Carbonated sediment–peridotite interaction and melting at 7.5–12GPa

Bulatov, Vasily V.; Brey, Gerhard P.; Гирнис, А. В.; Gerdes, Axel; Höfer, Heidi E.

doi:10.1016/j.lithos.2014.05.010

Cited by 39 publications

(34 citation statements)

References 83 publications

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“…The ZrSiO 4 phases from the 12-GPa experiments differ from the lower-pressure zircons by their very high TiO 2 contents (2-6 vs. <0.1 wt%, Supplementary Table A1). Bulatov et al (2014) reported similar high-Ti ZrSiO 4 from high-pressure experiments on sediment-peridotite interaction and attributed this to the zircon-reidite phase transition (Ono et al 2004).…”

Section: Zrsiomentioning

confidence: 72%

“…Like for our previous experiments on sediment-peridotite interaction (Bulatov et al 2014), two starting materials with different K 2 O/Na 2 O ratios were used (Table 1). One composition [referred to as Na-gloss and equivalent to the GLOSS mixture of Bulatov et al (2014)] was identical in major element proportions to GLOSS. In the other, K 2 O was increased at the expense of Na 2 O [hereafter, K-gloss and identical to GLOSS −Na of Bulatov et al (2014)].…”

Section: Experimental and Analytical Methodsmentioning

confidence: 99%

“…One composition [referred to as Na-gloss and equivalent to the GLOSS mixture of Bulatov et al (2014)] was identical in major element proportions to GLOSS. In the other, K 2 O was increased at the expense of Na 2 O [hereafter, K-gloss and identical to GLOSS −Na of Bulatov et al (2014)]. The choice of two materials with different K/Na values takes into account Table 1 Major element compositions of global subducting sediments estimated by Plank and Langmuir (1998) and Plank (2014) and starting materials (Na-gloss and K-gloss) used in our experiments, wt%…”

Section: Experimental and Analytical Methodsmentioning

confidence: 99%

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Reduced sediment melting at 7.5–12 GPa: phase relations, geochemical signals and diamond nucleation

Brey

Гирнис

Bulatov

et al. 2015

Contrib Mineral Petrol

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garnet. Clinopyroxene stability depends strongly on the Na content in the starting mixture; it remains in the Na-gloss composition up to 1600 °C at 12 GPa, but was not observed in K-gloss experiments above 1200 °C. The composition of melt or fluid changes gradually with increasing temperature from hydrous carbonate-rich (<10 wt% SiO 2 ) at 800-1000 °C to volatile-rich silicate liquids (up to 40 wt% SiO 2 ) at high temperatures. Trace elements were analyzed in melts and crystalline phases by LA ICP MS. The garnetmelt and clinopyroxene-melt partition coefficients are in general consistent with results from the literature for volatile-free systems and silicocarbonate melts derived by melting carbonated peridotites. Most trace elements are strongly incompatible in kyanite and silica polymorphs (D < 0.01), except for V, Cr and Ni, which are slightly compatible in kyanite (D > 1). Aragonite and Fe-Mg carbonate have very different REE partition coefficients (D Mst-Sd/L ~ 0.01 and D Arg/L ~ 1). Nb, Ta, Zr and Hf are strongly incompatible in both carbonates. The bearthite/melt partition coefficients are very high for LREE (>10) and decrease to ~1 for HREE. All HFSE are strongly incompatible in bearthite. In contrast, Ta, Nb, Zr and Hf are moderately to strongly compatible in ZrSiO 4 and TiO 2 phases. Based on the obtained partition coefficients, the composition of a mobile phase derived by sediment melting in deep subduction zones was calculated. This phase is strongly enriched in incompatible elements and displays a pronounced negative Ta-Nb anomaly but no Zr-Hf anomaly. Although all experiments were conducted in the diamond stability field, only graphite was observed in low-temperature experiments. Spontaneous diamond nucleation and the complete transformation of graphite to diamond were observed at temperatures above 1200-1300 °C. We speculate that the observed character of graphite-diamond transformation is controlled by relationships between the kinetics of metastable graphite Abstract Melting of carbonated sediment in the presence of graphite or diamond was experimentally investigated at 7.5-12 GPa and 800-1600 °C in a multianvil apparatus. Two starting materials similar to GLOSS of Plank and Langmuir (Chem Geol 145:325-394, 1998) were prepared from oxides, carbonates, hydroxides and graphite. One mixture (Na-gloss) was identical in major element composition to GLOSS, and the other was poorer in Na and richer in K (K-gloss). Both starting mixtures contained ~6 wt% CO 2 and 7 wt% H 2 O and were doped at a ~100 ppm level with a number of trace elements, including REE, LILE and HFSE. The near-solidus mineral assemblage contained a silica polymorph (coesite or stishovite), garnet, kyanite, clinopyroxene, carbonates (aragonite and magnesite-siderite solid solution), zircon, rutile, bearthite and hydrous phases (phengite and lawsonite at <9 GPa and the hydrous aluminosilicates topaz-OH and phase egg at >10 GPa). Hydrous phases disappear at ~900 °C, and carbonates persist up to 1000-1100 °C. At temperatures >1200 °C, the ...

