In situ X-ray observations of the coesite-stishovite transition: reversed phase boundary and kinetics

Zhang, Jianzhong; Li, Baosheng; Utsumi, Wataru; Liebermann, Robert C.

doi:10.1007/bf00202987

Cited by 294 publications

(134 citation statements)

References 20 publications

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“…In the second experiment, S70, the boundary was determined under higher temperatures (1400 -1700 K). Under some P-T conditions near the phase boundary, no obvious changes in the relative integral intensities of diffraction peaks of two phases were observed because of a kinetics effect of the phase transition [Zhang et al 1996 …”

Section: Resultsmentioning

confidence: 96%

In situ Observation of ilmenite‐perovskite phase transition in MgSiO₃ using synchrotron radiation

Ono¹,

Katsura²,

Ito³

et al. 2001

Geophysical Research Letters

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Abstract. In situ observations of the ilmenite-perovskite transition in MgSiO3 were carried out in a multianvil high-pressure apparatus interfaced with synchrotron radiation. The phase boundary between ilmenite and perovskite in the temperature range of 1300-1600 K was determined to be P (GPa) = 28.4(ñ0. Under these circumstances, information on the stability field of the perovskite phase in the MgSiO3 system would also provide some insight into the structure of the mantle.4High-pressure and high-temperature X-ray diffraction measurements using synchrotron radiation are very advantageous for phase equilibrium studies compared to the conventional quenching method, because in this method both the phase present and the pressure value are determined simultaneously. Kato et al. [ 1995] first tried to determine the ilmenite-perovskite phase boundary in MgSiO3 by in situ measurements to 25 GPa and 1473 K, in a double-staged multianvil system interfaced to synchrotron radiation. Owing to considerable temperature fluctuations during measurements and associated large uncertainties in pressure determination, however, it was not possible to reliably define phase boundary from their results. Recently we have developed a multianvil assembly for X-ray diffraction measurements, which provides the stable conditions to 25 GPa and 2000 K for a long duration runs. The purpose of the present paper is to report our results on the ilmenite-perovskite transition obtained in this multianvil facility. (Fig. 1) consists of octahedral pressure medium made of precast Cr203-doped MgO. A cylindrical LaCrO3-furnace inside a composite thermal insulator of ZrO2-and MgO-sleeves was used as a heater. The sample was put into a tantalum chamber. Temperatures were measured by a W3%Re/W25%Re thermocouple, the junction of which was placed on the outside of the sample chamber in the center of the furnace. No correction was made for the effect of pressure on thermocouple emf. A more important correction arose from the temperature distribution in the sample because the pressure value determined via the equation of state of gold is quite sensitive to temperature. In order to decrease the temperature gradient throughout the sample, we used the 835 Experimental procedure

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Section: Resultsmentioning

confidence: 96%

In situ Observation of ilmenite‐perovskite phase transition in MgSiO₃ using synchrotron radiation

Ono¹,

Katsura²,

Ito³

et al. 2001

Geophysical Research Letters

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“…The graphite-diamond boundary (G͞D) is from Kennedy and Kennedy (14). The coesite-stishovite boundary (C͞S) is from Zhang et al (58).…”

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confidence: 99%

Fossilized high pressure from the Earth's deep interior: The coesite-in-diamond barometer

Sobolev

Fursenko

Goryaĭnov

et al. 2000

Proc. Natl. Acad. Sci. U.S.A.

148

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Mineral inclusions in diamonds provide an important source of information about the composition of the continental lithosphere at depths exceeding 120 -150 km, i.e., within the diamond stability field. Fossilized high pressures in coesite inclusions from a Venezuela diamond have been identified and measured by using laser Raman and synchrotron x-ray microanalytical techniques. MicroRaman measurements on an intact inclusion of remnant vibrational band shifts give a high confining pressure of 3.62 (؎0.18) GPa. Synchrotron single-crystal diffraction measurements of the volume compression are in accord with the Raman results and also revealed direct structural information on the state of the inclusion. In contrast to olivine and garnet inclusions, the thermoelasticity of coesite favors accurate identification of pressure preservation. Owing to the unique combination of physical properties of coesite and diamond, this ''coesite-in-diamond'' geobarometer is virtually independent of temperature, allowing an estimation of the initial pressure of Venezuela diamond formation of 5.5 (؎0.5) GPa.S pecimens of Earth materials from great depths often contain mineralogical or textural clues, such as metastable highpressure polymorphs or characteristic mineral assemblages implicating their high-pressure genealogy (1-3). The actual pressure, however, is seldom preserved and observed. For such observations, the sample must be retained in a strong container with appropriate relative thermoelastic properties, and nondestructive analytical techniques must be developed to probe the fossilized pressure condition in situ in the container. Diamond is the strongest possible container. Infrared absorption spectroscopy has been used as the probe for fluid inclusions in diamond (4), and high residual pressures have been reported on the basis of infrared spectra of quartz and CO 2 inclusions in the material (5, 6). In these studies, bulk spectra of diamond and numerous microscopic inclusions were measured; pressures and phases of different inclusions were not determined individually. Herein, we present direct measurements of pressures up to 3.6 GPa in individual coesite inclusions in diamond, a thermoelastic couple most favorable for pressure preservation. We use micro-Ramanand micro-single-crystal x-ray diffraction techniques to probe the pressure of each inclusion separately and precisely. Application to coesite inclusions in diamond from Venezuela provides a determination of the pressure-temperature (P-T) conditions of its formation.Diamond and its inclusions contain rich information about the petrogenesis and geochemistry of the Earth's deep interior (7,8). Although coesite-and diamond-bearing rocks (9-12) undoubtedly have a high-pressure origin, individually, coesite and diamond cover a wide P-T domain of stability (13, 14) that precludes their use as a precise and accurate geobarometer, because they give only a lower bound on the pressure of formation. In many cases, much higher pressures are suggested (15) based on mineral equilibria d...

