Annales Societatis Geologorum Poloniae (2013), vol. 83: 113-132. PROVENANCE OF LOWER CRETACEOUS DEPOSITS OF THE WESTERN PART OF THE SILESIAN NAPPE IN POLAND (OUTER CARPATHIANS): EVIDENCE FROM GEOCHEMISTRY Patrycja WÓJCIK-TABOL & Andrzej ŚLĄCZKA Institute of Geological Sciences, Jagiellonian University, Oleandry 2a, PL-30-063, Krakow, Poland; e-mails: p.wojcik-tabol@uj.edu.pl, andrzej.slaczka@uj.edu.pl Wójcik-Tabol, P. & Slączka, A., 2013. Provenance of Lower Cretaceous deposits of the western part of the Silesian Nappe in Poland (Outer Carpathians): evidence from geochemistry. Annales Societatis Geologorum Poloniae, 83: 113-132. Abstract: The turbiditic to hemipelagic, fine-grained deposits ofthe Hradiste Formation (Hauterivian, 132 Ma) to the Lhoty Formation (Albian-Cenomanian, 99 Ma) in the western part of the Silesian Nappe (Polish Outer Car- pathians) were studied mineralogically and geochemically to determine if the main factors controlling the che- mistry of the sedimentary material can be attributed to provenance, or to post-depositional processes. A high degree of weathering of the source rocks is indicated by the chemical index of alteration (CIA) that varies from 75.98 to 89.86, and Th/U ratios (~4 with outliers at 1.85 and >6). The co-occurrence of rounded and unabraded grains of zircon and rutile, the enrichment in Zr and Hf, as well as the high Zr/Sc ratios suggest that the Hradiste and Verovice Formations contain recycled material. Plots of La/Th versus Hf and Th against Sc show that samples occur in the field of felsic and mixed felsic/basic sources. On a ternary La-Th-Sc diagram, all of the sediments studied are referable to the continental island-arc field. The European Plate, as an alimentary area, has a mosaic structure consisting of Cadomian and Variscan elements. The Proto-Silesian Ridge was detached from the conti- nent, because of rifting. Therefore, it could have corresponded to a continental island arc. The concentrations of Fe and trace metals (e.g., Mo, Au, Cu) in the Verovice Formation and silica and potassium additions to the Verovice and Lhoty Formations, as well as the fractionation of REE, and Nb, Ta, Zr, Hf, and Y can be explained by the action of basinal brines. The fluids were of hydrothermal origin and/or were released, owing to the dewatering of clay minerals. Diagenetic processes could have exerted a greater influence on sedimentary rock chemistry than the provenance and sedimentary processes. A distinction between primary, terrigenous elements and those changed diagenetically is necessary for the reliable determination of provenance. Key words: Silesian Nappe, Lower Cretaceous, mineral composition, geochemistry, provenance, diagenesis. Manuscript received 17 December 2012, accepted 28 October 2013 INTRODUCTION The source rocks of the turbiditic sedments of the Outer Carpathians have been investigated for many years and are reasonably well defined (e.g., Książkiewicz, 1962; Poprawa et al., 2002; Cieszkowski et al., 2012). The exter- nal basins, such as the Silesian, Subsilesian and Skole bas- ins, were supplied generally by SE- and NE-flowing palaeo- currents from the European Platform and the Proto-Silesian Ridge (known earlier as the Silesian Cordiltera), which were built of continental crust (Slączka, 1976; Strzeboński et al., 2009; Slączka et al., 2012). Exotics of crystaltine rocks (gneisses, granites, igneous rocks with a porphyrytic texture, mica schists) and sedimentary rocks, such as: Car- boniferous sandstones and coals, Triassic and Jurassic car- bonates and Lower Cretaceous (Urgonian-type) limestones (Cieszkowski et al., 2012) indicate that the detritus was de- livered from the crystalline basement and its sedimentary co- ver. This is supported by the heavy minerals assemblage (garnet, rutile, tourmatine, and zircon, as well as apatite, monazite and epidote), which was exammed in samples from the sandstones and conglomerates of the turbiditic suc- cession (Wieser, 1948; Unrug, 1968; Burtan et al., 1984; Winkler and Slączka, 1992; Grzebyk and Leszczyński, 2006). The rounded grains of heavy minerals occur together with unabraded crystals, indicating a provenance from both the ciystanine basement and the older sedmentary rocks. Reworkmg of the siliciclastic material and redeposition is also documented in numerous olistostromes that occurred during every stage in the evotution of the flysch batin (Cieszkowski et al., 2012). The geochemtstry of fine-grained sedments can pro i vide information regardmg provenance, as well as the tec- tonic setting and the palaeo-environmental evolution of sed- 114 P. WÓJCIK-TABOL & A. ŚLĄCZKA Fig. 1. Location of study area within context of main geo logical units. A - simplified tectonic scheme of Alpine orogens; PKB - Pieniny Klippen Belt (after Kovac et al., 1998, modified); B - central part of Polish Carpathians (after Oszczypko & Oszczypko-Clowes, 2009); C - Geological map of area around Lipnik (after Geroch & Nowak, 1963; modified) and Rzyki (after Uchman and Cieszkowski, 2008) PROVENANCE OF LOWER CRETACEOUS DEPOSITS 115 imentary basins. The chemical composition of the sedi- ments is a function of several variables, including the nature of the parent rocks, the weathering processes active in the source area, sorting during transportation, reworking of older sediments, as well as sedimentary and post-sedimen- tary conditions (e.g., Nesbitt and Young, 1982; Johnsson, 1993; McLennan et al., 1993; Fedo et al., 1995). It is neces- sary to consider the diagenetic processes that involved the alteration of unstable minerals and the precipitation of new phases, usually associated with chemical changes (Gonzä- lez-Alvarez and Kerrich, 2010). The purpose of this study was to characterise and deter- mine the provenance of material, deposited in the Silesian Basin between Hauterivian and Cenomanian times (132-99 Ma according to IUGS 2012). Special attention was given to the fine-grained deposits, the origin of which was deter- mined by means of geochemical data. The geochemical fin- gerprints of the source rocks were compared to the studies of heavy minerals and the petrology of exotic rocks that have been widely prei ented by other investigators. This study took into consideration the influence of weathering of the parent rocks and the sorting and recycling of detritus as governing the chemical composition of siliciclastic deposits and changing their chemistry relative to that of the fresh source rocks. Furthermore, diagenetic processes must be taken into account as influencing on the chemical composi- tion of sedimentary rock. This investigation attempted to determine if the main factors responsible for the chemical composition of the material studied are reiated to prove i nance, or to post-depositional processes. Samples were collected from the Lipnik and Rzyki sec- tions, situated in the W part of the Silesian Nappe (Fig. 1). The Lipnik section (Geroch and Nowak, 1963) is located in the E part of the city of Bielsko-Biała and exposes a contin- uous section from the Cisownica Shale Member (Hauteri- vian) that represents the lower part of the Hradiste Forma- tion (Golonka et al., 2008) through the Verovice Formation (Lower Barremian-Lower Aptian, according to Gedl, 2003) and the Lhoty Formation (Albian-Cenomanian), up to the Godula Beds (Turonian) with almost no tectonic disturbance. In Rzyki village, S of Andrychów, part of the Cretace- ous success ion is exposed along the stream Wieprzówka (Cieszkowski et al., 2001; Uchman and Cieszkowski, 2008). The profile studied represents the Barremian-Lower Albian Verovice Formation and the lower part of the Lhoty Formation (Gedl, 2003), strongly tectonized. GEOLOGY OUTLINE The Outer Carpathians form the NE part of a great mountain arc, which stretches for more than 1,300 km (Fig. 1A). Structurally, the Outer Carpathians consist of several nappes and thrust sheets: the Magura Nappe, outcropping in the south, the Fore-Magura group of nappes, and the Sile- sian, Sub-Silesian and Skole nappes, exposed in sequence toward the NE (Książkiewicz, 1968; Kovac et al., 1998; Slączka et al., 2006). The Outer Carpathian Flysch com- prises deep-water sediments, deposited mainly by mass gra- vity flows and particularly by turbidity currents. The Carpa- thian tectonic units were thrust from the S on to each other and over the North Euiopean Platiorm (Golonka et al., 2006; Oszczypko et al., 2006). The study area is situated in the W part of the Silesian Nappe, in the Polish Outer Carpathians (Fig. 1B). Sedimen- tation in the W part of the Silesian Basin started in the Late Jurassic (Bieda et al., 1963; Slączka et al., 2006) and began with dark grey, calcareous mudstones (Lower Cieszyn Beds = Vendryne Formation after Golonka et al., 2008) that pass upwards into grey marls and calciturbidites with calcareous, pelagic intercalations of the Tithonian-Beriassian Cieszyn Limeitone Formation (Książkiewicz, 1951; Bieda et al., 1963). The clastic material was derived from the adj acent calcareous platforms. The Cieszyn Limestone Formation is covered by dark grey and black, calcareous shales with si- deritic mudstone (Upper Cieszyn Shales, equivaient to the Cisownica Shale Member, after Golonka et al., 2008) that represent the lower part of the Hradiste Formation, dated as Valanginian-Hauterivian (after Golonka et al., 2008). Lo- cally, within the upper part of the Hradiste Formation, there are intercalations of thick-bedded sandstones and conglom- erates (Piechówka Sandstone Member, after Golonka et al., 2008). In the Barremian part, the calcareous sediments pass upwards into the black shales of the Verovice Shale, dated as Barremian-Aptian (e.g., Olszewska, 1997) and Barre- mian-Early Albian (Koszarski and Nowak, 1960; Geroch and Nowak, 1963). In the Bielsko-Biała region, the age of the succession ranges from the Late Barremian to Late Ap- tian (Gedl, 2003). Golonka et al. (2008) proposed the limi- tation of the Verovice Formation to the non-calcareous black shales, excluding the lowermost, partly calcareous, black shales that should be assigned to the Hradiste Forma- tion. This sequence records the early stages of development of the Silesian Batin. The latter sequence locally begins with thick-bedded sandstones and conglomerates that pass upwards into thin- and medium-bedded quartzitic sand- stones, intercalated with black, greenish shales (the Albian- Cenomanian Lgota Beds of Bieda et al., 1963; the Lhoty Formation after Golonka et al., 2008; Fig. 2B). They repre- sent deposits derived mainly from the northern margin of the basin and from intrabasinal ridges during their uplift and corresponding sea-floor subsidence (Książkiewicz, 1962; Oszczypko, 2006). Deposition in the lower part of the Early Cretaceous occurred during relatively low sea levels and was characterized by a slowing rate of sedimentation from 165 to less than 40 m/My (Poprawa et al., 2006). Deposition of the siliciclastic Lhoty Formation ociurred during ini creases in oceanic level and was accompanied by an accel- eration