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Manure nitrogen (N) mineralization is the process that converts organic N to plant available N and is influenced by environmental and soil factors. Field and laboratory incubation studies were conducted to determine the N mineralization and fertilizer equivalence of locally available manures. Available N from solid beef manure amendments (SBM) increased as the studies progressed due to mineralization. Liquid swine manure (LSM) behaved similarly to commercial fertilizer with high initial concentrations of ammonium N which declined continuously as the studies progressed. Manure N mineralization varied significantly (p<0.01) due to the influence soil moisture, manure types and study period as well as their interaction. The fertilizer equivalence of SBM in loamy soil was initially low compared to LSM and finally approached 80 % of ammonium nitrate fertilizer. These studies suggested that manure N mineralization requires emphasis on the initial form of N in manures besides soil moisture, soil temperature, and aeration.

The Kemess North porphyry Au-Cu-Mo deposit (300 Mt resource @ 0.30 g/t Au and 0.16% Cu)i s situated in the Toodoggone district, along the eastern margin of the Stikinia terrane in British Columbia. Mineralization is genetically related to the ca. 202 Ma, moderately SE-plunging, Kemess North diorite and is also hosted by proximal Takla Group basalt country rock. The nearby 202.7 ± 1.9 Ma Sovereign diorite has a comparable emplacement age, mineralogy, and chemistry to the Kemess North diorite, but is unmineralized. Toodoggone Formation volcaniclastic rocks (199.1 ± 0.3 Ma) crop out as prominent N-trending ridges or as isolated, fault-bounded blocks within Takla Group basalt. The unmineralized, (197.3 + 1.1/0.9 Ma) Duncan pluton intrudes Takla Group basalt. Seven vein types are separated into four stages of formation with respect to Au-Cu-Mo mineralization. Early-stage veins include magnetite stringer veins and later quartz-magnetite-pyrite + chalcopyrite + molybdenite veins. These veins are restricted mainly to the diorite, are associated with locally preserved potassic (biotite) alteration, and resulted in most of the Au-Cu-Mo mineralization at Kemess North. Main-stage quartz-pyrite + chalcopyrite ± molybdenite veins are the most abundant vein type and are present in the diorite and proximal Takla Group basalt. The veins are associated with phyllic (sericite-quartz) alteration and have a Re-Os molybdenite age of 201.8 ± 1.2 Ma. Late-stage pyrite-chalcopyrite and anhydrite ± pyrite ± chalcopyrite veins and associate phyllic (sericite-chlorite-pyrite) alteration occur in diorite and Takla Group country rocks. Lastly, post-mineralizationan hydrite and carbonate-zeolite veins cut all rocks. Fluid inclusion studies indicate that early-and main-stage ore fluids deposited Au-Cu-Mo at similar temperatures (about 400°C to 375°C) and pressures (0.9 to 3.0 kbar), corresponding to crustal depths of 3 to 10 km. Sulfur and Pb isotope compositions suggest that metals from the early-stage fluid were derived from the Kemess North diorite; metals in the main-stage fluid were derived from the diorite and probably Takla Group country rock and meteoric fluids. An E-striking, steeply S-dipping fault truncates the northern extremity of the ore body. Late NW- to NE-striking normal faults vertically displace the deposit resulting in graben-and-horst block shuffling of the stratigraphy.

