Stability limits of hydrous minerals in sediment and mid‐ocean ridge basalt compositions: Implications for water transport in subduction zones

Ono, Shigeaki

doi:10.1029/98jb01351

Cited by 232 publications

(178 citation statements)

References 45 publications

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“…The mineral proportion changes in the MORB composition as a function of pressure at subducting slab temperatures (800-1200°C) have been investigated by previous studies (e.g., Irifune et al, 1986;Ono, 1998;Maruyama, 1999, 2004;Aoki and Takahashi, 2004). These studies reported that the M cpx is~0.5-0.7 at about 4 GPa.…”

Section: Connectivity Of Hydrous Liquid In the Eclogite Systemmentioning

confidence: 97%

Morphological stability of hydrous liquid droplets at grain boundaries of eclogite minerals in the deep upper mantle

Matsukage

Hashimoto

Nishihara

2017

Journal of Mineralogical and Petrological Sciences

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The morphological stability of hydrous liquid droplets at grain boundaries of eclogite minerals in the basaltic part of a subducting slab were investigated based on experimental constraints for the dihedral angles. We measured the dihedral angles in the eclogite-H 2 O system at a temperature of 1000°C and at pressures ranging from 4 to 16 GPa. The dihedral angle of hydrous liquid versus garnet-garnet (θ GG-L ) increased with increasing pressure from 46°at 4 GPa to 66°at 12 GPa, although it showed a weak decreasing trend at pressures higher than 12 GPa. The dihedral angle of hydrous liquid versus clinopyroxene-clinopyroxene (θ CC-L ) was almost constant with increasing pressure (61 and 59°at 4 and 10 GPa, respectively). The dihedral angle of hydrous liquid versus garnet-clinopyroxene (θ GC-L ) was 73-76°at 4-10 GPa, and it was always higher than θ GG-L and θ CC-L . By applying the morphological stability criteria for liquid in a system with two solid phases (garnet and clinopyroxene) and bond percolation theory for a three-dimensional lattice of tetracoordination, we found that the hydrous liquid was isolated at the grain edges and corners of eclogite minerals in the cold slab under a wide range of pressure conditions of the upper mantle from 4-14 GPa when the grain size of garnet was equal to that of clinopyroxene. Thus, basaltic crust containing hydrous liquid droplets may carry water to the lowermost upper mantle and the mantle transition zone when the slab is cold.

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Section: Connectivity Of Hydrous Liquid In the Eclogite Systemmentioning

confidence: 97%

Morphological stability of hydrous liquid droplets at grain boundaries of eclogite minerals in the deep upper mantle

Matsukage

Hashimoto

Nishihara

2017

Journal of Mineralogical and Petrological Sciences

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“…Beyond ca. 9 GPa, after dehydration of lawsonite and phengite (Schmidt and Poli 1998;Ono 1998), only few hydrous phases remain stable, for example, topaz-OH and phase egg in peraluminous sediments (Ono 1998) and hydrous alphabet phases in peridotite (Komabayashi et al 2004). With depth, these hydrous phases become minor in abundance, and most of the H 2 O in the subducting slab becomes stored in nominally anhydrous phases .…”

mentioning

confidence: 99%

“…The strategy to study a carbonated water-poor or dry pelite results from the fact that after the reaction of phengite to K-hollandite near 9 GPa (Domanik and Holloway 1998;Ono 1998) hydrous minerals are limited or absent and flush melting (Poli and Schmidt 2002) of sediments assisted by fluids derived from underlying oceanic basalts or serpentinized peridotites is limited to 9 and 6-7 GPa, respectively (Kawamoto et al 1996;Schmidt and Poli 1998). Furthermore, sodium becomes compatible in clinopyroxene at C3.5 GPa , leaving potassium that strongly depresses the solidus temperature of subducted sediments.…”

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confidence: 99%

Melting of carbonated pelites at 8–13 GPa: generating K-rich carbonatites for mantle metasomatism

