de tri tal zir con pat tern pro vided by the Batowice 2 con glom er ate those pro vided pre vi ously by in ves ti ga tion of fine-grained sed i - from the edge of MB may reflect a com mu ni ca tion only betw een ments (Fig. 10F). The age of main peaks is marked. the mar gins of Gond wana (Late Cadomian clasts) and south ern The di agrams were constrained on 206Pb/238U ages up to Baltica (pre-Svecofennian clasts). These ev i dences, provided 1000 Ma, and 206Pb/207Pb ages if the 206Pb/238U ages are older by prox i mal de pos its, in di cate more di rectly the close spatial than 1000 Ma. 338 Ryszard Habryn, Ewa Krzemińska, Leszek Krzemiński, Marek Markowiak and Grzegorz Zieliński

CONCLUDING REMARKS 707 ±14 Ma. All these plutonic-vol ca nic events were iden - ti fied else where within BVT; The first SHRIMP U-Pb de tri tal zir con age rec ogni tion of 4 – the age of older com ponents of 2624 ±24 Ma (Neo - con glom er ates from the Potrójna IG 1 (near the Bielsko-Biała archean), re flect ing ero sion of the lo cal base ment (Racie - Dome) and Raciechowice 1 (Rzeszotary Horst) bore holes in cho wice 1), un equiv ocally related to the Rzeszotary Horst; the Up per Silesia Block, and from the Batowice 2 bore hole in 5 – the ages of zir con grains de rived from plutonic and vol - the Małopolska Block (close to the Kraków-Lubliniec Fault ca nic lithoclasts of the Batowice 2 (MB) con glom er ate of Zone), us ing an ad equate num ber of anal yses (n >100) for 532 ±10 Ma, 551 ±16 Ma, 594 ±8 Ma and 649 ±12Ma, ac - each sam ple, points to as fol lows: com pa nied with the char ac ter is tic pre-Svecofennian 1 – the youngest zir con age of 549 Ma for both (Potrójna IG group peaked at 2071 ±10 Ma, may docu ment a tectono - 1, Raciechowice 1) con glom er ates in USB con firms their -sed i men tary in ter ac tion be tween the Gond wana and Lat est Ediacaran age of de posi tion; Baltica palaeocontinets dur ing Early Paleo zoic time. 2 – the youngest zir con age of 482 Ma for Batowice 2 in MB does not al low for pre cise de ter mi na tion of de po si tion Ac knowl edge ments. This work was made pos si ble through age, sug gest ing rather a lag time. fund ing from the Min is try of Sci ence and Higher Ed uca tion 3 – the dom i nant clus ters of zir con ages of 579 ±4, 585 ±3 PGI-NRI in ter nal grant No 61.2501.1201.00.0 led by R. Habryn. and 628 ±8, 630 ±4 and 638 ±8 Ma from the Potrójna IG 1 The re sults ob tained dur ing the pro ject 61.2901.1502.00, task and Raciechowice 1 (USB) bore holes are in ter preted as No 4, con ducted by E. Krzemińska, were also used. M. Recho - an age of prox i mal source rocks, which is con sis tent with wicz is thanked for zir con sep ara tion and mount prep ara tion. An - the dis tri bu tion of Cadomian magmatism within the near - a lyt i cal as sis tance with the SHRIMP IIe/MC cal i bra tion pro ce - est orogenic belt, in clud ing those pre vi ously obtained in dure was pro vided by Z.J. Czupyt. The authors would like to ac - the Kęty-8 (579 ±2.7 Ma) and Roztropice (582.7 Ma) knowl edge two anon y mous re view ers for their crit i cal com ments bore holes, and less com mon Early Cadomian ep i sode of that helped to im prove the pa per sub stan tially.

