An oceanic core complex, or megamullion, is a seabed geologic feature that forms a long ridge perpendicular to a mid-ocean ridge. It contains smooth domes that are lined with transverse ridges like a corrugated roof. They can vary in size from 10 to 150 km in length, 5 to 15 km in width, and 500 to 1500 m in height. Their counterparts on land are metamorphic core complexes, which form in areas of continental crustal extension or stretching.

History, distribution and exploration

The first oceanic core complexes described were identified in the Atlantic Ocean. Since then numerous such structures have been identified primarily in oceanic lithosphere formed at intermediate, slow- and ultra-slow spreading mid-ocean ridges, as well as back-arc basins. Examples include 10-1000 square km expanses of ocean floor and therefore of the oceanic lithosphere, particularly along the Mid-Atlantic Ridge and the Southwest Indian Ridge. Some of these structures have been drilled and sampled, showing that the footwall can be composed of both mafic plutonic and ultramafic rocks (gabbro and peridotite primarily, in addition to diabase), and a thin shear zone that includes hydrous phyllosilicates. Oceanic core complexes are often associated with active hydrothermal fields.

Formation

Oceanic core complex structures form at slow-spreading diverging oceanic plate boundaries with only a limited supply of upwelling magma. These zones have low upper mantle temperatures and long transform faults develop. Rift valleys do not develop along the expansion axes of slow-spreading boundaries. Expansion takes place along low-angle detachment faults. The core complex builds on the uplifted side of the fault, where most of the gabbroic (or crustal) material is stripped away to expose mantle rocks at the seabed. They consist of peridotites, ultramafic rocks of the mantle and to a lesser extent gabbroic rocks from the Earth's crust. Each detachment fault has three notable features: a breakaway zone where the fault began, an exposed fault surface that rides over the dome, and a termination, which is usually marked by a valley and adjacent ridge. However, the formation process through detachment faults hypothesis has its limitations, such as the scarce seismic evidence that low-angle normal faulting exists, where the presumably significant offset along such faults - which transect the lithosphere at a low angle - should be involved with some friction. The rarity of eclogite in oceanic core complexes also casts doubt on the likelihood of a deep source in such domains. The abundance of peridotites in oceanic core complexes could be accounted for by a unique variation of ocean-ocean subduction at the junction of slow-spreading oceanic ridges and fracture zones. Analog models of subduction show that density contrast of more than 200 kg/m3 between two juxtaposed lithospheric slabs would result in the underthrusting of the denser one to a depth of about 50 km, where phase transformation causes remineralization of pyroxenes into garnets. This increases the density of the slab, accelerating its drive into the mantle, provided that the friction between the slabs is low. There is ground to presume that at slow ridge and fracture zone intersections, the density contrast of the juxtaposed slabs would exceed 200 kg/m3, the friction between the slabs would be low, the thermal gradient would be about 100 C/km, and with about 5% water content, the drop of the solidus (a boundary transition on a phase diagram) of basalt at relatively low pressure would enable the co-occurrence of serpentinites and peridotites, the abundant rock-types in oceanic core complexes.

Examples

Some 50 oceanic core complexes have been identified, including:

Research

Scientific interest in core complexes has dramatically increased following an expedition in 1996 which mapped the Atlantis Massif. This expedition was the first to associate the complex structures with detachment faults. Research includes:

Sources