Jarosite crystals from Sierra Peña Blanca, Aldama, Chihuahua, Mexico (5.6 × 3.1 × 1.6 cm)
Jarosite has a trigonal crystal structure and is brittle, with basal cleavage, a hardness of 2.5–3.5, and a specific gravity of 3.15–3.26. It is translucent to opaque with a vitreous to dull luster, and is colored dark yellow to yellowish-brown. It can sometimes be confused with limonite or goethite with which it commonly occurs in the gossan (oxidized cap over an ore body). Jarosite is an iron analogue of the potassium aluminium sulfate, alunite.
Solid solution series
The alunite supergroup includes the alunite, jarosite, beudantite, crandallite and florencite subgroups. The alunite supergroup minerals are isostructural with each other and substitution between them occurs, resulting in several solid solution series. The alunite supergroup has the general formula AB3(TO4)2(OH)6. In the alunite subgroup B is Al, and in the jarosite subgroup B is Fe3+. The beudantite subgroup has the general formula AB3(XO4)(SO4)(OH)6, the crandallite subgroup AB3(TO4)2(OH)5•H2O and the florencite subgroup AB3(TO4)2(OH)5 or 6.
Crystal structure of jarosite Color code: Potassium, K: purple; Sulfur, S: olive; Iron, Fe: violet-blue; Cell: sky-blue.
In the jarosite-alunite series Al may substitute for Fe and a complete solid solution series between jarosite and alunite, KAl3(SO4)2(OH)6, probably exists, but intermediate members are rare. The material from Kopec, Czech Republic, has about equal Fe and Al, but the amount of Al in jarosite is usually small.
When jarosite forms from pyriteoxidation in sedimentary clays, the main sources of K+ are illite, a non-swelling clay, or K-feldspar. In other geological settings mica's alteration can also be a source of potassium.
In the jarosite-natrojarosite series Na substitutes for K to at least Na/K = 1:2.4 but the pure sodium end member NaFe3(SO4)2(OH)6 is not known in nature. Minerals with Na > K are known as natrojarosite. End member formation (jarosite and natrojarosite) is favoured by a low temperature environment, less than 100 °C, and is illustrated by the oscillatory zoning of jarosite and natrojarosite found in samples from the Apex Mine, Arizona, and Gold Hill, Utah. This indicates that there is a wide miscibility gap between the two end members,[5] and it is doubtful whether a complete series exists between jarosite and natrojarosite.
In hydroniumjarosite[6] the hydronium ion H3O+ can also substitute for K+, with increased hydronium ion content causing a marked decrease in the lattice parameter c, although there is little change in a.[7] Hydroniumjarosite will only form from alkali-deficient solutions, as alkali-rich jarosite forms preferentially.
Divalent cations may also substitute for the monovalent cation K+ in the A site.[8] Charge balance may be achieved in three ways.
Firstly by replacing two monovalent cations by one divalent cation, and leaving an A site vacancy, as in plumbogummite, Pb2+Al3(PO4)2(OH)5.H2O, which is a member of the crandallite subgroup.
Secondly by incorporating divalent ions in the B sites, as in osarizawaite, Pb2+Cu2+Al2(SO4)2(OH)6, alunite subgroup, and beaverite, Pb2+Cu2+(Fe3+,Al)2(SO4)2(OH)6, jarosite subgroup.
Thirdly by replacing divalent anions with trivalent anions, as in beudantite, PbFe3+3(AsO4)3−(SO4)(OH)6, beudantite subgroup.
History
Jarosite was first described in 1852 by August Breithaupt in the Barranco del Jaroso in the Sierra Almagrera (near Los Lobos, Cuevas del Almanzora, Almería, Spain). The name jarosite is directly derived from "jara", the Spanish name of a yellow flower that belongs to the genus Cistus and grows in the sierra. The mineral and the flower have the same color.
Mysterious spheres of clay, 1.5 to 5 inches (40 to 125 mm) in diameter and covered with jarosite, have been found beneath the Temple of the Feathered Serpent, an ancient six-level stepped pyramid 30 miles (50 km) from Mexico City.[9]
Mars exploration
Ferric sulfate and jarosite have been detected by three martian rovers: Spirit, Opportunity and Curiosity. These substances are indicative of strongly oxidizing conditions prevailing at the surface of Mars. In May 2009, the Spirit rover became stuck when it drove over a patch of soft ferric sulfate that had been hidden under a veneer of normal-looking soil.[10]
Because iron sulfate has very little cohesion, the rover's wheels could not gain sufficient traction to pull the body of the rover out of the iron sulfate patch. Multiple techniques were attempted to extricate the rover, but the wheels eventually sank so deeply into the iron sulfate that the body of the rover came to rest on the Martian surface, preventing the wheels from exerting any force on the material below them. As the JPL team failed to recover the mobility of Spirit, it signified the end of the journey for the rover.
Antarctica deep borehole
On Earth, jarosite is mainly associated with the ultimate stage of pyrite oxidation in clay environment, and can also be found in mine tailings waste where acidic conditions prevail. Against all expectations, jarosite has also been fortuitously discovered in minute quantities in the form of small dust particles in ice cores recovered from a deep borehole in Antarctica. That surprising discovery was made by geologists who were searching for specific minerals capable of indicating ice age cycles within the layers of a 1620-meter-long ice core.[11] Geologists speculate that jarosite dust could also have accumulated within ice in glaciers on Mars.[12] However, that hypothesis is a matter of controversy because, on Mars, jarosite deposits can be very thick (up to 10 meters). However, Mars is also a very dusty planet and, in the absence of plate tectonics on Mars, glacial dust deposits might have accumulated over long periods of time.
^Anthony, John W.; Bideaux, Richard A.; Bladh, Kenneth W.; Nichols, Monte C. (2005). "Jarosite"(PDF). Handbook of Mineralogy. Mineral Data Publishing. Retrieved 14 March 2022.
^Wills, A. S.; Harrison, A.; Ritter, C.; Smith, R.; et al. (2000). "Magnetic properties of pure and diamagnetically doped jarosites: Model kagomé antiferromagnets with variable coverage of the magnetic lattice". Phys. Rev. B. 61 (9): 6156–6169. Bibcode:2000PhRvB..61.6156W. doi:10.1103/PhysRevB.61.6156.
Palache C., Berman H., and Frondel C. (1951) Dana's system of mineralogy, (7th edition), v. II, 560–562.
