Elena A. Miranda

Oceanic Core Complex Development in Modern and Ancient Oceanic Lithosphere: Gabbro‐Localized versus Peridotite‐Localized Detachment Models

Drilling and submersible studies of the Atlantis Bank (Southwest Indian Ridge) and the Atlantis Massif (Mid‐Atlantic Ridge) oceanic core complexes reveal “gabbro‐localized” and “peridotite‐localized” end‐member models of strain localization and deformation during core complex development, in which the gabbroic fault rocks exhibit extensive and rare high‐temperature ductile‐deformation fabrics, respectively. Both models emphasize a footwall cored by gabbroic intrusions, therefore precluding an amagmatic origin of core complex formation. We test these models by using relict oceanic core complexes preserved in the western Mirdita Ophiolite in Albania. The Puka and Krabbi massifs display traits of the peridotite‐localized detachment model, whereby amagmatic tectonic extension is not required for the formation of this category of core complexes.

Strain localization along the Atlantis Bank oceanic detachment fault system, Southwest Indian Ridge

Microstructural observations and mineral thermometry from in situ samples collected from the Atlantis Bank oceanic core complex (SW Indian Ridge) indicate that detachment faulting was initiated under hypersolidus conditions in the ductile regime and continued through subgreenschist temperatures through the ductile, semibrittle, and brittle regimes as strain localized along the exposed, now subhorizontal fault surface. Ductile, semibrittle, and brittle fabrics are developed within dominantly gabbroic rocks. Footwall rocks exhibit crystal plastic fabrics distributed over a structural thickness up to 400 m below the denuded fault surface exposed at the seafloor, whereas semibrittle and brittle fabrics are concentrated in the 80 and 30 m immediately below the principal slip surface of the detachment fault, respectively. Sample fabrics suggest that strain localization was achieved by dynamic recrystallization of plagioclase at temperatures between 910°C and 650°C, by amphibole-accommodated dissolution-precipitation creep at temperatures ∼750°C–450°C, by chlorite-accommodated reaction softening at temperatures ∼450°C–300°C, and by brittle fracturing and cataclasis at temperatures <300°C.