Physics and Chemistry of Minerals

, Volume 23, Issue 1, pp 1–10 | Cite as

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

  • Jianzhong Zhang
  • Baosheng Li
  • Wataru Utsumi
  • Robert C. Liebermann
Original Paper


Using a DIA-type, cubic-anvil, high-pressure apparatus (SAM-85) in conjunction with in situ X-ray diffraction, we have investigated phase relations between coesite and stishovite up to 12 GPa and 1530 °C using synthetic powders of the two phases as the starting materials. The phase transition between coesite and stishovite was identified by observing the first appearance of a phase that did not already exist or by a change in the relative intensity of the two patterns. In most experiments, the diffraction patterns on samples were collected within 10 minutes after reaching a pressure and temperature condition. On this time scale, two phase boundaries associated with the coesite-stishovite transition have been determined: (1) for the stishovite-to-coesite transition, observations were made in the temperature range of 950–1530 °C, and (2) for the coesite-to-stishovite transition from 500 to 1300 °C. These observations reveal that there exists a critical temperature of about 1000 °C to constrain the coesite-stishovite equilibrium phase boundary. Above this temperature, both boundaries are linear, have positive dP/dT slopes, and lie within a pressure interval of 0.4 GPa. Below this temperature, the dP/dT slope for the stishovite-to-coesite phase boundary becomes significantly larger and that for the coesite-tostishovite phase boundary changes from positive to negative. As a result, an equilibrium phase boundary can only be determined from the results above 1000 °C and is described by a linear equation P (GPa)=6.1 (4)+ 0.0026 (2) T (°C). This dP/dT slope is in good agreement with that of Zhang et al. (1993) but more than twice that of Yagi and Akimoto (1976). For the kinetics of the phase transition, preliminary rate data were obtained for the stishovite-to-coesite transition at 1160 and 1430 °C and are in agreement with the simple geometric transformation model of Avrami and Cahn.


Phase Transition Mineral Resource Critical Temperature Phase Boundary Material Processing 
These keywords were added by machine and not by the authors. This process is experimental and the keywords may be updated as the learning algorithm improves.


Unable to display preview. Download preview PDF.

Unable to display preview. Download preview PDF.


