Open main menu

A convergent boundary is an area on Earth where two or more lithospheric plates collide. One plate eventually slides beneath the other causing a process known as subduction. The subduction zone can be defined by a plane where many earthquakes occur, called the Benioff Zone.[1] These collisions happen on scales of millions to tens of millions of years and can lead to volcanism, earthquakes, orogenesis, destruction of lithosphere, and deformation. Convergent boundaries occur between oceanic-oceanic lithosphere, oceanic-continental lithosphere, and continental-continental lithosphere. The geologic features related to convergent boundaries vary depending on crust types.

Plate tectonics is driven by convection cells in the mantle. Convection cells are the result of heat generated by radioactive decay of elements in the mantle escaping to the surface and the return of cool materials from the surface to the mantle.[2] These convection cells bring hot mantle material to the surface along spreading centers creating new crust. As this new crust is pushed away from the spreading center by the formation of newer crust, it cools, thins, and becomes denser. Subduction initiates when this dense crust converges with the less dense crust. The force of gravity helps drive the subducting slab into the mantle. Evidence supports that the force of gravity will increase plate velocity.[3] As the relatively cool subducting slab sinks deeper into the mantle, it is heated causing dehydration of hydrous minerals. This releases water into the hotter asthenosphere, which leads to partial melting of asthenosphere and volcanism. Both dehydration and partial melting occurs along the 1000 °C isotherm, generally at depths of 65 – 130  km.[4][5]

Simplified schematic of different convergent boundary types.

Some lithospheric plates consist of both continental and oceanic lithosphere. In some instances, initial convergence with another plate will destroy oceanic lithosphere, leading to convergence of two continental plates. Neither continental plate will subduct. It is likely that the plate may break along the boundary of continental and oceanic crust. Seismic tomography reveals pieces of lithosphere that have broken off during convergence.

Contents

Subduction zonesEdit

Subduction zones are areas where one lithospheric plate slides beneath another at a convergent boundary due to lithospheric density differences. These plates dip at an average of 45° but can vary. Subduction zones are often marked by an abundance of earthquakes, the result of internal deformation of the plate, convergence with the opposing plate, and bending at the oceanic trench. Earthquakes have been detected to a depth of 670  km. The relatively cold and dense subducting plates are pulled into the mantle and help drive mantle convection.[6]

Oceanic - Oceanic ConvergenceEdit

In collisions between two oceanic plates, the cooler, denser oceanic lithosphere sinks beneath the warmer, less dense oceanic lithosphere. As the slab sinks deeper into the mantle, it releases water from dehydration of hydrous minerals in the oceanic crust. This water reduces the melting temperature of rocks in the asthenosphere and causes partial melting. Partial melt will travel up through the asthenosphere, eventually, reach the surface, and form volcanic island arcs.

Continental - Oceanic ConvergenceEdit

When oceanic lithosphere and continental lithosphere collide, the dense oceanic lithosphere slides beneath the less dense continental lithosphere. An accretionary wedge forms on the continental crust as deep-sea sediments and oceanic crust are scraped from the oceanic plate. Volcanic arcs form on continental lithosphere as the result of partial melting due to dehydration of the hydrous minerals of the subducting slab.

Continental - Continental ConvergenceEdit

Some lithospheric plates consist of both continental and oceanic crust. Subduction initiates as oceanic lithosphere slides beneath continental crust. As the oceanic lithosphere subducts to greater depths, the attached continental crust is pulled closer to the subduction zone. Once the continental lithosphere reaches the subduction zone, subduction processes are altered as continental lithosphere is more buoyant and resists subduction beneath other continental lithosphere. A small portion of the continental crust may be subducted until the slab breaks, allowing the oceanic lithosphere to continue subducting, hot asthenosphere to rise and fill the void, and rebound of the continental lithosphere.[7] Evidence of this continental rebound include ultrahigh pressure metamorphic rocks which form at depths of 90 – 125 km that are exposed at the surface.[8]

Volcanism and Volcanic ArcsEdit

The oceanic crust contains hydrated minerals such as the amphibole group. During subduction, oceanic lithosphere is heated and metamorphosed causing dehydration of these hydrous minerals contained within basalts, releasing water into the asthenosphere. The release of water into the asthenosphere leads to partial melting. Partial melting allows the rise of more buoyant, hot material and can lead to volcanism at the surface and emplacement of plutons in the subsurface. These processes which generate magma are not entirely understood.