The Kemess North porphyry Au-Cu-Mo deposit (300 Mt resource @ 0.30 g/t Au and 0.16% Cu)i s situated in the Toodoggone district, along the eastern margin of the Stikinia terrane in British Columbia. Mineralization is genetically related to the ca. 202 Ma, moderately SE-plunging, Kemess North diorite and is also hosted by proximal Takla Group basalt country rock. The nearby 202.7 ± 1.9 Ma Sovereign diorite has a comparable emplacement age, mineralogy, and chemistry to the Kemess North diorite, but is unmineralized. Toodoggone Formation volcaniclastic rocks (199.1 ± 0.3 Ma) crop out as prominent N-trending ridges or as isolated, fault-bounded blocks within Takla Group basalt. The unmineralized, (197.3 + 1.1/0.9 Ma) Duncan pluton intrudes Takla Group basalt. Seven vein types are separated into four stages of formation with respect to Au-Cu-Mo mineralization. Early-stage veins include magnetite stringer veins and later quartz-magnetite-pyrite + chalcopyrite + molybdenite veins. These veins are restricted mainly to the diorite, are associated with locally preserved potassic (biotite) alteration, and resulted in most of the Au-Cu-Mo mineralization at Kemess North. Main-stage quartz-pyrite + chalcopyrite ± molybdenite veins are the most abundant vein type and are present in the diorite and proximal Takla Group basalt. The veins are associated with phyllic (sericite-quartz) alteration and have a Re-Os molybdenite age of 201.8 ± 1.2 Ma. Late-stage pyrite-chalcopyrite and anhydrite ± pyrite ± chalcopyrite veins and associate phyllic (sericite-chlorite-pyrite) alteration occur in diorite and Takla Group country rocks. Lastly, post-mineralizationan hydrite and carbonate-zeolite veins cut all rocks. Fluid inclusion studies indicate that early-and main-stage ore fluids deposited Au-Cu-Mo at similar temperatures (about 400°C to 375°C) and pressures (0.9 to 3.0 kbar), corresponding to crustal depths of 3 to 10 km. Sulfur and Pb isotope compositions suggest that metals from the early-stage fluid were derived from the Kemess North diorite; metals in the main-stage fluid were derived from the diorite and probably Takla Group country rock and meteoric fluids. An E-striking, steeply S-dipping fault truncates the northern extremity of the ore body. Late NW- to NE-striking normal faults vertically displace the deposit resulting in graben-and-horst block shuffling of the stratigraphy.

The Kemess North porphyry Au-Cu-Mo deposit (300 Mt resource @ 0.30 g/t Au and 0.16% Cu)i s situated in the Toodoggone district, along the eastern margin of the Stikinia terrane in British Columbia. Mineralization is genetically related to the ca. 202 Ma, moderately SE-plunging, Kemess North diorite and is also hosted by proximal Takla Group basalt country rock. The nearby 202.7 ± 1.9 Ma Sovereign diorite has a comparable emplacement age, mineralogy, and chemistry to the Kemess North diorite, but is unmineralized. Toodoggone Formation volcaniclastic rocks (199.1 ± 0.3 Ma) crop out as prominent N-trending ridges or as isolated, fault-bounded blocks within Takla Group basalt. The unmineralized, (197.3 + 1.1/0.9 Ma) Duncan pluton intrudes Takla Group basalt. Seven vein types are separated into four stages of formation with respect to Au-Cu-Mo mineralization. Early-stage veins include magnetite stringer veins and later quartz-magnetite-pyrite + chalcopyrite + molybdenite veins. These veins are restricted mainly to the diorite, are associated with locally preserved potassic (biotite) alteration, and resulted in most of the Au-Cu-Mo mineralization at Kemess North. Main-stage quartz-pyrite + chalcopyrite ± molybdenite veins are the most abundant vein type and are present in the diorite and proximal Takla Group basalt. The veins are associated with phyllic (sericite-quartz) alteration and have a Re-Os molybdenite age of 201.8 ± 1.2 Ma. Late-stage pyrite-chalcopyrite and anhydrite ± pyrite ± chalcopyrite veins and associate phyllic (sericite-chlorite-pyrite) alteration occur in diorite and Takla Group country rocks. Lastly, post-mineralizationan hydrite and carbonate-zeolite veins cut all rocks. Fluid inclusion studies indicate that early-and main-stage ore fluids deposited Au-Cu-Mo at similar temperatures (about 400°C to 375°C) and pressures (0.9 to 3.0 kbar), corresponding to crustal depths of 3 to 10 km. Sulfur and Pb isotope compositions suggest that metals from the early-stage fluid were derived from the Kemess North diorite; metals in the main-stage fluid were derived from the diorite and probably Takla Group country rock and meteoric fluids. An E-striking, steeply S-dipping fault truncates the northern extremity of the ore body. Late NW- to NE-striking normal faults vertically displace the deposit resulting in graben-and-horst block shuffling of the stratigraphy. / Science, Faculty of / Earth, Ocean and Atmospheric Sciences, Department of / Graduate

