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Siderite

Siderite
General
CategoryCarbonate mineral
Formula
(repeating unit)
FeCO3
IMA symbolSd[1]
Strunz classification5.AB.05
Dana classification14.01.01.03
Crystal systemTrigonal
Crystal classHexagonal scalenohedral (3m)
H-M symbol: (3 2/m)
Space groupR3c
Unit cella = 4.6916
c = 15.3796 [Å]; Z = 6
Identification
ColorPale yellow to tan, grey, brown, green, red, black and sometimes nearly colorless
Crystal habitTabular crystals, often curved; botryoidal to massive
TwinningLamellar uncommon on{0112}
CleavagePerfect on {0111}
FractureUneven to conchoidal
TenacityBrittle
Mohs scale hardness3.75–4.25
LusterVitreous, may be silky to pearly
StreakWhite
DiaphaneityTranslucent to subtranslucent
Specific gravity3.96
Optical propertiesUniaxial (−)
Refractive indexnω = 1.875
nε = 1.633
Birefringenceδ = 0.242
DispersionStrong
References[2][3][4]

Siderite is a mineral composed of iron(II) carbonate (FeCO3). Its name comes from the Ancient Greek word σίδηρος (sídēros), meaning "iron". A valuable iron ore, it consists of 48% iron and lacks sulfur and phosphorus. Zinc, magnesium, and manganese commonly substitute for the iron, resulting in the siderite-smithsonite, siderite-magnesite, and siderite-rhodochrosite solid solution series.[3]

Siderite has Mohs hardness of 3.75 to 4.25, a specific gravity of 3.96, a white streak and a vitreous lustre or pearly luster. Siderite is antiferromagnetic below its Néel temperature of 37 K (−236 °C) which can assist in its identification.[5]

It crystallizes in the trigonal crystal system, and are rhombohedral in shape, typically with curved and striated faces. It also occurs in masses. Color ranges from yellow to dark brown or black, the latter being due to the presence of manganese.

Siderite is commonly found in hydrothermal veins, and is associated with barite, fluorite, galena, and others. It is also a common diagenetic mineral in shales and sandstones, where it sometimes forms concretions, which can encase three-dimensionally preserved fossils.[6] In sedimentary rocks, siderite commonly forms at shallow burial depths and its elemental composition is often related to the depositional environment of the enclosing sediments.[7] In addition, a number of recent studies have used the oxygen isotopic composition of sphaerosiderite (a type associated with soils) as a proxy for the isotopic composition of meteoric water shortly after deposition.[8]

Carbonate iron ore

Although carbonate iron ores, such as siderite, have been economically important for steel production, they are far from ideal as an ore.

Their hydrothermal mineralisation tends to form them as small ore lenses, often following steeply dipping bedding planes.[i] This makes them not amenable to opencast working, and increases the cost of working them by mining with horizontal stopes.[10] As the individual ore bodies are small, it may also be necessary to duplicate or relocate the pit head machinery, winding engine and pumping engine, between these bodies as each is worked out. This makes mining the ore an expensive proposition compared to typical ironstone or haematite opencasts.[ii]

The recovered ore also has drawbacks. The carbonate ore is more difficult to smelt than a haematite or other oxide ore. Driving off the carbonate as carbon dioxide requires more energy and so the ore 'kills' the blast furnace if added directly. Instead the ore must be given a preliminary roasting step. Developments of specific techniques to deal with these ores began in the early 19th century, largely with the work of Sir Thomas Lethbridge in Somerset.[12] His 'Iron Mill' of 1838 used a three-chambered concentric roasting furnace, before passing the ore to a separate reducing furnace for smelting. Details of this mill were the invention of Charles Sanderson, a steel maker of Sheffield, who held the patent for it.[13]

These differences between spathic ore and haematite have led to the failure of a number of mining concerns, notably the Brendon Hills Iron Ore Company.[14]

