Anoceanic core complex, ormegamullion, is a seabedgeologic feature that forms a long ridge perpendicular to amid-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.[citation needed] Their counterparts on land aremetamorphic core complexes, which form in areas of continentalcrustal extension or stretching.[1]
The first oceanic core complexes described were identified in the Atlantic Ocean.[2] Since then numerous such structures have been identified primarily in oceaniclithosphere formed at intermediate, slow- and ultra-slow spreadingmid-ocean ridges, as well asback-arc basins.[3] Examples include 10-1000 square km expanses of ocean floor and therefore of the oceanic lithosphere, particularly along theMid-Atlantic Ridge[4][5] and theSouthwest Indian Ridge.[6] Some of these structures have been drilled and sampled, showing that thefootwall can be composed of bothmafic plutonic andultramafic rocks (gabbro andperidotite primarily, in addition todiabase), and a thinshear zone that includes hydrousphyllosilicates. Oceanic core complexes are often associated with active hydrothermal fields.
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,[7] where the presumably significant offset along such faults - which transect the lithosphere at a low angle - should be involved with some friction. The rarity ofeclogite 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.[8][full citation needed] 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 thesolidus (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.
TheSaint Peter and Saint Paul Archipelago and complex lies in the equatorialAtlantic Ocean. It is 90 km long and 4000 m tall. The apex forms the Saint Peter and Paul Rocks. This is one of the few known examples where sea floor mantle rocks are exposed above sea level.
Scientific interest in core complexes has dramatically increased following an expedition in 1996 which mapped theAtlantis Massif. This expedition was the first to associate the complex structures with detachment faults. Research includes:
The complexes provide cross sections of mantle material which could only otherwise be found by drilling deep into the mantle. The deep drilling that is required to penetrate 6-7 km through the crust is beyond current technical and financial constraints. Selective sample drilling into the complex structures are already underway.
To investigate the development of oceanic core complexes:
In 2005 scientists from theWoods Hole Oceanographic Institute discovered a series of complexes in the North Atlantic, 1,500 miles (2,400 km) fromBermuda.[4] These structures are at various stages in their evolution—from bumps that indicated the emergence of a core complex to the faded grooves of long-exhumed core complexes that had been eroded away over millions of years. Such features will enable scientists to see active detachment faults in operation and understand their development.
To study mineralisation and the release of minerals from the mantle:
A steeply sloping detachment fault which penetrates deeply can be a conduit for hot mineral-richhydrothermal fluids to circulate towards the surface and buildmineral deposits. These deposits can grow massive because detachment faults persist for hundreds of thousands of years. The Woods Hole Institution is studying one such site, called the TAG hydrothermal field on the Mid-Atlantic Ridge.
To investigate marine magnetic anomalies:
The conventional view that marinemagnetic anomalies arose in the upper, extrusive layer of theoceanic crust requires a rethink because perfectly normal magnetic anomalies arise at core complexes, where the crust has been stripped away. This suggests that the lower part of the ocean crust contains a substantial magnetic signature.
^Loocke, M.; Snow, J.E.; Ohara, Y. (2013). "Melt stagnation in peridotites from the Godzilla Megamullion Oceanic Core Complex, Parece Vela Basin, Philippine Sea".Lithos.182–183:1–10.Bibcode:2013Litho.182....1L.doi:10.1016/j.lithos.2013.09.005.
