Geo log i cal Quar terly, 2018, 62 (1): 120–133 DOI: http://dx.doi.org/10.7306/gq.1393
Miospore ev i dence for the Car bon if er ous age of rocks from the Œwiebodzice Unit (Sudetes, SW Po land)
Kamil PLUTA1 and Anna GÓRECKA-NOWAK1, *
1 Uni ver sity of Wroc³aw, In sti tute of Geo log i cal Sci ences, pl. M. Borna 9, 50-204 Wroc³aw, Po land
Pluta, K., Górecka-Nowak, A., 2018. Miospore ev i dence for the Car bon if er ous age of rocks from the Œwiebodzice Unit (Sudetes, SW Po land). Geo log i cal Quar terly, 62 (1): 120–133, doi: 10.7306/gq.1393
As so ci ate Ed i tor – Grzegorz Racki
The pa per pro vides new re sults of palynological stud ies of rocks from the Œwiebodzice Unit. An abun dant Car bon if er ous miospores were found in rocks of the Pogorza³a For ma tion from the south ern part of this unit. These miospores oc cur in rocks con tain ing also macrofloral and ma rine macrofaunal fos sils, partly re worked, which were usu ally con sid ered Up per De vo nian. Two miospore sub-as sem blages of dif fer ent ages and colours have been dis tin guished. One of them con sists of poorly pre served miospores, dark in col our, which in di cate the Late Visean–Serpukhovian age of the rocks. The other sub-as sem blage, found only in a few sam ples, con sists of much lighter and well-pre served miospores of the Asturian age.
Their pres ence is con sid ered as a re sult of strati graphi cal leak age. Ob ser va tion of the miospore col our in di cates that the ther mal event oc curred af ter the Late De vo nian and be fore the Asturian and the palaeotemperature ex ceeded ~180°C.
These new data in di cate that the geo log i cal his tory of the Œwiebodzice Unit lasted lon ger and was much com plex than it was pre vi ously con sid ered.
Key words: Œwiebodzice Unit, De vo nian, Car bon if er ous, redeposition, strati graphi cal leak age, ther mal event.
INTRODUCTION
The Œwiebodzice Unit (called also the Œwiebodzice De pres - sion or Œwiebodzice Fold Struc ture) is a part of the Cen tral Sudetes (Fig. 1). It is filled with an ~4000 m thick coarse-grained rocks rep re sented not only by con glom er ates but also by mudstones, sand stones, less com mon marls, and rare lime - stones. Two rock suc ces sions have been rec og nized. One of them con sists of con glom er ates. Porêbski (1981) di vided them into two lithostratigraphic units: the Ksi¹¿ and Chwaliszów for ma - tions. The other suc ces sion is heterolithic and di vided into the Pogorza³a and Pe³cznica for ma tions (Porêbski, 1981). All these rocks are con sid ered synorogenic and ac cu mu lated in a fan-delta slope/ba sin plain depositional sys tem (Nemec et al., 1980; Porêbski, 1981, 1984, 1987). Wojewoda (2014, 2016a, b) dis tin guished turbidites, hemipelagic and pe lagic fa cies in the heterolithic se ries with olistolites and slumps of older rocks oc - cur ring near ba sin mar gins.
Porêbski (1987, 1990) and Wojewoda (2014, 2016a, b) as - sumed that the rhom boid shape of the Œwiebodzice Unit, bounded by ac tive faults, re fers to a pull-apart ba sin, but these au thors pre sented dif fer ent mod els on its de vel op ment. The
geo log i cal struc ture of this unit and the age of its infill show se ri - ous re gional im pli ca tions, so it is very im por tant that their stra tig - ra phy is thor oughly un der stood and any con tro versy ex plained.
Un for tu nately, the pres ent-day un der stand ing of the geo log i cal set ting and stra tig ra phy is not sat is fac tory. One of the key strati - graphic prob lems of this unit is the great lithological di ver sity due to com plex spa tial re la tion ships be tween lithologically di verse rocks. In ad di tion, this area is poorly out cropped and fol low ing the con ti nu ity of the rock units is usu ally im pos si ble. Con se quently, nei ther the strati graphic se quence nor cor re la tion of rocks are ob vi ous. Be fore 1945, most re search ers, in clud ing Berg et al.
(1910), as sumed that the coarse-grained suc ces sion was youn - ger than the heterolithic rocks. Teisseyre (1948, 1952, 1956a, b, 1968; Teisseyre et al., 1957) and Porêbski (1981, 1984, 1987, 1990) also agreed with this opin ion. The op po site opin ion was put foreward by Cramer et al. (1924) who con sid ered the gneiss con glom er ates (pres ently the Ksi¹¿ For ma tion) as older than heterolithic rocks, cur rently clas si fied as the Pogorzala For ma - tion. In turn, Gunia (1968) sup posed that con glom er ates from the Ksi¹¿ and Chwaliszów for ma tions are stratigraphically equal to fine-grained fa cies with car bon ate sed i ments and were formed in mar ginal parts of the ba sin from the late Frasnian to the Tournaisian. Re cently, Wojewoda (2014, 2016a, b) pre sented a new model of the Œwiebodzice Unit de vel op ment in which rocks from the cen tral part of this unit, mainly con glom er ates, are con - sid ered stratigraphically older than rocks in mar ginal parts. Ac - cord ing to this model, con glom er ates of the Chwaliszów and
* Corresponding author, e-mail: anna.gorecka-nowak@uwr.edu.pl Received: May 15, 2017; accepted: October 23, 2017; first published online: December 21, 2017
Ksi¹¿ for ma tions are older than heterolitic rocks of the Pogorza³a and Pe³cznica for ma tions (Wojewoda, 2014, 2016a, b).
Nu mer ous De vo nian and Car bon if er ous macrofossils of ma rine fauna as well as Car bon if er ous macrofloral fos sils were found in rocks of this geo log i cal unit. These fos sils are the main strati graphic ev i dence, but they are gen er ally poorly pre served and ma jor ity of them are long-rang ing taxa. They are un evenly dis trib uted, i. e. many rocks re main with out any palaeonto -
logical ev i dence. Ad di tion ally, some De vo nian fos sils are con - sid ered re worked as they oc cur in peb bles in youn ger rocks and this com pli cates the strati graphic in ter pre ta tion.
Dis cus sion on the stra tig ra phy of the Œwiebodzice Unit has con tin ued since the 19th cen tury and the fun da men tal prob lem was the De vo nian or Car bon if er ous age of its infill. Ac cord ing to Gunia (1968), the ma jor ity of these rocks be long to both stages of the Up per De vo nian – the Frasnian and the Famennian, and Fig. 1A – geological sketch-map of the central part of the Sudetes (after ¯elaŸniewicz et al., 2011, simplified);
B – geological map of the Œwiebodzice Unit (after Kaczorowski and Wojewoda, 2011)
A – I-KM – Izera–Karkonosze Mas sif, KGP – Karkonosze Gran ite Pluton, NSS – North Sudetic Synclinorium, KGSFB – Kaczawa greenstone-and-slate fold belt, WWGS – W¹dro¿e Wielkie Gneiss Mas sif, S-SGP – Strzegom–Sobótka Gran - ite Pluton, ŒG-SM – Œlê¿a Gab bro-Serpentynite Mas sif, GSGM – Góry Sowie Gneiss Mas sif, R-MG – Roztoka–Mokrzeszów Graben; B – SMF – Sudetic Mar ginal Fault, SzF – Szczawienko Fault, SF – Struga Fault
sed i men ta tion fin ished there in the Tournaisian. This strati - graphic scheme was used for the model of sed i men ta tion pre - sented by Porêbski (1981, 1984, 1987, 1990) and it be came com monly ac cepted and, con se quently, there was no strati - graphi cal study for nearly a half of cen tury. The only ex cep tion was a palynostratigraphic study by Krawczyñska-Grocholska (1973), who proved the oc cur rence of Car bon if er ous miospore as sem blages in rocks from the north ern part of the Œwiebodzice Unit. Un for tu nately, this in ter est ing con clu sion was not taken into ac count in sub se quent in ter pre ta tions. The re cently pub lished pa per on De vo nian brachi o pods (Halamski, 2013) is a har bin ger of a new stage of palaeontological and biostratigraphical stud ies in this area. An at tempt to the re con - struc tion of the De vo nian palaeoenviron ment was un der taken by Pluta (2016).
