The phase boundary between CaSiO3 perovskite and Ca2SiO4 + CaSi2O5 determined by in situ X‐ray observations

Sueda, Yuichiro; Irifune, Tetsuo; Yamada, Akihiro; Inoue, Toru; Liu, Xi; Funakoshi, Kengo

doi:10.1029/2006gl025772

Cited by 14 publications

(8 citation statements)

References 19 publications

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“…Some recent works point out its presence in alkaline silica-undersaturated rocks associations (Ruberti et al, 2012) and ijolites from Prairie Lake Carbonatite Complex (Canada) (Zurevinski and Mitchell, 2015). Wollastonite (CaSiO 3 ) is a low-pressure precursor of Ca-perovskites (Sueda et al, 2006). In our experiments, after Di crystallization to consume all available magnesium in the liquid, wollastonite is the natural Ca-rich crystallized phase.…”

Section: Experiments Tºcmentioning

confidence: 71%

Study of silica-undersaturated magmas through the Kalsilite- Nepheline-Diopside-Silica system at 4.0 GPa and dry conditions

Souza

Conceição

Cedeño

et al. 2018

Geol. USP. Sér. cient.

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This study experimentally investigates the Kalsilite-Nepheline-Diopside-Silica system at high pressure and temperature, with emphasis on silica-undersaturated volume (leucite-nepheline-diopside -Lct-Nph-Di; and kalsilite-nepheline-diopside -Kls + Nph + Di -planes), at 4.0 GPa (~120 km deep), temperatures up to 1,400ºC and dry conditions, to better understand the influence of K 2 O, Na 2 O, and CaO in alkali-rich silica-undersaturated magma genesis. In the Lct-Nph-Di plane, we determined the stability fields for kalsilite (Kls ss ), nepheline (Nph ss ) and clinopyroxene (Cpx ss ) solid solutions, wollastonite (Wo) and sanidine (Sa); and three piercing points: (i) pseudo-eutectic Kls + Nph + Di + liquid (Lct 62 Nph 29 Di 9 ) at 1,000ºC; (ii) Kls + Sa + (Di + Wo) + liquid (Lct 75 Nph 22 Di 2 ) at 1,200ºC; and (iii) pseudo-eutectic Kls + Di + Wo + liquid (Lct 74 Nph 17 Di 9 ) at 1,000ºC. Kalsilite stability field represents a thermal barrier between ultrapotassic/potassic vs. sodic compositions. In the plane Kls-Nph-Di, we determined the stability fields for Kls ss , Nph ss and Cpx ss and two aluminous phases in smaller proportions: spinel (Spl) and corundum (Crn). This plane has a piercing point in Kls + Nph + Di(± Spl) + liquid (Kls 47 Nph 43 Di 10 ) at 1,100ºC. Our data showed that pressure extends K dissolution in Nph (up to 39 mol%) and Na in Kls (up to 27 mol%), and that these solid solutions, if present, determinate how much enriched in K and Na an alkaline magma will be in an alkaline-enriched metasomatic mantle. Additionally, we noted positive correlation between K 2 O and SiO 2 concentration in experimental melts, negative correlation between CaO and SiO 2 , and no evident correlation between Na 2 O and SiO 2 .Keywords: Experimental petrology; Alkaline rocks; Potassium; Mantle. ResumoEste trabalho trata do estudo experimental do sistema kalsilita-nefelina-diopsídio-sílica em condições mantélicas, com ên-fase em sua parte subsaturada em sílica (planos leucita-nefelina-diopsídio -Lct-Nph-Di; e kalsilita-nefelina-diopsídio -Kls + Nph + Di), a 4 GPa (profundidade de aproximadamente 120 km), até 1.400ºC em condições anidras. O objetivo é melhor compreender como K 2 O, Na 2 O e CaO influenciam a gênese de magmas ricos em álcalis e subsaturados em sílica. Para o plano Lct-Nph-Di, foram determinados campos de estabilidade para as soluções sólidas kalsilita (Kls ss ), nefelina (Nph ss ) e clinopiroxênios (Cpx ss ), além de wollastonita (Wo) e sanidina (Sa). Foram também definidos os pontos invariantes: (i) pseudoeutético Kls+Nph+Di+líquido (Lct 62 Ne 29 Di 9 ) a 1.000ºC; (ii) Kls + Sa + (Di + Wo) + líquido (Lct 75 Nph 22 Di 2 ) a 1.200ºC; (iii) pseudoeutético Kls + Di + Wo + líquido (Lct 74 Nph 17 Di 9 ) a 1.000ºC. O campo da kalsilita, nesse diagrama, representa um alto termal entre os extremos composicionais potássico/ultrapotássico vs. sódico. No plano Kls-Nph-Di, encontramos campos de estabilidade para Kls ss , Nph ss e Cpx ss , além de pequenas quantidades de espinélio (Spl) e coríndon (Crn) e um ponto...

