Omphacite

Omphacite
Picture of pieces of eclogite (type of rock) from the Western Gneiss Region in Norway. The rock contains the minerals omphacite (green), pyrope-garnet (red), quartz (milky), kyanite (blue) and some phengite (golden white).
General
CategoryPyroxene
Formula
(repeating unit)		(Ca,Na)(Mg,Fe2+,Al)Si2O6
IMA symbolOmp[1]
Strunz classification9.DA.20
Dana classification65.01.03b.01
(clinopyroxene)
Crystal systemMonoclinic
Crystal classPrismatic (2/m)
(same H-M symbol)
Space groupP2/n or C2/c
Unit cella = 9.66, b = 8.81,
c = 5.22 [Å]; β = 106.56°; Z = 4
Identification
ColorGreen to dark green; colorless to pale green in thin section
Crystal habitRarely in rough crystals; anhedral, granular to massive
TwinningSingle and polysynthetic twinning common on {100}
CleavageGood on {110}, {110} ^ {110} ≈87°; parting on {100}
FractureUneven to conchoidal
TenacityBrittle
Mohs scale hardness5–6
LusterVitreous to silky
StreakGreenish white
DiaphaneityTranslucent
Specific gravity3.16–3.43
Optical propertiesBiaxial (+)
Refractive indexnα = 1.662 – 1.701 nβ = 1.670 – 1.712 nγ = 1.685 – 1.723
Birefringenceδ = 0.023
PleochroismWeak; X = colorless; Y = very pale green; Z = very pale green, blue-green
2V angleMeasured: 58° to 83°, Calculated: 74° to 88°
References[2][3][4][5]

Omphacite is a member of the clinopyroxene group of silicate minerals with formula: (Ca, Na)(Mg, Fe2+, Al)Si2O6. It is a variably deep to pale green or nearly colorless variety of clinopyroxene. It normally appears in eclogite, which is the high-pressure metamorphic rock of basalt. Omphacite is the solid solution of Fe-bearing diopside and jadeite.[6] It crystallizes in the monoclinic system with prismatic, typically twinned forms, though usually anhedral. Its space group can be P2/n or C2/c depending on the thermal history.[7] It exhibits the typical near 90° pyroxene cleavage. It is brittle with specific gravity of 3.29 to 3.39 and a Mohs hardness of 5 to 6.

Formation and occurrence

Phase diagram of slab crust in the Earth's upper mantle from 200 to 500 km depth.[8] Omphacite general dissolves into garnet as depth increases. Omphacite can stable up to ~500 km depth.

Omphacite is the dominated phase in the subducted oceanic crust in the Earth's upper mantle. The Mid-Ocean Ridge Basalt, which makes up oceanic crust, goes through ultrahigh-pressure metamorphic process and transforms to eclogite at depth ~60 km in the subduction zones.[9] The major mineral components of eclogite include omphacite, garnet and high-pressure silica phases (coesite and stishovite).[8] As depth increases, the omphacite in eclogite gradually transforms to majoritic garnet. Omphacite is stable up to 500 km depth in the Earth's interior.[8][10] Considering the cold geotherm of subducted slabs, omphacite can be stable even in deeper mantle.

It also occurs in blueschist facies and ultrahigh-pressure metamorphic rocks.[11] It is also found in eclogite xenoliths from kimberlite as well as in crustal rocks metamorphosed at high pressures.[12] Associated minerals in eclogites except the major minerals include rutile, kyanite, phengite, and lawsonite. Minerals such as glaucophane, lawsonite, titanite, and epidote occur with omphacite in blueschist facies metamorphic rocks. The name "jade", usually referring to rocks made of jadeite, is sometimes also applied to rocks consisting entirely of omphacite.

Chemical composition

Omphacite is the solid solution of Fe-bearing diopside (CaMgSi2O6) and jadeite (NaAlSi2O6). Depending on how much the coupled substitution of (Na, Al)-(Mg-Fe, Ca) happens, the chemical composition of omphacite varies continuously from pure diopside to pure jadeite.[6] Due to the relatively small radius of (Na, Al) atoms, the unit cell volume linearly decreases as jadeite component increases.[13] In addition, the coupled substitution also stiffens the crystals. The bulk and shear modulus linearly increases as jadeite component increases.[6]

Space group

Although omphacite is the solid solution of diopside and jadeite, its space group may be different with them. The space group of diopside and jadeite is C2/c. However, omphacite can show both P2/n and C2/c space group. At low temperature, the partial coupled substitution of (Na, Al)-(Mg-Fe, Ca) in omphacite orders the atoms in the unit cell and makes omphacite shows a relatively low symmetry space group P2/n.[14] As temperature increases, the movements of the atoms increase and finally the coupled substitution will not influence the order of the structure. When temperature reaches ~700–750 °C, the structure of omphacite becomes totally disordered and the space group will transform to C2/c.[7] Natural omphacite may show C2/c structure even at room temperature if the omphacite crystal went through fast temperature decreasing.[15]

Although the atomic positions in the two space groups have a subtle difference, it does not clearly change the physical properties of omphacite.[6] The absolute unit cell volumes are a little different for the two different space group, the compressibility and thermal expansion does not show obviously different within experimental uncertainties.[13][16][17]

Etymology and history

It was first described in 1815 in the Münchberg Metamorphic complex, Franconia, Bavaria, Germany. The name omphacite derives from the Greek omphax or unripe grape for the typical green color.

