Partition coefficients of trace elements: Application to volcanic rocks of St. Vincent, West Indies

Dostál, J.; Dupuy, C.; Carron, Jean-Paul; Kerneizon, M. Le Guen de; Maury, René C.

doi:10.1016/0016-7037(83)90275-2

Cited by 160 publications

(45 citation statements)

References 43 publications

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“…Therefore, partial melting of either the lower continental crust or subducted slab would produce magmas with Cu considerably higher than the corresponding sources. The partition coefficients chosen in our modelling are 0.05 for amphibole, 0.5 for plagioclase (Dostal et al 1983), 0.5 for garnet, 0.2 for plagioclase and 1 for rutile. The partition coefficients for Sr, Y are from Rollinson (1993) for plagioclase and Xiong et al (2006) for other minerals (Table 1).…”

Section: Modelling Resultsmentioning

confidence: 99%

The genetic association of adakites and Cu–Au ore deposits

Sun

Zhang

Ling

et al. 2010

International Geology Review

215

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Section: Modelling Resultsmentioning

confidence: 99%

The genetic association of adakites and Cu–Au ore deposits

Sun

Zhang

Ling

et al. 2010

International Geology Review

215

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“…Disruption led to a molten and outgassed IVA source body that contained metallic and silicate liquids stripped of an olivine-rich mantle. Kennedy et al (1993); (3) Jones and Layne (1997); (4) Ulmer (1989); (5) Ewart et al (1973); (6) This study, inferred from Cr-Al co-variation and assuming D Al = 0.043; (7) Mysen (1976); (8) Keleman and Dunn (1992); (9) Weill and McKay (1975); (10) Irving and Frey (1984); (11) Schwandt and McKay (1998); (12) Beattie (1994); (13) Leeman and Scheidegger (1976); (14) Dunn (1987); (15) Klock and Palme (1998); (16) McKay and Weill (1976Weill ( , 1977; (17) Ewart and Griffin (1994); (18) Bougalt and Hekinian (1974); (19) Dostal et al (1983); (20) Duke (1976); (21) Gaetani and Grove (1997); (22) Takahashi (1978); (23) Watson (1977); (24) Paster et al (1974); (25) Villemant et al (1981); (26) Hart and Davis (1978); (27) Beattie (1993); (28) Nielsen et al (1992); (29) Larsen (1979)…”

Section: Discussionmentioning

confidence: 99%

Differentiation and evolution of the IVA meteorite parent body: Clues from pyroxene geochemistry in the Steinbach stony-iron meteorite

Ruzicka

Hutson

2006

Meteoritics &Amp; Planetary Science

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Abstract-We analyzed the Steinbach IVA stony-iron meteorite using scanning electron microscopy (SEM), electron microprobe analysis (EMPA), laser ablation inductively-coupled-plasma mass spectroscopy (LA-ICP-MS), and modeling techniques. Different and sometimes adjacent low-Ca pyroxene grains have distinct compositions and evidently crystallized at different stages in a chemically evolving system prior to the solidification of metal and troilite. Early crystallizing pyroxene shows evidence for disequilibrium and formation under conditions of rapid cooling, producing clinobronzite and type 1 pyroxene rich in troilite and other inclusions. Subsequently, type 2 pyroxene crystallized over an extensive fractionation interval. Steinbach probably formed as a cumulate produced by extensive crystal fractionation (~60-70% fractional crystallization) from a high-temperature (~1450-1490 °C) silicate-metallic magma. The inferred composition of the precursor magma is best modeled as having formed by ≥30-50% silicate partial melting of a chondritic protolith. If this protolith was similar to an LL chondrite (as implied by O-isotopic data), then olivine must have separated from the partial melt, and a substantial amount (~53-56%) of FeO must have been reduced in the silicate magma. A model of simultaneous endogenic heating and collisional disruption appears best able to explain the data for Steinbach and other IVA meteorites. Impact disruption occurred while the parent body was substantially molten, causing liquids to separate from solids and oxygen-bearing gas to vent to space, leading to a molten metal-rich body that was smaller than the original parent body and that solidified from the outside in. This model can simultaneously explain the characteristics of both stony-iron and iron IVA meteorites, including the apparent correlation between metal composition and metallographic cooling rate observed for metal.

