Lithos 119 (2010) 251–268

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Magma generation in an alternating transtensional–transpressional regime, theKraków–Lubliniec Fault Zone, Poland

Ewa Słaby a,⁎, Christoph Breitkreuz b, Jerzy Żaba c, Justyna Domańska-Siuda d, Krzysztof Gaidzik c,Katarzyna Falenty e, Andrzej Falenty f

a Institute of Geological Sciences, Polish Academy of Sciences, Research Centre in Warsaw, 00-818 Warszawa, Twarda 51/55, Polandb Institut für Geologie und Paläontologie, TU Bergakademie, 09599 Freiberg, Bernhard von Cotta Str. 2, Germanyc Department of Fundamental Geology, University of Silesia, 41-200 Sosnowiec, Będzińska 60, Polandd Institute of Geochemistry, Mineralogy and Petrology, Warsaw University, 02-089 Warszawa, Żwirki i Wigury 93, Polande Mineralogy Department GZG, Georg-August-University, 37077 Göttingen, Goldschmidtstrasse 1, Germanyf Leibnitz Institute for Baltic Sea Research Warnemünde, 18119 Rostock-Warnemünde, Seestrasse 15, Germany

⁎ Corresponding author. Fax: +48 22 6206223.E-mail address: e.slaby@twarda.pan.pl (E. Słaby).

0024-4937/$ – see front matter © 2010 Elsevier B.V. Aldoi:10.1016/j.lithos.2010.07.003

a b s t r a c t

a r t i c l e i n f o

Article history:Received 9 November 2009Accepted 12 July 2010Available online 8 August 2010

Keywords:Late Carbonifereous–Permian magmatismEast-European cratonGondwana blocksVariscan forelandPaleozoic amalgamationTrace element signature

In the Kraków–Lubliniec Fault Zone (KLFZ) late Carbonifereous–Permian volcanic rocks mark the boundarybetween the Małopolska Block (thinned marginal sector of Baltica) and the Upper Silesian Block (a sector ofthe Brunovistulia composite Terrane). The Zone is a part of the major Hamburg–Kraków–Dobrogeatranscontinental strike–slip tectonic zone separating the Laurussian craton and Gondwana blocks whichcame together to form it. The geochemistry of the volcanic rocks reflects the collisional nature of thetectonism. However, it also presents a signature compatible with extensional magmatism. The paperpresents models of magma generation and evolution in what was a zone of alternating transpression andtranstension. The magmatism in this zone of amalgamated terranes was related to two different sources:enriched mantle and primitive crust. The lithospheric mantle beneath some blocks of the amalgamatedterranes may have experienced enrichment processes during previous subduction events. The metasoma-tism may have also occurred as a result of crustal thickening during transpression followed by delamination,subsidence and melting. These metasomatised blocks reacted with decompressional melting. Our resultsshow that magma generation and evolution in the zone seem to be not typical examples of lateCarbonifereous–Permian magmatism, which is known from other locations throughout Central Europe.

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1. Introduction

The amalgamation of terranes is usually accompanied by intensivemagmatic activity. The Trans-European Suture Zone (TESZ), one of themost important composite suture zones in Europe, separates the East-European craton from a mosaic of western European compositeblocks. In the Kraków–Lubliniec Fault Zone (part of the majorHamburg–Kraków–Dobrogea transcontinental strike–slip tectoniczone), parallel to TESZ, late Carbonifereous–Permian volcanic rocksmark the boundary between the Małopolska Block (a thinnedmarginal sector of Baltica) and the Upper Silesian Block (a sector ofthe Brunovistulia composite Terrane) (Brochwicz-Lewiński et al.,1986b; Dadlez et al., 1994; Buła et al., 1997; Żaba, 1999; Malinowski etal., 2005; Żelaźniewicz et al., 2009). Although clearly related to suturezones, the present tectonic and stratigraphic settings do not provide aclear answer to the origin of themagmatismwithin Kraków–Lubliniec

Fault Zone. The present work aims to present a new model of magmageneration and subsequent evolution in what was both a transpres-sional and transtensional regime (a fold-and-thrust belt) between thecollided blocks derived from Gondwana and Baltica respectively. Themodel is based on new and previously published geochemical data.

The cause of the late Carboniferous–Permian magmatism withinthe northern Variscan foreland remains a matter of intensivediscussion (Kramer, 1977; Jakowicz, 1994; Benek et al., 1996; Ziegler,1996; Breitkreuz and Kennedy, 1999; Romer et al., 2001; Breitkreuz etal., 2007). Data on the volcanic rocks along the strike–slip Kraków–

Lubliniec Fault Zone have been scarce (Czerny and Muszyński, 1997;Żelaźniewicz et al., 2008) and this paper attempts to fill this gap.

2. Geological setting

The Kraków–Lubliniec Fault Zone is considered to be a suture zonebetween the Upper Silesian Block and Małopolska Block: the latter is,in turn, attached to the Łysogóry Block (Fig. 1a) (Dadlez et al., 1994;Buła et al., 1997; Pharaoh, 1999; Żaba, 1999; Buła, 2000; Żelaźniewiczet al., 2009). The blocks are inferred to have been derived from either

Fig. 1. a) Structural setting of the Upper Silesian Block andMałopolska Block (after Żaba, 1995, 1999—modified), 1—magmatic phenomena, areas of granitoid intrusions:M—Myszków-Mrzygłód area, Z — Zawiercie area, P — Pilica area, D — Dolina Będkowska area; 2 — study area; TESZ — Trans-European Suture Zone; KLFZ — Kraków-Lubliniec Fault Zone, KChF —

Krzeszowice-Charsznica Fault, RH— Rzeszotary Horst; A–B— line of geological cross— section (see— Fig. 1b). b) Contact of the Upper Silesian Block andMałopolska Block in the Krakówarea (Buła et al., 2008—modified), 1— Permian–Mesozoic–Cenozoic cover rocks, 2—Upper Carboniferous coal-bearing deposits of theUpper SilesianCoal Basin, 3— Lower Carboniferousclastic deposits, 4 — Devonian and Lower Carboniferous carbonate deposits, 5— Silurian rocks, 6 — Lower Cambrian rocks of the Upper Silesian Block, 7 — Ediacaran anchimetamorphicsiliciclastic rocks, and 8 — Archean–Lower Protorozoic (Karelian) crystalline rocks of the Upper Silesian Block.

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Gondwana or Baltica and most are considered as terranes (Pożaryski,1990). The Upper Silesian Block may have Gondwana affinity (Buła etal., 1997). The oldest rocks of the Małopolska and Łysogóry blocksshow faunal and lithological affinities to those of Baltica (Dzik, 1983;Orłowski, 1992; Moczydłowska, 1995; Żylińska, 2002) and arebelieved to have been detached, transported around its margin andfinally re-accreted to it as microplates (Pharaoh, 1999; Winchesterand Team, 2002; Nawrocki et al., 2007b). Their dextral movementalong the side of Baltica to their present location terminated duringthe Carboniferous (Lewandowski, 1993) and has been related toclosure of the Tornquist sea (Berthelsen, 1998). The Thor–Thornquistsuture, known as the Caledonian Deformation Front, is located southof both terranes and is approximately parallel to the TESZ (Guterchand Polonaise, 1999; Fig. 1a). Its south-eastern segment is theKraków–Lubliniec Fault Zone, the south-east continuation of theElbe Line (Winchester and Team, 2002). This Zone is a deep, intensivebrittle fold and fault system that underwent repeated reactivation andmulti-stage deformation (Żaba, 1996; Żaba, 1999; Żaba, 2000),accompanied by intensive late Carboniferous–early Permian magma-tism (Skowroński, 1974; Lewandowska et al., 2007; Nawrocki et al.,2007a). Consequently the Kraków–Lubliniec Fault Zone marks thecontact between Baltica and Paleozoic European Platform.

The magmatism (Fig. 1a, b), involved a bimodal suite of mafic–intermediate (trachybasalts–trachyandesites, with minor lampro-phyres) and felsic (dacites–trachydacites–rhyolites) rocks (Rozen,1909; Bolewski, 1939; Słaby, 1987; Słaby, 1990;Muszyński and Pieczka,1994; Muszyński, 1995; Muszyński and Pieczka, 1996; Czerny andMuszyński, 1997; Lewandowska and Rospondek, 2003; Falenty, 2004;Gniazdowska, 2004). They occur as laccoliths, lava domes (associatedwith pyroclastic rocks), lavas, dykes and sills (Heflik and Muszyński,1993; Muszyński and Czerny, 1999; Czerny et al., 2000; Lewandowskaand Bochenek, 2001; Podemski, 2001). The late Paleozoic magmatism

also comprised deep-seated, calc-alkaline, granodiorite–diorite toquartz monzonite–monzogranite intrusions known from numerousdrill holes (Markiewicz, 2002, 2006). Enclaves of similar compositionhave been found in Zalas laccoliths (Heflik andMuszyński, 1993; Czernyet al., 2000).

