On the spatial and temporal distribution of near-inertial energy in the Southern Ocean

We use an eddying realistic primitive equation model of the Southern Ocean to examine the spatial and temporal distribution of near-inertial wind-power input (WPI) and near-inertial energy (NIE) in the Southern Ocean. We find that the modelled near-inertial WPI is almost proportional to inertial wind-stress variance (IWSV), while the modelled NIE is modulated by the inverse of the mixed-layer depth. We go on to assess recent decadal trends of near-inertial WPI from trends of IWSV based on reanalysis wind-stress. Averaged over the Southern Ocean, annual-mean IWSV is found to have increased by 16 percent over the years 1979 through 2011. Part of the increase of IWSV is found to be related to the positive trend of the Southern Annular Mode over the same period. Finally, we show that there are horizontal local maxima of NIE at depth that are almost exclusively associated with anticyclonic eddies

Sea Surface Salinity And Barrier Layer Variability In The Equatorial Pacific As Seen From Aquarius And Argo

ISI Document Delivery No.: AB6DZ Times Cited: 0 Cited Reference Count: 52 Cited References: Alory G, 2012, J GEOPHYS RES-OCEANS, V117, DOI 10.1029/2011JC007802 Ando K, 1997, J GEOPHYS RES-OCEANS, V102, P23063, DOI 10.1029/97JC01443 Argo Steering Team, 1998, 21 ARG STEER TEAM IN, V21 BINGHAM FM, 1995, DEEP-SEA RES PT I, V42, P1545, DOI 10.1016/0967-0637(95)00064-D Bosc C, 2009, J GEOPHYS RES-OCEANS, V114, DOI 10.1029/2008JC005187 Boutin J, 2013, OCEAN SCI, V9, P183, DOI 10.5194/os-9-183-2013 Boyer TP, 2002, J GEOPHYS RES-OCEANS, V107, DOI 10.1029/2001JC000829 Chen D, 2004, J TROP OCEANOGR, V23, P1 Cronin MF, 2002, J GEOPHYS RES-OCEANS, V107, DOI 10.1029/2001JC001171 de Boyer Montegut C., 2004, J GEOPHYS RES, V109, DOI 10.1029/2004JC002378 Delcroix T, 2002, J GEOPHYS RES-OCEANS, V107, DOI 10.1029/2001JC000862 DELCROIX T, 1992, J GEOPHYS RES-OCEANS, V97, P5423, DOI 10.1029/92JC00127 Fujii Y, 2003, J GEOPHYS RES-OCEANS, V108, DOI 10.1029/2002JC001745 GODFREY JS, 1989, J GEOPHYS RES-OCEANS, V94, P8007, DOI 10.1029/JC094iC06p08007 Hasegawa T, 2013, J CLIMATE, V26, P8126, DOI 10.1175/JCLI-D-12-00187.1 Henocq C, 2010, J ATMOS OCEAN TECH, V27, P192, DOI 10.1175/2009JTECHO670.1 Johnson ES, 2002, J GEOPHYS RES-OCEANS, V107, DOI 10.1029/2001JC001122 Juza M, 2012, J OPER OCEANOGR, V5, P45 Kalnay E, 1996, B AM METEOROL SOC, V77, P437, DOI 10.1175/1520-0477(1996)0772.0.CO;2 Kessler WS, 1998, J CLIMATE, V11, P777, DOI 10.1175/1520-0442(1998)0112.0.CO;2 KESSLER WS, 1990, J GEOPHYS RES-OCEANS, V95, P5183, DOI 10.1029/JC095iC04p05183 Lagerloef G., 2013, AQ014OPS0016 Lagerloef G, 2008, OCEANOGRAPHY, V21, P68 Lee T, 2012, GEOPHYS RES LETT, V39, DOI 10.1029/2012GL052232 Levitus S., 1982, 13 NOAA LINDSTROM E, 1987, NATURE, V330, P533, DOI 10.1038/330533a0 LUKAS R, 1991, J GEOPHYS RES-OCEANS, V96, P3343 Maes C, 2004, GEOPHYS RES LETT, V31, DOI 10.1029/2004GL019867 Maes C, 2008, J GEOPHYS RES-OCEANS, V113, DOI 10.1029/2007JC004297 Maes C, 2011, SOLA, V7, P97, DOI 10.2151/sola.2011-025 Maes C, 2006, GEOPHYS RES LETT, V33, DOI 10.1029/2005GL024772 Maes C, 2000, GEOPHYS RES LETT, V27, P1659, DOI 10.1029/1999GL011261 Maes C, 2002, GEOPHYS RES LETT, V29, DOI 10.1029/2002GL016029 Maes C, 2005, J CLIMATE, V18, P104, DOI 10.1175/JCLI-3214.1 Lukas R, 1996, J GEOPHYS RES-OCEANS, V101, P12209, DOI 