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Abstract: The dunite bodies, which extend as the direction of W-E, are exposed to the southeast of Elaz?g located within the Eastern Taurus Belt of Turkey. Mafic-Ultramafic section in the Guleman ophiolite consists of dunite which containing disseminated chromites, wehrlite, gabbros (isotrope gabbro and layered gabbro) and clinopyroxenite. Dunite blocks above the harzburgite massif have irregular contacts with the enclosing peridotites. Dunite blocks are generally around a few of meters. Dunite blocks consist of gabbro and pyroxenite patches. The origin of dunite blocks are belong to the transition zone of harzburgitic ophiolites which is located at the base of the mafic layered section. They are entirely or largely magmatic formed by olivine and chromite ponds at the base of the crustal magma chamber. The rather around of rock pieces within dunite bodies are foliated such as features have been ascribed to the ophiolite being impregnated by and reacting with a melt. Rocks in the bodies show depleted in incompatible trace elements such as Ba, Nbet al., characteristic of subduction related magma. Furthermore, the high LREE/HREE and high Rb/Th ratios indicates a mantle that has been enrichmented by subduction. As a result, isotopic data, petrographic and geochemical of bodies’s result suggest a parental magma derived from an enrichmed source of subduction zone. A few meters of the large dunite bodies, and ascribes to the central dunites a cumulative origin by fractionation from a picritic melt.
Key words: Neotethyan, Turkey, dnite bodies, subduction zone, ophiolite, geochemistry.
1. Introduction
Anatolia comprises a significant part of the Alpine-Himalayan folded belt, which is one of the most remarkable collision zones on the earth. The Neotethies ocean opened in the Triassic and closed in the Upper Cretaceous, played a significant part in the evolution of Turkey [1, 2]. The remnants of Neotethys, in a structurally descending order are characterized by ophiolites, metamorphic soles and ophiolitic melanges. These ophiolites and related subduction accretion units were generated during the closing stages of the Neotethys oceanic basins in the Late Cretaceous [1]. Well-preserved Neotethys ophiolites in Turkey are subduction zone type [1-6] and display a consistent sequence of events during their formation and emplacement (Fig. 1).
Late Cretaceous ophiolites in Turkey are located in five zones which are from north to south, (1) Pontide ophiolite, (2) Anatolian ophiolite belt, (3) Tauride ophiolite belt, (4) Southeast Anatolian ophiolites and(5) The peri-Arabian platform ophiolites [1].
The Guleman ophiolite is one of southeast Anatolian ophiolites and the best preserved Neotethies oceanic lithospheric remnants in southeast Turkey.
Recent field studies on ophiolites (examples: Tulameen complex in British Columbia, Trinity) [7, 8]. The petrological and geochemical studies of Brouxel et al. [8, 10] mapped in detailed the ultramafics which in the China Mountain-Mt Eddy Quadrangle within the frame of petrological and geochemical study are supported. Boudier and co-workers [7, 11, 12] covered structurally the entire masif. They support Lindsley-Griffin’s conclusion about the ophiolitic association of the mafic and ultramafic sections. Ref.[13] shows the same discrepancy between mafic-ultramafic section of the ophiolites.
They tend to consider them as independent intrusions and surrounded by peridotites. Dunite bodies within the Guleman ophiolite consist of serpantinit,gabbro, clinopyroxenite around a dunite core. These bodies are emplacemented by faulting in the magma chamber or are tectonically emplacemented of ophiolite. As magma crystallizes and differentiates, cyclically layered sequences form [14]. An ideal cycle is consisted of basal dunite followed upward by a harzburgite or ortopyroxene layer [15]. These cyclic units vary in thickness. For example, in the Bushveld complex they are present on a milimetre scale, at Great Dyke on centimetre scale [15]. Olivine composition of this complexs ranges of Fo 77 and Fo 35. The specific characters of them show that they formed along an environment similar to a modern island arc or a back arc basin as proposed by Yodogzinski et al. [16, 17]. This paper aims to present petrographical and geochemical properties of dunite bodies.
