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; Masozera et al. 2007 ) that have analyzed the impact of Hurricane Katrina on environmental, social, and biophysical aspects of the affected areas, several studies have tried to analyze the impact of Katrina on forest vegetation. Rodgers et al. ( Rodgers et al. 2009 ) investigated the vegetation changes in the Weeks Bay Reserve after Hurricane Katrina using normalized difference vegetation index (NDVI) data and found that the NDVI values were suppressed after Katrina because of the increased salinity
; Masozera et al. 2007 ) that have analyzed the impact of Hurricane Katrina on environmental, social, and biophysical aspects of the affected areas, several studies have tried to analyze the impact of Katrina on forest vegetation. Rodgers et al. ( Rodgers et al. 2009 ) investigated the vegetation changes in the Weeks Bay Reserve after Hurricane Katrina using normalized difference vegetation index (NDVI) data and found that the NDVI values were suppressed after Katrina because of the increased salinity
% surface irrigation system and complete adoption of greater-efficiency irrigation systems is probably unrealistic because surface irrigation predominates in some regions for certain crops and for salinity control. Additionally, more advanced irrigation infrastructure often requires a larger investment that cannot be offset by the crop revenue ( Seo et al. 2008 ; Schuck et al. 2005 ). Therefore, we prefer to view this result for the western United States not as predictions of actual adaptation but
% surface irrigation system and complete adoption of greater-efficiency irrigation systems is probably unrealistic because surface irrigation predominates in some regions for certain crops and for salinity control. Additionally, more advanced irrigation infrastructure often requires a larger investment that cannot be offset by the crop revenue ( Seo et al. 2008 ; Schuck et al. 2005 ). Therefore, we prefer to view this result for the western United States not as predictions of actual adaptation but
large albedo increase; (iii) the town of San Luis, Argentina; and (iv) a saline lake (Salinas del Bebedero). (e),(f) Quickbird images accessed through Google Earth showing a close up of the recent increase in albedo (ii) resulting from a decrease in vegetative cover likely from grazing. Figure 7. An example of albedo decreases associated with reservoirs in arid regions. Gray areas mask low quality data. (a) Change in albedo in a region of interest near the
large albedo increase; (iii) the town of San Luis, Argentina; and (iv) a saline lake (Salinas del Bebedero). (e),(f) Quickbird images accessed through Google Earth showing a close up of the recent increase in albedo (ii) resulting from a decrease in vegetative cover likely from grazing. Figure 7. An example of albedo decreases associated with reservoirs in arid regions. Gray areas mask low quality data. (a) Change in albedo in a region of interest near the
generate the SOCV. The source of heat is inflow of the North Atlantic Deep Water (NADW), which indicates a large-scale link between the Northern and Southern Hemispheres. The SOCV signal generated in the South Atlantic also propagates to the North Atlantic via different processes. Swingedouw et al. (2009) proposed three ways of connections: deep-water adjustment via oceanic waves, salinity anomaly advection, and wind impact on the NADW cell. Each has different response time scales in the model, of
generate the SOCV. The source of heat is inflow of the North Atlantic Deep Water (NADW), which indicates a large-scale link between the Northern and Southern Hemispheres. The SOCV signal generated in the South Atlantic also propagates to the North Atlantic via different processes. Swingedouw et al. (2009) proposed three ways of connections: deep-water adjustment via oceanic waves, salinity anomaly advection, and wind impact on the NADW cell. Each has different response time scales in the model, of
the next sampling period. A subsample of the rainwater samples was tested for salinity using a Brix refractometer at the time of collection. Vacutainers were stored in a refrigerator (4°C) in the laboratory until analysis at the Laboratory of Stable Isotope Ecology in Tropical Ecosystems (University of Miami). A total of 49 rainwater samples were analyzed in triplicate for δ 18 O and δD by mass spectrometry using methods described by Vendramini and Sternberg ( Vendramini and Sternberg 2007
the next sampling period. A subsample of the rainwater samples was tested for salinity using a Brix refractometer at the time of collection. Vacutainers were stored in a refrigerator (4°C) in the laboratory until analysis at the Laboratory of Stable Isotope Ecology in Tropical Ecosystems (University of Miami). A total of 49 rainwater samples were analyzed in triplicate for δ 18 O and δD by mass spectrometry using methods described by Vendramini and Sternberg ( Vendramini and Sternberg 2007
