Chondrodite

Chondrodite
General
Category	Nesosilicates
Formula; (repeating unit)	Mg; 5(SiO; 4); 2F; 2
Strunz classification	9.AF.45 (10th edition) ; 8/B.04-20 (8th edition)
Dana classification	52.3.2b.2
Crystal system	Monoclinic
Crystal class	Prismatic (2/m) ; (same H-M symbol)
Space group	P21/a
Identification
Formula mass	351.6 g/mol
Color	Yellow, orange, red or brown, rarely colorless
Crystal habit	Typically anhedral masses or grains, or as plates flattened on {010}, {001} or {100}.[1]
Twinning	Simple or multiple twinning common on {001}, also reported on {105} and {305}.[1]
Cleavage	Poor to good on (001)
Fracture	Conchoidal to Uneven
Tenacity	Brittle
Mohs scale hardness	6 to 6.5
Luster	Vitreous to Greasy
Streak	Grey or Yellow
Diaphaneity	Translucent
Specific gravity	3.1 to 3.26
Optical properties	Biaxial(+)
Refractive index	nα = 1.592 - 1.643, nβ = 1.602 - 1.655, nγ = 1.619 - 1.675,
Birefringence	0.027 - 0.032
Pleochroism	X golden yellow to orange, Y and Z light yellow to almost colorless[2]
Solubility	Soluble in HCl and H2SO4
Other characteristics	Some specimens fluoresce orange yellow under shortwave and orange under longwave UV. Not radioactive.
References	[3][4][5][6][7]

Chondrodite is a nesosilicate mineral with formula (Mg,Fe)
₅(SiO
₄)
₂(F,OH,O)
₂. Although it is a fairly rare mineral, it is the most frequently encountered member of the humite group of minerals. It is formed in hydrothermal deposits from locally metamorphosed dolomite. It is also found associated with skarn and serpentinite. It was discovered in 1817 on Mt. Somma, part of the Vesuvius complex in Italy, and named from the Greek for "granule", which is a common habit for this mineral.

Formula

Mg
₅(SiO
₄)
₂F
₂ is the end member formula as given by the International Mineralogical Association,[8] molar mass 351.6 g. There is usually some OH in the F sites, however, and Fe and Ti can substitute for Mg, so the formula for the naturally occurring mineral is better written (Mg,Fe,Ti)
₅(SiO
₄)
₂(F,OH,O)
₂.[4]

Structure

The chondrodite structure is based on a slightly distorted hexagonal close packed array of anions O, OH and F with metal ions in the octahedral sites resulting in zigzag chains of M(O,OH,F)
₆ octahedra. Chains are staggered so that none of the independent tetrahedral sites occupied by Si has OH or F corners.[1] Half of the octahedral sites are filled by divalent cations, principally Mg, and one tenth of the tetrahedral sites are filled by Si. There are three distinct octahedra in the array: Fe is ordered in the M1 sites but not in the larger M2 and smaller M3 sites.[9] Ti is ordered in the M3 positions, which are the smallest, but Ti concentration appears never to exceed 0.5 atoms Ti per formula unit in natural specimens.[10] In the humite series Mg²⁺ is replaced by Fe²⁺, Mn²⁺, Ca²⁺ and Zn²⁺ in that order of abundance, though Mg²⁺ always predominates.[1]

Unit cell

Space Group: P2₁/b
Unit Cell Parameters:
Synthetic F end member a=7.80 Å, b=4.75 Å, c=10.27 Å, beta=109.2^o.
Synthetic OH end member a=7.914 Å, b=4.752 Å, c=10.350 Å, beta=108.71^o.
Natural chondrodite has a=7.867 to 7.905 Å, b=4.727 to 4.730 Å, c=10.255 to 10.318 Å, beta=109.0^o to 109.33^o. Z=2.

Color

Chondrodite with magnetite, Tilly Foster mine, Brewster, New York, USA

Chondrodite is yellow, orange, red or brown, or rarely colorless, but zoning of different color intensity is common, and intergrown plates of chondrodite, humite, clinohumite, forsterite and monticellite have been reported.[1]

Optical properties

Chondrodite is biaxial(+), with refractive indices variously reported as n_α = 1.592 - 1.643, n_β = 1.602 - 1.655, n_γ = 1.619 - 1.675, birefringence = 0.025 - 0.037, and 2V measured as 64° to 90°, calculated: 76° to 78°. Refractive indices tend to increase from norbergite to clinohumite in the humite group. They also increase with Fe²⁺ and Ti⁴⁺ and with (OH)⁻ substituting for F⁻.[1] Dispersion: r > v.

Environment

Chondrodite is found largely in metamorphic contact zones between carbonate rocks and acidic or alkaline intrusions where fluorine has been introduced by metasomatic processes. It is formed by the hydration of olivine, (Mg,Fe²⁺)₂SiO₄, and is stable over a range of temperatures and pressures that include those existing in a portion of the uppermost mantle.[11]

Titanian chondrodite has been found as inclusions in olivine in serpentinite in West Greenland, where it is associated with clinohumite, olivine, magnesite, magnetite and Ni-Co-Pb sulfides in a matrix of antigorite.[12][13]

References

Phillips, W R and Griffen, D T (1981) Optical Mineralogy, pages 142 to 144
European Journal of Mineralogy (2002) 14: 1027-1032
Mineralienatlas
Gaines et al (1997) Dana's New Mineralogy Eighth Edition, Wiley
http://www.mindat.org/min-1027.html Mindat
http://webmineral.com/data/Chondrodite.shtml
http://rruff.geo.arizona.edu/doclib/hom/chondrodite.pdf
http://rruff.info/ima
American Mineralogist (1970): 55: 1182-1194
American Mineralogist (1979) 64:1027
Physics and Chemistry of Minerals (1999) 26: 297-303
http://petrology.oxfordjournals.org/content/29/6/1353.short
http://geology.gsapubs.org/content/39/7/663.short

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[P&G-1] Phillips, W R and Griffen, D T (1981) Optical Mineralogy, pages 142 to 144

[EJM-2] European Journal of Mineralogy (2002) 14: 1027-1032

[3] Mineralienatlas

[Dana-4] Gaines et al (1997) Dana's New Mineralogy Eighth Edition, Wiley

[mindat-5] ttp://www.mindat.org/min-1027.html Mindat

[webmin-6] ttp://webmineral.com/data/Chondrodite.shtml

[HOM-7] ttp://rruff.geo.arizona.edu/doclib/hom/chondrodite.pdf

[IMA-8] ttp://rruff.info/ima

[AM55-9] American Mineralogist (1970): 55: 1182-1194

[AM64-10] American Mineralogist (1979) 64:1027

[PCM-11] Physics and Chemistry of Minerals (1999) 26: 297-303

[12] ttp://petrology.oxfordjournals.org/content/29/6/1353.short

[13] ttp://geology.gsapubs.org/content/39/7/663.short