Structure of Southern Ocean fronts at 140°E

Sokolov, Serguei; Rintoul, Stephen R.

doi:10.1016/s0924-7963(02)00200-2

Cited by 250 publications

(271 citation statements)

References 23 publications

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“…Deep water masses were identified by the following criteria: CDW ¼ oxygen minimum (Upper Circumpolar Deep) or salinity maximum (Lower Circumpolar Deep); AABW ¼ deep potential temperature minimum; AAIW ¼ salinity minimum 18 . The major fronts of the SO, which coincide with strong horizontal gradients in temperature and salinity 19,30 , separate regions with similar surface water properties. The AZ lies south of the Polar Front (which was at 51°S during sampling), whereas the PFZ lies between the Polar Front and the Subantarctic Front.…”

Section: Methodsmentioning

confidence: 99%

Advection shapes Southern Ocean microbial assemblages independent of distance and environment effects

et al. 2013

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Section: Methodsmentioning

confidence: 99%

Advection shapes Southern Ocean microbial assemblages independent of distance and environment effects

et al. 2013

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“…Rintoul and Sokolov (2001) have estimated mass, heat, salt and nutrient fluxes from these sections. Frontal variations from these sections were reported in Sokolov and Rintoul (2002).…”

Section: Introductionmentioning

confidence: 91%

“…Between the PF and the SAF exists another high temperature gradient zone extending to the full depth of the observation and forming a separate front. Since it marks the northern limit of T min and bounds the upper circumpolar deep water to the south, we identify it as a polar front also, although Sokolov and Rintoul (2002) This double PF structure is apparently a regional phenomenon near some major topography. Sparrow et al (1996) found the separate surface and sub-surface expressions of the PF near the Kerguelen Plateau just west of our XBT/XCTD transects.…”

mentioning

confidence: 93%

Upper ocean thermohaline structure and its temporal variability in the southeast Indian Ocean

Yuan¹,

Martinson²,

Dong³

2004

Deep Sea Research Part I: Oceanographic Research Papers

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We examine the upper ocean thermohaline structure in the southeast Indian Ocean and its We find a strong temporal variation in the upper ocean thermal structure in the polar ocean southeast the Kerguelen Plateau. The depths of the mixed layer and T min layer increase over time. The mixed layer temperature decreases while the T min temperature increases during the same period. In addition, we see an increase from 1998 to 2002 in the length of the ice-free period prior to each XBT/XCTD sampling and surface wind forcing, calculated as the friction velocity cubed during the ice-free period. Our analysis suggests that the longer the ocean is exposed to the atmosphere and the stronger the wind stirring, the more enhanced is the turbulent mixing. This results in a greater mixed layer depth and more entrainment of colder water from the T min layer to the mixed layer. This surface forcing also enhances internal diffusive processes that mix the T min water with the warmer waters above and below the T min layer. The surface forcing is apparently dominant in determining the upper ocean thermal structure in this polar region.

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“…1) is characterized by a number of fronts that separate the major water masses of the region (Sokolov and Rintoul, 2002, 2007, 2009. At the northern end of the section, the presence of the weak Subtropical Front (STF, Fig.…”

Section: Hydrography Of the Regionmentioning

confidence: 99%

Carbon uptake and biogeochemical change in the Southern Ocean, south of Tasmania

et al. 2017

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Abstract. Biogeochemical change in the water masses of the Southern Ocean, south of Tasmania, was assessed for the 16-year period between 1995 and 2011 using data from four summer repeats of the WOCE-JGOFS-CLIVAR-GO-SHIP (Key et al., 2015;Olsen et al., 2016) SR03 hydrographic section (at ∼ 140 • E). Changes in temperature, salinity, oxygen, and nutrients were used to disentangle the effect of solubility, biology, circulation and anthropogenic carbon (C ANT ) uptake on the variability of dissolved inorganic carbon (DIC) for eight water mass layers defined by neutral surfaces (γ n ). C ANT was estimated using an improved back-calculation method. Warming (∼ 0.0352 ± 0.0170 • C yr −1 ) of Subtropical Central Water (STCW) and Antarctic Surface Water (AASW) layers decreased their gas solubility, and accordingly DIC concentrations increased less rapidly than expected from equilibration with rising atmospheric CO 2 (∼ 0.86 ± 0.16 µmol kg −1 yr −1 versus ∼ 1 ± 0.12 µmol kg −1 yr −1 ). An increase in apparent oxygen utilisation (AOU) occurred in these layers due to either remineralisation of organic matter or intensification of upwelling. The range of estimates for the increases in C ANT were 0.71 ± 0.08 to 0.93 ± 0.08 µmol kg −1 yr −1 for STCW and 0.35 ± 0.14 to 0.65 ± 0.21 µmol kg −1 yr −1 for AASW, with the lower values in each water mass obtained by assigning all the AOU change to remineralisation. DIC increases in the Sub-Antarctic Mode Water (SAMW, 1.10 ± 0.14 µmol kg −1 yr −1 ) and Antarctic Intermediate Water (AAIW, 0.40 ± 0.15 µmol kg −1 yr −1 ) layers were similar to the calculated C ANT trends. For SAMW, the C ANT increase tracked rising atmospheric CO 2 . As a consequence of the general DIC increase, decreases in total pH (pH T ) and aragonite saturation ( Ar ) were found in most water masses, with the upper ocean and the SAMW layer presenting the largest trends for pH T decrease (∼ −0.0031 ± 0.0004 yr −1 ). DIC increases in deep and bottom layers (∼ 0.24 ± 0.04 µmol kg −1 yr −1 ) resulted from the advection of old deep waters to resupply increased upwelling, as corroborated by increasing silicate (∼ 0.21 ± 0.07 µmol kg −1 yr −1 ), which also reached the upper layers near the Antarctic Divergence (∼ 0.36 ± 0.06 µmol kg −1 yr −1 ) and was accompanied by an increase in salinity. The observed changes in DIC over the 16-year span caused a shoaling (∼ 340 m) of the aragonite saturation depth (ASD, Ar = 1) within Upper Circumpolar Deep Water that followed the upwelling path of this layer. From all our results, we conclude a scenario of increased transport of deep waters into the section and enhanced upwelling at high latitudes for the period between 1995 and 2011 linked to strong westerly winds. Although enhanced upwelling lowered the capacity of the AASW layer to uptake atmospheric CO 2 , it did not limit that of the newly forming SAMW and AAIW, which exhibited C ANT storage rates (∼ 0.41 ± 0.20 mol m −2 yr −1 ) twice that of the upper layers.

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Structure of Southern Ocean fronts at 140°E

Cited by 250 publications

References 23 publications

Advection shapes Southern Ocean microbial assemblages independent of distance and environment effects

Advection shapes Southern Ocean microbial assemblages independent of distance and environment effects

Upper ocean thermohaline structure and its temporal variability in the southeast Indian Ocean

Carbon uptake and biogeochemical change in the Southern Ocean, south of Tasmania

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