The age of rocks of the Œwiebodzice Unit has fun da men tal sig nif i cance in the in ter pre ta tion of geo log i cal set ting and evo lu - tion of the Cen tral Sudetes. Close prox im ity of sed i men tary rocks, in ter preted as Up per De vo nian to Lower Car bon if er ous (Gunia, 1968), and low-grade meta mor phosed rocks of De vo - nian and Visean age of the ad ja cent Kaczawa Mts. (Urbanek, 1975, 1978; Chorowska, 1978) is one of the facts dif fi cult to ex - plain.
An other im por tant topic is time re la tion be tween clastic rocks of the Œwiebodzice Unit and gneiss es of the Sowie Mts., which com monly oc cur as peb bles in the for mer. Dur ing all dis - cus sions, it has been con sid ered as an ax iom that the Sowie Mts. gneiss es and their ex hu ma tion have to be older than De - vo nian (Zinkiewicz, 1973; Gunia, 1985). Cur rently, the fi nal stage of the meta mor phic event of the Sowie Mts. block is dated as Late De vo nian, pre cisely at 385–370 Ma on the ba sis of U-Pb and Rb-Sr data (van Breemen et al., 1988; Bröcker et al., 1998; Timmermann et al., 2000), and this re sult has been used for geo log i cal syn the ses cov er ing the en tire Sudetes (Mazur et al., 2006).
Nu mer ous miospores were found dur ing re cent palynostratigraphical stud ies un der taken in the Œwiebodzice Unit. Ma jor ity of them is un de ter min able due to very poor pres - er va tion caused by high ther mal al ter ation. Miospore data from the south ern part of this geo log i cal unit pro vided amaz ing re - sults, as they re vealed oc cur rence of rec og niz able Car bon if er - ous miospores in rocks in ter preted be fore as De vo nian. Two miospore sub-as sem blages were dis tin guished and the older of them con sists of hardly rec og niz able and dark-col oured miospores. Some better pre served miospore spec i mens in di - cate Late Visean–Serpukhovian age. The other miospore sub-as sem blage con sists of well-pre served spec i mens in di cat - ing the Asturian age (for mer Westphalian D). Their strati graphic in ter pre ta tion is not easy and the geo log i cal sig nif i cance of these two Car bon if er ous dates is dis cussed here af ter. They ap - point a dif fer ent time frame of the Œwiebodzice Unit de vel op - ment, com pared to the pre vi ously ac cepted opin ions, in di cat ing that the geo log i cal his tory of this unit is still un clear and ap par - ently more com pli cated than it was pre vi ously thought.
Palynological re search ap peared to be a per spec tive method for the study of strati graphi cal prob lems in this area.
MATERIAL AND METHODS
Palynostratigraphical stud ies were re cently un der taken in the whole Œwiebodzice Unit (Fig. 1B). Forty-seven sam ples were taken from fine-grained rocks, mainly mudstones. Sam - ples from the Pe³cznica For ma tion were taken near the vil lages of Chwaliszów and Pe³cznica. Five sam ples were taken from an
out crop of mudstones near a field road close to Chwaliszów (lo - cal ity no. 1 in Fig. 1B; N50°52’27.56’’, E16°13’34.53’’). Two lo - cal i ties close to Pe³cznica were sam pled: 5 sam ples were taken near the an cient yew Bolko (out crop no. 2 in Fig. 1B;
N50°50’52.77’’, E16°17’28.01’’) and 4 sam ples were taken near cas cade on the Pe³cznica River (out crop no. 3 in Fig. 1B and nos. 44 and 44a of Gunia, 1968; N50°51’26.7’’, E16°18’41.37’’).
One sam ple was taken from mudstones on the shore of Daisy Lake close to Mokrzeszów (out crop no. 4 in Fig. 1B and no.15 of Gunia, 1968; N50°49’28.17’’, E16°21’41.71’). The Pogorza³a For ma tion was also sam pled near the vil lages of Lubiechów and Witoszów Górny. The quarry in Lubiechów (no. 5 in Fig. 1B and no. 26 of Gunia, 1968) is lo cated in the Ksi¹¿ Land scape Park, ~2 km south of Lubiechów (N: 50°49’2.03’’, E16°19’48.05’’; Fig. 2A), which is the NE dis trict of Wa³brzych.
Teisseyre (1956a) con sid ered this place as the cen tre of the Pogorza³a syncline. From this quarry, 19 rock sam ples for the palynological stud ies were taken. Sam ples were taken also from two lo cal i ties near Witoszów Górny. One of them is the quarry of slate roof tiles (out crop no. 7 in Fig. 1B and no. 3 of Gunia, 1968; N50°49’19.05’’, E16°22’57.56’’) where 3 sam ples were taken. Ten rock sam ples were taken from mudstones from an other out crop in Witoszów Górny (no. 6 in Fig. 1B), lo cated on the left bank of the creek be tween Witoszów Górny and Pogorza³a (N50° 48’ 57.97’’, E16° 22’ 31.29’’) in a place re - garded by Teisseyre (1956b) as the south ern wing of the Pogorza³a syncline. This out crop and the quarry in Lubiechów are de scribed in de tail be low, as they pro vided abun dant miospore data.
Palynological sam ples were thor oughly cleaned and then crushed. The first step of their chem i cal pro cess ing was the use of hy dro chlo ric acid (HCl) to dis solve car bon ates. The sam ples were then pro cessed in 40% hy dro gen flu o ride. Next each sam - ple was di vided into two parts: in tended for ther mal ma tu rity as - sess ment and palynostratigraphical stud ies. The Schulze method of ox i da tion was ap plied only to the lat ter sam ples, and 65% ni tric acid and po tas sium chlo rate were used. Af ter the pu - ri fi ca tion, mi cro scopic slides were made from the re sid uum.
The slides were sub se quently analysed us ing a Nikon Optiphot 2 mi cro scope. Pho to mi cro graphs were made us ing a dig i tal cam era Canon PowerShot A640. All slides are stored at the In - sti tute of Geo log i cal Sci ences, Uni ver sity of Wroc³aw.
RESULTS
Rocks from all stud ied sites yielded miospores, but ma jor ity of them are un rec og niz able due to very poor pres er va tion caused by the high ther mal al ter ation. The abun dant and well-pre served miospores oc curred in seven sam ples of the Pogorza³a For ma tion. They were found in rocks from the Lubiechów Quarry (no. 5 in Fig. 1B) and the out crop near Witoszów Górny (no. 6 in Fig. 1B) in the south ern part of the Œwiebodzice Unit. The com pli cated geo log i cal struc ture of rocks oc cur ring in these two lo ca tions is worth dis cuss ing be cause it in - flu ences the strati graphic in ter pre ta tion of miospore data.
THE LUBIECHÓW QUARRY
The quarry con sists of two parts, but mudstones suit able for palynological stud ies oc cur only in its up per part. Main lithological types are con glom er ates, sand stones, mudstones and very rare lime stones. The com plex ity of spa tial re la tions among lithological va ri et ies is shown in Fig ure 2B, C and D.