in sedimentation rate (31-63 m/My; Oszczypko, 2006). This succession is part of the widespread Early Creta- ceous Flysch within the Alpine Domain that is characterized by the presence of black, pelitic deposits (Slączka, 1976; Lemoine, 2003). Usually, these sediments are connected with basins, underlain by oceanic crust, and mark the con- tact between internal and external zones of the Alpine chains in Europe (Puglisi, 2009). In the case of the external Carpathian basins (Silesian, Subsilesian and Skole basins), the sedimentation of black, pelitic sediments took place dur- ing extensional fault movements that embraced the S part of 116 P. WÓJCIK-TABOL & A. ŚLĄCZKA Fig. 2. Lithostratigraphy. A. Lithological log of Rzyki and Lipnik sections; B. Lithostratigraphy of Jurassic-Cretaceous Proto- Silesian Basin; tesch. - igneous rocks of teschenite association (after Golonka et al., 2008, modified) PROVENANCE OF LOWER CRETACEOUS DEPOSITS 117 Fig. 3. Dark sediments of upper part of Hradiste and Verovice formations in both studied exposures. A. Lower Cretaceous black shales exposed in Lipnik stream; B. Wieprzówka stream section. C. Dark marly shales interbedded with light grey marls of Hradiste Formation in Lipnik section. D. Black shales of Verovice Formation in Lipnik section. E. Fissile black shales with ferrous staining of the Verovice Formation in Lipnik section. F. Black shales intercalated with fine-grained, siliceous sandstones in upper part of Verovice Formation. G. Siderite lenses exposed in Rzyki section (Verovice Formation). H. Burrows filled with fine-grained sandstones in Lipnik section (Vero- vice Formation) the North European Platform. This extensional movement opened and gradually widened the sedimentary basins until the Aptian (Golonka et al., 2006; Oszczypko et al., 2006). Generally, these basins were elongate and narrow (less than 200 km) and 2000-4000 m deep. The Silesian Basin was in- fluenced by magmatism, lasting through 20 Ma from Titho- nian/Beriassian to Barremian/Aptian (Ivan et al., 1999; Lu- cińska-Anczkiewicz et al., 2002; Grabowski et al., 2004; Oszczypko et al., 2012). Hydrothermal activity since the Albian was mentioned by Geroch et al. (1985). At the con- tact with sedimentary host rocks, thermal metamorphism gave rise to hornfels. Igneous bodies and sediments are cut by white to pinkish hydrothermal veinlets. Hydrothermal mineralization is represented by Ca-Fe-Mg carbonates, quartz, chlorite and sulphides (Dolnicek et al., 2010, 2012). Sections studied The complete section of the Lower Cretaceous part of the Silesian Nappe is exposed in the Lipnik stream, E of Bielsko-Biała (Figs 1C, 3A). The section is 500 m long and exposes continuous sequences from the Cieszyn Limesto- nes Formation to the Godula Beds, with almost no tectonic disturbances, unconformities, hiatuses or repetitions (Fig. 2A; Geroch and Nowak, 1963). The samples labelled LP were coll ected from the upper part of the Hradiste Forma- 118 P. WÓJCIK-TABOL & A. SLĄCZKA Fig. 4. Lhoty Formation, as seen in Rzyki and Lipnik sections. A, B. Uppermost Lhoty Formation at tectonic contact with Variegated Shales in Wieprzówka stream. C. Mikuszowice Chert developed as medium-bedded siliceous sandstones with green shales in Lipnik sec- tion. D. Thin- and medium-bedded, glauconitic sandstones intercalated with grey to black, non-calcareous shales of middle part of Lhoty Formation exposed in quarry near Wieprzówka stream. For explanation, see Fig. 1C tion, from the Verovice Formation and from the Lhoty For- mation. The Aptian Verovice Formation and the overlying Lhoty Formation (Albian-Cenomanian; Cieszkowski et al., 2001) are well exposed and were sampled (samples desi g- nated R and RZ) along the stream Wieprzówka in Rzyki vil- lage, S of Andrychów (Figs 1C, 2A, 3B). In the Lipnik section, the Hradiste Formation is compo- sed of dark, marly shales, interbedded with light grey shales, and with rare, thin int ercalations of grey marls and black, micaeous mudstones (Fig. 3C). This formation grad- ually passes into the Verovice Formation. The lowermost part of the Verovice Formation consists of black, weakly calcareous shales (Fig. 3D). The Verovice Formation be - comes more siiiceous up-section and is repre tented by a succession of non-calcareous, siliciclastic turbidites, includ- ing: (1) fissile black shales with ferrous staining (Fig. 3E), interbedded with sideritic mudstone layers (samples: RZ 1-2/07; Fig. 3G), and fine-grained sandstones (sample RZ 2); and (2) hemipelagic, black shales in the upper part of section, intercalated with fine-grained, siliceous sandstones (Fig. 3F-H). The lower part of the Lhoty Formation in the Lipnik section consists mainly of fine-and coarse-grained, thick- bedded glauconitic sandstones, with intercalations of grey, non-caliareous shales, while the Rzyki section iniludes only sporadic intercalations of thick-bedded sandstones. The middle part of the Lhoty Formation consists of blu- ish grey, thin- and medium-bedded, glauconitic, quartzitic sandstones with parallel lamination and cross-lamination, intercalated with grey to black, non-calcareous shales (Fig. 4D). The upper part of the Lhoty Formation, exposed in the Wieprzówka stream, is developed as thin- to medium-bed- ded, black, quartzitic sandstones, intercalated with dark grey, fissile shales (Fig. 4A, B). PROVENANCE OF LOWER CRETACEOUS DEPOSITS 119 Fig. 5. Microfacies of material studied (all images under transmitted light, in parallel nicols if not stated differently). A, B. Mudstones of Hradiste Formation with laminas of fine-grained sandstone (Qz - quartz, Cb - carbonates, Glt - glauconite, OM - organic matter, Ms - muscovite, f - foraminiferids). C, D, E. Poorly rounded heavy minerals (= HM) from Hradiste Formation (Tur - tourmaline; Ky - kyan- ite). F, G. Burrows filled with grey, quartzitic sandstones in siliceous shales of Verovice Formation (G - crossed nicols). H. Recrystallised tests of foraminiferids in mudstones of Verovice Formation. I, J. Heavy minerals (= HM) from Verovice Formation. K. Dark biotur- bations in green shales of Lhoty Formation. L, M. Conglomerate of Lhoty Formation, extraclasts of felsic igneous and metamorphic rocks and limestones containing fragments of echinoderms (crossed nicols) Green, spotted, fissile shales, intercalated the medium- bedded siiiceous sandstones, (Fig. 4C) are typical for the shales of the uppermost part of the Mikuszowice Cherts (upper part of the Lhoty Formation). ANALYTICAL METHODS Microfacies were investigated in thin-section, using an optical microscope, the Nikon ECLIPSE, E 600 POL. Every rock sample was hand-pulveri sed, using a ceramic mortar and pestle, to the fraction passing through a 200-mesh sieve. A classical whole-rock analysis for 11 major oxides (SiO2, Al2O3, Fe2O3, MgO, CaO, Na2O, K2O, TiO2, P2O5, MnO, &2O3) by ICP-emission spectrometry followed lithium bo- rate fusion and dilute acid digestion of a 0.2 g sample pulp. ICP-OES analyses of maj or oxi des package included loss on ignition (LOI), which is the weight difference after igni- tion at 1000°C. Rare earths and refractory elements were re- ported after lithium borate decomposition to give the total abundances. The amounts of precious metals, base metals and their as so ci ated path finder el e ments were ob tained from aqua regia digestion (ACME Analytical Laboratories, Ltd., 2013). The detection limits and the standards used are given in Table 1. The maj or, minor and trace elements in the mateiial studied were compared to those in the standard sediments, Post-Archean Austraiian Shale (PAAS, after Tayior and McLennan, 1985) and upper continental crust (UCC, after Rudnick and Gao, 2003; Hu and Gao, 2008). The Eu anom- aly expressed by the Eu/Eu* ratio was calcuiated, using Eu/Eu* = Eun /(SmN x GdN)°'5 ratio, where N is the ele- ment content, normalized to UCC. The inter-elemental rela- tionship was evaluated, using Pearson’s correlation factor (r). An assumption is that an element positively correiated with Al2O3 has a terrigenous derivation. Aluminum is the most important element, which stays inert in biological and diagenetic processes. An additional advantage of using Al is its low abundance in seawater and high concentration in aluminosilicates. The chemical index of alteration (CIA; Nesbitt and Young, 1982) was used to determine the degree of weather- ing of the source area. The index is calculated, using molec- uiar proportions in the foliowing equation: CIA = [Al2O3/ (Al2O3 + CaO* + Na2O + K2O)] x 100. The degree of wea- thering can be presented on an A-CN-K (Al2O3 - CaO* + Na2O - K2O) triangul ar plot (Nesbitt and Young, 1984). CaO* is the amount of CaO incorporated in the silicate frac- tion. If CaO has an affinity to carbonates and LOI is low, and there is no CO2 and/or P2O5, the use of Na2O as a sub- stitute for (CaO* + Na2O) is considered to be valid (cf. McLennan, 1993; Hofer et al., 2013). A correction for K en- richment can be made by the projection of lines from the K apex through the data points to the ideal weathering line and reading the value off the CIA axis (Fedo et al., 1995). RE SULTS Microfacies The marly shales of the Hradiste Formation contain silt-sized grains of quartz, flakes of phyllosilicates, and indi- Major and trace element geochemistry for Lower Cretaceous deposits recovered from Rzyki and Lipnik sections of Silesian Napp 120 P. WÓJCIK-TABOL & A. ŚLĄCZKA A H 0 0 CN os wo os 0 OS wo © ro wo ro © © © © © © © © © © © © U3 © © u no 0 O wo CN ro ro so © © CN © 00 "T3 © ro © ro © © © OS wo ip © © PW © © G u rb wb sd rb wb rb G Ö © G 0 rb G wb G G © © © G rb © ro © rb p so "T3 wo r- 00 CN Os CN wo ro so 0 ro 1.5 ppb DO O O O O O O O 0 so SO © © 0 © © © © © © © © © © © © © © < OO OS wo CN ro CN ip p © © CN ro "T3 © © © © © © © so rb © © © T3 T3 © © 00 < CN OO sd G rb © © © wb 0 © rb sd wb o-l © © of © G © 0 0 od © od Ph SO "T3 r- CN SO 0 03 CN CN wo ro 00 0 CN 0 Lhoty Formation SO WO r- so CN SO O •d- © CN © CN OS 00 wo 00 © © © © © © © © © © © © © © © © so O OO 0 os OO CN ro r- © © ip © r-j 00 © so WO © r-; so G WO 00 wo r-; © od CN © wo so G os •'t of G Ö of 0 © G © © SO © od 00 rb G r- o-l © G G © © © © so sd a* SO r- OS WO ro wo ro wo OS SO CN wo CN r- CN © CN 00 wo CN wo © © © © 0 © © © © © © © © © © © CN of wo CN SO ■p ro r-; SO © © OO © CN so © OS so © •d- wo CN G wo © of so of of © wo © of of G rb •d- Ö rb Ö © © so © © r- © 00 © rb G © © G rb © © of od wb a- SO r~- •d- ro CN of CT\ r- CN OS OO ro CN OO © CN CN CN wo © © © © © © © © © © © © © © wo Ph sd ro OS r-j of ro O SO © 3 ip © OS © © OS •d; © ip SO •d; CN Os Os © CN © © WO r-; Os G so sd rb Ö Ö rb Ö © © G © © 00 © 00 G G o-l 00 rb o-l G © © wb of G wb r- OS OS CN wo OO SO ON CN CN OS CN O r- ro © CN © CN wo © © © © © © © © © © © © © © wo Ph of ■d; CN ro ■d; ro of r-; © © ro © OS SO © OS ■d- © r-; ip CN •d; CN of SO r~- © © Os © wo of G of G rb Ö Ö rb Ö © © 00 © © © © 00 sd rb rb •d- G G rb G G sd © © © od G sd so OO r- •d- OS CN CN wo r- CN wo OS so ro wo CN •d- SO © ro CN ro os © © © © © © © © © © © © © © © © CN Ph O ro os CN ro OS wo © © sd © CN CN © r-; © © © CN © •d; 00 Os ro © ip WO wo wo © r-; WO G CN rb G Ö Ö G Ö © © © © o-l © wb rb G rb © 00 o-l © o-l G of of © © G G © wb r- r~- SC r- © ro wo SO OO os r- WO •d- CN ro wo CN © CN ro os WO OO © © © © © 0 © © © © 0 © © so Ph of CN ■d; ip OO ro OS ip © © •d; © CN wo © SO wo © © WO ip G OS SO wo of ro © © © CN ro r-; G 3 sd rb Ö Ö rb Ö © © G © © so © OO sd wb •d- wb 00 OS © G G G o-l © © rb ro od G r- OS SO ro so CN OO 0 r- os r- r- © •d- 00 ro ro © © © © © © © © © © © © © © © © os CN of 0 ro wo o-; wo of ip © 3 os © WO CN © wo © © ro •d; CN •d; CN SO CN r-; CN CN 00 ro so P«H rb sd •d- Ö G 0 © © 00 © © •d- © wb CN G rb •d- © G G wb o-l © © sd so sd so 00 00 CN CN of OO •d- CN OO •d- •d" wo OO ro © •d- wo CN ro ro © © © © © © © © © © © © © © © © P«H r- so of SO r-; sc sc r-; © © wo © © ro © wo SO © CN wo ro CN of ro of od © © of OS ip ip 3 G rb Ö Ö G Ö © © G © 00 © wb rb rb rb •d- G G of o-l sd od sd 00 CN wo wo wo •d- 0 ro 0 OO so ro © ro ro 00 •d- © © © © © © © O © O © © © © r- OO Os r-; OS OS ■d; r-; so © © OO © CN Os © ip © wo Os •d; © © wo CN 00 © © © of of 00 a wb wb rb Ö Ö rb Ö © © so © © wb © G sd wb rb rb •d- G © o-l © © wb o-l wb G so r~- os wo ro CN sc r- of ro ro wo so 0 so OO r- © CN WO 0 ro ro © © © © © © © © © © © © © © © © OS p OO so rb OS r-; ro rb wo © © ro © CN wo © wo SO © OS rb G •d; WO ip CN 00 ro CO © wo o-l CN © rb 00 G Ö Ö © © G © © 00 © wb G G CN rb © o-l G G G © © CN G G a so r- 00 © so Verovice Formation 0 so so so r- OO OO wo wo © ro os wo 00 © © © © © © © © © © © © © © © © CN SO SO O ro OS OS ■d; CN r-; © © wo © OS CN © so OS © sq ■p OO 00 CN OO OS 00 of 00 sq of © ro of a O G wb Ö Ö rb Ö © © o-l © © OO © 00 •d- rb rb wb •d- rb rb G of o-l © © of of od SO r- os CN •d- ro ro r- of 0 r- CN CN so OS wo CN © ro 00 © OS © © © © © © © © © © © © © © © 0 © al wo OS 00 CN ■d; G ■d; © © wb © © © © r-; OS © © OS © ■p ro ro rb of 00 rb ro WO 00 ro of CN wb G Ö Ö Ö © © © 00 © wb G © rb © © rb © 00 o-l of © © G od wb r- so © 00 00 CN of r- of O OS •d- wo CN OO OS SO © wo os os CN © © © © © © © © © © O © © © © © p of of OO •d; ■d; •d- CN ■d- © © os © ro •d- 0 o-l 00 © so OS 00 ■p wo ip © © sq wo wo wo OS sq r-; CN sd OS G G rb Ö Ö © © G © © 00 © WO G © sd G © G of o-l of rb © © CN od wb a SO © wo © wo CN of OO CN so OO r- os OO CN © •d- ro r- © © © © © © © © © © © © © © wo o of O os 0 CN •d- CN •d- © © r- © 00 r~- ro OS © © wo 00 G wo © OS sq OS CN 00 wo of Os © p rb G rb Ö 0 G Ö © © SO © © © © G CN rb rb © sd 00 © 00 G G G G © © wb G G a r- 00 © r~- OS © CN CN so r- CN r- 0 •d- wo r- r- OS CN © •d- 00 r- © os © © © © © © © © © © © © © © © © of of O of ro SC •d- O'; •d- © © SO © © CN © ip G © so ro 00 os so © rb r-; WO CN so wo © Os so a of rb Ö Ö 0 © © © 00 © wb G 0-1 o-l G © 00 od o-l rb © CN G wb r- r- so r- os 00 of wo OS OO 0 CN 0 OS ro © wo r- r~- •d- © © © 0 © © © © © © © © © © of ro OS r-; ro wo of os CN os © © OO © r- wo © 00 OS © © wo SO 00 •d; wo © 00 00 © of OS © ro wo a o-l 00 G Ö Ö rb Ö © © o-l © © © © © G wb © ro rb of of G wb © © G of © WO 00 CN so 00 ro of wo OO r- O OO OO © SO r- © •d- © © © © © © O © © © © © © © © © © OJ ro so Os ■d; OS OO r- © © •d- © © OS r- 00 CN © 00 CN © © ro of of 00 © r~- wo © CO so © a^ G rb Ö Ö G 0 © © so © © © wb wb wb OO G sd rb rb © wb © © so G od o-l so 00 © CN CN ro ro r- CN CN © r- wo © © © © © © 0 ro of OS •d- r- os wo ro os 3 ©" © ro CN © © © ip © © © CN wo © © © OO © © © © so Ph rb G CN wo 0 CN OO ro © V 00 © © so © SO © ip WO rb wb wo 00 so wb sd © ro sd OS G OO G Ö Ö Ö Ö Ö G © 00 © •d- sd G 00 ro ro © of G © G © CN G ro CN OO OS wo CN •d- r- OO © © © os © © © © © © © © © © © © © © © © os Ph rb ■d; CN OS SO •d- 00 •d- © © •d; 3 SO SO © ip wo © wo OS ip 00 r~- so of of r-; CN of OS os CO ro G r- G Ö Ö Ö 0 © © 00 © © G © wb rb 00 G o-l rb so © od rb G G G © © CN o-l wb oc so r- 00 of O CN wo wo OS 0 CN SO OS ro © ro so •d- © © © © 0 © © © © © © wo © © Ph wb 0 CN sc r-j of O wo © © •d; © wo ro © os © r-; so OS © so © 00 © CN © © © r- G SO rb of Ö G Ö © © © © G © G wb G G G © G rb SO G © V od of sd 00 os 00 os OS CN CN wo ON SO OS WO SO so wo r- r- CN © •d- •d- © © © © © © © © © © © © © © © © r-; CN •d; SO p 3 sc r-; © © •d; 3 SO Os © ro © ro ■d- © 00 wo r-; ip of OS of © © wb of OO G sd wb Ö Ö G 0 © © o-l © © G © G sd wb wb © G © of of SO G ro OS o-l SO 00 os CN © r- of OS CN •d- CN wo OO os CN © © ro ro © © © © © © © 0 O 0 © © © © © © CN OO wo r-; wo SO WO ro so © © 00 3 SO 00 © wo CN © wo WO Os ro ro OS 00 of OO 00 CN WO © £3 G •d- wb Ö Ö G Ö © © © © G © wb G •d- so wb sd G G G © © © o-l od SO 00 00 © 00 so ro ro so r- os r- OS OS r- ro © so r- •d- © © © © © © © © © © © © © wo © © os CN 0 SO SO SO CN O OO CN © CN © © 00 © 00 OO © •d; CN 00 © CN 00 SO wo ro Os CN © © SO wo WO CN sd Ö G Ö © © •d- © © o-l © wb sd •d- OO © G wb rb rb G © V rb of od 00 CN os CN wo CN ro r- Hradiste Formation I SO SO SO ro © © © © 0 OO CN •d- WO CN CN 3 r- r- ro © © ro r-; ro wo OO © © © •d; •d; © © © wo © © © wo © ro so r- sd ip ro CN G SO © © ro © © G © wb © 00 •d- G o-l OS of ip rb o-l CN © © © wb G 3 •d- G Ö Ö © © G 00 © 00 rb rb OS ro © G G ro © V ro sc CN SO ro ro ro O OS CN r- CN © ro r- •d- so r~- © © © © © © © © © © © © © © © 00 of OO CN OO OO SC CN ro © © r-; © © 00 O •d; OO © G ro wo CN wo so r-; © OS CN © so so WO so ^3 of G Ö sd Ö Ö © © sd © rb © o-l rb sd G 00 © © wb so © © © wb © rb wo 00 © ro wo OO r- ro CN CN 0 •d- ro OO SO wo ro ro CN CN CN wo © © © © © © © © © 0 © © © wo © © r- Ph so CN O ro ro CN 0 sc © © © © r- •d- © Os © © wo 00 © OO OS CN OS sd SO WO CN © r-; of CN G wo G •d- OS Ö G Ö © © •d- © © 00 © 00 wb o-l rb rb G wb © o-l G CN G © © V G © sd r- © os CN wo ro r- os •d- •d- os os OO CN sq © CN 00 sq of ro e” CN WO ■d; of ro OO OO so 00 ro os SO rb wo © so rb of CN CN rb rb OS o-l 5T CN o-l wo -2 OO •d- G rb sd rb G Ö © © wo CN wo 00 o-l CN 00 G © sd so ro wo © w rb CN rb WO © CN ro CN of j •d- CN CN 0 0 0 O O O © © © © wb O CN © © © wo © CN © © © © © wo © © © Ö Ö 0 Ö Ö Ö Ö © © © © © © © © © © 's 55 55 1 P P-i O 0 0 q o’ bij 0 0 0 d O c d O dfc O O 0 bO O oa < G S 3 Z H g G Ö Ö O 00 Ś 00 H e3 P ^3 s < < O fP MDL - minimal detection limit; 1 - standard STD DS8; Cr - calculated from according to stoichiometry; N-UCC normalization (Rudnick & Gao, 2003; Hu & Gao, 2008); Ce/Ce* - cerium anomaly calculated using Ce/Ce* = Ce^/fLa^ x Ppn)0'5 ratio; Eu/Eu* - europium anomaly calculated using Eu/Eu* = Eun/YSiitn x Gd^)0'5 ratio; PAAS according to Taylor and McLennan, 1985; UCC according to Rudnick and Gao (2003), supplemented by Hu and Gao (2008); CIA - chemical index of alteration (after Nesbitt and Young, 1982); nd - no data PROVENANCE OF LOWER CRETACEOUS DEPOSITS 121 u 0 0 0 O O 0 ro 0 r- ri SO SO ro os OS CN 0 0 r---; 0 O r- OS OO ro ro CO ro CN ro OO q ri p P ri •ri 0 ro Ö P © P © © ro ro ro so CN ro O 0 0 SO r¬ O O SCO © ro os ro r¬ CN ro ro © © 00 OS so SO r- ri O 00 ri 00 ri q © os © OS © OO P q ro © S ro P •ri 0 ri P © P © CO © © © 0 ri ro P Ph ro ri Lhoty Formation O r- 0 CN CN so OO ri so ri © r¬ ro © so ro ro ri OO 0 r- ro SCO so so O ro SCO ro q OS © 00 © ri © q q O'; sd ri 0 ro Ö ro Ö P © P © ri © © CN ri ro a* CN O ri CN OO ro os ri ri CN © r- © OS © OS Ph OO os SCO ro ri CO SCO ri CO SCO q q q OO 00 © ro © q SCO q £ s Ö CN Ö CN Ö P Ö q © q © ri © © P ri P P a- CS CN ro os O O O r¬ ri 00 SCO ri r- SCO ro CN SCO ro © Ph O ri r---; OO SCO ro SCO q CN ro q O'; 00 O'; © OO © CN OO OS ro © J CN ri Ö CN Ö Ö © r---; © ro © © © q p SO 00 P CN ro OO O O SCO SO O OS ro os SCO SCO OO SO so © ro ri Ph OS ri 3 ro ri Os SO SCO CN 00 q 3 SCO q OS © ri ro q ri ro J ro ro Ö CN Ö P Ö q © © p q © © ro P Os ro CN O O 0 OS SCO OO ro SCO SCO 00 00 © ri © OS SCO © r- r- r- OO OO SCO OO ro ro SCO q CN OO CN ri ro so ro os os ri q ro q q ä 00 CN Ö Ö P Ö © © P q © © © P ri 00 ri ro 0 ri CN OO OO ri CN r- SO SO SCO 00 os SCO CN ri SCO SO ro O OO q SCO CN so CN ro ro ro q so OS © ro ri q © SO ro ä Os ri Ö P Ö CO Ö P © P © ri © © © q P P OS ri CN ro O O ri ri OO OO os © so os ri ro ro 00 os os © Os CN CN OS os 0 q 00 sq 00 CO OS q ri 00 CN © OS © q © ro q ri Ph sd ri Ö ri Ö ro Ö © © ro © q © © ro ri Os ro CN O O OO r- OS r- OS OS © r- r- OS ro ro SCO ro 00 © SCO Ph ri SO q ri SCO ro SCO r- CN 00 q ri 00 OO © © © ro 00 q ri ri 0 ro Ö ro Ö q © © ri © © P so 00 P CN ro O O ro ro SCO SO 0 ri ro SO ro so ro SO so os © © 00 © r¬ CN OO Os SCO q SCO sq CN ro SCO q q Os OS © OS © ro os ri q q a P ri Ö ro Ö ro Ö P © p © ro © © © ro ri 00 P CN ro r- O OS so ro SCO CN CN ri 00 os ro OS SO CN CN © SCO SCO 0 OO 4 r- SCO SCO O SO OO ro 00 CN © OS OO © CN ri ro ri ro CN ri 0 ro Ö ro Ö © © SO © © SO ri Os P a CN ro Verovice Formation O O SCO SCO so r- SO r- SCO 00 CN OS © ro ro ro so r- ri SO OS CN OO CN SCO ri SO 0 ro © ro r- OS OS ro OS © © 00 q ro ri a CN P Ö ro Ö ro Ö P © P © SO © © q © P ri © P ro ro r- O ri OS SCO ro O ri 00 SCO © ro ri © OS ro ro 00 ri © ISJ § O ro so q ri so SCO q CN CN q OS © os © OS © © ro q os 00 Ph < Ö ro Ö CN Ö P Ö © q © ro © © q so P 00 Os CN CN ro CN r- O os ri OO ri os CN SCO os OO ri SCO CN SCO © ro SCO r- 0 q 00 0 OS 00 SCO 00 sq ri q ro SCO q q OS © q 00 os ri q CN ro ri¬ ri Ö ri Ö P © P © Os © © © © CN ri ri a CN ro O ro r- ro r- OS r- os O © SCO © OS 00 q r- O sco ■ri SCO 0 00 00 ri ro ro ro so q 00 Os OS © q q ri 0 Os SO SO ri 0 P © P © q © © © CN P 00 ro a CN O O r¬ SCO CN 0 0 CN r- 00 os CN ri © 00 SO CN ri O r---; os ri r- 00 3 00 ro OS CN ro SO SCO OO OS 3 00 q q © ri a ro ri-' Ö ri Ö ro 0 © r---; © q © ri © © © P P od ro CN O 0 ro CN so ri SO ro CN ro SCO © CN ri CN SO © ri ro SCO ri ro OO ro SCO so O q SCO SCO q SCO q OO © os OS © 00 q q r¬ 00 a ri 00 P ro © ro © CO © © © © ri ro © P ri ro O O OO r- SO OO os ri so CN ro ri ro SCO OS SCO © ri CN r¬ OJ in os ■ri SCO os CO SCO ro SCO ri q q OS © © © os q © a^ p so SO so ro © ro © © © © © ri ro ri 00 ro ro O 0 SO OS ri ri OO ro ri 00 r- OO ri 0 SCO r¬ q ro ICO 0 •ri O CO ri SCO q CN r- q q 00 q ri 00 © os © 00 os Os ä CN Ö P Ö P Ö © q © P © © © © © P © ro SCO CN O O ri 0 O SCO so 00 so SCO CN so OS OO ro © so Ph so SCO q O SCO O SCO SCO CN CN q os OS © Os OS © © ri q ro Os hJ Ö ro Ö ro Ö ro Ö r---; © q © p © © © ri P © P CN ro O O O OS ro ro 0 ro ro SCO CN ri r¬ so ro r- SO SCO © SCO Ph ri OO OO SCO SCO SCO r---; CN ro os ro ro os os OS OS 00 OO ri 00 00 hJ P ro Ö ro Ö ro Ö P © P © P © © © © © p P 00 P CN ro OS O O OO ri CN r- SCO OO r- CN SCO ri OS © os SCO SCO © ro so 00 Ph WO Os q ro ro 00 ri 0 SCO OS SCO 00 SO SO © © q ro q q hJ Ö P P P ri © ro © OŚ © © ro ro ri ro OO O O OO r- O SO ro O OS ri r- ri SCO SCO © ro SCO ro © © r- 00 Ph SCO SO ■ri ro SO ro ri q ri q r¬ r¬ © © q © Os q so hJ ro so ro © ro © OŚ © © P ro ro ro O O OO OO so r¬ ro os © © SCO CN CN ri os os OS r- ri O ■ri so OS SO os q CO q ri ri q ro OS © © q r¬ ro q 00 ä P P P Ö P Ö P © P © P © q © © P ri Os ri ro ro Hradiste Formation O O OO SCO OO ri so os so ri SCO ro so SCO os r- os r- ro SO OO O OO CN SCO q sq Os ro © q q OS © © ro q q q P ä ri ri Ö ro Ö ro Ö © P © ri © © p ri © ro CN ri O 0 r- CN CN ro SCO CN so ro