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“…Phase diagrams of the MgCO 3 -SiO 2 system at (a) 9 GPa, (b) 13 GPa, and (c) 26 GPa. Eutectic point: this study; Melting points of magnesite: Katsura and Ito (1990); Melting points of SiO 2 : Ottonello et al (2013) and Usui and Tsuchiya (2010); transformation boundary of coesite-stishovite: Zhang et al (1996). Filled circle, triangle, and square symbols indicate the eutectic point of each system at 9, 13, and 26 GPa, respectively.…”

Section: Discussionmentioning

confidence: 99%

“…Pressure was estimated by room temperature calibration of the following phase transitions: ZeTe (6, 9.7, 12 GPa), ZnS (15.6 GPa), GaP (23 GPa). We also conducted pressure calibration at high temperature using coesite-stishovite (Zhang et al, 1996) and α-γ Fe 2 SiO 4 (Yagi et al, 1978) transformations. Furthermore, the pressure was estimated by using the α-β-γ transformations in the Mg 2 SiO 4 , (Mg 0.9 Fe 0.1 ) 2 SiO 4 , and (Mg 0.8 Fe 0.2 ) 2 SiO 4 compositions (Akaogi et al, 1989) and the pyroxene-garnet transformation in the enstatite (MgSiO 3 )-pyrope (Mg 3 Al 2 Si 3 O 12 ) join with 5 mol% or 10 mol% Al 2 O 3 component (Akaogi et al, 2002), depending on the pressure used in each experiment.…”

Section: Quench Experimentsmentioning

confidence: 99%

“…On the other hand, Litasov et al (2008) conducted their experi- (Katsura and Ito, 1990). The thin solid line shows the phase diagram of MgSiO 3 (Gasparik, 2003), and the thin broken line shows the phase diagram of SiO 2 (Bose and Ganguly, 1995;Zhang et al, 1996). Qtz, quartz; Coe, coesite; St, stishovite; OEn, orthoenstatite; Cen, clinoenstatite; Mj, majorite; β, wadsleyite; γ, ringwoodite; Ak, akimotite; Brg, bridgmanite (Mg-perovskite); Mgs, magnesite.…”

Section: In Situ X-ray Experimentsmentioning

confidence: 99%

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Decarbonation and melting in MgCO<sub>3</sub>–SiO<sub>2</sub> system at high temperature and high pressure

Kakizawa

Inoue

Suenami

et al. 2015

Journal of Mineralogical and Petrological Sciences

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The decarbonation reaction boundary and the melting temperature in the MgCO 3 -SiO 2 system were investigated up to 26 GPa using a multi-anvil apparatus. It was found that the decarbonation reaction (MgCO 3 + SiO 2 → MgSiO 3 + CO 2 ) occurs below 8 GPa, but it becomes a melting reaction above 8 GPa. The melting system shows a simple eutectic relation. The eutectic point shifts to a higher temperature and more MgCO 3 -rich composition with increasing pressure. The eutectic temperatures at~9 GPa and~26 GPa were found to bẽ 1700°C and~2000°C, respectively. Our results show that magnesite remains stable through the mantle geotherm, at least up to uppermost lower mantle, and that carbon can be transported to the lower mantle as magnesite. If a hot plume brings magnesite back to the upper mantle, it generates carbonatite magma or CO 2 fluid.

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In situ X-ray observations of the coesite-stishovite transition: reversed phase boundary and kinetics

Cited by 294 publications

References 20 publications

In situ Observation of ilmenite‐perovskite phase transition in MgSiO₃ using synchrotron radiation

In situ Observation of ilmenite‐perovskite phase transition in MgSiO₃ using synchrotron radiation

Fossilized high pressure from the Earth's deep interior: The coesite-in-diamond barometer

Decarbonation and melting in MgCO<sub>3</sub>–SiO<sub>2</sub> system at high temperature and high pressure

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In situ X-ray observations of the coesite-stishovite transition: reversed phase boundary and kinetics

Cited by 294 publications

References 20 publications

In situ Observation of ilmenite‐perovskite phase transition in MgSiO3 using synchrotron radiation

In situ Observation of ilmenite‐perovskite phase transition in MgSiO3 using synchrotron radiation

Fossilized high pressure from the Earth's deep interior: The coesite-in-diamond barometer

Decarbonation and melting in MgCO<sub>3</sub>–SiO<sub>2</sub> system at high temperature and high pressure

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In situ Observation of ilmenite‐perovskite phase transition in MgSiO₃ using synchrotron radiation

In situ Observation of ilmenite‐perovskite phase transition in MgSiO₃ using synchrotron radiation