Where these magmas reach the surface they create volcanic arcs. Volcanic arcs can form as island arc chains or as arcs on continental crust. Three series of volcanic rocks generally form arcs, Tholeiitic (low iron basalts), calc-alkaline (moderately enriched in potassium and incompatible elements), and alkaline (highly enriched in potassium) which are very rare.[5]

Back arc basinsEdit

Back arc basins form behind a volcanic arc and are associated with extensional tectonics and high heat flow, often being home to seafloor spreading centers. These spreading centers are like mid ocean ridges, though the magma composition of back arc basins is generally more varied and contains a higher water content than mid ocean ridge magmas.[9] Back arc basins are often characterized by thin, hot lithosphere. Opening of back arc basins are still being studied but it is possible that movement of hot asthenosphere into lithosphere causes extension.[10]

Oceanic trenchesEdit

Oceanic trenches are narrow topographic lows that mark convergent boundaries or subduction zones. Oceanic trenches can be average 50 – 100  km wide and can be several thousand kilometers long. Oceanic trenches form as a result of bending of the subducting slab. Depth of oceanic trenches seems to be controlled by age of the oceanic lithosphere being subducted.[5] Sediment fill in oceanic trenches varies and generally depends on abundance of sediment input from surrounding areas. An oceanic trench, the Mariana Trench, is the deepest point of the ocean at a depth of approximately 11,000 m.

EarthquakesEdit

Earthquakes are common along convergent boundaries. A region of high earthquake activity, the Benioff zone, generally dips 45° and marks the subducting plate. Earthquakes will occur to a depth of 670  km along the Benioff. Both compressional and extensional forces act along convergent boundaries. On the inner walls of trenches, compressional faulting or reverse faulting occurs due to the relative motion of the two plates. Reverse faulting scrapes off ocean sediment and leads to the formation of an accretionary wedge. Reverse faulting can lead to massive earthquakes, such as the magnitude 9.1 Sumatra earthquake of 2004.  Tensional or normal faulting occurs on the outer wall of the trench, likely due to bending of the down going slab.[11]

Accretionary WedgeEdit

Accretionary wedges (also called accretionary prisms) form as sediment is scraped from the subducting lithosphere and emplaced against the overriding lithosphere. These sediments include igneous crust, turbidite sediments, and pelagic sediments. Imbricate thrust faulting along a basal decollement surface occurs in accretionary wedges as forces continue to compress and fault these newly added sediments.[5] The continued faulting of the accretionary wedge leads to overall thickening of the wedge.[12] Seafloor topography plays some role in accretion, especially emplacement of igneous crust.[13]

Convergent Boundaries and Natural DisastersEdit

Some of the deadliest natural disasters have occurred due to convergent boundary processes. The 2004 Indian Ocean earthquake and tsunami was triggered by an earthquake along the convergent boundary of the Indian plate and Burma microplate and killed over 200,000 people.  The 2011 tsunami off the coast of Japan, which caused 16,000 deaths and did US$360 billion in damage, was caused by a magnitude 9 earthquake along the convergent boundary of the Eurasian plate and Pacific Plate.

