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The Dinaride Ophiolite Belt formed from the Jurassic part of the Neotethys. The investigated Ozren ophiolite complex in Bosnia and Herzegovina consists of peridotites, plagioclase peridotites, plagiogranites, troctolites and other gabbroic rocks, and fewer basalts. Lherzolites and harzburgites contain corroded ortho- and clinopyroxene1 porphyroclasts enclosed in the olivine matrix. The boundaries between olivine aggregates and pyroxene1 and spinel1 are infilled by medium-grained undeformed aggregates of clinopyroxene2, less orthopyroxene2, spinel2, and often clinopyroxene3-spinel3 symplectites. These textures indicate the final crystallization of peridotite in subsolidus conditions. Partial dissolution of deformed pyroxene1 porphyroclasts and coarse-grained spinel1 most likely occurred due to their reaction with the rest melt present in the grain boundaries. The Al decrease from pyroxene1 to pyroxene2 and 3, or the Cr decrease and Al increase from spinel1 to spinel2 and 3 is characteristic. Peridotites are associated with inferred remnants of a gabbro-dolerite layer, whereas basalts and radiolarites occur as rare dm-size fragments in an ophiolitic breccia. Troctolites display interstitial crystallization of plagioclase, clinopyroxene, less Na-Ti-rich amphiboles, and phlogopite in the olivine-spinel matrix, indicating the replacive character of impregnating melt within the dunite layers. Clinopyroxene-plagioclase-ilmenite-±amphibole gabbroic and fewer basaltic dykes in peridotites formed due to subridge extension, mantle thinning, and the deeper mantle melting. Iron-enriched olivines occur in the peridotite-dyke interfaces and troctolites. Hydrated ultramafics and mafics contain amphiboles, biotite, phlogopite, clinozoisite, epidote, and chlorite aggregates. Estimated magmatic to subsolidus T from peridotite two-pyroxene thermometry are 1000–850 °C, for the spinel facies. Ca-in-orthopyroxene1 thermometry provided T of 1028–1068 °C, and Ca-in-orthopyroxene2 thermometry gave 909–961 °C at estimated P of 1.1–0.9 GPa. However, the gabbroic dyke magmatic crystallization T was constrained to 1200–1100 °C at P of 0.45–0.15 GPa by single clinopyroxene thermobarometry. The obtained P–T conditions constrained the deeper mantle environment for the formation of peridotites than troctolites and crosscutting dykes. The ophiolitic thrust-sheet hanging wall conditions in an obduction-related accretionary wedge were estimated from amphibolites at 620 °C and 0.85 GPa by Ti-in-amphibole thermometry and amphibole-plagioclase thermobarometry. 300 °C and 0.5 GPa were determined from an exhumation shear zone using a combination of chlorite thermometry and Si-in-phengite barometry.

The Austroalpine nappe stack of the Pohorje Mountains (Mts.) in northeastern Slovenia comprises a suite of eclogite facies metamorphic rocks that were partially assigned to Eo‐Alpine ultrahigh‐pressure metamorphism (UHPM). We selected a micaschist, which was previously related to this metamorphism, for a detailed study including the chemical zonation of garnet and potassic white mica, the identification of mineral inclusion assemblages, pseudosection modelling with PERPLE_X, and monazite in‐situ dating with the electron microprobe. Polymetamorphism was revealed by (at least) two generations of garnet and phengite and four populations of monazite yielding ages of 283.6 ± 6.1 (2σ), 94.1 ± 3.7, 47.9 ± 10.8 and 26.2 ± 2.8 Ma. The Permian monazite population is characterized by relatively high Y contents (~1.15 wt% Y) and low La/Gd mass ratios (8.7) indicating its formation before the growth of porphyroblastic garnet. The Eo‐Alpine population, however, grew synchronously with garnet based on low Y contents (~0.05 wt%) and high La/Gd ratios (21.4). The older Tertiary population (48 Ma) shows also high Y contents (1.1 wt%) and low La/Gd ratios (10.6) whereas the younger Tertiary population is characterized by low Y contents. The Permian P–T conditions of 7.5–10 kbar at 600–650°C were obtained using the inclusion assemblage of staurolite+rutile+biotite in porphyroblastic garnet. High pressure (HP) but no UHPM was reconstructed for both Eo‐Alpine coarse phengite (Si = 3.22 per formula unit = pfu) and small Tertiary garnet+fine‐grained phengite (Si = 3.27 pfu) at peak pressures ~16 kbar and 18.5–23 kbar respectively. Maximum temperatures close to 650°C were likely reached during the Eo‐Alpine HP event, whereas those of the Tertiary HP event were probably ~580°C. These HP metamorphic events suggest that the Pohorje Mts. experienced both an Eo‐Alpine and a Tertiary subduction–exhumation history, the latter of which was mainly reported for underlying Penninic nappes so far., MOST Special Fund from the State Key Laboratory of GPMR and the 111 Project (BP0719022), National Natural Science Foundation of China http://dx.doi.org/10.13039/501100001809

Websterite and garnet orthopyroxenite and clinopyroxenite dykes crosscutting harzburgite occur in the hanging wall of a Cretaceous eclogitized continental fragment of the Upper Austroalpine Unit in the Eastern Alps. The dyke textures reflect pressure–temperature changes from the mantle, subduction channel and an accretionary wedge. A clinopyroxenite dyke, dated at 252 ± 2 Ma on zircon by U Pb SIMS, provided eHf(t) zircon values of 16–8 (av. 11 from 18 spots) suggesting a depleted mantle source. The rock modal mineral composition and the mineral and whole-rock chemistry revealed that the pyroxenite dykes' petrogenesis is most likely related to sub-crustal cumulate-type melt derivates, less evolved for websterites and highly evolved for clino- and orthopyroxenites. The porphyroclastic clinopyroxene1 (10–13 mol% Ca-Ts), orthopyroxene1, spinel1 and amphibole1 are inferred remnants after magmatic phases. They contain Ti-spinel and ilmenite exsolutions which indicate cooling of the dykes in harzburgite in a Spl stability field (D0-1 stage). Garnet exsolutions in Cpx1, Opx1 and Amp1, and Cpx exsolutions in Amp1 document continuous cooling and/or pressure increase (D0-2 stage). The Grt coronas around Spl1, Opx1, Cpx1 and Amp1, and the granoblastic matrix of Prp–Grs-rich Grt (or Cr-Spl in websterites), low-Al Cpx, low-Al Opx, Fe-enriched olivine, zoisite, kyanite, rutile and pargasite record a subduction channel compression (D1 stage). While the formation of Cpx–Grt or Amp-Grt symplectites replacing the Cpx1 and Amp1 rims suggests the HP–HT decompression (D2-1 exhumation stage). The Grt (or Cr-Spl) replacement by Spl, and Opx1, Cpx1 and Prg replacement by Ol–Spl, Opx–Spl or Prg–Spl symplectites document continuous HT decompression (D2-2 exhumation stage). The MP/MT–LT conditions were estimated from tremolite, Grs-rich Grt, Sr-epidote, clinozoisite, Cl-apatite, titanite, Ce-allanite, chlorite, serpentine and talc assemblage (D3 stage). Anticlockwise P–T path was reconstructed for the D0 to D1 stages followed by almost isothermal exhumation (D2) and emplacement in the Cretaceous accretionary wedge (D3). The pseudosection P–T calculation from a clinopyroxenite dyke yielded 850–825 °C and 25–28 kbar (D1). The whole-rock and mineral trace element data of relic Cpx1 and Amp1, Grt(1–3), Ep–Zo, and younger zircon ages due to Pb-loss, reflect the impact of metamorphic fluids during the D1 to D3 evolutionary stages.

We studied representative samples from a peridotite body situated NE of Sedlice village within the Central- Carpathian Paleogene sediments in the Central Western Carpathians. The relationship of the peridotite to the surrounding Paleogene sediments is not clear. The fractures of the brecciated peridotite margin are healed with secondary magnesite and calcite. On the basis of the presented bulk-rock and electron microprobe data, the wt. % amounts of mineral phases were calculated. Most of calculated “modal” compositions of this peridotite corresponds to harzburgites composed of olivine (∼70-80 wt. %), orthopyroxene (∼17-24 wt. %), clinopyroxene ( < 5 wt. %) and minor spinel ( < 1 wt. %). Harzburgites could originate from lherzolitic protoliths due to a higher degree of partial melting. Rare lherzolites contain porphyroclastic 1-2 mm across orthopyroxene (up to 25 wt. %), clinopyroxene (∼ 5-8 wt. %) and minor spinel ( < 0.75 wt. %). On the other hand, rare, olivine-rich dunites with scarce orthopyroxene porphyroclasts are associated with harzburgites. Metamorphic mineral assemblage of low-Al clinopyroxene (3), tremolite, chrysotile, andradite, Cr-spinel to chromite and magnetite, and an increase of fayalite component in part of olivine, indicate low-temperature metamorphic overprint. The Primitive Mantle normalized whole-rock REE patterns suggest a depleted mantle rock-suite. An increase in LREE and a positive Eu anomaly may be consequence of interactive metamorphic fluids during serpentinization. Similar rocks have been reported from the Meliatic Bôrka Nappe overlying the Central Western Carpathians orogenic wedge since the Late Cretaceous, and they could be a potential source of these peridotite blocks in the Paleogene sediments.

