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  • 2010-2014  (11)
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Year
  • 1
    Type of Medium: Book
    Pages: S. 2051 - 2315 , graph. Darst
    Series Statement: Deep sea research 58.2011,21/22
    Language: English
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  • 2
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    Unknown
    PANGAEA
    In:  Supplement to: Croot, Peter L; Bowie, Andrew R; Frew, Russell; Maldonado, Maria T; Hall, Julie A; Safi, Karl A; La Roche, Julie; Boyd, Philip W; Law, Cliff S (2001): Retention of dissolved iron and Fe II in an iron induced Southern Ocean phytoplankton bloom. Geophysical Research Letters, 28(18), 3425-3428, https://doi.org/10.1029/2001GL013023
    Publication Date: 2023-01-13
    Description: During the 13 day Southern Ocean Iron RE-lease Experiment (SOIREE), dissolved iron concentrations decreased rapidly following each of three iron-enrichments, but remained high (〉1 nM, up to 80% as FeII) after the fourth and final enrichment on day 8. The former trend was mainly due to dilution (spreading of iron-fertilized waters) and particle scavenging. The latter may only be explained by a joint production-maintenance mechanism; photoreduction is the only candidate process able to produce sufficiently high FeII, but as such levels persisted overnight (8 hr dark period) -ten times the half-life for this species- a maintenance mechanism (complexation of FeII) is required, and is supported by evidence of increased ligand concentrations on day 12. The source of these ligands and their affinity for FeII is not known. This retention of iron probably permitted the longevity of this bloom raising fundamental questions about iron cycling in HNLC (High Nitrate Low Chlorophyll) Polar waters.
    Keywords: Comment; Date/Time of event; DEPTH, water; Error; Event label; GOFLO; Go-Flo bottles; Iron, dissolved; Iron, dissolved, conditional complex stability; Iron-binding ligand, dissolved; Latitude of event; Longitude of event; SOIREE; Southern Ocean - Australasian-Pacific Sector; T1136-1; T1139-1; T1140-6; T1141-6; T1144-6; T1151-5; T1152-5; T1158-5; T1159-6; T1160-3; T1162-4; T1171-5; Tangaroa; Voltammetry
    Type: Dataset
    Format: text/tab-separated-values, 64 data points
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  • 3
    Publication Date: 2023-07-08
    Keywords: AMT1/1995-09-25; AMT1/1995-09-26; AMT1/1995-09-27; AMT1/1995-09-28; AMT1/1995-09-29; AMT1/1995-09-30; AMT1/1995-10-02; AMT1/1995-10-03; AMT1/1995-10-04; AMT1/1995-10-05; AMT1/1995-10-06; AMT1/1995-10-07; AMT1/1995-10-08; AMT1/1995-10-09; AMT1/1995-10-10; AMT1/1995-10-11; AMT1/1995-10-12; AMT1/1995-10-13; AMT1/1995-10-14; AMT1/1995-10-15; AMT1/1995-10-16; AMT1/1995-10-17; AMT1/1995-10-18; AMT1/1995-10-19; AMT1/1995-10-20; AMT10/2000-04-15; AMT10/2000-04-17; AMT10/2000-04-19; AMT10/2000-04-20; AMT10/2000-04-22; AMT10/2000-04-23; AMT10/2000-04-24; AMT10/2000-04-25; AMT10/2000-04-26; AMT10/2000-04-28; AMT10/2000-04-29; AMT10/2000-05-01; AMT10/2000-05-02; AMT2/1996-04-23; AMT2/1996-04-24; AMT2/1996-04-25; AMT2/1996-04-29; AMT2/1996-04-30; AMT2/1996-05-01; AMT2/1996-05-02; AMT2/1996-05-03; AMT2/1996-05-04; AMT2/1996-05-05; AMT2/1996-05-06; AMT2/1996-05-07; AMT2/1996-05-08; AMT2/1996-05-09; AMT2/1996-05-10; AMT2/1996-05-11; AMT2/1996-05-12; AMT2/1996-05-14; AMT2/1996-05-15; AMT2/1996-05-16; AMT2/1996-05-17; AMT2/1996-05-18; AMT2/1996-05-19; AMT2/1996-05-20; AMT2/1996-05-21; AMT3/1996-09-24; AMT3/1996-09-25; AMT3/1996-09-26; AMT3/1996-09-27; AMT3/1996-09-28; AMT3/1996-09-29; AMT3/1996-09-30; AMT3/1996-10-02; AMT3/1996-10-03; AMT3/1996-10-04; AMT3/1996-10-05; AMT3/1996-10-06; AMT3/1996-10-07; AMT3/1996-10-08; AMT3/1996-10-09; AMT3/1996-10-10; AMT3/1996-10-11; AMT3/1996-10-12; AMT3/1996-10-13; AMT3/1996-10-14; AMT3/1996-10-15; AMT3/1996-10-16; AMT3/1996-10-23; AMT3/1996-10-24; AMT3/1996-10-25; AMT4/1997-04-21; AMT4/1997-04-22; AMT4/1997-04-23; AMT4/1997-04-30; AMT4/1997-05-01; AMT4/1997-05-02; AMT4/1997-05-03; AMT4/1997-05-04; AMT4/1997-05-05; AMT4/1997-05-06; AMT4/1997-05-07; AMT4/1997-05-08; AMT4/1997-05-09; AMT4/1997-05-10; AMT4/1997-05-11; AMT4/1997-05-12; AMT4/1997-05-13; AMT4/1997-05-14; AMT4/1997-05-15; AMT4/1997-05-16; AMT4/1997-05-17; AMT4/1997-05-18; AMT4/1997-05-19; AMT4/1997-05-20; AMT4/1997-05-21; AMT4/1997-05-22; AMT4/1997-05-23; AMT5/1997-09-17; AMT5/1997-09-18; AMT5/1997-09-19; AMT5/1997-09-20; AMT5/1997-09-21; AMT5/1997-09-22; AMT5/1997-09-25; AMT5/1997-09-26; AMT5/1997-09-27; AMT5/1997-09-28; AMT5/1997-09-29; AMT5/1997-09-30; AMT5/1997-10-01; AMT5/1997-10-02; AMT5/1997-10-03; AMT5/1997-10-04; AMT5/1997-10-05; AMT5/1997-10-06; AMT5/1997-10-07; AMT5/1997-10-08; AMT5/1997-10-09; AMT5/1997-10-10; AMT5/1997-10-11; AMT5/1997-10-12; AMT5/1997-10-13; AMT5/1997-10-14; AMT5/1997-10-15; AMT5/1997-10-16; AMT6/1998-05-16; AMT6/1998-05-17; AMT6/1998-05-21; AMT6/1998-05-22; AMT6/1998-05-23; AMT6/1998-05-24; AMT6/1998-05-25; AMT6/1998-05-27; AMT6/1998-05-28; AMT6/1998-05-29; AMT6/1998-05-30; AMT6/1998-05-31; AMT6/1998-06-01; AMT6/1998-06-02; AMT6/1998-06-03; AMT6/1998-06-04; AMT6/1998-06-05; AMT6/1998-06-06; AMT6/1998-06-07; AMT6/1998-06-08; AMT6/1998-06-09; AMT7/1998-09-15; AMT7/1998-09-16; AMT7/1998-09-17; AMT7/1998-09-22; AMT7/1998-09-23; AMT7/1998-09-25; AMT7/1998-09-26; AMT7/1998-09-27; AMT7/1998-09-28; AMT7/1998-09-29; AMT7/1998-10-01; AMT7/1998-10-02; AMT7/1998-10-03; AMT7/1998-10-04; AMT7/1998-10-05; AMT7/1998-10-06; AMT7/1998-10-07; AMT7/1998-10-08; AMT7/1998-10-09; AMT7/1998-10-10; AMT7/1998-10-11; AMT7/1998-10-12; AMT7/1998-10-13; AMT7/1998-10-14; AMT7/1998-10-15; AMT7/1998-10-16; AMT8/1999-05-05; AMT8/1999-05-06; AMT8/1999-05-07; AMT8/1999-05-08; AMT8/1999-05-09; AMT8/1999-05-10; AMT8/1999-05-12; AMT8/1999-05-13; AMT8/1999-05-18; AMT8/1999-05-19; AMT8/1999-05-20; AMT8/1999-05-21; AMT8/1999-05-22; AMT8/1999-05-23; AMT8/1999-05-24; AMT8/1999-05-25; AMT8/1999-05-26; AMT8/1999-05-27; AMT8/1999-05-28; AMT8/1999-05-29; AMT8/1999-05-30; AMT8/1999-05-31; AMT8/1999-06-01a; AMT8/1999-06-01b; AMT8/1999-06-02; AMT8/1999-06-03; AMT8/1999-06-04; Atlantic; Calculated after Luo et al. (2012); Date/Time of event; DEPTH, water; Diazotrophs, total biomass as carbon; Event label; Latitude of event; Light microscope; Longitude of event; MAREDAT_Diazotrophs_Collection; MULT; Multiple investigations; Sample comment; Trichodesmium, biomass as carbon; Trichodesmium, carbon per trichome; Trichodesmium abundance, colonies; Trichodesmium abundance, total
    Type: Dataset
    Format: text/tab-separated-values, 1342 data points
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  • 4
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    Unknown
    PANGAEA
    In:  Supplement to: Cossa, Daniel; Heimbürger, Lars-Eric; Lannuzel, Delphine; Rintoul, Stephen R; Butler, Edward C V; Bowie, Andrew R; Averty, Bernard; Watson, Roslyn J; Remenyi, Tomas (2011): Mercury in the Southern Ocean. Geochimica et Cosmochimica Acta, 75(14), 4037-4052, https://doi.org/10.1016/j.gca.2011.05.001