10.1029/96JC01204 MCPHADEN MJ, 1992, J GEOPHYS RES-OCEANS, V97, P14289, DOI 10.1029/92JC01197 MCPHADEN MJ, 1990, SCIENCE, V250, P1385, DOI 10.1126/science.250.4986.1385 PALMER TN, 1984, NATURE, V310, P483, DOI 10.1038/310483a0 Picaut J, 2001, J GEOPHYS RES-OCEANS, V106, P2363, DOI 10.1029/2000JC900141 Picaut J, 1997, SCIENCE, V277, P663, DOI 10.1126/science.277.5326.663 Qu TD, 1999, J PHYS OCEANOGR, V29, P1488, DOI 10.1175/1520-0485(1999)0292.0.CO;2 Qu TD, 2013, J PHYS OCEANOGR, V43, P1551, DOI 10.1175/JPO-D-12-0180.1 Qu TD, 2008, GEOPHYS RES LETT, V35, DOI 10.1029/2008GL035058 Reverdin G., 2013, OCEANOGRAPHY, V26, P4857, DOI 10.5670/oceanog.2013.04 Riser SC, 2008, OCEANOGRAPHY, V21, P56 Rodier M., 2000, J OCEANOGR, V56, P463, DOI 10.1023/A:1011136608053 SHINODA T, 1995, J GEOPHYS RES-OCEANS, V100, P2523, DOI 10.1029/94JC02486 Singh A, 2011, J GEOPHYS RES-OCEANS, V116, DOI 10.1029/2010JC006862 Song Y. T., 2013, J GEOPHYS R IN PRESS SPRINTALL J, 1992, J GEOPHYS RES-OCEANS, V97, P7305, DOI 10.1029/92JC00407 Takahashi K, 2011, GEOPHYS RES LETT, V38, DOI 10.1029/2011GL047364 Yu JY, 2007, J GEOPHYS RES-ATMOS, V112, DOI 10.1029/2006JD007654 Qu, Tangdong Song, Y. Tony Maes, Christophe NSF [OCE11-30050]; NASA [NNX12AG02G]; Jet Propulsion Laboratory, California Institute of Technology, under NASA; IRD T. Qu was supported by NSF through grant OCE11-30050 and by NASA as part of the Aquarius Science Team investigation through grant NNX12AG02G. Y. T. Song was supported by the Jet Propulsion Laboratory, California Institute of Technology, under contracts with NASA. C. Maes is supported by IRD. The authors are grateful to N. Schneider and I. Fukumori for useful discussion on the topic, to K. Yu for assistance in processing the Aquarius data, and to two anonymous reviewers for valuable comments on this manuscript. School of Ocean and Earth Science and Technology contribution number 9054 and International Pacific Research Center contribution IPRC-1033. 0 AMER GEOPHYSICAL UNION WASHINGTON J GEOPHYS RES-OCEANSThis study investigates the sea surface salinity (SSS) and barrier layer variability in the equatorial Pacific using recently available Aquarius and Argo data. Comparison between the two data sets indicates that Aquarius is able to capture most of the SSS features identified by Argo. Despite some discrepancies in the mean value, the SSS from the two data sets shows essentially the same seasonal cycle in both magnitude and phase. For the period of observation between August 2011 and July 2013 Aquarius nicely resolved the zonal displacement of the SSS front along the equator, showing its observing capacity of the western Pacific warm pool. Analysis of the Argo data provides further information on surface stratification. A thick barrier layer is present on the western side of the SSS front during all the period of observation, moving back and forth along the equator with its correlation with the Southern Oscillation Index exceeding 0.80. Generally, the thick barrier layer moves eastward during El Nino and westward during La Nina. The mechanisms responsible for this zonal displacement are discussed. Key Points Aquarius nicely resolved the SSS front along the equator in the western Pacific A thick barrier layer is always present on the western side of the SSS front Both the SSS front and thick barrier layer are highly correlated with ENS