References

  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. ^ Hurlbut, Cornelius S.; Klein, Cornelis, 1985, Manual of Mineralogy, 20th ed., pp. 398 - 405, John Wiley and Sons, New York ISBN 0-471-80580-7
  3. ^ Handbook of Mineralogy
  4. ^ Mindat.org
  5. ^ Webmineral data
  6. ^ a b c d Hao, Ming; Pierotti, Caroline E.; Tkachev, Sergey; Prakapenka, Vitali; Zhang, Jin S. (2019). "The single-crystal elastic properties of the jadeite-diopside solid solution and their implications for the composition-dependent seismic properties of eclogite". American Mineralogist. 104 (7): 1016–1021. Bibcode:2019AmMin.104.1016H. doi:10.2138/am-2019-6990. ISSN 0003-004X. S2CID 195790171.
  7. ^ a b Fleet, M. E.; Herzberg, C. T.; Bancroft, G. M.; Aldridge, L. P. (1978). "Omphacite studies; I, The P2/n-->C2/c transformation". American Mineralogist. 63: 1100–1106.
  8. ^ a b c Aoki, Ichiro; Takahashi, Eiichi (2004). "Density of MORB eclogite in the upper mantle". Physics of the Earth and Planetary Interiors. New Developments in High-Pressure Mineral Physics and Applications to the Earth's Interior. 143–144: 129–143. Bibcode:2004PEPI..143..129A. doi:10.1016/j.pepi.2003.10.007. ISSN 0031-9201.
  9. ^ Ahrens, Thomas J.; Schubert, Gerald (1975). "Gabbro-eclogite reaction rate and its geophysical significance". Reviews of Geophysics. 13 (2): 383–400. Bibcode:1975RvGSP..13..383A. doi:10.1029/RG013i002p00383. ISSN 1944-9208.
  10. ^ Irifune, T.; Sekine, T.; Ringwood, A. E.; Hibberson, W. O. (1986). "The eclogite-garnetite transformation at high pressure and some geophysical implications". Earth and Planetary Science Letters. 77 (2): 245–256. Bibcode:1986E&PSL..77..245I. doi:10.1016/0012-821X(86)90165-2. ISSN 0012-821X.
  11. ^ Guillot, S.; Mahéo, G.; de Sigoyer, J.; Hattori, K. H.; Pêcher, A. (2008). "Tethyan and Indian subduction viewed from the Himalayan high- to ultrahigh-pressure metamorphic rocks". Tectonophysics. Asia out of Tethys: Geochronologic, Tectonic and Sedimentary Records. 451 (1): 225–241. Bibcode:2008Tectp.451..225G. doi:10.1016/j.tecto.2007.11.059. ISSN 0040-1951.
  12. ^ Jacob, D. E. (2004). "Nature and origin of eclogite xenoliths from kimberlites". Lithos. Selected Papers from the Eighth International Kimberlite Conference. Volume 2: The J. Barry Hawthorne Volume. 77 (1): 295–316. Bibcode:2004Litho..77..295J. doi:10.1016/j.lithos.2004.03.038. ISSN 0024-4937.
  13. ^ a b Pandolfo, Francesco; Cámara, Fernando; Domeneghetti, M. Chiara; Alvaro, Matteo; Nestola, Fabrizio; Karato, Shun-Ichiro; Amulele, George (2015). "Volume thermal expansion along the jadeite–diopside join". Physics and Chemistry of Minerals. 42 (1): 1–14. Bibcode:2015PCM....42....1P. doi:10.1007/s00269-014-0694-9. hdl:2318/153763. ISSN 1432-2021. S2CID 96677363.
  14. ^ Skelton, Richard; Walker, Andrew M. (2015). "The effect of cation order on the elasticity of omphacite from atomistic calculations". Physics and Chemistry of Minerals. 42 (8): 677–691. Bibcode:2015PCM....42..677S. doi:10.1007/s00269-015-0754-9. ISSN 1432-2021. S2CID 92245503.
  15. ^ Bhagat, Snehal S.; Bass, Jay D.; Smyth, Joseph R. (1992). "Single-crystal elastic properties of omphacite-C2/c by Brillouin spectroscopy". Journal of Geophysical Research: Solid Earth. 97 (B5): 6843–6848. Bibcode:1992JGR....97.6843B. doi:10.1029/92JB00030. ISSN 2156-2202.
  16. ^ Hao, Ming; Zhang, Jin S.; Pierotti, Caroline E.; Ren, Zhiyuan; Zhang, D. (2019). "High-Pressure Single-Crystal Elasticity and Thermal Equation of State of Omphacite and Their Implications for the Seismic Properties of Eclogite in the Earth's Interior". Journal of Geophysical Research: Solid Earth. 124 (3): 2368–2377. Bibcode:2019JGRB..124.2368H. doi:10.1029/2018JB016964. ISSN 2169-9356.
  17. ^ Nishihara, Yu; Takahashi, Eiichi; Matsukage, Kyoko; Kikegawa, Takumi (2003). "Thermal equation of state of omphacite". American Mineralogist. 88 (1): 80–86. Bibcode:2003AmMin..88...80N. doi:10.2138/am-2003-0110. ISSN 0003-004X. S2CID 101319641.
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