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“…From the limited data available, it is not possible to determine the variation of partition coefficients in P-T-X space. The following regression lines are used to relate partition coefficient (K) for a given element between amphibole and melt to absolute temperature (T) using compilations of Arth and Hanson (1975), Pearce and Norry (1979), and Irving (1978) and additional values from Dostal et al (1983) and Irving and Frey (1984) Errors on these values are high but do not affect the principal conclusions. Comparable equations for magnetite, clinopyroxene and Plagioclase are also used, but these have little effect on the La/Sm and Zr/Sm ratios when modeling amphibolite melting.…”

Section: Theoretical Amphibolite Melt Compositionsmentioning

confidence: 99%

Boninite and Harzburgite from Leg 125 (Bonin-Mariana Forearc): A Case Study of Magma Genesis during the Initial Stages of Subduction

Pearce¹,

Laan²,

Arculus³

et al. 1992

Proceedings of the Ocean Drilling Program

290

265

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Holes drilled into the volcanic and ultrabasic basement of the Izu-Ogasawara and Mariana forearc terranes during Leg 125 provide data on some of the earliest lithosphere created after the start of Eocene subduction in the Western Pacific. The volcanic basement contains three boninite series and one tholeiite series. (1) Eocene low-Ca boninite and low-Ca bronzite andesite pillow lavas and dikes dominate the lowermost part of the deep crustal section through the outer-arc high at Site 786. (2) Eocene intermediate-Ca boninite and its fractionation products (bronzite andesite, andesite, dacite, and rhyolite) make up the main part of the boninitic edifice at Site 786. (3) Early Oligocene intermediate-Ca to high-Ca boninite sills or dikes intrude the edifice and perhaps feed an uppermost breccia unit at Site 786. (4) Eocene or Early Oligocene tholeiitic andesite, dacite, and rhyolite form the uppermost part of the outer-arc high at Site 782. All four groups can be explained by remelting above a subduction zone of oceanic mantle lithosphere that has been depleted by its previous episode of partial melting at an ocean ridge. We estimate that the average boninite source had lost 10-15 wt% of melt at the ridge before undergoing further melting (5-10%) shortly after subduction started. The composition of the harzburgite (<2% clinopyroxene, Fo content of about 92%) indicates that it underwent a total of about 25% melting with respect to a fertile MORB mantle. The low concentration of Nb in the boninite indicates that the oceanic lithosphere prior to subduction was not enriched by any asthenospheric (OIB) component.The subduction component is characterized by (1) high Zr and Hf contents relative to Sm, Ti, Y, and middle-heavy REE, (2) light REE-enrichment, (3) low contents of Nb and Ta relative to Th, Rb, or La, (4) high contents of Na and Al, and (5) Pb isotopes on the Northern Hemisphere Reference Line. This component is unlike any subduction component from active arc volcanoes in the Izu-Mariana region or elsewhere. Modeling suggests that these characteristics fit a trondhjemitic melt from slab fusion in amphibolite facies. The resulting metasomatized mantle may have contained about 0.15 wt% water. The overall melting regime is constrained by experimental data to shallow depths and high temperatures (1250°C and 1.5 kb for an average boninite) of boninite segregation. We thus envisage that boninites were generated by decompression melting of a diapir of metasomatized residual MORB mantle leaving the harzburgites as the uppermost, most depleted residue from this second stage of melting. Thermal constraints require that both subducted lithosphere and overlying oceanic lithosphere of the mantle wedge be very young at the time of boninite genesis. This conclusion is consistent with models in which an active transform fault offsetting two ridge axes is placed under compression or transpression following the Eocene plate reorganization in the Pacific. Comparison between Leg 125 boninites and boninites and related rocks e...

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Partition coefficients of trace elements: Application to volcanic rocks of St. Vincent, West Indies

Cited by 160 publications

References 43 publications

The genetic association of adakites and Cu–Au ore deposits

The genetic association of adakites and Cu–Au ore deposits

Differentiation and evolution of the IVA meteorite parent body: Clues from pyroxene geochemistry in the Steinbach stony-iron meteorite

Boninite and Harzburgite from Leg 125 (Bonin-Mariana Forearc): A Case Study of Magma Genesis during the Initial Stages of Subduction

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