REFERENCES

Bassett, K.N., 2000. Iso to pic prov e nance anal y sis and terrane tec - zoicznego podłoża (in Pol ish). Przewodnik 76 Zjazdu Polskie- tonics: a warning about sed i ment trans port dis tances. In: Un der- go Towarzystwa Geologicznego, Rudy k/Rybnika: 14–42. stand ing Planet Earth: search ing for a sus tain able fu ture (eds. Warszawa. C. Skilbeck, and T.C. Hubble). Ab stracts of the 15th Aus tralian Buła, Z., Żaba, R., 2008. Struc ture of the Precam brian base ment of Geo log i cal Con ven tion. Uni ver sity of Tech nol ogy, Syd ney, the east ern part of the Upper Silesia block (Brunovistulicum) (in NSW, Aus tra lia. Pol ish with Eng lish sum mary). Przegląd Geologiczny, 56: Belka, Z., Ahrendt, H., Franke, W., Wemmer, K., 2000. The 473–480. Baltica-Gond wana su ture in Central Eu rope; ev i dence from Buła, Z., Jachowicz, M., Żaba, J., 1997. Prin ci pal char ac ter is tics of K-Ar ages of de tri tal mus co vites and biogeographical data. the Upper Silesian Block and Małopolska Block bor der zone Geo log i cal So ci ety Spe cial Pub li ca tions, 179: 87–102. (south ern Po land). Geo log i cal Mag a zine, 134: 669–677. Belka, Z., Valverde-Vaquero, P., Dörr, W., Ahrendt, H., Wemmer, Buła, Z., Żaba, J., Habryn, R., 2008. Tec tonic sub di vi sion of Po land K., Franke, W., Schaefer, J., 2002. Ac cre tion of first Gond wana (Up per Silesian Block and Małopolska Block) (in Polish with – de rived ter ranes at the mar gin of Baltica. Geo log i cal So ci ety Eng lish ab stract). Przegląd Geologiczny, 56: 912–920. Spe cial Pub li ca tions, 201: 19–36. Buła, Z., Habryn, R., Jachowicz-Zdanowska, M., Żaba, J., 2015. Bhatia, M.R., Crook, K.A., 1986. Trace el e ment char ac ter is tics of Precam brian and Lower Paleo zoic of the Brunovistulicum (east - graywackes and tec tonic set ting, dis crim i na tion of sed i men tary ern part of the Upper Silesian Block, southern Poland) – the bas ins. Con tri bu tion to Min er al ogy and Pe trol ogy, 90: 181–193. state of the art. Geolog i cal Quarterly , 59 (1): 123–134. Black, L.P., Kamo, S.L., Allen, C.M., Dav is, D.W., Aleinikoff, J.N., Burda, J., Woskowicz-Ślęzak, B., Klötzli, U., Gawęda, A., 2019. Val ley, J.W., Mundil, R., Campbell, I.H., Korsch, R.J., Wil- Cadomian protolith ages of ex otic mega blocks from Bugaj and liams, I.S., Foudoulis, C., 2004. Im proved 206Pb/238U micro- Andrychów (West ern outer Carpathians, Po land) and their probe geo chron ol ogy by the mon i tor ing of a trace-el e ment-re- palaeogeographic sig nif i cance. Geochronometria, 46: 25–36. lated ma trix ef fect; SHRIMP, ID–TIMS, ELA–ICP–MS and ox y- Bylina, P., Żelaźniewicz, A., Dörr, W., 2000. Archean base ment in gen iso tope doc u men ta tion for a se ries of zir con stan dards. the Up per Silesia Block: U-Pb zircon age from am phi bo lites of Chem i cal Ge ol ogy, 205: 115–140. the Rzeszotary horst. Ab stracts, Joint Meet ing EUROPROBE Buła, Z., 2000. The Lower Palaeozoic of the Up per Silesia and West and PACE pro jects, Zakopane: 11–12. Małopolska (in Pol ish with Eng lish sum mary). Prace Cathelineau, M., 1988. Cation site oc cu pancy in chlorites and illites Państwowego Instytutu Geologicznego, 171: 1–63. as a func tion of tem pera ture. Clay Miner als, 23: 471–485. Buła, Z., Habryn, R. eds., 2008. Geo log i cal-struc tural at las of the Cathelineau, M., Nieva, D., 1985. A chlorite solid solu tion Palaeozoic base ment of the Outer Carpathians and Carpathian