Carbonatos y otros minerales autigénicos asociados a las lateritas niquelíferas de Cerro Matoso y su posible relación con actividad hidrotermal y reducción de sulfatos

dc.contributorGuerrero Díaz, Javier
dc.creatorCastrillón Peña, Andrés
dc.date.accessioned2021-02-03T18:06:42Z
dc.date.available2021-02-03T18:06:42Z
dc.date.created2021-02-03T18:06:42Z
dc.date.issued2019-09-23
dc.identifierCastrillón A. (2019). Carbonatos y otros minerales autigénicos asociados a las lateritas niquelíferas de Cerro Matoso y su posible relación con actividad hidrotermal y reducción de sulfatos. Thesis Doctoral. Universidad Nacional de Colombia. 213p.
dc.identifierhttps://repositorio.unal.edu.co/handle/unal/79059
dc.description.abstractLa mineralogía, difractometría de rayos X y los valores disminuidos de isotópos de δ13C y δ18O de las arcillas y carbonatos que conforman el sustrato fosilífero en una parte del Pit-1 de Cerro Matoso-CM, indican que los filosilicatos y la siderita precipitaron en ambientes oceánicos. El carácter autigénico de los filosilicatos y las temperaturas registradas por estos y la siderita diagenética, permiten reportar la primera comunidad de ventilas hidrotermales en Colombia. Esta comunidad fósil, compuesta de gusanos siboglinidae, bivalvos y gasterópodos, entre otros, hace parte de una sucesión de sedimentos marinos que sobreyacen localmente las peridotitas de CM. Con estos resultados se propone un modelo más preciso para el desarrollo del depósito laterítico de níquel en CM, que incluye la influencia de un sistema hidrotermal Tipo II (Kelley & Shank, 2010), que se hospedó en las rocas ultramáficas cuando se exhumaron en el fondo oceánico, a través de fallas de transformación, formando lo que sería un oceanic core complex -OCC en la antigua dorsal meso-oceánica del Pacífico. Los sedimentos marinos, conformaron un perfil laterítico atípico en el Pit-1, que contenía las mayores concentraciones de níquel en el yacimiento (>8%). Al sur de la mina o Pit-2, las peridotitas desarrollaron, producto de la meteorización, un perfil laterítico típico, con concentraciones de níquel que no exceden el 4%. Filosilicatos de Fe (greenalita, berthierina, nontronita) y siderita, reconocidos en sección delgada e identificados por medio de XRD estándar, XRF y BSE-EDX, constituyen las principales asociaciones minerales en la sucesión de sedimentos en CM. Estos se distinguen en: sedimentos hidrotermales, conformados de base a tope por las facies: lodolitas fisuradas y brechadas (fb-M), arcillolitas fosilíferas verdes (gf-C) con abundantes concreciones de siderita (sC) y arcillolitas oxidadas cafés (bo-C). Lateralmente adyacentes o sobreyaciendo esta sucesión, se encuentran sedimentos metalíferos, conformados de base a tope por las facies: lodolitas conglomeráticas negras, con sus dos variedades (BCM I & BCM II), las cuales contienen intraclastos rojos y verdes bien cementados (gr-CC), además, fósiles y fragmentos serpentinizados de peridotitas; sobre estas rocas se encuentra a facies de arcillolitas rojas (RC) y la facies de arcillolitas naranjas con láminas de hierro (oil-C). Berthierina, greenalita, nontronita, goethita, y nimita se consideran de origen autigénico y de acuerdo con el Full Width at Half Maximum -FWMH, reflejan un alto grado de madurez ¨alta cristalinidad¨ asociados a temperaturas elevadas durante su precipitación. Debido a la influencia de la temperatura, siderita y magnetita tendrían un origen biogénico, en la que participan bacterias termófilas (>45°C) reductoras de hierro, que son usuales en los sistemas hidrotermales. Las condiciones propicias para la precipitación de los sedimentos marinos en CM, se dió en ambientes reductores, alcalinos, ricos en Fe y a temperaturas entre 20o y 160o C. Los valores disminuidos de δ13C (-27.1 to -5.57‰) y δ18O (-11.01‰ to -1.88‰), tienen la firma isotópica del metano - CH4 del sistema hidrotermal del que provienen, y están relacionados a eventos de oxidación de metano y/o una mezcla de CH4 con carbón inorgánico disuelto -DIC en el fondo del mar, los cuales favorecen el crecimiento de filosilicatos