ExamplesEdit

See alsoEdit

ReferencesEdit

  1. ^ 1946-, Wicander, Reed (2013). Geol. Monroe, James S. (James Stewart), 1938- (2nd ed.). Belmont, CA: Cengage Wadsworth. ISBN 978-1133108696. OCLC 795757302.
  2. ^ Tackley, Paul J. (2000-06-16). "Mantle Convection and Plate Tectonics: Toward an Integrated Physical and Chemical Theory". Science. 288 (5473): 2002–2007. Bibcode:2000Sci...288.2002T. doi:10.1126/science.288.5473.2002. ISSN 1095-9203. PMID 10856206.
  3. ^ Conrad, Clinton P.; Lithgow‐Bertelloni, Carolina (2004-10-01). "The temporal evolution of plate driving forces: Importance of "slab suction" versus "slab pull" during the Cenozoic". Journal of Geophysical Research: Solid Earth. 109 (B10). doi:10.1029/2004JB002991. ISSN 2156-2202.
  4. ^ Bourdon, Bernard; Turner, Simon; Dosseto, Anthony (2003-06-01). "Dehydration and partial melting in subduction zones: Constraints from U-series disequilibria". Journal of Geophysical Research: Solid Earth. 108 (B6): 2291. Bibcode:2003JGRB..108.2291B. doi:10.1029/2002JB001839. ISSN 2156-2202.
  5. ^ a b c d P., Kearey (2009). Global tectonics. Klepeis, Keith A., Vine, F. J. (3rd ed.). Oxford: Wiley-Blackwell. ISBN 9781405107778. OCLC 132681514.
  6. ^ Widiyantoro, Sri; Hilst, Rob D. Van Der; Grand, Stephen P. (1997-12-01). "Global seismic tomography: A snapshot of convection in the earth". GSA Today. 7 (4). ISSN 1052-5173.
  7. ^ Condie, Kent C. (2016-01-01). "Crustal and Mantle Evolution". Earth as an Evolving Planetary System. Academic Press. pp. 147–199. doi:10.1016/b978-0-12-803689-1.00006-7. ISBN 9780128036891.
  8. ^ Ernst, W. G.; Maruyama, S.; Wallis, S. (1997-09-02). "Buoyancy-driven, rapid exhumation of ultrahigh-pressure metamorphosed continental crust". Proceedings of the National Academy of Sciences of the United States of America. 94 (18): 9532–9537. Bibcode:1997PNAS...94.9532E. doi:10.1073/pnas.94.18.9532. ISSN 0027-8424. PMC 23212. PMID 11038569.
  9. ^ Taylor, Brian; Martinez, Fernando (March 2002). "Mantle wedge control on back-arc crustal accretion". Nature. 416 (6879): 417–420. Bibcode:2002Natur.416..417M. doi:10.1038/416417a. ISSN 1476-4687. PMID 11919628.
  10. ^ Tatsumi, Yoshiyuki; Otofuji, Yo-Ichiro; Matsuda, Takaaki; Nohda, Susumu (1989-09-10). "Opening of the Sea of Japan back-arc basin by asthenospheric injection". Tectonophysics. 166 (4): 317–329. Bibcode:1989Tectp.166..317T. doi:10.1016/0040-1951(89)90283-7. ISSN 0040-1951.
  11. ^ Oliver, J.; Sykes, L.; Isacks, B. (1969-06-01). "Seismology and the new global tectonics". Tectonophysics. 7 (5–6): 527–541. Bibcode:1969Tectp...7..527O. doi:10.1016/0040-1951(69)90024-9. ISSN 0040-1951.
  12. ^ Konstantinovskaia, Elena; Malavieille, Jacques (2005-02-01). "Erosion and exhumation in accretionary orogens: Experimental and geological approaches". Geochemistry, Geophysics, Geosystems. 6 (2): Q02006. Bibcode:2005GGG.....6.2006K. doi:10.1029/2004GC000794. ISSN 1525-2027.
  13. ^ Sharman, George F.; Karig, Daniel E. (1975-03-01). "Subduction and Accretion in Trenches". GSA Bulletin. 86 (3): 377–389. doi:10.1130/0016-7606(1975)862.0.CO;2 (inactive 2019-07-07). ISSN 0016-7606.