2. Geological Background
The Guleman ophiolite is one of the best southeast Turkey ophiolites and is exposed to the northeast of Maden and the east of Hazar Lake. It is thrust over by the well-exposed sedimentary succession of the Hazar Group, Maastrichtian-Paleocene in age [17-19]. The Guleman ophiolite comprises mantle tectonites and ultramafic to mafic cumulates, layered gabbros, isotrope gabbros, plagiogranite, klinopyroxenite. Diabase dikes cut through the above mentioned rocks at different structural levels [18] determined the age by Ar-Ar dating in plagioclase 72.4 Ma for Guleman ophiolite. In outside of study area, the Guleman ophiolite covers Maden complex (Middle Eocene) tectonically (Fig. 2). Middle Eocene Maden complex uncomformably overlies the Hazar Group. The Maden complex comprises mudstone, sandstone, lots of limestone olistolithes, agglomerate, basaltic and andesitic lavas. The Hazar groupe (Upper Meastrichtian-Middle Eocene) is largely comprised of siltstone, limestone, sandstone, claystone and marl.
3. Analytical Tchniques
Major and trace element analyse of nine samples from dunite bodies is given in Table 1. Samples were carried out at AAL (Acme Analitical Laboratories) in Canada [18]. A total of 2 g of powdered sample was mixed with 0.9 g of wax, the mixture was pressed at 20 N in a automatic pres machine to get a pressed disc. REE (rare earth element) analyses of 9 samples were performed using ICP-MS (iductively coupled plasma-mass spectrometry) following a LiBO2 fusion and dilute nitric digestion on representative powders. Plagioclases were seperated from the gabro sample(Table 2), which has very fresh and chemically homogeneous grains. Geochronology of plagioclase was undertaken by laser 40Ar/39Ar dating (Fig. 3).
4. Petrography
The Guleman ophiolite comprises mantle tectonites and ultramafic to mafic cumulates, layered gabbros, isotrope gabbros, throctolite, plagiogranite and Klinopyroxenite. Diabase dikes cut through the above mentioned rocks at different structural levels. Mantle tectonites are more than 4 km thick and form at least 60% of the whole ophiolite body [6]. They are dominated by harzburgites which contain dunite and podiform chromite, generally 0.5-10 m in thick [20]. The mantle tectonites are gradually overlain by layered cumulates, which starts with dunites containing disseminated and banded chromites, followed by alternations of gabbros, wehrlite and clinopyroxenite.
The gabbroic level is represented by throctolite, layered gabbro, isotrope gabbros and plagiogranite. The transition between layered gabbro or foliated gabbro and isotropic gabbros in posibility ophiolites show that it is difficult to draw a line between them. The layered gabbros progressively lose their layering and grade into poorly foliated gabro, where it is enrichment on favor of pyroxenes. The isotropic gabbros are characterized by agreat heterogenity in grain size. The gabbros exhibit adcumulate and heteradcumulate textures suggesting a slow rate of crystallization [20, 21]. The products of anatexis are leucocratic tonalites and plagiogranites which invade the gabbros as a dike or vein-like network and locally dismember them into a magmatic breccia. Distinguishing plagiogranites produce by this anatexis from others ascribed to the crystallization of highly evolved melt at the top of the chamber [22, 23]. A sheeted-dike complex in the Guleman ophiolite was not preserved, possibly because of erosion after emplacement [18, 19]. Dunite bodies such as transition zone characteristic below the layered gabbros and above mantle tectonites. These bodies having approximatelly 1.5-2 m size which comprises clinopyroxenite around dunite core, serpantinized harzburgite and gabbros (Fig. 4a). The rocks of bodies characterized by well fabrics (Fig. 4b) are found in random orientations within apparently cumulates gabbbro and dunite core from the base of the magma chamber (such as trinity ophiolite) [10, 24]. The rather around of rock pieces within dunite bodies are foliated(Fig. 5). In the gabbros diffuse aggregates of feldspar and clinopyroxene are observed. Such features have been ascribed to the ophiolite being impregnated by and reacting with a melt [24, 25]. Another characteristic of dunite bodies is including rich in Mg-silicate rocks. Serpentinite and forsteritic olivine are common silicates with high magnesium contents. The dunite core of Fo-olivine riches consists of diopsitic augite and chromite. Alteration products comprise carbonate, magnetite and talc (Fig. 6).
