SummaryThe Sierras de San Luis, which are part of the Sierras Pampeanas, are located in Central Argentina. The crystalline basement of the Sierras de San Luis is built up of three main blocks (western block, central block, and eastern block), which are separated by mylonite zones. The western and the eastern block are dominated by migmatites, whereas the central block is mostly lower in metamorphic grade ranging from greenschist facies to amphibolite facies, and locally to granulite facies in the vicinity of numerous ma®c bodies. Most parts of the central block is built up of amphibolite facies rocks. These were formed during a ®rst metamorphic event (M1-A) which is characterized by a mineral assemblage of stauroliteÀgarnetÀbiotiteÀmuscoviteÀ plagioclaseÀquartzÀilmeniteAE®broliteAEchlorite. The PT conditions of M1-A are about 570 C to 600 C and 5 to 5.7 kbar. A ma®c intrusion, now seen as numerous ma®c lenses included in the basement rocks caused local granulite facies metamorphism. The observed mineral assemblage consists of garnetÀcordieriteÀsillimaniteÀbiotiteÀK-feldsparÀplagioclaseÀquartzÀrutileÀilmeniteAEorthopyroxene (M2-G). The PT estimates for granulite facies conditions are 740 C to 790 C and 5.7 to 6.4 kbar. During cooling a mylonite zone developed within the central block retrograding most of the granulite facies rocks to amphibolite facies conditions. The newly formed mineral assemblage consists of garnetÀbiotiteÀsillimaniteÀplagioclaseÀmuscoviteÀquartzÀ rutileAEK-feldspar (M3-A). The PT estimates of the locally overprinting second amphibolite facies event (M3-A) are about 590 C to 650 C and 5.4 to 6.0 kbar. The deduced PT path shows a near isobaric heating from M1-A to M2-G. The mylonite mineral assemblage M3-A equilibrated at pressures close to M2-G. The PT path can be explained best by heating of an amphibolite facies middle crust by a ma®c intrusion. During near-isobaric cooling tectonic activity in discrete parts of the basement caused mylonitization at amphibolite facies conditions.
Troctolitic gabbros from Valle Fe´rtil and La Huerta Ranges, San Juan Province, NW-Argentina exhibit multi-layer corona textures between cumulus olivine and plagioclase. The corona mineral sequence, which varies in the total thickness from 0.5 to 1 mm, comprises either an anhydrous corona type I with olivine|orthopyroxene|clinopyroxene+spinel symplectite|plagioclase or a hydrous corona type II with olivine|orthopyroxene|amphibole|amphibole+spinel symplectite|plagioclase. The anhydrous corona type I formed by metamorphic replacement of primary olivine and plagioclase, in the absence of any fluid ⁄ melt phase at <840°C. Diffusion controlled metamorphic solid-state replacement is mainly governed by the chemical potential gradients at the interface of reactant olivine and plagioclase and orthopyroxene and plagioclase. Thus, the thermodynamic incompatibility of the reactant minerals at the gabbro-granulite transition and the phase equilibria of the coronitic assemblage during subsequent cooling were modelled using quantitative lMgO-lCaO phase diagrams. Mineral reaction textures of the anhydrous corona type I indicate an inward migration of orthopyroxene on the expense of olivine, while clinopyroxene+spinel symplectite grows outward to replace plagioclase. Mineral textures of the hydrous corona type II indicate the presence of an interstitial liquid trapped between cumulus olivine and plagioclase that reacts with olivine to produce a rim of peritectic orthopyroxene around olivine. Two amphibole types are distinguished: an inclusion free, brownish amphibole I is enriched in trace elements and REEs relative to green amphibole II. Amphibole I evolves from an intercumulus liquid between peritectic orthopyroxene and plagioclase. Discrete layers of green amphibole II occur as inclusion-free rims and amphibole II+spinel symplectites. Mineral textures and geochemical patterns indicate a metamorphic origin for amphibole II, where orthopyroxene was replaced to form an inner inclusion-free amphibole II layer, while clinopyroxene and plagioclase were replaced to form an outer amphibole+spinel symplectite layer, at <770°C. Calculation of the possible net reactions by considering NCKFMASH components indicates that the layer bulk composition cannot be modelled as a ÔclosedÕ system although in all cases the gain and loss of elements within the multi-layer coronas (except H 2 O, Na 2 O) is very small and the main uncertainties may arise from slight chemical zoning of the respective minerals. Local oxidizing conditions led to the formation of orthopyroxene+magnetite symplectite enveloping and ⁄ or replacing olivine. The sequence of corona reaction textures indicates a counter clockwise P-T path at the gabbro-granulite transition at 5-6.5 kbar and temperatures below 900°C.
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