All the warm deserts of the world exhibit gypsum crusts in favourable localities, generally areas with a source of gypsum and less than 250 mm of rainfall annually. The features, comprising loose powdery or cemented crystalline accumulations of calcium sulphate dihydrate, are found at the surface or within the uppermost 10 m of regolith. Thicknesses vary from a few millimetres to several metres and purities range from about 15% to nearly 100% gypsum. A review of the literature on gypsum soils and crusts reveals that the classification of types requires both standardizing and simplifying. A preliminary classification of crusts into three types can be made on the basis of structural and stratigraphic characteristics of examples from southern Tunisia and the Central Namib Desert. The types consist of subaerial aqueous evaporites, two subsurface and three surface forms. Detailed physical and chemical analyses justify a broadly similar genetic classification though one subsurface form is believed to be a primary pedogenic type of which the surface forms represent relics at various stages of solutional deterioration. Examples of subaerial aqueous evaporites are all products of shallow-water sedimentation in seasonally flooded chotts and sabkhas. The non-pedogenic subsurface type, croûte de nappe, is produced by displacive crystallization at the surface of a fluctuating water table. Gypsum precipitation results from either evaporation or mixing of saline waters causing saturation with respect to gypsum. Surface gypsum crusts are subsurface illuvial accretions exposed by erosion of overlying material. The gypsum is derived from solution of surface aeolian, atmospheric, colluvial or alluvial deposits by meteoric waters which percolate into the upper soil zone replenishing the antecedent soil moisture deficit. Subsurface accumulation results from displacive crystallization at host sediment grain contacts when gypsum saturated soil moisture evaporates.

In this thesis, column experiments were conducted in order to determine the effect of irrigation with local groundwater on mobilization of lead and zinc in 50 years old sulfate-acid mine tailings. In addition, the influence of soluble oxalic acid, a common rhizosphere organic acid, was assessed by varying its concentration across an environmentally relevant range. In general, metal contaminant dissolution was not affected by the presence of oxalic acid. In both tailings, Zn mobilization was higher than Pb suggesting the presence of more kinetically labile Zn phases, regardless of the treatment used. Lead mobilization was also low because effluent solutions were near to equilibrium conditions with respect to gypsum, preventing Pb dissolution from Pb-sulfate minerals. Geochemical modeling also indicated that lead release was controlled by anglesite and plumbojarosite dissolution. Zinc release appears to be controlled by Zn-talc and goslarite.

Thesis (M.S.)--University of Missouri-Columbia, 2004. / Typescript. Includes bibliographical references (leaves 24-25). Also available on the Internet.

Thesis (Ph. D.)--University of California, Riverside, 2009. / Includes abstract. Includes bibliographical references. Issued in print and online. Available via ProQuest Digital Dissertations.

This study investigates jarosite formation and stability patterns at the abandoned Davis Pyrite Mine in Rowe, Massachusetts. Jarosite, an iron-sulfate hydroxide, is found in acid mine drainage (AMD) environments, in acid sulfate soils, and on Mars. Jarosite and the iron oxides goethite and hematite are present at the site. Soil samples from the site were examined by XRD, SEM, and EDS. Five mineralogical areas were found, based on mineral abundance patterns. Jarosite exists in four of these areas. Two jarosite morphologies were identified. “Variable” jarosite, with partly-dissolved crystals of about 0.5 to 5 micrometers diameter, exists in spoil pile samples. “Donut” jarosite, with tightly-packed, sharp-edged crystals less than 0.5 micrometers that form a thin mantle on the surface of a second mineral, exists in native soil samples. Donut jarosite has not been previously characterized. These jarosite morphologies are controlled by the presence and relative mobility of pyrite oxidation products Fe and SO4, which in turn are controlled by water saturation levels. Three pathways are possible. On Path 1, both ions are mobile, go into solution, and variable jarosite forms at a distance from the pyrite source. On Path 2, only sulfur ions are mobile, an iron-oxide gossan develops. No jarosite forms. On Path 3, neither ion is mobile, and donut jarosite forms. On this path, Fe and SO4 ions are trapped in a thin film of stagnant water covering the pyrite. When sufficient ions are present, donut jarosite precipitates.

