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Cristobalite spherulites formed by devitrification from the obsidian matrix.
Specimen from California, US; size: 5.9 cm × 3.8 cm × 3.8 cm (2.3 in × 1.5 in × 1.5 in).
CategoryOxide mineral, quartz group
(repeating unit)
IMA symbolCrs[1]
Strunz classification4.DA.15
Dana classification75.1.1.1
Crystal systemTetragonal
Crystal classTrapezohedral (422)
Space groupP41212, P43212
Unit cella = 4.9709(1) Å,
c = 6.9278(2) Å;
Z = 4 (α polytype)
Jmol (3D)Interactive image
ColorColorless, white
Crystal habitOctahedra or spherulites up to several cm in diameter
Twinningon {111}
Mohs scale hardness6–7
Specific gravity2.32–2.36
Optical propertiesUniaxial (−)
Refractive indexnω = 1.487
nε = 1.484
Melting point1,713 °C (3,115 °F) (β)[2]

Cristobalite (/krɪˈstbəˌlt/) is a mineral polymorph of silica that is formed at very high temperatures. It has the same chemical formula as quartz, SiO2, but a distinct crystal structure. Both quartz and cristobalite are polymorphs with all the members of the quartz group, which also include coesite, tridymite and stishovite. It is named after Cerro San Cristóbal in Pachuca Municipality, Hidalgo, Mexico.

It is used in dentistry as a component of alginate impression materials as well as for making models of teeth.[7]



Cristobalite is stable only above 1470 °C, but can crystallize and persist metastably at lower temperatures. The persistence of cristobalite outside its thermodynamic stability range occurs because the transition from cristobalite to quartz or tridymite is "reconstructive", requiring the breaking up and reforming of the silica framework. These frameworks are composed of SiO4 tetrahedra in which every oxygen atom is shared with a neighbouring tetrahedron, so that the chemical formula of silica is SiO2. The breaking of these bonds, required to convert cristobalite to tridymite and quartz, requires considerable activation energy and may not happen on a human time frame at room temperature. Framework silicates are also known as tectosilicates.

When devitrifying silica, cristobalite is usually the first phase to form, even when well outside its thermodynamic stability range. This is an example of Ostwald's step rule. The dynamically disordered nature of the β phase is partly responsible for the low enthalpy of fusion of silica.


There is more than one form of the cristobalite framework. At high temperatures, the structure is called β-cristobalite. It is in the cubic crystal system, space group Fd3m (No. 227, Pearson symbol cF104).[8] It has the diamond structure but with linked tetrahedra of silicon and oxygen where the carbon atoms are in diamond. A chiral tetragonal form called α-cristobalite (space group either P41212, No. 92,[9] or P43212, No. 96, at random) occurs on cooling below about 250 °C at ambient pressure and is related to the cubic form by static tilting of the silica tetrahedra in the framework. This transition is variously called the low-high or transition. It may be termed "displacive"; i.e., it is not generally possible to prevent the cubic β form from becoming tetragonal by rapid cooling. Under rare circumstances the cubic form may be preserved if the crystal grain is pinned in a matrix that does not allow for the considerable spontaneous strain that is involved in the transition, which causes a change in shape of the crystal. This transition is highly discontinuous. Going from the α form to the β form causes an increase in volume of 3[10] or 4[11] percent. The exact transition temperature depends on the crystallinity of the cristobalite sample, which itself depends on factors such as how long it has been annealed at a particular temperature.

The cubic β phase consists of dynamically disordered silica tetrahedra. The tetrahedra remain fairly regular and are displaced from their ideal static orientations due to the action of a class of low-frequency phonons called rigid unit modes. It is the "freezing" of one of these rigid unit modes that is the soft mode for the α–β transition.