122 Kamil Pluta and Anna Górecka-Nowak
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On the east ern wall of the quarry, mudstones and con glom - er ates form a kind of trough, which is ~5 m wide (Fig. 2B). The con glom er ates are sur rounded by mudstones. The bed ding in mudstones is vari able and masked by fre quent cracks and slick en sides, but re fers gen er ally to the shape of the con glom - er ate body. Small sand stone bod ies oc cur ring as dis crete loafs and in jec tions of mudstones, prob a bly form ing clastic dykes, oc cur within the con glom er ate body. Con glom er ates con sist of Sphaerocodium balls – oncoids with Sphaerocodium zimmermanni Rothpletz, also known as Girvanella (Pia, 1937).
These oncoids are up to 5 cm across and oc cur in the sand - stone ma trix. They were de scribed by Zimmerman (1911) who con sid ered them Late De vo nian in age and syngenetic with con glom er ates in which they oc cur. Schindewolf (1925) agreed that the Sphaerocodium balls are in situ and sup posed that they orig i nated in a shal low-ma rine en vi ron ment and are re lated to the crush ing of coral reefs.
The north ern wall of this quarry is com posed mainly of con - glom er ates with sandy ma trix and mudstones (Fig. 2C, D).
Small bod ies of sand stones and lime stones also oc cur. The bed ding in mudstones is con cor dant with the out line of the con - glom er ate body, which seems to have a len tic u lar shape. Con - glom er ates con tain peb bles of dif fer ent rocks and in fre quent oncoids. In ad di tion, mudstones that fill “slits” in the con glom er - ate body seem to be clastic dykes and con tain some sharp-edged blocks of sand stones and con glom er ates. Fur - ther more, sev eral lime stone blocks oc cur in the mid dle part of the wall (Fig. 2C). They are ~30 cm thick and oc cur along the bor der of the “slit”, in one line, at tain ing ~2 m in length. They are prob a bly frag ments of a crushed lime stone plate. The pres - ent-day ar range ment of rock bod ies was in ter preted by Porêbski (1981) as rock re cord of grav ity flow. This au thor con - sid ered the oc cur rence of con glom er ate bod ies by the “rigid stop per" mech a nism in rocks of slid ing char ac ter. Wojewoda (2016a, b) sup posed that rocks oc cur ring in this quarry are a fos sil slump sheet of pre sumed Visean age.
Gunia (1968) found quite nu mer ous macrofossils of ma rine fauna in rocks from this quarry: Rugosa cor als and Amphipora sp. oc cur in the con glom er ate ma trix, where also nu mer ous un - rec og niz able frag ments of brachi o pod shells were found. Lat ter rem nants oc cur also in oncoids. Poorly pre served fos sils de ter - mined as clams Buchiola palmata and B. retrostriata, as well as goniatites Tornoceras auris (Quenstedt) and T. paucistriatum (Archiac et Verneuili) were found in mudstones. Gunia (1968) as signed these rocks to the Up per Frasnian.
An im print of the Car bon if er ous fern leaf Adiantites antiquus (Ettingshausen) Stur (Fig. 3) and un de ter min able im prints of stems were found dur ing our field work in a mudstone block near the east ern wall of the quarry (Pluta, 2012). Abun dant frag - ments of crushed fos sils – stomatoporoids, cor als, prob a bly brachi o pods and clams – were found in mudstones and con - glom er ates (Fig. 4). They oc cur among sharp-edged frag ments of rocks and oncoids, and some of them were ob served also in - side oncoids. The mi cro scopic ob ser va tions of macrofauna shells or their frag ments of ten re veal pres ence of very thin lithic sheaths around shell frag ments (Fig. 4D, E). This in di cates that some macrofossils con sid ered as bioclasts in fact ap peared to be lithoclasts (Pluta, 2012) and their oc cur rence in rocks sug - gests redeposition. Oncoids com monly oc cur ring in con glom er - ates, ac cord ing to a re cent model, grew at a muddy bot tom in low-en ergy con di tions (Peryt, 1981; Pluta, 2016).
OUTCROP IN WITOSZÓW
The main lith o logic type in this out crop is rep re sented by dark grey or grey, clearly bed ded mudstones with rip ple marks and in ter ca la tions of sand stones. These rocks are cov ered by con glom er ates con tain ing rounded peb bles of lime stones and gneiss es (Fig. 5). The loaf-shaped body of well-sorted sand - stone oc curs in mudstones and its thick ness var ies from centi - metres to a few metres. Sand stones and con glom er ates lie
124 Kamil Pluta and Anna Górecka-Nowak
Fig. 3. Imprint of Adiantites antiquus (Ettingshausen) Stur found in a mudstone block in the Lubiechów Quarry (phot. Kamil Pluta)
Fig. 4. Record of the fossils redeposition in rocks of the Pogorza³a Formation from the Lubiechów Quarry (samples from the north wall of the quarry,
marked as lithological samples A–E in Fig. 2C, D)
A – peb bly sand stone, sharp edged lithoclasts of oncoid lime stones (a), sep a rate oncoids (b), frag ments of brachi o pod shells sur rounded by very thin lithic sheaths (c), frag ments of Amphipora sp. with pre - served lime stone sheaths (d), frag ments of lime stones (e); B – peb bly sand stone with oncoids show ing pre served in ter nal struc ture (a); C – com pact Spherocodium con glom er ate with oncoids (a), frag ments of brachi o pod shells sur rounded by very thin lithic sheaths (b), frag ments of Amphipora sp. with pre - served lime stone sheaths (c); D – peb bly sand stone – thin sec tion in po lar ized light, frag ments of brachi - o pod shells (a), frag ments of Amphipora sp. with prom i nent lime stone sheaths (b), sharp-edged frag ments of lime stones (c) in the sandy ma trix; E – peb bly sand stone – thin sec tion in po lar ized light, frag ments of brachi o pod shells (a), frag ments of Amphipora sp. with prom i nent lime stone sheaths (b), sharp-edged frag ments of lime stones (c) in the sandy ma trix, oncoids which grew on a thin shell of a brachi o pod or a clam (d)
con cor dantly be tween sur round ing mudstones. The pres ence of gneiss peb bles and the anal y sis of rip ple-mark asym me try in - di cate that the rock ma te rial was trans ported from the south.
Porêbski (1981) sug gested that these sed i ments are of grav - ity-flow or i gin.
Gunia (1968) de scribed many macrofaunal fos sils in lime - stone peb bles from con glom er ates over ly ing the mudstones.
Rugosa cor als, stromatoporoids and brachi o pod Spinatrypa are found there. Macrofossils in the mudstones are rel a tively rare, but Gunia (1968) re ported oc cur rence of un de ter min able rem nants of macroflora and a poorly pre served in ter nal mold of cephalopod Bactrites cf. ausavensis. On this ba sis, the rocks were as signed to the Up per Frasnian.
CHARACTERISTICS OF MIOSPORE ASSEMBLAGES
The miospore as sem blages de ter mined in pro duc tive sam - ples from the Lubiechów Quarry and the out crop near Witoszów Górny (Figs. 2 and 5) are pe cu liar. Each of them con sists of two miospore sub-as sem blages that dif fer in col our (Figs. 6 and 7).
The sub-as sem blage of dark miospores con tains dark brown to black, hardly rec og niz able spec i mens. The de ter mi na - tion of miospores from this group was pos si ble only if the miospore struc ture was pre served de spite its high ther mal al - ter ation or the spec i men was slightly better pre served. Rocks from the Lubiechów Quarry con tained the fol low ing gen era:
Bascaudaspora, Densosporites, Knoxisporites, Kraeuseli - sporites, Lycospora, Radiizonates Schulzospora, Vallatis - porites, and two spe cies: Cingulizonates bialatus1 and Rotaspora knoxi. Sam ples from Witoszów Górny yielded abun - dant dark miospores and gen era Lycospora and Densosporites were rec og nized among them (Ap pen dix 1*).