Felsic to mafic granulite xenoliths from late Neogene basalt pyroclastics in four localities of the western Pannonian Basin (Beistein, Kapfenstein, Szigliget and Kaptalantoti (Sabar-hegy) were studied to find out their metamorphic and fluid history. The characteristic mineral assemblage of the granulites consists of Pl + Opx + Qtz ± Cpx ± Bt ± Grt ± Kfs. Based on abundant magmatic relic microstructural domains occurring in these rocks, the potential precursors might have been predominantly felsic igneous or high to ultrahigh temperature rocks. Ternary feldspar thermometry provides a rough estimate of temperatures of about 920–1070 °C. The first fluid invasion event, which is linked with this early high to ultrahigh temperature stage is characterised by primary pure CO2 inclusions in apatite and zircon. The densest primary CO2 inclusions indicate 0.52–0.64 GPa pressure at the estimated temperature range of crystallization. According to mineral equilibria and geothermobarometry, the high to ultrahigh temperature rock cooled and crystallized to granulite of predominantly felsic composition at about 750–870 °C and 0.50–0.75 GPa in the middle crust, between 20 and 29 km depths. The second fluid invasion event is recorded by primary CO2-rich fluid inclusions hosted in the granulitic mineral assemblage (plagioclase, quartz and orthopyroxene). In addition to CO2, Raman spectroscopy revealed the presence of minor N2, H2S, CO and H2O in these inclusions. Partial melting of biotite-bearing assemblages could be connected to the next fluid invasion shown by secondary CO2-rich fluids recorded along with healed fractures in plagioclase, clinopyroxene and orthopyroxene. This event could have happened at depths similar to the previous ones. The final step in the granulite evolution was the sampling in the middle crust and transportation to the surface in form of xenoliths by mafic melt. This event generated temperature increase and pressure decrease and thus, limited melting of the xenoliths. The youngest fluid inclusion generation, observed mostly in healed fractures of felsic minerals, could be associated with this event.

*Corresponding author Unique, perovskite(Prv)–andradite(Adr)-bearing serpentinized harzburgite fragments occur in Late Jurassic–Early Cretaceous subduction–accretionary wedge complex of the Meliata tectonic Unit (Slovakia, Western Carpathians). These rocks reflect magmatic (E1) and partial melting (E2) mantle events followed by metamorphic blueschist-facies (E3) and fluid–rock interaction (E4) events accompanied by crystallization of Prv and/or Adr. The incompletely solidified slightly depleted (residual) harzburgite composed of early-magmatic assemblage of Ol, Opx 1 , Cr-Spl ± Cpx 1 (E1 event) underwent partial melting (E2 event) under subsolidus mantle conditions. The late-magmatic aggregates of Cpx 2 , Cr-Spl, scarce Opx 2 , due to this batch melting, occur around the Opx 1 (±Cpx 1 ) porphyroclasts. The fractures and cleavage planes of the kinked Opx 1 porphyroclasts are filled by Cpx 3 as a result of subsolidus recrystallization of the Opx 1 . Cloudy lower Al Cpx 4 associated with pargasite in reaction rims between the Opx 1 and Cpx 2 , or antigorite replacing Ol, could represent the E3 high-pressure metamorphic event (dated at 160 to 150 Ma, according to published 40 Ar– 39 Ar data for “phengitic” white mica from blueschists) in serpentinites. Serpentinized zones of harzburgite contain Prv, which occurs in serpentinized Opx 1 porphyroclasts. Orthopyroxene (Opx 1 ) breakdown and formation of Prv, (Ti-rich) Adr and chrysotile appears to be postdating the closure of the Meliata back-arc basin (c. 200 to 160 Ma) and HP metamorphism. Perovskite genesis can therefore be bound to the exhumation-related serpentinization in subduction channel and emplacement of serpentinites into subduction–accretionary wedge (E4 event at 300–500 oC/5–15 kbar, at 150 to 130 Ma?). The bulk-rock trace-element patterns suggest enrichment in LREE, Ba, Cs, U, Pb, Sb and Li in comparison with HREE, HFSE, Rb and Sr. Such element mobility indicates fluid–rock interaction. Pervading aqueous fluids rich in CO 2 were transporting Ca, Ti, Fe, LREE partitioned into Prv grown along the Cpx exsolution lamellae in Opx 1 . The sources of such fluids might have been the blueschist- to greenschist-facies rocks from the Meliata melange type subduction–accretionary wedge. The late-metamorphic H 2 O–CO 2 /Si–Fe–Mn-rich fluids caused partial replacement of Prv by pyrophanite and crystallization of (Ti-rich) Adr at the expense of Cpx and Prv.

The ophiolites in southeast Turkey crop out along two distinct belts. The ophiolites in the north are attached to Tauride active margin and represented by Göksun, Berit, İspendere, Kömürhan and Guleman ophiolites. Whereas the ophiolites in the south are observed as tectonically overlying the Arabian continental margin and characterized mainly by Kizildag (Hatay) and Koçali ophiolites. In this paper, new U-Pb and Sm-Nd isotopic ages are presented. The zircons extracted from the gabbroic cumulates of the Kömürhan ophiolite yielded a concordia age of 87.2 ± 3.1 Ma. The zircons in the gabbroic cumulates of the İspendere ophiolite yielded a Concordia age of 84.5 ± 3.9 Ma. Moreover, the Sm-Nd age of the gabbroic cumulates of the İspendere ophiolite yielded 85.1 ± 7.1 Ma (?Nd = + 7.8). The gabbroic rocks of the Kizildag (Hatay) ophiolite yielded 110 ± 11 Ma (?Nd = + 7.3) Sm-Nd isochron age. The new and already published U-Pb and Sm-Nd ages from the Kizildag ophiolite suggest that the time span between the melt generation in a subduction zone setting and SSZ-type oceanic crust crystallization was ?3 my. All the ages from the Southeast Anatolian ophiolites suggest that the ophiolites between the Bitlis-Pütürge continent and the Arabian platform formed around 99-102 Ma whereas the ophiolites between the Bitlis-Pütürge continent and the Tauride platform formed around 84-90 Ma, suggesting that the peri-Arabic belt ophiolites are 10 My older than the ophiolite attached to the Malatya-Keban platform in the north. Detailed comparison suggests that there are number of differences between the ophiolites to the north and south of the Bitlis-Pütürge continental unit based on the geological, geochronological, petrological, internal stratigraphy of the ophiolites as well as their relationships with the continental fragments during the late Cretaceous. Therefore, the ophiolites were rooted from two different oceanic basins, one to the north and other to the south of the Bitlis-Pütürge continent. © 2014 Taylor & Francis. Türkiye Bilimsel ve Teknolojik Araştirma Kurumu MMF2009D11 106Y231 This work is a part of PhD study of Fatih Karaoğlan. Financial support from the TÜBİTAK (106Y231) and Çukurova University Research Foundation (MMF2009D11) is gratefully acknowledged. We would like to thank Monika Horschinik for performing Sm–Nd analyses. The first author acknowledges International Research Fellowship Programme support by TÜBITAK–BİDEB. Erdinç Yiğitbaş and Yann Rolland are acknowledged for their critical reviews that improved the quality of the paper. Erdin Bozkurt is thanked for editorial handling.

The Kızıldağ (Hatay) ophiolite in Turkey represents remnants of the southern Neotethyan ocean and is characterized by a complete ocean lithospheric section. It formed in a fore-arc setting above a N-dipping intraoceanic subduction zone, and represents the undeformed, more northerly part of the same thrust sheet that also forms the Baer–Bassit ophiolite to the south. The ophiolite was emplaced southwards from the southerly Neotethyan ocean in Maastrichtian time. U–Pb and Sm–Nd dates are used to constrain the crystallization age and duration of magmatic activity of the Kızıldağ ophiolite. U–Pb dating yielded ages of 91.7 ± 1.9 Ma for a plagiogranite and 91.6 ± 3.8 Ma for a cumulate gabbro. The cumulate gabbro also yielded a Sm–Nd isochron age of 95.3 ± 6.9 Ma. The measured ages suggest that the oceanic crust of the Kızıldağ ophiolite formed in a maximum time period of 6 Ma, and that the plagiogranite may have formed later than the gabbroic section. The U–Pb zircon ages from the Kızıldağ ophiolite and the cooling age of a metamorphic sole beneath the Baer–Bassit ophiolite are indistinguishable within the analytical uncertainties. This indicates the presence of young and hot oceanic lithosphere at the time of intraoceanic subduction/thrusting in the southern Neotethys. The U–Pb zircon ages from the Kızıldağ, the Troodos and the Semail ophiolites overlap within analytical uncertainties, suggesting that these ophiolites are contemporaneous and genetically and tectonically related within the same Late Cretaceous southern Neotethyan ocean.

