The pyroxenes are a group of important rock-forming inosilicate minerals found in many igneous and metamorphic rocks.
They share a common structure consisting of single chains of silica tetrahedra and they crystallize in the monoclinic and orthorhombic systems.
Pyroxenes have the general formula XY(Si,Al)2O6 (where X represents calcium, sodium, iron+2 and magnesium and more rarely zinc, manganese and lithium and Y represents ions of smaller size, such as chromium, aluminium, iron+3, magnesium, manganese, scandium, titanium, vanadium and even iron+2). Although aluminium substitutes extensively for silicon in silicates such as feldspars and amphiboles, the substitution occurs only to a limited extent in most pyroxenes.
The upper mantle of Earth is composed mainly of olivine and pyroxene.
The chain silicate structure of the pyroxenes offers much flexibility in the incorporation of various cations and the names of the pyroxene minerals are primarily defined by their chemical composition. Pyroxene minerals are named according to the chemical species occupying the X (or M2) site, the Y (or M1) site, and the tetrahederal T site. Cations in Y (M1) site are closely bound to 6 oxygens in octahedral coordination. Cations in the X (M2) site can be coordinated with 6 to 8 oxygen atoms, depending on the cation size. Twenty mineral names are recognised by the International Mineralogical Association’s Commission on New Minerals and Mineral Names and 105 previously used names have been discarded (Morimoto et al., 1989).
A typical pyroxene has mostly silicon in the tetrahedral site and predominately ions with a charge of +2 in both the X and Y sites, giving the approximate formula XYT2O6. The names of the common calcium – iron – magnesium pyroxenes are defined in the ‘pyroxene quadrilateral’ shown in Figure 2. The enstatite-ferrosilite series ([Mg,Fe]SiO3) contain up to 5 mol.% calcium and exists in three polymorphs, orthorhombic orthoenstatite and protoenstatite and monoclinic clinoenstatite (and the ferrosilite equivalents). Increasing the calcium content prevents the formation of the orthorhombic phases and pigeonite ([Mg,Fe,Ca][Mg,Fe]Si2O6) only crystallises in the monoclinic system. There is not complete solid solution in calcium content and Mg-Fe-Ca pyroxenes with calcium contents between about 15 and 25 mol.% are not stable with respect to a pair of exolved crystals. This leads to a miscibility gap between pigeonite and augite compositions. There is an arbitrary separation between augite and the diopside-hedenbergite (CaMgSi2O6 – CaFeSi2O6) solid solution. The divide is taken at >45 mol.% Ca. As the calcium ion cannot occupy the Y site, pyroxenes with more than 50 mol.% calcium are not possible. A related mineral wollastonite has the formula of the hypothetical calcium end member but important structural differences mean that it is not grouped with the pyroxenes.
Magnesium, calcium and iron are by no means the only cations that can occupy the X and Y sites in the pyroxene structure. A second important series of pyroxene minerals are the sodium-rich pyroxenes, corresponding to nomenclature shown in Figure 3. The inclusion of sodium, which has a charge of +1, into the pyroxene implies the need for a mechanism to make up the “missing” positive charge. In jadeite and aegirine this is added by the inclusion of a +3 cation (aluminium and iron(III) respectively) on the Y site. Sodium pyroxenes with more than 20 mol.% calcium, magnesium or iron(II) components are known as omphacite and aegirine-augite, with 80% or more of these components the pyroxene falls in the quadrilateral shown in figure 2.
Table 1 shows the wide range of other cations that can be accommodated in the pyroxene structure, and indicates the sites that they occupy.
In assigning ions to sites the basic rule is to work from left to right in this table first assigning all silicon to the T site then filling the site with remaining aluminium and finally iron(III), extra aluminium or iron can be accommodated in the Y site and bulkier ions on the X site. Not all the resulting mechanisms to achieve charge neutrality follow the sodium example above and there are several alternative schemes:
- Coupled substitutions of 1+ and 3+ ions on the X and Y sites respectively. For example Na and Al give the jadeite (NaAlSi2O6) composition.
- Coupled substitution of a 1+ ion on the X site and a mixture of equal numbers of 2+ and 4+ ions on the Y site. This leads to e.g. NaFe2+0.5Ti4+0.5Si2O6.
- The Tschermak substitution where a 3+ ion occupies the Y site and a T site leading to e.g. CaAlAlSiO6.
In nature, more than one substitution may be found in the same mineral.
- Clinopyroxenes (monoclinic)
- Aegirine (Sodium Iron Silicate)
- Augite (Calcium Sodium Magnesium Iron Aluminium Silicate)
- Clinoenstatite (Magnesium Silicate)
- Diopside (Calcium Magnesium Silicate, CaMgSi2O6)
- Esseneite (Calcium Iron Aluminium Silicate)
- Hedenbergite (Calcium Iron Silicate)
- Jadeite (Sodium Aluminium Silicate)
- Jervisite (Sodium Calcium Iron Scandium Magnesium Silicate)
- Johannsenite (Calcium Manganese Silicate)
- Kanoite (Manganese Magnesium Silicate)
- Kosmochlor (Sodium Chromium Silicate)
- Namansilite (Sodium Manganese Silicate)
- Natalyite (Sodium Vanadium Chromium Silicate)
- Omphacite (Calcium Sodium Magnesium Iron Aluminium Silicate)
- Petedunnite (Calcium Zinc Manganese Iron Magnesium Silicate)
- Pigeonite (Calcium Magnesium Iron Silicate)
- Spodumene (Lithium Aluminium Silicate)
- Orthopyroxenes (orthorhombic)
- Hypersthene (Magnesium Iron Silicate)
- Donpeacorite, (MgMn)MgSi2O6
- Enstatite, Mg2Si2O6
- Ferrosilite, Fe2Si2O6
- Nchwaningite (Hydrated Manganese Silicate)