The other sub-as sem blage con sists of light-col oured spec i - mens – yel low–or ange to or ange–brown. These miospores are
better pre served (Figs. 6 and 7) and ap peared to be tax o nom i - cally di verse, as 73 miospore taxa were de ter mined in this sub-as sem blage (Ap pen dix 1). The most tax o nom i cally di verse miospores were found in sam ples Lub 6 and Lub 9 (Ap pen dix 1).
A sim i lar, al though not so nu mer ous miospore as sem blage, was rec og nized from Witoszów Górny. The sim i lar pres er va tion and tax o nom i cally com pa ra ble com po si tion of miospore data from these two lo ca tions sug gest that they may be dis cussed and in - ter preted to gether. The char ac ter is tic fea ture of this as so ci a tion is the pres ence of gen era Calamospora, Cingulizonates, Cyclogranisporites, Densosporites, Lycospora, Punctatisporites, Radiizonates, Raistrickia and Verrucosi sporites. Some stratigraphically im por tant miospore spe cies in clude Ahrensisporites guerickei, Alatisporites pustulatus, A. trialatus, Apiculatasporites spinulistratus, Cadiospora magna, Crassispora kosankei, Latensina trileta, Microreticulatisporites nobilis, Planisporites magnus, Reticulatisporites reticulatus and Westphalensisporites irregularis. A fairly large va ri ety of miospores from the Monoletes group was found. It in cludes rel a - tively nu mer ous spec i mens of the Laevigatosporites and Punctatosporites, as well as some less com mon spec i mens of Torispora and Thymospora. The com po si tion of the as sem blage is com ple mented by pol len grains, mainly of the Florinites type, but they are not abun dant (Figs. 6 and 7; Ap pen dix 1).
STRATIGRAPHICAL INTERPRETATION
The miospore data from the Pogorza³a For ma tion, con sid ered be fore as De vo nian (Gunia, 1968), clearly in di cate their Car bon if - er ous age. The co ex is tence of two miospore sub-as sem blages of dif fer ent colours sug gests that this miospore as sem blage is mixed. The anal y sis of tax o nomic com po si tion and the strati - graphi cal ranges of miospore taxa con firm this sup po si tion, as these sub-as sem blages dif fer also in strati graphi cal po si tion.
126 Kamil Pluta and Anna Górecka-Nowak
Fig. 5. The Witoszów Górny outcrop A – location of the outcrop; B – sketch of the outcrop
* Supplementary data associated with this article can be found, in the online version, at doi: 10.7306/gq.1393
1 Full names of determined miospore species with names of creators are listed in Appendix 1
Fig. 6. Miospores from rocks of the Lubiechów Quarry
1 – Calamospora mutabilis, sam ple Lub 9, si dle 3, M 10,2; 2 – Verrucosisporites microtuberosus, sam ple Lub 6, slide 1, N 29,2; 3 – Planisporites magnus, sam ple Lub 6, slide 3, M 55,3; 4 – Planisporites magnus, sam ple Lub 6, slide 3, Q 21,4; 5 – Cadiospora magna, sam - ple Lub 6, slide 1, Z 24; 6 – *Knoxisporites sp., sam ple Lub 2, slide 2, M 54; 7 – *Bascaudaspora sp., sam ple Lub 9, slide 3, M 17,1; 8 – Raistrickia superba, sam ple Lub 6, slide 2, N 12,3/O 12,1; 9 – Reticulatisporites reticulatus, sam ple Lub 6, slide 1, A 26,2; 10 – Cristatisporites indignabundus, sam ple Lub 6, slide 7, J 45,3/K 45,1; 11 – Densosporites variabilis, sam ple Lub 6, slide 4, M 52,3; 12 – Densosporites variabilis, sam ple Lub 6, slide 2, A 36,3; 13 – Densosporites intermedius, sam ple Lub 6, slide 1, C 48; 14 – Densosporites sphaerotriangularis, sam ple Lub 6, slide 1, Q 12,3; 15 – Densosporites triangularis, sam ple Lub 6, slide 1, Y 49,4; 16 – Westphalensisporites irregularis, sam ple Lub 9, slide 4, Z 30,3; 17 – Rotaspora knoxi, sam ple Lub 6, slide 6, B 42,3/C 42,1; 18 – Lycospora pusilla, sam ple Lub 6, slide 2, W 3,4; 19 – Lycospora pusilla, sam ple Lub 6, si dle 9, R 36; 20 – *Lycospora sp., sam ple Lub 9, slide 1, W 20,4/X 20,2; 21 –
*Lycospora sp., sam ple Lub 1o, slide 1, S 26,1; 22 – Cingulizonates loricatus, sam ple Lub 6, slide 2, Q 35,3; 23 – Cirratriradites anuliformis, sam ple Lub 6, slide 6, G 13,4; 24 – Cirratriradites anulatus, sam ple Lub 6, slide 6, P 10,1/P 10,3; * – taxon be longs to the Visean–Serpukhovian sub-as sem blage
128 Kamil Pluta and Anna Górecka-Nowak
Fig. 7. Miospores from rocks of the Lubiechów Quarry and the outcrop near Witoszów Górny
1 – Radiizonates striatus, sam ple Lub 6, slide 1, P 56,1; 2 – *Radiizonates sp., sam ple Lub 5, slide 6, N 28,1; 3 – Crassispora kosankei, sam - ple Lub 6, slide 4, X 45; 4 – Latensina trileta, sam ple Lub 9, slide 2, Z 55,1; 5 – *Kraeuselisporits sp., sam ple Lub 9, slide 1, Y 7; 6 –
*Vallatisporites sp., sam ple Lub onk 1, slide 1, O 12; 7 – Punctatosporits minutus, sam ple Lub 1, sam ple 1, D 34,2; 8 – Punctatosporites minutus, sam ple Lub 1, sam ple 1, D 42,4; 9 – Punctatosporites cingulatus, sam ple Lub 2, slide 1, M 24,1/M 24,3; 10 – Punctatosporites punctatus, sam ple Lub 6, slide 1, P 54,1; 11 – Torispora securis, sam ple Lub 9, slide 2, X 39,1; 12 – Thymospora obscura, sam ple Lub 9, slide 2, N 43,3; 13 – Thymospora pseudothiessenii, sam ple WG 6, slide 2, P 61; 14 – Alatisporites trialatus, sam ple Lub 6, slide 4, Z 35; 15 –
*Schulzospora sp., sam ple Lub 3 o, slide 1, Z 41,2; 16 – un de ter mined, sam ple Lub 6, slide 1, O 23,3; 17 – un de ter mined, sam ple Lub 6, slide 1, S4 0,3/T 40,1; 18 – un de ter mined, sam ple Lub 1, slide 1, T 9; 19 – *un de ter mined, sam ple Lub 9, slide 1, F 48,1; 20 – *un de ter mined, sam - ple Lub 9, slide 1, Z 44,1; 21 – *un de ter mined, sam ple Lub 6, slide 1, Z 31,2; 22 – *un de ter mined, sam ple Lub 6, slide 2, N 12; 23 – *un de ter - mined, sam ple Lub 9, slide 1, F 50,3; 24 – *un de ter mined, sam ple Lub 3, slide 1, R 36,2; * – taxon be longs to the Visean–Serpukhovian sub-as sem blage
The im por tant age in di ca tor for the dark-col oured miospore sub-as sem blage is the ge nus Lycospora. This ge nus, as dis - persed miospore, oc cur in Eu rope in rocks not older than Visean. The oc cur rence of Rotaspora knoxi, a spe cies with a rel a tively short strati graphic range, lim its the age of this sub-as - sem blage to the in ter val from the Raistrickia nigra–Triquitrites marginatus (NM) to Stenozonotriletes triangulus–Rotaspora knoxi (TK) palynozones, cor re spond ing to the Late Visean and Early Serpukhovian (Clay ton et al., 1977; Owens et al., 2004;
Fig. 8). The anal y sis of strati graphic ranges of all taxa rec og - nized in this sub-as sem blage in di cates that they are of Late Visean–Serpukhovian age.