3. The origin of the Kraków–Lubliniec Fault Zone magmaticsuite — review of previous work

The petrogenesis of the Kraków–Lubliniec Fault Zone magmas hasbeen the subject ofmany research studies. Rozen (1909) assigned all thevolcanic rocks to differentiation of calc-alkaline magmas. However,Bolewski (1939) related the magmas to two different sources, yieldingcalc-alkaline and high potassium–alkaline suites. The high potassiumnature of the parental melts was questioned by Słaby (1987, 1990,2000), because of the recognition of wide-spread fluid–rock reactionsthat gave rise to adularization and albitization among others. Harańczyk(1989) argued for four different magma types (basic, rhyodacitic,trachytic and lamprophyric). Czerny and Muszyński (1997) recognizedthree types ofmelt (basic, lamprophyric and rhyodacitic) and explainedtrace element concentrations in the rocks as due to variable degrees ofmixing between mafic and lamprophyric melts. Earlier, Bukowy andCebulak (1964) also related the compositional differences to magmamixing, where the end-member magmas were mafic and felsic.Rospondek et al. (2004) considered the intermediate and felsic rocksto be related through fractional crystallization (FC) and, following this,Gniazdowska (2004) and Falenty (2004) demonstrated magmadifferentiation in both the more intermediate and felsic rocks, usinggeochemical modelling of major elements and selected trace elements.They showed that both suites of magmas evolved by fractionalcrystallization but did not, however, consider the mafic and felsicrocks to be comagmatic.

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The present work is based on a compilation of geochemical data formembers of the bimodal suite published by Czerny and Muszyński(1997), Falenty (2004), Gniazdowska (2004), Heflik and Muszyński(1993), Muszyński and Pieczka (1994), Muszyński and Pieczka (1996)and on granitoids published by Heflik and Muszyński (1993) andMarkiewicz (2002). These data were complemented by newgeochemical and isotopic determinations on selected samples (inter-mediate: Tenczynek, Alwernia, Regulice, Belwender lava flows — TAR,Niedźwiedzia Góra sill— NG; acid: Miękinia lava dome—M, and Zalas–Orlej laccolith—ZOR; Fig. 2; Tables1, 2). TheZalas–Orlej laccolith aswellas the Niedźwiedzia Góra sill are high-level intrusions, the textures ofwhich appear to relate them to extrusive rocks of the area. Accordinglythey are considered together with the extrusive group. The rocks aredated at 300 Ma (Nawrocki et al., 2007a).

The volcanic rocks, both intermediate and acid, are generallyporphyritic with holocrystalline matrices. The mineral assemblage issimilar for all intermediate and acid rocks but they differ in their modesand textures. The primary phases of the mafic rocks are plagioclase(An62−40Ab35−57Or2−3), clinopyroxene (En49−38Fs23−14Wo42−36),orthopyroxene (En35− 32Fs66− 63Wo2) and olivine — (Fo60− 57),usually altered. Subordinate components include anorthoclase(Ab52−61Or42−28An6−11), opaque oxides and apatite (Falenty, 2004).Sieve- texture is common inplagioclases in somesamples (e.g. 7, 20, and22).

The acid melts crystallized sodic sanidine (Or85−80Ab20−15),plagioclase (An47−27Ab71−51Or2), biotite (K1.8−1.7Na0.2−0.1)(Al0.2−0.1

Ti0.6−0.5Fe2.0−1.6 Mg3.6−3.2)(Si5.7−5.6Al2.4−2.3)O20(OH)4 and amphi-bole (Na0.9−0.6 K0.1)(Ca1.9−1.8 Mg3.0−2.8Fe2.0−1.6Ti0.3−0.2Al0.9−0.2)(Si6.8−6.3Al1.7−1.2)O22(OH)2;minor components include opaque oxides,apatite, titanite and zircon (Gniazdowska, 2004). The plagioclases show

Fig. 2. The area of investigations; abbreviation: M — Miękinia lava dome, NG — Niedźwiextrusions (after Brochwicz-Lewiński et al., 1986a; Czerny and Muszyński, 2000).

discontinuous, patchy zones with resorption and abundant meltinclusions. Some amphibole contains relics of clinopyroxene (Sutowicz,1982).

The fault zone underwent repeated reactivation and permittedeasy circulation of hydrous fluids. Accordingly much of the primarymineralogy and textures are modified by secondary mineralization(Karwowski, 1988). Among the products are highly potassic feldsparsthat partly replace the plagioclases and also crystallized freely in voidspaces (Słaby, 1987, 1990). The reaction removed calcium and leftremnant albite (Słaby, 1987, 1994). Calcium was immobilized next incarbonates. Alkali feldspars were not altered but sheet silicates, rich inmagnesium were developed in the primary mafic minerals.

Information on the phase composition of granodiorite–diorite toquartz monzonite–monzogranite intrusions is sparse. The rocks aremedium-grained and porphyritic. Plagioclases (An46−26) have con-spicuous, sometimes patchy, zonation with some resorption planes.Alkali feldspar, Mg–hornblende and biotite are mentioned as majorphases by Markiewicz (1998, 2006). Apatite, zircon and titanite areaccessoryminerals. Alteration products are comparable to those in theacid volcanic rocks (Markiewicz, 2006).

4. Analytical methods

Major elements were determined at the Laboratoire Magmas etVolcans, Clermont-Ferrand, using a plasma-source atomic-emissionspectrometer with coupled induction (Jobin-Yvon 70, type Ultima-C);sample treatment was by acid or by alkali fusion. Trace elements wereanalysed at the ACME Analytical Laboratories, Vancouver, (Canada) byICP-MS (Rare Earth and refractory elements by lithium tetraboratefusion and base metals by Aqua Regia digestion).

edzia Góra sill, ZOR — Zalas–Orlej laccolith, TAR — Tęczynek–Alwernia–Regulice lava

1 Numbers given in parentheses refer to data taken from cited papers.

Table 1Chemical composition of intermediate extrusive rocks.

Samplewt.%

5 6 7 15 16 20 21 22 26 27 28 29

Niedźwiedzia Góra (NG) Tęczynek–Alwernia–Regulice (TAR)

SiO2 53.6 53.7 53.3 51.2 52.9 53.6 52.8 52.8 52.3 51.9 50.5 51.8Al2O3 15.5 15.6 15.5 15.9 16.2 16.6 16.5 16.7 15.6 15.6 16.2 15.6Fe2O3 10.9 11.0 11.1 8.97 8.59 8.42 9.80 9.27 11.0 11.0 11.1 9.92MnO 0.16 0.15 0.17 0.10 0.10 0.08 0.14 0.13 0.16 0.16 0.09 0.10MgO 4.01 4.20 4.04 4.94 4.67 4.08 3.82 4.28 3.74 3.59 4.15 3.90CaO 6.37 6.47 6.47 7.18 7.49 8.02 7.05 7.28 7.00 6.91 4.63 6.34Na2O 3.59 3.85 3.76 2.98 3.31 3.64 3.81 3.45 3.41 3.56 3.63 3.51K2O 1.83 1.98 2.08 2.50 2.17 0.67 1.05 0.98 2.39 2.36 3.23 3.07TiO2 1.72 1.80 1.81 1.58 1.61 1.63 1.60 1.62 1.63 1.62 1.71 1.61P2O5 0.79 0.85 0.83 0.48 0.47 0.37 0.66 0.48 0.63 0.60 0.02 0.56LOI 1.62 1.16 1.2 4.1 2.4 2.97 2.55 2.83 2.44 2.28 3.99 2.67Sum 100.1 100.8 100.3 99.9 99.9 100.1 99.8 99.8 1003 99.6 99.0 99.1A/CNK 0.80 0.77 0.77 0.77 0.76 0.78 0.81 0.84 0.74 0.74 0.90 0.76Mg# 0.42 0.43 0.42 0.52 0.52 0.49 0.44 0.48 0.40 0.39 0.43 0.44ppmBa 728 806 1021 1032 1030 1210 1042 1133 1105 1191Be 2 2 2 1 2 1 1 2 2 2Co 25 26 26 25 25 25 28 30 30 21Cs 1.30 0.50 6.40 1.10 0.70 1.10 1.60 0.90 0.90 0.90Ga 21 21 19 20 20 21 20 20 22 21Hf 8.7 8.9 5.6 6.6 5.5 7.3 5.6 6.9 6.8 7.0Ni 32 29 58 61 64 43 69 41 42 48Nb 38 39 17 17 16 23 17 24 25 22Rb 37 42 42 28 38 53 34 45 44 55Sr 444 477 891 892 933 1 082 907 960 966 960Ta 2.2 2.2 1.1 1.1 1.0 1.4 1.0 1.5 1.5 1.4Th 5.9 7.0 12.3 11.2 12.0 14.1 12.5 13.0 13.7 15.2U 1.0 1.2 1.6 1.7 1.7 1.8 1.4 1.1 1.2 1.8V 118 125 166 157 167 176 159 162 154 164Zr 345 371 219 221 213 269 220 270 275 258Y 44 48 31 32 30 38 37 36 36 37La 55.5 59.8 60.9 61.5 61.3 82.1 68.1 73.8 70.5 76.7Ce 122.6 131.0 126.4 129.3 125.7 173.2 133.4 154.7 149.3 159.1Pr 14.6 15.8 15.0 15.0 14.8 20.6 16.4 18.0 17.9 19.2Nd 56.7 61.7 56.5 56.7 57.8 75.6 60.9 65.1 66.5 69.6Sm 11.0 12.3 9.9 9.9 9.5 13.0 10.9 12.5 12.1 12.6Eu 2.9 2.9 2.7 2.8 2.6 3.5 2.8 3.1 3.2 3.2Gd 9.1 9.9 7.1 7.5 7.0 9.2 8.0 8.4 8.8 9.1Tb 1.6 1.6 1.1 1.1 1.0 1.4 1.2 1.3 1.3 1.3Dy 8.3 8.6 5.8 5.7 5.6 7.0 6.2 7.0 7.0 7.0Ho 1.6 1.6 1.1 1.1 1.1 1.3 1.2 1.3 1.3 1.3Er 4.5 5.0 3.0 3.2 2.9 3.8 3.4 3.7 3.5 3.5Tm 0.6 0.7 0.4 0.5 0.4 0.5 0.5 0.5 0.5 0.5Yb 4.0 4.3 2.5 2.7 2.5 3.3 2.9 3.3 3.3 3.0Lu 0.6 0.6 0.4 0.4 0.4 0.5 0.5 0.5 0.5 0.5Nb/Y 0.8 0.8 0.6 0.5 0.5 0.6 0.5 0.7 0.7 0.6La/Yb 13.9 13.9 24.5 23.0 24.2 25.0 23.6 22.5 21.7 25.5(ΣLILE/Nb)N 10.6 11.1 29.1 27.5 27.8 24.9 27.8 22.6 22.2 28.0(Sr/Ce)N 0.30 0.31 0.59 0.58 0.62 0.53 0.57 0.52 0.54 0.51(P/Nd)N 0.95 0.90 0.56 0.55 0.42 0.57 0.52 0.64 0.59 0.55LaN 13.9 13.9 24.5 23.0 24.2 25.0 23.6 22.5 21.7 25.5LaN/YbN 9.2 9.2 16.1 15.2 16.0 16.5 15.6 14.9 14.3 16.8143Nd/144Nd 0.512419 0.512369 0.51237787Sr/86Sr 0.706659 0.707475