The Great Gossan Lead is a Ne-Sw trending belt of sulfide mineralization extending over 28 kilometers through Carroll and Grayson Counties in southwestern Virginia. The zone, which occurs in the metamorphic Late Precambrian Ashe formation, consists of a series of an echelon mineralized pods which pinch and swell irregularly along strike and are essentially concordant with the foliation. Ore mineralogy is dominated by hexagonal pyrrhotite with minor amounts of sphalerite and chalcopyrite. All other phases--galena, arsenopyrite, pyrite, cubanite, mackinawite, tetrahedrite, stannite, and native bismuth--are disseminated throughout the ores. Pyrite is locally common as corroded primary euhedrae in some are bodies. Sphalerite occurs as disseminated anhedral aggregates commonly containing oriented lamellae and blebs of chalcopyrite and pyrrhotite. Chalcopyrite and galena occur as disseminated grains and as veinlets squeezed into fractured gangue minerals. A strongly developed metamorphic fabric, the absence of mineral zoning, and the presence of a zone of iron depletion surrounding the ores indicate that the ores and host rocks have been subject to the same metamorphism. At a thermal maximum of 4l5-455°C, the ore assemblage would have developed a sulfur activity of approximately 10-9 to 10-7 atm. and would have been subject to an oxygen activity of about 10 -25 to 10 -27 atm. The Great Gossan Lead is interpreted to have formed either as synsedimentary deposits or massive pyritic volcanism. Later metamorphism to the epidote-amphibolite facies and subsequent deformation roduced the present mineral assemblage and deformation features. / Master of Science

Orientador: Jose Mauro Granjeiro / Tese (doutorado) - Universidade Estadual de Campinas, Instituto de Biologia / Made available in DSpace on 2018-08-14T17:09:02Z (GMT). No. of bitstreams: 1 Paiva_KatiuciaBatistadaSilva_D.pdf: 3483379 bytes, checksum: 7c286d954d5465463a66555914cbdafc (MD5) Previous issue date: 2007 / Resumo: O objetivo deste trabalho foi delinear o perfil de expressão temporal e espacial das MMP-2 e -9, TIMP-1 e -2 e RECK durante os eventos de formação de tecidos mineralizados (osso, esmalte e dentina) em camundongos em fase embrionária, recém nascidos e indivíduos adultos através de imunohistoquímica e hibridização in situ. Durante a amelogênese em incisivos de rato adulto, na fase de secreção, as MMPs e RECK foram imunocoradas na região infracelular dos ameloblastos de secreção e RECK foi ainda detectado difuso no citoplasma destas células. MMP-9 foi localizada nas células do retículo estrelado e RECK nas células do epitélio externo. Na fase de transição, detectados uma fraca imunomarcação ao nível da membrana dos ameloblastos de transição para as MMPs e RECK esteve difuso no citoplasma destas células. Na camada papilar, as MMPs e RECK foram imunomarcadas nos macrófagos ou células dendríticas. Do início ao final da fase de maturação, a expressão de RECK foi aumentando nos ameloblastos de maturação e nas células da camada papilar, enquanto que a expressão das MMPs foi diminuindo nestas células. AS TIMPs foram detectadas somente nos ameloblastos na fase de maturação. Nós observamos RECK e a MMP-9 no citoplasma do odontoblastos, provavelmente, no complexo de Golgi ou na rede do retículo endoplasmático rugoso. Durante a ossificação intramembranosa da mandíbula e maxila, os osteoblastos foram imunocorados pelas MMPs, TIMPs e RECK. Na degradação da cartilagem de Meckel, MMPs, TIMPs e RECK foram imunomarcadas nas células do pericôndrio, bem como o mRNA de RECK. Durante a odontogênese, RECK foi imunocorado nas células do epitélio oral migrando ao ecto-mesênquima, na fase de broto, no epitélio interno do órgão do esmalte, na fase de capuz e em odontoblastos e ameloblastos na fase final de campânula. Transcritos de RECK foram localizados em todo o germe dentário na fase de capuz, mais concentrado no nó-do-esmalte secundário, na fase de campânula inicial e nos odontoblastos e ameloblastos, na fase final de campânula. O osso alveolar foi marcado em todos os períodos. Durante a ossificação endocondral, os condrócitos foram