geothermometer. The Los Azufres (Mex ico) geo ther mal sys tem. Foredeep. Państwowy Instytut Geologiczny, Warszawa. Con tri bu tion to Min er al ogy and Pe trol ogy, 91: 235–244. Buła, Z., Habryn, R., 2011. Precam brian and Palaeozoic base ment Cawood, P.A., Hawkesworth, B., Dhuime, B., 2012. Detri tal zircon of the Carpathian foredeep and the ad ja cent Outer Carpatians record and tectonic setting. Geol ogy , 40: 875–878. (SE Po land and Western Ukraine). Annales Societatis Cebulak, S., 1958. Zlepieńce paleozoiczne w Batowicach koło Geologorum Poloniae, 81: 221–239. Krakowa (in Polish). Przegląd Geologiczny, 6: 395–396. Buła, Z., Jachowicz, M., 1996. The lower Palaeozoic sed i ments in Cocks, L.R.M., Torsvik, T.H., 2005. Baltica from the late Pre cam - Up per Silesia Block. Geo log i cal Quar terly, 40 (3): 299–336. brian to mid-Palaeozoic times: the gain and loss of a terrane’s Buła, Z., Żaba, J., 2005. Pozycja tektoniczna Górnośląskiego Za - iden tity. Earth-Sci ence Re views, 72: 39–66. głębia Węglowego na tle prekambryjskiego i dolno paleo - Detri tal zir con age data from the con glom erates in the Up per Silesian and Małopolska blocks, and their im pli ca tions... 339

Compston, W., Sambridge, M.S, Reinfrank, R.F., Moczy - with English sum mary). Biuletyn Państwowego Instytutu. Geolo - dłowska, M., Vidal, G., Claesson, S., 1995. Nu mer i cal ages of gicznego, 459: 61–82. vol ca nic rocks and the earli est faunal zone within the Late Pre - Jaworowski, K., Sikorska-Jaworowska, M., 2006. Łysogóry Unit cam brian of east Po land. Jour nal of the Geolog i cal So ci ety, 152: (Central Poland) ver sus East Eu ro pean Craton: ap pli ca tion of 599–611. sedimentological data from Cam brian siliciclastic as so ci a tion. Coutts, D.S., Mattiews, W.A., Hubbart, S.M., 2019. As sess ment of Geo log i cal Quar terly, 50 (1): 77–88. widely used meth ods to de rive depositional ages from de tri tal Johansson, A.E., 2009. Baltica, Amazonia and the SAMBA con - zir con pop u la tions. Geoscience Frontiers, 10: 1421–1435. nec tion – 1000 mil lion years of neighbour hood during the Pro - Dadlez, R., Narkiewicz, M., Stephenson, R.A., Visser, M.T.M., tero zoic? Pre cam brian Re search, 175: 221–234. van Wees, J.-D., 1995. Tec tonic evo lu tion of the Mid-Pol ish Kalvoda, J., Babek, O., Fatka, O., Leichmann, J., Melichar, R., Trough: mod el ling im pli ca tions and sig nif i cance for cen tral Eu - Nehyba, S., Spacek, P., 2008. Brunovistulian terrane (Bohe - ro pean ge ol ogy. Tectonophysics, 252: 179–195. mian Mas sif, Cen tral Eu rope) from late Protero zoic to late Pa - Dadlez R. 2001. Holy Cross Mts. area — crustal struc ture, geophys - leo zoic: a re view. In terna tional Jour nal of Earth Sci ences, 97: i cal data and gen eral ge ol ogy. Geo log i cal Quar terly, 45 (1): 497–518. 99–106. Kodama, Y., 1994. Downstream changes in the li thol ogy and grain Dadlez, R., Grad, M., Guterch, A., 2005. Crustal struc ture below size of fluvial grav els, the Watarase River, Ja pan: ev i dence of the Pol ish Ba sin: is it com posed of proxi mal ter ranes de rived the role of abrasion in down stream fin ing. Jour nal of Sed i men - from Baltica? Tectonophysics, 411: 111–128. tary Research, A64: 68–75. Dickinson, W.R., Gehrels, G.E., 2009. Use of U-Pb ages of de tri tal Konior, K., 1974. Geo log i cal struc ture of Rzeszotary ele va tion in zir cons to in fer max i mum depositional ages of strata: a test the light of re cent geo physi cal and drill ing data (in Pol ish with against a Col o rado Pla teau Me so zoic da ta base. Earth and Eng lish sum mary). Annales Societatis Geologorum Poloniae, Plan e tary Sci ence Let ters, 288: 115–125. 