The other set of miospores is rep re sented by well-pre - served spec i mens of rel a tively light col our. Some stratigraphically im por tant taxa were found in this sub-as sem - blage, al low ing ex act age in ter pre ta tion. One of them is Lycospora, which is the most com mon ge nus of the Eu ro pean Car bon if er ous, but it oc curs in rocks not older than Visean. An - other im por tant taxon is Crassispora kosankei. Its oc cur rence shows that this miospore sub-as sem blage is not older than Serpukhovian. In turn, the pres ence of Reticulatisporites reticulatus in di cates an age not older than Late Namurian (Owens et al., 2004). This sub-as sem blage con tains also youn - ger taxa, for ex am ple Cingulizonates loricatus and the ge nus Punctatosporites im por tant for the Langsettian (for mer Westphalian A). The first of them ap peared at the be gin ning of the Langsettian. Slightly later, but still in the Langsettian, the ge - nus Punctatosporites is re corded for the first time. The oc cur - rence of Westphalensisporites irregularis and Microreticulati - sporites nobilis proves that the sub-as sem blage is not older than Duckmantian (Westphalian B). The youn gest taxa are the monolete gen era Torispora and Thymospora, as well as the spe cies Cadiospora magna and Latensina trileta. All these taxa are char ac ter is tic for the Asturian (for mer Westphalian D), al - though Torispora ap peared slightly ear lier. The com po si tion of the sub-as sem blage of dis persed miospores is cor re lated to the miospore zone Thymospora obscura–T. thiessenii (OT), which cor re sponds to the Asturian (Clay ton et al., 1977; Fig. 8).
REMARKS ON PALAEOTEMPERATURE
The above-pre sented palynological data al low the re con - struc tion of palaeothermal his tory of rocks stud ied based on miospore col our. This in ter pre ta tion is pos si ble, as miospores of dif fer ent ages vary in col our, but, un for tu nately, not all rules of ther mal al ter ation as sess ment could be ap plied here. The miospore col our was as sessed partly on the ox i dized palynological ma te rial, and it was im pos si ble to use a sin gle miospore taxon for this pur pose, so the ob ser va tion was made on dif fer ent taxa. These me thod i cal mod i fi ca tions caused that ob tained re sults of ther mal al ter ation as sess ment should be con sid ered ap prox i mate. The oc cur rence of two miospore sub-as sem blages of dif fer ent colours in di cate their dif fer ent ther mal his to ries. The ob ser va tion of dark-col oured miospores be fore the sam ple ox i da tion re veals that all these spec i mens are black. The same sub-as sem blage af ter ox i da tion shows a slight dif fer ence in col our be tween fully black miospores from Daisy Lake near Mokrzeszów (out crop no. 4 in Fig. 1B) and dark brown to black miospores from all re main ing sites. The de - ter mi na tion of miospores from this sub-as sem blage is usu ally im pos si ble. None of black miospores from Daisy Lake is de ter - mi na ble, but rocks from this site are dated at the Up per De vo - nian by macrofaunal fos sils, partly in liv ing po si tion (Gunia, 1968). Black col our of all miospores in these De vo nian rocks sug gests that they were heated up to ~180°C (Bat ten, 1996).
The dark miospore sub-as sem blage oc cur ring in rocks in - cluded to the Up per Visean-Serpukhovian, be sides of black miospores con tain also some dark brown spec i mens. These colours in di cate that the max i mum palaeotemperature prob a bly did not ex ceed 160–170°C (Bat ten, 1996). The ob ser va tions point to two events of heat ing re corded in the dark-col oured miospore sub-as sem blages. The first one took place be tween the Frasnian and late Visean. The sec ond one was af ter the late Visean–Serpukhovian and be fore the Asturian, as miospores of this age are much lighter in col our. The yel low-or ange to or - ange-brown colours of the Asturian miospores in di cate much lower ther mal al ter ation in a tem per a ture not higher than 70°C (Bat ten, 1996).
DISCUSSION
The re sults of palynological anal y sis of rocks from the Œwiebodzice Unit pro vided com pletely new data. Rocks of the Pogorza³a For ma tion, for merly in ter preted as De vo nian (Gunia, 1968), yielded a num ber of Car bon if er ous miospores. Their oc - cur rence in these rocks in di cates the Car bon if er ous age. This re sult changes the ear lier views of Gunia (1968) on their De vo - nian age and fits well with the model of the Œwiebodzice Unit de - vel op ment pre sented by Wojewoda (2016a, b).
The im por tant fea ture of this miospore as sem blage is that it con sists of two sub-as sem blages of dif fer ent ages and ther mal his to ries. They were found in rocks abun dant in De vo nian and Car bon if er ous macrofossils, partly re worked, iden ti fied by pre - vi ous re search ers. That means that the as sem blage of fos sils is very com plex and its strati graphi cal in ter pre ta tion is ex tremely dif fi cult.
Tak ing into con sid er ation the re sults of all pre vi ous and re - cent biostratigraphical stud ies from the Œwiebodzice Unit, a rel - a tively long strati graphic in ter val from the Late De vo nian (Frasnian) to Late Penn syl va nian (Asturian) should be de ter - mined. Three shorter in ter vals are biostratigraphically dem on - strated and they are the im por tant dates in his tory of this geo - log i cal unit.
The old est in ter val spans the early Frasnian to Tournaisian, as proved by palaeontological ev i dence. The De vo nian fos sils (Mid dle Frasnian cor als) were stud ied by Zobell and Carnall (1831), Dames (1868), Gürich (1909) and Ró¿kowska (1962).
Sys tem atic strati graphi cal stud ies were later con ducted by Gunia (1962, 1966a, b, 1968) who de ter mined 182 fos sil taxa of De vo nian ma rine macrofauna, mainly brachi o pods and clams, also Rugosa cor als and stromatoporoids. The most im por tant fos sils are ammonoids which are poorly pre served and not nu - mer ous. Gunia (1968) ac cepted partly Tournaisian age of the Ksi¹¿ con glom er ates based on Lepidodendron sp. found by Zimmerman (1936). That au thor re jected all other Car bon if er - ous datings and con sid ered that the strati graphic in ter val from the Early Frasnian to Tournaisian houses the en tire his tory of the Œwiebodzice Unit (Gunia, 1968).
The next in ter val is at the Visean/Serpukhovian tran si tion, ev i denced in this pa per by an as sem blage of dark, poorly pre - served miospores from Lubiechów and Witoszów Górny. A spec i men of Adiantites antiquus (Ettingshausen) Stur, found dur ing our field work in a rocky block in the Lubiechów Quarry (Fig. 3), may also in di cate this age. A sim i lar re sult was re ported by Krawczyñska-Grocholska (1973) from the Chwaliszów area where a mixed miospore as sem blage was found. There are some pre vi ous Car bon if er ous datings, based on fos sil macroflora and ma rine fauna, and they prob a bly also be long to this strati graphic in ter val. They orig i nate from the vi cin ity of Witoszów Górny, where fos sil clams Posidonia becheri,
Edmondia and Protoschizodus were found in slate roof tiles (Dames, 1868; Bederke, 1924). Some typ i cally Car bon if er ous taxa of macroflora: Mesocamites roemeri (Goeppert) Hirmer, Cala mites tenuissimus Goeppert and Sigillaria minutissima Goeppert were rec og nized from the same quarry (Cramer et al., 1924). Zim mer mann (1936) com pleted the list of iden ti fied flora by Rhodea zygopteris and Lepidodendron sp. Some Car - bon if er ous plant spec i mens from the vi cin ity of Mokrzeszów are in the col lec tion of the Geo log i cal Mu seum of the Uni ver sity of Wroc³aw, in clud ing Ulodendron subdiscophorum Weiss et Sterzel (cat a log no. 287p) and Asterocalamites scrobiculatus (Brongniart) Zeiller (cat a log no. 6374p). Un for tu nately, their or i - gin and ex act lo ca tion are un known. None of these Car bon if er - ous datings were taken into ac count by Gunia (1968).