imunopositivos para as MMPs, TIMPs e RECK, na fase de diferenciação dos condrócitos (E13). Na fase de molde cartilaginoso (E14) os condrócitos hipertróficos foram imunocorados para as MMPs e RECK. RECK e TIMPs foram também encontradas no pericôndrio. Na fase de invasão vascular e celular (E15), MMPs, TIMPs e RECK foram expressos por células que migram do colar ósseo para o centro da diáfise, bem como por osteoclastos/condroclastos próximos ao septo transverso. Os condrócitos hipertróficos continuam imunocorados. De E16 a PN1, as MMPs, TIMPs e RECK foram expressas por osteoblastos e condrócitos hipertróficos na placa de crescimento e pelas células do periósteo e pericôndrio. Os resultados obtidos apontam para a expressão diferenciada de MMPs, TIMPs e RECK nos diversos eventos estudados, sugerindo que a atividade biológica destas proteínas regula a degradação da matriz extracelular tanto durante o desenvolvimento dos tecidos como sua manutenção. Além disso, pela primeira vez, demonstra-se a expressão de RECK pelas células formadoras de tecido ósseo e dentário. / Abstract: Our objective was to analyse the spatial-temporal distribution of MMP-2, MMP-9, TIMP-1, TIMP-2 and RECK during development of mineralized tissue (bone, enamel, and dentine) in embryos, newborn, and adult mice by immunohistochemistry and in situ hybridization. During rat amelogenesis, at the secretion phase, MMPs and RECK were immunostained in the ameloblast infracelular region and RECK was also detected in the cytoplasm of these cells. MMP-9 was localized in the stellated cells and RECK in the outer enamel epithelium cells. At the transition phase, a weak immunostaining was observed at the ameloblast membranes for MMPs and RECK. RECK was also detected in the cytoplasm of these cells. At the papillary layer, MMPs and RECK have been observed in macrophages and/or dendritic cells. At early and late maturation phases, MMPs and Reck profiles were similar to the transition phase, but the immunostaining was less pronounced. TIMPs were identified exclusively in maturation ameloblasts throughout the maturation phase. We also observed that the cytoplasm of odontoblasts, probably at the Golgi apparatus and/or the RER network were immunostained for Reck and MMP-9. During mandible and maxillae intramembranous ossification, osteoblasts were immunostained for MMPs (early stage), TIMPs (late stage) and RECK. In Meckel cartilage degradation, MMPs, RECK and TIMPs mRNA and protein were found in perichondrial cells. During odontogenesis migrating epithelial cells in bud stage, enamel inner epithelial cells in cap stage, and ameloblasts and odontoblasts in bell stage were immunostained for RECK. Also, RECK mRNA was found difuse in all tooth germ in cap stage, mainly localized in primary enamel knout in early bell stage, and in ameloblasts and odontoblasts in late bell stage. The alveolar bone was immunolabelled in all periods. During endochondral ossification, chondrocytes were immunopositive for MMPs, RECK, and TIMPs during chondrocyte differentiation (E13). At the cartilaginous template (E14), the hypertrophic chondrocytes (HC) were immunostained for MMPs and RECK. RECK and TIMPs immunopositive cells were found in the perichondrium. At the vascular and cellular invasion (E15), MMPs, RECK and TIMPs were expressed by migrating cells from bone collar as well as by osteoclasts/chondroclasts close to the transverse septum. HC remained immunostained. From E16 to PN1, MMPs, TIMPs, and RECK were expressed by osteoblasts and HC in the growth plate and by cells in the perichondrium and periosteum. The results show the differential expression of MMPs, TIMPs, and RECK during the processess studied, sugesting that the biological activity these proteins regulates the MEC degradation and its maintenance in tissue development. Our results show for the first time that RECK is expressed by bone-forming and tooth-forming cells during mouse endochondral and intramembranous and in embryonic and adult odontogenesis, even if these cells are from different embryonic origins. / Doutorado / Bioquimica / Doutor em Biologia Funcional e Molecular