In β-cristobalite, there are right-handed and left-handed helices of tetrahedra (or of silicon atoms) parallel to all three axes. In the α–β phase transition, however, only the right-handed or the left-handed helix in one direction is preserved (the other becoming a two-fold screw axis), so only one of the three degenerate cubic crystallographic axes retains a fourfold rotational axis (actually a screw axis) in the tetragonal form. (That axis becomes the "c" axis, and the new "a" axes are rotated 45° compared to the other two old axes. The new "a" lattice parameter is shorter by approximately the square root of 2, so the α unit cell contains only 4 silicon atoms rather than 8.) The choice of axis is arbitrary, so that various twins can form within the same grain. These different twin orientations coupled with the discontinuous nature of the transition (volume and slight shape change) can cause considerable mechanical damage to materials in which cristobalite is present and that pass repeatedly through the transition temperature, such as refractory bricks.


Cristobalite occurs as white octahedra or spherulites in acidic volcanic rocks and in converted diatomaceous deposits in the Monterey Formation of the US state of California and similar areas.

The micrometre-scale spheres that make up precious opal exhibit some X-ray diffraction patterns that are similar to that of cristobalite, but lack any long-range order so they are not considered true cristobalite. In addition, the presence of structural water in opal makes it doubtful that opal consists of cristobalite.[12][13]


  1. ^ Warr, L. N. (2021). "IMA–CNMNC approved mineral symbols". Mineralogical Magazine. 85 (3): 291–320. Bibcode:2021MinM...85..291W. doi:10.1180/mgm.2021.43. S2CID 235729616.
  2. ^ Deer, W. A.; Howie, R. A.; Zussman, J. (1966). An Introduction to the Rock Forming Minerals. Longman. pp. 340–355. ISBN 0-582-44210-9.
  3. ^ Mineralienatlas.
  4. ^ Cristobalite Archived 2010-07-15 at the Wayback Machine. Handbook of Mineralogy.
  5. ^ Cristobalite. Mindat.
  6. ^ "Cristobalite Mineral Data". Webmineral.
  7. ^ Anusavice, Kenneth J. (2013). Phillips' science of dental materials. Elsevier/Saunders. ISBN 978-1-4377-2418-9. OCLC 934359978.
  8. ^ Wright A. F., Leadbetter A. J. (1975). "The structures of the b-cristobalite phases of SiO2 and AlPO4". Philosophical Magazine. 31 (6): 1391–1401. Bibcode:1975PMag...31.1391W. doi:10.1080/00318087508228690.
  9. ^ Downs R. T., Palmer D. C. (1994). "The pressure behavior of a cristobalite" (PDF). American Mineralogist. 79: 9–14. Archived from the original (PDF) on 2019-05-15. Retrieved 2009-12-15.
  10. ^ R.E. Smallman & R.J. Bishop (1999). "2". Modern Physical Metallurgy and Materials Engineering (6 ed.). Butterworth-Heinemann. ISBN 978-0-7506-4564-5.
  11. ^ A.J. Leadbetter & A.F. Wright (1976). "The α—β transition in the cristobalite phases of SiO2 and AIPO4 I. X-ray studies". The Philosophical Magazine. 33 (1): 105–112. Bibcode:1976PMag...33..105L. doi:10.1080/14786437608221095.
  12. ^ Deane K. Smith (1998). "Opal, cristobalite, and tridymite: Noncrystallinity versus crystallinity, nomenclature of the silica minerals and bibliography". Powder Diffraction. 13 (1): 2–19. Bibcode:1998PDiff..13....2S. doi:10.1017/S0885715600009696. S2CID 97394861.
  13. ^ "Silica, Crystalline - Overview | Occupational Safety and Health Administration" (PDF). Archived from the original (PDF) on 2016-03-04.

Further reading[edit]

  • American Geological Institute Dictionary of Geological Terms.
  • Durham, D. L., "Monterey Formation: Diagenesis". in: Uranium in the Monterey Formation of California. US Geological Survey Bulletin 1581-A, 1987.
  • Reviews in Mineralogy and Geochemistry, vol. 29., Silica: behavior, geochemistry and physical applications. Mineralogical Society of America, 1994.
  • R. B. Sosman, The Phases of Silica. (Rutgers University Press, 1965)

External links[edit]