Grassi

Schmidt

2010

Contrib Mineral Petrol

104

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The melting behaviour of three carbonated pelites containing 0-1 wt% water was studied at 8 and 13 GPa, 900-1,850°C to define conditions of melting, melt compositions and melting reactions. At 8 GPa, the fluidabsent and dry carbonated pelite solidi locate at 950 and 1,075°C, respectively; [100°C lower than in carbonated basalts and 150-300°C lower than the mantle adiabat. From 8 to 13 GPa, the fluid-present and dry solidi temperatures then increase to 1,150 and 1,325°C for the 1.1 wt% H 2 O and the dry composition, respectively. The melting behaviour in the 1.1 wt% H 2 O composition changes from fluid-absent at 8 GPa to fluid-present at 13 GPa with the pressure breakdown of phengite and the absence of other hydrous minerals. Melting reactions are controlled by carbonates, and the potassium and hydrous phases present in the subsolidus. The first melts, which composition has been determined by reverse sandwich experiments, are potassium-rich Ca-FeMg-carbonatites, with extreme K 2 O/Na 2 O wt ratios of up to 42 at 8 GPa. Na is compatible in clinopyroxene with D cpx=carbonatite Na ¼ 10À18 at the solidus at 8 GPa. The melt K 2 O/Na 2 O slightly decreases with increasing temperature and degree of melting but strongly decreases from 8 to 13 GPa when K-hollandite extends its stability field to 200°C above the solidus. The compositional array of the sediment-derived carbonatites is congruent with alkali-and CO 2 -rich melt or fluid inclusions found in diamonds. The fluid-absent melting of carbonated pelites at 8 GPa contrasts that at B5 GPa where silicate melts form at lower temperatures than carbonatites. Comparison of our melting temperatures with typical subduction and mantle geotherms shows that melting of carbonated pelites to 400-km depth is only feasible for extremely hot subduction. Nevertheless, melting may occur when subduction slows down or stops and thermal relaxation sets in. Our experiments show that CO 2 -metasomatism originating from subducted crust is intimately linked with K-metasomatism at depth of [200 km. As long as the mantle remains adiabatic, lowviscosity carbonatites will rise into the mantle and percolate upwards. In cold subcontinental lithospheric mantle keels, the potassic Ca-Fe-Mg-carbonatites may freeze when reacting with the surrounding mantle leading to potassium-, carbonate/diamond-and incompatible element enriched metasomatized zones, which are most likely at the origin of ultrapotassic magmas such as group II kimberlites.

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“…Various studies have been conducted to date to clarify the stability of hydrous phases in peridotitc, basalt, and sediment compositions at high pressure and temperature [e.g., Schmidt and Poll, 1998; Ono, 1998]. …”

Section: Introductionmentioning

confidence: 99%

Stability field of new hydrous phase, δ‐AlOOH, with implications for water transport into the deep mantle

Ohtani¹,

Litasov²,

Suzuki³

et al. 2001

Geophysical Research Letters

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Abstract. We report stability field of a new hydrous phase b-A1OOH, which is a high pressure polymorph of diaspore. This phase is stable at pressures from 17 GPa to at least up 25 GPa at around 1000 to 1200øC, which are likely conditions expected in the slabs descending into the lower mantle. This phase contains significant amounts of octahedrally coordinated Mg and Si in solid solution. The oxygen arrangement of 6-A1OOH is similar to that of the post-stishovite phase, CaC12 type SiO2, which exists in the deep lower mantle. 6-A1OOH may play an important role as a water reservoir in subducting slabs. introductionWater We have synthesized a new ultrahigh pressure phase of aluminium oxide hydoxide 6-AIOOH in the pressure range above 17 GPa. This phase is iso-strucutral with some hydrous phases such as 6-FeOOH and I•-CrOOH. It has a calculated density of 3.533g/era 3 which is about 4.5% and 15% greater than that of diaspore and boehmite, low pressure polymorphs of AIOOH, respectively. The detailed results of analysis of its crystal structure are given in Suzula' et al. [2000]. It is noteworthy that the framework of oxygen packing of 6-AIOOH is almost identical to the CaCI 2 structure, i.e., the distorted rutile structure. The crystal structures of 6-AIOOH and CaCI2 type of SiO2 are schematically shown in Figure 1, which clearly depicts their structural similarity. In this study we have investigated the stability field of 6-AIOOH at high pressure and temperature and discuss the importance of this phase in transportation of water into the deep mantle.•Institute of Mnieralogy, Petrology, and Economic Geology,

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Stability limits of hydrous minerals in sediment and mid‐ocean ridge basalt compositions: Implications for water transport in subduction zones

Cited by 232 publications

References 45 publications

Morphological stability of hydrous liquid droplets at grain boundaries of eclogite minerals in the deep upper mantle

Morphological stability of hydrous liquid droplets at grain boundaries of eclogite minerals in the deep upper mantle

Melting of carbonated pelites at 8–13 GPa: generating K-rich carbonatites for mantle metasomatism

Stability field of new hydrous phase, δ‐AlOOH, with implications for water transport into the deep mantle

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