Cirene : air-sea iInteractions in the Seychelles-Chagos thermocline ridge region

Author Posting. © American Meteorological Society, 2009. This article is posted here by permission of American Meteorological Society for personal use, not for redistribution. The definitive version was published in Bulletin of the American Meteorological Society 90 (2009): 1337-1350, doi:10.1175/2008BAMS2499.1.The Vasco—Cirene program ex-plores how strong air—sea inter-actions promoted by the shallow thermocline and high sea surface temperature in the Seychelles—Chagos thermocline ridge results in marked variability at synoptic, intraseasonal, and interannual time scales. The Cirene oceano-graphic cruise collected oceanic, atmospheric, and air—sea flux observations in this region in Jan-uary—February 2007. The contem-poraneous Vasco field experiment complemented these measure-ments with balloon deployments from the Seychelles. Cirene also contributed to the development of the Indian Ocean observing system via deployment of a moor-ing and 12 Argo profilers. Unusual conditions prevailed in the Indian Ocean during Janu-ary and February 2007, following the Indian Ocean dipole climate anomaly of late 2006. Cirene measurements show that the Seychelles—Chagos thermocline ridge had higher-than-usual heat content with subsurface anomalies up to 7°C. The ocean surface was warmer and fresher than average, and unusual eastward currents prevailed down to 800 m. These anomalous conditions had a major impact on tuna fishing in early 2007. Our dataset also sampled the genesis and maturation of Tropical Cyclone Dora, including high surface temperatures and a strong diurnal cycle before the cyclone, followed by a 1.5°C cool-ing over 10 days. Balloonborne instruments sampled the surface and boundary layer dynamics of Dora. We observed small-scale structures like dry-air layers in the atmosphere and diurnal warm layers in the near-surface ocean. The Cirene data will quantify the impact of these finescale features on the upper-ocean heat budget and atmospheric deep convection.CNES funded the Vasco part of the experiment; INSU funded the Cirene part. R/V Suroît is an Ifremer ship. The contributions from ODU, WHOI, and FOI (Sweden) are supported by the National Science Foundation under Grant Number 0525657. The participation of the University of Miami group was funded though NASA (NNG04HZ33C). PMEL participation was supported through NOAA’s Office of Climate Observation

A comparison of five surface mixed layer models with a year of observations in the North Atlantic

Five upper ocean mixed layer models driven by ERA-Interim surface forcing are compared with a year of hydrographic observations of the upper 1000 m, taken at the Porcupine Abyssal Plain observatory site using profiling gliders. All the models reproduce sea surface temperature (SST) fairly well, with annual mean warm biases of 0.11  ° C (PWP model), 0.24  ° C (GLS), 0.31  ° C (TKE), 0.91  ° C (KPP) and 0.36  ° C (OSMOSIS). The main exception is that the KPP model has summer SSTs which are higher than the observations by nearly 3 ° . Mixed layer salinity (MLS) is not reproduced well by the models and the biases are large enough to produce a non-trivial density bias in the Eastern North Atlantic Central Water which forms in this region in winter. All the models develop mixed layers which are too deep in winter, with average winter mixed layer depth (MLD) biases between 160 and 228 m. The high variability in winter MLD is reproduced more successfully by model estimates of the depth of active mixing and/or boundary layer depth than by model MLD based on water column properties. After the spring restratification event, biases in MLD are small and do not appear to be related to the preceding winter biases. There is a very clear relationship between MLD and local wind stress in all models and in the observations during spring and summer, with increased wind speeds leading to deepening mixed layers, but this relationship is not present during autumn and winter. We hypothesize that the deepening of the MLD in autumn is so strongly driven by the annual cycle in surface heat flux that the winds are less significant in the autumn. The surface heat flux drives a diurnal cycle in MLD and SST from March onwards, though this effect is much more significant in the models than in the observations. We are unable to identify one model as definitely better than the others. The only clear differences between the models are KPP’s inability to accurately reproduce summer SSTs, and the OSMOSIS model’s more accurate reproduction of MLS

