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The Indo-Burma Range, also called the Indo-Burmese Range, or the Indo-Burman Range, is a mountain range that forms the boundary between the Indian subcontinent and mainland southeast Asia. It sits at the convergent boundary of the Indian and Burma plates in Myanmar. The mountain belt comprises various mountains: the Arakan-Yoma mountains and the Chin, Naga, Maniour, Lushai and Patkai hills. The Indo-Burman Range merged with Eastern Himalayan Syntaxis further north, submerged into the Andaman Sea, and resurfaced as Andaman Islands further south.

The subduction between the Indian plate and the Burma plate resulted in the development of accretionary wedges, in order to accommodate the EW shortening along the convergent boundary. Later, thrusting, folding and uplifting formed the Indo-Burman Ranges.

The Indo-Burman Range bulges towards the west at the center (about 22°N), forming an arc-shaped structure. This arc-shaped structure implies restriction on the convergent motion along the Indian-Burma boundary, therefore the collision intensity varies along the range.

The collision is at a maximum at the center of the Indo-Burman Range around 24°N, which is presented with a broad, high range (up to 20 km wide) and evolves to narrow, low hills in the south (16°N). The collision strikes in NW-SE at the northern part of the Indo-Burman Range (Naga Domain).

Lithology

The Indo-Burman Range is a sedimentary belt mainly consisted of Cenozoic flysch sediments and a core of Mesozoic ophiolites dated back to late Jurassic overlain on a thick Mesozoic sequence. All the above unconformity lies on a metamorphic basement dated back to pre-Triassic.

The core Mesozoic ophiolites consists of serpentinite peridotites, pillow basalts and red cherts etc. The obduction of ophiolites is interpreted as the closure of several Neo-Tethys between the Shan-Thai block, Burma microplate and Indian Plate.

The sedimentary sequence overlain by the ophiolites ranges from Late Triassic to Orbitoides-bearing Late Cretaceous carbonates and shales, where part of the sedimentary sequence has undergone high pressure/low temperature blue-schist metamorphism.

The pre-Triassic metamorphic basement composed of Kampetlet schist and gneisses were exposed in the Mount Victoria area in Myanmar. The flysch type sediments in the western flank of the Indo-Burman Range are relatively younger than the folded and thrusted eastern flank.

References

1. ^ Wang, Yu; Sieh, Kerry; Tun, Soe Thura; Lai, Kuang-Yin; Myint, Than (2014-04-01). "Active tectonics and earthquake potential of the Myanmar region". Journal of Geophysical Research: Solid Earth. 119 (4): 2013JB010762. doi:10.1002/2013JB010762. hdl:10220/19774. ISSN 2169-9356.
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3. Sikder, Arif Mohiuddin; Alam, M.Mustafa (2003). "2-D modelling of the anticlinal structures and structural development of the eastern fold belt of the Bengal Basin, Bangladesh". Sedimentary Geology. 155 (3–4): 209–226. doi:10.1016/s0037-0738(02)00181-1.
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5. Maurin, Thomas; Rangin, Claude (2009-04-01). "Structure and kinematics of the Indo-Burmese Wedge: Recent and fast growth of the outer wedge". Tectonics. 28 (2): TC2010. doi:10.1029/2008TC002276. ISSN 1944-9194.
6. ^ Brunel, Maurice (2002). "Late Cretaceous to Eocene metamorphism of internal zones of the Indo-Burma range (western Myanmar): geodynamic implications. About the paper by Anne Socquet et al". Comptes Rendus Geoscience. 334 (12): 875–876. doi:10.1016/s1631-0713(02)01824-2.
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