The symmetry of garnets on the pyrope (Mg3Al2Si3O12)‐majorite (MgSiO3) join

Parise, John B.; Wang, Yanbin; Gwanmesia, Gabriel D.; Zhang, Jianzhong; Sinelnikov, Yegor; Chmielowski, Josef; Weidner, Donald J.; Liebermann, Robert C.

doi:10.1029/96gl03613

Cited by 39 publications

(12 citation statements)

References 26 publications

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“…X-ray diffraction collected at ambient condition gives the unit-cell volume V 0 = 1,500.43 ± 0.08 Å 3 . This value is about 0.1 % smaller than the values of 1,501.9 ± 0.1 Å 3 and 1,501.4 Å 3 reported by Parise et al (1996) and Sinogeikin and Bass (2000), respectively. Figure 3 shows the roomtemperature unit-cell volumes (V) of pyrope garnet as a function of pressure (P).…”

Section: Room-temperature Equation Of State (Eos)contrasting

confidence: 61%

Thermal equation of state of Mg3Al2Si3O12 pyrope garnet up to 19 GPa and 1,700 K

et al. 2012

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Thermoelastic properties of synthetic Mg 3 Al 2-Si 3 O 12 pyrope garnet have been measured at high pressure and high temperature by using in situ energy-dispersive X-ray diffraction, using a Kawai-type multi-anvil apparatus. Measurements have been conducted up to 19 GPa and 1,700 K, equivalent to the P-T conditions of the middle part of mantle transition zone. Analyses of the room-temperature P-V data to a third-order Birch-Murnaghan (BM) equation of state (EoS) yields: V 0 = 1,500 ± 1 Å 3 , K 0 = 167 ± 6 GPa and K 0 0 = 4.6 ± 0.3. When fitting the entire P-V-T data using a high-temperature Birch-Murnaghan (HTBM) EoS at a fixed K 0 T0 = 4.6, we obtain V 0 = 1,500 ± 2 Å 3 , K T0 = 167 ± 3 GPa, (qK/qT) P = -0.021 ± 0.009 GPa K -1 and a 300 = (2.89 ± 0.33) 9 10 -5 K -1 . Fitting the present data to the Mie-Grüneisen-Debye (MGD) EoS with Debye temperature H 0 = 806 K gives c 0 = 1.19 and 1.15 at fixed q = 1.0 and 1.5, respectively. Comparison of these fittings with two different approaches, we propose to constrain the bulk modulus and its pressure derivative to K 0 = 167 GPa and K 0 0 = 4.4-4.6, as well as the Grüneisen parameter to c 0 = 1.15-1.19.

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Section: Room-temperature Equation Of State (Eos)contrasting

confidence: 61%

Thermal equation of state of Mg3Al2Si3O12 pyrope garnet up to 19 GPa and 1,700 K

et al. 2012

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“… a Italic values indicate estimated by other end‐member with same mineral structure. References, indicated in brackets, are 1, Zhang [1998]; 2, Guyot et al [1996]; 3, Hazen [1976]; 4, Matsui and Manghnani [1985]; 5, Meng et al [1993]; 6, Watanabe [1982]; 7, Graham and Barsch [1969]; 8, Zha et al [1996]; 9, Isaak et al [1989]; 10, Graham et al [1988]; 11, same as forstelite; 12, Sumino [1979]; 13, Sinogeikin and Bass [2000], 14, Sinogeikin and Bass [2002b]; 15, Parise et al [1996]; 16, Suzuki and Anderson [1983]; 17, Yagi et al [1987]; 18, assumed; 19, Zhang et al [1999]; 20, Skinner [1956]; 21, Wang and Ji [2001]; 22, same as pyrope; 23, Bass [1989]; 24, Conrad et al [1999]; 25, Isaak et al [1992]; 26, Pavese et al [2001]; 27, Sinogeikin and Bass [2002a]; 28, Pacalo and Weidner [1997]; 29, Wang et al [1998]; 30, Yusa et al [1993]; 31, Pacalo et al [1992]; 32, Irifune et al [1982]; 33, Angel and Jackson [2002]; 34, Jackson et al [1999]; 35, Smyth and McCormick [1995]; 36, Hugh‐Jones and Angel [1994]; 37, Zhao et al [1995]; 38, Flesch et al [1998]; 39, Chai et al [1997]; 40, Duffy and Anderson [1989]; 41, Bass and Weidner [1984]; 42, same as enstatite; 43, Hugh‐Jones [1997]; 44, Sueno et al [1976]; 45, Ita and Stixrude [1992]; 46, Zhang et al [1997]; 47, Zhao et al [1998]; 48, Cameron et al [1973]; 49, Finger and Ohashi [1976]; 50, Krupka et al [1985]; 51, Levien et al [1979]; 52, Haselton et al [1987]; 53, same as diopside; 54, ...…”