-dominated vegetation is adapted to saline conditions and sedimentation provides a source of soil nutrients. We found no clear trend in vegetation cover in coastal plain, although we did observe local mortality of shrubs due to salt-kill, as well as ground subsidence caused by permafrost thaw ( Whitley et al. 2018 ). Reports from YKD elders provide intriguing evidence of vegetation changes both during the intercomparison period, and entirely preceding the satellite record. These reports provide evidence of stress
-dominated vegetation is adapted to saline conditions and sedimentation provides a source of soil nutrients. We found no clear trend in vegetation cover in coastal plain, although we did observe local mortality of shrubs due to salt-kill, as well as ground subsidence caused by permafrost thaw ( Whitley et al. 2018 ). Reports from YKD elders provide intriguing evidence of vegetation changes both during the intercomparison period, and entirely preceding the satellite record. These reports provide evidence of stress
). Although the coastal ocean is 0.5% of the total ocean volume, it contributes > 30% of the entire air–ocean CO 2 exchange. These exchange processes account for > 80% of the oceanic organic matter burial ( Chen and Borges 2009 ). The ability of the coastal ocean to act as a CO 2 sink mainly depends on salinity, solubility, temperature, and the gas transfer velocity ( Yang et al. 2021 ) through the wind-induced turbulent mixing in the atmospheric surface layer (ASL) ( Mari 2008 ; Riebesell et
). Although the coastal ocean is 0.5% of the total ocean volume, it contributes > 30% of the entire air–ocean CO 2 exchange. These exchange processes account for > 80% of the oceanic organic matter burial ( Chen and Borges 2009 ). The ability of the coastal ocean to act as a CO 2 sink mainly depends on salinity, solubility, temperature, and the gas transfer velocity ( Yang et al. 2021 ) through the wind-induced turbulent mixing in the atmospheric surface layer (ASL) ( Mari 2008 ; Riebesell et
, including Soil Moisture and Ocean Salinity (SMOS) mission ( Kerr et al. 2010 ) and the recently launched Soil Moisture Active Passive (SMAP; Entekhabi et al. 2010 ). While these products cover large areas, the spatial resolution is often coarse (e.g., 35–50 km for SMOS, 10 km for SMAP) and measure only the top 5 cm of soil. This combined with the difficulty to validate these products make them unsuitable for some applications requiring soil water storage dynamics in the entire root zone (~0–100 cm
, including Soil Moisture and Ocean Salinity (SMOS) mission ( Kerr et al. 2010 ) and the recently launched Soil Moisture Active Passive (SMAP; Entekhabi et al. 2010 ). While these products cover large areas, the spatial resolution is often coarse (e.g., 35–50 km for SMOS, 10 km for SMAP) and measure only the top 5 cm of soil. This combined with the difficulty to validate these products make them unsuitable for some applications requiring soil water storage dynamics in the entire root zone (~0–100 cm
cumulative gridcell area for harvested grid cells as a percentage of total global gridcell area. Figure 7. Global map of coastal hypoxic areas in relation to N application in fertilizers. Figure 2a is overlain with selected global basins that discharge into saline receiving waters (where nitrogen represents the dominant limiting nutrient) and location of documented hypoxic areas from Diaz and Rosenberg ( Diaz and Rosenberg 2008 ). Table
cumulative gridcell area for harvested grid cells as a percentage of total global gridcell area. Figure 7. Global map of coastal hypoxic areas in relation to N application in fertilizers. Figure 2a is overlain with selected global basins that discharge into saline receiving waters (where nitrogen represents the dominant limiting nutrient) and location of documented hypoxic areas from Diaz and Rosenberg ( Diaz and Rosenberg 2008 ). Table
the model, including temperature and salinity, are configured for the North Atlantic grid using Levitus climatology. Detailed description of this model, its skill assessment, and relevant results were presented in Chaudhuri et al. (2011a , b) . A major goal of this effort was to study the mean response of the GS to representative low and high NAO condition/forcing. This model was able to realistically reproduce the GS path ( Chaudhuri et al. 2011a ) and was then used to study the impact of
the model, including temperature and salinity, are configured for the North Atlantic grid using Levitus climatology. Detailed description of this model, its skill assessment, and relevant results were presented in Chaudhuri et al. (2011a , b) . A major goal of this effort was to study the mean response of the GS to representative low and high NAO condition/forcing. This model was able to realistically reproduce the GS path ( Chaudhuri et al. 2011a ) and was then used to study the impact of
