Formation of Denmark Strait overflow water and its hydro-chemical composition

Tanhua, Toste; Olsson, Kristina; Jeansson, Emil

doi:10.1016/j.jmarsys.2005.05.003

Cited by 69 publications

(105 citation statements)

References 51 publications

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“…Our low surface dAl values agreed with literature values for the ENAB (Barrett et al, 2015;Kramer et al, 2004;Measures et al, 2008;Ussher et al, 2013) and IrB (Middag et al, 2015b), and coincided with low pAl 10 concentrations except over the Greenland shelf (See subsection 3.2.4) (Fig. 2).…”

Section: Regional and Hydrographical Settingssupporting

confidence: 89%

“…Similar observations have been reported for laboratory studies and in the field where dAl decreased as a function of diatom growth and/or the presence of enhanced quantities of biogenic particles (Hydes, 1979;Kremling, 1985;Kremling and Hydes, 1988;Measures et al, 1986;Measures et al, 1984;Orians and Bruland, 1986;Stoffyn, 1979;van Bennekom, 1981). In addition, the transfer from dAl to pAl has been observed in 25 coastal regions (Brown et al, 2010;Moran and Moore, 1988a) and the North Atlantic (Barrett et al, 2015).…”

Section: Dynamic Equilibrium Between Dissolved and Particulate Al Phasessupporting

confidence: 83%

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Aluminium in the North Atlantic Ocean and the Labrador Sea (GEOTRACES GA01 section): roles of continental inputs and biogenic particle removal

Barraqueta¹,

Schlösser²,

Planquette³

et al. 2018

Preprint

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The distribution of dissolved aluminium (dAl) in the water column of the North Atlantic and Labrador Sea was studied along GEOTRACES section GA01 to unravel the sources and sinks of this element. Surface water dAl concentrations were low (median of 2.5 nM) due to low aerosol deposition and removal by phytoplankton. However, surface water dAl concentrations were enhanced on the Iberian and Greenland shelves (up to 30.9 nM) due to continental inputs (rivers, glacial flour and ice melt). A 20 negative correlation was observed between dAl in surface waters and primary production, phytoplankton community structure and biogenic opal production. The abundance of diatoms exerted a significant (p<0.01) control on the surface particulate Al (pAl) to dAl ratios by decreasing dAl levels and increasing pAl levels. Dissolved Al concentrations generally increased with depth and correlated strongly with silicate (R 2 >0.76) west of the Iberian Basin, suggesting net release of dAl at depth during remineralization of sinking biogenic opal containing particles. Enrichment of dAl at near-bottom depths was 25 observed due to resuspension of sediments near the sediment-water interface. The highest dAl (up to 38.7 nM) concentrations were observed in Mediterranean Overflow Waters which act as a major source of dAl to mid depth waters of the eastern North Atlantic. This study clearly shows that the vertical and lateral distribution of dAl in the North Atlantic differs when compared to other regions of the North Atlantic and global ocean due to the large spatial differences both in the main source of Al, atmospheric deposition, and the main sink for Al, particle scavenging, between different oceanic regions. 30Biogeosciences Discuss., https://doi

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Section: Regional and Hydrographical Settingssupporting

confidence: 89%

Section: Dynamic Equilibrium Between Dissolved and Particulate Al Phasessupporting

confidence: 83%

Aluminium in the North Atlantic Ocean and the Labrador Sea (GEOTRACES GA01 section): roles of continental inputs and biogenic particle removal

Barraqueta¹,

Schlösser²,

Planquette³

et al. 2018

Preprint

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“…8). Apparently, this isopycnal connects two endpoints, a relatively saline and a relatively fresh variety of DSOW near $ 601N, DSOW S and DSOW F respectively, endpoints that also were proposed by Tanhua et al (2005) to contribute to the formation of DSOW.…”

Section: The Thermohaline Structure Of the Dsow Variabilitymentioning

confidence: 72%

“…The overflow, appropriately named Denmark Strait Overflow Water, imports the densest source water type for the formation of the water mass that occupies the cold branch of the Atlantic Meridional Overturning Circulation (AMOC), the North Atlantic Deep Water (NADW). According to Tanhua et al (2005) deep water types of both the Nordic seas (low salinity component) and the Arctic Ocean (high salinity component) are important for the formation of DSOW. At approximately 601N along the AR7E section, DSOW (Fig.…”