44: 321–375. Dudek, A., 1980. The crys tal line base ment block of the Outer Korja, A., Lahtinen, R., Raimo, T., Nironen, M., 2006. The Carpathians in Moravia: Bruno-Vistulicum. Rozpravy Česko- Svecofennian orogen: a col lage of microcontinents and is land -Slovenské Akademie Věd, Řada Matematicko -přírodních Věd., arcs. Geo log i cal So ci ety Mem oirs, 32: 561–578. 90: 1–85. Kozłowski, W., Domańska-Siuda, J., Nawrocki, J., 2014. Geo- Fer gu son, R., Hoey, T., Wathen, S., Werritty, A., 1996. Field ev i - chemis try and petrol ogy of the upper Silu rian greywackes from dence for rapid downstream fin ing of river grav els through se - the Holy Cross Moun tains (cen tral Po land): im pli ca tions for the lec tive trans port. Ge ol ogy, 24: 179–182. Cal edo nian his tory of the south ern part of the Trans-Eu ropean Fin ger, F., Tichomirowa, M., Pin, C., Hanžl, P., 2000. Relics of Su ture Zone (TESZ). Geo log i cal Quar terly, 58 (2): 311–336 early-Panafrican metabasite – metarhyolite forma tion in the Kranidiotis, P., MacLean, W.H., 1987. Sys tem at ics of chlorite al ter- Brno Mas sif, Moravia, Czech Re pub lic. In ter na tional Jour nal of ation at the Phelps Dodge mas sive sul fide de posit, Matagami, Earth Sci ences, 89: 328–335. Que bec. Eco nomic Ge ol ogy, 82: 1898–1911. Friedl, G., Finger , F., Paquette, J.L., von Quadt, A., McNaughton, Kröner, A., Štěpská, P., Schulmann, K., Jaeckel, P., 2000. Chro- N., Fletcher, I.R., 2004. Pre-Variscan geolog i cal events in the nolog i cal constraints on the pre-Variscan evo lu tion of the north - Aus trian part of Bohe mian Mas sif de duced from U-Pb zir con east ern margin of the Bo he mian Mas sif, Czech Re pub lic. Geo - ages. In terna tional Jour nal of Earth Sci ences, 93: 802–823. log i cal So ci ety Spe cial Pub li ca tions, 179: 175–197. Gawęda, A., Golonka, J., Waśkowska, A., Szopa, K., Chew, D., Krzemińska, E., 2010. Geochem i cal and isoto pic recon struc tion of Starzec, K., Wieczorek, A., 2019. Neoproterozoic crys tal line the tec tonic set ting of the Mazowsze Domain in the Pre cam brian ex otic clasts in the Pol ish Outer Carpathian flysch: remnants of base ment of north-eastern Poland (in Pol ish with Eng lish sum - the Proto-Carpathian con ti nent? In ter na tional Jour nal of Earth mary). Prace Państwowego Instytutu Geologicznego, 195: Sci ences, 108: 1409–1427. 5–57. Gehrels, G., 2012. De tri tal Zir con U-Pb Geo chron ol ogy: cur rent Krzemińska, E., Krzemiński, L., 2019. Mag matic ep i sodes in the Meth ods and New Op por tu ni ties. In: Tec ton ics of Sed i men tary Holy Cross Mountains, Po land – new contri butions from Bas ins: Re cent Ad vances (eds. C. Busby and A. Azor): 45–62. multi-age zir con pop ula tions (in Eng lish with Pol ish sum mary). Blackwell Pub lish ing Ltd. Biuletyn Państwowego Instytutu Geologicznego, 474: 43–58. Gorbatschev, R., Bogdanova, S.V., 1993. Frontiers in the Bal tic Lewandowski, M., 1993. Paleomagnetism of the Pa leo zoic rocks of Shield. Precam brian Research , 64: 3–21. the Holy Cross Mts (Cen tral Po land) and the ori gin of the Habryn, R., Buła, Z., Nawrocki, J., 2014. The Kraków sec tor of the Variscan orogen. Pub li ca tions of the In sti