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Nd and Sr isotope analyses were performed on 100 mg powdersamples at the Institute of Geological Sciences of the PolishAcademy of Sciences in Warsaw; 143Nd/144Nd isotopic ratios weredetermined on a VG Sector 54 mass spectrometer in multi-collectordynamic mode. 143Nd/144Nd ratios were normalized to 146Nd/144Nd=0.7219. εT(Nd??) values were calculated using values of thepresent-day depleted mantle as: 143Nd/144Nd=0.512638 and147Sm/144Nd=0.1967 following a radiogenic linear growth for themantle with εNd=0 at 4.568 Ga. The 87Sr/86Sr ratios and Rb and Srconcentrations were measured with a VG Sector 54 mass spec-trometer in multi-collector dynamic mode. All results werenormalized to 86Sr/88Sr=0.1194 to correct for machine fraction-ation. Replicate analyses of NBS SRM 987 standard gave an averagenormalized 87Sr/86Sr ratio of 0.710252±0.000020 (2σ, n=22).

5. Geochemistry

The intermediate volcanic rocks show a fairly small range in Mg#(atomic Mg/(Mg+Fe) 0.39–0.52 (0.33–0.57)1) and in SiO2 content(50.5–53.7 wt.%; Table 1) (up to 56.6 wt.%). According to the TASdiagram (Le Maitre et al., 1989) (Fig. 3a), they are mainly basaltic–trachyandesites to basaltic andesites. Glass, found by Rospondek et al.(2004) in the rock groundmass, is peraluminous rhyolite. Theintermediate volcanic rocks are metaluminous (Fig. 3b), calc-alkalineand medium-K to shoshonitic (Rickwood, 1989) (Fig. 3c), with Na2O/K2O ratio of 1.1–5.4 (1.26–1.89)1. The steep increase in K content

Table 2Chemical composition of acid extrusive rocks.

Samplewt.%

1 2 3 4 8 9 10 11 12 13 14 23 24 25

Zalas–Orlej (ZOR) Miękinia (M) Zalas–Orlej (ZOR)

SiO2 65.9 67.0 69.2 68.3 68.2 68.3 67.8 68.3 66.6 67.7 68.1 68.8 69.1 64.5Al2O3 13.9 14.2 14.9 14.8 15.2 15.4 15.1 15.4 15.2 15.4 15.2 14.9 14.5 14.1Fe2O3 2.47 2.62 2.81 3.14 3.65 3.74 3.56 3.74 3.47 3.63 3.76 3 2.89 3.57MnO 0.04 0.04 0.03 0.03 0.02 0.02 0.02 0.02 0.03 0.02 0.03 0.05 0.05 0.07MgO 1.32 1.42 1.07 1.31 0.48 0.51 0.64 0.51 0.65 0.71 0.65 0.84 0.88 1.25CaO 1.89 1.55 2.1 2.74 2.59 2.77 2.6 2.77 3.09 2.8 3.19 2.91 2.61 3.06Na2O 0.88 0.92 4.22 4.25 3.23 3.18 3.12 3.18 2.36 3.05 3.34 3.73 3.64 2.26K2O 7.84 7.77 3.79 2.99 4.2 4.47 4.81 4.47 4.56 5.12 3.61 3.69 3.6 4.7TiO2 0.39 0.39 0.38 0.43 0.5 0.51 0.49 0.51 0.5 0.49 0.49 0.38 0.38 0.39P2O5 0.12 0.11 0.10 0.13 0.27 0.26 0.39 0.26 0.69 0.38 0.52 0.09 0.08 0.07LOI 4.64 4.42 1.15 1.82 0.89 1.39 0.91 1.39 3.11 1.3 1.72 2.15 2.54 5.07Sum 99.4 100.4 99.8 99.9 99.2 100.6 99.4 100.6 100.3 100.6 100.6 100.5 100.3 99.0A/CNK 1.04 1.11 1.00 0.97 1.04 1.02 1.00 1.02 1.05 0.98 1.00 0.96 0.99 0.98Mg# 0.51 0.52 0.43 0.45 0.21 0.21 0.26 0.21 0.27 0.28 0.25 0.36 0.38 0.41ppmBa 662 753 895 824 836 901 818 825 817 832.2Be 1.0 2.0 2.0 1.0 1.0 2.0 1.0 1.0 2.0 2.0Co 4.5 5.1 3.4 3.3 4.1 3.3 4.6 6.6 4.6 4.8Cs 20 2.3 3.3 3.6 4.8 5.0 3.5 5.6 2.5 4.6Ga 16 17 19 18 17 18 17 19 19 18Hf 3.6 4.0 5.2 4.5 4.8 5.0 4.5 4.4 3.5 3.8Ni 2.7 3.0 3.8 3.9 4.1 3.9 3.2 4.5 2.6 2.4Nb 7.8 9.1 11.7 11.1 11.3 11.8 10.9 10.8 9.2 9.4Rb 166 88 108 111 120 133 115 108 88 98.6Sr 38 270 270 266 227 250 250 267 266 209.1Ta 0.7 0.8 1.0 0.9 1.0 1.0 1.1 1.0 0.8 0.8Th 7.1 8.9 9.5 9.0 9.0 10.0 8.5 7.9 9.5 8.3U 1.7 2.1 1.5 1.3 1.5 1.4 1.6 1.2 1.5 1.3V 38 40 55 51 53 53 50 48 39 36Zr 118 130 168 163 159 168 161 157 126 125Y 14 15 17 16 17 18 16 16 14 15La 23.2 25.7 32.9 31.4 32.0 34.0 32.1 30.5 25.5 25.7Ce 45.6 51.3 63.5 59.0 59.6 64.5 59.5 58.6 48.8 50.6Pr 5.1 5.6 6.7 6.4 6.7 6.9 6.6 6.4 5.3 5.6Nd 18.1 19.8 24.0 24.6 23.7 25.3 23.1 23.0 19.3 19.9Sm 3.5 3.6 4.2 4.2 4.0 4.2 4.1 4.2 3.7 3.8Eu 0.78 0.97 1.08 1.12 0.99 1.07 1.02 0.97 0.85 0.92Gd 2.8 3.1 3.3 3.2 3.2 3.3 3.3 3.2 2.9 3.0Tb 00...4 0...5 0...6 0...5 0...5 0...5 0...5 0...5 0...5 0...5Dy 2.2 2.6 3.1 2.7 3.1 3.1 2.8 2.7 2.5 2.6Ho 0.5 0.5 0.6 0.5 0.6 0.6 0.5 0.5 0.5 0.5Er 1.4 1.5 1.6 1.5 1.7 1.7 1.6 1.6 1.4 1.5Tm 0.2 0.3 0.2 0.3 0.2 0.2 0.2 0.2 0.2 0.2Yb 1.2 1.3 1.6 1.6 1.5 1.4 1.5 1.4 1.4 1.4Lu 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2 0.2Nb/Y 0.6 0.6 0.7 0.7 0.7 0.6 0.7 0.7 0.6 0.6La/Yb 18.7 19.9 20.6 19.9 21.1 23.8 21.3 21.5 18.9 18.1(ΣLILE/Nb)N 70.9 45.0 40.9 42.5 43.4 43.8 44.7 40.6 45.2 44.4(Sr/Ce)N 0.07 0.44 0.36 0.38 0.32 0.33 0.35 0.38 0.46 0.35(P/Nd)N 0.40 0.34 0.73 0.68 1.07 0.67 1.06 1.47 0.29 0.27LaN 73.7 81.6 104.4 99.7 101.6 107.9 101.9 96.8 81.0 81.6LaN/YbN 13.2 12.5 13.6 13.1 13.9 15.7 14.0 14.2 12.5 12.0143Nd/144Nd 0.512224 0.512232 0.512219 0.512218 0.51221687Sr/86Sr 0.709858 0.710638 0.712192 0.712059 0.711994

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cannot entirely be due to magma differentiation and partly reflectsalteration leading to the formation of K-rich hydrothermal feldspars(Słaby, 1987, 1990, 1994, 2000).