SO SO 00 OS 3 OS SCO q © os ro © ä ri CN •ri OS ro q ro © © © © © OS OS OS © q q Os ri CN Ö Ö Ö ri © © © ri ro ro CN O O ro SCO O r- CN SCO 00 OO 0 ri SO © © CN ro ro Ph CN SCO r- OO SCO o-; SO r- CN Os CN q © 00 © © OS SCO ro r- © © hJ ro ro 0 P Ö P Ö q © © ro q © © © P ro ri so CN ro 0 ” SCO so SCO CN OO OS O SCO r- CN SO -2 ri ro OS CN ri CO SO OO CN q CN W Ö ro Ö Ö © © to J ro SCO CN SCO 0 SCO CN ro © SCO © Ö O O O Ö O O © © © © Ö Ö Ö Ö Ö © © '5 a P & Ph T3 a T3 O z OO 2 O £ Q X & 5 £ 2 vidual tests of recrystallized foraminiferids, dis- persed in a marly matrix (Fig. 5A). Thin-bedded mudstones display dark trace fossils. The mud- stones contain laminae of fine- grained sand- stone, composed of quartz, carbonates, layered silicates and scarce grains of glauconite, as well as heavy minerals (i.e. zircon, rutile, tourmatine and kyanite; Fig. 5B-E). The mudstone and shale microfacies of the Verovice Formation contain clay and silt frac- tions with dispersed fine-grained quartz, flakes of phyllosilicates, and glauconite. Scarce micro- faunal tests (foraminiferids, radiolaria and sponge spicules) are recrystallized as microcry- stalline quartz (Fig. 5H, I). Grains of heavy min- erals (i.e. zircon, rutile, tourma-ine) are poorly rounded or abraded (Fig. 5I, J). Single rhombo- hedra of carbonates are visible in the lower part of this formation (Fig. 5I). The matrix is sili- ceous and darkly colored with organic matter and reddish Fe oxyhydroxides. Some samples of mudstone and shale contain burrows, up to 1 cm in diameter and filled with grey quartzitic sand- stone (Fig. 5F, G). Occasionally within the hori- zons of grey, fine-grained depostts dark ichno- fossils occur. Grains of mica, quartz and glau- conite are dispersed in the clayey matrix of shales of the Lhoty Formation (Fig. 5K). Hori- zons, enriched in pyrite concretions, 1 mm in di- ameter, occur episodically. Coarse-grained lay- ers consist of extraclasts of felsic igneous and metamorphic rocks (chloritoid schists, phyllite, quartzite and hydrothermally altered basic rocks), as well as carbonate bioclasts (Fig. 5L, M). Geochemistry Major elements All samples of fine-grained material in this study are dominated by SiO2 and Al2O3 (Tab. 1). The distribution patterns of major and minor el- ements, normalized relative to UCC (Rudnick and Gao, 2003) for the material stud-ed, are shown on the Figure 6. The SiO2 and Al2O3 contents in the Lhoty Formation are most simi- lar to those of UCC. The Hradiste Formation is enriched in CaO only (Fig. 6). Generally, the material stud-ed is depleted in most of maj or and minor elements in comparison to UCC. All samples are strongly depleted in Na2O. The Lhoty Formation and particular samples of the Verovice Formation are enriched in K2O. The samples of the Verovice Formation that are rich in K2O also have relatively high TiO2 and Al2O3 content (Fig. 6). Al2O3 and TiO2 are cha- racterized by a strong corre-ation (0.84 < r < 0.96) in all formations, whereas the correlation between Al2O3 and K2O is variable, i.e. coeffi- cient r = 0.6-0.96 with outtier r = -0.4 in the 122 P. WÓJCIK-TABOL & A. ŚLĄCZKA Fig. 6. Spider plots of major and minor elements in Lower Cretaceous deposits of western part of the Silesian Nappe normalized to UCC (Rudnick and Gao, 2003; Hu and Gao, 2008) Lhoty Formation from the Rzyki (Tab. 2). SiO2 content is inversely correlated with Al2O3, CaO and LOI, as well as with most of oxides of the major and minor elements (Tab. 2). A positive correlation exists between SiO2 and MnO (r = 0.5), and between MgO and K2O in the Lhoty Formation from the Rzyki sections (r = 0.7), as well as between SiO2 and MnO in the Lhoty Formation from the Lipnik section (r = 0.9; Tab. 2). The concentrations of MgO, K2O and TiO2 increase up- wards in the rock sequence studted, but Fe2O3 and Na2Ü reach their highest values in the Verovice Formation (Tab. 1). A positive corretation of MgO and Fe2O3 with Al2O3 (r < 0.5) occurs in samples from the Lipnik section. In the upper part of the Verovice Formation, MgO and Fe2O3 show a correlation with CaO (r ~0.9; Tab. 2). The relationship between Na2O and Al2O3 is signifi- cantly positive (0.7 < r < 0.8) in both formations sampled in the Rzyki section. A reversed correlation of Na2O with Al2O3 (r = -0.7) occurs in the Lhoty Formation at the Lip- nik section. In other formations from the Lipnik section, the correlation coefficient is r < 0.5 (Tab. 2). Large ion lithophile elements (LILE): Rb, Sr Rb reveals a consistently strong, positive correlation with K2O (r > 0.9) and an irregut ar corret ation relative to Al2O3. The corretation coefficient is strong (r = 0.76 and 0.93) in the Verovice Formation from both sections, a mod- erately positive correlation (r = 0.6) occurs in the Lhoty For- mation from the Lipnik section and a weakly negative one typ-ties the Lhoty Formation from the Rzyki section (r = -0.3). In the Lhoty Formation from the Rzyki section, Rb has a posttive corretation with MgO (r = 0.88). Sr is post- tively correlated with Al2O3 (0.87 < r < 0.97) in the Vero- vice Formation from both sections and in the Lhoty Forma- tion from the Lipnik section. A positive Sr-CaO correlation is common for the material studied (0.6 < r < 0.99; Tab. 2). The pattern of multi-elements, normalized to UCC, shows a pronounced Sr depletion (Fig. 7). High field strength trace elements (HFSE: Zr, Hf, Nb, Ta) and Th, U, REE The amounts of Zr, Hf in the material studied are lower than those in the UCC, whereas the concentrations of Th, Nb, U, Y and REE are variable (Tab. 1). The strongest en- richment in U, Nb, Ta and REE is noted for samples from the Verovice Formation (Fig. 8). A postive corretation of Th, Sc, REE with Al2O3, K2O and TiO2 was commonly rec- ognized in the material studied. The weakest values of cor- retation coefficient (r < 0.5) typtfy the Lhota Formation from the Rzyki section. The retationship of U relative to Al2O3, K2O and TiO2 is irregutar. The most vistble is the correlation of U with K2O and TiO2 (r > 0.4). Zr and Hf in the Verovice Formation from the Lipnik section display a negative correlation with Al2O3 and a postive one with SiO2 (Fig. 7, Tab. 2). The samples generally have a low ELREE/EHREE ratio, rang tng from 9.15 to 16.7, with an outlier at 7.6. Many samples record LREE enrichment pro- nounced in LaN/YbN > 1. The REE patterns for the Hradiste and Lhoty formations show LREE sloping down to HREE, in some cases with an MREE depletion (Fig. 8) apparent in low GdN/YbN ratios and Eu/Eu* < 1 (Tab. 1). A few sam- ples from the Verovice Formation slope upward from La to Lu on the UCC-normaltzed plots. A convex-up MREE is seen often (Fig. 8). The values of Ce anomaly vary in range PROVENANCE OF LOWER CRETACEOUS DEPOSITS 123 Table 2 Pearson’s correlation coefficients (r) between selected major and trace elements for Lower Cretaceous deposits of the Silesian Nappe Rzyki section, Verovice Formation SiO2 Al2O3 Fe2O3 MgO CaO Na2O k2o TiO2 P2O5 MnO Zr Th LOI Rb Sr Eu/Eu* Ce/Ce* Y Nb U Sc La Cr SiO2 1.00 Al2O3 -0.74 1.00 Fe2O3 -0.55 -0.15 1.00 MgO -0.59 -0.07 0.99 1.00 CaO -0.22 -0.49 0.93 0.89 1.00 Na2O -0.53 0.75 -0.08 -0.06 -0.34 1.00 K2O -0.61 0.97 -0.30 -0.21 -0.61 0.59 1.00 TiO2 -0.80 0.95 0.01 0.07 -0.33 0.88 0.85 1.00 P2O5 -0.04 -0.17 0.23 0.13 0.28 0.36 -0.34 0.05 1.00 MnO -0.53 -0.13 0.90 0.89 0.85 -0.34 -0.20 -0.08 -0.05 1.00 Zr -0.66 0.57 0.36 0.38 0.09 0.86 0.38 0.76 0.33 0.04 1.00 Th -0.82 0.97 0.02 0.11 -0.34 0.77 0.92 0.97 -0.13 -0.01 0.69 1.00 LOI -0.62 0.84 -0.32 -0.27 -0.54 0.34 0.87 0.68 -0.51 -0.03 0.08 0.73 1.00 Rb -0.59 0.93 -0.28 -0.18 -0.59 0.51 0.98 0.79 -0.47 -0.16 0.34 0.88 0.87 1.00 Sr -0.94 0.87 0.27 0.33 -0.05 0.64 0.77 0.90 0.06 0.29 0.58 0.90 0.77 0.71 1.00 Eu/Eu* 0.21 -0.56 0.47 0.42 0.61 -0.07 -0.70 -0.33 0.23 0.21 0.23 -0.44 -0.78 -0.68 -0.41 1.00 Ce/Ce* 0.07 0.37 -0.42 -0.35 -0.52 0.57 0.34 0.42 -0.22 -0.61 0.44 0.38 0.03 0.34 0.04 0.22 1.00 Y -0.56 0.58 0.14 0.12 -0.09 0.94 0.39 0.77 0.59 -0.17 0.90 0.63 0.19 0.29 0.59 0.05 0.34 1.00 Nb -0.78 0.92 0.04 0.10 -0.29 0.90 0.80 0.99 0.06 -0.08 0.81 0.95 0.62 0.75 0.86 -0.23 0.47 0.81 1.00 U -0.48 0.10 0.59 0.54 0.52 0.49 -0.15 0.37 0.60 0.36 0.60 0.19 -0.17 -0.24 0.41 0.56 0.06 0.63 0.42 1.00 Sc -0.68 0.85 -0.06 -0.05 -0.35 0.90 0.72 0.91 0.32 -0.18 0.74 0.83 0.69 0.65 0.79 -0.38 0.25 0.88 0.91 0.37 1.00 La -0.82 0.95 0.00 0.04 -0.33 0.79 0.86 0.97 0.03 0.00 0.63 0.93 0.83 0.80 0.93 -0.45 0.24 0.70 0.95 0.34 0.92 1.00 Rzyki section, Lhoty Formation SiO2 Al2O3 Fe2O3 MgO CaO Na2O k2o TiO2 P2O5 MnO Zr Th LOI Rb Sr Eu/Eu* Ce/Ce* Y Nb U Sc La Cr SiO2 1.00 Al2O3 -0.77 1.00 Fe2O3 -0.47 0.06 1.00 MgO 0.43 -0.48 -0.34 1.00 CaO -0.05 -0.55 0.31 -0.02 1.00 Na2O -0.53 0.84 -0.09 -0.76 -0.40 1.00 k2o 0.19 -0.43 0.31 0.74 0.05 -0.84 1.00 TiO2 -0.99 0.84 0.36 -0.48 -0.05 0.63 -0.29 1.00 P2O5 -0.43 0.08 0.17 0.17 0.29 -0.25 0.37 0.41 1.00 MnO 0.52 -0.41 -0.74 0.17 0.30 -0.04 -0.44 -0.47 -0.35 1.00 Zr -0.35 0.02 0.70 0.31 0.04 -0.46 0.82 0.25 0.53 -0.83 1.00 Th -0.68 0.83 -0.05 -0.25 -0.45 0.55 -0.17 0.77 0.56 -0.45 0.19 1.00 LOI 0.42 -0.57 -0.55 0.52 0.60 -0.36 -0.08 -0.44 -0.19 0.89 -0.49 -0.55 1.00 Rb 0.09 -0.31 0.25 0.79 -0.01 -0.77 0.98 -0.19 0.40 -0.44 0.83 -0.07 -0.06 1.00 Sr -0.67 0.28 0.11 -0.21 0.57 0.29 -0.35 0.64 0.27 0.21 -0.09 0.19 0.37 -0.27 1.00 Eu/Eu* 0.84 -0.66 -0.05 0.13 -0.09 -0.48 0.28 -0.83 -0.27 0.05 -0.06 -0.53 -0.08 0.13 -0.85 1.00 Ce/Ce* 0.90 -0.96 -0.24 0.52 0.33 -0.80 0.41 -0.94 -0.13 0.44 -0.11 -0.76 0.51 0.29 -0.48 0.78 1.00 Y -0.59 0.59 -0.18 0.02 -0.08 0.48 -0.32 0.60 -0.07 0.16 -0.14 0.33 0.30 -0.15 0.72 -0.91 -0.66 1.00 Nb -0.78 0.42 0.39 0.06 0.16 -0.01 0.33 0.75 0.85 -0.56 0.67 0.67 -0.31 0.41 0.49 -0.63 -0.53 0.33 1.00 U -0.76 0.25 0.76 -0.02 0.35 -0.08 0.37 0.64 0.43 -0.60 0.74 0.20 -0.25 0.42 0.55 -0.59 -0.47 0.37 0.77 1.00 Sc -0.45 0.63 0.00 0.28 -0.60 0.25 0.21 0.45 -0.05 -0.39 0.36 0.45 -0.41 0.36 0.09 -0.56 -0.60 0.67 0.37 0.39 1.00 La -0.15 0.00 -0.37 0.74 0.10 -0.30 0.35 0.12 0.36 0.23 0.18 0.15 0.57 0.49 0.43 -0.55 -0.04 0.62 0.45 0.28 0.51 1.00 Cr -0.33 0.02 0.43 -0.23 0.45 0.15 -0.21 0.23 -0.42 0.10 -0.03 -0.42 0.28 -0.19 0.60 -0.43 -0.23 0.50 -0.06 0.52 0.13 0.04 1.00 from 0.89 to 1.15, and Eu/Eu* yield values of between 0.82 and 1.06. Only a few samples of the Verovice Formation show a REE pattern similar to UCC. There is visible, posi- tive correlation of Eu/Eu* with Al2O3 (r = 0.3 in the Lhoty Formation, r > 0.8 in the Hradiste and Verovice formations) in the Lipnik section, whereas an inverse Eu/Eu*-Al2O3 correlation (-0.55 and -0.66) occurs for the formation from the Rzyki section. The re lationthip between Ce/Ce* and Al2O3 is not clear. Exceptionally, a clear inverse correlation (r = -0.96) is vistble for the Lhoty Formation from the 124 P. WÓJCIK-TABOL & A. ŚLĄCZKA Table 2 continuation Lipnik section, Hradiste Formation SiO2 Al2O3 Fe2O3 MgO CaO Na2O k2o TiO2 P2O5 MnO Zr Th LOI Rb Sr Eu/Eu* Ce/Ce* Y Nb U Sc La Cr SiO2 1.00 Al2O3 -0.77 1.00 Fe2O3 -0.62 0.98 1.00 MgO -0.62 0.98 1.00 1.00 CaO -0.01 -0.63 -0.78 -0.78 1.00 Na2O 0.28 0.39 