Assessment of composite global sampling: Sea surface wind speed

Zhang, Huai‐Min; Bates, John J.; Reynolds, Richard W.

doi:10.1029/2006gl027086

Cited by 259 publications

(184 citation statements)

References 14 publications

(14 reference statements)

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“…For the wind data we used the multiple-satellite blended Sea Winds product 39 , which has a space and time resolution of 0.25 • and 6 hours, respectively. SST and ice concentration were acquired from an optimum interpolated, blended analysis of satellite and in-situ data provided once per day at 0.25 • spatial resolution 40 .…”

Section: Methodsmentioning

confidence: 99%

Surprising return of deep convection to the subpolar North Atlantic Ocean in winter 2007–2008

et al. 2008

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Section: Methodsmentioning

confidence: 99%

Surprising return of deep convection to the subpolar North Atlantic Ocean in winter 2007–2008

et al. 2008

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“…This study analyzed the following datasets: (1) daily global sea-surface pressure with a resolution of 1.125°lati-tude 9 1.125°longitude, from the reanalysis of the European Centre for Medium-Range Forecasts (ECMWF) (ERA-40, Uppala et al 2005); (2) daily global sea-surface winds with a high horizontal resolution of 0.25°lati-tude 9 0.25°longitude, from the National Oceanic and Atmospheric Administration (NOAA) (Zhang et al 2006) and National Climatic Data Center (NCDC) (Smith and Reynolds 2004), for which wind speeds are generated by blending observations from six satellites and for which wind directions from the National Center for Environment Prediction (NCEP) Reanalysis 2 (NRA-2) (Kanamitsu et al 2002) are interpolated into the blended speed grids; (3) daily optimum interpolation SST (OISST) analysis data (AVHRR ? AMSR-E products) from the NOAA Satellite and Information Service with the same resolution as sea surface winds and weekly OISST with horizontal resolution of 1°latitude 9 1°longitude; (4) daily SST, ocean latent heat flux, sensible heat flux, net radiation flux, longwave and shortwave radiation at the sea surface with a resolution of 1°latitude 9 1°longitude obtained from the Objectively Analyzed Air-Sea Fluxes (OAFlux) for the Global Oceans, sponsored by the Woods Hole Oceanographic Institution (WHOI) Cooperative Institute for Climate and Ocean Research (CICOR); and (5) pentad total downward heat flux at the surface, ocean current, salinity, mixed-layer depth,and potential temperature profiles (1/3°l atitude by 1°longitude, 40 levels) taken from the NCEP Global Ocean Data Assimilation System (GODAS) (Ji et al 1995) for accurate air-sea processes.…”

Section: Data Descriptionmentioning

confidence: 99%

Air–sea interaction and formation of the Asian summer monsoon onset vortex over the Bay of Bengal

Guan

Liu

et al. 2011

Clim Dyn

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In spring over the southern Bay of Bengal (BOB), a vortex commonly develops, followed by the Asian summer monsoon onset. An analysis of relevant data and a case study reveals that the BOB monsoon onset vortex is formed as a consequence of air-sea interaction over BOB, which is modulated by Tibetan Plateau forcing and the land-sea thermal contrast over the South Asian area during the spring season. Tibetan Plateau forcing in spring generates a prevailing cold northwesterly over India in the lower troposphere. Strong surface sensible heating is then released, forming a prominent surface cyclone with a strong southwesterly along the coastal ocean in northwestern BOB. This southwesterly induces a local offshore current and upwelling, resulting in cold sea surface temperatures (SSTs). The southwesterly, together with the near-equatorial westerly, also results in a surface anticyclone with descending air over most of BOB and a cyclone with ascending air over the southern part of BOB. In the eastern part of central BOB, where sky is clear, surface wind is weak, and ocean mixed layer is shallow, intense solar radiation and low energy loss due to weak surface latent and sensible heat fluxes act onto a thin ocean layer, resulting in the development of a unique BOB warm pool in spring. Near the surface, water vapor is transferred from northern BOB and other regions to southeastern BOB, where surface sensible heating is relatively high. The atmospheric available potential energy is generated and converted to kinetic energy, thereby resulting in vortex formation. The vortex then intensifies and moves northward, where SST is higher and surface sensible heating is stronger. Meanwhile, the zonal-mean kinetic energy is converted to eddy kinetic energy in the area east of the vortex, and the vortex turns eastward. Eventually, southwesterly sweeps over eastern BOB and merges with the subtropical westerly, leading to the onset of the Asian summer monsoon.

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“…[41] Various data sets were used in the sensitivity test, including mean geostrophic velocity data derived from the mean SSH of Maximenko and Niiler [2005] and GRACE [Tapley et al, 2003]; Ekman velocity-derived data from the surface wind stress fields of the National Center for Environmental Prediction/National Center for Atmospheric Research (NCEP/NCAR) reanalysis and that from a blended sea wind product from the National Climate Data Center [Zhang et al, 2006]; a mixed layer depth climatology from de Boyer Montegut et al [2004], World Ocean Atlas 1994 (WOA94), and the World Ocean Atlas 2001 (WOA01). No significant differences in the RMS imbalance were found using various geostrophic and Ekman velocity fields.…”

Section: Appendix A: Sensitivity Of the Salinity Budget To Choice Of mentioning

confidence: 99%

An assessment of the seasonal mixed layer salinity budget in the Southern Ocean

Dong

Garzoli²,

Baringer³

2009

J. Geophys. Res.

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[1] The seasonal cycle of mixed layer salinity and its causes in the Southern Ocean are examined by combining remotely sensed and in situ observations. The domain-averaged terms of oceanic advection, diffusion, entrainment, and air-sea freshwater flux (evaporation minus precipitation) are largely consistent with the seasonal evolution of mixed layer salinity, which increases from March to October and decreases from November to February. This seasonal cycle is largely attributed to oceanic advection and entrainment; air-sea freshwater flux plays only a minimal role. Both oceanic advection-diffusion and the freshwater flux are negative throughout the year, i.e., reduce mixed layer salinity, while entrainment is positive year-round, reaching its maximum in May. The advection-diffusion term is dominated by Ekman advection. Although the spatial structure of the air-sea freshwater flux and oceanic processes are similar for the steady state, the magnitude of the freshwater flux is relatively small when compared to that of the oceanic processes. The spatial structure of the salinity tendency for each month is also well captured by the sum of the contributions from the air-sea freshwater flux, advection-diffusion, and entrainment processes. However, substantial imbalances in the salinity budget exist locally, particularly for regions with strong eddy kinetic energy and sparse in situ measurements. Sensitivity tests suggest that a proper representation of the mixed layer depth, a better freshwater flux product, and an improved surface salinity field are all important for closing the mixed layer salinity budget in the Southern Ocean.

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Assessment of composite global sampling: Sea surface wind speed

Cited by 259 publications

References 14 publications

Surprising return of deep convection to the subpolar North Atlantic Ocean in winter 2007–2008

Surprising return of deep convection to the subpolar North Atlantic Ocean in winter 2007–2008

Air–sea interaction and formation of the Asian summer monsoon onset vortex over the Bay of Bengal

An assessment of the seasonal mixed layer salinity budget in the Southern Ocean

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