Section: Resultsmentioning

confidence: 99%

Seismological signature of chemical differentiation of Earth's upper mantle

2005

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[1] Chemical differentiation from pyrolite to harzburgite due to partial melting and melt extraction process causes the chemical heterogeneity in Earth's upper mantle that can be detected by seismological observations. The variation in major element chemistry in natural samples reflects complicated processes that include not only partial melting but also other various magmatic processes. On the basis of a comparison of chemical and mineralogical compositions of natural peridotites with those from melting experiment, density and seismic velocities of various peridotites are calculated for the range of pressure and temperature in the upper mantle using the latest data on mineral thermoelasticity. We conclude that the seismic velocities of shallow oceanic peridotites is characterized by a single parameter such as Mg # (molar ratio Mg/(Mg + Fe)), whereas the characterization of the deep continental peridotites requires two parameters, Mg # and Opx # (volume fraction of orthopyroxene). In agreement with previous studies, we find that in spinel stability field, the seismic velocities have positive correlation with Mg # from pyrolite to residual harzburgite, while in garnet stability field, seismic velocities of residual harzburgite are indistinguishable from those of pyrolite. The seismic velocities of the deep continental peridotites are lower than those of pyrolite and residual harzburgite because of the high concentration of orthopyroxene with low seismic velocities and have large pressure dependence. A jump of seismic velocity will occur at 300 km in orthopyroxenerich continental harzburgite due to the orthorhombic to high-pressure monoclinic phase transition in (Mg, Fe)SiO 3 pyroxene. This phase transition may correspond to the X discontinuity.

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“…To date, these studies have been restricted to pyrope-rich compositions (less than 38 mole % majorite), which are characterized by cubic symmetry. Since Parise et al (1996) have shown that the symmetry changes to tetragonal at composition about Mj75, it is important to determine the elasticity of these lower symmetry garnets at elevated pressures and temperatures.…”

Section: Introductionmentioning

confidence: 99%

Sound velocities in MgSiO₃‐garnet to 8 GPa

Gwanmesia

Chen

Liebermann

1998

Geophysical Research Letters

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Abstract. Velocities of acoustic compressional (P) and shear (S) waves were measured to 8 GPa at room temperature for dense (99.7% of theoretical density), isotropic polycrystalline specimens of MgSiO3-majorite garnet using the phase comparison method of ultrasonic interferometry in a 1000-ton split-cylinder apparatus (USCA-1000).The pressure derivatives of the adiabatic bulk modulus (Ks) and the shear modulus (G) are Ko '= (3Ks/3P)T = 6.7 + 0.4 and Go '= (3G/3P)T = 1.9 + 0

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The symmetry of garnets on the pyrope (Mg₃Al₂Si₃O₁₂)‐majorite (MgSiO₃) join

Cited by 39 publications

References 26 publications

Thermal equation of state of Mg3Al2Si3O12 pyrope garnet up to 19 GPa and 1,700 K

Thermal equation of state of Mg3Al2Si3O12 pyrope garnet up to 19 GPa and 1,700 K

Seismological signature of chemical differentiation of Earth's upper mantle

Sound velocities in MgSiO₃‐garnet to 8 GPa

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The symmetry of garnets on the pyrope (Mg3Al2Si3O12)‐majorite (MgSiO3) join

Cited by 39 publications

References 26 publications

Thermal equation of state of Mg3Al2Si3O12 pyrope garnet up to 19 GPa and 1,700 K

Thermal equation of state of Mg3Al2Si3O12 pyrope garnet up to 19 GPa and 1,700 K

Seismological signature of chemical differentiation of Earth's upper mantle

Sound velocities in MgSiO3‐garnet to 8 GPa

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The symmetry of garnets on the pyrope (Mg₃Al₂Si₃O₁₂)‐majorite (MgSiO₃) join

Sound velocities in MgSiO₃‐garnet to 8 GPa