tute of Geo phys ics, Kraków-Lubliniec tec tonic zone in the light of data ob tained from Pol ish Academy of Sciences A23, 265: 3–85. new boreholes of Trojanowice 2 and Cianowice 2 (in Polish with Linnemann, U., 2007. Ediacaran rocks from the Cadomian base - Eng lish sum mary). Biuletyn Państwowego Instytutu Geolo - ment of the Saxo-Thuringian Zone (NE Bohe mian Mas sif, Ger- gicznego, 459: 45–60. many): age constraints, geotectonic set ting and ba sin de vel op - Hajná, J., Žak, W., Dörr, V., Kachlík, J., Sláma, J., 2018. New con- ment. Geo log i cal So ci ety Spe cial Pub li ca tions, 286: 35–51. straints from de tri tal zir con ages on pro longed, multiphase tran- Linnemann, U., Gerdes, A., Drost, K., Buschmann, B., 2007. The si tion from the Cadomian accretionary orogen to a pas sive mar - con tin uum be tween Cadomian orogen esis and open ing of the gin of Gond wana. Precam brian Re search, 317: 159–178. Rheic Ocean: con straints from LA-ICP-MS U-Pb zir con dat ing Hanžl, P., Janousek, V., Soejono, I., Burianek, D., Svojtka, M., and anal ysis of plate-tec tonic set ting (Saxo-Thuringian zone, Hrdlickova, K., Erban, V., Pin, Ch., 2019. The rise of the north east ern Bo he mian Mas sif, Ger many). GSA Spe cial Pa per, Brunovistulicum: age, geo log i cal, pet ro log i cal and geo chem i cal 423: 61–96. char ac ter of the Neoproterozoic mag matic rocks of the Central Linnemann, U., Gerdes, A., Hofmann, M., Marko, L., 2014. The Ba sic Belt of the Brno Mas sif. In ter na tional Jour nal of Earth Sci - Cadomian Orogen: Neoproterozoic to Early Cambrian crustal ences, 108: 1165–1199. growth and orogenic zoning along the pe riph ery of the West Afri - Heflik, W., Konior, K., 1972. Up per Si lu rian con glom er ates in the can Craton – Con straints from U-Pb zir con ages and Hf iso topes profile of the bore hole Raciborsko 2 south-west of Wieliczka (in (Schwarzburg Antiform, Germany ). Precam brian Research, Pol ish with Eng lish sum mary). Annales Societatis Geologorum 244: 236–27. Poloniae, 42: 327–346. Łydka, K., Siedlecki, St., Tomczyk, H., 1963. On the Mid dle Jachowicz-Zdanowska, M., 2011. Or ganic microfossil assem - Ludlovian con glom erates in the Cra cow Region. Bul le tin of the blages from the late Ediacaran rocks of the Małopolska Block, Pol ish Acad emy of Sci ences, Se ries Ge ol ogy et Ge og ra phy, 11: south east ern Po land. Geo log i cal Quar terly, 55 (1): 85–94. 93–99. Jachowicz-Zdanowska, M., 2014. The Terreneuvian and Late Malinowski, M., Żelaźniewicz, A., Grad, M., Guterch, A., Janik, Ediacaran organic microfossils from the Kraków area (in Pol ish T., CELEBRATION 2000 Working Group, 2005. Seismic and 340 Ryszard Habryn, Ewa Krzemińska, Leszek Krzemiński, Marek Markowiak and Grzegorz Zieliński

geolog i cal struc ture of the crust in the tran si tion from Baltica to Pożaryski, W., Grocholski, A., Tomczyk, H., Karnkowski, P., Palaeozoic Eu rope in SE Po land – CELEBRATION 2000 exper i - Moryc, W., 1992. The tec tonic map of Po land in the Variscan ep- ment, profile CEL02. Tectonophysics, 401: 55–77. och (in Pol ish with Eng lish sum mary). Przegląd Geologiczny, Mazur, S., Jarosiński, M., 2006. Deep base ment struc ture of the 40: 643–651. Pa leo zoic plat form in SW Po land in the light of POLONAISE-97 Salwa, S., Trela, W., 2019. Lower Or do vi cian (Tremadocian) seis mic ex per i ment. Prace Państwowego Instytutu Geolo- tuffaceous mudstones from the Holy Cross Moun