Section: Introductionmentioning

confidence: 99%

Hydrographic variability of Denmark Strait Overflow Water near Cape Farewell with multi-decadal to weekly time scales

Aken

Jong

2012

Deep Sea Research Part I: Oceanographic Research Papers

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This article appeared in a journal published by Elsevier. The attached copy is furnished to the author for internal non-commercial research and education use, including for instruction at the authors institution and sharing with colleagues.Other uses, including reproduction and distribution, or selling or licensing copies, or posting to personal, institutional or third party websites are prohibited. a b s t r a c tData in temperature and salinity from near-bottom layer of Denmark Strait Overflow Water in the Irminger Sea near 601N are presented. These are hydrographic section data from data archives, literature, and CTD observations along the former WOCE AR7E line, as well as data from continuous measurements at two locations. For both salinity and temperature, hydrographic variability was present at all time scales that could be analysed, from multi-decadal to weekly. A mechanistic explanation for the primal cause of the hydrographic variability is still lacking. The direct cause of the observed variability has to be sought in variations of the properties of the source water types involved in the overflow across the sill in Denmark Strait, variations in the mutual ratios of these source water types, and in inhomogeneities in the DSOW layer. The strongest changes occurred at the longest time scales, as is often found for ultimately randomly forced geophysical time series. However, a significant annual cycle of the DSOW, not reported before, was observed at the foot of the East Greenland continental slope, likely a deterministic contribution to the hydrographic variability signal.

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“…The use of SF 6 as a transient tracer in the ocean is restricted to well-ventilated water masses where the partial pressure is above the detection limit of the analytical system (≈ 0.1 fmol kg −1 or ≈ 0.4 ppt at salinity 35 and potential temperature 4 • C). SF 6 has been used for deliberate tracer release experiments and as such there is potential for undefined offsets in concentrations in such survey areas and their surroundings (Tanhua et al, 2005(Tanhua et al, , 2008. …”

Section: Sulfur Hexafluoridementioning

confidence: 99%

Perspectives of transient tracer applications and limiting cases

2015

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Abstract. Currently available transient tracers have different application ranges that are defined by their temporal input (chronological transient tracers) or their decay rate (radioactive transient tracers). Transient tracers range from tracers for highly ventilated water masses such as sulfur hexafluoride (SF 6 ) through tritium ( 3 H) and chlorofluorocarbons (CFCs) up to tracers for less ventilated deep ocean basins such as argon-39 ( 39 Ar) and radiocarbon ( 14 C). In this context, highly ventilated water masses are defined as water masses that have been in contact with the atmosphere during the last decade. Transient tracers can be used to empirically constrain the transit time distribution (TTD), which can often be approximated with an inverse Gaussian (IG) distribution. The IG-TTD provides information about ventilation and the advective/diffusive characteristics of a water parcel.Here we provide an overview of commonly used transient tracer couples and the corresponding application range of the IG-TTD by using the new concept of validity areas. CFC-12, CFC-11 and SF 6 data from three different cruises in the South Atlantic Ocean and Southern Ocean as well as 39 Ar data from the 1980s and early 1990s in the eastern Atlantic Ocean and the Weddell Sea are used to demonstrate this method. We found that the IG-TTD can be constrained along the Greenwich Meridian south to 46 • S, which corresponds to the Subantarctic Front (SAF) denoting the application limit. The Antarctic Intermediate Water (AAIW) describes the limiting water layer in the vertical. Conspicuous high or lower ratios between the advective and diffusive components describe the transition between the validity area and the application limit of the IG-TTD model rather than describing the physical properties of the water parcel. The combination of 39 Ar and CFC data places constraints on the IG-TTD in the deep water north of the SAF, but not beyond this limit.

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Formation of Denmark Strait overflow water and its hydro-chemical composition

Cited by 69 publications

References 51 publications

Aluminium in the North Atlantic Ocean and the Labrador Sea (GEOTRACES GA01 section): roles of continental inputs and biogenic particle removal

Aluminium in the North Atlantic Ocean and the Labrador Sea (GEOTRACES GA01 section): roles of continental inputs and biogenic particle removal

Hydrographic variability of Denmark Strait Overflow Water near Cape Farewell with multi-decadal to weekly time scales

Perspectives of transient tracer applications and limiting cases

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