    Publication Date: 2023-12-13
    Description: We present here the first mercury speciation study in the water column of the Southern Ocean, using a high-resolution south-to-north section (27 stations from 65.50°S to 44.00°S) with up to 15 depths (0-4440 m) between Antarctica and Tasmania (Australia) along the 140°E meridian. In addition, in order to explore the role of sea ice in Hg cycling, a study of mercury speciation in the 'snow-sea ice-seawater' continuum was conducted at a coastal site, near the Australian Casey station (66.40°S; 101.14°E). In the open ocean waters, total Hg (Hg(T)) concentrations varied from 0.63 to 2.76 pmol/L with 'transient-type' vertical profiles and a latitudinal distribution suggesting an atmospheric mercury source south of the Southern Polar Front (SPF) and a surface removal north of the Subantartic Front (SAF). Slightly higher mean Hg(T) concentrations (1.35 ± 0.39 pmol/L) were measured in Antarctic Bottom Water (AABW) compared to Antarctic Intermediate water (AAIW) (1.15 ± 0.22 pmol/L). Labile Hg (Hg(R)) concentrations varied from 0.01 to 2.28 pmol/L, with a distribution showing that the Hg(T) enrichment south of the SPF consisted mainly of Hg(R) (67 ± 23%), whereas, in contrast, the percentage was half that in surface waters north of PFZ (33 ± 23%). Methylated mercury species (MeHg(T)) concentrations ranged from 0.02 to 0.86 pmol/L. All vertical MeHg(T) profiles exhibited roughly the same pattern, with low concentrations observed in the surface layer and increasing concentrations with depth up to an intermediate depth maximum. As for Hg(T), low mean MeHg(T) concentrations were associated with AAIW, and higher ones with AABW. The maximum of MeHg(T) concentration at each station was systematically observed within the oxygen minimum zone, with a statistically significant MeHg(T) vs Apparent Oxygen Utilization (AOU) relationship (p 〈0.001). The proportion of Hg(T) as methylated species was lower than 5% in the surface waters, around 50% in deep waters below 1000 m, reaching a maximum of 78% south of the SPF. At Casey coastal station Hg(T) and Hg(R) concentrations found in the 'snow-sea ice-seawater' continuum were one order of magnitude higher than those measured in open ocean waters. The distribution of Hg(T) there suggests an atmospheric Hg deposition with snow and a fractionation process during sea ice formation, which excludes Hg from the ice with a parallel Hg enrichment of brine, probably concurring with the Hg enrichment of AABW observed in the open ocean waters. Contrastingly, MeHg(T) concentrations in the sea ice environment were in the same range as in the open ocean waters, remaining below 0.45 pmol/L. The MeHg(T) vertical profile through the continuum suggests different sources, including atmosphere, seawater and methylation in basal ice. Whereas Hg(T) concentrations in the water samples collected between the Antarctic continent and Tasmania are comparable to recent measurements made in the other parts of the World Ocean (e.g., Soerensen et al., 2010; doi:10.1021/es903839n), the Hg species distribution suggests distinct features in the Southern Ocean Hg cycle: (i) a net atmospheric Hg deposition on surface water near the ice edge, (ii) the Hg enrichment in brine during sea ice formation, and (iii) a net methylation of Hg south of the SPF.
