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dc.contributor.authorJohns, William E.
dc.contributor.authorBaringer, Molly O.
dc.contributor.authorBeal, L. M.
dc.contributor.authorCunningham, S. A.
dc.contributor.authorKanzow, Torsten
dc.contributor.authorBryden, Harry L.
dc.contributor.authorHirschi, J. J. M.
dc.contributor.authorMarotzke, J.
dc.contributor.authorMeinen, C. S.
dc.contributor.authorShaw, B.
dc.contributor.authorCurry, Ruth G.
dc.date.accessioned2011-06-13T17:32:57Z
dc.date.available2011-11-15T09:28:55Z
dc.date.issued2011-05-15
dc.identifier.citationJournal of Climate 24 (2011): 2429–2449en_US
dc.identifier.urihttp://hdl.handle.net/1912/4643
dc.descriptionAuthor Posting. © American Meteorological Society, 2011. This article is posted here by permission of American Meteorological Society for personal use, not for redistribution. The definitive version was published in Journal of Climate 24 (2011): 2429–2449, doi:10.1175/2010JCLI3997.1.en_US
dc.description.abstractContinuous estimates of the oceanic meridional heat transport in the Atlantic are derived from the Rapid Climate Change–Meridional Overturning Circulation (MOC) and Heatflux Array (RAPID–MOCHA) observing system deployed along 26.5°N, for the period from April 2004 to October 2007. The basinwide meridional heat transport (MHT) is derived by combining temperature transports (relative to a common reference) from 1) the Gulf Stream in the Straits of Florida; 2) the western boundary region offshore of Abaco, Bahamas; 3) the Ekman layer [derived from Quick Scatterometer (QuikSCAT) wind stresses]; and 4) the interior ocean monitored by “endpoint” dynamic height moorings. The interior eddy heat transport arising from spatial covariance of the velocity and temperature fields is estimated independently from repeat hydrographic and expendable bathythermograph (XBT) sections and can also be approximated by the array. The results for the 3.5 yr of data thus far available show a mean MHT of 1.33 ± 0.40 PW for 10-day-averaged estimates, on which time scale a basinwide mass balance can be reasonably assumed. The associated MOC strength and variability is 18.5 ± 4.9 Sv (1 Sv ≡ 106 m3 s−1). The continuous heat transport estimates range from a minimum of 0.2 to a maximum of 2.5 PW, with approximately half of the variance caused by Ekman transport changes and half caused by changes in the geostrophic circulation. The data suggest a seasonal cycle of the MHT with a maximum in summer (July–September) and minimum in late winter (March–April), with an annual range of 0.6 PW. A breakdown of the MHT into “overturning” and “gyre” components shows that the overturning component carries 88% of the total heat transport. The overall uncertainty of the annual mean MHT for the 3.5-yr record is 0.14 PW or about 10% of the mean value.en_US
dc.description.sponsorshipThis research was supported by the U.S. National Science Foundation under Awards OCE0241438 and OCE0728108, by the U.K. RAPID Programme (RAPID Grant NER/T/S/2002/00481), and by the U.S. National Oceanic and Atmospheric Administration, as part of its Western Boundary Time Series Program.en_US
dc.format.mimetypeapplication/pdf
dc.language.isoen_USen_US
dc.publisherAmerican Meteorological Societyen_US
dc.relation.urihttp://dx.doi.org/10.1175/2010JCLI3997.1
dc.subjectAtlantic Oceanen_US
dc.subjectMeridonial overturning circulationen_US
dc.subjectSea surface temperatureen_US
dc.subjectTransporten_US
dc.subjectAnomaliesen_US
dc.titleContinuous, array-based estimates of Atlantic Ocean heat transport at 26.5°Nen_US
dc.typeArticleen_US
dc.identifier.doi10.1175/2010JCLI3997.1


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