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1. Introduction The repeated occupation of full-depth ocean profiles along selected ocean transects are providing a globally distributed time series of highly accurate ocean properties. These time series data enable the broad-scale quantification of temperature and salinity changes in the deep ocean ( Purkey and Johnson 2010 ; Kouketsu et al. 2011 ; Purkey and Johnson 2013 ). In particular, these studies show significant warming and freshening in the high-latitude ocean basins, with the
1. Introduction The repeated occupation of full-depth ocean profiles along selected ocean transects are providing a globally distributed time series of highly accurate ocean properties. These time series data enable the broad-scale quantification of temperature and salinity changes in the deep ocean ( Purkey and Johnson 2010 ; Kouketsu et al. 2011 ; Purkey and Johnson 2013 ). In particular, these studies show significant warming and freshening in the high-latitude ocean basins, with the
1. Introduction Since the beginning of the 2000s, the Argo international program has strongly changed our understanding of the oceanic variability by providing nearly global-scale estimates of temperature and salinity in the upper 2000 dbar ( Argo Science Team 1998 ) and is now recognized as a key component of the global ocean observing system (GOOS). One of the most valuable contributions of the present Argo array is the observation of climate-related ocean variability on broad spatial scales
1. Introduction Since the beginning of the 2000s, the Argo international program has strongly changed our understanding of the oceanic variability by providing nearly global-scale estimates of temperature and salinity in the upper 2000 dbar ( Argo Science Team 1998 ) and is now recognized as a key component of the global ocean observing system (GOOS). One of the most valuable contributions of the present Argo array is the observation of climate-related ocean variability on broad spatial scales
1. Introduction The vertical displacement of waves can be employed to transfer deep, nutrient-rich water to the surface of the ocean using a rather simple pump design originally conceived by Isaacs et al. (1976) . A modern version of this concept is depicted in Fig. 1 . It consists of a vertical pipe attached to a free-floating surface buoy. A valve that opens and closes at opposite phases of a wave cycle is installed at the bottom end of the pipe. As the buoy moves down the surface of a wave
1. Introduction The vertical displacement of waves can be employed to transfer deep, nutrient-rich water to the surface of the ocean using a rather simple pump design originally conceived by Isaacs et al. (1976) . A modern version of this concept is depicted in Fig. 1 . It consists of a vertical pipe attached to a free-floating surface buoy. A valve that opens and closes at opposite phases of a wave cycle is installed at the bottom end of the pipe. As the buoy moves down the surface of a wave
1. Introduction In this paper we report on the multiyear Simple Ocean Data Assimilation (SODA) effort to reconstruct the changing physical climate of the global ocean. The data assimilation approach used is an application of sequential estimation in which a numerical model driven by observed surface forcing is used to provide a first guess of the evolving ocean state, which is then corrected based on direct observations. The resulting ocean reanalysis provides an estimate of the state, which is
1. Introduction In this paper we report on the multiyear Simple Ocean Data Assimilation (SODA) effort to reconstruct the changing physical climate of the global ocean. The data assimilation approach used is an application of sequential estimation in which a numerical model driven by observed surface forcing is used to provide a first guess of the evolving ocean state, which is then corrected based on direct observations. The resulting ocean reanalysis provides an estimate of the state, which is
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SOLO, an Upper-Ocean Autonomous Turbulence-Profiling Float1. Introduction Neutrally buoyant floats have been used for ocean observation since at least as early as the 1950s ( Swallow 1955 ). Over the next few decades, float observations focused on following subsurface currents using acoustic tracking ( Rossby and Webb 1970 ). Acoustic tracking required the support of either moorings or ships, limiting its usefulness to regions where that support was practical. The addition of buoyancy adjustment permitted periodic surfacing of the autonomous
1. Introduction Neutrally buoyant floats have been used for ocean observation since at least as early as the 1950s ( Swallow 1955 ). Over the next few decades, float observations focused on following subsurface currents using acoustic tracking ( Rossby and Webb 1970 ). Acoustic tracking required the support of either moorings or ships, limiting its usefulness to regions where that support was practical. The addition of buoyancy adjustment permitted periodic surfacing of the autonomous