The clinopyroxenite around of dunitic core is medium to coarse grained and has black green clinopyroxene and partialy serpentinized olivine. The clinopyroxenites commonly exhibit mineral foliations. Magnetite is very found as a blotchy. It is suggested that possibly oxidation of the magma chamber. The gabbros within dunite bodies comprises of plagioclase, clinopyroxene and accessory chlorite (Fig. 6). Fluids made chemical remobilization of minerals and it caused sosuritization of plagioclase, kaolinitization of feldispar.
References
[1] A.H.F. Robertson, Overview of the genesis and emplacement of Mesozoic ophiolites in the Eastern Mediterranean Tethyan region, Lithos. 65 (2002) 1-67.
[2] A.M.C. ?eng?r, Y. Y?lmaz, Tethyan evolution of Turkey: In terms of plate tectonics is a custom array of geosciences, in: Geology Conference of Turkey, No.1, Ankara, 1983.
[3] U. Bajc?, O. Parlak, Petrology of the Tekirova (Antalya) ophiolite (Southern Turkey): Evidence for diverse magma generations and their tectonic implications during Neotethyan subduction, International Journal of Earth Sciences 98 (2) (2009) 387-405.
[4] O. Parlak, Geochemistry and geochronology of the Mersin ophiolite within the eastern Mediterranean tectonic frame, Ph.D. Thesis, University of Geneva, Switzerland, 1996.
[5] O. Parlak, V. H?ck, M. Delalove, Suprasubduction zone origin of the Pozant?-Karsant? ophiolite (southern Turkey) deducted from whole rock and mineral chemistry of the gabbroic cumulates, in: E. Bozkurt, J.A. Winchester, J. Piper (Eds.), Tectonics and Magmatism in Turkey and Its Surroundings, Geological Society of London Special Publications 173, 2000, pp. 219-234.
[6] O. Parlak, T. R?zao?lu, U. Ba?c?, F. Karao?lan, V. H?ck, Tectonic significance of the geochemistry and petrology of ophiolites in southeast Anatolia, Turkey, Tectonophysics 473 (1-2) (2008) 173-187.
[7] T.N. Irvine, Layering and related structures in the Duke island and Skaergaard intrusions: Smilarities, differences, and origins, in: I. Parsons (Ed.), Origins of Igneous Layering, NATO ASI Series, 1986, pp. 185-245.
[8] T. Clark, Petrology of the Turnagain ultramafic complex, Northwestern British Columbia, Canadian Journal of Earth Sciences 17 (1980) 744-757.
[9] M. Brouxel, H. Lapierre, Geochemical study of an early Paleozoic island-arc-back-arc basin system, Geol. Soc. Amer. Bull. 100 (1) (1988) 1111-1119.
[10] J.E. Quick, Petrology and petrogenesis of the Trinity peridotite an upper mantle diapir in the eastern Klamath mountains, Northern California, J. Geophys. Res. 86 (1981) 11837-11863.
[11] E. Lesuer, F. Boudier, M. Cannat, G. Ceuleneer, A. Nicolas, The Trinity mafic-ultramafic complex: First results of the structural study of an untypical ophiolite, Ofioliti 9 (1984) 487-498.
[12] F. Boudier, E. Le Sueur, A. Nicolas, Structures in the trinity complex (eastern Klamath mountains), a typical ophiolite, Geol. Soc. Amer. Bull. 101 (1989) 820-833.
[13] C.J. Hawkesworth, J.M. Hergt, F. McDermott, R.M. Ellam, Destructive magrin magmatism and the contributions from the mantle wedge and subducted crust, Austral. J. Earth. Sci. 38 (1991) 577-594.
[14] J.G. Fitton, D. James, W.P. Leeman, Basic magmatism associated with Late Cenozoic extension in the Western United States: Compositional variations in space and time, J. Geophys. Res. 96 (1991) 13693-13711.