0.58 0.58 -0.96 1.00 K2O -0.41 0.89 0.97 0.97 -0.91 0.76 1.00 TiO2 -0.51 0.94 0.99 0.99 -0.86 0.68 0.99 1.00 P2O5 0.58 0.07 0.28 0.28 -0.82 0.94 0.51 0.41 1.00 MnO -0.42 0.90 0.97 0.97 -0.91 0.76 1.00 0.99 0.50 1.00 Zr -0.51 0.94 0.99 0.99 -0.85 0.68 0.99 1.00 0.40 0.99 1.00 Th -0.80 1.00 0.97 0.97 -0.60 0.36 0.88 0.93 0.03 0.88 0.93 1.00 LOI -0.71 0.11 -0.11 -0.11 0.71 -0.87 -0.35 -0.24 -0.98 -0.34 -0.23 0.14 1.00 Rb -0.22 0.79 0.90 0.90 -0.97 0.88 0.98 0.95 0.67 0.98 0.95 0.76 -0.53 1.00 Sr -0.11 -0.54 -0.71 -0.71 0.99 -0.99 -0.86 -0.80 -0.88 -0.86 -0.79 -0.51 0.99 -0.95 1.00 Eu/Eu* -0.97 0.90 0.79 0.79 -0.23 -0.04 0.61 0.70 -0.37 0.62 0.70 0.92 0.52 0.44 -0.13 1.00 Ce/Ce* -0.97 0.61 0.42 0.43 0.23 -0.49 0.19 0.30 -0.75 0.20 0.31 0.64 0.85 -0.01 0.33 0.89 1.00 Y -0.61 0.97 1.00 1.00 -0.79 0.59 0.97 0.99 0.29 0.97 0.99 0.97 -0.12 0.90 -0.72 0.79 0.42 1.00 Nb -0.45 0.91 0.98 0.98 -0.89 0.73 1.00 1.00 0.47 1.00 1.00 0.90 -0.30 0.97 -0.84 0.65 0.24 0.98 1.00 U -0.27 0.82 0.92 0.92 -0.96 0.85 0.99 0.97 0.63 0.99 0.96 0.80 -0.48 1.00 -0.93 0.49 0.05 0.93 0.98 1.00 Sc -0.86 0.99 0.93 0.93 -0.50 0.25 0.82 0.88 -0.08 0.82 0.88 0.99 0.26 0.68 -0.41 0.96 0.72 0.93 0.84 0.72 1.00 La -0.55 0.96 1.00 1.00 -0.83 0.65 0.99 1.00 0.36 0.99 1.00 0.94 -0.19 0.93 -0.77 0.74 0.35 1.00 0.99 0.95 0.90 1.00 Cr -0.53 0.95 0.99 0.99 -0.84 0.66 0.99 1.00 0.38 0.99 1.00 0.94 -0.21 0.94 -0.78 0.72 0.33 1.00 1.00 0.96 0.89 1.00 1.00 Lipnik section, Verovice Formation SiO2 Al2O3 Fe2O3 MgO CaO Na2O k2o TiO2 P2O5 MnO Zr Th LOI Rb Sr Eu/Eu* Ce/Ce* Y Nb U Sc La Cr SiO2 1.00 Al2O3 -0.98 1.00 Fe2O3 -0.94 0.91 1.00 MgO -0.89 0.81 0.87 1.00 CaO -0.64 0.60 0.48 0.49 1.00 Na2O -0.26 0.24 0.33 0.53 -0.44 1.00 K2O -0.77 0.73 0.73 0.88 0.12 0.81 1.00 TiO2 -0.95 0.97 0.96 0.82 0.46 0.35 0.76 1.00 P2O5 -0.90 0.86 0.72 0.71 0.76 0.01 0.58 0.73 1.00 MnO -0.76 0.59 0.66 0.82 0.84 -0.42 0.08 0.54 0.64 1.00 Zr 0.46 -0.40 -0.18 -0.51 -0.35 -0.33 -0.60 -0.24 -0.66 0.24 1.00 Th -0.88 0.94 0.87 0.73 0.31 0.44 0.78 0.97 0.67 0.26 -0.27 1.00 LOI -0.96 0.89 0.85 0.85 0.72 0.15 0.69 0.81 0.97 0.82 -0.58 0.72 1.00 Rb -0.81 0.76 0.80 0.89 0.15 0.76 0.99 0.79 0.64 0.16 -0.56 0.80 0.75 1.00 Sr -0.98 0.97 0.88 0.90 0.67 0.29 0.78 0.92 0.87 0.80 -0.53 0.87 0.92 0.79 1.00 Eu/Eu* -0.82 0.81 0.75 0.77 0.18 0.62 0.92 0.79 0.75 -0.13 -0.63 0.83 0.79 0.95 0.79 1.00 Ce/Ce* 0.08 0.08 0.06 -0.17 -0.64 0.43 0.17 0.21 -0.34 -0.55 0.37 0.39 -0.33 0.14 -0.09 0.18 1.00 Y -0.60 0.61 0.74 0.72 -0.13 0.81 0.83 0.76 0.22 0.10 -0.07 0.77 0.40 0.82 0.59 0.68 0.51 1.00 Nb -0.81 0.84 0.90 0.77 0.15 0.59 0.82 0.94 0.49 0.27 -0.11 0.94 0.62 0.83 0.78 0.78 0.45 0.93 1.00 U -0.47 0.57 0.43 0.52 -0.03 0.66 0.70 0.62 0.20 -0.10 -0.27 0.74 0.24 0.61 0.58 0.55 0.57 0.76 0.73 1.00 Sc -0.95 0.96 0.94 0.88 0.48 0.42 0.81 0.99 0.72 0.61 -0.30 0.95 0.81 0.82 0.95 0.78 0.16 0.79 0.93 0.68 1.00 La -0.90 0.88 0.87 0.95 0.35 0.64 0.96 0.90 0.71 0.53 -0.52 0.88 0.81 0.95 0.92 0.89 0.10 0.82 0.89 0.71 0.94 1.00 Cr -0.98 0.95 0.90 0.93 0.70 0.28 0.77 0.91 0.88 0.88 -0.51 0.83 0.94 0.79 0.99 0.77 -0.17 0.58 0.77 0.51 0.94 0.91 1.00 Rzyki section. The Ce/Ce*-CaO correlation factor is nega- tive for the Verovice Formation from both sections and weakly to strongly posttive for the Lhoty Formation from both the Rzyki section and the Lipnik section (r = 0.33 and 0.8, respectively). Diagrams of multi-elements, normalized to UCC (Fig. 7), show posttive anomalies for Y relative to Yb in the Verovice Formation and a slight Y depletion in particutar samples from the Lhoty Formation. There are common negative ano- malies for Zr-Hf, relative to Nd and Sm. One sample from the Verovice Formation from the Lipnik section (LP 13) is significantly enriched in Zr-Hf. TiÜ2 shows enrichment relative to Y in the Hradiste and Lhoty formations and depletion in the Verovice Forma- PROVENANCE OF LOWER CRETACEOUS DEPOSITS 125 Ta ble 2 con tin u a tion Lipnik section, Lhoty Formation SiO2 Al2O3 Fe2O3 MgO CaO Na2O k2o TiO2 P2O5 MnO Zr Th LOI Rb Sr Eu/Eu* Ce/Ce* Y Nb U Sc La Cr SiO2 1.00 Al2O3 -0.99 1.00 Fe2O3 -0.53 0.48 1.00 MgO -0.65 0.52 0.28 1.00 CaO -0.80 0.68 0.44 0.97 1.00 Na2O 0.60 -0.67 -0.73 0.13 -0.10 1.00 k2o -0.72 0.62 0.10 0.95 0.94 0.12 1.00 TiO2 -0.94 0.90 0.25 0.78 0.86 -0.29 0.89 1.00 P2O5 -0.09 0.21 0.49 -0.62 -0.43 -0.85 -0.63 -0.24 1.00 MnO 0.98 -0.93 -0.48 -0.80 -0.91 0.42 -0.85 -0.97 0.12 1.00 Zr -0.63 0.55 -0.13 0.87 0.83 0.24 0.97 0.86 -0.70 -0.76 1.00 Th -0.94 0.96 0.70 0.41 0.61 -0.83 0.45 0.76 0.42 -0.85 0.32 1.00 LOI -0.91 0.97 0.47 0.28 0.47 -0.81 0.40 0.77 0.43 -0.80 0.35 0.96 1.00 Rb -0.68 0.58 0.02 0.94 0.91 0.18 1.00 0.87 -0.67 -0.82 0.99 0.39 0.36 1.00 Sr -0.96 0.95 0.73 0.53 0.71 -0.77 0.54 0.80 0.31 -0.90 0.41 0.99 0.99 0.49 1.00 Eu/Eu* -0.32 0.25 -0.45 0.72 0.61 0.55 0.84 0.63 -0.86 -0.48 0.93 -0.02 0.05 0.88 0.06 1.00 Ce/Ce* -0.95 0.91 0.76 0.65 0.80 -0.67 0.62 0.81 0.19 -0.93 0.47 0.95 0.83 0.57 0.98 0.12 1.00 Y -0.82 0.71 0.56 0.94 0.99 -0.21 0.88 0.84 -0.31 -0.92 0.75 0.67 0.52 0.84 0.77 0.49 0.87 1.00 Nb -0.99 0.95 0.58 0.73 0.87 -0.54 0.77 0.93 0.02 -0.99 0.66 0.91 0.85 0.73 0.95 0.35 0.97 0.89 1.00 U -0.16 0.12 -0.66 0.52 0.39 0.62 0.68 0.49 -0.83 -0.29 0.83 -0.17 -0.04 0.74 -0.12 0.97 -0.09 0.26 0.16 1.00 Sc -0.61 0.49 0.04 0.97 0.91 0.26 0.99 0.81 -0.73 -0.76 0.96 0.31 0.25 0.99 0.42 0.87 0.53 0.85 0.67 0.72 1.00 La 0.43 -0.50 -0.78 0.24 0.02 0.97 0.29 -0.09 -0.91 0.25 0.43 -0.71 -0.65 0.35 -0.65 0.72 -0.56 -0.10 -0.39 0.79 0.41 1.00 Cr -0.78 0.67 0.44 0.98 1.00 -0.09 0.93 0.85 -0.44 -0.90 0.82 0.59 0.46 0.90 0.70 0.60 0.80 0.99 0.86 0.38 0.91 0.03 1.00 Hradiśtś Formation Vefovice Formation Lhoty Formation Fig. 7. Spider plots of setected trace elements in Lower Cretaceous depostts of western part of Silesian Nappe normaltzed to UCC (Rudnick and Gao, 2003; Hu and Gao, 2008) tion. Variable U/Th ratios stem from a wide range of U con- centrations (high in the Verovice Formation, low in the Lhoty Formation). Positive anomalies of Nb, relative to Ce, and Nb-Ta fractionation, are ob t erved frequently. These features show a general trend to greater decoupting of Ce from P2O5, as well as Nb-Ta and MREE from Zr-Hf, and TiÜ2 from Y (Fig. 7). DISCUSSION Compositional alteration and provenance The negative correlation of SiÜ2 with Al2Ü3 (-0.98 < r < -0.74) suggests that quartz grains occur together with sili- ceous skeletons and diagenetic siltca. The presence of ra- diolarians, sponge needles and agglutinated foraminiferids, 126 P. WOJCIK-TABOL & A. SLĄCZKA Fig. 8. UCC normalized REE patterns for studied samples as well as cryptocrystalline quartz, was confirmed micro- scopically. In general, terrigenous-derived oxides (K2O, TiÜ2, Na2Ü) show a positive correlation with Al2Ü3, indi- cating an important role of mica-type phyllosilicates. How- ever, there are instances of reduced correlation (see the sec- tion on major elements) and they are interpreted as the ef- fect of weathering, transport and post-depositional pro- cesses. The postive LOI-CaO (Tab. 2) corret ation in the Hradiste Formation and Lhoty Formation from the Rzyki section demonstrates that CaO is largely derived from car- bonates (Von Eynatten, 2004). Importance of subaerial weathering The siliciclastic rocks consist of debris, originating from the decomposition of parent rocks that were affected by a combination of chemical and physical weathering, as well as transport sorting and post-depositional chemtt al changes. Hydrolytic weathering of unstable minerals, such as feldspar, led to the loss of Na and Ca ions. As weathering continued, K-feldtpars should also have been weathered, releasing K (Fedo et al., 1995, 1997; Nesbitt et al., 1997). Finally, it resulted in the formation of clayey deposits, rich in illite and kaolinite, and Fe-oxyhydroxides. The expected pathways of increasing degrees of weath- ering for igneous rocks can be traced on the A-CN-K trian- gular plot (Nesbitt and Young, 1984). Progressive weather- ing shifts the residual composition towards the Al2O3 apex and ever-higher CIA values (Fedo et al., 1995). In the A-CN-K diagram, the results are located in up- per part of triangle, closer to the A-K join (Fig. 9A). The actual trend of the samples differs from the predicted weath- ering trend (solid arrow). The CIA values of 50 or below are characteristic for unweathered igneous rocks, while residual clays, enriched in kaolinite and Al oxyhydroxides produced under intense weathering, have CIA values close to 100. The CIA values, ranging from 70 to 75 in the typical Phane- rozoic shales, reflect muscovite, illite and smectite compo- nents and indicate a moderately weathered source (Nesbitt and Young, 1982, 1984; McLennan et al., 1993). The CIA values calculated in this study vary from 75 to 89 (Tab. 1), whereas CIA for the PAAS and UCC is 75 and 61 re tpectively. It is neces t ary to con tider the effect of K-enrichment resulting from K-metasomatism or sedimen- tary incorporation of K-feldspar, suggested by the elevated contents of K2O, normaltzed to UCC (see Fig. 6), and the negative correlation of K2O with Al2Ü3 for the Lhoty For- mation from the Rzyki section (Tab. 2). CIA values correc- ted for potassium-addition vary from 85 to 93.5 (Fig. 9A). Generally, the detritus in the samples is strongly weathered. The intensity of weathering could be reflected in an in- crease in the Rb/Sr ratio. Sr is liberated during the decom- position of silicates, whereas Rb is retained in the clay frac- tion. Therefore, the weathered material is depleted in Sr (Nesbitt et al., 1980; McLennan et al., 1983). Sr depletion in the material studied, excluding the calcareous Hradiste Formation, is pronounced on diagrams of multi-elements, normaltzed to UCC (Fig. 7). In material studted, Rb dis - plays a stronger affinity to K2O than to Al2Ü3 (Tab. 2). If the K-feldspathization exerted an influence on the material studied that caused the addition of Rb, then the Rb/Sr ratios would not indicate the degree of weathering of the parent rocks. The ratio of Th/U can be used as a weathering indicator, because of the low solubility of Th and the oxidation of U4+ to the soluble U6+ (Taylor and McLennan, 1985; McLennan et al., 1993). The Th/U ratios in the material studied differ from ratio for UCC and PAAS (3.9 and 4.7, respectively; Taylor and McLennan, 1985; Rudnick and Gao, 2003). Out- liers at 1.8 and > 6 occur for the Verovice Formation and PROVENANCE OF LOWER CRETACEOUS DEPOSITS 127 CN K 1 10 100 0.00 0.02 0.04 0.06 Th [ppm] Na;0/AIA Fig. 9. Weathering indices of detritus in Lower Cretaceous deposits of western part of Silesian Nappe. A - Ternary A-CN-K plot of molecular proportions of AhO3-(CaO*+Na2O)-K2O for studied material of western part of the Silesian Nappe and chemical index of al- teration shown as CIA scale (Nesbitt and Young, 1984). Pl - plagioclase; Kfs - K-feldspars; Ilt - illite; Ms - muscovite; Sme - smectite; Kln - kaolinite; Gbs - gibbsite; Chl - chlorite. Stars: 1 - gabbro; 2 - tonalite; 3 - granodiorite; 4 - granite; 5 - A-type granite from Fedo et al. (1997). Solid arrow indicates theoretical weathering