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Metamorphism and Plate Tectonics • at Present, the Geothermal Gradients Observed Are Strongly Affected by Plate Tectonics

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Metamorphism and Plate Tectonics • at Present, the Geothermal Gradients Observed Are Strongly Affected by Plate Tectonics METAMORPHISM IN RELATION TO PLATE TECTONICS • Metamorphic rocks result from the forces active during plate tectonic processes. The collision of plates, subduction, and the sliding of plates along transform faults create differential stress, friction, shearing, compressive stress, folding, faulting, and increased heat flow. • The tectonic forces deform and break the rock, creating openings, cracks, faults, breccias, and zones of weakness along which magmas can rise. Generally speaking, the greater the tectonic forces, the higher the pressures and temperatures affecting a rock mass and the greater the amount of resulting structural deformation and metamorphism. Dynamo thermal Metamorphism, Before collision, in subduction zone Continental-continental collision • In convergent margin settings where ocean basins close, continental lithosphere can approach and eventually collide with continental lithosphere on the opposing plate. As the two plates with continental lithosphere begin to collide, subduction will eventually cease as it becomes difficult to subduct low density continental lithosphere. • Compressional stresses generated in the collision zone will result in folding and thrust faulting of the rocks to ultimately create a fold-thrust mountain belt. Some rocks will be thrust upward to create the high peaks of the mountain range and some will be pushed downward to higher temperatures and pressures and become metamorphosed. Such collisional events are currently taking place along the Alpine Himalayan belt which extends from western Europe to southern Asia and has resulted in the mountain ranges known as the Alps and the Himalayas. An overview of metamorphism in relation to tectonic regimes: • Areas of crustal thickening and mountain building: greenschists, amphibolites granulites and eclogites (particularly if there are magmatic intrusions). • Subduction zones: Characterized by low geothermal gradients: zeolite pumpellyite-actinolite facies / lawsonite albite facies blueschist facies, eclogites • Ridges and rift valleys: characterized by high geothermal gradients contact and ocean floor metamorphism. • Areas of magmatic activity; volcanic - plutonic complexes: greenschists, amphibolites, granulites. Metamorphism and Plate Tectonics • At present, the geothermal gradients observed are strongly affected by plate tectonics. • Along zones where subduction is occurring, magmas are generated near the subduction zone and intrude into shallow levels of the crust. Because high temperature is brought near the surface, the geothermal gradient in these regions, and may be in the range of 50 to 70°C/km, and contact metamorphism (hornfels facies) results. • Because compression occurs along a subduction margin (the oceanic crust moves toward the volcanic arc) rocks may be pushed down to depths along either a normal or slightly higher than normal geothermal gradient 25°C/km. Actually the geothermal gradient is likely to be slightly higher than B (30°C/km), because the passage of magma through the crust will tend to heat the crust somewhat. In these regions we expect to see greenschist, amphibolite, and granulite facies metamorphic rocks. • Along a subduction zone, relatively cool oceanic lithosphere is pushed down to great depths. This results in producing a low geothermal gradient (temperature increases slowly with depth) of 10 - 15°C/km. This low geothermal gradient ("C") in the diagram above, results in metamorphism into the blueschist and eclogite facies. Examples of this type include the Franciscan (with the Sierra Nevada) in the western U.S.A., and the Sanbagawa (and Abukuma) belts in Japan. • B- Stable continental interiors and deep sedimentary basins: These are characterized by burial metamorphism with clockwise P-T paths, and peak T in the greenschist to epidote amphibolite facies. • C- Divergent Plate Boundaries: Ocean Floor Metamorphism: Continental rifts: In such settings, it is very common to find “metamorphic core complexes”, defined as areas that are topographically high and that consist of igneous and metamorphic rocks that display anomalous deformation and metamorphism relative to the surrounding rocks. Conservative Plate Boundaries: Cataclasis and Mylonitization.
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