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Section: Experiments Tºcmentioning

confidence: 71%

Study of silica-undersaturated magmas through the Kalsilite- Nepheline-Diopside-Silica system at 4.0 GPa and dry conditions

Souza

Conceição

Cedeño

et al. 2018

Geol. USP. Sér. cient.

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“…Multi-anvil experimental data: G94, Gasparik et al (1994) ( 9 ); LHDAC experimental data: SL95, Shen and Lazor (1995) ( 7 ) and Z97, Zerr et al (1997) ( 10 ); and previous computational data based on ab initio calculations: BS19, Braithwaite and Stixrude (2019) ( 11 ); WS21, Wilson and Stixrude (2021) ( 12 ); and H22, Hernandez et al (2022) ( 13 ). Black lines display the phase transition boundaries of solid phases below 13 GPa ( 9 , 16 , 17 ).…”

Section: Resultsmentioning

confidence: 99%

“…At ambient conditions, calcium silicate CaSiO 3 is stable in the form of wollastonite. After a series of solid-solid phase transitions underwent at pressures below ~13 GPa, it transforms into a perovskite phase ( 9 , 16 , 17 ). At low temperature (below ~1000 K), the perovskite phase has a tetragonal structure.…”

Section: Introductionmentioning

confidence: 99%

Davemaoite as the mantle mineral with the highest melting temperature

Yin,

Belonoshko,

et al. 2023

Sci. Adv.

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Knowledge of high-pressure melting curves of silicate minerals is critical for modeling the thermal-chemical evolution of rocky planets. However, the melting temperature of davemaoite, the third most abundant mineral in Earth’s lower mantle, is still controversial. Here, we investigate the melting curves of two minerals, MgSiO 3 bridgmanite and CaSiO 3 davemaoite, under their stability field in the mantle by performing first-principles molecular dynamics simulations based on the density functional theory. The melting curve of bridgmanite is in excellent agreement with previous studies, confirming a general consensus on its melting temperature. However, we predict a much higher melting curve of davemaoite than almost all previous estimates. Melting temperature of davemaoite at the pressure of core-mantle boundary (~136 gigapascals) is about 7700(150) K, which is approximately 2000 K higher than that of bridgmanite. The ultrarefractory nature of davemaoite is critical to reconsider many models in the deep planetary interior, for instance, solidification of early magma ocean and geodynamical behavior of mantle rocks.

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“…Hence, hydrous carbonate-silicate melt (or supercritical fluid) can be obtained from subducted sediment, if the temperature of the slab is not high and does not prevent hydrous silicate (lawsonite and phengite) transport to great depths. Such conditions are characteristic of cold subducted slabs (Syracuse et al, 2010).…”

Section: Breyite Crystallization Under Hydrous Conditionsmentioning

confidence: 99%

“…Kanzaki et al (1991) observed breyite decomposition to larnite (Ca 2 SiO 4 ) and titanitestructured CaSi 2 O 5 at 12 GPa and 1500 • C. This reaction was studied in detail by Kubo et al (1997) and Akaogi et al (2004). Sueda et al (2006) experimentally demonstrated that the larnite + CaSi 2 O 5 assemblage transforms to CaSiO 3 perovskite at a pressure of ∼ 14 GPa. Gasparik et al (1994) determined the melting temperatures of CaSiO 3 polymorphs at pressures of 8-16 GPa.…”

Section: Introductionmentioning

confidence: 97%

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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The phase boundary between CaSiO₃ perovskite and Ca₂SiO₄ + CaSi₂O₅ determined by in situ X‐ray observations

Cited by 14 publications

References 19 publications

Study of silica-undersaturated magmas through the Kalsilite- Nepheline-Diopside-Silica system at 4.0 GPa and dry conditions

Study of silica-undersaturated magmas through the Kalsilite- Nepheline-Diopside-Silica system at 4.0 GPa and dry conditions

Davemaoite as the mantle mineral with the highest melting temperature

Breyite inclusions in diamond: experimental evidence for possible dual origin

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