trend for tonalite. Correction for K-enrichment can be made by projection of lines from K-apex through data points to ideal weathering line and reading off CIA axis (after Fedo et al., 1995). B - Discrimination plot of Th vs. Th/U (McLennan et al., 1993). Dashed lines - Th/U and Th content of UCC. Star - PAAS (Taylor and McLennan, 1985). C - Th/U versus Na2Ü/Al2Ü3 diagram Lhoty Formation, respectively (Tab. 1).The Th/U ratios cor- relate positively with Al2Ü3, suggesting that the Th/U ratio was not drastically changed during and/or after deposition. The diagram of the retationship of Th/U relative to Na2Ü/ Al2Ü3 (Fig. 9C) shows that Na2Ü/Al2Ü3 and Th/U ratios decrease together in all formations. The graph of Th vs. Th/U (Fig. 9B; McLennan et al., 1993) shows that the sam- ples from the Lhoty Formation are more weathered and fol- low the weathering trend. The black shales of the Hradiste and Verovice formations that are below the UCC limit have Th/U ratios additionally diminished, owing to the accumu- lation of U in organic matter and deposition under reducing conditions (McManus et al., 2005). Nevertheless, this re- concentration of U did not disturb the detrital Th/U ratio. Mineral debris, deposited in the formations studied, was produced by strong chemfeal weathtring, promoted by a warm and humid climate in Late Jurassic-Cret aceous time. This study yields the conclusion that weathering is not the main factor controlling the chemistry of the siliciclastics. Provenance of detritus La, Th and Hf tend to be concentrated in silicic rocks more readily than in basic rocks that accommodate Sc, Cr and other compatible elements (Cox et al., 1995; Cullers, 2000). On the basis of its affinity to Al2Ü3, it is inferred that only Th has a detrital derivation in all of the formations studied. A terrigenous origin for La, Sc and Cr can be postu- lated for the Hradiste and Verovice formations. The plot of La/Th versus Hf, proposed by Floyd and Leveridge (1987), shows that the samples fall into the field of felsic and mixed felsic/batic sources (Fig. 10A). This corresponds to the diagram of Th against Sc (McLennan et al., 1993) that reveals the continental nature of an alimen- tary area (Fig. 12B). Samples from the Lhoty Formation do not separate from the others. Thus the influence of deposi- tional and later processes was not significant for the concen- tration of La and Hf. Ternary La-Th-Sc diagrams (Bhatia and Crook, 1986) were used to determine the provenance and tectonic settings for the deposition of the succession studted. All of the sediments studted occupy the field of continental island arcs (= CIA; Fig. 11). The Early Cretaceous Silesian Basin was fed by debris origmatmg from the North European Platform, the Baska- Inwałd and Proto-Silesian Ridges, and the Bohemian Mas- sif (Slączka, 1976; Golonka et al., 2006; Strzeboński et al., 2009). The Baska-Inwałd Ridge and the Proto-Silesian Ridge, as topographically uplifted elements of the North European Platform (Książkiewicz, 1964; Golonka et al., 2006), are exposed parts of the Variscan orogen with late Precambrian (Cadomian) protoliths. The Bohemian Massif is part of the West European plate. It consists of the Va- riscan orogenic belt and the Cadomian forel and terrane of the Brunovistulicum, composed of metamorphic rocks (Poprawa et al., 2004; Golonka et al., 2006). In general, the alimentary area was established on con- tinental crust (Sandulescu, 1988; Klominsky et al., 2010). It is evidenced by exotic rocks, such as granttes and porphy- rites, sericite-chlorite schists, gneisses, and siliciclastics (Cieszkowski et al., 2012 and references therein). Likewise, heavy-mineral assemblages (tourmaline, zircon as well as apatite, monazite and epidote) indicate that non-metamor- phic to low-grade metamorphic rocks of granitic continental crust (granitoids, as well as sedimentary pelites and psam- 128 P. WOJCIK-TABOL & A. SLĄCZKA Fig. 10. Discrimination diagrams for provenance of samples studied. A - La/Th versus Hf diagram (Floyd and Leveridge, 1987); B - Th versus Sc diagram from McLennan et al. (1993) mites) were the primary parent rocks for turbiditic deposits in the Cretaceous Silesian Basin. However, the mosaic structure of the European Plate and the contribution of metamorphic rocks of granulite and partly eclogite facies is reflected in the association of heavy minerals (garnet and rutile; Unrug, 1968; Winkler and Slączka, 1992; Grzebyk and Leszczyński, 2006). Granulite and eclogite facies typtfy the conditions of regional meta- morphism that act during orogenesis. They can be con nected to the old Variscan orogenic belt of the Bohemian Massif. The present studies are in agreement with the pub- lished results, because the appropriate heavy minerals were found with kyanite, which is typical for the granulite facies. Moreover, evtdence for continental crust as the chief al-- mentary area was the geochemical signatures and the posi- tion of the Carpathian basin as a back-arc basin (Golonka et al, 2006; Oszczypko et al., 2006; Puglisi, 2009), bonded to the CIA tectonic province. Sort ing and re cy cling Sorting during transportation exerts a major influence on the composition of clastic sedtments (Johnsson, 1993; Nesbitt et al., 1997). Gravitational fractionation can result in the separation of quartz and heavy minerals from phyllo- silicates. The influence of detrital heavy minerals on geo- chemistry was tested, using an inverse correlation with Fig. 11. Discrimination diagram La-Th-Sc for tectonic setting (Bhatia and Crook, 1986) Fig. 12. Ternary 10 x Al2Ü3-200 x TiÜ2-Zr plot showing possi- ble sorting trend Al2Ü3 (Tab. 2). TiÜ2 can occur in clay minerals and heavy minerals (e.g. rutile). The most plausible and consistent car- rier of Zr and Hf is zircon. In the material studied, a strong positive correlation be- tween TiO2 and Al2O3 (Tab. 2) suggests an affinity of tita- nium to phyllosilicates. In the Hradiste and Lhoty forma- tions from the Lipnik section and the Verovice Formation from the Rzyki section, the TiÜ2 concentration parallels those of Zr and Hf (Tab. 2). Thus, the presence of heavy minerals is possible. Nevertheless, the highest concentra- tions of TiÜ2 and Zr occur in samples from the Verovice Formation (Fig. 7) and the accumulation of heavy minerals is assumed. Zircon can be interpreted as recycled material. The addition of zircon is illustrated on the La/Th vs. Hf dia- gram (Floyd and Leveridge, 1987; Fig. 10B) and on the ter- nary plot of 10 x Al2Ü3-200 x TiÜ2-Zr (Garcia et al., 1991; Fig. 12) The Verovice Formation falls along a trend involv- ing the addition of zircon. Zircon, rutile and tourmatine form an association of heavy minerals that occur in rewor- PROVENANCE OF LOWER CRETACEOUS DEPOSITS 129 ked material and were recognized in thin-section (see the section on microfacies). The presence of recycled material within siliciclastic sequences is gener ally acc epted. Veizer and MacKenzie (2003) concluded that about 90% of sedimentary rocks are reworked to produce more sedtmentary rocks. The Carpa- thian successions contain abundant material that underwent several sedimentary cycles. The co-occurrence of rounded and fresh, unabraded grains of heavy minerals suggests a mixed provenance of the clastic material, both from crystal- line and older sedtmentary rocks (Unrug, 1968; Grzebyk and Leszczyński, 2006). Cieszkowski et al. (2012) descri- bed the occurrence of olistoliths and olistostromes in many levels of the Silesian Series and also within the Lower Cre- tateous sequences of the Hradiste, Verovice and Lhoty formations, investigated here. Diagenetic changes The diagenetic addition of potassium into siliciclastic deposits is widely known (Fedo et al., 1995; Campos Alva- rez and Roser, 2007). The post-depositional potassic alter- ation in fine-grained samples from the Lower Cretaceous sedtments of the Silesian Unit is supported by the clayey, illite-rich matrix (Fig. 5), the K2O enrichment seen on the plots of major element oxides, normalized to UCC (Fig. 6) and the lack of to negative corretation between K2O and Al2Ü3 (Tab. 2). The secondary introduction of K into a sediment can be related to the transformation of smectite to illite. Illitization with increasing depth of burial can release certain amounts of water, enriched in Fe and Mg (Bozkaya and Yalęm, 2004), that later play a crucial role during diagenetic pro- cesses. Gonzalez-Alvarez and Kerrich (2010) postdated that the dehydration of the smectite minerals is a likely source of diagenetic brines. The influence of these flutds can be postut ated, on the basis of erratic patterns of REE and HFSE distribution. The analysis of the hydrothermally altered Cretaceous picrite from the Czech Republ ic led to the conclusion that parent hydrothermal solutions were produced by the dewa- tering of clay minerals in diagenetically mod-ied flysch sediments (Dolnicek et al., 2010, 2012). Therefore, the ma- terial studied could have been affected by similar processes. Mobility of REE and HFSE REE, Th, Sc and Co are recognized as source-rock indi- cators (Taylor and McLennan, 1985) and can be mobile un- der certain conditions of a sedimentary system. Diagenesis at the sediment-water interface, decomposition of the unsta- ble detritus (e.g. volcanic debris), or detrital/biogenic disso- lution allow the fractionation of trace elements (Abanda and Hannigan, 2006; McLennan et al., 2006). Certain samples (Lhoty Fm.: LP 16, RZ WP 2/07, RZ WP 3/07, RZ 3/07; Verovice Fm.: RZ 1/07, RZ 2/07, RZ 2A/07) have enrichment in Nb, relative to Ta (Fig. 7). Values of the Nb/Ta ratio are between 12.8 and 27, with one outlier at 36.3, whereas UCC ratios = 13.3 (Rudnick and Gao, 2003). This indicates that certain horizons within the sedn mentary profile studied were influenced by Nb-rich fluids. The Zr budget was probably controlled by zircon, which can maintain Zr/Hf ratios through geo^g^al pro t cesses, such as weathering, transportation, diagenesis and metamorphism. Zr/Hf ratios, ranging from ~35 to ~70, typ- ify an igneous origin of zircon (Murali et al., 1983; Belou- sova et al., 2002). Nonetheless, hydrothermal or authigenic processes can exert an in fluence on zircon and cause the fractionation of trace elements (Hoskin, 2005). In the mate- rial studied, the Zr/Hf ratios are between 29.8 and 39.7, in- dicating Zr depletion at particular levels (e.g., the upper part of the Verovice Formation in the Rzyki section - RZ 2A/07; the upper part of the Lhoty Formation in the Rzyki section - RZ WP 2/07, RZ WP 3/07). The high correlation coefficient (r > 0.8) of Zr, relative to K2O, in the Lhoty Formation indi- cates post-depositional alteration of the Zr content. An REE distribution lytng far away from the UCC pattern re flects the influence of post-depositional processes. Samples from the Rzyki section have a negative Eu/Eu* - Al2Ü3 correla- tion that indicates diagenetic Eu depletion. The REE frac- tionation indicated by LaN/YbN does not strictly depend on Al2O3 and permits the inference