    Keywords: GEOTRACES; Global marine biogeochemical cycles of trace elements and their isotopes; International Polar Year (2007-2008); IPY
    Type: Dataset
    Format: application/zip, 3 datasets
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  • 5
    Publication Date: 2024-04-16
    Keywords: Date/Time of event; DEPTH, water; Event label; GOFLO; Go-Flo bottles; Graphite furnace atomic absorption spectrometer (GF-AAS); Iron; Iron, dissolved; Iron, standard deviation; JGOFS; Joint Global Ocean Flux Study; Latitude of event; Longitude of event; SOIREE; Southern Ocean - Australasian-Pacific Sector; T1136-1; T1139-1; T1140-6; T1143; T1144-6; T1147-2; T1151-13; T1151-5; T1152-5; T1154-2; T1158-5; T1159-6; T1160-3; T1162-4; T1171-10; T1171-5; Tangaroa
    Type: Dataset
    Format: text/tab-separated-values, 174 data points
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  • 6
    Publication Date: 2022-05-25
    Description: Author Posting. © The Author(s), 2011. This is the author's version of the work. It is posted here by permission of Elsevier B.V. for personal use, not for redistribution. The definitive version was published in Marine Chemistry 126 (2011): 108-113, doi:10.1016/j.marchem.2011.04.004.
    Description: Photosynthesis by marine phytoplankton requires bioavailable forms of several trace elements that are found in extremely low concentrations in the open ocean. We have compared the concentration, lability and size distribution (〈 1 nm and 〈 10 nm) of a suite of trace elements that are thought to be limiting to primary productivity as well as a toxic element (Pb) in two High Nutrient Low Chlorophyll (HNLC) regions using a new dynamic speciation technique, Diffusive Gradients in Thin-film (DGT). The labile species trapped within the DGT probes have a size that is smaller or similar than the pore size of algal cell walls and thus present a proxy for bioavailable species. Total Dissolvable trace element concentrations (TD concentration) varied between 0.05 nM (Co) and 4.0 nM (Ni) at K2 (Northwest Pacific Ocean) and between 0.026 nM (Co) and 4.7 nM (Ni) in the Southern Ocean. The smallest size fractionated labile concentrations (〈 1 nm) observed at Southern Ocean sampling stations ranged between 0.002 nM (Co) and 2.1 nM (Ni). Moreover, large differences in bioavailable fractions (ratio of labile to TD concentration) were observed between the trace elements. In the Northwest Pacific Ocean Fe, Cu and Mn had lower labile fractions (between 10 and 44%) than Co, Cd, Ni and Pb (between 80 and 100%). In the Southern Ocean a similar trend was observed, and in addition: (1) Co, Cd, Ni and Pb have lower labile fractions in the Southern Ocean than in the Northwest Pacific and (2) the ratios of 〈1nm to dissolvable element concentrations at some Southern Ocean stations were very low and varied between 4 and16 %.
    Description: This research was supported by Federal Science Policy Office, Brussels, through contracts EV/03/7A, SD/CA/03A, the Research Foundation Flanders through grant G.0021.04 and Vrije Universiteit Brussel via grant GOA 22, as well as for K2, the VERTIGO program funding primarily by the US National Science Foundation programs in Chemical and Biological Oceanography
    Keywords: Trace elements ; Speciation ; Bioavailability ; Pacific Ocean ; Southern Ocean
    Repository Name: Woods Hole Open Access Server
    Type: Preprint
    Format: application/pdf
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  • 7
    Publication Date: 2022-05-25
    Description: Author Posting. © The Author(s), 2011. This is the author's version of the work. It is posted here by permission of Elsevier B.V. for personal use, not for redistribution. The definitive version was published in Deep Sea Research Part II: Topical Studies in Oceanography 58 (2011): 2094-2112, doi:10.1016/j.dsr2.2011.05.027.