As for the intermediate rocks, the acid rocks display a relativelynarrow range of SiO2 content (64.5–69.2 wt.%; Table 2); (68.3–70.0 wt.%1; 64.9–78.9 wt.%1 for granitoids). The Mg# ranges from 0.21to 0.45 (Table 2); (0.21–551; 0.31–0.601 for granitoids). Two sampleswith higher Mg# value (0.51–0.52) show some alteration. The rocksare mostly trachydacites–dacites (Fig. 3a); with a few rhyolites. Therocks are calc-alkaline, high-K to shoshonitic; compared to theintermediate rocks, they are more potassic (Fig. 3c). As in theintermediate rocks, K-enrichment probably reflects secondary alter-ation. A/CNK indices (Shand, 1943) of 0.96–1.16 (up to 1.29)1 placethem and the granitoids into both the metaluminous and peralumi-nous fields. The acid rocks have compositions nearby the quartz–

feldspar cotectics in the hydrous granitic system being consistent withpressures ranging between 5 and 10 kbars (not shown) (Winkler,1974). The pressure calculated from the Al-in-amphibole geobarom-eter (Schmidt, 1992) in Miękinia and Zalas–Orlej rocks, gave similarresults: 5.7–7.4±0.6 kbar.

Compositional variation in the extrusive and intrusive suites isshown in Figs. 4 and 5. Most elements in both suites, extrusive acidand intermediate, show negative correlations with silica (Fig. 4).Usually the data for the acid and intermediate suites indicate twodifferent trends that appear unrelated. Compositions of the granitoidsoverlap with those of the acid extrusive rocks. The glass composition,with the exception of Fe and Al, does not match any group (Fig. 4). Inthe intermediate rocks the trends are vertical. The acid rocks tend notto show a clear trend. Those from Miękinia and Zalas–Orlej aresometimes weakly separated from each other (Table 2, Fig. 4) and the

Fig. 3. Rock compositions (I — intermediate, A — acid, GR — granitoids, and G — glass).a) TAS diagram (Le Maitre et al., 1989), (full symbols — own data), open symbols datafrom Czerny and Muszyński (1997); Heflik and Muszyński (1993); Muszyński andPieczka (1994); Markiewicz (2002); and Rospondek et al. (2004). b) Al2O3/(Na2O+K2O) vs. Al2O3/(CaO+Na2O+K2O) molar diagram (Shand, 1943)— intermediate rocksare metaluminous whereas acid rock plot on the boundary between metaluminous andperaluminous composition; and c) K2O vs. SiO2 diagram shows the calc-alkaline,shoshonitic affinity of the rocks; scattered data may point to post-magmatic alteration.

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absence of a clear relationship between the two extrusive suites is alsoshown on the Mg# plots (Fig. 5). On some plots, the acid rocks show adistinct separation into two groups, Miękinia (M) and Zalas–Orlej(ZOR).

The Mg# diagrams show that the most magnesian members werenot primary magmas. The magmas can be derived from a metasoma-tized source. They can be as well significantly affected by crustalcontamination. Zonation of the plagioclases shows, in many cases, acomplex pattern with sieve-like textures and resorption surfaces. Thegeochemistry furthermore points to alterations which can affectselectively some major and trace elements. It is clear that adulariza-tion has caused a remarkable change in the alkali content. Calciumextraction during deuteric alteration shows a limited range of

mobility with a consistent trend. In the felsic rocks alteration of themafic minerals probably caused a slight increase in Mg# (comparewith the description of phase composition). The change is regardedas insignificant because Mg and Fe trends vs. silica content areconsistent.

Using Th as a differentiation index (Fig. 5), variation plots for theintermediate rocks also show a single trend. However, for someelements the acid rocks from Miękinia and Zalas–Orlej there are two,weakly separated trends, generally parallel to each other (comparedata in Table 2 and plots on Fig. 5). Generally there is no accordancebetween the trends for the intermediate and acid rocks, with theexception of Ba. Because of the lack of data it is not possible to relatethe chemistry of the granitoid rocks to that of the extrusive rocks.

The intermediate rocks from Teczynek–Alwernia–Regulice havesmooth, chondrite-normalized LREE-enriched patterns, with LaN/YbN=14.3–16.5 (8.2–17.4)1 (Fig. 6, Table 1). The samples with thehighest and lowest LREE enrichments are indicated on the diagrams.The progressive depletion in HREE is not systematic in all rocks; forexample, the Niedźwiedzia Góra group shows flatter patterns, withLaN/YbN=9.2–9.3 (up to 12.2)1 (Fig. 6, Table 1). These patterns, as theonly ones within the intermediate rocks, are also characterized bysmall Eu anomaly.

The REE patterns of the extrusive acid rocks show lower LREEenrichment than the intermediate rocks. They do not differ muchbetween Miękinia (97bLaNb104) and Zalas–Orley (81bLaNb82)(Table 2). The intrusive rocks are poor in REE relative to the extrusiverocks (Fig. 6). As for the intermediate rocks, the two extrusive sampleswith the highest and lowest LREE enrichment are indicated on thediagrams. All samples show a small negative Eu anomaly Eu/Eu*=0.74–0.90 (Eu/Eu*=EuN/[(SmN+GdN)/2]), almost undetect-able for Miękinia (Fig. 6; sample 13) and slightly larger for Zalas–Orlej(Fig. 6; sample 24). The anomaly may have been caused by minorfractional crystallization of plagioclase.

Primitive mantle-normalized (Sun and McDonough, 1989) traceelement plots (Fig. 7) show Rb, Nb, Sr, P, Zr and Ti anomalies.Rubidium demonstrates similar depletion level as potassium, whichcan be related to the characteristic of their source material. It may alsobehave as compatible (or less incompatible) during melting. Gener-ally all rocks are enriched in LILE relative to Nb. (Nb/LILE)N shows nocorrelation with any differentiation indices (Tables 1, 2) and,inferentially, it has been inherited from the parental magma. Apartfrom the deep negative anomalies for NbN and smaller ones for TiN,the multi-element diagram for Tęczynek–Alwernia–Regulice group issmooth (sample 27, Fig. 7a), suggesting the possibility of an islandarc-related environment. The slight change of Sr and P concentrationin Fig. 7a is inconsistent with either partial melting or fractionation. Itmay be caused by a slight crustal contamination. Smooth REEN patternand no change in the transition elements concentration within thegroup (Table 1) excludes fractionation as a process, which can accountfor the TiN anomaly. This can be linked up to a titanium-rich phase in aresiduum after partial melting.

The normalized multi-element diagram for the Niedźwiedzia Góraintermediate volcanic rocks is quite different and indicates greateraffinity to the pattern for the acid rocks which have significant Sr, P, Zrand Ti anomalies. The origin of these anomalies can be determinedusing the ratio of the normalized element preceding the anomaly tothat of the element exhibiting the anomaly vs. differentiation index(Słaby and Martin, 2008) (Fig. 7).

Both the acid rock group and intermediate Niedźwiedzia Góragroup possess a SrN anomaly. The acid rocks also show clear EuNanomalies in contrast to the intermediate Niedźwiedzia Góra rocks,where the anomaly is weak. The (Sr/Ce)N ratios in both suitesdecreasewith differentiation (cf. the ratio values withMg# in Tables 1and 2). Furthermore, EuN correlates well with SrN in both suites. As Srand Eu are compatible in plagioclase, the Sr anomaly could beexplicable in terms of plagioclase fractionation.

Fig. 4. Harker diagrams. Compilation of own data and data from Czerny and Muszyński (1997), Rospondek et al. (2004) (squares I — intermediate extrusive, circles A — acidextrusives, and hexagon G — glass). The acid rocks show two, weakly separated trends, formed by the Miękinia (M) and Zalas–Orlej (ZOR) data.

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In the acid rocks, a change in the (P/Nd)N ratio from N1 (positiveanomaly decreasing to zero for Miękinia ) to b1 (negative anomaly forZalas–Orlej rocks) and its negative correlation with the differentiationindex (Table 2) point to a role for fractionation and/or accumulation ofan accessory mineral or minerals during magma evolution. The (Ti/Gd)N ratio is negatively correlated with Mg# in the acid rocks and inthe intermediate NG group. The Ti anomaly in the acid rocks may bedue to fractionation of a Ti-rich phase or a refractory Ti-rich phase inthe melting residuum.

The acid rocks show slightly positive Zr anomalies and a positive Zranomaly is also present in the Niedźwiedzia Góra intermediate rocks.The value of (Zr/Sm)N ratio is N1 for both suites, suggesting parentalmagmas that were relatively enriched in Zr or which accumulated aZr-rich phase during magma evolution. This phase is probably also

Nb–Hf–HREE rich (Tables 1, 2). Extraction of it can also explain moreflat REEN patterns for Niedźwiedzia Góra rocks (Fig. 6).

The multi-element diagram for the granitoids has some similarityto those for the acid volcanic rocks. Some patterns are consistent withaccessory minerals and inconsistent with plagioclase fractionation.Some suggest a small degree of fractionation of both accessoryminerals and plagioclase. All extrusive and intrusive rock samplesdisplay a significant Nb anomaly, which can be related to the meta-mafic magma source (Foley et al., 2002; Rapp et al., 2003).