The Kalplats platinum group metal deposit is located in the Northwestern Province of South Africa, 80 km southwest of Mafikeng, in the Stella Layered Intrusion. The Stella Layered Intrusion intruded into the Kraaipan Greenstone Belt and is dated at 3.03 billion years. The Kraaipan Greenstone Belt is host to the 80 000 ounce per annum Kalgold Gold Mine. Platinum Group Element mineralized layers in the Stella Layered Intrusion are interpreted to occur in the overturned western limb of folds, formed by an eastward vergent compressional event. Three major reefs have been identified, namely the Lower Grade (LG) reef, the Mid Reef and the Main Reef. High grade reefs occur within these three. The average Pt:Pd ratio of the Main Reef is 1:1. Highest total precious metals content is concentrated in the Upper Main and Lower Main Reefs and the average grade for these two reefs is 4g/t. Open pit mining is suggested. The total inferred precious metals resource equates to 84Mt at an average grade of 1.4 g/t Pt+Pd+Au, for 3.9million ounces. Platinum, palladium and gold occur as fine grains. Maximum recoveries of approximately 72% are possible, from sulphide ore, using a twostage mill-float circuit. The estimated reserve (non-JORC compliant) is 26 Mt at an average grade of 2.01g/t Pt+Pd+Au, for 1.68 million ounces. A financial evaluation was done on the viability of the Kalplats deposit, using a discounted cash flow model. Future projections used were a R/$ exchange rate of R6-50 to the dollar and long-term metals prices of US$ 800/oz Pt, US$ 200/oz Pd and US$ 400/oz Au. The result of the discounted cash flow model was negative and indicated no return on capital and a negative Nett Present Value (NPV) of –R206 million at a discount of 13%. Factors impacting negatively on the viability of the project, include grade, metallurgical recovery, smelter fees, government royalties, metals prices and the Rand-US$ exchange rate. / Dissertation (MSc (Geology))--University of Pretoria, 2008. / Geology / unrestricted

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L’imagerie du petit animal est incontournable pour le développement des recherches dans les secteurs de labiologie, de la médecine et de l’industrie pharmaceutique. Parmi les différentes modalités d’imagerie développéeschez l’humain et adaptées à l’animal, l’imagerie tomographique à rayons X est devenue une référencepour l’analyse des caractères anatomiques et phénotypiques chez la souris. Elle permet de réaliser des étudeslongitudinales in vivo et des analyses haute résolution ex vivo de façon non invasives et en 3D. L’analyse deces images 3D nécessite des outils spécifiques à chaque problématique.Dans ce contexte, notre travail de thèse a permis d’apporter des contributions sur les thématiques suivantes :1. le développement d’outils d’analyse, à la fois quantitatifs et qualitatifs, pour l’imagerie des tissusminéralisés et adipeux2. l’application des méthodologies développées à des problématiques de recherche biomédicale3. l’étude comparative et "multi-échelle" de différentes technologies de tomographie X pour l’imagerie dupetit animal4. la mise au point d’une méthode originale par résonnance paramagnétique électronique pour la dosimétried’un acte d’imagerie X chez le petit animalEn conclusion, les outils d’imagerie 3D que nous avons développés représentent un nouvel apport pour la dissectionvirtuelle de l’animal de laboratoire, permettant l’exploration de nombreux tissus et organes et rivalisantavec les méthodes d’histologie et de microscopie électronique.L’application de ces méthodes d’imagerie pour la recherche fondamentale et pré-clinique ouvre la perspectived’une alternative nouvelle dans l’expérimentation animale. / Small animal imaging is highly necessary for the development of biomedical research and pharmaceuticalapplications. Amongst various available imaging methods, X-Ray tomography is now considered as a goldstandard for anatomical and phenotypical analysis in mice. CT imaging allows non invasive longitudinal studiesin vivo and high resolution analysis ex vivo. The 3D image analysis requires the development of specific toolsdepending on the biomedical problematics.In this context, we have investigated the following research areas :1. Development of 3D image tools for qualitative and quantitative image analysis of mineralized andadipose tissues in murin models2. Application of our tools to biomedical investigations3. Comparative and multi-scale analysis of various tomography technologies for small animal imaging4. Development of an original method using Electronic Paramagnetic Resonance (EPR) for X-ray dosimetryin miceIn conclusion, our 3D imaging methods are potentially of high interest for the virtual dissection of laboratoryanimals, allowing extended analysis of various tissues and organs complementary to standard histological andmicroscopic approaches.