On the Upwelling off the Southern Tip and along the West Coast of India

The processes of upwelling off the southern tip (the Kanyakumari coast) and the west coast of India are highly localised features with different forcing mechanisms, and they cannot be treated as a uniform wind-driven upwelling system. Off the Kanyakumari coast, upwelling is due to the south-west mon...

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Bibliographic Details
Published inJournal of coastal research Vol. 24; no. sp3; pp. 95 - 102
Main Authors Smitha, B. R., Sanjeevan, V. N., Vimalkumar, K. G., Revichandran, C.
Format Journal Article
LanguageEnglish
Published Fort Lauderdale Coastal Education and Research Foundation (CERF) 01.07.2008
Allen Press Inc
Subjects
Chlorophylls
Coasts
Kelvin waves
local temperature anomaly
Marine
mass transport
Monsoons
Ocean circulation
Oceanography
Oceans
Offshore
Planetary waves
Rainy seasons
Saline water
Salinity
Sea level
Seas
south-eastern Arabian Sea and Kanyakumari coast
south-west monsoon
Stress propagation
Upwelling
Upwelling water
Wave propagation
Wind
Wind stress
Wind velocity
Winds
India
ISW, India, Kerala, Kanyakumari
ISW, India, Karnataka, Dakshina Kannada Dist., Mangalore
ISW, India, Kerala, Kollam Dist., Kollam
ISW, Arabian Sea
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Summary:The processes of upwelling off the southern tip (the Kanyakumari coast) and the west coast of India are highly localised features with different forcing mechanisms, and they cannot be treated as a uniform wind-driven upwelling system. Off the Kanyakumari coast, upwelling is due to the south-west monsoon winds that are tangential to the coast. Along the west coast, the area between 8° N and 9° N represents the shadow zone to the influence of the remote forcing on the upwelling; the latter is forced by the longshore wind stress. Moderate to relatively intense upwelling occurs along the Kollam to Mangalore coast (9° N to 13° N) due to the combined action of the longshore wind stress, the coastally trapped Kelvin waves, and the offshore propagating Rossby waves. North of this area (13° N to 15° N), upwelling is weak due to weak wind stress and is closely confined to the coastal belt. This results from the suppressive effect of the southwards-flowing Arabian Sea high saline water on the process of upwelling along this coastal stretch.
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ISSN:0749-0208
1551-5036
DOI:10.2112/06-0779.1