Zussmanite

Zussmanite K(Fe++,Mg,Mn)₁₃[AlSi₁₇O₄₂](OH)₁₄ is a hydrated iron-rich silicate which was found in 1960 by Stuart Olof Agrell, in the Laytonville quarry, Mendocino County, California. Zussmanite is named in honor of Jack Zussman, Head of the University of Manchester’s Department of Geology and co-author of Rock-Forming Minerals, a bible for mineralogists. Zussmanite is found as a pale green crystal with perfect cleavage. In the Laytonville quarry, Zussmanite occurs in metamorphosed shales, siliceous ironstones and impure limestones of the Franciscan Formation. It is a location of high pressure and low temperatures where blueschist-facies metamorphic rocks occur. This is also the locality in which Deerite and Howieite were also first discovered. This type of locality also produces micas, which have a similar structure as Zussmanite. Some investigations as to the stability of Zussmanite have been performed to get an idea of end members and the pressure-temperature stability range.

Additional recommended knowledge

Recognize and detect the effects of electrostatic charges on your balance

Guide to balance cleaning: 8 simple steps

Daily Sensitivity Test

Introduction

The locality in which Zussmanite occurs is one of ultra high to high pressure and low temperatures. This baric type of metamorphism is usually distinguished by the P/T range rather than the ranges in pressure and temperatures (Miyashiro et al.,1973). The three principal baric types are low P/T type, medium P/T type, and high P/T type. The high P/T type, referred to as glaucophanic metamorphism, is characterized by the presence of glaucophane and forms glaucophane schists (Miyashiro et al.,1973). Glaucophane schists , commonly referred to as blueschist-facies, result from metamorphism of basaltic rocks and are usually located in folded geosynclinal terrains (Deer, Howie, Zussman et al.,1992). Glaucophane schists are characterized by low temperature (100-250 C) high pressure (4-9 kbar) metamorphism (Deer, Howie, Zussman et al.,1992). Zussmanite is commonly found with stilpnomelane and quartz, usually forming abundant porphyroblasts up to 1mm in size, in the newly discovered locality in Southern Central Chile ( Massonne et al., 1998).

Composition

The blueschist-facies phyllosilicate mineral occurs as a result of subduction of oceanic crustal rocks and oceanic-continental margin sediments along convergent plate boundaries. The ideal formula for Zussmanite is KFe13Si17AlO42(OH)14 with possible substitutions of Sodium (Na) for Potassium (K), in extremely small amounts (Lopes et al.,1969). The possible Iron (Fe2+) substitutes are mainly Magnesium (Mg) with trace amounts that could include: Manganese (Mn), Aluminum (Al), Iron3+ (Fe3+) and Titanium (Ti) (Lopes et al.,1969). Zussmanite was discovered in combination with Deerite and Howieite, two new minerals discovered in the Franciscan formation, Mendocino County, California. A unique thing differing these two minerals and Zussmanite is that while Deerite and Howieite have been found at other locations, Zussmanite has only been found at this type locality, making it a rare occurring mineral. Experiments have revealed that Zussmanite is stable up to 600oC at pressures between 10kb and 30kb and that the end members of Zussmanite are Orthoferrosilite, Biotite and Quartz. The example of the reaction is KFe13[AlSi17042](OH)14 (Zussmanite) yields 10FeSiO3 (Orthoferrosilite) + ½ K2Fe6Si6Al2O20(OH)4 (Biotite) + 4SiO2 (Quartz) + 6H20 (water) (Dempsey et al.,1981). The manganese analogue of Zussmanite, Coombsite, has been found in manganese-rich siliceous rocks in Otago Schist, New Zealand.

Structure

The space group and cell of Zussmanite are R*3, ahex 11.66 and chex28.69 Angstroms (Agrell et al., 1965). The structure of Zussmanite contains continuous sheets of rhombohedrally stacked layers of Fe-O octahedral parallel to (0001) (Lopes et al.,1967) and to either side of these are attached (Si,Al)-O tetrahedral in a way to produce a rhombohedral unit cell(Lopes et al.,1969). These layers are linked to one another by Potassium (K) atoms and also by three-member rings of tetrahedra that share oxygens with the six-members; displayed in figure 2 (Lopes et al.,1967). Zussmanite’s structure has a close affinity to that of the trioctahedral micas which have a layer of Fe-O octahedral sandwiched between inward pointing tetrahedral. It differs from the micas because its Si-O ratio is 9:21 which results in a sharing coefficient 1.83, as compared with 2.5 and 1.75 for micas, and 1.2 and 2.0 for framework silicates (Lopes et al.,1969). The Fe-(O,OH) mean distance in the first octahedron is 2.1 Angstroms, the second octahedron is 2.14 Angstroms, and in the third Octahedron is 2.17 Angstroms. The mean distance in the Si-O bonds in Zussmanite are 1.61 Angstroms for the first tetrahedron, 1.61 Angstroms for the second tetrahedron, and 1.65 Angstroms for the third tetrahedron; data given in table I (Lopes et al.,1969). The six-member rings are not directly linked to one another which allows for adjustment by tilting outwards of all tetrahedral, as opposed to many micas where rotations and tilts are used to achieve the larger dimensions of the octahedral layer. The flattening of the octahedral layer perpendicular to the layer is pronounced in Zussmanite due to shared and unshared edges. This flattening could be due to the tendency for shared oxygens to come closer and shields iron (Fe) atoms from other neighboring iron (Fe) atoms.

Physical Properties

Zussmanite occurs in pale green tabular crystals with perfect cleavage; seen in figure 4 from Laytonville quarry. It tends to be uniaxial, weakly pleochroic and a specific gravity of 3.146 (Agrell et al.,1965). Other types of Zussmanite found in Laytonville, which are of fine-grained samples are assumed to be late-stage metamorphic products. The perfect cleavage is a result of the continuous sheets of (Fe,Mg)-(O,OH) octahedra parallel to (0001). The optical properties, given in table 2, result from virtually pure Zussmanite that was separated from thin sections, approximately 200 microns thick, under a polarizing microscope by means of a microdrill. The indices of refraction compare well with those determined be Agrell et al.,1965 for the chemically different Zussmanite from the Laytonville quarry (Massonne et al., 1998).

References

1. Agrell, S.O.; Bown, M.G.; McKie, D. (1965). Deerite, Howieite and Zussmanite, Three New Minerals from the Franciscan of the Laytonville District, Mendocino County, California. Mineralogical Magazine. Volume 50. Page 278.
2. Deer, W.; Howie, R; Zussman, J. (1993). An Introduction to the Rock-Forming Minerals. Pearson Education Limited publishing. 2nd edition.
3. Dempsey, M.J. (1981) Zussmanite Stability; A Preliminary Study. Progress in Experimental Petrology. Volume 5. Pages 58-60.
4. Lopes-Vieira, A.; Zussman J. (1967). The Crystal Structure of the Mineral Zussmanite. Mineralogical Magazine. Volume 36, Issue 278. Pages 292-293.
5. Lopes-Vieira, A.; Zussman J. (1969). Further Detail on the Crystal Structure of Zussmanite. Mineralogical Magazine. Volume 37, Issue 285. Pages 28-60.
6. Massonne, H.-J. (1998). Zussmanite in ferruginous metasediments from Southern Central Chile. Mineralogical Magazine. Volume 62, Issue 6. Pages 869-876.
7. http://www.mindat.org/photo-82023.html. Photo Copyright at California Institute of Technology.
8. Miyashiro A.(1973). Metamorphism and metamorphic belts. Allen & Unwin, London, 492 pp.