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Section: Zrsiomentioning

confidence: 72%

Section: Experimental and Analytical Methodsmentioning

confidence: 99%

Section: Experimental and Analytical Methodsmentioning

confidence: 99%

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Reduced sediment melting at 7.5–12 GPa: phase relations, geochemical signals and diamond nucleation

Brey

Гирнис

Bulatov

et al. 2015

Contrib Mineral Petrol

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“…Sufficient time must have elapsed to develop high 87 Sr/ 86 Sr ratios before this source was tapped early in the Earth's history to provide the metasomatizing agent. The source may have been subducted carbonated pelites or carbonated peridotite, with magnesite and alkali carbonates derived from melts subducted carbonated pelites (Foley, 2010;Grassi and Schmidt, 2011;Bulatov et al, 2014) or from seafloor altered basalts (carbonate bearing eclogites). Any of these sources would provide the requisite parent-daughter isotope fractionations and observed isotopic compositions.…”

Section: The Ancient Character Of the Metasomatic Agent And Its Sourcmentioning

confidence: 99%

Ancient mantle metasomatism recorded in subcalcic garnet xenocrysts: Temporal links between mantle metasomatism, diamond growth and crustal tectonomagmatism

Shu

Brey

2015

Earth and Planetary Science Letters

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“…This implies that a CO 2 -rich gas phase is absent, and diamond will remain stable in both metasediment and peridotite. Interaction of metasediment-derived melt with peridotite will result in reduction accompanied by Fe and Mg transfer from peridotite to melt and SiO 2 transfer from melt to peridotite (Bulatov et al, 2014). If the melt is saturated in diamond (melt is derived in a diamond-bearing metasediment), its reduction will immediately result in diamond crystallization.…”

Section: Breyite Crystallization Under Hydrous Conditionsmentioning

confidence: 99%

Breyite inclusions in diamond: experimental evidence for possible dual origin

et al. 2020

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Inclusions of breyite (previously known as walstromite-structured CaSiO 3 ) in diamond are usually interpreted as retrogressed CaSiO 3 perovskite trapped in the transition zone or the lower mantle. However, the thermodynamic stability field of breyite does not preclude its crystallization together with diamond under uppermantle conditions (6-10 GPa). The possibility of breyite forming in subducted sedimentary material through the reaction CaCO 3 + SiO 2 = CaSiO 3 + C + O 2 was experimentally evaluated in the CaO-SiO 2 -C-O 2 ± H 2 O system at 6-10 GPa, 900-1500 • C and oxygen fugacity 0.5-1.0 log units below the Fe-FeO (IW) buffer. One experimental series was conducted in the anhydrous subsystem and aimed at determining the melting temperature of the aragonite-coesite (or stishovite) assemblage. It was found that melting occurs at a lower temperature (∼ 1500 • C) than the decarbonation reaction, which indicates that breyite cannot be formed from aragonite and silica under anhydrous conditions and an oxygen fugacity above IW -1. In the second experimental series, we investigated partial melting of an aragonite-coesite mixture under hydrous conditions at the same pressures and redox conditions. The melting temperature in the presence of water decreased strongly (to 900-1200 • C), and the melt had a hydrous silicate composition. The reduction of melt resulted in graphite crystallization in equilibrium with titanite-structured CaSi 2 O 5 and breyite at ∼ 1000 • C. The maximum pressure of possible breyite formation is limited by the reaction CaSiO 3 + SiO 2 = CaSi 2 O 5 at ∼ 8 GPa. Based on the experimental results, it is concluded that breyite inclusions found in natural diamond may be formed from an aragonite-coesite assemblage or carbonate melt at 6-8 GPa via reduction at high water activity. Published by CopernicusPublications on behalf of the European mineralogical societies DMG, SEM, SIMP & SFMC. A. B. Woodland et al.: Breyite inclusions in diamond

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Carbonated sediment–peridotite interaction and melting at 7.5–12GPa

Cited by 39 publications

References 83 publications

Reduced sediment melting at 7.5–12 GPa: phase relations, geochemical signals and diamond nucleation

Reduced sediment melting at 7.5–12 GPa: phase relations, geochemical signals and diamond nucleation

Ancient mantle metasomatism recorded in subcalcic garnet xenocrysts: Temporal links between mantle metasomatism, diamond growth and crustal tectonomagmatism

Breyite inclusions in diamond: experimental evidence for possible dual origin

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