[15] R. Hebert, Petrography and mineralogy of oceanic peridotites and gabbros: Some comparisons with ophiolite examples, Ophioliti 2/3 (1982) 299-324.
[16] G.M. Yodogzinski, O.N. Volynets, A.V. Koloskov, N.I. Sel?verstov, V.V. Matvenkov, Magnesian andesites and the subduction component in strongly calc-alkaline series at Piip volcano, far western Aleutians, Journal of Petrology 35 (1993) 163-204.
[17] H. Lapierre, F. Albarede, J. Albers, B. Cabanis, C. Coulon, Early Devonian volcanism in the eastern Klamath Mountains, California: Evidence for an immature island arc, Canad. J. Earth Sci. 22 (1985) 214-227.
[18] M. Abdel-Fattah, E.N. Philip, Cenozoic volcanism in the Middle Easth: Petrogenesis of alkali basalts from northern Lebanon, Geol. Mag. 141 (5) (2004) 545-563.
[19] A.D. Kilic, Examination of Guleman Ophiolite in terms of Magma Chamber Dynamics, Individual Project, Project No. 1538, Elaz??, Turkey, 2007.
[20] A.D. K?l??, Dunite Blocks in mafic-ultramafic sequence: Evidence for magma chamber, in: Tectonic Crossroads Meeting of the Evolving Orogens of Eurasia-Africa-Arabia, Ankara, Turkey, 2010.
[21] Y.Z. ?zkan, ?. ?ztunal?, Petrology of the magmatic rocks of the Guleman ophiolite, in: Int. Symp. on the Taurus Belt, MTA, 1984, pp. 285-293.
[22] G.R. Himmelberg, R.A. Loney, Petrology of ultramafic and gabbroic rocks of the Canyon mountain ophiolite, Oregon, Amer. J. Sci. 280 (1980) 232-268.
[23] N. Chamot-Rooke, X. Le Pichon, Zenisu ridge: Mechanical model of formation, Tectonophysics 117(1989) 205-257.
[24] J.S. Pallister, C.A. Hopson, Samail ophiolite plutonic suite: Field relations, phase variations, cyriptic variation and layering, and a model of a spreading ridge magma chamber, J. Geophys. Res. 86 (1981) 2593-2644.
[25] S.B. Jacobsen, J.E. Quick, G.J. Wasserburg, A Nd and Sr isotopic study of the Trinity peridotite: Implications for mantle evolution, Earth and Planet. Sci. Lett. 68 (1984) 360-378.
[26] A. Edwards, M. Menzies, M. Thirlwall, Evidence from Muriah, Indonesia, for the interplay of supra-subduction zone and interplate processes in the genesis of potassic alkaline magmas, J. Petrol. 32 (3) (1991) 555-592.
[27] D. Elton, J.F. Casey, S. Komor, Cryptic mineral chemistry variations in a detailed traverse through the cumulate ultramafic rocks of the North Arm Mountain masif of the Bay of Islands ophiolite, New found land, Geol. Soc. London Sp. Publ. 13 (1984) 83-97.
[28] D.A. Voormeij, G.J. Simandl, Geological, ocean and mineral CO2 sequestration options: A technical review, Geosci. Can. 31 (1) (2004) 11-22.
[29] H.R. Shaw, The fracture mechanism of magma transport from the mantle to the surface, in: R.B. Hargraves (Ed.), Physics of Magmatic Processes, Princeton Univ. Press, 1980, pp. 201-264.
[30] R.J. Arculus, R. Powel, Source component mixing in the regions of arc magma generation, Journal of Geophysical Research 91 (1986) 5913-5926.
[31] M. Cannat, F. Boudier, Structural study of intra-oceanic thrusting in the Klamath Mountains, northern California: Implications on accretion geotermy, Tectonics 4 (1985) 435-452.
[32] J.A. Pearce, Role of the sub-continental lithosphere in magma genesis at active continental magrin, in: C.J. Hawkesworth, M.J. Norry (Eds.), Continental Basalts and Mantle Xenoliths, Shiva Publishing, Cambridge, 1983, pp. 230-249.
