chondrodite
{{Short description|Nesosilicate mineral}}
{{ distinguish|Chondrite}}
{{Infobox mineral
| name = Chondrodite
| category = Nesosilicates
| boxwidth = 24
| boxbgcolor =
| image = Chondrodite-225224.jpg
| imagesize = 260px
| caption =
| formula = {{chem|Mg|5|(Si|O|4|)|2|F|2}}
| molweight = 351.6 g/mol
| strunz = 9.AF.45 (10th edition)
8/B.04-20 (8th edition)
| dana = 52.3.2b.2
| system = Monoclinic
| class = Prismatic (2/m)
(same H-M symbol)
| symmetry = P21/a
| color = Yellow, orange, red or brown, rarely colorless
| habit = Typically anhedral masses or grains, or as plates flattened on {010}, {001} or {100}.
| lattice =
| twinning = Simple or multiple twinning common on {001}, also reported on {105} and {305}.
| cleavage = Poor to good on (001)
| fracture = Conchoidal to uneven
| tenacity = Brittle
| mohs = 6 to 6.5
| luster = Vitreous to greasy
| refractive = nα = 1.592 – 1.643, nβ = 1.602 – 1.655, nγ = 1.619 – 1.675,
| opticalprop = Biaxial(+)
| birefringence = 0.027 – 0.032
| pleochroism = X golden yellow to orange, Y and Z light yellow to almost colorlessEuropean Journal of Mineralogy (2002) 14: 1027-1032
| streak = Grey or yellow
| gravity = 3.1 to 3.26
| density =
| melt =
| fusibility =
| diagnostic =
| solubility = Soluble in HCl and H2SO4
| diaphaneity = Translucent
| other = Some specimens fluoresce orange yellow under shortwave and orange under longwave UV. Not radioactive.
| references = {{cite web |url=https://www.mineralienatlas.de/lexikon/index.php/MineralData?mineral=Chondrodite |website=Mineralienatlas |title=Chondrodite}}{{cite web |url=http://www.mindat.org/min-1027.html |website=Mindat |title=Chondrodite}}{{Cite web|url=http://webmineral.com/data/Chondrodite.shtml|title = Chondrodite Mineral Data |website=WebMineral}}{{cite web |url=http://rruff.geo.arizona.edu/doclib/hom/chondrodite.pdf |title=Chondrodite |website=RRUFF |access-date=14 June 2024}}
}}
Chondrodite is a nesosilicate mineral with formula {{chem|(Mg|,Fe)|5|(Si|O|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 at Pargas in Finland, and named from the Greek for "granule", which is a common habit for this mineral.{{cite journal |last1=Hintze |first1=C. |title=Humitgruppe |journal=Silicate und Titanate |date=31 December 1897 |pages=370–406 |doi=10.1515/9783112361047-011 |isbn=9783112361047 |quote=The usually granular occurrence in the limestone of Pargas in Finland was described by D'OHSSON (Vet. Akad. Handl. Stockh. 1817, 206) after χονδρος "granule" as chondrodite}}
Formula
{{chem|Mg|5|(Si|O|4|)|2|F|2}} is the end member formula as given by the International Mineralogical Association,{{Cite web|url=http://rruff.info/ima|title=IMA Mineral List with Database of Mineral Properties}} 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 {{chem|(Mg|,Fe|,Ti)|5|(Si|O|4|)|2|(F|,OH|,O)|2}}.Gaines et al (1997) Dana's New Mineralogy Eighth Edition, Wiley
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 {{chem|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.Phillips, W R and Griffen, D T (1981) Optical Mineralogy, pages 142 to 144 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.American Mineralogist (1970): 55: 1182-1194 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.American Mineralogist (1979) 64:1027 In the humite series Mg2+ is replaced by Fe2+, Mn2+, Ca2+ and Zn2+ in that order of abundance, though Mg2+ always predominates.
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 = 109.2o.
Synthetic OH end member a = 7.914 Å, b = 4.752 Å, c = 10.350 Å, beta = 108.71o.
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 = 109.0o to 109.33o.
Z = 2.
Color
Image:Chondrodite with magnetite and silicate Basic magnesium fluosilicate Tilly Foster Mine, Brewster, Putnam County, New York 2659.jpg, Tilly Foster mine, Brewster, New York, US]]
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.
Optical properties
Chondrodite is biaxial(+), with refractive indices variously reported as nα = 1.592 – 1.643, nβ = 1.602 – 1.655, nγ = 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−. 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, {{chem2|(Mg,Fe(2+))2SiO4}}, and is stable over a range of temperatures and pressures that include those existing in a portion of the uppermost mantle.Physics and Chemistry of Minerals (1999) 26: 297-303
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.{{cite web |url=http://petrology.oxfordjournals.org/content/29/6/1353.short |title=Petrogenesis of Ultramafic Metamorphic Rocks from the 3800 Ma Isua Supracrustal Belt, West Greenland |website=petrology.oxfordjournals.org |access-date=27 January 2022 |archive-url=https://archive.today/20130920185252/http://petrology.oxfordjournals.org/content/29/6/1353.short |archive-date=20 September 2013 |url-status=dead}}{{Cite journal|url=http://geology.gsapubs.org/content/39/7/663.short|doi = 10.1130/G31904.1|title = Dunites from Isua, Greenland: A ca. 3720 Ma window into subcrustal metasomatism of depleted mantle|year = 2011|last1 = Friend|first1 = C.R.L.|last2 = Nutman|first2 = A.P.|journal = Geology|volume = 39|issue = 7|pages = 663–666|bibcode = 2011Geo....39..663F}}
See also
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