that the REE pattern was changed during diagenesis. Positive Ce anomalies typify most of material studied. The negative anomalies of Ce in the Hradiste Formation are associated with calcite and inherited a Ce depletion similar to that of seawater. Higher values of Ce/Ce* occur in the Verovice Formation, particularly in samples from the Rzyki section. This could be explained by the scavenging of less soluble Ce4+ by suspended particles that settled through the water column (Sholkovitz et al., 1994) or Ce adsorption on Fe-Mn minerals (Elderfield et al., 1990). The fractionation of REE and Zr-Hf could have been caused by diagenetic processes that involved basinal brines. Gonzalez-Alvarez and Kerrich (2010) concluded that HFSE and HREE are mobile in oxidized alkaline brines. In fluids with a high pH, REE (preferentially HREE) have an affinity to dicarbonate complexes. Carbon dioxide can be generated by the degradation of organic matter or during the volcanic outgassing, associated with rifting. The birth of the Outer Carpathian basin was as a result of the European margin rifting in the Late Jurassic-Early Cretaceous (Golonka et al., 2006; Oszczypko, 2006; Slą- czka et al., 2006). During the Early Cretaceous time oce- anic-crust has been extended (Larson, 1991). The rifting of the European Platform was a main factor controlling the re- gional subsidence of the Silesian Basin, and accompanied by the mafic volcanism (Ivan et al., 1999; Lucińska-Ancz- kiewicz et al., 2002; Grabowski et al., 2004; Oszczypko et al., 2012). Igneous rocks of the teschenite association are widespread in the area between Hranice in the Czech Re- public and Bielsko-Biała in Poland. The magmatic rocks are classified as teschenites, picrites, monchiquites and alkaline basalts and form intrusive veins, submarine extrusions and piltow lavas (Smulikowski 1930; Kudelaskova, 1987; Na- rębski, 1990). Analysis of the Cretaceous hydrothermally altered picrite from the Czech Repubtic led to the conclu- sion that the hydrothermal fluids were released by the dia- genetically dewatered clay minerals in flysch sediments (Dolnicek et al., 2010, 2012). Therefore, the material stu- died could have been affected by similar processes. 130 P. WOJCIK-TABOL & A. SLĄCZKA CON CLU SIONS Continuous sedimentation of dark turbiditic to hemipe- lagic deposits in the western part of the Silesian Basin lasted more than 20 Ma, from the Late Jurassic to the Early Creta- ceous. The sed-mentation of siliciclastics rich in organic matter in the Silesian basin, was controlled by such global events as climatic and CCD changes, as was the case for other black shales (Emeis and Weissert, 2009; Jenkyns, 2010), but also by more local factors, such as the shape of the basin and its evotution, the production of detritus, and sedimentary and diagenetic processes. The warm and humid climate of Late Jurassic-Creta- ceous time promoted chemical weathering. Intense weather- ing of the source rocks was inferred from Na, Sr, and U de- pletion, expressed as negative anomalies in multi-elements patterns normalized to UCC, 75.98 < CIA < 89.86 and sam- ples plotting at the A apex on the A-CN-K diagram, and Th/U ratios (~4 with outliers at 1.85 and >6). Heavy mineral associations, including both rounded and unabraded grains of zircon and rutile, enrichment in Zr and Hf, as well as high Zr/Sc ratios suggest that the Hradiste and Verovice forma- tions contain recycled material. On plots of La/Th versus Hf and Th against Sc, the data occupy the field of felsic material with admixtures from ba- sic sources. The tectonic province of the source area can be determined on the basis of a La-Th-Sc diagram as a conti- nent al isl and arc (CIA). Diagenetic processes could have exerted an influence on the Lower Cretaceous sequences of the Silesian Unit. Concentrations of Fe and trace metals (e.g., Mo, Au, Cu) in the Verovice Formation and silica and potassium additions in the Verovice and Lhoty formations, as well as fractionation of REE and Nb, Ta, Zr, Hf, and Y, can be explained as resulting from the action of basinal bri- nes. The flu-ds were of hydrothermal origin and/or were released, owing to the dewatering of clay minerals. The im- pact of diagenetic processes on the sed-ment chem-stry is even greater than that of provenance and sedimentary pro- cesses. Ac knowl edg ments This work was supported by the Pol- sh Min-stry of Science and Higher Education (Grant N 307 256139). Many thanks are of- fered to T. Malata, C. J. Hetherington, and B. Budzyń for critical comments on the first version of the paper, I. Gonzal ez-Alvarez for additional remarks and to A. Uchman, F. Simpson and W. Mi- zerski for linguistic and editorial corrections. REFERENCES Abanda, P. A. & Hannigan, R. E., 2006. Effect of diagenesis on trace element partitioning in shales. Chemical Geology, 230: 42-59. Belousova, E. A, Griffin, W. L., O’Reilly, S. Y. & Fisher, N. J., 2002. Igneous zircon: trace element composition as an indica- tor of source rock type. Contributions to Mineralogy and Pe- trology, 143: 602-622. Bhatia, M. R. & Crook, K. A. W., 1986. Trace element character- istics of graywackes and tectonic setting discrimination of sedimentary basins. Contributions to Mineralogy and Petrol- ogy, 92: 181-193. Bieda, F., Geroch, S., Koszarski, L., Książkiewicz, M. & Żytko, K., 1963. Stratigraphia wniechnikh polskikh Karpat . Biuletyn Instytutu Geologicznego, 181: 1-174. [In Russian]. Bland, W. & Rolls, D. 1998. Weathering. An Introduction to the Scientific Principles. Arnold Publishers, London, 271 pp. Bozkaya, Ö. & Yalęm, H., 2004. Diagenetic to low-grade meta- morphic evolution of clay mineral assemblages in Palaeozoic to early Mesozoic rocks of the Eastern Taurides, Turkey. Clay Minerals, 39: 481-500. Burtan, J., Chowaniec, J. & Golonka, J., 1984. Preliminary results of studies on exotic carbonate rocks in the western part of the Polish flysch Carpathians. Biuletyn Instytutu Geologicznego, 346: 147-156. [In Polish, English summary]. Campos Alvarez, N. O. & Roser, B. P., 2007. Geochemtstry of black shales from the Lower Cretaceous Paja Formation, Eastern Cordillera, Colombia: Source weathering, prove- nance, and tectonic setting. Journal of South American Earth Sciences, 23: 271-289. Cieszkowski, M., Gedl, E., Slączka, A. & Uchman, A., 2001. Stop C2-Rzyki village. In: Cieszkowski, M. & Slączka, A. (eds), Silesian & Subsilesian Units. 12th Meeting of the Association of European Geological Societies & LXXII Zjazd Polskiego Towarzystwa Geologicznego, Field Trip Guide. Pol-sh Geo- logical Institute, Warszawa, pp. 115-118. Cieszkowski, M., Golonka, J., Slączka, A. & Waśkowska, A., 2012. Role of the olistostromes and olistoliths in tectonostra- tigraphic evotution of the Silesian Basin in the Outer West Carpathians. Tectonophysics, 568-569: 248-265. Cox, R., Lowe, D. R. & Cullers, R. L., 1995. The influence of sedi- ment recycling and basement composition on evolution of mudrock chemtstry in the southwestern United-States. Geo- chimica et Cosmochimica Acta, 59: 2919-2940. Cullers, R. L., 2000. The geochemtstry of shales, siltstones and sandstones of Pennsylvanian-Permian age, Colorado, USA: implications for provenance and metamorphic studies. Lithos, 51: 181-203. Dolnicek, Z., Kropac, K., Janickova, K. & Urubek, T., 2012. Diagenetic source of fu-ds caus-ng the hydrothermal alter- ation of teschenites in the Silesian Unit, Outer Western Car- pathians, Czech Republic: Petroleum-bearing vein mineral- ization from the Stfibrnik site. Marine and Petroleum Geol- ogy, 37: 27-40. Dolnicek, Z., Urubek, T. & Kropac, K., 2010. Post-magmatic hy- drothermal mineralization associated with Cretaceous picrite (Outer Western Carpathians, Czech Republic): interaction be- tween host rock and externally derived fluid. Geologica Car- pathica, 61, 4: 327-339. Elderfield, H., Upstill-Goodard, R. & Sholkovitz, E. R., 1990. The rare earth elements in rivers, estuaries and coastal sea waters: processes affecting crustal input of elements to the ocean and their significance to the composition of seawater. Geochimica et Cosmochimica Acta, 55: 1807-1813. Emeis, K.C. & Weissert, H., 2009. Tethyan-Mediterranean or- ganic carbon-rich sed-ments from Mesozoic black shales to sapropeles. Sedimentology, 56: 247-266. Eynatten, H., von, 2004. Statistical modelling of compositional trends in sediments. Sedimentary Geology, 171: 79-89. Fedo, C. M., Nesbitt, H. W. & Young, G.M. 1995. Unraveling the effects of potassium metasomatism in sedimentary rocks and paleosols, with implications for paleoweathering conditions and provenance. Geology, 23: 921-924. Fedo, C. M., Young, G. M., & Nesbitt, G. M., 1997. Paleoclimatic control on the composition of the Paleoproterozoic Serpent PROVENANCE OF LOWER CRETACEOUS DEPOSITS 131 Format ion, Huronian Supergroup, Canada: A greenhouse to icehouse transition. Precambrian Research, 86: 201-223. Floyd, P. A. & Leveridge, B. E., 1987. Tectonic environment of the Devonian Gramscatho basin south Cornwall: framework mode and geochemi cal evi dence from turbiditic sandstones. Journal of the Geological Society, 144: 531-542. Garcia, D., Coelho, J. & Perrin, M., 1991. Fractionation between TiÜ2 and Zr as a measure of sort-ng within shale and sand- stone series (northern Portugal). European Journal of Miner- alogy, 3: 401-414. Gedl, E., 2003. Biostratygrafia i paleoekologia warstw wierzow- skich i lgockich jednostki slaskiej polskich Karpat fliszowych na zachód od Raby w świetle badan palinologicznych. Un- pub-ished Ph.D. thesis, Jagiellonian University, 246 pp. [In Polish]. Geroch, S., Gucwa, I. & Wieser, T., 1985. Manganese nodules and other indications of regime and ecological environment in lower part of the Upper Cretaceous - exemplified by Lancko- rona profile. In: Wieser T. (ed.), 13th Congress of Carpatho- Balkan Geological Association: Fundamental Researches in the Western Part of the Polish Carpathians, Guide to Excur- sion I. CBGA XIII Congress, Cracow 1985. Geological Insti- tute, Cracow, pp. 88-100. Geroch, S. & Nowak, W., 1963. Lower Cretaceous in Lipnik near Bielsko, Western Carpathians. Rocznik Polskiego Towarzy- stwa Geologicznego, 33: 241-263. [In Polish, Eng-ish sum- mary]. Golonka, J., Gahagan, L., Krobicki, M., Marko, F., Oszczypko, N. & Slączka, A., 2006. Plate-tectonic evolution and paleogeo- graphy of the circum-Carpathian region. In: Golonka, J. & Picha, F. (eds), The Carpathians and their Foreland: Geology and Hydrocarbon Resources. American Association of Petro- leum Geologists Memoir, 84: 11-46. Golonka, J., Krobicki, M., Waśkowska-Oliwa, A., Słomka, T., Skupien, P, Vasicek, Z., Cieszkowski, M. & Slączka, A., 2008. Lithostratigraphy of the Upper Jurassic and Lower Cre- taceous deposits of the western part of Outer Carpathians (discussion proposition). Geologia, 34: 9-31. [InPolish, Eng- lish summary]. Gonzalez-Alvarez, I. & Kerrich, R., 2010. REE and HFSE mobil- ity due to protracted flow of basinal brines in the Mesopro- terozoic Belt-Purcell Supergroup, Laurentia. Pre cam brian Research, 