[33] Y. Dilek, A. Polat, Suprasubduction zone ophiolites and Archean tectonics, Geology 36 (2008) 431-435.
[34] R. Hebert, Comparison of the ophiolitic rocks in Cyprus Apennin and ophiolitic rocks in the Quebec and petrology, Ph.D. Thesis, University of Bretagne Occidentale, Brest, 1985.
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[40] Y. Dilek, M.F.J. Flower, Arc-trench rollback and forearc accretion: 2. A model template for ophiolites in Albania, Cyprus, and Oman, in: Y. Dilek, P.T. Robinson (Eds.), Ophiolites in Earth History, Geological Society, Special Publications, London, 2003, pp. 43-68.
Key words: Neotethyan, Turkey, dnite bodies, subduction zone, ophiolite, geochemistry.
1. Introduction
Anatolia comprises a significant part of the Alpine-Himalayan folded belt, which is one of the most remarkable collision zones on the earth. The Neotethies ocean opened in the Triassic and closed in the Upper Cretaceous, played a significant part in the evolution of Turkey [1, 2]. The remnants of Neotethys, in a structurally descending order are characterized by ophiolites, metamorphic soles and ophiolitic melanges. These ophiolites and related subduction accretion units were generated during the closing stages of the Neotethys oceanic basins in the Late Cretaceous [1]. Well-preserved Neotethys ophiolites in Turkey are subduction zone type [1-6] and display a consistent sequence of events during their formation and emplacement (Fig. 1).
Late Cretaceous ophiolites in Turkey are located in five zones which are from north to south, (1) Pontide ophiolite, (2) Anatolian ophiolite belt, (3) Tauride ophiolite belt, (4) Southeast Anatolian ophiolites and(5) The peri-Arabian platform ophiolites [1].
The Guleman ophiolite is one of southeast Anatolian ophiolites and the best preserved Neotethies oceanic lithospheric remnants in southeast Turkey.
Recent field studies on ophiolites (examples: Tulameen complex in British Columbia, Trinity) [7, 8]. The petrological and geochemical studies of Brouxel et al. [8, 10] mapped in detailed the ultramafics which in the China Mountain-Mt Eddy Quadrangle within the frame of petrological and geochemical study are supported. Boudier and co-workers [7, 11, 12] covered structurally the entire masif. They support Lindsley-Griffin’s conclusion about the ophiolitic association of the mafic and ultramafic sections. Ref.[13] shows the same discrepancy between mafic-ultramafic section of the ophiolites.
They tend to consider them as independent intrusions and surrounded by peridotites. Dunite bodies within the Guleman ophiolite consist of serpantinit,gabbro, clinopyroxenite around a dunite core. These bodies are emplacemented by faulting in the magma chamber or are tectonically emplacemented of ophiolite. As magma crystallizes and differentiates, cyclically layered sequences form [14]. An ideal cycle is consisted of basal dunite followed upward by a harzburgite or ortopyroxene layer [15]. These cyclic units vary in thickness. For example, in the Bushveld complex they are present on a milimetre scale, at Great Dyke on centimetre scale [15]. Olivine composition of this complexs ranges of Fo 77 and Fo 35. The specific characters of them show that they formed along an environment similar to a modern island arc or a back arc basin as proposed by Yodogzinski et al. [16, 17]. This paper aims to present petrographical and geochemical properties of dunite bodies.
2. Geological Background
The Guleman ophiolite is one of the best southeast Turkey ophiolites and is exposed to the northeast of Maden and the east of Hazar Lake. It is thrust over by the well-exposed sedimentary succession of the Hazar Group, Maastrichtian-Paleocene in age [17-19]. The Guleman ophiolite comprises mantle tectonites and ultramafic to mafic cumulates, layered gabbros, isotrope gabbros, plagiogranite, klinopyroxenite. Diabase dikes cut through the above mentioned rocks at different structural levels [18] determined the age by Ar-Ar dating in plagioclase 72.4 Ma for Guleman ophiolite. In outside of study area, the Guleman ophiolite covers Maden complex (Middle Eocene) tectonically (Fig. 2). Middle Eocene Maden complex uncomformably overlies the Hazar Group. The Maden complex comprises mudstone, sandstone, lots of limestone olistolithes, agglomerate, basaltic and andesitic lavas. The Hazar groupe (Upper Meastrichtian-Middle Eocene) is largely comprised of siltstone, limestone, sandstone, claystone and marl.