y carbonatos de Fe. La relación de dependencia del fraccionamiento de δ18O con la temperatura, descrita por Zhang et al. (2001) en la ecuación: 103 lnsid-wt = 2.56 * 106 T-2 (K) +1.69, proporciona una buena correlación lineal en los datos obtenidos en los sedimentos marinos de CM. Anomalías positivas de Eu y negativas de Ce en la facies lodolitas conglomeráticas negras, indican un origen asociado a la precipitación de plumas hidrotermales y registran la firma de la dilución de estos elementos en el fondo marino. Los procesos de serpentinización de rocas ultramáficas a profundidades abisales, generan cantidaes importantes de H2, que favorecen la síntesis de CH4 mediante la reacción tipo Fischer-Tropsch (FTT) (4H2 + CO2 => CH4 + 2H2O), y generan ambientes geoquímicos propicios para la instalación de comunidades extremófilas, en donde procesos de oxidación anaerobia de metano AOM son realzados por organismos oxidantes y/o reductores de sulfato, que intervienen en los procesos de precipitación mineral. El sistema hidrotermal Tipo II hospedado en las peridotitas de CM, alcanzó temperaturas alrededor de 150°C, en lugar de 300°C, lo que impidió que la energía del sistema fuese suficiente para generar cantidades importantes de sulfuros de Ni, como millerita o eventualmente pentlandita, por lo tanto, su aporte en Ni, es menor, comparado con el níquel encontrado en las particulas orgánicas fracción arcilla, en las arcillas (nimita) y en carbonatos. Una evidencia adicional de sistemas hidrotermales son la listvenitas usualmente infrayaciendo la facies de lodolitas conglomeráticas negras. Las concentaciones adicionales de Ni en CM provienen por lo tanto de los sedimentos metalíferos generados por el sistema hidrotermal Tipo II hospedado en la peridotitas, lo que hizo al depósito de CM especial, al compararlo con las cantidades habituales de níquel, que presentan rocas ultramáficas similares al ser sometidas a procesos de meteorización y lixiviación en condiciones supergénicas. Durante el Cretácico, todo el conjunto de rocas (ultramáficas y sedimentarias), se adosó al continente, para exhumarse finalmente durante la última fase de la Orogenia Andina. Esto expuso las peridotitas y rocas sedimentarias asociadas, al ambiente húmedo tropical, permitiendo que los procesos de enriquecimiento de Ni supergénico, conformaran el perfil de lateritas de CM como se conoce hoy en día, con sus extraordinariamente altos contenidos de Ni.
dc.description.abstractThe mineralogy, X-ray diffractometry and depleted isotope values of δ13C and δ18O of clays and carbonates forming the fossiliferous substrate at Pit-1 of Cerro Matoso -CM, indicate that phyllosilicates and siderite precipitated in oceanic environments. The authigenic phyllosilicates and diagenetic siderite record temperatures that allows to report the first hydrothermal vents community in Colombia. This fossil community, formed by siboglinidae, bivalves and gastropods, among others is part of a succession of marine sediments overlying locally the CM peridotites. With these results, a more precise model is proposed for the genesis of the nickel laterites of CM, which includes the influence of a hydrothermal system Type II (Kelley & Shank, 2010), hosted in the ultramafic rocks when were exhumed in the ocean deep through transformation faults, forming what would be an oceanic core complex -OCC at the ancient mid-oceanic Pacific Ridge. The marine sediments formed an atypical lateritic profile at Pit-1, with the highest concentrations of nickel in the mine (> 8%). To the south of the mine or Pit-2, the peridotites weathered developed a typical lateritic profile with nickel concentrations that do not exceed 4%. Fe_phyllosilicates (greenalite, berthierine, nontronite) and siderite recognized in thin section and identified by XRD, XRF and BSE-EDX, form up the mineral associations in the sedimentary sucession of CM. The sediments are described as: hydrothermal, formed from base to top by the facies: fissured and brecciated mudstone (fb-M), green fossiliferous claystone (gf-C), with abundant siderite (sC) concretions, brown oxidized claystone (bo-C). Laterally adjacent or overlaying this succession, metalliferous sediments are composed from base to top by the facies: black conglomeratic mudstone, with two varieties (BCM I & BCM II), which contain well-cemented red and green intraclasts (gr-CC), together with fossils and serpentinized fragments of peridotites; overlaying these facies, are the facies of red claystone (RC) and orange iron laminated claystone (oil-C). Berthierine, greenalite, nontronite, goethite, nimite, are considered authigenic in origin and according with the Full Width at Half Maximum -FWMH, reflect a high degree of maturity "high crystallinity" associated with high temperatures during their precipitation, due to the participation of thermophilic (> 45 ° C) bacteria that reduce iron, which are common in hydrothermal systems. The favorable conditions for the precipitation of marine sediments in CM, occurred in reducing, alkaline, Fe-rich environments at temperatures between 20o y 160o C. Depleted isotope values of δ13C (-27.1 to -5.57 ‰) and δ18O (-11.01 ‰ to -1.88 ‰), have the CH4 isotopic sign of an ancient hydrothermal system in CM and are related to methane oxidation events and/or a mixed with dissolved inorganic carbon -DIC at the deep sea, which favor the growth of Fe_phyllosilicates and carbonates. The dependence relationship of δ18O fractionation with the temperature described by Zhang et al. (2001) in the equation: 103 lnsid-wt = 2.56 * 106 T-2 (K) +1.69 provides a good linear correlation in the marine sediments of CM. Positive anomalies of Eu and negative of Ce, in the black conglomeratic mudstone facies, indicate an origin associated with the precipitation of hydrothermal plumes, signing the dilution of these elements on the seawater. The serpentinization processes in abyssal ultramafic rocks, produce important amounts of H2, favoring the CH4 synthesis according with Fischer-Tropsch (FTT) (4H2 + CO2 => CH4 + 2H2O) reactions, generating a geochemical environment, appropriated to installation of extremophilic communities, anaerobic oxidants methane -AOM or sulfate reducers organisms, which are involved in the mineral precipitation. The hydrothermal system Type II hosted in the CM peridotites, reach temperatures about 150 ° C instead 300 ° C, that block the necessary energy to generate significant amounts of Ni sulfides such as millerite or eventually pentlandite, therefore, its contribution in Ni is less, compared to the nickel found in organic agglomerates clay fraction, in clays (nimite) and carbonates. An additional evidence of a hydrothermal system are listvenites usually underlaying the black conglomeratic mudstone facies. The additional concentrations of Ni in CM come from the metalliferous sediments generated by hydrothermal system Type II hosted in the peridotites, which made the CM deposit special, when compared to the usual amounts of nickel that present similar ultramafic rocks, when are exposed to weathering and leaching processes under supergenic conditions. During Cretaceous, the whole rocks set (ultramafic and sediments) was accreted to the continent, to finally be exhumed during the last phase of the Andean Orogeny. This exposed the peridotites and associated sedimentary rocks, to the tropical humid environment, allowing the supergene Ni enrichment processes to form the laterite profile of CM as it is known today, with its extraordinarily high Ni content.
dc.languagespa
dc.publisherBogotá - Ciencias - Doctorado en Geociencias
dc.publisherDepartamento de Geociencias
dc.publisherUniversidad Nacional de Colombia - Sede Bogotá
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dc.rightsAtribución-NoComercial-SinDerivadas 4.0 Internacional
dc.rightshttp://creativecommons.org/licenses/by-nc-nd/4.0/
dc.rightsAcceso abierto
dc.rightsinfo:eu-repo/semantics/openAccess
dc.titleCarbonatos y otros minerales autigénicos asociados a las lateritas niquelíferas de Cerro Matoso y su posible relación con actividad hidrotermal y reducción de sulfatos
dc.typeOtro


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