Phenology and time series trends of the dominant seasonal phytoplankton bloom across global scales

Aim This study examined phytoplankton blooms on a global scale, with the intention of describing patterns of bloom timing and size, the effect of bloom timing on the size of blooms, and time series trends in bloom characteristics. Location Global. Methods We used a change‐point statistics algorithm to detect phytoplankton blooms in time series (1998–2015) of chlorophyll concentration data over a global grid. At each study location, the bloom statistics for the dominant bloom, based on the search time period that resulted in the most blooms detected, were used to describe the spatial distribution of bloom characteristics over the globe. Time series of bloom characteristics were also subjected to trend analysis to describe regional and global changes in bloom timing and size. Results The characteristics of the dominant bloom were found to vary with latitude and in localized patterns associated with specific oceanographic features. Bloom timing had the most profound effect on bloom duration, with early blooms tending to last longer than later‐starting blooms. Time series of bloom timing and duration were trended, suggesting that blooms have been starting earlier and lasting longer, respectively, on a global scale. Blooms have also increased in size at high latitudes and decreased in equatorial areas based on multiple size metrics. Main conclusions Phytoplankton blooms have changed on both regional and global scales, which has ramifications for the function of food webs providing ecosystem services. A tendency for blooms to start earlier and last longer will have an impact on energy flow pathways in ecosystems, differentially favouring the productivity of different species groups. These changes may also affect the sequestration of carbon in ocean ecosystems. A shift to earlier bloom timing is consistent with the expected effect of warming ocean climate conditions observed in recent decades

Couche mélangée océanique et bilan thermohalin de surface dans l'Océan Indien Nord

PARIS-BIUSJ-Thèses (751052125) / SudocPARIS-BIUSJ-Sci.Terre recherche (751052114) / SudocSudocFranceF

Dossier d'étude du promoteur (reflet de l'application des bonnes pratiques cliniques)

Les essais cliniques nécessitent la participation de nombreux centres dans de multiples pays, ceci posant des problèmes notamment au niveau des différentes législations. Les ICH ont permis grâce aux recommandations qu'elles fournissent de poser des bases communes à la mise en place et au déroulement d'un essai. Une des recommandations essentielles concerne les Bonnes Pratiques Cliniques qui ont été intégrées dans les législations européennes, japonaises et nord-américaines. Le dossier d'étude du promoteur peut être considéré comme le reflet de l'application des BPC au cours des essais cliniques, les différentes étapes de l'étude étant retracées à travers les documents archivés dans ce dossier. Ce dossier, témoin de la collaboration des intervenants participant aux études, garantit un médicament dont le développement a été effectué dans le respect des BPC et des recommandations des ICH.TOULOUSE3-BU Santé-Centrale (315552105) / SudocTOULOUSE3-BU Santé-Allées (315552109) / SudocSudocFranceF

Role of fronts in the formation of Arabian Sea barrier layers during summer monsoon

The barrier layer (BL) - a salinity stratification embedded in the upper warm layer - is a common feature of the tropical oceans. In the northern Indian Ocean, it has the potential to significantly alter the air-sea interactions. In the present paper, we investigate the spatio-temporal structure of BL in the Arabian Sea during summer monsoon. This season is indeed a key component of the Asian climate. Based on a comprehensive dataset of Conductivity-Temperature-Depth (CTD) and Argo in situ hydrographic profiles, we find that a BL exists in the central Arabian Sea during summer. However, it is highly heterogeneous in space, and intermittent, with scales of about similar to 100 km or less and a couple of weeks. The BL patterns appear to be closely associated to the salinity front separating two water masses (Arabian Sea High Salinity Water in the Northern and Eastern part of the basin, fresher Bay of Bengal Water to the south and to the west). An ocean general circulation model is used to infer the formation mechanism of the BL. It appears that thick (more than 40 m) BL patterns are formed at the salinity front by subduction of the saltier water mass under the fresher one in an area of relatively uniform temperature. Those thick BL events, with variable position and timing, result in a broader envelope of thinner BL in climatological conditions. However, the individual patterns of BL are probably too much short-lived to significantly affect the monsoonal air-sea interactions