tains, Po land: gicznego, 188: 203–222. min eral com po si tion and early diagenetic sili ci fi ca tion. Mineralo - Moczydłowska, M., 1997. Pro tero zoic and Cam brian suc ces sion in gia Spe cial Pa pers, 49: 79. Upper Silesia, an Avalonian terrane in south ern Poland. Geol - Sircombe, K.N., 1999. Trac ing prov enance through the iso tope ogy, 134: 679–689. ages of lit to ral and sed i men tary de tri tal zir cons, East ern Aus tra - Nance, R.D., Murphy, J.B., 1996. Base ment iso to pic sig na tures lia. Sed i men tary Ge ol ogy, 124: 47–67. and Neoproterozoic paleogeography of Avalonian-Cadomian Shumlyanskyy, L., Hawkesworth, C., Dhuime, B., Billström, K., and related ter ranes in the circum-North At lan tic. GSA Spe cial Claesson, S., Story, C., 2015. 207Pb/ 206Pb ages and Hf iso tope Pa per, 304: 333–346. com posi tion of zir cons from sed i men tary rocks of the Ukrai nian Narkiewicz, M., 2002. Or do vi cian through ear li est De vo nian de vel - shield: Crustal growth of the south-west ern part of East Eu ro- opment of the Holy Cross Mts. (Poland): con straints from sub si - pean craton from Archaean to Neoproterozoic. Pre cam brian Re- dence anal y sis and ther mal ma tu rity data. Geo log i cal Quar terly, search, 260: 39–54. 46 (3): 255–266. Shumlyanskyy, L., Nosova, A., Billström, K., Söderlund, U., Narkiewicz, M., Grad, M., Guterch, A., Janik, T., 2011. Crustal Andreasson, P.G., Kuzmenkova, O., 2016. The U-Pb zir con seismi c veloc i ty structure of southern Poland: preserved mem - and baddeleyite ages of the Neoproterozoic Volyn Large Igne - ory of a pre-Devo nian terrane ac cre tion at the East Eu ropean ous Prov ince: Im pli ca tion for the age of the magmatism and the Plat form mar gin. Geo log i cal Mag a zine, 148: 191–210. nature of a crustal con tam i nant. Geologiske Foreningen Narkiewicz, M., Maksym, A., Malinowski, M., Grad, M., Guterch, Forhandlinger (GFF), 138: 17–30. A., Probulski, J., Janik, T., Majdański, M., Środa, P., Czuba, Soejono, I., Janoušek, V., Žáčková, E., Sláma, J., Konopásek, J., W., Gaczyński, E., Jankowski, L., 2015. Transcurrent na ture of Machek, M., Hanžl, P., 2017. Long-last ing Cadomian mag matic the Teisseyre-Tornquist Zone in Cen tral Eu rope: results of the ac tiv ity along an ac tive north ern Gondwana margin: U-Pb zir con POLCRUST-01 deep reflec tion seismi c profile. Inter na tional and Sr–Nd iso to pic ev i dence from the Brunovistulian Domain, Jour nal of Earth Sci ences, 104: 775–796. eastern Bohe mian Massif. Inter na tional Journal of Earth Sci - Nawrocki, J., Poprawa, P., 2006. De vel op ment of Trans-Eu ro pean ences, 106: 2109–2129. Su ture Zone in Poland: from Ediacaran rift ing to Early Spencer, C.J., Kirkland, C.L., Richard, J.M., Tay lor, R.J.M., 2016. Palaeozoic ac cre tion. Geo log i cal Quar terly, 50 (1): 59–76. Strate gies towards statis ti c ally robust inter pre ta tions of in situ Nawrocki, J., Buła, Z., Grabowski, J., Habryn, R., Jachowicz, M., U-Pb zir con geo chron ol ogy. Geoscience Frontiers, 7: 581–589. Jarosiński, M., Jóźwiak, W., Krzywiec, P., Poprawa, P., Svojtka, M., Breiter, K., Ďurišova, J., Ackerman, L., Veselovsky, Żylińska, A., 2001. Early Palaeozoic Palaeoge ogra phy of Upper F., Šmerda, J., 2017. Geochem is try and U-Pb zir con ages of Silesian Terrane (S Po land). Joint meet ing of Europrobe TESZ, Derflice granodiorite from the Thaya (Dyje) Massif (in Czech Timpebar, Uralides and SW - Ibe ria