1. Introduction The oceanic mixed layer provides a connection between atmosphere and ocean and thus plays a central role in climate variability. For example, recent studies suggest that changes in the maximum depth of the mixed layer from one winter to the next may explain the reemergence of sea surface temperature (SST) anomalies and thus persistence of wintertime SST patterns ( Alexander et al. 2001 ; Timlin et al. 2002 ; Deser et al. 2003 ). Here we exploit the availability of a newly
1. Introduction The oceanic mixed layer provides a connection between atmosphere and ocean and thus plays a central role in climate variability. For example, recent studies suggest that changes in the maximum depth of the mixed layer from one winter to the next may explain the reemergence of sea surface temperature (SST) anomalies and thus persistence of wintertime SST patterns ( Alexander et al. 2001 ; Timlin et al. 2002 ; Deser et al. 2003 ). Here we exploit the availability of a newly
1. Introduction The global mechanical energy budget was posed as an outstanding first-order problem in the theory of the ocean general circulation 14 years ago ( Munk and Wunsch 1998 ), yet today remains largely unsolved. It is typically assumed that the winds working on the surface general circulation provide the dominant power source ( Munk and Wunsch 1998 ; Wunsch and Ferrari 2004 ). The rate of this forcing has been estimated recently as 0.90 ± 0.05 TW ( Scott and Xu 2009 ) in agreement
1. Introduction The global mechanical energy budget was posed as an outstanding first-order problem in the theory of the ocean general circulation 14 years ago ( Munk and Wunsch 1998 ), yet today remains largely unsolved. It is typically assumed that the winds working on the surface general circulation provide the dominant power source ( Munk and Wunsch 1998 ; Wunsch and Ferrari 2004 ). The rate of this forcing has been estimated recently as 0.90 ± 0.05 TW ( Scott and Xu 2009 ) in agreement
Performance Statistics of a Real-Time Pacific Ocean Weather Sensor Network1. Introduction Over the past century, a tremendous expansion in sampling of the ocean has facilitated broad progress in our understanding of ocean processes ( Davis et al. 2019 ). Ship-based sampling, underwater gliders, Argo floats, and moored platforms have all contributed to monitoring of chemical, biological, and physical dynamics in the ocean. Despite this progress, Earth’s oceans remain heavily undersampled because of the vast scale. In contrast to land and space-based sensing
1. Introduction Over the past century, a tremendous expansion in sampling of the ocean has facilitated broad progress in our understanding of ocean processes ( Davis et al. 2019 ). Ship-based sampling, underwater gliders, Argo floats, and moored platforms have all contributed to monitoring of chemical, biological, and physical dynamics in the ocean. Despite this progress, Earth’s oceans remain heavily undersampled because of the vast scale. In contrast to land and space-based sensing
1. Introduction The ocean mixed layer is a near-surface layer of fluid with quasi-uniform properties such as temperature, salinity, and density. The width of this mixed layer and its time rate of change both strongly influence the ocean’s role in air–sea interaction. However, the width of the near-surface layer of quasi-uniform temperature (MLT) may differ from the width of the near-surface layer of quasi-uniform density (MLD). MLT may be thicker than MLD when positive salinity stratification
1. Introduction The ocean mixed layer is a near-surface layer of fluid with quasi-uniform properties such as temperature, salinity, and density. The width of this mixed layer and its time rate of change both strongly influence the ocean’s role in air–sea interaction. However, the width of the near-surface layer of quasi-uniform temperature (MLT) may differ from the width of the near-surface layer of quasi-uniform density (MLD). MLT may be thicker than MLD when positive salinity stratification
1. Introduction The energy budget of a tropical cyclone is primarily dictated by air–sea fluxes of heat and momentum ( Emanuel 1991 ). The total heat flux between the ocean and atmosphere under tropical cyclone–force winds is dominated by latent heat flux. Generally, in the warm tropical waters where a hurricane forms, the latent heat flux pumps energy into the atmosphere, occasionally exceeding 1000 W m −2 over warm sea surface temperature (SST) during high winds. SST can be greatly reduced
1. Introduction The energy budget of a tropical cyclone is primarily dictated by air–sea fluxes of heat and momentum ( Emanuel 1991 ). The total heat flux between the ocean and atmosphere under tropical cyclone–force winds is dominated by latent heat flux. Generally, in the warm tropical waters where a hurricane forms, the latent heat flux pumps energy into the atmosphere, occasionally exceeding 1000 W m −2 over warm sea surface temperature (SST) during high winds. SST can be greatly reduced
