Wüstite

Crystal structure of Wüstite

Wüstite (FeO) is a mineral form of iron(II) oxide found with meteorites and native iron. It has a gray color with a greenish tint in reflected light. Wüstite crystallizes in the isometric - hexoctahedral crystal system in opaque to translucent metallic grains. It has a Mohs hardness of 5 to 5.5 and a specific gravity of 5.88. Wüstite is a typical example of a non-stoichiometric compound.

Wüstite was named for Fritz Wüst (1860–1938), a German metallurgist and founding director of the Kaiser-Wilhelm-Institut für Eisenforschung (presently Max Planck Institute for Iron Research GmbH).^[1]

In addition to the type locality in Germany, it has been reported from Disko Island, Greenland; the Jharia coalfield, Jharkhand, India and as inclusions in diamonds in a number of kimberlite pipes. It also is reported from deep sea manganese nodules.

Its presence indicates a highly reducing environment.

Wüstite Redox Buffer

Main article: Mineral redox buffer

Wüstite, in geochemistry, defines a redox buffer of oxidation within rocks at which point the rock is so reduced that Fe³⁺ and thus hematite is absent.

As the redox state of a rock is further reduced, magnetite is converted to wüstite. This occurs by conversion of the Fe³⁺ ions in magnetite to Fe²⁺ ions. An example reaction is presented below:

FeO.Fe₂O₃ + C --> 3FeO + CO

magnetite + graphite/diamond --> wüstite + carbon monoxide

The formula for magnetite is more accurately written as FeO.Fe₂O₃ than as Fe₃O₄. Magnetite is one part FeO and one part Fe₂O₃, rather than a solid solution of wüstite and hematite. The magnetite is termed a redox buffer because until all Fe³⁺ magnetite is converted to Fe²⁺ the oxide mineral assemblage of iron remains wüstite-magnetite, and furthermore the redox state of the rock remains at the same level of oxygen fugacity. This is similar to buffering in the H⁺/OH⁻ acid-base system of water.

Once the Fe³⁺ is consumed, then oxygen must be stripped from the system to further reduce it and wüstite is converted to native iron. The oxide mineral equilibrium assemblage of the rock becomes wüstite-magnetite-iron.

In nature, the only natural systems which are chemically reduced enough to even attain a wüstite-magnetite composition are rare, including carbonate-rich skarns, meteorites and perhaps the mantle where reduced carbon is present, exemplified by the presence of diamond and/or graphite.

Effects upon silicate minerals

The ratio of Fe²⁺ to Fe³⁺ within a rock determines, in part, the silicate mineral assemblage of the rock. Within a rock of a given chemical composition, iron enters minerals based on the bulk chemical composition and the mineral phases which are stable at that temperature and pressure. Iron may only enter minerals such as pyroxene and olivine if it is present as Fe²⁺; Fe³⁺ cannot enter the lattice of fayalite olivine and thus for every two Fe³⁺ ions, one Fe²⁺ is used and one molecule of magnetite is created.

In chemically reduced rocks, magnetite may be absent due to the propensity of iron to enter olivine, and wüstite may only be present if there is an excess of iron above what can be used by silica. Thus, wüstite may only be found in silica-undersaturated compositions which are also heavily chemically reduced, satisfying both the need to remove all Fe³⁺ and to maintain iron outside of silicate minerals.

In nature, carbonate rocks, potentially carbonatite, kimberlites, carbonate-bearing melilitic rocks and other rare alkaline rocks may satisfy these criteria. However, wüstite is not reported in most of these rocks in nature, potentially because the redox state necessary to drive magnetite to wüstite is so rare.

Historical use

According to Vagn Fabritius Buchwald, wustite was an important component during the Iron age to facilitate the process of forge welding. In ancient times, when blacksmithing was performed using a charcoal forge, the deep charcoal pit in which the steel or iron was placed provided a highly-reducing, virtually oxygen-free environment, producing a thin wustite layer on the metal. At the welding temperature, the iron becomes highly reactive with oxygen, and will spark and form thick layers of slag when exposed to the air, which makes welding the iron or steel nearly impossible. To solve this problem, ancient blacksmiths would toss small amounts of sand onto the white-hot metal. The silicon in the sand then reacts with the wustite to form fayalite, which melts just below the welding temperature. This produced an effective flux that shielded the metal from oxygen and helped extract oxides and impurities, leaving a pure surface that can weld readily. Although the ancients had no knowledge of how this worked, the ability to weld iron contributed to the movement out of the Bronze age and into the modern.^[2]

Related minerals

Wüstite forms a solid solution with periclase (MgO), and Fe substitutes for Mg. Periclase, when hydrated, forms brucite (Mg(OH)₂), a common product of serpentinite metamorphic reactions.

Oxidation of wüstite forms goethite-limonite.

Zinc, aluminium and other transition metals may substitute for Fe in wüstite.

Wüstite in dolomite skarns may be related to siderite (Fe-carbonate), wollastonite, enstatite, diopside and magnesite.

See also

• Normative mineralogy
• Redox
• Kimberlite
• Skarn
• Periclase

References

1. ↑ Schenck, Rudolf & Dingmann, Th.; 1927: Gleichgewichtsuntersuchungen über die Reduktions-, Oxydations- und Kohlungsvorgänge beim Eisen III, in: Zeitschrift für anorganische und allgemeine Chemie 166, p. 113-154, here p. 141.
2. ↑ Iron and Steel in Ancient Times By Vagn Fabritius Buchwald -- Det Kongelige Danske Videnskabernes Selskab 2005 Page 65

• Mineral Data Pub. PDF file Accessed 3/5/2006
• Euromin Accessed 3/5/2006
• Wüstite on Mindat.org Accessed 3/5/2006
• Webmineral data Accessed 3/5/2006