Sedimentology can shed light on the emplacement of oceanic lithosphere (i.e. ophiolites) onto continental crust and post-emplacement settings. An example chosen here is the well-exposed Jurassic Mirdita ophiolite in southern Albania. Successions studied in five different ophiolitic massifs (Voskopoja, Luniku, Shpati, Rehove and Morava) document variable depositional processes and palaeoenvironments in the light of evidence from comparable settings elsewhere (e.g. N Albania; N Greece). Ophiolitic extrusive rocks (pillow basalts and lava breccias) locally retain an intact cover of oceanic radiolarian chert (in the Shpati massif). Elsewhere, ophiolite-derived clastics typically overlie basaltic extrusives or ultramafic rocks directly. The oldest dated sediments are calpionellid- and ammonite-bearing pelagic carbonates of latest (?) Jurassic-Berrasian age. Similar calpionellid limestones elsewhere (N Albania; N Greece) post-date the regional ophiolite emplacement. At one locality in S Albania (Voskopoja), calpionellid limestones are gradationally underlain by thick ophiolite-derived breccias (containing both ultramafic and mafic clasts) that were derived by mass wasting of subaqueous fault scarps during or soon after the latest stages of ophiolite emplacement. An intercalation of serpentinite-rich debris flows at this locality is indicative of mobilisation of hydrated oceanic ultramafic rocks. Some of the ophiolite-derived conglomerates (e.g. Shpati massif) include well-rounded serpentinite and basalt clasts suggestive of a high-energy, shallow-water origin. The Berriasian pelagic limestones (at Voskopoja) experienced reworking and slumping probably related to shallowing and a switch to neritic deposition. Mixed ophiolite-derived clastic and neritic carbonate sediments accumulated later, during the Early Cretaceous (mainly Barremian-Aptian) in variable deltaic, lagoonal and shallow-marine settings. These sediments were influenced by local tectonics or eustatic sea-level change. Terrigenous sediment gradually encroached from neighbouring landmasses as the ophiolite was faulted or eroded. An Aptian transgression was followed by regression, creating a local unconformity (e.g. at Boboshtica). A Turonian marine transgression initiated widespread Upper Cretaceous shelf carbonate deposition. In the regional context, the southern Albania ophiolites appear to have been rapidly emplaced onto a continental margin in a subaqueous setting during the Late Jurassic (Late Oxfordian-Late Tithonian). This was followed by gradual emergence, probably in response to thinning of the ophiolite by erosion and/or exhumation. The sedimentary cover of the south Albanian ophiolites is consistent with rapid, relatively short-distance emplacement of a regional-scale ophiolite over a local Pelagonian-Korabi microcontinent.

The Southeast Anatolian Orogen resulted from collision of the Afro-Arabian and the Eurasian plates following the Cretaceous to Miocene closure of the southern Neotethyan oceanic basin. In this orogenic belt, there are number of tectonomagmatic/stratigraphic units in the Kahramanmaraş-Malatya-Elazi{dotless}g region that are important to understand the geological evolution of southeast Anatolia during the Late Cretaceous. These are (a) metamorphic massifs (i.e. Malatya-Keban platform), (b) ophiolites (i.e. Göksun, İspendere, Kömürhan), (c) ophiolite-related metamorphics (i.e. Berit metaophiolite) and (d) granitoids (i.e. Göksun, Doganşehir and Baskil). The Baskil granitoid crops out to the northwest of Elazi{dotless}g and is a large magmatic body (170 km2) that intruded all of the above-mentioned units during Late Cretaceous time. The Baskil granitoid comprises both mafic and felsic plutonic/sub-plutonic rock associations. The felsic plutonic phase includes granite, granodiorite, tonalite and quartz monzonite whereas the felsic sub-plutonic phase is characterized by aplite, granophyre, granite porphyry and granodiorite porphyry. The granite and granodiorite contain mafic microgranular enclaves (MME). The mafic plutonic phase comprises gabbro, diorite, quartz diorite, whereas the mafic sub-plutonic phase is represented by diabase, microdiorite, quartz microdiorite, diorite porphyry, quartz diorite porphyry and dykes of orbicular gabbro dyke. Geochemically, the Baskil granitoid rocks have I-type, metaluminous-peraluminous calc-alkaline characteristics. The REE- and ocean ridge granite-normalized multi-element patterns and tectonomagmatic discrimination diagrams, together with biotite geochemistry suggest that the granitoids were formed in a volcanic arc setting. The40Ar/39Ar geochronology of the granitoid rocks yielded biotite ages of 81.9 ± 0.7 Ma and 81.5 ± 0.8 Ma (95% confidence level). Coexisting hornblende, and hornblende from additional samples, yielded ages ranging from 84.0 ± 0.7 Ma to 81.5 ± 1.1 Ma. The ophiolites are believed to have formed in a suprasubduction zone tectonic setting, whereas the ophiolite-related metamorphic rocks formed either during the initiation of intraoceanic subduction or later-stage thrusting (~ 90 Ma). These units were then thrust beneath the Malatya-Keban platform during the progressive closure of the southern Neotethys. This was followed by intrusion of the granitoids (85-82 Ma) along the Tauride active continental margin of the southern Neotethys. © 2008 Elsevier B.V. All rights reserved. Firat University Scientific Research Projects Management Unit: FBE2002-08 102Y041 This paper is a part of the PhD study of Tamer Rızaoğlu. This study was supported by two research project grants (Scientific and Technological Research Council of Turkey, TÜBİTAK with a project number 102Y041 and Niğde University Scientific Research Projects Unit, with a project number FBE2002-08). The authors would like to thank two anonymous reviewers and Alastair Robertson for suggesting improvements to the manuscript. Osman Parlak also acknowledges the financial support from the Turkish Academy of Sciences, in the frame of the Young Scientist Award Program (TÜBA-GEBİP). We are also grateful to Professor Fikret Isler for thoughtful discussions on the evolution of the granitoid bodies in the SE Anatolia.

Mesozoic ophiolitic and related rocks in the Eastern Carpathians occur in three areas, from north to south: Rarau, Haghimas and Persani Mts. They are found as blocks ranging from few metres to a few kilometers in size and as centimetre-sized in breccias, most likely embedded in the Late Barremian–Early Albian Wildflysch formation. Compositionally, they range from lherzolites and harzburgites to mafics such as FeTi gabbros, dolerites, basalts, and to andesites. The volcanics comprise highly-depleted basalts/andesites to enriched-type mid-ocean ridge basalts; additionally they include ocean island basalts and calc-alkaline basalts/andesites and trachytes. Based on paleontological evidence, their age is Middle to ?Late Triassic. They can be clearly compared with remnants of the Meliata–Hallstatt Ocean in the Western Carpathians, but do not match the Jurassic ophiolites and island arc volcanics in the Mures Zone of the Southern Apuseni Mts. We propose a Triassic ocean connected with the Meliata–Hallstatt Ocean, between (a) the Bucovinian/Sub-Bucovinian continental crust, (b) the Infrabucovinian and finally (c) the Northern Apuseni microcontinents. This ocean closed in the Late Triassic to Early Jurassic causing close juxtaposition of all three microcontinents. An ophiolite complex together with ocean island basalts and calc-alkaline basalts/andesites remained from this ocean and was subsequently eroded and transported as blocks of different size into the Lower Cretaceous Wildflysch basin, together with blocks and clasts of limestones similar to the Mesozoic sedimentary sequences in the Northern Apuseni realm. The Wildflysch formation was thrust as an independent unit during the Albian over the Bucovinian Nappe in the Eastern Carpathians and the Northern Apuseni continental crust, respectively.

In the Transylvanian Depression (Romania) a number of deep wells were drilled to investigate and exploit methane gas fields. From these, only a few penetrated the Middle to Upper Jurassic volcanics in the basement. From three boreholes (Deleni, Cenade and Zoreni) rock samples were available for investigations. Deleni and Cenade show calc-alkaline basalts to andesites which are similar to the island arc volcanics of the Southern Apuseni Mountains. Zoreni basalts and basaltic andesites show a boninitic affinity, which was not found up to now in outcrops. The distribution of the volcanics in the basement of the Transylvanian Depression, which correlates with a geomagnetic anomaly, can be explained by the presence of a magnetite-rich ophiolite layer beneath the island arc volcanics. Comparable oceanic crust rocks are found further west, in the Southern Apuseni Mountains. They are considered to be remnants of a marginal or back-arc basin, in which a volcanic arc including boninites developed. Upon the westward-directed subduction of an open ocean, the island arc and part of the back-arc basin were overthrusted eastwards onto continental crust during the Late Jurassic or Early Cretaceous. A flip in the subduction direction caused late Early Cretaceous westward thrusting of the back-arc basin and island arc rocks onto the crystalline basement of the Tisia continent.

Rock, soil, and plant (terrestrial moss, European mountain ash leaves, mountain birch leaves, bark and wood, and spruce needles and wood) samples, collected at 3 km intervals along a 120 km long transect (40 sites) cutting the city of Oslo, Norway, were analysed for their Pb concentration and Pb-isotope ratios. A general decrease in 206 Pb/ 207 Pb, 208 Pb/ 207 Pb and 206 Pb/ 208 Pb ratios, with a characteristic low variability in all plant materials and the plant-derived O-horizon of soil profiles, compared to rocks and mineral soils, is observed along the transect. It is demonstrated that minerogenic and biogenic sample materials belong to two different spheres, the lithosphere and biosphere, and that geochemical processes determining their chemical and isotopic compositions differ widely. Background variation for both sample materials needs to be established and documented at the continental and global scale before the anthropogenic influence on the geochemistry of the earth’s surface can be reliably estimated.