  1. Akaogi M, Navrotsky A (1984) The quartz-coesite-stishovite transformations: new calorimetric measurements and calculation of phase diagrams. Phys Earth Planet Int 36: 124–134Google Scholar
  2. Akaogi M, Yusa H, Shiraishi K, Suzuki T (1995) Thermodynamic properties of a quartz, coesite and stishovite and equilibrium phase relations at high pressures and high temperatures. J Geophys Res 100: 22337–22347Google Scholar
  3. Akimoto S (1972) The system MgO-FeO-SiO2 at high pressures and temperatures: phase equilibria and elastic properties. Tectonophys 13: 161–187Google Scholar
  4. Akimoto S, Syono Y (1969) Coesite-stishovite transition. J Geophys Res 74: 1653–1659Google Scholar
  5. Bohlen SR, Boettcher AL (1982) The quartz+coesite transformation: A precise determination and the effects of other components. J Geophys Res 87: 7073–7078Google Scholar
  6. Cahn JW (1956) The kinetics of grain boundary nucleated reactions. Acta Metall 4: 313–320Google Scholar
  7. Christian JW (1975) The theory of transformations in metals and alloys, Part I. Pergamon, New YorkGoogle Scholar
  8. Decker DL (1971) High-pressure equation of state for NaCl, KC1, and CsCl. J Appl Phys 42: 3239–3244Google Scholar
  9. Fei Y, Saxena SK, Navrotsky A (1990) Internally consistent data and equilibrium phase relations for compounds in the system MgO-SiO2 at high pressure and high temperature. J Geophys Res 95: 6915–6928Google Scholar
  10. Fiquet G, Andrault D, Itie JP, Gillet P, Richet P (1995) X-ray diffraction of periclase in a laser-heated diamond-anvil cell. Phys Earth Planet Interior (submitted)Google Scholar
  11. Jackson I (1976) Melting of the silica isotypes SiO2, BeF2 and GeO2 at elevated pressures. Phys Earth Planet Interior 13: 218–231Google Scholar
  12. Kanzaki M (1991) Melting of silica up to 7 GPa. J Am Ceram Soc 73: 3706–3707Google Scholar
  13. Liebermann RC, Wang Y (1992) Characterization of sample environment in a uniaxial split-sphere apparatus. In: Syono Y, Manghnani MH (ed) High-Pressure Research: Application to Earth and Planetary Sciences. AGU, Washington DC, pp 19–31Google Scholar
  14. Liu J, Topor L, Zhang J, Navrotsky A, Liebermann RC (1996) Calorimetry study of the coesite-stishovite transformation and calculation of the phase boundary. Phys Chem Minerals 23: 11–16Google Scholar
  15. Ostrovsky IA (1965) Experimental fixation of the position coesite-stishovite equilibrium curve. Izv Acad Sci USSR Geol Ser 10: 132–135Google Scholar
  16. Saxena SK, Chartterjee N, Fei Y, Shen G (1993) Thermodynamic Data on Oxides and Silicates: an assessed data set based on thermochemistry and high pressure phase equilibrium. Springer-Verlag, Berlin, Heidelberg, New YorkGoogle Scholar
  17. Serghiou G, Zerr A, Chudinovskikh L, Boehler R (1995) The coesite-stishovite transition in a laser-heated diamond cell. Geophys Res Lett 22: 441–444Google Scholar
  18. Shen G, Lazor P (1995) Melting of minerals under lower mantle conditions: I. Experimental results. J Geophys Res 100: 17699–17713Google Scholar
  19. Shimomura O, Utsumi W, Taniguchi T, Kikegawa T, Nagashima T (1992) A new high pressure and high temperature apparatus with sintered diamond anvils for synchrotron radiation use. In: Syono Y, Manghnani MH (ed) High-Pressure Research: Applications to Earth and Planetary Sciences. AGU, Washington DC, pp 3–11Google Scholar
  20. Suito K (1977) Phase relations of pure Mg2SiO4 up to 200 kilobars. In: Manghnani MH, Akimoto S (ed) High Pressure Research: Application to Geophysics. Academic, San Diego, Calif, pp 365–371Google Scholar
  21. Utsumi W, Weidner DJ, Liebermann RC (1994) Volume measurement of MgO under high pressures and high temperatures. EOS Trans AGU Fall Meeting Suppl 75: 696Google Scholar
  22. Watanabe H (1982) Thermochemical properties of synthetic high-pressure compounds relevant to the Earth mantle. In: Akimoto S, Manghnani MH (ed) High-Pressure Research in Geophysics. Center for Academic Publications, Tokyo, pp 411–464Google Scholar
  23. Weidner DJ, Vaughan MT, Ko J, Wang Y, Liu X, Yeganeh-haeri A, Pacalo RE, Zhao Y (1992) Characterization of stress, pressure, and temperature in SAM 85, a DIA type high pressure apparatus. In: Syono Y, Manghnani MH (ed) High-Pressure Research: Application to Earth and Planetary Sciences. AGU, Washington DC, pp 13–117Google Scholar
  24. Weidner DJ, Wang Y, Vaughan MT (1994) Yield strength at high pressure and temperature. Geophys Res Lett 21: 753–756Google Scholar
  25. Yagi T, Akimoto S (1976) Direct determination of coesitestishovite transition by in situ X-ray measurements. Tectonophysics 35: 259–270Google Scholar
  26. Zhang J, Li B, Liebermann RC, Weidner DJ, Wang Y (1992) In situ X-ray study of the coesite-stishovite transition. EOS Trans AGU Fall Meeting 73: 566Google Scholar
  27. Zhang J, Liebermann RC, Gasparik T, Herzberg CT, Fei Y (1993) Melting and subsolidus relations of SiO2 at 9–14 GPa. J Geophys Res 98: 19785–19793Google Scholar
  28. Zhang J, Li B, Utsumi W, Liebermann RC (1994) Reversal of the coesite-stishovite phase transformation. EOS AGU Spring Meeting 75: 346Google Scholar

Copyright information

© Springer-Verlag 1996

Authors and Affiliations

  • Jianzhong Zhang
    • 1
  • Baosheng Li
    • 1
  • Wataru Utsumi
    • 1
  • Robert C. Liebermann
    • 1
  1. 1.Center for High Pressure Research and Department of Earth and Space SciencesUniversity at Stony BrookStony BrookUSA

Personalised recommendations