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Indian plate

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This article is about the geological term. For the large plated meal in Indian restaurants, see Thali.
Not to be confused with Indian subcontinent.

The Indian plate (or India plate) is a minor tectonic plate straddling the equator in the Eastern Hemisphere. Originally a part of the ancient continent of Gondwana, the Indian plate broke away from the other fragments of Gondwana 100 million years ago and began moving north, carrying Insular India with it.[2] It was once fused with the adjacent Australian plate to form a single Indo-Australian plate; recent studies suggest that India and Australia have been separate plates for at least 3 million years.[3] The Indian plate includes most of modern South Asia (the Indian subcontinent) and a portion of the basin under the Indian Ocean, including parts of South China, western Indonesia,[4][5] and extending up to but not including Ladakh, Kohistan, and Balochistan in Pakistan.[6][7][8]

Indian plate
TypeMinor
Approximate area11,900,000 km2 (4,600,000 sq mi)[1]
Movement1North-east
Speed126–36 mm/a (1.0–1.4 in/year)[citation needed]
FeaturesIndian subcontinent, Indian Ocean, Arabian Sea, Himalayas
1Relative to the African plate

Plate movements

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Due to plate tectonics, Insular India, situated over the Indian plate, split from Madagascar and collided (c. 55 Mya) with the Eurasian plate, resulting in the formation of the Himalayas.

Until roughly 140 million years ago, the Indian plate formed part of the supercontinent, Gondwana, together with modern Africa, Australia, Antarctica, and South America. Gondwana fragmented as these continents drifted apart at different velocities;[9] a process which led to the opening of the Indian Ocean.[10]

In the late Cretaceous approximately 100 million years ago, and subsequent to the splitting from Gondwana of conjoined Madagascar and India, the Indian plate split from Madagascar and formed Insular India. It began moving north, at about 20 cm (7.9 in) per year,[9] and is believed to have begun colliding with Asia as early as 55 million years ago,[11] in the Eocene epoch of the Cenozoic. However, some authors suggest the collision between India and Eurasia occurred much later, around 35 million years ago.[12] If the collision occurred between 55 and 50 Mya, the Indian plate would have covered a distance of 3,000 to 2,000 km (1,900–1,200 mi), moving more quickly than any other known plate. In 2012, paleomagnetic data from the Greater Himalaya was used to propose two collisions to reconcile the discrepancy between the amount of crustal shortening in the Himalaya (~1,300 km or 800 mi) and the amount of convergence between India and Asia (~3,600 km or 2,200 mi).[13] These authors propose a continental fragment of northern Gondwana rifted from India, traveled northward, and initiated the "soft collision" between the Greater Himalaya and Asia at ~50 Mya. This was followed by the "hard collision" between India and Asia occurred at ~25 Mya. Subduction of the resulting ocean basin that formed between the Greater Himalayan fragment and India explains the apparent discrepancy between the crustal shortening estimates in the Himalaya and paleomagnetic data from India and Asia. However, the proposed ocean basin was not constrained by paleomagnetic data from the key time interval of ~120 Mya to ~60 Mya. New paleomagnetic results of this critical time interval from southern Tibet do not support this Greater Indian Ocean basin hypothesis and the associated dual collision model.[14]

In 2007, German geologists[9] suggested the reason the Indian plate moved so quickly is that it is only half as thick (100 km or 62 mi) as the other plates[15] which formerly constituted Gondwana. The mantle plume that once broke up Gondwana might also have melted the lower part of the Indian subcontinent, which allowed it to move both more quickly and farther than the other parts.[9] The remains of this plume today form the Marion hotspot (Prince Edward Islands), the Kerguelen hotspot, and the Réunion hotspots.[10][16] As India moved north, it is possible the thickness of the Indian plate degenerated further as it passed over the hotspots and magmatic extrusions associated with the Deccan and Rajmahal Traps.[10] The massive amounts of volcanic gases released during the passage of the Indian plate over the hotspots have been theorised to have played a role in the Cretaceous–Paleogene extinction event, generally held to be due to a large asteroid impact.[17]

In 2020, however, geologists at the University of Oxford and the Alfred Wegener Institute found that new plate-motion models displayed increased movement speeds in all mid-ocean ridges during the late Cretaceous, a result irreconcilable to current theories of plate tectonics and a refutation of the plume-push hypothesis. Pérez-Díaz concludes that the accelerated movement of the Indian plate is an illusion wrought by large errors in geomagnetic reversal timing around the Cretaceous–Paleogene boundary, and that a recalibration of the time scale shows no such acceleration exists.[18][19]

The collision with the Eurasian plate along the boundary between India and Nepal formed the orogenic belt that created the Tibetan Plateau and the Himalaya Mountains, as sediment bunched up like earth before a plow.