Major discoveries in metamorphic petrology, as well as other geological disciplines, have been made in the Alps. The regional distribution of Late Cretaceous-Tertiary metamorphic conditions, documented in post-Hercynian metasediments across the entire Alpine belt from Corsica-Tuscany in the west to Vienna in the east, is presented in this paper. In view of the uneven distribution of information, we concentrate on type and grade of metamorphism; and we elected to distinguish between metamorphic paths where either pressure and temperature peaked simultaneously, or where the maximum temperature was reached at lower pressures, after a significant temperature increase on the decompression path. The results show which types of process caused the main metamorphic imprint: a subduction process in the western Alps, a collision process in the central Alps, and complex metamorphic structures in the eastern Alps, owing to a complex geodynamic and metamorphic history involving the succession of the two types of process. The western Alps clearly show a relatively simple picture, with an internal (high-pressure dominated) part thrust over an external greenschist to low-grade domain, although both metamorphic domains are structurally very complex. Such a metamorphic pattern is generally produced by subduction followed by exhumation along a cool decompression path. In contrast, the central Alps document conditions typical of subduction (and partial accretion), followed by an intensely evolved collision process, often resulting in a heating event during the decompression path of the early-subducted units. Subduction-related relics and (collisional/decompressional) heating phenomena in different tectonic edifices charac- terize the Tertiary evolution of the Eastern Alps. The Tuscan and Corsica terrains show two differ- ent kinds of evolution, with Corsica resembling the western Alps, whereas the metamorphic history in the Tuscan domain is complex owing to the late evolution of the Apennines. This study confirms that careful analysis of the metamorphic evolution of metasediments at the scale of an entire orogen may change the geodynamic interpretation of mountain belts.

Forty samples each of leaves, bark and wood of mountain birch ( Betula pubescens EHRH.) were collected along a 120 km long south–north transect running through Norway’s largest city, Oslo. Concentrations of 26 chemical elements (Ag, As, Au, B, Ba, Ca, Cd, Co, Cr, Cu, Fe, Hg, K, La, Mg, Mn, Mo, Na, Ni, P, Pb, S, Sb, Sr, Ti and Zn) as well as loss on ignition for the three sample materials are reported. By far the highest concentrations of most elements appear in the leaves. Prominent exceptions are Au and Pb, both of which are enriched in wood, indicating the importance of root-uptake, and As which is enriched in bark. Bedrock lithology, ore occurrences, soil pH and urban contamination all have a visible influence on the element concentrations in mountain birch leaves, bark and wood. It is often impossible to differentiate between all the factors that can influence element concentrations in the three sample materials. Mountain birch bark shows the strongest anthropogenic impact of the city of Oslo for dust-related elements (Fe, La, Ti) and Sb. Even in mountain birch bark the influence of the city on element concentrations is no longer discernible from the background variation at a distance of less than 20 km from Oslo centre. Compared to terrestrial moss, mountain birch appears to be of little value as a biomonitor for urban contamination.

Forty samples each of leaves of birch (Betula pubescens Ehrh.), European mountain ash (Sorbus aucuparia (L.)) and bracken fern (Pteridium aquilinum (L.) Kuhn) as well as spruce needles (Picea abies (L.) Karsten) were collected along a 120 km south-north transect running through Norway's largest city, Oslo. Concentrations of 25 chemical elements (Ag, Au, B, Ba, Ca, Cd, Co, Cr, Cu, Fe, Hg, K, La, Mg, Mn, Mo, Na, Ni, P, Pb, S, Sb, Sr, Ti, and Zn) as well as loss on ignition for the 4 sample materials are reported. The decline of input of sea spray with distance from the coast, geology, pH and anthropogenic contamination all played a role for the observed element concentrations in the leaves. Although growing under exactly the same natural conditions each plant species displayed quite unique uptake characteristics. Plant-species dependency and individual differences in the reaction of the plant leaves to different element sources make the investigated species of very limited value as bioindicators of anthropogenic activities. Anthropogenic contamination influences plant-leaf element content within a limited distance ( approximately 20 km) from the source.

Rock samples and the C-, B- and O-horizons of soils developed on these rocks were collected in forested areas along a 120-km south–north transect in southern Norway, passing through the city of Oslo. Forty samples (1 site/3 km) were analysed for 37 chemical elements (Ag, Al, As, Au, B, Ba, Bi, Ca, Cd, Co, Cr, Cu, Fe, Ga, Hg, K, La, Mg, Mn, Mo, Na, Ni, P, Pb, S, Sb, Sc, Se, Sr, Te, Th, Ti, Tl, U, V, W and Zn) following an aqua regia digestion; pH (water extract) and loss on ignition were also determined. The O-horizon soils were additionally analysed for Pt. Gold is the only element that shows a clear anthropogenic peak in the O-horizon soils collected from the city of Oslo. Silver, Au, Bi, Cd, Hg, Pb, S, Sb, Se and Sr all show a strong enrichment in the O-horizon when compared to the underlying C-horizon or the bedrock along the full length of the transect. Neither geology nor anthropogenic input of elements dominate the observed patterns. The most important factors for the observed element concentrations in the O-horizon are weathering, uptake (or rejection) of elements by plants and the kinetics of decay of the organic material in the O-horizon. Climate, especially temperature and precipitation, has an important influence on the formation and decay rates of the organic soil layer. Acid precipitation will delay the decomposition of the organic layer and lead to a natural enrichment of several metals in the O-horizon. Land use change, deforestation and liming can all increase the decay kinetics of organic matter and thus result in a release of the stored element pool.

The ophiolitic rocks of the easternmost Penninic unit, the Koszeg-Rechnitz series, were analyzed for their H, C and O stable isotope compositions. Serpentinite, gabbro, blueschist, talc deposits, ophicarbonates, as well as calcite and inclusion fluids from quartz segregation veins were analyzed in order to determine the effects of different metamorphic events on the stable isotope compositions. The oxygen isotope compositions have a wide range depending on rock type and locality. Gabbro and serpentinite of Bienenhutte (Bernstein Window) have preserved mantle-like δ 18O values (5.9 to 6.3‰; all values are in ‰ relative to V-SMOW), whereas the serpentinite of Glashutten and Rumpersdorf (Koszeg-Rechnitz Window) and the silicate minerals of the ophicarbonate rocks show a strong 18O-enrichment (up to 16.2‰). The 18O-enrichment may have been induced by low-temperature serpentinization or interaction with 18O-rich fluids that had been in equilibrium with sedimentary rocks. Contrary to the O isotope comp...

The Albanian (Mirdita) Ophiolites are part of a large NNW-SSE striking ophiolite zone, which comprises the Dinaric Ophiolites as well as some Greek ophiolites such as Pindos, Vourinos or Othris. Their Jurassic age is constrained by palaeontological evidence of the sediments on top of the ophiolites, by the age of the metamorphic soles and by the age determinations of the intrusive plagiogranite (BORTOLOTTI et al, 2004; DILEK et al., 2005 and references herein). The origin of the Albanian ophiolites is essential to restore the continent/ocean distribution in the Jurassic in the Eastern Mediterranean realm and the possible sites of the subduction zones and related thrusts. The environment of formation of these ophiolites and the mode of their emplacement is still controversial.

Elevated P contents of up to 0.086 apfu (1.21 wt.% P2O5) were found in garnet from leucocratic granitic rocks (orthogneisses, granites, barren to highly evolved pegmatites) in the Moldanubicum and Silesicum, Czech Republic, and in complex granitic pegmatites from southern California, USA, and Australia. Minor concentrations (0.15–0.55 wt.% P2O5) appear ubiquitous in garnet from leucocratic granitic rocks of different origins and degrees of fractionation. Concentrations of P are not related to Mn/(Mn + Fe) that vary from 0.12–0.86 and to textural types of garnet (i.e., isolated anhedral to euhedral grains and nodules, graphic and random garnet–quartz aggregates, subsolidus veins of fine-grained garnet). Garnet compositions exhibit negative correlations for P/Si and P/R2+ where R2+ = Fe + Mn + Mg + Ca, while Al is constant at ∼2.05 apfu. Concentrations of Na are largely below 0.02 apfu but positively correlate with P. The main substitution may involve A-site vacancy and/or the presence of some light element(s) in the crystal structure. The substitution □P2 R2+−1Si−2 and/or alluaudite-type Na□P3 R2+−1Si−3 seem the most likely P-incorporating mechanisms. The partitioning of P among garnet and associated minerals in granitic systems remains unclear; however, it directly affects the distribution of Y and REEs.

Three major groups (A-C) of Central European Variscan granitoids can be distinguished based on petrologic and chemical data: A. Low-K, high-Na, calc-alkaline, alkali-calcic, met/peraluminous, I- and S-type, trondhjemitic (slightly granodioritic)-suite, mostly magnesian granitoids formed at the early stage of continent-continent collision (353-356 Ma). These types of granitoids occur in the northern part of the Central Bohemian Plutons (CBP) in the Moldanubian Zone or in the Austroalpine Zone of the outer belt of the Western Carpathian Plutons (WCP). The granitoid melt source originated from partially melted oceanic and continental crusts due to compression. B. High-K, high-Mg, calc-alkaline, metaluminous, I-type, monzonitic-suite granitoids with lamprophyre-derived small, ultrapotassic, Mg-rich intrusions formed in the post-collision zone, where the melts originated from the partially melted, uplifted, LIL-rich mantle and continental crust, due to extension (334-354 Ma) after earlier compression. These in...