projects, 51–52. Middle East with English sum mary). Geoscience Research Re ports, 50: Tech ni cal Uni ver sity An kara – Tur key. 17–24. Nawrocki, J., Żylińska, A., Buła, Z., Grabowski, J., Krzywiec, P., Ślączka, A., 1985. Potrójna IG-1. Kambr, Prekambr. Profil Poprawa, P., 2004. Early Cambrian lo ca tion and af fin i ties of the litologiczno -stratygraficzny (in Pol ish). Pro file Głębokich Otwo- Brunovistulian terrane (Central Eu rope) in the light of palaeo - rów Wiertniczych Instytutu Geologicznego, 59: 38-41. magnetic data. Journal of the Geolog i cal So ci ety, 161: 513–522. Teipel, U., Eichhorn, R., Loth, G., Rohrmüller, J., Höll, R., Ken- Nawrocki, J., Dunlap, J., Pecskay, Z., Krzeminski, L., Żylinska, nedy, A., 2004. U-Pb SHRIMP and Nd iso to pic data from the A., Fanning, M., Kozłowski, W., Salwa, S., Szczepanik, Z., west ern Bo he mian Mas sif (Bayerischer Wald, Germany) : im pli - Trela, W., 2007. Late Neoproterozoic to Early Palaeozoic ca tions for Up per Vendian and Lower Ordo vi cian magmatism. palaoegeography of the Holy Cross Moun tains (Cen tral Eu - In ter na tional Jour nal of Earth Sci ences, 93: 782–801. rope): an inte grated approach. Jour nal of the Geo log i cal So ci - Terentiev, R.A., Santosh, M., Skryabin, V.Yu., 2016. U-Pb zircon ety, 164: 405–423. geo chron ol ogy and geo chem is try of Paleoproterozoic mag - Oberc-Dziedzic, T., Klimas, K., Kryza, R., Fanning, C.M., 2003. matic suite from East Sarmatian Orogen: tectonic impli c ations SHRIMP U-Pb zir con geo chron ol ogy of the Strzelin gneiss, SW on Colum bia supercontinent. Pre cam brian Re search, 273: Poland: evi dence for a Neoproterozoic thermal event in the 165–184. Fore-Sudetic Block, Cen tral Eu ropean Variscides. In ter na tional Timmerman, M., Krmiček, L., Krmičkova, S., Sláma, J., 2019. Jour nal of Earth Sci ences, 92: 701–711. LA-ICP-MS zir con ages of the Slavkov Terrane, Central Ba sic Pacześna, J., 2014. The fa cies de vel op ment of Terreneuvian de- Belt and Basal Clastics, Brunovistulicum, Czech Re public Con - pos its in the east ern part of the Upper Silesian Block (in Polish ference pa per 17th Meeting of the Cen tral Eu ropean Tec tonic with English sum mary). Biuletyn Państwowego Instytutu Groups, CETEG 2019, Rozdrojovice, 24–27 April, 2019, 84. Geologicznego, 459: 133–146. Trela, W., Bąk, E., Pańczyk, M., 2018. Up per Or do vi cian and Si lu - Pell, S.D., Williams, I.S., Chivas, A.R., 1997. The use of protolith rian ash beds in the Holy Cross Moun tains, Po land: pres erva tion zircon-age finger prints in deter min ing the protosource areas for in mudrock fa cies and re la tion to at mo spheric cir cu la tion in the some Aus tra lian dune sands. Sed i men tary Ge ol ogy, 109: South ern Hemi sphere. Jour nal of the Geo log i cal So ci ety, 175: 233–260. 352–360. Pharaoh, T.C., 1999. Palaeozoic terranes and their lithospheric Valverde-Vaquero, P., Dörr, W., Belka, Z., Franke, W., bound aries within the Trans-Eu ropean Su ture Zone (TESZ): a Wiszniewska, J., Schastok, J., 2000. U-Pb sin gle-grain dat ing re view. Tectonophysics, 314: 17–41. of de tri tal zir con in the Cam brian of cen tral Po land: im pli ca tions Poprawa, P., Krzywiec, P., Pacześna, J., Radkovets, N., for Gondwana versus Baltica prov enance stud ies. Earth and Krzemińska, E., Mazur, S., Rauball, J., 2018. Ediacaran rift at Plan e tary Sci ence Let ters, 184: 225–240. the SW mar gin of the East Eu ropean