The Indian plate is currently moving north-east at five cm (2.0 in) per year, while the Eurasian plate is moving north at only two cm (0.79 in) per year. This is causing the Eurasian plate to deform, and the Indian plate to compress at a rate of four mm (0.16 in) per year.[citation needed]

Geography

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The westerly side of the Indian plate is a transform boundary with the Arabian plate called the Owen Fracture Zone, and a divergent boundary with the African plate called the Central Indian Ridge (CIR). The northerly side of the plate is a convergent boundary with the Eurasian plate forming the Himalaya and Hindu Kush mountains, called the Main Himalayan Thrust.[citation needed]

See also

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Notes

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  1. ^ "Sizes of Tectonic or Lithospheric Plates". Geology.about.com. 2014-03-05. Archived from the original on 2016-06-05. Retrieved 2016-01-13.
  2. ^ Oskin, Becky (2013-07-05). "New Look at Gondwana's Breakup". Livescience.com. Retrieved 2016-01-13.
  3. ^ Stein, Seth; Sella, Giovanni F.; Okai, Emile A. (2002). "The January 26, 2001 Bhuj Earthquake and the Diffuse Western Boundary of the Indian Plate" (PDF). Geodynamics Series. American Geophysical Union: 243–254. doi:10.1029/GD030p0243. ISBN 9781118670446. Retrieved 2015-12-25.
  4. ^ Sinvhal, Understanding Earthquake Disasters, p. 52, Tata McGraw-Hill Education, 2010, ISBN 978-0-07-014456-9
  5. ^ Kumar, M. Ravi; Bhatia, S. C. (1999). "A new seismic hazard map for the Indian plate region under the global seismic hazard assessment programme". Current Science. 77 (3): 447. JSTOR 24102967.
  6. ^ M. Asif Khan, Tectonics of the Nanga Parbat syntaxis and the Western Himalaya, p. 375, Geological Society of London, 2000, ISBN 978-1-86239-061-4
  7. ^ Srikrishna Prapnnachari, Concepts in Frame Design, page 152, Srikrishna Prapnnachari, ISBN 978-99929-52-21-4
  8. ^ A.M. Celâl Şengör (1989). Tectonic evolution of the Tethyan Region, Springer ISBN 978-0-7923-0067-0
  9. ^ a b c d Kind 2007
  10. ^ a b c Kumar et al. 2007
  11. ^ Scotese 2001
  12. ^ Aitchison, Ali & Davis 2007
  13. ^ van Hinsbergen, D.; Lippert, P.; Dupont-Nivet, G.; McQuarrie, N.; Doubrivine, P.; Spakman, W.; Torsvik, T. (2012). "Greater India Basin hypothesis and a two-stage Cenozoic collision between India and Asia". Proceedings of the National Academy of Sciences. 109 (20): 7659–7664. Bibcode:2012PNAS..109.7659V. doi:10.1073/pnas.1117262109. PMC 3356651. PMID 22547792.
  14. ^ Qin, Shi-Xin; Li, Yong-Xiang; Li, Xiang-Hui; Xu, Bo; Luo, Hui (2019-01-17). "Paleomagnetic results of Cretaceous cherts from Zhongba, southern Tibet: New constraints on the India-Asia collision". Journal of Asian Earth Sciences. 173: 42–53. Bibcode:2019JAESc.173...42Q. doi:10.1016/j.jseaes.2019.01.012. ISSN 1367-9120. S2CID 134469511.
  15. ^ The lithospheric roots in South Africa, Australia, and Antarctica are 300 to 180 km (190 to 110 mi) thick. (Kumar et al. 2007) See also Kumar et al. 2007, figure 1
  16. ^ Meert, J.G.; Tamrat, Endale (2006). "Paleomagnetic evidence for a stationary Marion hotspot: Additional paleomagnetic data from Madagascar". Gondwana Research. 10 (3–4): 340–348. Bibcode:2006GondR..10..340M. doi:10.1016/j.gr.2006.04.008.
  17. ^ Schulte, Peter; et al. (5 March 2010). "The Chicxulub Asteroid Impact and Mass Extinction at the Cretaceous-Paleogene Boundary" (PDF). Science. 327 (5970). AAAS: 1214–1218. Bibcode:2010Sci...327.1214S. doi:10.1126/science.1177265. ISSN 1095-9203. PMID 20203042. S2CID 2659741.
  18. ^ Pérez-Díaz, L.; Eagles, G.; Sigloch, K. (2020). "Indo-Atlantic plate accelerations around the Cretaceous-Paleogene boundary: A time-scale error, not a plume-push signal". Geology. 48 (12): 1169–1173. Bibcode:2020Geo....48.1169P. doi:10.1130/G47859.1.
  19. ^ Andrews, Robin George (14 April 2021). "The New Historian of the Smash That Made the Himalayas". Quanta Magazine. Retrieved 15 April 2021.

References

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