177: 291-307. Grabowski, J., Krzemiński, L., Nescieruk, P., Paszkowski, M., Szydło, A., Pecskay, Z. & Wojtowicz, A., 2004. New data on the age of teschenitic roks (Outer Carpathians, Silesian Unit) - results of the K-Ar dating. Przegląd Geologiczny, 52: 40- 46. [In Polish, English summary]. Grzebyk , J. & Leszczyński, S., 2006. New data on heavy minerals from the Upper Cretaceous-Paleogene flysch of the Beskid Sląski Mts. (Pol-sh Carpathians). Geological Quarterly, 50: 265-280. Hofer, G., Wagreich, W. & Neuhuber, S., 2013. Geochemistry of fine-grained sediments of the upper Cretaceous to Paleogene Gosau Group (Austria, Slovakia): Implications for paleoenvi- ronmental and provenance studies. Geoscience Frontiers, 4: 449-468. Hoskin, P. W. O., 2005. Trace-element composition of hydrother- mal zircon and the alteration of Hadean zircon from the Jack Hills, Australia. Geochimica et CosmochimicaActa, 69: 637- 648. Hu, Z. & Gao, S., 2008. Upper crustal abundances of trace ele- ments: A revision and update. Chemical Geology, 253: 205- 221. Ivan, P., Hovorka, D. & Meres, S., 1999. Riftogenic volcanism in the Western Carpathian geologkal history: a review. Geo- line, 9: 41-47. Jenkyns, H. C., 2010. Geochemtstry of oceanic anoxic events. Geochemistry Geophysics Geosystems, 11: 1-30. Johnsson, M. J. 1993. The system controlling the composition of clastic sediments. In: Johnsson, M. J. & Basu, A. (eds), Pro- cesses Controlling the Composition of Clastic Sediments. Geological Society of America Special Paper, 285: 1-19. Klominsky, J., Jarchovsky, T. & Rajpoot, G. S. (eds), 2010. Atlas of Plutonic Rocks and Orthogneisses in the Bohemian Massif. Czech Geological Survey, Prague. Koszarski, L. & Nowak, W., 1960. Notes on the age of the Lgota Beds (Carpathian Flysch). Kwartalnik Geologiczny, 4: 468- 483. [In Polish]. Kovac, M., Nagymarosy, A., Oszczypko, N., Slączka, A., Cson- tos, L., Marunteanu, M., Matenco, L. & Marton, E., 1998. Palinspastic reconstruction of the Carpathian-Pannonian re- gion during the Miocene. In: Rakus, M. (ed.), Geodynamic Development of the Western Carpathians. Slovak Geological Survey, Bratislava. pp. 189-217. Książkiewicz, M., 1951. Objaśnienia arkusza Wadowice. Ogólna mapa geologiczna Polski 1: 50 000. Państwowy Instytut Geo- logiczny, Warszawa, 283 pp. [In Polish]. Książkiewicz, M., 1962 (ed.). Geological Atlas of Poland. Strati- graphic and Facial Probtems, 1:600 000, Book 13, Cretat ceous and Early Tertiary in the Polish External Carpathians. Instytut Geologiczny. [In Polish, English summary]. Książkiewicz, M., 1964. On the tectonics of the Cieszyn Zone. A reinterpretation. Bultetin of the Polish Academy of Sciences, 12: 251-260. Książkiewicz, M., 1968. Evolution structurale des Carpathes polo- naises. Memoires de la Societe Geologique de France, 42: 529-562. Kudelaskova, J., 1987. Petrology and geochemtstry of se-ected rock types of teschenite associat ion, Outer Western Carpa- thians. Geologica Carpathica, 38: 545-573. Larson, R. L., 1991. Latest pulse of Earth: Evidence for mid-Cre- taceous superplume. Geology, 19: 547-550. Lemoine, M., 2003. Schistes lustres from Corsica to Hungary: back to original sediments and tentative dating of partly azoic metasediments. Bulletin de la. Societe Geologique de France, 174: 197-209. Lucińska-Anczkiewicz, A., Villa, I. M., Anczkiewicz, R. & Slączka, A., 2002. 39Ar/40Ar dating of alkaline lamprophyres from Polish Western Carpathians. Geologica Carpathica, 53: 45-52. McManus, J., Berelson, W. M., Klinkhammer, G. P., Hammond, D. E., Holm, C., 2005. Authigenic uranium: re-ationship to oxygen penetration depth and organic carbon rain. Geochi- mica et Cosmochimica Acta, 69: 95-108. McLennan, S. M., 1993. Weathering and global denudation. Jour- nal of Geology, 101: 295-303. McLennan, S.M., Hemming, D.K. & Hanson, G.N., 1993. Geo- chemical approaches to sedimentation, provenance, and tec- tonics. Geological Society of America, Special Publications, 284: 21-40. McLennan, S. M., Tay-or, S. R. & Eriksson, K. A. 1983. Geo- chem-stry of Archean shales from the Pilbara Supergroup, Western Australia. Geochimica et Cosmochimica Acta, 47: 1211-1222. McLennan, S. M.,. Taylor, S. R. & Hemming, S. R., 2006. Com- position, differentiation, and evolution of continental crust: constrains from sedimentary rocks and heat flow. In: Brown, M. & Rushmer, T. (eds), Evolution and Differentiation of the Continental Crust. Cambridge University Press, pp. 92-134. 132 P. WÓJCIK-TABOL & A. SLĄCZKA Murali, A. V., Parthasarathy, R., Mahadevan, T. M. & Sankar Das, M., 1983. Trace element characteristics, REE patterns and partition coefficients of zircons from different geological en- vironments - A case study on Indian zircons. Geochimica et Cosmochimica Acta, 47: 2047-2052. Narębski, W., 1990. Early rift stage in the evotution of western part of the Carpathians: geochemical evidence from limbur- gite and teschenite rock series. Geologica Carpathica, 41: 521-528. Nesbitt, H. W., Fedo, C. M. & Young, G. M., 1997. Quartz and feldspar stability, steady and nonsteady-state weathering, and petrogenesis of siliciclastic sands and muds. Journal of Geol- ogy, 105: 173-191. Nesbitt, H. W., Markovics, G. & Price, R. C., 1980. Chemical pro- cesses affecting alkalies and alkaline earths during chemical weathering. Geochimica et Cosmochimica Acta, 44: 1659- 1666. Nesbitt, H. W. & Young, G. M. 1982. Early Proterozoic climates and plate motions inferred from major element chemistry of lutites. Nature, 199: 715-717. Nesbitt, H. W. & Young, G. M. 1984. Prediction of some weather- ing trends of plutonic and volcanic rocks based on thermody- namic and kinetic considerations. Geochimica Cosmochimica Acta, 48: 1523-1534. Olszewska, B., 1997. Foraminiferal biostratigraphy of the Poli sh Outer Carpathians: a record of basin geohistory. Annales So- cietatis Geologorum Poloniae, 67: 325-337. Oszczypko, N., 2006. Late Jurassic-Miocene evolution of the Outer Carpathian fold-and-thrust belt and its foredeep basin (Westtrn Carpathians, Po-and). Geological Quarterly, 50: 169-194. Oszczypko, N. & Oszczypko-Clowes, M., 2009. Stages in the Magura Bas in: a case study of the Poli sh sect or (Western Carpathians). Geodinamica Acta, 22: 83-100. Oszczypko, N., Salata, D. & Krobicki, M., 2012. Early Cretaceous intra-plate volcanism in the Pieniny Klippen Belt - a case study of the Velykyi Kamenets’/Vilkhivchyk (Ukraine) and Biała Woda (Poland) sections. Geological Quarterly, 56: 629-648. Oszczypko, N., Krzywiec, P., Popadiuk, I. & Peryt, T., 2006. Carpathian Foredeep Basin (Po-and and Ukraine): Its sedt mentary, structural, and geodynamic evolution. In: Golonka, J. & Picha, F. (eds), The Carpathians and their foreland: Ge- ology and hydrocarbon resources. American Association of Petroleum Geologists Memoir, 84: 261- 318. Poprawa, P., Malata, T. & Oszczypko, N., 2002. Tectonic evolu- tion of the Polish part of Outer Carpathian’s sedimentary bas- ins - constraints from subsidence analysis. Przegląd Geolo- giczny, 50: 1092-1108. [In Polish, English summary]. Poprawa P., Malata, T., Oszczypko, N., Słomka, T. & Golonka, J., 2006. Analysis of tectonic subsidence and sedyment deposi- tion rate for the sedtmentary bastns of the Western Outer Carpathians. In: Oszczypko, N., Uchman, A. & Malata, E. (eds), Palaeotectonic Evolution of the Outer Carpathian and Pieniny Klippen Belt Basins. Instytut Nauk Geologicznych Uniwersytetu Jagiellońskiego, Kraków. pp. 179-199. [In Pol- ish, English Sumary]. Poprawa, P., Malata, T., Pecskay, Z. & Banaś, M., 2004. Geochron- ology of crystal-ine basement of the Western Outer Carpa- thians’ sediment source areas-preliminary data. Polskie Towa- rzystwo Mineralogiczne - Prace Specjalne, 24: 329- 332. Puglisi, D., 2009. Early Cretaceous flysch from Betic-Maghrebian and Europe Alpine Chains (Gibraltar Strait to the Balkans); comparison and palaeotectonic implications. Geologica Bal- canica, 37: 15-22. Rudnick, R. L. & Gao, S., 2003. The composition of the continen- tal crust. In: Holland, H. D. & Turekian, K. K. (eds), Trea tise on Geochemistry. Elsevier-Pergamon, pp. 1-64. Sandulescu, M., 1988. Cenozoic tectonic history of the Carpa- thians. In: Royden, L. H & Horvath, F. (eds), The Panonian Basin, a Study in Basin Evotution. American Association of Petroleum Geologists Memoir, 45: 17-26. Sholkovitz, E. R., Landtng, W. M. & Lewis, B. L., 1994. Ocean particle chemistry: The fractionation of rare earth elements between suspended particles and seawater. Geochimica et Cosmochimica Acta, 58: 1567-1579. Smulikowski, K., 1930. Les roches eruptives de la zone subbes- kidique en Silesie et Moravie. Kosmos A 54: 3-4. Strzeboński, P., Golonka, J., Waśkowska-Oliwa, A., Krobicki, M., Słomka, T., Skupień, P. & Vasicek, Z., 2009. Verovice For- mation deposits during Early Cretaceous sedimentological re- gimes in the western part of the proto-Silesian Basin (Mo- ravia, the Czech Republic). Geologia, 35: 31-38. [In Polish, English summary]. Slączka, A., (ed.), 1976. Atlas of Paleotransport of Detrital Sedi- ments in the Carpathian - Balkan Mountain System. Instytut Geologiczny, Warszawa, 10 pp. Slączka, A., Kruglow, S., Golonka, J. Oszczypko, N. & Popadyuk, I. 2006. The general geology of the Outer Carpathians, Po- land, Slovakia, and Ukraine. In: Golonka, J. & Picha, F. (eds), The Carpathians and Their Fore land: Geology and Hydro- carbon Resources. American Association of Petroleum Geol- ogists Memoir, 84: 221-258. Slączka, A., Renda, P., Cieszkowski M., Golonka, J. & Nigro, F. 2012. Sedimentary basins evolution and olistoliths formation: The case of Carpathian and Sicilian regions. Tectonophysics, 568-569: 306-319. Taylor, S. R. & McLennan, S. M., 1985. The Continental Crust: Its Composition and Evolution. Blackwell, Oxford, 312 pp. Uchman, A. & Cieszkowski, M., 2008. Stop 1, Zagórnik - the Verovice Beds and their transition to the Lgota Beds: ichno- logy of Early Cretaceous black flysch deposits. In: Pieńkow- ski, G. & Uchman, A. (eds), Ichnological Sites of Poland; The Holy Cross Mountains and the Carpathian Flysch. The Sec- ond In terna tional Congress on Ichnology, Cracow, Potand, August 29-September 8, 2008; Pre-Congress and Post-Con- gress Field Trip Guidebook. Polish Geological Institute, War- szawa, pp. 99-104. Unrug, R., 1968. Kordyliera śląska jako obszar źródłowy mate- riału klastycznego piaskowców fliszowych Beskidu Sląs- kiego i Beskidu Wyspowego. Rocznik Polskiego Towarzy- stwa Geologicznego, 38: 81-164. [In Pol-sh, Eng-ish sum- mary]. Veizer, J. & Mackenzie, F. T., 2003. Evo-ution of sed-mentary rocks. In: Holland, H. D & Turekian, K. K. (eds), Trea tise on Geo chem is try, 7. Elsevier-Pergamon, Oxford, pp. 369-407. Wieser, T., 1948. Egzotyki krystaliczne w kredzie śląskiej okolic Wadowic. Rocznik Polskiego Towarzystwa Geologicznego, 18: 109-150. [In Polish, English summary]. Winkler, W. & Slączka, A., 1992. Sediment dispersal and prove- nance in the Silesian, Dukla and Magura flysch nappes (Outer Carpathians, Po-and). International Journal of Earth Scien- ces, 81: 1437-3254.