There are several pre-orogenic Neoproterozoic granitoid and metavolcanic rocks in the Lufilian–Zambezi belt in Zambia and Zimbabwe that are interpreted to have been emplaced in a continental-rift setting that is linked to the break-up of the Rodinia supercontinent. However, no geochemical data were previously available for these rocks in the Zambian part of the belt to support this model. We conducted petrographic and whole-rock chemical analyses of the Neoproterozoic Nchanga Granite, Lusaka Granite, Ngoma Gneiss and felsic metavolcanic rocks from the Lufilian–Zambezi belt in Zambian, in order to evaluate their chemical characteristics and tectonic settings. Other magmatic rocks of importance for understanding the evolution of the belt in Zambia, included in this study, are the Mesoproterozoic Munali Hills Granite and associated amphibolites and the Mpande Gneiss. The Neoproterozoic rocks have monzogranitic compositions, aluminum-saturation indices (ASI) < 1.1, and high contents of high field strength elements (HFSE) and rare earth elements (REE). The chondrite-normalised spider diagrams are similar to those of A-type granites from the Lachlan fold belt and show negative Sr, P, and Ti anomalies. On various tectonic discrimination diagrams the Neoproterozoic rocks plot mainly in A-type granite fields. These petrographic and trace element compositions indicate that these rocks are A-type felsic rocks, but they do not have features of granites and rhyolites emplaced in true continental-rift settings, as previously suggested. On the basis of the A-type features and independent regional geological and geochronological data, we suggest that the Neoproterozoic granitoid and felsic metavolcanic rocks were emplaced during the earliest extensional stages of continental rifting in the Lufilian–Zambezi belt. The apparent continental-arc like chemistry of the granitoid and felsic metavolcanic rocks is thus inferred to be inherited from calcalkaline sources. The Mesoproterozoic Munali Hills Granite and Mpande Gneiss have trace element features e.g., Nb–Ta depletions, which indicate that that these gneisses were emplaced in a convergent-margin setting. The MORB-normalised spider diagram of co-magmatic amphibolites exhibit a fractionated LILE/HFSE pattern recognized in subduction zones. This inference is consistent with remnants of ocean crust, juvenile Island arcs and ophiolites elsewhere in the Mesoproterozoic Irumide belt in Zambia and Zimbabwe. In addition, we report the first U–Pb zircon age of 1090.1 ± 1.3 Ma for the Munali Hills Granite. The age for the Munali Hills Granite provides new constraints on correlation and tectono-thermal activity in the Lufilian–Zambezi belt. The age of the Munali Hills Granite indicates that some supracrustal rocks in the Zambezi belt of Zambia, which were previously thought to be Neoproterozoic and correlated with the Katanga Supergroup in the Lufilian belt, are Mesoproterozoic or older. Consequently, previous regional lithostratigraphic correlations in the Lufilian–Zambezi belt would require revision. � 2005 Elsevier Ltd. All rights reserved.

Leaves of up to eleven different plant species (terrestrial moss: Hylocomium splendens and Pleurozium schreberi ; blueberry: Vaccinium myrtillus and Vaccinium uliginosum ; cowberry: Vaccinium vitis-idaea ; crowberry: Empetrum nigrum ; birch: Betula pubescens and Betula nana ; willow: Salix spp.; pine: Pinus sylvestris ; and spruce: Picea abies ) have been collected from up to nine catchments (size 14–50 km 2 ) spread over a 1 500 000 km 2 area in northern Europe and analysed for ‘total’ (digestion by 16M HNO 3 ) sulphur concentrations. Soil samples were taken of the O- and C-horizon at each plant sample site. The soil samples were analysed for ‘total’ (digestion by 16M HNO 3 for O-horizon, aqua regia for C-horizon) and ‘soluble’ (ammonium acetate extraction buffered at pH 4.5, O-horizon only) S concentrations. The overall median S concentration for all plants is 1290 mg kg −1 . The median S concentration is 965 mg kg −1 in moss; 990 mg kg −1 in conifers; 1490 mg kg −1 in shrubs; and 1900 mg kg −1 in deciduous trees. Total S concentrations in the leaves of the 11 plant species are very different within and between the catchments. Compared to the total regional variance, the local variance within just one catchment is very high. One of the nine catchments was located directly adjacent (5–10 km S) to the nickel smelter and refinery at Monchegorsk, Kola Peninsula, Russia, one of the largest SO 2 (and metal) emitters in Europe. Only spruce needles returned significantly higher S concentrations (by a factor of 2) in all samples collected near Monchegorsk. Otherwise pollution is reflected in a higher variance rather than in high concentrations. Willow leaves show by far the highest total S concentrations. They are, however, not related to pollution but were observed in the catchment nearest to the coast of the Barents Sea. The measured S concentrations in the leaves do not correlate well either with ‘available’ or total S in the soils. Several different pathways must be considered for leaf uptake of S in all plants. The important role of S as a major plant nutrient and the consequently high background concentrations and variations prohibit the use of leaves as reliable indicators of SO 2 pollution levels in air. It is not possible to establish general ‘background’ S concentrations in plant leaves for a very large area.

Within the western belt of the southern Albanian ophiolites, the Voskopoja ophiolite consists of three subunits: Voskopoja, Morava and Rehove. These are predominantly lherzolites with minor harzburgites and dunites in the mantle section. Above come ultramafic and mafic cumulates including wehrlites, troctolites and olivine gabbros. Gabbronorites are restricted to the Morava subunit. Isotropic clinopyroxene gabbros, extrusives and sediments are present only in Rehove and Voskopoja. The volcanic section is dominated by basaltic breccias, including megablocks with sheeted dykes, pillow lavas and isolated dykes. The basaltic breccias grade upwards into sandstones, in turn, interlayered with argillites and cherts of Jurassic age. The basalts are predominantly clinopyroxene–plagioclase basalts, either aphyric or plagioclase phyric. Geochemically, they are divided into four groups: (1) an intermediate Ti and Zr group with low Ni (hereafter called low-Ni group), (2) an intermediate Ti–Zr group with high Ni (hereafter called high-Ni group), (3) a high-Ti–Zr group and (4) a low-Ti–Zr group. The high-Ni content in group 2 is interpreted as originating from olivine and spinel xenocrysts. Apart from the high-Ni content, groups 1 and 2 are comparable with the volcanics of the “low- to high-Ti intermediate ophiolites.” By contrast, group 3 is more comparable to the high-Ti ophiolitic extrusives in the western ophiolite belt of northern Albania. Group 4 consists SSZ-type basalts and is widespread in the volcanics of the eastern ophiolite belt. Comparison of the ultramafic–mafic cumulates and the basaltic volcanics with those in the northern part of the western belt in Albania and the Pindos ophiolite indicates that there is a systematic variation in petrography and geochemistry from north to south in the western belt, with an increasingly distinct SSZ signature towards the south. Ultramafic and mafic cumulates, as well as basalts from the Shebenik massif in the eastern belt, are similar to those of Voskopoja, implying a genetic relationship.

Silicate melt inclusions are frequent in the phenocryst phases (quartz, plagioclase, orthopyroxene, ilmenite and accessory minerals) of the Miocene silicic pyroclastic rocks of the Bukkalja Volcanic Field, Northern Hungary. These melt inclusions were trapped at different stages of magma evolution; therefore, they provide important information on the petrogenetic processes. The melt inclusions in the Bukkalja pyroclastic rocks show various textures such as (1) wholly enclosed type; (2) hourglass inclusions and (3) reentrant or embayment glass. Among the wholly enclosed type melt inclusions further textural subgroups can be distinguished based on their shape: negative crystal, rounded, elongated and irregular shaped. These various textures reflect differences in the time of entrapment prior to eruption and in the post-entrapment condition in the magma chamber. The largest textural variation was found in the quartz-hosted melt inclusions. However, the major element compositions of these melt inclusions do no...

Weinsberg type granite’ as it is doubtful whether it should PREFACE be named according to IMA rules in view of its very The comment by Finger & Clemens (2002) nicely concomplex origin. Even if we look at these rocks in a firms the statement in the introduction of our paper purely descriptive sense, neglecting all genetic aspects, (Klotzli et al., 2001) on p. 1622: ‘Unravelling the origin the granitoids range in composition from minor quartz of a given granite still requires a major analytical effort monzodiorites to a majority of quartz monzonites and and commonly ends in some contradictory results’. Finger granites according to the IMA nomenclature. The in& Clemens raise a number of issues, both minor and terpretation of Finger & Clemens (2002) that all the rocks major. We will discuss all of them, as far as they are are quartz monzodiorites is an oversimplification and relevant to the subject. We will start with the problem conflicts with the geochemical composition of the pyrof nomenclature. After that we will address the problem of oxene-bearing rocks, their K contents (4–6 wt % K2O) remnants of an old crustal component versus a cumulate and the constant high amount of modal K-feldspar. In origin and the problem of the age of the crustal remnants. addition, in all norm calculations the amount of normative K-feldspar has to be corrected according to the measured preserved feldspar composition of Or0·78 PETROLOGY Ab0·20An0·01Cs0·01 (F. Koller, 2000). Finger & Clemens (2002) in their comment accept the Opxand cpx-bearing Weinsberg type granitoid rocks formation of the Weinsberg granite sensu lato magma are widespread in an area of >15–20 km surrounding under granulite-facies conditions within the stability field the villages of Sarleinsbach, Sprinzenstein and Arnreit of opx, as was already postulated by Koller & Hock in the Southern Bohemian Massif (Klotzli et al., 2001, (1993). Finger & Clemens interpret opx and cpx as a figs 1 and 2). This type of rock shows a wide variation product of fractional crystallization of a quartz-monzoin chemical and mineralogical composition. The most dioritic magma after partial melting of biotite-bearing conspicuous features are large K-feldspars up to 20 cm lower-crustal rocks. Consequently, in their view the pyrin size. As a consequence, the determination of modal oxenes are cumulate phases. In contrast, we interpret mineralogy must take into account the large size of the the pyroxenes as part of an older magmatic event K-feldspar megacrysts and be carried out on large samples only. We referred to this rock as ‘pyroxene-bearing with a superimposed granulite-facies re-equilibration