Craton. CETEG 2018, Ver ni ers, J., Maletz, J., Křiž, J., Žigaite, Ž., Paris, F., Schonlaub Central Eu ropean Tec tonic Groups, 16th Meet ing, Rytro, Po - H.P., Wrona, R., 2008. Si lu rian. In: The Geol ogy of Central Eu - land, 18–21 April 2018 Ab stract vol ume: 183–184. rope, Vol ume 1: Pre cam brian and Palaeozoic (ed. T. McCann): Pożaryski, W., 1991. The strike-slip terrane model for the North 249-302. Geo log i cal So ci ety of Lon don. Ger man-Pol ish Caledonides. Pub li ca tions of the In sti tute of Walczak, A., Belka, Z., 2017. Fin ger print ing Gond wana ver sus Geo phys ics, Pol ish Acad emy of Sci ences, A-19, 236: 3–15. Baltica prov enance: Nd and Sr iso topes in Lower Paleo zoic Detri tal zir con age data from the con glom erates in the Up per Silesian and Małopolska blocks, and their im pli ca tions... 341

clastic rocks of the Małopolska and Łysogóry terranes, south ern Po land and south east ern Ro ma nia. Geo log i cal Quar terly, 53 Po land. Gond wana Re search, 45: 138–151. (1): 93–124. Wiedenbeck, M., Allé, P., Corfu, F., Griffin, W.L., Meier, M., Żelaźniewicz, A., Seghedi, A., Jachowicz, M., Bobiński, W., Oberli, F., von Quadt, A., Roddick, J.C., Spiegel, W., 1995. Buła, Z., Cwojdziński, S., 2001. U-Pb SHRIMP data confirm Three natu ral zir con stan dards for U-Th-Pb, Lu-Hf, trace-el e - the pres ence of a Vendian foreland flysch ba sin next to the East ment and REE anal y ses. Geostandards News let ter, 19: 1–23. Euro pean Craton In: ESF EUROPROBE Meet ing “Neoprotero- Wil liams, I.S., Krzemińska, E., Wiszniewska, J., 2009. An exten - zoic–Early Palaeozoic Time-Slice Sympo sium: Orog eny and sion of the Svecofennian orogenic prov ince into NE Po land: ev i - Cratonic Brunovistulian terrane 521 Response on the Mar gins of dence from geo chem is try and de tri tal zir con from Paleoprotero- Baltica”, Ankara, Ab stracts (eds. T.C. Pha raoh and D. Gee): zoic paragneisses. Pre cam brian Re search, 17: 234–254. 98–100. Mid dle East Tech ni cal Uni ver sity, An kara. Winchester, J.A., Pharaoh, T.C., Ver niers, J., 2002. Palaeozoic Żylińska, A., 2013. The old est Cam brian trilobites from the Holy amal gam ation of Cen tral Eu rope: an in tro duc tion and syn the sis Cross Moun tains, Po land: taxo nomic, strati graphic and biogeo - of new re sults from re cent geo log i cal and geo phys i cal in ves ti ga - graphic re ap praisal. Acta Geologica Polonica, 63: 57–87. tions. Geo log i cal So ci ety Spe cial Pub li ca tions, 201: 1–18. Żylińska, A., Masiak, M., 2007. Cam brian trilobites from Brzechów, Zang, W., Fyfe, W.S., 1995. Chloritization of the hydro ther mally al- Holy Cross Mountains (Po land) and their sig nif i cance in strati - tered bedrock at the Igarapé Bahia gold de posit, Carajás, Brazil. graphic cor re la tion and biogeographic re con struc tions. Geo log i - Mineralium Deposita, 30: 30–38. cal Mag a zine, 144: 661–686. Żelaźniewicz, A., Fanning, C.M., 2020. Neoarchean to Paleopro - Żylińska, A., Szczepanik, Z., 2009. Tri lo bite and acritarch assem - terozoic frag ments in the Brunovistulia terrane, S Poland: a blages from the Lower-Middle Cam brian bound ary in terval in the com po nent of the Co lum bia Supercontinent? Geo log i cal Quar- Holy Cross Mountains (Po land). Acta Geologica Polonica, 59: terly 64 (1): 120–129. 413–458. Żelaźniewicz, A., Bula, Z., Fanning, M., Seghedi, A., Żaba, J., 2009. More ev i dence on Neoproterozoic terranes in South ern