Spathic iron ores are rich in manganese and have negligible phosphorus. This led to their one major benefit, connected with the Bessemer steel-making process. Although the first demonstrations by Bessemer in 1856 were successful, others' initial attempts to replicate his method infamously failed to produce good steel.[15] Work by the metallurgist Robert Forester Mushet showed that the reason for the discrepancy was the nature of the Swedish ores that Bessemer had innocently used; they were very low in phosphorus. Using a typical European high-phosphorus ore in Bessemer's converter gave a poor quality steel. To produce high quality steel from a high-phosphorus ore, Mushet realised that he could operate the Bessemer converter for longer, burning off all the steel's impurities including the unwanted phosphorus but also the carbon (which is an essential ingredient in steel), and then re-adding carbon, along with manganese, in the form of a previously obscure ferromanganese ore with no phosphorus, spiegeleisen.[15] This created a sudden demand for spiegeleisen. Although it was not available in sufficient quantity as a mineral, steelworks such as that at Ebbw Vale in South Wales soon learned to make it from the spathic siderite ores.[16] For a few decades, spathic ores were therefore in demand and this encouraged their mining. In time though, the original 'acidic' liner of the Bessemer converter, made from siliceous sandstone or ganister, was replaced by a 'basic' liner in the newer Gilchrist Thomas process. This removed the phosphorus impurities as slag produced by chemical reaction with the liner, and no longer required spiegeleisen. From the 1880s demand for the ores fell once again and many of their mines, including those of the Brendon Hills, closed soon after.

Gallery

Notes

  1. ^ Some siderite, along with goethite, also forms in bog iron deposits,[9] but these are small and economically minor.
  2. ^ Both ironstones and banded iron formations are sedimentary formations, thus the economically viable deposits may be considerable thicker and more extensive.[11]

References

  1. ^ Warr, L. N. (2021). "IMA–CNMNC approved mineral symbols". Mineralogical Magazine. 85 (3): 291–320. Bibcode:2021MinM...85..291W. doi:10.1180/mgm.2021.43. S2CID 235729616.
  2. ^ "Siderite". Handbook of Mineralogy: Borates, Carbonates, Sulfates (PDF). Tucson, Arizona: Mineral Data Publishing. 2003. ISBN 9780962209741. Archived from the original (PDF) on 13 March 2022. Retrieved 2022-11-30.
  3. ^ a b Siderite, Mindat.org, retrieved 2022-11-30
  4. ^ Siderite Mineral Data, WebMineral.com, retrieved 2022-11-30
  5. ^ Frederichs, T.; von Dobeneck, T.; Bleil, U.; Dekkers, M. J. (January 2003). "Towards the identification of siderite, rhodochrosite, and vivianite in sediments by their low-temperature magnetic properties". Physics and Chemistry of the Earth, Parts A/B/C. 28 (16–19): 669–679. Bibcode:2003PCE....28..669F. doi:10.1016/S1474-7065(03)00121-9.
  6. ^ Garwood, Russell; Dunlop, Jason A.; Sutton, Mark D. (2009). "High-fidelity X-ray micro-tomography reconstruction of siderite-hosted Carboniferous arachnids". Biology Letters. 5 (6): 841–844. doi:10.1098/rsbl.2009.0464. PMC 2828000. PMID 19656861.
  7. ^ Mozley, P. S. (1989). "Relation between depositional environment and the elemental composition of early diagenetic siderite". Geology. 17: 704–706.
  8. ^ Ludvigson, G. A.; Gonzalez, L. A.; Metzger, R. A.; Witzke, B. J.; Brenner, R. L.; Murillo, A. P.; White, T. S. (1998). "Meteoric sphaerosiderite lines and their use for paleohydrology and paleoclimatology". Geology. 26: 1039–1042.
  9. ^ Sedimentary Geology, p. 304.
  10. ^ Jones (2011), p. 34–35,37.
  11. ^ Prothero, Donald R.; Schwab, Fred (1996). Sedimentary Geology. New York: W. H. Freeman and Company. pp. 300–302. ISBN 0-7167-2726-9.
  12. ^ Jones, M. H. (2011). The Brendon Hills Iron Mines and the West Somerset Mineral Railway. Lightmoor Press. pp. 17–22. ISBN 9781899889-5-3-2.
  13. ^ GB 7828, Charles Sanderson, "Smelting Iron Ores", issued October 1838 
  14. ^ Jones (2011), p. 99.
  15. ^ a b Jones (2011), p. 16.
  16. ^ Jones (2011), p. 158.
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Siderite
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