Leaves of 9 different plant species (terrestrial moss represented by: Hylocomium splendens and Pleurozium schreberi; and 7 species of vascular plants: blueberry, Vaccinium myrtillus; cowberry, Vaccinium titis-idaea; crowberry, Empetrum nigrum; birch, Betula pubescens; willow, Salix spp.; pine, Pinus sylvestris and spruce, Picea abies) have been collected from up to 9 catchments (size 14-50 km2) spread over a 1500000 km2 area in Northern Europe. Soil samples were taken of the O-horizon and of the C-horizon at each plant sample site. All samples were analysed for 38 elements (Ag, Al, As, B, Ba, Be, Bi, Ca, Cd, Co, Cr, Cu, Fe, Hg, K, Li, Mg, Mn, Mo, Na, Ni, P, Pb, Rb, S, Sb, Sc, Se, Si, Sn, Sr, Th, Tl, U, V, Y, Zn and Zr) by ICP-MS, ICP-AES or CV-AAS (for Hg-analysis) techniques. The concentrations of some elements vary significantly between different plants (e.g. Cd, V, Co, Pb, Ba and Y). Other elements show surprisingly similar levels in all plants (e.g. Rb, S, Cu, K, Ca, P and Mg). Each group of plants (moss, shrubs, deciduous and conifers) shows a common behaviour for some elements. Each plant accumulates or excludes some selected elements. Compared to the C-horizon, a number of elements (S, K, B, Ca, P and Mn) are clearly enriched in plants. Elements showing very low plant/C-horizon ratios (e.g. Zr, Th, U, Y, Fe, Li and Al) can be used as an indicator of minerogenic dust. The plant/O-horizon and O-horizon/C-horizon ratios show that some elements are accumulated in the O-horizon (e.g. Pb, Bi, As, Ag, Sb). Airborne organic material attached to the leaves can thus, result in high values of these elements without any pollution source.

The Suqii-Wagga two-mica granite, situated in the western Ethiopian Precambrian, is emplaced in a high-grade migmatitic terrane. It is composed of feldspars + quartz + muscovite + biotite ± garnet + zircon ± allanite ± apatite + Fe-Ti oxides + Fe sulphide. Textural studies and microprobe analyses revealed two generations of almandine-spessartine-rich magmatic garnet. The first is euhedral, fine-grained (300–350 μm), commonly occurs as inclusions in plagioclase and alkali feldspars, and exhibits chemical zoning with almandine-rich cores and spessartine-rich rims. In contrast, the second variety is medium- to coarse-grained (1–7 mm) and shows reverse zoning with spessartine-rich cores and almandine-rich rims. Primary and secondary muscovites were discriminated based on the concentrations of Ti, Fe, Mn and Na. Biotite is characterised by a higher alumina saturation index than biotites of other granitoids in the area, suggesting considerable alumina concentration in the source magma. Garnet-biotite thermometry and phengite barometry were used to estimate the P-T conditions of crystallisation for the Suqii-Wagga two-mica granite pluton at ∼ 7 kbar and ∼ 670°C. Mineral paragenesis, the composition of aluminous minerals and the P-T conditions of crystallisation indicate that samples containing fine-grained garnet crystallised earlier than those containing medium- to coarse-grained garnet. Field and petrographic investigations, mineral chemistry, and whole rock major and trace element studies suggest that the Suqii-Wagga two-mica granite has the characteristics of anatectic granite. Highly variable normative Ab/Or ratios suggested melting under varying aH2O conditions and/or source characteristics. The relatively high Rb/Sr, Rb/Ba and low CaO/Na2O (

[No abstract available]

Crystalline rocks from the western Ethiopian Precambrian terrain comprise two major rock groups: (1) the often migmatised eastern and western high-grade gneisses; and (2) the central low-grade metavolcanosedimentary rocks. Granitoid bodies of different ages and compositions intrude these rocks. Field observations, petrographic investigations, and geochemical features support a two-fold classification of the granitoid rocks. The volcanic arc granitoids (VAG) are most common and include the Ujjukka granite and granodiorite, and the Dhagaa Booqa and Guttin K-feldspar megacrystic granites. The second and geographically more restricted group represents within-plate or anorogenic (A-type) granitoids, typified by the Tullu Kapii syenite. Geochemically, the Tullu Kapii syenite is characterised by moderate to high contents of SiO2, total alkalis, Y, Nb, Ta, Hf, Zn, Zr, Ga, ΣREE, higher ratios of Fe2O3(total)/MgO, Rb Sr , Rb Ba , and lower contents of CaO, MgO, Sr, and Ba, compared to the other granitoids. The VAG group shows chondrite-normalised REE patterns with slightly enriched LREE and flat HREE patterns without significant Eu anomalies. In contrast, the Tullu Kapii A-type granitoid is characterised by a nearly horizontal REE pattern with variable negative Eu anomalies. The Ujjukka granite and granodiorite; and the Dhagaa Booqa and Guttin K-feldspar megacrystic granites originated in a two-step process, which involves batch equilibrium melting of basaltic or andesitic material producing tonalitic magma, followed by fractional crystallisation. The Tullu Kapii syenite was the product of partial melting of source rocks enriched in high field strength elements.

The ReOs and SmNd isotopic systematics of polymetamorphic massif peridotite bodies, which have been described as ophiolites, are examined. The serpentinized mantle rocks from different tectonic units of the Eastern Alps reveal that Os isotopes are robust and provide information that field studies, petrographic and major and trace element studies do not. Presumed Paleozoic (e.g., Kraubath and Hochgrossen) and Mesozoic (e.g., Reckner Complex) bodies have uniform 187Os/188Os ratios that are slightly higher than, but within the range of, abyssal peridotites, which are presumed to represent the depleted mid-ocean ridge basalt source mantle (DMM). One serpentinite from the Penninic unit yields 187Os/188OS much lower than DMM. This mantle rock must have had a source in a long-term Re-depleted reservoir of the upper mantle. Although our understanding of the ReOs isotope system of upper mantle reservoirs is still limited, this system can be used to help constrain the tectonic evolution of diverse terrains.

The BayonNeoproterozoic plutonic complex located in Western Cameroon intrudes gneisses of Paleo to Neo Proterozoic age. The complex is composed of gabbro, monzogabbro and monzonites frequently crosscut by trachytic and granitic veins. The primary mineral assemblages of the gabbro and monzogabbro is plagioclase (An 30 - An 69 ), clinopyroxene (En 40 – 42 Fs 12 – 18 Wo 45 - 47 ) hypersthene (En 62 – 65 Fs 34 – 37 Wo 1- 4 ) and orthoclase (Or 78 -Or 91 ) whilebiotite, magnetite, Ilmenite and apatite constitute accessory minerals. Monzonite is formed of plagioclase (An22 to An 39 ), orthoclase (Or 80 -Or 87 ),clinopyroxene (En 38-39 Fs 14-20 Wo 45-46 ), biotite and quartz. Amphiboles occur as secondary minerals. Ilmenite and apatite are accessory minerals in monzonite.The rocks are mafic to intermediate in composition (41 – 61 wt % SiO 2 ) and transalkaline with high-K and have shoshonitic features. Bayon plutonic rocks have high abundance of Ba, Sr ,V and Zr but possesses low concentrations of Rb, Sc, Y and Th.Gabbroic rocks show moderately fractioned REE patterns (La N /Lu N = 14 – 27) with none or negligible Eu anomalies. The monzonite shows also moderate fractionatedpatterns (La N /Lu N = 20 – 27) with fairly positive Eu anomalies. All the studied rocks show flat HREE features. The primitive mantle- normalized element patterns are almost homogeneous with negative anomalie in Ta, Nb, Th, P and Ti. Sm/Nd-wr-Cpx-Pl ages of the complex are 580 ± 13 Ma; 553 ± 32 Ma for the monzogabbro and 547 ± 26 Ma for the monzonite. The Nd/Sr isotopic compositions show that the Bayon plutonic rocks were generated by partial melting of subcontinental lithospheric mantle. The depleted mantle Nd model age TD M of 1.6 – 1.7 Ga indicates that the studied rocks originated by partial melting of Mesoproterozoic mantle. KEYWORDS: West Cameroon, Panafrican, Pluton, Geochemistry, partial meting