3. Analytical Tchniques
Major and trace element analyse of nine samples from dunite bodies is given in Table 1. Samples were carried out at AAL (Acme Analitical Laboratories) in Canada [18]. A total of 2 g of powdered sample was mixed with 0.9 g of wax, the mixture was pressed at 20 N in a automatic pres machine to get a pressed disc. REE (rare earth element) analyses of 9 samples were performed using ICP-MS (iductively coupled plasma-mass spectrometry) following a LiBO2 fusion and dilute nitric digestion on representative powders. Plagioclases were seperated from the gabro sample(Table 2), which has very fresh and chemically homogeneous grains. Geochronology of plagioclase was undertaken by laser 40Ar/39Ar dating (Fig. 3).
4. Petrography
The Guleman ophiolite comprises mantle tectonites and ultramafic to mafic cumulates, layered gabbros, isotrope gabbros, throctolite, plagiogranite and Klinopyroxenite. Diabase dikes cut through the above mentioned rocks at different structural levels. Mantle tectonites are more than 4 km thick and form at least 60% of the whole ophiolite body [6]. They are dominated by harzburgites which contain dunite and podiform chromite, generally 0.5-10 m in thick [20]. The mantle tectonites are gradually overlain by layered cumulates, which starts with dunites containing disseminated and banded chromites, followed by alternations of gabbros, wehrlite and clinopyroxenite.
The gabbroic level is represented by throctolite, layered gabbro, isotrope gabbros and plagiogranite. The transition between layered gabbro or foliated gabbro and isotropic gabbros in posibility ophiolites show that it is difficult to draw a line between them. The layered gabbros progressively lose their layering and grade into poorly foliated gabro, where it is enrichment on favor of pyroxenes. The isotropic gabbros are characterized by agreat heterogenity in grain size. The gabbros exhibit adcumulate and heteradcumulate textures suggesting a slow rate of crystallization [20, 21]. The products of anatexis are leucocratic tonalites and plagiogranites which invade the gabbros as a dike or vein-like network and locally dismember them into a magmatic breccia. Distinguishing plagiogranites produce by this anatexis from others ascribed to the crystallization of highly evolved melt at the top of the chamber [22, 23]. A sheeted-dike complex in the Guleman ophiolite was not preserved, possibly because of erosion after emplacement [18, 19]. Dunite bodies such as transition zone characteristic below the layered gabbros and above mantle tectonites. These bodies having approximatelly 1.5-2 m size which comprises clinopyroxenite around dunite core, serpantinized harzburgite and gabbros (Fig. 4a). The rocks of bodies characterized by well fabrics (Fig. 4b) are found in random orientations within apparently cumulates gabbbro and dunite core from the base of the magma chamber (such as trinity ophiolite) [10, 24]. The rather around of rock pieces within dunite bodies are foliated(Fig. 5). In the gabbros diffuse aggregates of feldspar and clinopyroxene are observed. Such features have been ascribed to the ophiolite being impregnated by and reacting with a melt [24, 25]. Another characteristic of dunite bodies is including rich in Mg-silicate rocks. Serpentinite and forsteritic olivine are common silicates with high magnesium contents. The dunite core of Fo-olivine riches consists of diopsitic augite and chromite. Alteration products comprise carbonate, magnetite and talc (Fig. 6).
The clinopyroxenite around of dunitic core is medium to coarse grained and has black green clinopyroxene and partialy serpentinized olivine. The clinopyroxenites commonly exhibit mineral foliations. Magnetite is very found as a blotchy. It is suggested that possibly oxidation of the magma chamber. The gabbros within dunite bodies comprises of plagioclase, clinopyroxene and accessory chlorite (Fig. 6). Fluids made chemical remobilization of minerals and it caused sosuritization of plagioclase, kaolinitization of feldispar.