The great sur prise is, how ever, the palynostratigraphical re - sult in di cat ing the Asturian age, which is ev i denced by well-pre - served, light-col oured miospores found in the Pogorza³a For -
ma tion rocks. This is the third im por tant date in the his tory of the Œwiebodzice Unit, which had not been known ear lier.
The sig nif i cance of each of these three dates is not ob vi ous and re quires dis cus sion.The oc cur rence of dis persed Car bon if - er ous miospores is cru cial in the con text of Car bon if er ous age of stud ied rocks, but the miospore as sem blages in di cate two Car bon if er ous dates. The ap pli ca tion of clas si cal rules of strati - graphic in ter pre ta tion would lead to the con clu sion on the Asturian age of dis cussed rocks, as miospores of this age are the youn gest fos sils. How ever, such a state ment seems to be doubt ful be cause Asturian miospores are very rare in the stud - ied rocks. They were found only in seven out of nearly fifty sam - ples and their fre quency in these pro duc tive sam ples is un even.
Dis tri bu tion of sam ples con tain ing Asturian miospores in the Lubiechów Quarry (Fig. 2C, D) and the Witoszów Górny out - crop (Fig. 5B) is ir reg u lar and cha otic, and can not be ex plained by pro cesses from time of sed i men ta tion.
130 Kamil Pluta and Anna Górecka-Nowak
Fig. 8. Stratigraphic scheme of the Pogorza³a Formation from the southern part of the Œwiebodzice Unit (miospore zonation of the Carboniferous in Europe
according to Clayton et al., 1977 and Owens et al., 2004)
The sub-as sem blage of dark miospores oc curs in all stud - ied rocks, so it is more con ve nient for the strati graphic pur pose, al though these miospores are very poorly pre served. They in di - cate the Late Visean–Serpukhovian age that is con sid ered the age of the stud ied Pogorza³a For ma tion rocks. This con clu sion in te grates well the rocks into the palaeo geo graphi cal sit u a tion and al lows the cor re la tion with rocks oc cur ring in neigh bour ing geo log i cal units – the Intrasudetic Ba sin and the Bardo Unit (Górecka-Nowak and Muszer, 2011). Ac cord ing to this strati - graphic in ter pre ta tion, all De vo nian fos sils in the Œwiebodzice Unit should be con sid ered re worked; how ever, the oc cur rence of Asturian miospores also re quires elu ci da tion.
Redeposition of De vo nian macrofossils has been known for a very long time. Re worked macrofossils were de scribed and de ter mined from lime stone peb bles oc cur ring in the Up per Frasnian con glom er ates (Gunia, 1962, 1966a, b, 1968). All re - main ing De vo nian macrofossils were con sid ered co eval with the rocks and stratigraphically im por tant (Gunia, 1962, 1966a, b, 1968). Ac tu ally, the de gree of macrofossil re work ing is dif fi - cult to es ti mate. Re worked macrofossils prob a bly oc cur also in larger blocks and olistoliths, as de scribed spec i mens of De vo - nian ben thic macrofauna are found in liv ing po si tion (Halamski, 2013). Our ob ser va tions of rocks from the Lubiechów Quarry sug gest that prob a bly at least part of the De vo nian fos sils in mudstones of the Pogorza³a For ma tion are also re worked. It would elu ci date the rea son of some pre vi ous con tra dic tory biostratigraphical in ter pre ta tions, al though this topic re quires fur ther stud ies on macrofossils to elu ci date their strati graphic sig nif i cance, and make a re vi sion of pre vi ous re sults.
The oc cur rence of the Asturian miospores in rocks dated as Visean/Serpukhovian may be ex plained by their mi gra tion in wa ter which has pen e trated al ready con sol i dated rocks of the Pogorza³a For ma tion. The wa ter might use tec tonic cracks which are very com mon in rocks from the Lubiechów Quarry and the out crop near Witoszów Górny. This phe nom e non is called the strati graphi cal leak age (Wil son, 1964; Streel and Bless, 1980) and elu ci dates ir reg u lar dis tri bu tion of Asturian miospores in stud ied rocks. Sim i lar cases that older rocks are con tam i nated by youn ger microfossils, mainly miospores, were de scribed from many lo cal i ties (e.g., Guennel, 1963;
Steemans, 1995). Un doubt edly, the pres ence of the Asturian miospores is a re cord of the fi nal stage of the Œwiebodzice Unit de vel op ment, when this area was al ready up lifted. On its sur - face sed i men ta tion in the con ti nen tal con di tions took place.
Miospores found in the stud ied rocks orig i nated from sed i ments de pos ited then and eroded later. This Asturian stage of the Œwiebodzice Unit his tory was dur ing the Late Variscan vol -
cano-mag matic ac tiv ity (Awdankiewicz and Kryza, 2010; Kryza and Awdankiewicz, 2012; Turniak et al., 2014).
As sem blages of fos sils dis cussed in this pa per re sem ble sim i lar as sem blages found in the Car bon if er ous suc ces sion from the base ment of the Fore-Sudetic Homocline. They are also con sid ered as mixed with great par tic i pa tion of re worked fos sils. In both cases miospore data al lowed proper strati - graphic in ter pre ta tion, ter mi nat ing long-stand ing con tro versy (Górecka-Nowak, 2007, 2008, 2009, 2010; Mazur et al., 2010).
New miospore data prove that geo log i cal his tory of the Œwiebodzice Unit was more com plex than pre vi ously as sumed.
Re sults pre sented in this pa per in di cate that this geo log i cal unit ur gently re quires new multidisciplinary geo log i cal stud ies to elu - ci date its geo log i cal set ting, stra tig ra phy and re la tions to the neigh bour ing units.
CONCLUSIONS
Re sults of the palynostratigraphical stud ies of the Pogorza³a For ma tion from the south ern part of the Œwiebodzice Unit clearly in di cate the Car bon if er ous age of rocks which were re garded be fore as De vo nian based on ma rine fos sils (Gunia, 1968). The miospore as sem blage found in these rocks is mixed. It con sists of two sub-as sem blages of dif fer ent colours and ages. The rocks are con sid ered late Visean/Serpukhovian in age. All older rocks and fos sils found in these rocks are re de - pos ited. The oc cur rence of Asturian miospores in the Visean–Serpukhovian rocks is a re sult of miospore redeposition of strati graphic leak age type (Fig. 8). Ob ser va - tions of miospore colours in di cate that the ther mal event, which oc curred be fore Asturian and prob a bly in two stages. The first one was af ter the Late De vo nian and be fore the Late Visean–Serpukhovian, and the palaeotemperature ex ceeded
~180°C at that time. The sec ond stage was af ter the Serpukhovian and be fore the Asturian, and the palaeotemperature was not higher than 160–170°C. The re - sults of this palaeothermal anal y sis con firm that rocks fill ing the Œwiebodzice Unit are synorogenic.
Ac knowl edge ments. Our stud ies were sup ported by a grant of the Uni ver sity of Wroc³aw 1017/S/ING/16-4. We are grate ful to the re view ers, J. Bek (Czech Acad emy of Sci ences) and P. Filipiak (Uni ver sity of Silesia, Poland), as well as to an anon y mous re viewer for their con struc tive com ments that al - lowed im prov ing this pa per.
REFERENCES
Awdankiewicz, M., Kryza, R., 2010. The Che³miec subvolcanic in - tru sion (Intrasudetic Ba sin, SW Po land): pre lim i nary SHRIMP zir con age. Mineralogia Spe cial Pa pers, 37: 69.