WOS: 000317545800003 The Inner Tauride ocean separated the Tauride-Anatolide Block from the Central Anatolian Crystalline Complex. This oceanic basin was consumed as a result of north-dipping subduction and closed during the latest Cretaceous to early Cenozoic times. Subduction-related magmatism and metamorphism occurred at different stages during the closure of the Inner Tauride ocean. The ophiolites and granitoids record the tectonic events. In this paper, we present new U-Pb zircon age determinations by LA-MC-ICP-MS and Ar-40-Ar-39 age dating of selected ophiolites (Mersin, Pozanti-Karsant, Pinarbasi and Divrigi) and granitoids (Horozkoy and Divrigi) along the Inner Tauride suture zone. The results show that: (i) the crystallization age of SSZ oceanic crust is similar to 89 Ma and the magmatic activity continued until just prior to ophiolite emplacement onto the Tauride-Anatolide platform during the latest Cretaceous (Maastrichtian), (ii) the timing of intraoceanic thrusting/subduction is constrained as similar to 89 Ma, which is consistent with steady-state subduction in a forearc tectonic setting, (iii) the timing of collision of the Tauride-Anatolide passive margin with the subduction trench of the Inner Tauride ocean and subsequent slab break-off occurred from 76 to 67 Ma, and (iv) the timing of continent-continent collision between the Central Anatolian Crystalline Complex and the Tauride-Anatolide Block is constrained as Eocene (50-49 Ma). The first three tectonic stages overlap each other during the closure of the Inner Tauride oceanic basin. 'Soft' collision of the subduction trench with the passive margin was followed by hard-collision and suture tightening similar to 8-10 My later. (C) 2012 Elsevier Ltd. All rights reserved. TUBITAKTurkiye Bilimsel ve Teknolojik Arastirma Kurumu (TUBITAK) [106Y231]; Cukurova University Research FoundationCukurova University [MMF2011BAP16]; TUBITAK-BIDEBTurkiye Bilimsel ve Teknolojik Arastirma Kurumu (TUBITAK) This work is supported by TUBITAK (Project no: 106Y231) and partly by Cukurova University Research Foundation (project no: MMF2011BAP16). Fatih Karaoglan acklowledges International Research Fellowship Programme support from TUBITAK-BIDEB. Alastair Robertson, Yener Eyuboglu and Erdin Bozkurt are thanked for their valuable comments and suggestions that improved the manuscript.

Major-, trace-, rare-earth-element, and RbSr and SmNd isotope data of the various low-grade metamorphosed magmatic units in the Pan-African Gariep Belt, southwestern Namibia, presented in this paper, provide the basis for the reconstruction of the evolution of the late Proterozoic Adamastor ocean between the South American and Kalahari Cratons. The Gariep Belt is subdivided into two major zones, a para-autochthonous, predominantly sedimentary rift and passive continental margin succession (Port Nolloth Zone, PNZ) and the allochthonous, predominantly mafic Marmora Terrane. The latter has been thrust in southeasterly direction over the former. All of the magmatic activity in the PNZ can be related to lithospheric stretching. The earliest magmatic activity is expressed as bimodal volcanism with continental within-plate affinity along an embryonic rift graben (Rosh Pinah Formation) and is found within the older sediment package of the para-autochthonous external zone of the orogen. After ∼ 24 Ma, this was followed by the intrusion of mafic, tholeftic dykes into the basement and the lower parts of the PNZ, heralding the opening of the Gariepian basin at 717 Ma. There is evidence of a series of seamounts, or an aseismic ridge, with oceanic within-plate characteristics in the Marmora Terrane. Such volcanic piles make up most of the Schakalsberge Complex and parts of the Chameis Complex. Both complexes are separated by turbidites (Oranjemund Complex), which are interpreted as continental slope deposits. In the Chameis Complex, metagabbros predominate. Most of them are part of the oceanic seamounts, but some have a markedly different chemistry, indicative of a mid-ocean ridge setting. During Pan-African collision, the Marmora Terrane formed an accretionary wedge that was thrust over the passive continental margin succession. Peak metamorphism in the thickened crust was reached at ∼ 545 Ma, with erosion of the orogen having commenced as early as 540 Ma.

The Stravaj ophiolite compex, part of the western Mirdita ophiolite belt in Albania, is located east of the Shpati massif, and west of the Shebenik massif. The Stravaj ophiolite sequence itself consist of MOR-related and subduction-related volcanic rocks (Hoeck et al. 2007) formed by pillow lavas and various dykes. The deeper units are formed by gabbros and plagioclase-bearing peridotites. The pillow lavas are intersected by basaltic dykes with a rather primitive composition. The studied basaltic dyke contains former relics of olivine, fresh spinel and clinopyroxene phenocrysts in a glassy groundmass. The silicate phases are strongly altered. The spinels appear as fresh, opaque grains preserved in totally altered olivine phenocrysts. The spinels host negative crystal shaped, multiphase silicate melt inclusions. The inclusions consist commonly of clinopyroxene daughter minerals, glass and rare sulphide blebs. A series of heating experiments were conducted, using the furnace technique to homogenize the silicate melt, in order to obtain homogenized silicate melt inclusions for major and trace element composition analysis and to determine their homogenization temperatures. Therefore, samples were heated to and quenched from 1200±20°C to 1240°C. The melt inclusions homogenized between 1220-1240±20°C. The major element composition of the homogenized melt inclusions is 48.3-51.2 wt% SiO2, 5.4-6.7 wt% FeO, 9.9-12.6 wt% MgO, 14.5-17.3 wt% Al2O3, 1.9-2.4 wt% Na2O and 12.1-13.0 wt% CaO. This result is highly comparable with the host mafic rock composition. The trace element composition of the homogenized silicate melt shows characteristic LREE-depleted patterns (La: 0.24-0.35 ppm), while the MREE and HREE patterns are generally flat: average PM-normalized La/Lu is 0.094. The average contents of compatible trace elements such as Cr, Ni, V, Co are up to 621 ppm, 825 ppm, 235 ppm and 80 ppm, respectively. Based on the major composition, trace element characteristics and the calculated oxygen fugacity, the studied silicate melt inclusions show strong similarities to MOR-related volcanic rocks found commonly in the Stravaj Massif. These chromite-bearing basalt dykes define extreme primitive MORB related melts in the upper part of the pillow lava section.

The Axum volcanic rocks constitute an important outcrop of trap basalts at the northern end of the great Ethiopian flood basalt province. They constitute about 5–480-m-thick sequences exposed around Axum and Shire regions covering a total area of about 900 km2. Even though the Axum volcanic rocks were previously assigned to the low-Ti (LT) tholeiitic basalts of the northwestern Ethiopian volcanic province, our geochemical studies on rocks from this region reveal that these rocks are alkaline to transitional in composition with distinct geochemical characteristics. Their petrologic diversity is very significant, the lavas ranging from basanites to tephrites and trachy-andesites. The variation in the major element (TiO2 and Fe2O3) concentrations, incompatible trace elements, and the rare earth element (REE) concentrations and ratios (e.g., (La/Yb)n = 5.0–14.0) indicate a complex petrogenetic evolution of the flood basalts. The Axum volcanic rocks are entirely alkaline to transitional in nature and are classified here into the Lower Sequence (Low-Ti) basalts and the Upper Sequence (High-Ti) basalts. Both these sub-divisions are also reflected in their unique chondrite-normalized REE patterns and multi-element diagrams: the Lower Sequence basalts show enhanced REE fractionation and higher concentrations of the highly incompatible trace elements; whereas the Upper Sequence basalts exhibit less REE fractionation and relatively high concentrations of the moderately incompatible trace elements. The mineralogical and geochemical variations among the basalts of Axum provide clues about the complexity of the northern and northwestern Ethiopian flood basalts and their petrogenetic evolution.

Scapolite is an important mineral in the metamorphism of calc-silicates, marbles, amphibolites, and metagabbros in the Lufilian–Zambezi belt of Zambia. Both field and petrographic studies on granite gneisses, amphibolites, and metagabbros from the Munali hills area, in the southern part of the Lufilian–Zambezi belt indicated that scapolitization was due to metasomatism. The scapolite occurs as a pervasive replacement of plagioclase in the Munali hills granite gneiss, amphibolites, and metagabbros, and is associated with mineral assemblages that are indicative of amphibolite-facies metamorphism. Results of mineral analyses show that all the scapolites have calcian–marialite compositions, which range from 27 to 47 Me % and XCl contents of 0.37–0.50 a.p.f.u. The anorthite equivalent (31–46 EqAn %) of the scapolites overlaps with that of coexisting plagioclase (21–48 XAn %). The composition of scapolite is similar to that of the Copperbelt region of Zambia, where there is documented evidence of evaporite horizons. Moderate to high NaCl salinities, which range from 0.2–0.5 mol, and high contents of Cl in scapolite indicate that metamorphism in the belt was accompanied by metasomatic introduction of NaCl-rich fluids, which were derived from evaporite horizons that existed in the metasedimentary succession in the belt. This study shows that evaporites, from which NaCl-rich fluids were derived, were widespread in the Lufilian–Zambezi belt and played an important role in the metamorphic history of the belt.