    Description: This paper presents iron (Fe) profiles in the upper 1000 m from nine short-term (transect) stations and three long-term (process) stations occupied in the Australian sector of the Southern Ocean during the SAZ-Sense expedition in austral summer (January–February) 2007. Strong vertical and horizontal gradients in Fe concentrations were observed between the 18 sampled profiles (i.e. 0.09–0.63 nmol/l dissolved Fe (dFe)). Average dFe concentrations in surface waters in the northern Sub-Antarctic Zone (SAZ-N) West (station P1) were 0.27±0.04 nmol/l. This is lower than in the SAZ-N East region (station P3 and around) where average dFe values in the mixed layer were 0.48±0.10 nmol/l. The Polar Front (PF) station (P2) exhibited the lowest average surface Fe values (i.e. 0.22±0.02 nmol/l). Iron concentrations in deep waters down to 1000 m were more uniform (0.25–0.37 nmol/l dFe), which is in accordance with values reported elsewhere in remote waters of the Southern Ocean, but lower than those observed in the North Atlantic and North Pacific basins. A strong decoupling was observed between dFe and nutrient cycles at all stations. Particulate Fe levels were generally very low for all SAZ stations (〈0.08 – 1.38 nmol/l), with higher values observed at stations collected near Tasmania and in the SAZ-N East region. The intrusion of subtropical waters, enriched with Fe from sediments or dust further north, is thought to mediate Fe input to the SAZ-N and STZ areas, while input from below would be the main source of Fe in the PF region. We applied the tracer Fe* (Fe*= [dFe]-RFe:P × [PO4 3-], where RFe:P is the algal uptake ratio) to estimate the degree to which the water masses were Fe limited. In this study, Fe* tended to be negative and decreased with increasing depths and latitude. Positive Fe* values, indicating Fe sufficiency, were observed in the (near-)surface waters collected in the SAZ-N East and near continental sources, where primary production was higher and ultimately limited by the lack of macro-nutrients, not Fe. Micro-organisms residing in the SAZ-N West and PF on the other hand experienced negative Fe*, indicating a strong co-limitation by low silicic acid concentration and Fe supply (and light in the case of PF).
    Description: This research was supported by the Belgian Federal Science Policy Office (contracts SD/CA/03A, OA/00/025), the Australian Government Cooperative Research Centres Program through the Antarctic Climate and Ecosystems CRC (ACE CRC) and Australian Antarctic Science project #2720.
    Keywords: Iron ; Distributions ; Macro-nutrients ; Biogeochemistry ; Southern Ocean
    Repository Name: Woods Hole Open Access Server
    Type: Preprint
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  • 8
    Publication Date: 2022-05-25
    Description: Author Posting. © Association for the Sciences of Limnology and Oceanography, 2013. This article is posted here by permission of Association for the Sciences of Limnology and Oceanography for personal use, not for redistribution. The definitive version was published in Limnology and Oceanography: Methods 11 (2013): 62-78, doi:10.4319/lom.2013.11.62.
    Description: Atmospheric deposition of trace elements and isotopes (TEI) is an important source of trace metals to the open ocean, impacting TEI budgets and distributions, stimulating oceanic primary productivity, and influencing biological community structure and function. Thus, accurate sampling of aerosol TEIs is a vital component of ongoing GEOTRACES cruises, and standardized aerosol TEI sampling and analysis procedures allow the comparison of data from different sites and investigators. Here, we report the results of an aerosol analysis intercalibration study by seventeen laboratories for select GEOTRACES-relevant aerosol species (Al, Fe, Ti, V, Zn, Pb, Hg, NO3 , and SO42 ) for samples collected in September 2008. The collection equipment and filter substrates are appropriate for the GEOTRACES program, as evidenced by low blanks and detection limits relative to analyte concentrations. Analysis of bulk aerosol sample replicates were in better agreement when the processing protocol was constrained (± 9% RSD or better on replicate analyses by a single lab, n = 7) than when it was not (generally 20% RSD or worse among laboratories using different methodologies), suggesting that the observed variability was mainly due to methodological differences rather than sample heterogeneity. Much greater variability was observed for fractional solubility of aerosol trace elements and major anions, due to differing extraction methods. Accuracy is difficult to establish without an SRM representative of aerosols, and we are developing an SRM for this purpose. Based on these findings, we provide recommendations for the GEOTRACES program to establish consistent and reliable procedures for the collection and analysis of aerosol samples.