Bat ten, D.J., 1996. Chap ter 26B. Palynofacies and pe tro leum po - ten tial. Amer i can As so ci a tion of Strati graphic Paly nolo gists Foun da tion, 3: 1065–1084.
Bederke, E., 1924. Das Devon in Schlesien und das Al ter der Sudetenfaltung. Fortschritte der Geologie und Palaeontologie, 7: 1–50.
Berg, G., Dathe, E., Zim mer mann, E., 1910. Geologische Karte von Preussen und Benachbarten Bundesstaaten, 1:25 000.
Blatt Friedland in Schlesien, Berlin.
Bröcker, M., ¯elaŸniewicz, A., End ers, M., 1998. Rb-Sr and U-Pb geo chron ol ogy of migmatitic lay ers from the Góry Sowie (West Sudetes, Po land): the im por tance of Mid-Late De vo nian meta - mor phism. Jour nal of the Geo log i cal So ci ety, 155: 1025–1036.
Chorowska, M., 1978. Visean lime stones in the meta mor phic com - plex of the Kaczawa Mts. (Sudetes) (in Pol ish with Eng lish sum - mary). Annales Societatis Geologorum Poloniae, 48: 245–261.
Clay ton, G., Coquel, R., Doubinger, J., Gueinn, K.J., Loboziak, S., Owens, B., Streel, M., 1977. Car bon if er ous miospores of West ern Eu rope: il lus tra tion and zonation. Mededelingen Rijks Geologische Dienst, 29: 1–71.
Cramer, R., Finckh, L., Zim mer mann, E., 1924. Erläuterungen zur geologische Karte, Blatt Schweidnitz: 3–51. Berlin.
Dames, E. 1868. Ûber die in der Umgebung Freiburgs in Nieder-Schlesien auftretenden devonischen Ablagerrungen.
Zeitschrift der Deutschen Geologischen Gesellschaft, 20:
469–508.
Górecka-Nowak, A., 2007. Palynological con strains on the age of Car bon if er ous clastic suc ces sion of west ern Po land. Geo log i cal Quar terly, 51 (1): 39–56.
Górecka-Nowak, A., 2008. New in ter pre ta tions of the Car bon if er - ous stra tig ra phy of SW Po land based on miospore data. Bul le tin of Geosciences, 83: 101–116.
Górecka-Nowak, A., 2009. Palynological data from the Siciny IG 1 and Marcinki IG 1 bore holes and their sig nif i cance in the rec og - ni tion of the Car bon if er ous suc ces sion of SW Po land. Geo log i - cal Quar terly, 53 (2): 167–186.
Górecka-Nowak, A., 2010. Com ple men tary data on the palynostratigraphy of the Car bon if er ous suc ces sion of SW Po - land. Geo log i cal Quar terly, 54 (3): 337–356.
Górecka-Nowak, A., Muszer, J., 2011. Palynology of the up per Visean Paprotnia Beds (Bardo Unit, Pol ish Sudetes). Geo log i - cal Quar terly, 55 (2): 165–180.
Guennel, G.K., 1963. De vo nian spores in a Mid dle Si lu rian reef.
Grana Palynologica, 4: 245–261.
Gunia, T., 1962. Fauna and age of lime stone peb bles from the Culm of Ksi¹¿ (in Pol ish with Eng lish sum mary). Rocznik Polskiego Towarzystwa Geologicznego, 34: 493–523.
Gunia, T., 1966a. Fauna and age of lime stone peb bles from the Culm of Ksi¹¿ (in Pol ish with Eng lish sum mary). Geologia Sudetica, 2: 297–321.
Gunia, T., 1966b. New in ves ti ga tions of the stra tig ra phy and paleogeography of the Up per De vo nian of the Œwiebodzice Unit (in Pol ish with Eng lish sum mary). Z Geologii Ziem Zachodnich:
169–183.
Gunia, T., 1968. On the fauna, stra tig ra phy and con di tions of sed i - men ta tion of the Up per De vo nian in the Œwiebodzice de pres - sion (Mid dle Sudetes) (in Pol ish with Eng lish sum mary).
Geologia Sudetica, 4: 115–220.
Gunia, T., 1985. Geo log i cal po si tion of the Sowie Góry block and its in flu ence on the paleogeography of the Pa leo zoic of Cen tral Sudetes (in Pol ish with Eng lish sum mary). Geologia Sudetica, 20: 83–119.
Gürich, G., 1909. Clymenienkalk von der Conradmühle in Polsnitz bei Freiburg in Schlesien. Abhandlungen der Preussischen Geologischen Landesanstalt, 30: 341–344.
Halamski, A.T., 2013. Frasnian Atrypida (Brachiopoda) from Silesia (Po land) and the age of the eo-Variscan col li sion in the Sudetes.
Geodiversitas, 35: 289–308.
Kaczorowski, M., Wojewoda, J., 2011. Neotectonic ac tiv ity in ter - preted from a long wa ter-tube tiltmeter re cord at the SRC geodynamic lab o ra tory in Ksi¹¿, Cen tral Sudetes, SW Po land.
Acta Geodynamica et Geomaterialia, 8: 1–13.
Krawczyñska-Grocholska, H., 1973. Sporomorph as sem blage in sand stone and siltstone sam ples from Chwaliszów in the Œwiebodzice Dpression (Cen tral Sudetes) (in Pol ish with Eng - lish sum mary). Biuletyn Instytutu Geologicznego, 264: 211–222.
Kryza, R., Awdankiewicz, M., 2012. Am big u ous geo log i cal po si - tion of Car bon if er ous rhyodacites in the Intra-Sudetic Ba sin (SW Po land) clar i fied by SHRIMP zir con ages. Geo log i cal Quar terly, 56 (1): 55–66.
Mazur, S., Aleksandrowski, P., Kryza, R., Oberc-Dziedzic, T., 2006. The Variscian Orog eny in Po land. Geo log i cal Quar terly, 50 (1): 89–118.
Mazur, S., Aleksandrowski, P., Turniak, K., Krzemiñski, L., Mastalerz, K., Górecka-Nowak, A., Kurowski, L., Krzywiec, P., ¯elaŸniewicz, A., Fan ning, M.C., 2010. Up lift and late orogenic de for ma tion of the Cen tral Eu ro pean Variscan belt as re vealed by sed i ment prov e nance and struc tural re cord in the Car bon if er ous fore land ba sin of west ern Po land. In ter na tional Jour nal of Earth Sci ences, 99: 47–64.
Nemec, W., Porêbski, S.J., Steel, R.J. 1980. Tex ture and struc ture of resedimented con glom er ates: ex am ples from Ksi¹¿ For ma -
tion (Famennian-Tournaisian), south west ern Po land.
Sedimentology, 27: 519–538.
Owens, B., McLean, D., Bodman, D., 2004. A re vised palynozonation of Brit ish Namurian de pos its and com par i sons with East ern Eu rope. Micropaleontology, 50: 89–103.
Peryt, T., 1981. Phanerozoic oncoids – an over view. Fa cies, 4:
197–214.
Pia, J., von 1937. Die Wichtigsten Kalkalgen des Jungpaläozoikums und ihre Geologische Bedeutung. Deuxiéme Congres pour l’Avancement des Études de Stratigraphie Carbonifere, 2: 765–856.
Pluta, K., 2012. En vi ron ment and con di tions of sed i men ta tion of Up per De vo nian oncoid lay ers from Œwiebodzice de pres sion (in Pol ish with Eng lish sum mary). MSc. the sis, Wydzia³ Nauk o Ziemi i Kszta³towania Œrodowiska, Uniwersytet Wroc³awski.