In summary, the anomalies on the normalized plots for the inter-mediate rocks are primarily due to the nature of their source rocks.However the patterns for the acid and intermediate NiedźwiedziaGóra rocks are consistent with their being due to a) magma sourcecomposition and b) of some fractionational crystallization.

Fig. 5. Differentiation of extrusive intermediate (I — intermediate; G — glass) acid (A), intrusive (GR) rocks related to Mg# and Th (data source as for Fig. 3). Mostly the rocks formtwo different unrelated trends. Notice, that on the diagrams, where Mg# is chosen as the differentiation index, and the granitoids plot within the field of less differentiated rocks. Theacid rocks related to Th show two, weakly separated trends, formed by the Miękinia (M) and Zalas–Orlej (ZOR) data.

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143Nd/144Nd and 87Sr/86Sr ratios were determined on eightsamples (Tables 1, 2). Both 143Nd/144Nd and 87Sr/86Sr for intermediateand acid rocks show signatures indicative of inherited old lower crustwhereas the ratios for the intermediate rocks can be also related toderivation from metasomatised mantle.

εNd(T) and εSr(T) have been recalculated at 300 Ma, (the age of theZalas intrusion estimated using fission tracks in biotite, Skowroński(1974) and zircon using the SHRIMP method (Nawrocki et al.,2007a). The isotope ratios indicate two magma sources, both withnegative εNd(300) (Fig. 8). The intermediate rocks have higher εNd(T)than the acid ones; in the latter, the Miękinia samples have slightlyhigher εNd(T) than those from Zalas–Orlej. The relationship betweenεNd(T) and Th or 1/Nd ratio may indicate some mixing between theZOR and TAR groups (Fig. 8) but this is not confirmed by εNd(T) vs.εSr(T). The Sr isotope ratio may have been changed by alteration. The

Niedźwiedzia Góra isotope composition on those diagrams is notlinked to either group.

Different magma sources for the intermediate and the acid rocksare confirmed by discrimination diagrams (Fig. 9). Compositions ofthe intermediate and acid rocks point towards heterogeneous sourcemelting in which variable proportions of at least three end-memberswere involved: depleted MORB- (preferably E-MORB-) like source,enriched OIB-source and continental crust (CC) (Fig. 9). OIB–E-MORBcomponents seem to be predominant in the intermediate melts (Y/Nbvs. Zr/Nb, Zr/Nb vs. La/Nb, and Th/Yb vs. Ta/Yb). However, all traceelement ratios for intermediate rocks trend also toward LCC (LowerContinental Crust) indicating the presence of crustal components inthe melt. The observed shift may, however, indicate mantlemetasomatism by delaminated and melted crusts (Lustrino, 2005).The degree of enrichment of the mantle source that gave rise to the

Fig. 6. REE patterns of intermediate (Tęczynek–Alwernia–Regulice and Niedźwiedzia Góra), acid rocks (Miękinia and Zalas–Orlej) and granitoids — data source our data, andgranitoids from Markiewicz, 2002. Normalisation values are from Masuda et al. (1973) divided by 1.2.

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intermediate magmas is inferred to have been high (Fig. 6). Theenrichment preceded mantle melting (Martin et al., 2009).

The trace element ratios suggest that the acid melts originatedfrom complex sources. Similarly lower crustal sources, with a limitedupper crustal participation, are required to produce the variations.Y/Nb and Zr/Nb ratios show that lower crustally derivedmelts, mingledwith intermediatemelts could account for the acid series. Indeed all theplots in Fig. 9 suggest different contributions from heterogeneouscrustal and mantle sources as well as, probable mingling among thevarious melts.

Fig. 7. Primitive mantle-normalized (Sun and McDonough, 1989) trace elementvariation diagrams and inserted plots of different element ratios vs. differentiationindex for a) extrusive intermediate and acid rocks (samples with extremes REE contentare marked); and b) for whole extrusive and intrusive suit (data sources as for Fig. 6).

6. Petrogenesis

6.1. Geochemical modelling of magma evolution

6.1.1. Fractional crystallizationFelsic magmas in bimodal suites can be derived from mafic

magmas by large degrees of fractional crystallization (Macdonald etal., 1990; Furman et al., 1992; Martin and Sigmarsson, 2007). Thegeochemical data for both the intermediate and the acid rocksstrongly argue against significant fractional crystallization. Mantle-normalized- (Fig. 7) and chondrite normalized-diagrams (Fig. 6) forthe samples investigated show little evidence for fractional crystal-lization. Also the composition of the relic glass in the intermediaterocks, considered by Rospondek et al. (2004) to be products of

Fig. 8. Isotope composition. Isotopes show two different magma sources. Diagrams canalso indicate possible mixing between Miękinia–Zalas–Orlej group and Tęczynek–Alwernia–Regulice group.

Fig. 9. Zr/Y vs. Ti/Y, Th/Yb vs. Ta/Yb, Y/Nb vs. Zr/Nb and La/Nb vs. Zr/Nb plots. Note thatall the diagrams show partial melting of different mantle and crust source rocks. Datasource as for Fig. 3; A— acid rocks, I— intermediate, GR— granitoids. E-MORB, N-MORB,PM, and OIB, compositions from Sun and McDonough (1989), Taylor and McLennan(1985), Saunders and Tarney (1984) and Weavers (1991); on the Ta/Yb vs. Th/Yb plot,the mantle array is after Pearce (1982); LCCr (r-recommended), LLCe (extreme values)as well as UCCr and UUCe are compiled from Rudnick and Gao (2003).

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fractionation, is not consistent with the idea that the intermediatemagma evolved by fractional crystallization. Furthermore the traceelement diagrams vs. magma differentiation indices and isotope datado not accord with a fractionation origin involving two differentmagma sources (Figs. 4, 5, 8). In particular the concentration oftransition elements, always efficiently removed from the melt byfractional crystallization, do not change in either the intermediate orthe acid rocks with increasing degrees of magmatic evolution(Tables 1, 2). Fractional crystallization as a mechanism for derivingthe felsic magmas from the intermediate magmas must be thusexcluded.

6.1.2. Partial melting of enriched mantle sourceIntermediate rocks with an average SiO2 content below 54% and

Mg# ~0.45 cannot be generated by partial melting of crust. Onlyultramafic rocks can account for such a melt. On the other hand, themelt demonstrates low and stable transition element content (see forinstance Ni content in Table 1). Pichavant and Macdonald (2003)report intermediate magmas of similar composition from LesserAntilles arc, however they relate these magmas to a two-stagepetrogenetic process e.g. partial melting and fractionation. Such atwo-stage process is not recognized in intermediate rocks fromKraków–Lubliniec Fault Zone (with exception for some samples fromNiedźwiedzia Góra).

In turn chondrite-normalized REE plots for the intermediate rocksindicate a strongly enriched source for the magmas, implying areaction between ultramafic rocks and metasomatic agents prior tomelting (Martin et al., 2009). The mantle rocks may have beenmetasomatised by fluids or by melts. In most modern island arcs,hydrous fluids derived from crustal components are enriched in LILE,whereas melts derived from crustal components are silica-rich.Martin et al. (2009) proposed the use of Nb/Y and La/Yb ratios inorder to discriminate between both agents. These authors argue thatwhereas fluids would be unable to transfer Nb from the crust to themantle, melts would be able to do so. In addition, felsic slab-derivedmelts are characterized by low Y and Yb concentrations. Consequentlyfluids as a metasomatic agent can be distinguished by their very lowNb/Y (b0.25) and La/Yb (b16) ratios. Applying this characteristic to

the intermediate rocks under consideration, we conclude that themantle source had been metasomatised by felsic melts rather thanfluids.

The normalized REE and trace element plots are interpreted toimply a strongly metasomatised magma source. Consequently wehave modelled the trace element behaviour during partial melting(PM) of an enriched peridotite, using the Shaw (1970) equilibriummelting equation: (Cl=Co/[F+D(1−F)], where Cl is melt, Co sourcecomposition, D general distribution coefficient and F degree ofmelting). F and D need to be known.

The calculation of F was carried out for major elements using thelinear equation: Co=FCl+(1−F)Cs, (Co— composition of the magmasource, Cl— of the liquid, Cs— composition of the residue after melting,and F — degree of melting: Störmer and Nicholls, 1978) which permitscalculation of the chemical and modal compositions of the meltingresidue aswell as the degree ofmelting. Both Cs and Fwere determinedfor four samples (7, 20, 21, and 27) from the Tęczynek–Alwernia–Regulice and Niedźwiedzia Góra group, which are inferred to representmelts from the enriched mantle Cl (Fig. 8a). The metasomatised mantlecomposition (source Co) and the phase compositions were taken fromthe compilations by Ionov et al. (2002), Gregoire et al. (2002) and Zhanget al. (2007) of data from weakly to strongly metasomatised mantlexenoliths; those used in the models are shown in Table 3. The match ofallmodels donewith theuseofmajor elements is excellent (R2=0.002–0.006) and shows that small degrees of melting of hydrous peridotitecould account for the intermediate magmas in the Kraków–Lublinieczone. Moreover, small quantities of hydrous minerals remain in theresidue.