In the Nebelstein area, molybdenite-bearing greisens occur together with peraluminous leucogranites. In the compositional change of the granites to the greisens, there is an almost complete loss of Na, combined with a decrease in Ca, Mg, Sr, and Ti concentrations. The progressive alteration is reflected by lower homogenization temperatures and increasing salinity in aqueous fluid inclusions. The fluid regime prior to greisenization was water-dominated with low salt contents, while the early stage of the greisen development was characterized by a mixed fluid containing carbon dioxide and water. This was succeeded by a moderate saline aqueous fluid which caused the mineralization by exchange of metal ions for Na+(Ca2+, K+). A negative correlation between salt content in fluid inclusions and Na2O concentrations in the bulk rocks supports this model. Mass balance calculations for this interaction yield a minimum fluid-rock ratio of approximately 2 : I. Greisenization took place at a minimum pressure of 180 MPa (1.8 kb) and in a temperature range between 200 and < 400 °C.

Production of wood ash has increased strongly in the last ten years due to the increasing popularity of renewable and CO(2)-neutral heat and energy production via wood burning. Wood ashes are rich in many essential plant nutrients. In addition they are alkaline. The idea of using the waste ash as fertiliser in forests is appealing. However, wood is also known for its ability to strongly enrich certain heavy metals from the underlying soils, e.g. Cd, without any anthropogenic input. Concentrations of 26 chemical elements (Ag, As, Au, B, Ba, Ca, Cd, Co, Cr, Cu, Fe, Hg, K, La, Mg, Mn, Mo, Na, Ni, P, Pb, S, Sb, Sr, Ti, and Zn) in 40 samples each of birch and spruce wood ashes collected along a 120 km long transect in southern Norway are reported. The observed maximum concentrations are 1.3 wt.% Pb, 4.4 wt.% Zn and 203 mg/kg Cd in birch wood ashes. Wood ashes can thus contain very high heavy metal concentrations. Spreading wood ashes in a forest is a major anthropogenic interference with the natural biogeochemical cycles. As with the use of sewage sludge in agriculture the use of wood ashes in forests clearly needs regulation.

Andalusite occurs as an accessory mineral in many types of peraluminous felsic igneous rocks, including rhyolites, aplites, granites, pegmatites, and anatectic migmatites. Some published stability curves for And = Sil and the water-saturated granite solidus permit a small stability field for andalusite in equilibrium with felsic melts. We examine 108 samples of andalusite-bearing felsic rocks from more than 40 localities world-wide. Our purpose is to determine the origin of andalusite, including the T-P-X controls on andalusite formation, using eight textural and chemical criteria: size-compatibility with grain sizes of igneous minerals in the same rock; shape-ranging from euhedral to anhedral, with no simple correlation with origin; state of aggregation-single grains or clusters of grains; association with muscovite-with or without rims of monocrystalline or polycrystalline muscovite; inclusions--rare mineral inclusions and melt inclusions; chemical composition-andalusite with little significant chemical variation, except in iron content (0·08-1·71 wt % FeO); compositional zoning--concentric, sector, patchy, oscillatory zoning cryptically reflect growth conditions; compositions of coexisting phases-biotites with high siderophyllite-eastonite contents (Al iv ≈ 2·68 ± 0·07 atoms per formula unit), muscovites with 0·57-4·01 wt % FeO and 0·02-2·85 wt % TiO2, and apatites with 3· 53 ± 0·18 wt % F. Coexisting muscovite-biotite pairs have a wide range of F contents, and FBt = 1·612F Ms + 0·015. Most coexisting minerals have compositions consistent with equilibration at magmatic conditions. The three principal genetic types of andalusite in felsic igneous rocks are: Type 1 Metamorphic-(a) prograde metamorphic (in thermally metamorphosed peraluminous granites), (b) retrograde metamorphic (inversion from sillimanite of unspecified origin), (c) xenocrystic (derivation from local country rocks), and (d) restitic (derivation from source regions); Type 2 Magmatic-(a) peritectic (water-undersaturated, T↑) associated with leucosomes in migmatites, (b) peritectic (water-undersaturated, T↓), as reaction rims on garnet or cordierite, (c) cotectic (water-undersaturated, T↓) direct crystallization from a silicate melt, and (d) pegmatitic (water-saturated, T↓), associated with aplite-pegmatite contacts or pegmatitic portion alone; Type 3 Metasomatic-(water-saturated, magma-absent), spatially related to structural discontinuities in host, replacement of feldspar and/or biotite, intergrowths with quartz. The great majority of our andalusite samples show one or more textural or chemical criteria suggesting a magmatic origin. Of the many possible controls on the formation of andalusite (excess Al2O 3, water concentration and fluid evolution, high Be-B-Li-P, high F, high Fe-Mn-Ti, and kinetic considerations), the two most important factors appear to be excess Al2O3 and the effect of releasing water (either to strip alkalis from the melt or to reduce alumina solubility in the melt). Of particular importance is the evidence for magmatic andalusite in granites showing no significant depression of the solidus, suggesting that the And = Sil equilibrium must cross the granite solidus rather than lie below it. Magmatic andalusite, however formed, is susceptible to supra- or sub-solidus reaction to produce muscovite. In many cases, textural evidence of this reaction remains, but in other cases muscovite may completely replace andalusite leaving little or no evidence of its former existence., La lista completa de autores que integran el documento puede consultarse en el archivo., Centro de Investigaciones Geológicas

The Mesozoic ophiolites in the Eastern Alps are restricted to the Penninic windows: the Lower Engadin Window, Tauern Window and Rechnitz Window Group. The ophiolite sequence starts with serpentinites (harzburgitic chemistry) and some metamorphosed ultramafic cumulates which include rodingites and chloritites. The plutonic section comprises leucogabbros, ferrogabbros and rare plagiogranites. Pillow lavas, where recognizable, massive lava flows, and sometimes tuffs build up the extrusive series. Small bands of radiolarites, cherts and thick calc schists form the sedimentary cover. Ophicarbonates on top of the serpentinites are rare (Rechnitz Window Group). All ophiolites, apart from some oceanic alterations, have undergone a complex history of Alpine regional metamorphism of variable grade (pumpellyite-actinolite facies in the Lower Engadin Window, to greenschist to amphibolite facies in the Tauern Window). Geochemically, the plutonic section can be explained in terms of their Ti, V, Zr and Y concentration reflecting a fractional crystallization sequence with olivine, plagioclase, clinopyroxene, and later ilmenite and magnetite as cumulus phases. The volcanics show mid-ocean ridge basalt affinities. Five groups based on major-element variations can be observed: plag, ol and ilm-mag accumulations, and ol-plag-(cpx) and cpx-ol-plag fractionations. This grouping is also recognized in the trace elements. The variability in Zr/Y ratios within and between the groups can be explained by different degrees of partial melting and slight variation in the mantle source. This complex magmatic history indicates an oceanic ridge environment for the origin of the ophiolites with a structure similar to that of the North Atlantic and low spreading rates. Fracture zones may also play a certain role.

The southeastern Anatolia comprises numbers of tectono-magmatic/ stratigraphic units such as the metamorphic massifs, the ophiolites, the volcanic arc units and the granitoid rocks. All of them play important role for the late Cretaceous evolution of the southern Neotethys. The spatial and temporal relations of these units suggest the progressive development of coeval magmatism and thrusting during the late Cretaceous northward subduction/accretion. Our new U-Pb zircon data from the rhyolitic rocks of the wide-spread volcanic arc unit show ages of (83.1 ± 2.2)-(74.6 ± 4.4) Ma. Comparison of the ophiolites, the volcanic arc units and the granitoids suggest following late Cretaceous geological evolution. The ophiolites formed in a suprasubduction zone (SSZ) setting as a result of northward intra-oceanic subduction. A wide-spread island-arc tholeiitic volcanic unit developed on the top of the SSZ-type crust during 83-75 Ma. Related to regional plate convergence, northward under-thrusting of SSZ-type ophiolites and volcanic arc units was initiated beneath the Tauride platform (Malatya-Keban) and followed by the intrusion of I-type calc-alkaline volcanic arc granitoids during 84-82 Ma. New U-Pb ages from the arc-related volcanic-sedimentary unit and granitoids indicate that under-thrusting of ophiolites together with the arc-related units beneath the Malatya-Keban platform took place soon after the initiation of the volcanic arc on the top of the SSZ-type crust. Then the arc-related volcanic-sedimentary unit continued its development and lasted at ~75 Ma until the deposition of the late Campanian-Maastrichtian shallow marine limestone. The subduction trench eventually collided with the Bitlis-Pütürge massif giving rise to HP-LT metamorphism of the Bitlis massif. Although the development of the volcanic arc units and the granitoids were coeval at the initial stage of the subduction/accretion both tectono-magmatic units were genetically different from each other. © Elsevier B.V. All rights reserved. 106Y231 This work is a part of Ph.D study of Fatih Karaoğlan. Financial support from the TÜBİTAK (Project No. 106Y231 ) and Çukurova University Research Foundation (Project No. MMF2009D11 ) are gratefully acknowledged. The first author acknowledges International Research Fellowship Programme supported by TUBITAK–BİDEB. Ercan Aksoy and Yener Eyüboğlu are thanked for their valuable suggestions that improved the quality of the present paper.

Nicht alle Teile Gros-Wiens konnen direkt von der Ersten oder Zweiten Hochquellenwasserleitung versorgt werden. Fur hoher gelegene Gebiete reicht ihr Leitungsdruck nicht aus, weshalb Pumpwerke erforderlich sind. Manche Randgemeinden sind nicht an das Wiener Wasserleitungsnetz angeschlossen. Diese werden durch eigene Pumpwerke mit Quell- oder Brunnenwasser versorgt.