Pluta, K., 2016. Onkoidy w depresji Œwiebodzic – zapis kryzysu biotycznego na prze³omie fran/famen (in Pol ish). In: VI Polska Konferencja Sedymentologiczna POKOS 6 – „Granice Sedymentologii” 28.06–01.07.2016, Chêciny-Rzepka (eds. D.
Olszewska-Nejbert, A. Filipek, M. B¹bel and A. Wysocka):
169–170.
Porêbski, S.J., 1981. Œwiebodzice suc ces sion (Up per De vo - nian-low est Car bon if er ous): a prograding mass flow dom i nated fan-delta com plex (in Pol ish with Eng lish sum mary). Geologia Sudetica, 16: 101–192.
Porêbski, S.J., 1984. Clast size and bed thick ness trends in resedimented con glom er ates: ex am ple from a De vo nian fan-delta suc ces sion, south west Po land. Ca na dian So ci ety of Pe tro leum Ge ol o gists, Mem oir, 10: 399–411.
Porêbski, S.J., 1987. Œrodowisko depozycyjne i wp³yw tektoniki na sedymentacjê dewonu-karbonu w depresji Œwiebodzic (in Pol - ish). Przewodnik LVIII Zjazdu PTG, Wa³brzych: 114–130.
Porêbski, S.J., 1990. On set of coarse clastic sed i men ta tion in the Variscan realm of the Sudetes (SW Po land): an ex am ple from the Up per De vo nian-Lower Car bon if er ous Œwiebodzice suc ces - sion. Neues Jahrbuch für Geologie und Paläontologie Abhandlungen, 179: 259–274.
Ró¿kowska, M., 1962. The De vo nian coral lime stones by the Daisy Lake of Mokrzeszów (in Pol ish with Eng lish sum mary). Biuletyn Informacyjny Polskiego Towarzystwa Mi³oœników Nauk o Ziemi:
3–5.
Schindewolf, O.H., 1925. Einige Bemerkungen über das Sphaerocodien-Konglomerat von Alt-Liebichau bei Freiburg in Niederschlesien. Zeitschrift der Deutschen Geologischen Gesellschaft, 77: 84–95.
Steemans, P., 1995. Si lu rian and Lower Emsian spores in Saudi Ara bia. Re view of Palaeobotany and Palynology, 89: 91–104.
Streel, M., Bless, M., 1980. Oc cur rence and sig nif i cance of re - worked palynomorphs. Mededelingen Rijks Geologische Dienst, 32: 69–80.
Teisseyre, H., 1948. Sprawozdanie z prac geologicznych wykonanych w Sudetach w r. 1947 (in Pol ish). Badania fizjograficzne nad Polsk¹ Zachodni¹, 1: 6–47.
Teisseyre, H., 1952. Geo log i cal struc ture of the north ern re gion of Wa³brzych (in Pol ish with Eng lish sum mary). Biuletyn Instytutu Geologicznego, 62: 5–58.
Teisseyre, H., 1956a. Œwiebodzice De pres sion as a geo log i cal unit (in Pol ish with Eng lish sum mary). Biuletyn Instytutu Geologicznego, 106: 5–36.
Teisseyre, H., 1956b. Sed i men ta tion of the Up per De vo nian of Pogorza³a and Witoszów (Mid dle-Sudetes) (in Pol ish with Eng - lish sum mary). Acta Geologica Polonica, 6: 227–251.
Teisseyre, H., 1968. Stra tig ra phy and tec ton ics of the Œwiebodzice de pres sion. Biuletyn Instytutu Geologicznego, 222: 71–106.
Teisseyre, H., Smulikowski, K., Oberc, J., 1957. Geologia Regionalna Polski (in Pol ish). Tom III, 1: 1–300.
Timmermann, H., Parrish, R.R., No ble, S.R., Kryza, R., 2000.
New U-Pb monazite and zir con data from the Sudetes Moun - tains in SW Po land: ev i dence for a sin gle-cy cle Variscan orog - eny. Jour nal of the Geo log i cal So ci ety, 157: 265–268.
Turniak, K., Mazur, S., Domañska-Siuda, J., Szuszkiewicz, A., 2014. SHRIMP U-Pb zir con dat ing for granitoids from the
132 Kamil Pluta and Anna Górecka-Nowak
Strzegom–Sobótka Mas sif, SW Po land: Con straints on the ini - tial time of Permo-Me so zoic litho sphere thin ning be neath Cen - tral Eu rope. Lithos, 208: 415–429.
Urbanek, Z., 1975. On the oc cur rence of Up per De vo nian rocks in the epimetamorphic com plex of the Kaczawa Mts. (West ern Sudetes). Bul le tin de l‘Academie Po lo naise des Sci ences de la Terre, 22: 167–172.
Urbanek, Z., 1978. The sig nif i cance of the De vo nian cono dont fau - nas for the stra tig ra phy of the epi-meta mor phic rocks of north-east ern part of the Góry Kaczawskie. Geologia Sudetica, 13: 7–27.
Van Breemen, O., Bowes, D.R., Aftalion, M., ¯elaŸniewicz, A., 1988. De vo nian tectonothermal ac tiv ity in the Sowie Góry gneissic block, Sudetes, SW Po land: ev i dence from Rb-Sr and U-Pb iso to pic stud ies. Annales Societatis Geologorum Poloniae, 58: 3–19.
Wil son, L.R., 1964. Re cy cling, strati graphic leak age and faulty tech niques in palynology. Grana Palynologica, 5: 425–436.
Wojewoda, J., 2014. Œwiebodzice Unit re vis ited – ki ne matic, struc - tural and fa cial evo lu tion till now. Ab stracts of 15th Czech-Pol ish Work shop on Re cent Geodynamics of the Sudetes and the Ad - ja cent Ar eas, Karlov pod Pradedem: 63–64.
Wojewoda, J., 2016a. Basen œwiebodzki – granice, architektura osadów i ewolucja strukturalna (in Pol ish). In: VI Polska Konferencja Sedymentologiczna POKOS 6 – „Granice Sedymentologii” 28.06–01.07.2016, Chêciny-Rzepka (eds. D.
Olszewska-Nejbert, A. Filipek, M. B¹bel and A. Wysocka):
142–144.
Wojewoda, J., 2016b. About the need to de velop the sec ond edi - tion of the de tailed geo log i cal map of the Sudetes at the scale of 1:25,000 – ex am ples of a re vi sion of the geo log i cal pat tern us - ing the LIDAR Dig i tal El e va tion Mod els (in Pol ish with Eng lish sum mary). Przegl¹d Geologiczny, 64: 597–603.
Zim mer mann, E., 1911. Konglomerat mit Sphaerocodium und Spirifer verneuili aus dem Kalkgraben bei Liebichau unweit Freiburg in Schlesien. Zeitschrift der Deutschen Geologischen Gesellschaft, 63: 35–36.
Zim mer mann, F., 1936. Das Al ter der Gneiskonglomerate des Fürstensteiner Kulms. Jahrbuch der Preussischen Geologischen Landesanstalt, 56: 205–207.
Zinkiewicz, J., 1973. Ab so lute age de ter mi na tion of rocks by Rb-Sr method (in Pol ish with Eng lish sum mary). Przegl¹d Geologiczny, 21: 251–254.
Zobel, J., Carnall, R., 1832, Geognostische Beschreibung von einem Theile des Nieder-Schlesischen, Glätzischen und Böhmischen Gebirges. Archiv für Mineralogie, Geognosie, Bergbau und Hüttenkunde, 4: 3–173.
¯elaŸniewicz, A., Aleksandrowski, P., Bu³a, Z., Karnkowski, P.H., Konon, A., Oszczypko, N., Œl¹czka, A., ¯aba, J., ¯ytko, K., 2011. Regionalizacja tektoniczna Polski. Komitet Nauk Geologicznych PAN: 1–60.