Submitted by Mery Piedad Zamudio Igami (mery@ipen.br) on 2017-03-10T16:36:15Z No. of bitstreams: 0 / Made available in DSpace on 2017-03-10T16:36:15Z (GMT). No. of bitstreams: 0 / O fertilizante fosfatado brasileiro é obtido pela reação por via úmida da rocha fosfática de origem ígnea com ácido sulfúrico concentrado, obtendo como produto final, o ácido fosfórico e como resíduo, o fosfogesso, que é estocado em pilhas, a céu aberto, junto às instalações produtoras. Parte do fosfogesso vem sendo utilizada na agricultura como condicionador de solos, devido a sua alta solubilidade, podendo melhorar a estrutura do solo, reduzir a erosão do solo, aumentar os níveis de enxofre e fósforo disponíveis e melhorar a composição dos fertilizantes. Mas a presença de radionuclídeos e metais no fosfogesso impõem restrições sobre o uso na agricultura. Para garantir uma utilização segura, é importante estimar a lixiviação dos radionuclídeos e metais presente no fosfogesso. O objetivo deste trabalho foi estudar a disponibilidade dos radionuclídeos relevantes do ponto de vista radiológico (238U, 232Th, 226Ra, 228Ra, 210Pb e 210Po) e dos metais (As, Cd, Cr, Ni, Se, Hg e Pb) presentes no fosfogesso de procedência brasileira, levando em consideração sua aplicação em solo agricultável. Para esta finalidade, foi desenvolvido um protocolo experimental em escala de laboratório, no qual colunas foram preenchidas com misturas de solos arenosos e argilosos típicos brasileiros condicionados com fosfogesso. A essas colunas foi adicionada água, a fim de se alcançar uma extração branda desses elementos. Foi implantado um procedimento analítico para a determinação sequencial dos radionuclídeos de interesse na solução obtida na lixiviação. As frações disponíveis foram obtidas utilizando-se a razão entre as concentrações dos radionuclídeos no lixiviado e as concentrações dos radionuclídeos nas amostras de solo, solo condicionado com fosfogesso e fosfogesso. Os valores de concentração dos radionuclídeos 238U, 232Th, 226Ra, 228Ra, 210Pb e 210Po obtidos no fosfogesso das duas procedências variaram de 86 Bq kg-1 a 352 Bq kg-1. As concentrações de 226Ra e 228Ra obtidas no fosfogesso ficaram abaixo do limite máximo permitido pela resolução da Comissão Nacional de Energia Nuclear, atendendo às condições necessárias para o seu uso na agricultura. Os resultados obtidos para os metais As, Cd, Cr, Ni, Pb, Se e Hg no fosfogesso foram inferiores ao limite máximo para condicionador de solo e para fertilizantes estabelecidos pelo Ministério da Agricultura, Pecuária e Abastecimento, atendendo às condições necessárias para o seu uso na agricultura. Os radionuclídeos 226Ra, 210Pb, 210Po e 228Ra apresentaram frações disponíveis nos solos e solos condicionados com fosfogesso variando de 0,05% a 1,2%; para o 238U e 232Th as frações disponíveis apresentaram valores inferiores a 0,05%. Os metais apresentaram frações disponíveis nos solos e solos condicionados com fosfogesso variando de 0,05% a 1,07%. Os resultados obtidos para a fração disponível de metais e radionuclídeos no solo condicionado com fosfogesso demostraram que mesmo utilizando concentrações de fosfogesso dez vezes acima da dose recomendada, a disponibilização foi desprezível. Pode-se concluir que a utilização do fosfogesso como condicionador de solos é viável, no que concerne a disponibilidade dos metais e radionuclídeos estudados. / Tese (Doutorado em tecnologia Nuclear ) / IPEN/D / Instituto de Pesquisas Energéticas e Nucleares - IPEN-CNEN/SP

Les gisements uranifères nigériens sont localisés dans les formations carbonifères et jurassiques du bassin de Tim Mersoï. AREVA est actionnaire de 3 sites miniers de cette région: la SOMAÏR et la COMINAK dans le district d'Arlit, en exploitation depuis 50ans, et IMOURAREN, 80km plus au Sud, dont l'exploitation est programmée pour 2015. La minéralisation du gisement d'Imouraren est comprise dans la formation fluviatile du Tchirézrine 2 (Jurassique), formée de chenaux et de plaines d'inondation. Les faciès de remplissage de chenaux vont des grès grossiers aux grès très fins (cortège détritique : quartz et feldspaths), tandis que les faciès de débordement sont constitués d'analcimolites. La minéralogie secondaire est acquise lors de 2 évènements : 1- la diagenèse, avec formation de minéraux argileux, d'analcime, de quartz et d'albite secondaires, et 2- un épisode de circulations de fluides, qui induit une altération des minéraux détritiques et diagénétiques, la formation de nouvelles phases et le dépôt de l'uranium. Cette altération dessine une zonation minéralogique à l'échelle du gisement.L'hétérogénéité du Tchirézrine 2, tant au niveau des faciès que de la minéralogie, se perçoit lors du traitement du minerai, puisqu'il réagit différemment selon sa provenance, avec parfois des problèmes de récupération de l'U. Des essais de traitement de minerais, ont montré que analcimes et chlorites étaient les deux pénalisants, pour 3 raisons : 1- les piégeages des phases U au sein des analcimes, 2- la dissolution de ces 2 minéraux a tendance à faire sortir des conditions de solubilisation de l'U (pH et Eh) et à former de nombreux sulfates, 3- problèmes de percolation. Une méthode de détection des minerais riches en analcimes, basée sur la spectroscopie infrarouge, a été développée afin d'optimiser les mélanges de minerais et ainsi de réduire les effets néfastes des pénalisants lors du traitement. / Nigerian uraniferous deposits are located in carboniferous and jurassic formations of Tim Mersoï basin. AREVA is shareholder of 3 mine sites in this area: SOMAÏR and COMINAK, both in exploitation since 1960’s and IMOURAREN, 80km further South, whose exploitation is planned for 2015. Mineralization of Imouraren deposit is included in the fluvial formation of Tchirezrine 2 (Jurassic), composed of channels and flood plains. Facies of channel infillings range from coarse sandstones to siltstones, while overflow facies are composed of analcimolites.Secondary mineralogy was acquired during 2 stages: 1- diagenesis, with formation of clay minerals, analcime, secondary quartz and albites, and 2- stage of fluids circulations, which induced alteration of detrital and diagenetic minerals, formation of new phases and uranium deposition. A mineralogical zoning, at the scale of deposit resulted from this alteration. The heterogeneity of Tchirezrine 2, at the level of both facies and mineralogy, is also evidenced during ore treatment, as ore reacts differently depending on its source, with sometimes problems of U recovery. Ore treatment tests showed that analcimes and chlorites were both penalizing minerals, because of 1- the sequestration of U-bearing minerals into analcimes, 2- their dissolution which trends to move away from U solubilization conditions (pH and Eh) and to form numerous sulfates, and 3- problems of percolation. A detection method of analcime-rich ores, based on infrared spectroscopy, was developed in order to optimize ore blending and so to reduce negative effects during ore treatment process.