Group of The most abundant group of minerals in Earth's crust, the structure of silicates are dominated by the silica tetrahedron, SiO44-, with metal ions occurring between tetrahedra). The mesodesmic bonds of the silicon tetrahedron allow extensive polymerization and silicates are classified according to the amount of linking that occurs between the minerals, (Mg,Fe)2SiO4, with the compositional endpoints of Pure* magnesium end-member (Mg2SiO4) of the olivine solid solution series and an important mineral in meteorites. When magnesium (Mg) is completely substituted by iron, it yields the the pure Fe-olivine end member, fayalite (Fe2SiO4). The various Fe and Mg substitutions between these two end-members are described based on their forsteritic (Fo) (Mg2SiO4) and Pure* iron end-member (Fe2SiO4) of the olivine solid solution series and an important mineral in meteorites. When iron (Fe) is completely substituted by magnesium, it yields the the pure Mg-olivine end-member, forsterite (Mg2SiO4). The various Fe and Mg substitutions between these two end-members are described based on their forsteritic (Fo) (Fe2SiO4). Olivine is commonly found in all Chondrites are the most common meteorites accounting for ~84% of falls. Chondrites are comprised mostly of Fe- and Mg-bearing silicate minerals (found in both chondrules and fine grained matrix), reduced Fe/Ni metal (found in various states like large blebs, small grains and/or even chondrule rims), and various refractory inclusions (such within both the Fine grained primary and silicate-rich material in chondrites that surrounds chondrules, refractory inclusions (like CAIs), breccia clasts and other constituents. and Roughly spherical aggregate of coarse crystals formed from the rapid cooling and solidification of a melt at ~1400 ° C. Large numbers of chondrules are found in all chondrites except for the CI group of carbonaceous chondrites. Chondrules are typically 0.5-2 mm in diameter and are usually composed of olivine, achondrites including most primitive achondrites and some evolved achondrites, in pallasites as large yellow-green crystals (brown when terrestrialized), in the silicate portion of mesosiderites, and even in some silicated irons. Olivine and A class of silicate (SiO3) minerals that form a solid solution between iron and magnesium and can contain up to 50% calcium. Pyroxenes are important rock forming minerals and critical to understanding igneous processes. For more detailed information, please read the Pyroxene Group article found in the Meteoritics & Classification category. are the most common Inorganic substance that is (1) naturally occurring (but does not have a biologic or man-made origin) and formed by physical (not biological) forces with a (2) defined chemical composition of limited variation, has a (3) distinctive set of of physical properties including being a solid, and has a (4) homogeneous found in stony meteorites.
Meteoriticists usually state the composition of olivine present in a Work in progress. A solid natural object reaching a planet’s surface from interplanetary space. Solid portion of a meteoroid that survives its fall to Earth, or some other body. Meteorites are classified as stony meteorites, iron meteorites, and stony-iron meteorites. These groups are further divided according to their mineralogy and based on its fayalite content which corresponds to the percentage of iron in the olivine. So, Fa9.7 means the iron content in the olivine is 9.7%.
Complete solid solutions occur in both the forsterite-fayalite series, and the monticellite (CaMgSiO4) to kirschteinite (CaFeSiO4) series. Kirschteinite has been found in Sub-millimeter to centimeter-sized amorphous objects found typically in carbonaceous chondrites and ranging in color from white to greyish white and even light pink. CAIs have occasionally been found in ordinary chondrites, such as the L3.00 chondrite, NWA 8276 (Sara Russell, 2016). CAIs are also known as refractory inclusions since they and other Inclusions found predominantly in carbonaceous chondrites and are rich in refractory elements particularly calcium, aluminum and titanium that in various combinations form minerals such as spinel, melilite, perovskite and hibonite. There are two types of refractory inclusion: • Ca Al-rich inclusions (CAIs) • Amoeboid olivine aggregates (AOAs) Refractory inclusions were, some angrites and even in the matrices of some CV3 oxidixed chondrites where the CV3 The body from which a meteorite or meteoroid was derived prior to its ejection. Some parent bodies were destroyed early in the formation of our Solar System, while others like the asteroid 4-Vesta and Mars are still observable today. experienced hydrothermal alteration. The monticellite-kirschteinite series has larger Smallest repeating unit of a crystalline solid that can be used to describe the entire structure. Unit cells are like templates which can be copied to produce an entire crystal. than the forsterite-fayalite series, accommodating the larger Ca Positively charged ion..
Fe-Mn Replacement of one ion or ionic group for another in the same structural site in a mineral yielding a solid solution. Most substitution in minerals is of cations which are smaller and essentially sit in a lattice of oxygen anions. Anionic substitution does occur in halides. Substitutions are classified based forms a complete Compositional variation resulting from the substitution of one ion or ionic compound for another ion or ionic compound in an isostructural material. This results in a mineral structure with specific atomic sites occupied by two or more ions or ionic groups in variable proportions. Solid solutions can be complete (with between tephroite (Mn2SiO4) and fayalite (no image provided). There is more Mn and Ca substitution in Fe-rich end members than Mg-rich end members. Ni is commonly present in Mg-rich olivine. Tephroite is only a minor component in olivines. The fayalite/tephroite ratio is represented by the Fe/Mn ratio in olivine. All meteoritic olivines have high Fe/Mn ratios.
The olivine structure consists of Isolated (SiO4)4- tetrahedra pointing alternately up and down along rows parallel to c axis. Mg2+ and Fe2+ occur in octahedral coordination (M-cations) in two distinct octahedral sites: a distorted M1 site and a more regular M2 site. Layers occur parallel to (100) with edge-sharing octahedra cross-linked by isolated (SiO4)4- tetrahedra. Mg2+ and Fe2+ appear to occupy the M1 or M2 sites without preference in the Mg-Fe series. In CaMgSiO4 olivine, Ca2+ prefers M2 site with Mg2+ in the M1 site.
Olivine has several polymorphs. The α olivine structure described above is only stable in upper part of Earth’s Main silicate-rich zone within a planet between the crust and metallic core. The mantle accounts for 82% of Earth's volume and is composed of silicate minerals rich in Mg. The temperature of the mantle can be as high as 3,700 °C. Heat generated in the core causes convection currents in. At ~400 km depth, olivine transforms into High-pressure olivine polymorph with a spinel structure that is found in highly shocked meteorites (above ~50 GPa, shock level > S5) and the Earth's transition zone mantle (~13 GPa). Under even higher pressure in the lower mantle (~24 GPa), ringwoodite decomposes into perovskite (Mg,Fe)SiO3, and magnesiowüstite (Mg,Fe)O, whose properties are (γ Mg-Al oxide, MgAl2O4, found in CAIs. structure), which is about 10% denser. At still greater depths (~670 km), ringwoodite decomposes into magnesiowüstite, (Mg,Fe)O and (MgVI,FeVI)SiVIO3, which has a Term applied to A2+B4+O3 high-pressure minerals with a perovskite structure (general formula ABX3) where "A" is a metal that forms large cations such as Mg, Fe or Ca, "B" is another metal that forms smaller cations such as Si (called silicate perovskite), Ti and to a lesser degree Al, and structure (Si in octahedral coordination).
Some or all content above used with permission from J. H. Wittke.