References
[1] A.H.F. Robertson, Overview of the genesis and emplacement of Mesozoic ophiolites in the Eastern Mediterranean Tethyan region, Lithos. 65 (2002) 1-67.
[2] A.M.C. ?eng?r, Y. Y?lmaz, Tethyan evolution of Turkey: In terms of plate tectonics is a custom array of geosciences, in: Geology Conference of Turkey, No.1, Ankara, 1983.
[3] U. Bajc?, O. Parlak, Petrology of the Tekirova (Antalya) ophiolite (Southern Turkey): Evidence for diverse magma generations and their tectonic implications during Neotethyan subduction, International Journal of Earth Sciences 98 (2) (2009) 387-405.
[4] O. Parlak, Geochemistry and geochronology of the Mersin ophiolite within the eastern Mediterranean tectonic frame, Ph.D. Thesis, University of Geneva, Switzerland, 1996.
[5] O. Parlak, V. H?ck, M. Delalove, Suprasubduction zone origin of the Pozant?-Karsant? ophiolite (southern Turkey) deducted from whole rock and mineral chemistry of the gabbroic cumulates, in: E. Bozkurt, J.A. Winchester, J. Piper (Eds.), Tectonics and Magmatism in Turkey and Its Surroundings, Geological Society of London Special Publications 173, 2000, pp. 219-234.
[6] O. Parlak, T. R?zao?lu, U. Ba?c?, F. Karao?lan, V. H?ck, Tectonic significance of the geochemistry and petrology of ophiolites in southeast Anatolia, Turkey, Tectonophysics 473 (1-2) (2008) 173-187.
[7] T.N. Irvine, Layering and related structures in the Duke island and Skaergaard intrusions: Smilarities, differences, and origins, in: I. Parsons (Ed.), Origins of Igneous Layering, NATO ASI Series, 1986, pp. 185-245.
[8] T. Clark, Petrology of the Turnagain ultramafic complex, Northwestern British Columbia, Canadian Journal of Earth Sciences 17 (1980) 744-757.
[9] M. Brouxel, H. Lapierre, Geochemical study of an early Paleozoic island-arc-back-arc basin system, Geol. Soc. Amer. Bull. 100 (1) (1988) 1111-1119.
[10] J.E. Quick, Petrology and petrogenesis of the Trinity peridotite an upper mantle diapir in the eastern Klamath mountains, Northern California, J. Geophys. Res. 86 (1981) 11837-11863.
[11] E. Lesuer, F. Boudier, M. Cannat, G. Ceuleneer, A. Nicolas, The Trinity mafic-ultramafic complex: First results of the structural study of an untypical ophiolite, Ofioliti 9 (1984) 487-498.
[12] F. Boudier, E. Le Sueur, A. Nicolas, Structures in the trinity complex (eastern Klamath mountains), a typical ophiolite, Geol. Soc. Amer. Bull. 101 (1989) 820-833.
[13] C.J. Hawkesworth, J.M. Hergt, F. McDermott, R.M. Ellam, Destructive magrin magmatism and the contributions from the mantle wedge and subducted crust, Austral. J. Earth. Sci. 38 (1991) 577-594.
[14] J.G. Fitton, D. James, W.P. Leeman, Basic magmatism associated with Late Cenozoic extension in the Western United States: Compositional variations in space and time, J. Geophys. Res. 96 (1991) 13693-13711.
[15] R. Hebert, Petrography and mineralogy of oceanic peridotites and gabbros: Some comparisons with ophiolite examples, Ophioliti 2/3 (1982) 299-324.
[16] G.M. Yodogzinski, O.N. Volynets, A.V. Koloskov, N.I. Sel?verstov, V.V. Matvenkov, Magnesian andesites and the subduction component in strongly calc-alkaline series at Piip volcano, far western Aleutians, Journal of Petrology 35 (1993) 163-204.
[17] H. Lapierre, F. Albarede, J. Albers, B. Cabanis, C. Coulon, Early Devonian volcanism in the eastern Klamath Mountains, California: Evidence for an immature island arc, Canad. J. Earth Sci. 22 (1985) 214-227.
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