    Description: This work was partially funded by the following sources: US National Science Foundation (NSF) grant OCE- 0752832 (PLM, WML, and AM), National Science Council Taiwan grant 100-2628-M-001-008-MY4 (SCH), US NSF grant OCE-1137836 (AMA-I), United Kingdom Natural Environmental Research Council (NERC) grant NE/H00548X/1 (AR Baker), Australian Government Cooperative Research Centres Programme (AR Bowie), US NSF grant OCE-0824304 (CSB and Adina Paytan), US NSF grants OCE-0825068 and OCE- 0728750 (SG and Robert Mason), US NSF grant OCE-0961038 (MGH), US NSF grant OCE-0752609 (MH and Christopher Measures), US NSF grant ATM-0839851 (AMJ), US NSF grant OCE-1031371 (CM), UK NERC grant NE/C001931/1 (MDP and Eric Achterberg), US NSF grant OCE-1132515 (GS and Carl Lamborg), US NSF grant OCE-0851462 (AV and Thomas Church), and US NSF grant OCE-0623189 (LMZ). This paper is part of the Intercalibration in Chemical Oceanography special issue of L&O Methods that was supported by funding from the US National Science Foundation, Chemical Oceanography Program (grant OCE-0927285 to Gregory Cutter).
    Repository Name: Woods Hole Open Access Server
    Type: Article
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  • 9
    Publication Date: 2022-05-26
    Description: Author Posting. © American Geophysical Union, 2009. This article is posted here by permission of American Geophysical Union for personal use, not for redistribution. The definitive version was published in Global Biogeochemical Cycles 23 (2009): GB4034, doi:10.1029/2009GB003500.
    Description: Climate change is projected to significantly alter the delivery (stratification, boundary currents, aridification of landmasses, glacial melt) of iron to the Southern Ocean. We report the most comprehensive suite of biogeochemical iron budgets to date for three contrasting sites in subantarctic and polar frontal waters south of Australia. Distinct regional environments were responsible for differences in the mode and strength of iron supply mechanisms, with higher iron stocks and fluxes observed in surface northern subantarctic waters, where atmospheric iron fluxes were greater. Subsurface waters southeast of Tasmania were also enriched with particulate iron, manganese and aluminum, indicative of a strong advective source from shelf sediments. Subantarctic phytoplankton blooms are thus driven by both seasonal iron supply from southward advection of subtropical waters and by wind-blown dust deposition, resulting in a strong decoupling of iron and nutrient cycles. We discuss the broader global significance our iron budgets for other ocean regions sensitive to climate-driven changes in iron supply.
    Description: T.W. was supported by a BDI grant from CNRS and Région PACA, by CNRS PICS project 3604, and by the “Soutien à la mer” CSOA CNRS-INSU. P.W.B. was supported by the New Zealand FRST Coasts and Oceans OBI. This research was supported by the Australian Government Cooperative Research Centres Programme through the Antarctic Climate and Ecosystems CRC (ACE CRC) and Australian Antarctic Science project 2720.
    Keywords: Iron ; Southern Ocean ; Biogeochemical budget ; Subantarctic ; Polar ; Australian sector
    Repository Name: Woods Hole Open Access Server
    Type: Article
    Format: text/plain
    Format: application/pdf
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  • 10
    Publication Date: 2017-08-28
    Description: Iron limits phytoplankton growth and hence the biological carbon pump in the Southern Ocean1. Models assessing the impacts of iron on the global carbon cycle generally rely on dust input and sediment resuspension as the predominant sources2, 3. Although it was previously thought that most iron from deep-ocean hydrothermal activity was inaccessible to phytoplankton because of the formation of particulates4, it has been suggested that iron from hydrothermal activity5, 6, 7 may be an important source of oceanic dissolved iron8, 9, 10, 11, 12, 13. Here we use a global ocean model to assess the impacts of an annual dissolved iron flux of approximately 9×108 mol, as estimated from regional observations of hydrothermal activity11, 12, on the dissolved iron inventory of the world’s oceans. We find the response to the input of hydrothermal dissolved iron is greatest in the Southern Hemisphere oceans. In particular, observations of the distribution of dissolved iron in the Southern Ocean3 (Chever et al., manuscript in preparation; Bowie et al., manuscript in preparation) can be replicated in our simulations only when our estimated iron flux from hydrothermal sources is included. As the hydrothermal flux of iron is relatively constant over millennial timescales14, we propose that hydrothermal activity can buffer the oceanic dissolved iron inventory against shorter-term fluctuations in dust deposition.
    Type: Article , PeerReviewed
    Format: text
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