Search Results
1. Introduction Two salinity remote sensing satellite missions are expected to be launched in 2009–10. One mission is the Aquarius/Satelite de Aplicaciones Cientificas-D (SAC-D) science mission, developed jointly by the National Aeronautics and Space Administration (NASA) and the Comisión Nacional de Actividades Espaciales (CONAE), the Argentine space agency ( Lagerloef et al. 1995 , 2008 ; Koblinsky et al. 2003 ; Le Vine et al. 2007 ). The other mission is the Soil Moisture and Ocean
1. Introduction Two salinity remote sensing satellite missions are expected to be launched in 2009–10. One mission is the Aquarius/Satelite de Aplicaciones Cientificas-D (SAC-D) science mission, developed jointly by the National Aeronautics and Space Administration (NASA) and the Comisión Nacional de Actividades Espaciales (CONAE), the Argentine space agency ( Lagerloef et al. 1995 , 2008 ; Koblinsky et al. 2003 ; Le Vine et al. 2007 ). The other mission is the Soil Moisture and Ocean
consider vertical gradients of temperature T z < 0 and salinity S z < 0, such that no small-scale double-diffusive convection is initially present (cf. Simeonov and Stern 2007 ); such conditions exist in the Arctic Ocean above the Atlantic water. In the presence of horizontal gradients, this basic state is unstable to lateral intrusions driven by the molecular diffusivities ( Holyer 1983 ). The amplifying intrusion shear will rotate the undisturbed isotherms (isohalines), thereby generating an
consider vertical gradients of temperature T z < 0 and salinity S z < 0, such that no small-scale double-diffusive convection is initially present (cf. Simeonov and Stern 2007 ); such conditions exist in the Arctic Ocean above the Atlantic water. In the presence of horizontal gradients, this basic state is unstable to lateral intrusions driven by the molecular diffusivities ( Holyer 1983 ). The amplifying intrusion shear will rotate the undisturbed isotherms (isohalines), thereby generating an
formation of the saltier and denser Persian Gulf water (PGW) mass. The densest water forms during winter in the northern end of the gulf, where it has a salinity of about 41 psu and temperature maxima higher than 21°C ( Swift and Bower 2003 ). The resulting water deficit in the gulf is compensated for by an inflow of relatively warmer and less saline water of Arabian Sea origin (36.5–37 psu) through the Strait of Hormuz. The low-salinity inflow occurs along the northern side of the strait and spreads
formation of the saltier and denser Persian Gulf water (PGW) mass. The densest water forms during winter in the northern end of the gulf, where it has a salinity of about 41 psu and temperature maxima higher than 21°C ( Swift and Bower 2003 ). The resulting water deficit in the gulf is compensated for by an inflow of relatively warmer and less saline water of Arabian Sea origin (36.5–37 psu) through the Strait of Hormuz. The low-salinity inflow occurs along the northern side of the strait and spreads
-defined North Pacific water masses: high-salinity North Pacific Tropical Water (NPTW) and low-salinity North Pacific Intermediate Water. Figure 1 is a reproduction of their annual-mean salinity map on the σ θ = 25.0 surface, which lies near the high-salinity core of NPTW. At the mouth of the Luzon Strait (nearly parallel to 122°E), salinity is 34.76 psu. The salinity gradually decreases toward the southwest. Near 17°N, the 34.6-psu contour orients more or less in an east–west direction. South of 15°N
-defined North Pacific water masses: high-salinity North Pacific Tropical Water (NPTW) and low-salinity North Pacific Intermediate Water. Figure 1 is a reproduction of their annual-mean salinity map on the σ θ = 25.0 surface, which lies near the high-salinity core of NPTW. At the mouth of the Luzon Strait (nearly parallel to 122°E), salinity is 34.76 psu. The salinity gradually decreases toward the southwest. Near 17°N, the 34.6-psu contour orients more or less in an east–west direction. South of 15°N
1. Introduction A strong modification of surface air temperature in the North Atlantic during the past century has been established ( Mann et al. 1999 )—in the context of global warming. This temperature modification is concomitant with a modification of sea surface salinity (SSS) in the same region noted since the mid-1970s and is related to an increase of precipitation in the North Atlantic subpolar gyre ( Josey and Marsh 2005 ). A similar salinity modification has also been measured in the
1. Introduction A strong modification of surface air temperature in the North Atlantic during the past century has been established ( Mann et al. 1999 )—in the context of global warming. This temperature modification is concomitant with a modification of sea surface salinity (SSS) in the same region noted since the mid-1970s and is related to an increase of precipitation in the North Atlantic subpolar gyre ( Josey and Marsh 2005 ). A similar salinity modification has also been measured in the