On the basis of the data from this modelling bulk distributioncoefficients, DREE;LILE, were determined using the partition coefficientsin Table 3. An inverse equilibrium melting mass-balance model fortrace elements (Shaw, 1970) was calculated in order to test whetherthe calculated source composition fits the enrichment level inferred incollision zones. A direct model would not be meaningful because ofmantle wedge heterogeneity. Pervasive metasomatism or the pres-ence of veined lithospheric mantle implies heterogeneity, particularlywith regard to the trace elements (Lloyd and Bailey, 1975; Foley,1992). Mantle peridotite interacts with slab-derived melts and fluidsor carbonate–silicate melts, usually causing differential enrichment inincompatible elements, especially LILE and REE and a relativedepletion in HFSE (Blundy and Dalton, 2000; Gregoire et al., 2001;Ionov et al., 2002). The inverse model (Fig. 8b) shows that thecalculated source composition displays a strong affinity to peridotiteenriched in hydrous minerals. Garnet-, spinel- or even plagioclase-bearing peridotites are all potential source materials.

A low degree of partial melting favours strong melt enrichment inincompatible elements. The intermediate melts are deduced to haveequilibrated with Ni content between 40 and 70 ppm with metaso-matised ultramafic rocks. Such low contents imply low Ni contents inthe metasomatised source (~850 ppm) and consequently a consider-able degree of metasomatism. To estimate the latter we used theMoyen (2009) and Martin et al. (2009) method for determining F/aratio (a—mass fraction of metasomatic agent and slab-derived melt).Incompatible La (with D=0.03, previously calculated for the inverseequilibrium melting mass-balance model) was chosen as an elementwith low probability of change during post-magmatic processes. Theestimated F/a ratio is 0.25. Assuming that the un-metasomatisedultramafic rock (Ni content ~2000 ppm — from Sun, 1982) wasmetasomatised by slab-derived melt (Ni content 18 ppm — fromMartin et al., 2009) via mixing, and adopting the Langmuir et al.(1978) equation Cm=aCnm+(1−a)Csm (where Cm — elementconcentration in melt, a — degree of metasomatism, Cnm — elementconcentration in un-metasomatised mantle, and Csm — elementconcentration in slab-melt), the calculated Ni content in metasoma-tised mantle lay between 1700 and 1200 ppm. The melt equilibratedwith such a source had a Ni content of 87–54 ppm. The numbers are

Table 3Source composition — metasomatised mantle- and mineral-composition used for calculation of the residue after partial melting as well as partition coefficients used in the inversemelting model.

wt.% Metasomatised mantle Olivine Clinopyroxene Orthopyroxene Plagioclase An90–95 Spinel Garnet Phlogopite Amphibole

SiO2 44.79 39.9 53.45–56.31 55.65–57.52 45.36–44.07 – 41.53 44.47 42.72Al2O3 3.30 0.70 4.42–0.50 3.07–0.05 34.77–35.61 58.38–63.10 19.55 12.45 14.21Fe2O3 8.80 10.10 2.58–3.07 5.93–5.55 – 14.29–16.72 9.31 4.08 9.23MgO 39.85 48.80 16.14–16.54 34.43–36.53 – 22.62–24.83 20.21 27.05 17.86CaO 2.65 0.50 21.93–21.16 0.67–0.24 18.58–19.61 – 8.46 0.01 11.22Na2O 0.40 – 1.27–2.05 0.08–0.01 1.15–0.58 – – 0.10 3.22K2O 0.10 – 0.00–0.03 – 0.14–0.13 – – 10.86 0.76TiO2 0.10 – 0.13–0.23 0.02–0.04 – 0.00–0.07 0.93 0.95 0.77

Kda Olivine Clinopyroxene Orthopyroxene Plagioclase Spinel Garnet Phlogopite Amphibole

La 0.0067 0.056. 0.015 0.13 0.01 0.015 0.035 0.25Ce 0.0060–69 0.15–0.092 0.02 0.11 0.01 0.021 0.034 0.20–.84Nd 0.0066–59 0.31–23 0.03 0.07 0.01 0.087 0.032 0.33–1.34.Sm 0.0066–70 0.50–44. 0.05 0.05 0.01 0.217 0.031 0.5–1.80Eu 0.0068–74 0.51–48. 0.05 1.3 0.01 0.61 0.03 0.4–1.56Gd 0.0077–0.01 0.61–56. 0.09 0.04 0.01 1.2 0.03 0.63–2.02Dy 0.0096–0.013 0.68–58 0.15 0.031 0.01 2 0.03 0.64–2.02Er 0.011–26 0.65–58 0.23 0.026 0.01 3.3 0.034 0.55–1.74Yb 0.016–45 0.62–51 0.34 0.024 0.01 4.03 0.042 0.49–1.64

a Data sources: Pearce and Norry (1979); Irving and Frey (1978); Fujimaki et al. (1984); Green and Pearson (1985); Martin (1987); and McKenzie and O'Nions (1991).

Fig. 10. Partial melting (PM) model; small degrees of melting of metasomatisedperidotite (Co) can give liquid (Cl) of 3–27, 3–21, 3–07, 3–20 composition: a) residuecomposition (X(PM) — degree of melting, ol — olivine, cpx — clinopyroxene, opx —

orthopyroxene, amph— amphibole, phl— phlogopite, pl— plagioclase, gr— garnet, andsp — spinel; and b) inverse model shows the calculated trace element composition ofthe source (Co), which melting leads to Cl appearance; grey field–metasomatizedmantle composition (data compiled from Gregoire et al., 2002; Ionov et al., 2002; Zhanget al. (2007)).

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mostly too high to be seen in the intermediate rocks. A similarcalculation for V gives values N130 ppm in themelt, slightly too low tobe observed in the intermediate rocks from the Kraków–LubliniecFault Zone. Thus the relationships between Ni and V in theinvestigated rocks do not appear to reflect primordial ones. Weconsider the obvious discrepancies as a result of the alterationprocesses of transition metal-bearing phases (Fig. 10).

6.1.3. Model of crust melting in Kraków–Lubliniec Fault ZoneThe trace element and isotopic geochemistry of the acid rocks

points to a crustal magma source. The REE display strong fraction-ation, with high LREE and low HREE contents ((La/Yb)N and YbNTable 2; Fig. 11a), possibly implying an origin from melting of a maficsource with amphibole, clinopyroxene and garnet as residual phases(Rapp and Watson, 1995; Martin, 1999; Foley et al., 2002; Brophy,2008). In the residual phases La was strongly incompatible(D values≪1), whereas Yb was compatible (D values ~2–26). Thisled to the decoupling of both elements during partial melting and tothe relative melt depletion in HREE. Apart from the strongfractionation of LREE from HREE, the magmas originating frommeta-mafic magma sources tend to be Na–Sr-rich, with low Nb/Taand high Zr/Sm ratios, i.e. they show an affinity with tonalite–trondhjemite–granodiorite (TTG) or adakite (modern analogues ofTTG) (Rapp and Watson, 1995; Martin, 1999; Foley et al., 2002; Rappet al., 2003).

The (La/Yb)N ratios place the acid rocks of the Kraków–LubliniecFault Zone in the TTG field (Fig. 11a). The rocks are relatively Na–Sr-poor, with Na/K ratios different from those expected. However, it isdoubtful whether the magmatic values of these elements have beenretained because of plagioclase alteration. The rocks also have high Zr/Sm and low Nb/Ta ratios indicative for amphibolite melting (Fig. 11b),although the acid rocks do not precisely plot in the area ofexperimentally derived melts from a pure amphibolitic source (Foleyet al., 2002).

The fact that mafic rocks occur in the Upper Silesian Block supportsthe argument for the acid melts having a mafic source. Thus, anArchaean lower crustal amphibolite occurs at a convergent platemargin in the Rzeszotary Block (Żelaźniewicz et al., 2009). This blockin the Archaean/Paleoproterozoic basement was presumably part ofthe West African- or Amazonian craton (Tassinari and Macambira,1999) and suggests considerable elevation within the Kraków–

Fig. 11. Recognition of potential magma source for acid rocks; a) (La/Yb)N vs. YbNdiagram (after Martin, 1999) with the De Souza et al. (2007) batch melting model ofArchean Tholeiite (AT) with 0, 10, 25% garnet content (G0, G10, and G25) and ofenriched mantle (EM) adopted to volcanic rocks of Kraków–Lubliniec Fault Zone;labelled tick marks indicate percent of PM; b) Nb/Ta vs. Zr/Sm (after Foley et al., 2002);because of big scatter of the Kraków–Lubliniec Fault Zone data from references, they areplotted as open symbols; note, that intermediate rocks (full symbols— own data) formtwo different groups Tęczynek–Alwernia–Regulice with lower Zr/Sm ratio andNiedźwiedzia Góra with higher ratio (data source for a) and b): compilation of owndata and from Czerny and Muszyński (1997); Heflik and Muszyński (1993); Muszyńskiand Pieczka (1994); and Markiewicz (2002).

262 E. Słaby et al. / Lithos 119 (2010) 251–268

Lubliniec Fault Zone. Amphibolites constitute the main part of theblock and may therefore have contributed to the generation ofgranodioritic magma. The rocks are partly migmatized (Nowak et al.,unpubl. data in prep. after Żelaźniewicz et al., 2009).

Major elements were modelled for amphibolite partial meltingusing the same algorithm as before, viz. Störmer and Nicholls (1978).Data for the average composition of Archaean amphibolite were takenfrom Rapp and Watson (1995, 1999) and Blais et al. (1997) and areused to approximate the composition of the magma source (Co). Themineral compositions of potential restitic phases (Cs) were takenfrom Rapp and Watson (1995) (Table 4). Samples with the lowestSiO2 contents from the Zalas–Orlej (ZOR) group were assumed to berepresentative of themelt (Cl) derived from the Archaeanmafic rocks.The results of the calculations are presented in Fig. 12a; the right-sideof the partial melting (PM) axes represents a garnet-bearing residueafter amphibolite melting whilst the left-one indicates a solutionwithout residual garnet.