1. Introduction Understanding the structure and variability of the salinity distribution in an estuary is critical to many ecological and engineering management decisions. The salinity distribution is governed by a balance between downstream advection of salt by river flow and upstream transport of salt by dispersive processes. These up-estuary fluxes can be divided into a subtidal component due to residual velocity and salinity and an oscillatory tidal component associated with correlations in
1. Introduction Understanding the structure and variability of the salinity distribution in an estuary is critical to many ecological and engineering management decisions. The salinity distribution is governed by a balance between downstream advection of salt by river flow and upstream transport of salt by dispersive processes. These up-estuary fluxes can be divided into a subtidal component due to residual velocity and salinity and an oscillatory tidal component associated with correlations in
the terrestrial water cycle. Studying the freshwater flux over the ocean is very challenging because of the complicated and spatially sparse measurements and the reliance on bulk formulas for various flux products, resulting in large uncertainties between datasets ( Schanze et al. 2010 ). Because of these difficulties, the idea of using sea surface salinity (SSS) as a proxy of the integrated freshwater forcing has emerged ( Schmitt 2008 ; Gordon and Giulivi 2008 ). By removing (adding) freshwater
the terrestrial water cycle. Studying the freshwater flux over the ocean is very challenging because of the complicated and spatially sparse measurements and the reliance on bulk formulas for various flux products, resulting in large uncertainties between datasets ( Schanze et al. 2010 ). Because of these difficulties, the idea of using sea surface salinity (SSS) as a proxy of the integrated freshwater forcing has emerged ( Schmitt 2008 ; Gordon and Giulivi 2008 ). By removing (adding) freshwater
1. Introduction The water masses in the East China Sea (ECS) are characterized by various factors such as the Kuroshio water, river discharge, tidal mixing and atmospheric forcing ( Chang and Isobe 2003 ). Among these factors, the effect of freshwater dominates the distributions of surface salinity in summer when the rivers runoff are high, especially associated with the Changjiang River contributing about 90% of the whole river discharge into the interior of the ECS ( Beardsley et al. 1985
1. Introduction The water masses in the East China Sea (ECS) are characterized by various factors such as the Kuroshio water, river discharge, tidal mixing and atmospheric forcing ( Chang and Isobe 2003 ). Among these factors, the effect of freshwater dominates the distributions of surface salinity in summer when the rivers runoff are high, especially associated with the Changjiang River contributing about 90% of the whole river discharge into the interior of the ECS ( Beardsley et al. 1985
1. Introduction The sea surface temperature (SST) and salinity (SSS) in the tropical Indian Ocean (TIO) play a fundamental role in the density-driven ocean circulation and provide feedback to regional climate ( Schmitt 1994 , 2008 ; Pierce et al. 1995 ; Webster et al. 1999 ; Schott and McCreary 2001 ; Annamalai and Murtugudde 2004 ; Han and McCreary 2001 ; N. Zhang et al. 2016 ). Benefiting from abundant temperature measurements before the 1990s, in-depth investigations into the
1. Introduction The sea surface temperature (SST) and salinity (SSS) in the tropical Indian Ocean (TIO) play a fundamental role in the density-driven ocean circulation and provide feedback to regional climate ( Schmitt 1994 , 2008 ; Pierce et al. 1995 ; Webster et al. 1999 ; Schott and McCreary 2001 ; Annamalai and Murtugudde 2004 ; Han and McCreary 2001 ; N. Zhang et al. 2016 ). Benefiting from abundant temperature measurements before the 1990s, in-depth investigations into the
the boundary current. Allowing the boundary current to exchange buoyancy directly with the atmosphere is crucial in marginal seas such as the Nordic seas, where the boundary current enters at the surface. The surface heat flux depends strongly on the sea surface temperature, whereas the salt flux arising from the freshwater input is much more weakly dependent on the surface salinity. As a consequence, salinity generally adjusts on a longer length scale than temperature. We examine the effect this
the boundary current. Allowing the boundary current to exchange buoyancy directly with the atmosphere is crucial in marginal seas such as the Nordic seas, where the boundary current enters at the surface. The surface heat flux depends strongly on the sea surface temperature, whereas the salt flux arising from the freshwater input is much more weakly dependent on the surface salinity. As a consequence, salinity generally adjusts on a longer length scale than temperature. We examine the effect this