The calculated composition of the residue closely matches theresults of Rapp andWatson's (1995) low-degree dehydration melting

experiment performed on meta-basalts at low/medium pressures.The best match (R2=0.00 was found for a partial melt coexisting witha garnet-bearing granulitic composition (right-side of the partialmelting (PM) axes, Fig. 12a; (i) and (iii)), a poorer fit (R2=0.02–0.34)for melt coexisting with a garnet-free residuum (left-side of thepartial melting (PM) axes on Fig. 12a; (ii) and (iiii))). According to thismodel, the Zalas–Orlej (ZOR) acid melt was K-rich and resulted fromlow-degree melting (~14%). In the Rapp and Watson (1995)experiment, the low percentage melt was also silicic and K-rich. Thecomposition of the derived acid melt plots on the cotectics in thehydrous granitic system for pressures between 5 and 10 kbar,suggesting that the Rapp's and Watson's low-pressure experimentaldata are preferable. Consequently a model without garnet is morerealistic.

The degree of melting in the above model does not match that ofthe one calculated by De Souza et al. (2007), on the basis of anArchaean garnet-free and garnet-bearing meta-tholeiite (Fig. 9a). Inthe De Souza et al. (2007) model, acid rocks from the Kraków–

Lubliniec Fault Zone are close to a 25% partial melting curve forgarnet-free and or 10% garnet-bearing amphibolite.

A conclusive argument in this debate, i.e. garnet-in or garnet-out inthe residue, is provided by an inverse batch melting model (Shaw,1970), calculated from trace elements (Fig. 12b). Calculated REEconcentrations in the source compared to Archaean amphibolitecompositions (data from: Blais et al. (1997); Rapp and Watson(1995); and Rapp et al. (1999)) points towards a garnet-free residue.

The differences in the two models (done for the KLFZ usingStörmer and Nicholls/Shaw's algorithms and introduced into the DeSouza model) lead to the conclusion that melt formation was morecomplex. The relationship between εNd(T) and Th or 1/Nd ratio furtherindicates that melting can be accompanied by contamination. In turn,the De Souza et al. (2007) model for enriched mantle meltingperfectly accounts for the intermediate rocks of the Kraków–LubliniecFault Zone. Contamination of these rocks cannot be excluded due tothe relationship between εNd(T) and Th or 1/Nd ratio.

6.1.4. Mixing–contaminationTo test the possible intermediate–acid melt interactions, the

Langmuir et al. (1978) algorithm was used. The positive and negativeresults of the test, shown in Table 5, show that some intermediatecomposition samples could result from mantle-derived melts slightlyto moderately contaminated (8–22%) by felsic (Miękinia or Zalas–Orlej), amphibolite-derived melts. In contrast, the rhyodacite–dacitefromMiękinia (M) and Zalas–Orlej (ZOR) crystallized from acid meltsuncontaminated by mafic melt, even if the isotopes suggestcontamination.

6.2. Petrogenetic summary

Magmatic rocks from the Kraków–Lubliniec Fault Zone can berelated to two magma sources, viz. enriched mantle and crust. Weconclude that ultramafic mantle rocks were metasomatized by felsicmelts derived from meta-mafic sources. The degree of metasomatismwas significant. Similarly acid melts were derived from meta-maficsources. Two magma sources are clearly reflected in the isotopiccompositions. εNd(T) for both the intermediate and acid volcanic rocksvaries within a narrow range, −1 to −2 and −4 to −5, respectively.

The geochemistry of both suites resulted mainly from partialmelting. However, some lavas of intermediate composition representmafic melts slightly contaminated by acid melt. The occurrence ofsuch contaminated melts may indicate the beginning of melting ofcrustal rocks heated through contact with mafic magma.

Although partial melting was the dominant differentiationmechanism, it cannot alone account for the development of theMiękinia lava dome nor the Zalas–Orlej laccolith. The multi-elementdiagrams (Fig. 7) and the REEN patterns (Fig. 6) show that some facies

Table 4Source composition — Archaean amphibolite and mineral composition used for calculation of the residue after partial melting as well as partition coefficients used in the inversemelting model.

wt.% Average amphibolitea Clinopyroxeneb Magnetite Plagioclase An30b Garnetb Amphiboleb

SiO2 50.45 50.67 53.36 38.38 41.83Al2O3 14.44 6.62 29.87 22.14 14.44Fe2O3 11.41 11.94 100 – 21.33 16.40MgO 8.79 13.13 – 10.94 12.67CaO 10.70 14.52 12.37 6.24 8.97Na2O 2.71 2.43 4.40 0.10 3.17K2O 0.72 – – – 0.28TiO2 0.78 0.69 – 0.89 2.24

Kdc Clinopyroxene Magnetite Plagioclase Garnet Amphibole

La 0.3 0.22 0.13 0.05 0.2Ce 0.6 0.26 0.11 0.11 0.3Nd 1 0.3 0.07 0.27 0.8Sm 1.6 0.35 0.05 1.33 1.1Eu 1.5 0.26 1.3 3.00 1.3Gd 1.9 0.28 0.04 6.80 1.8Dy 1.9 0.28 0.031 13.00 2Er 1.8 0.22 0.026 18.00 1.9Yb 1.7 0.18 0.024 26.00 1.7

a Compilation of Rapp and Watson (1995, 1999) and Blais et al., (1997) data.b Rapp and Watson (1995).c Data sources: Martin (1987) and Rollinson (1993).

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in both magmatic bodies resulted from small degrees of fractionalcrystallization. Similarly some Niedźwiedzia Góra samples pointtowards a small degree of fractionation of plagioclase and accessory

Fig. 12. Model of amphibolite melting; a) acidic melts result from low-degree melting,leaving a garnet-bearing or garnet-free residuum and b) inverse model shows that agarnet-free residuum matches better the trace element pattern of the mafic source.

minerals. A petrogenetic model for the rocks of the Kraków–LubliniecFault Zone is presented in Fig. 13.

7. Discussion

Geochemical modelling of petrogenetic mechanisms has to be putinto a robust geological context, to establish the connectionsbetweenallprocesses from the micro- to macro-scales. The geochemistry of therocks investigated here and the derived models suggest a multiple,recurrent process of small-scale partial melting of at least two differentsources, a) enriched ultramafic and b) meta-mafic. In addition themetasomatic agent responsible for the enrichment of the ultramaficsource is inferred to be a melt that was also derived from a meta-maficsource.While themelts are postulated to have been derived frombelowthe Variscan orogen and transported into transtensional fissures in theKraków–Lubliniec Fault Zone (Żelaźniewicz et al., 2008), we suggestthat melting processeswere active in situ in the Fault Zone in the courseof its evolution under alternating transtensional and transpressional

Table 5Models of mixing of basic–intermediate (I) and acid (A) magmas (in italics — failedattempts). The calculation shows, that some of the samples of intermediatecomposition can be product of contamination by acid magma.

Ca — sampleacronym(rock group)type of melt

Cb — sampleacronym(rock group)type of melt

Cm — sampleacronym(rock group)type of melt

Xa R2 NTa Comments

21(TAR) I 13(M) A 20(TAR) 0.77 0.98 3021(TAR) I 08(M) A 13(M) 0.48 307(NG) I 08(M) A 13(M) 0.11 3026(TAR) I 13(M) A 20(TAR) 0.92 0.98 3021(TAR) I 24(ZOR) A 23(ZOR) 0.59 3021(TAR) I 24(ZOR) A 20(TAR) 0.78 0.98 3026(TAR) I 24(ZOR) A 20(TAR) 0.92 0.99 3026(TAR) I 25(ZOR) A 20(TAR) 0.88 0.95 0 Only major

elementsavailable

26(TAR) I 13(M) A 22(TAR) 0.90 0.99 3026(TAR) I 24(ZOR) A 13(M) A 0.04 30

Langmuir et al., (1978) algorithm: Cm=XaCa+(1−Xa)Cb, where Ca — magma, Cb —

contaminant, Cm — contaminated melt, Xa — degree of contamination of Ca magma;TAR — Tęczynek–Alwernia–Regulice, M — Miękinia, and ZOR — Zalas–Orlej.

a Number of trace elements used for calculation (+10 major element).

Fig. 13. Petrogeneticmodel for the intermediate and acid rocks of the Kraków–Lubliniec Fault Zone; explanations: PM— partialmelting, Xa— fraction of felsicmelt in hybrid, F— degree ofpartial melting, acronyms xx — sample numbers, and ZOR–M–TAR–NG — acronyms of acid-intermediate rock groups.

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tectonic regimes. Under alternating transtensional and transpressionaltectonic regimes mechanical coupling through the lower crust andupper lithospheric mantle is observed. The systems are preferentiallyintruded bymagmas (Vigneresse et al., 1996; Saint Blanquat et al., 1998;Vigneresse and Tikoff, 1999).

Though the Kraków–Lubliniec Fault Zone was initiated in theProterozoic, its long- lasting and multi-stage activity can best berelated to the Variscan orogeny and to the subsequent extensionalphase (Karwowski, 1988; Żaba, 1999; Żaba, 2000; Truszel et al., 2006).The Fault Zone lies within the Variscan foreland in which extensivemagmatism was well developed in the late Carboniferous–earlyPermian. Extensional structures at the terminations of wrench faultsparalleling the Trans-European Suture Zone (Ziegler, 1990; Ziegler etal., 2006) favored an E-MORB-OIB signature.

The Kraków–Lubliniec Fault Zone rocks have a collisional, arc-related, signature and this calc-alkaline character suggests that theyoriginated from an enriched, subduction-related source. The geody-namic setting precludes subduction in the late Carboniferous–earlyPermian period and the magmas could be derived from mantlesources that were modified by earlier subduction events. McCannet al. (2006) point to such mantle sources as common for the lateCarboniferous–Permian magmatism. Foreland magmatism with traceelement signatures not correlated with geodynamic setting wasobserved in the Halle Volcanic Complex (transtensional intraconti-nental Saare basin) by Romer et al. (2001). They related thegeochemistry of the extensional magmatism with subduction-zoneaffinities to the composition of underlying blocks that couldcorrespond to palaeo-terrane boundaries of ancient orogens.

In the Kraków–Lubliniec Fault Zone the subduction fingerprintscan be correlated with Ediacaran/Cambrian reorganization. Thisreorganization assumes that Baltica and West Gondwana in Rodinialay close in the Neoproterozoic (Brochwicz-Lewiński et al., 1986b;Lewandowski, 1993; Lewandowski, 1994; Danziel, 1997; Unrug et al.,1999; Finger et al., 2000; Nawrocki et al., 2004; Nance et al., 2008;Żelaźniewicz et al., 2009). The break-up of Rodinia gave rise to mutual

collisions of its constituent parts prior to dockingwith Baltica. Some ofthem assembled to form Brunovistulia which docked transpression-ally with Baltica along its passivemargin in latest Ediacaran times. At alate stage the Rzeszotary terrane collided with the Małopolska Block(Baltica thinned margin) at 560–550 Ma (Żelaźniewicz et al., 2009).Magmas generated from the subducting oceanic lithosphere wereable to modify the lithospheric mantle composition. Ediacaranmagmatism matches collisions between the Brunovistulian blocks(Finger et al., 1989; Finger et al., 2000; Murphy et al., 2004). It has acalc-alkaline character and was derived from magma sources in boththe mantle and the crust.

We conclude, however that the nature of later, Carboniferous–Permian melt generation had little to do with the ancient subduction,although this cannot be totally excluded. As has been pointed out, thefault zone experienced both transpressional–transtensional phases.The changing tectonic conditions permitted different mechanisms ofmantle enrichment and mantle–crust melting.

The geometry of the zone is typical of other sectors of the Variscanbelt (McCann et al., 2006) and resulted from strike–slip motions(Żaba, 1999; Żaba, 2000). The two most important tectonic phaseswere Silurian sinistral transpression and late Carboniferous dextraltranspression and transtension (Żaba, 1996, 1999, 2000). In the latePaleozoic the N–S compression within the Kraków–Lubliniec FaultZone changed to NE–SW; the northeastern part of the Upper SilesianBlock was thrust over the Małopolska Block (Żaba, 1999). LateCarboniferous, dextral-faulting was common at that time over vastareas between present North America and the Urals (Arthaud andMatte, 1975, 1977; Matte, 1986; Ziegler, 1986; Blés et al., 1989) andwas caused by transcontinental, dextral shearing initiated by thecollision of the African and European plates.

Silurian transpression was attended by the intrusion of doleritesand gabbros and also of granitoids (mainly granodiorites), mainlyemplaced in the Ordovician–Silurian sedimentary rocks (Truszel et al.,2006) (Fig. 14). In Carboniferous/Permian times, magmatism tookplace in a regime of recurring dextral transpression and transtension

Fig. 14. Strike–slip activity on the boundary zone between the Upper Silesian Block(USB) and Małopolska Block (MB), schematic model not to scale (based on Żaba, 1996,1999); explanations: 1 — acid volcanic rocks, 2 — granitoids, 3 — intermediate volcanicrocks, 4— sedimentary cover, 5—metasediments (low-grade complexes), 6— crystallinebasement; two-sided arrows — shortening direction (compression axis σ1); one-sidedarrows — direction and sense of relative movement; and KLFZ — Kraków–Lubliniec FaultZone.

Fig. 15. Permianmagmatic activity in the boundary zonebetween theUpper Silesian Block(USB) and Małopolska Block (MB), schematic model not to scale (based on Żaba, 1999);explanations: 1 — intermediate volcanic rocks, 2 — acid volcanic rocks, 3 — sedimentarycover; KLFZ — Kraków–Lubliniec Fault Zone, and KChF— Krzeszowice–Charsznica Fault.

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(Arthaud and Matte, 1977; Żaba, 1995). Accompanying magmatismwas principally of acid magmas yielding granitoid–porphyries andgranodiorites–dacites, preceded by basic extrusions (Markiewicz,2002; Truszel et al., 2006; Żelaźniewicz et al., 2008; Figs. 14 and 15).

Models by Jull and Keleman (2001) and Lustrino (2005) appear toreflect what we observe within the Kraków–Lubliniec Zone. This isparticularly so with regard to Lustrino's model. The transpressionalregimecauses crustal thickeningas a result of thrustingand faulting. Theover-thickening and resultant pressure increase, causes modification ofthe mafic lower crust to amphibolitic/eclogitic assemblages (Rapp andWatson, 1995; Jull and Kelemen, 2001) and their density can exceedthat of the upper mantle if the stable phase in them is garnet. Theincreased densitymay induce gravitational instability of the lower crust,permitting delamination, detachment and subsidence into the mantle(Jull and Keleman 2001; Lustrino, 2005). The subsiding lower crustmelts to produce magmas of TTG- or adakitic-affinity which interactwith the peridotitic mantle (Springer and Seck, 1997; Zegers and VanKeken, 2001; Xu et al., 2002). In the Kraków–Lubliniec Fault Zone,metasomatism of the mantle rocks was induced by felsic meltspercolating through them. According to Jull and Keleman (2001), theinstability time of the lower crust is ~10 Ma. The requisite hightemperatures would restrict such a process to arc-related, volcanic-rifted margins and areas underlain by thermal anomalies.

The OIB signature of the KLF Zone intermediate rocks suggests thepresence of a thermal anomaly. However, the presence of a thermalanomaly beneath the European lithosphere in Permian times is amatter of debate. Ro and Faleide (1992) argue in favor of it whereasPedersen and Van der Beek (1994) are skeptical. A weakly activemantle plume at the base of the lithosphere was inferred by Ziegler(1996). On the other hand, we propose a meta-mafic magma sourcefor the acid rocks in the Kraków–Lubliniec Fault Zone. Żelaźniewicz etal. (2008) proposed meta-psamites, granodiorites or tonalites as thesource for the granitic melts. However, the geochemistry of suchprotoliths precludes magma generation of granodioritic composition,the commonest composition among Kraków–Lubliniec Fault Zoneacid intrusions (Markiewicz, 2002; Truszel et al., 2006; Żelaźniewiczet al., 2008). The precursors for these magmas would have to havebeen more mafic. Partial melting of mafic rocks can occur only wherethe geothermal gradient is high, e.g. within or close to rift zones, orplume centres (Sigmarsson et al., 1991; Martin and Sigmarsson,2007). Melting of primitive basement crust argues in favor of athermal anomaly below the zone and would also accord with theextensional tectonism at the time.

The two tectonic stages, transpressional and transtensional,operating within Kraków–Lubliniec Zone, are reflected in mantlemetasomatism and the melting of the mantle and crust respectively.The low degrees of decompressional melting inferred from ourmodels were probably induced by the local destabilization ofheterogeneously enriched mantle and meta-mafic crust. The meltswere generated by this local reorganization and remobilization, whichalso involved interaction with material from the lithosphericboundary layer.

8. Conclusion

Our data show that the magma mobilization and evolution in theKraków–Lubliniec Fault Zonegave rise to the typical lateCarbonifereous–Permianmagmatism.However some of its featureswere quite specific tothis zone. During plate amalgamation in the Palaeozoic, many of the‘European’ lithospheric blocks had its own distinctive history. Thelithospheric mantle of some had been modified by magma and fluidsduring previous subduction events. During the late Carboniferous–Permian, transtensional movements occurred with each lithosphericblock reacting differently. Some ‘enriched’ blocks reacted with decom-pressional melting of lithospheric mantle providing the mantle andcrustal components to the magmas. Interactions with mantle–crustcomponents were common. The geochemistry of the Kraków–Lubliniec

266 E. Słaby et al. / Lithos 119 (2010) 251–268

Fault Zone volcanic rocks and our evolutionary models can be partlyrelated to such a scheme. However, the strong mantle enrichment andthe fingerprint of the enrichment related to the interaction with felsicmelts implies that the model needs to be amended. We conclude thattranspression within the zone caused lithospheric thickening, delami-nation and melting leading to mantle metasomatism. The extensionalphase following the compressional phase induced crust–mantlemelting:the bimodal acid–intermediate magmatic suite was the result of all ofthese processes.

Acknowledgements

We are grateful to two anonymous reviewers for their criticalreviews, as well as to G.N. Eby for editorial handling. We are indebtedto H. Martin, R. Macdonald, B. Upton and M. Paszkowski forstimulating and fruitful discussions. We also very much appreciatethe assistance by B. Upton, R. Macdonald and M. Mosdell with regardto the English style and grammar. The work was carried out withinVENTS (Volcanic Systems within the Central-European Permo-Carboniferous Intramontane Basins and their Basement) program.

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