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Sources and cycling of mercury in the paleo Arctic Ocean from Hg stable isotope variations in Eocene and Quaternary sediments
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Rekke forfattare: 72017 (engelsk)Inngår i: Geochimica et Cosmochimica Acta, ISSN 0016-7037, E-ISSN 1872-9533, Vol. 197, s. 245-262Artikkel i tidsskrift (Fagfellevurdert) Published
Abstract [en]

Mercury stable isotopic compositions were determined for marine sediments from eight locations in the Arctic Ocean Basin. Mass dependent fractionation (MDF) and mass independent fractionation (MIF) of Hg stable isotopes were recorded across a variety of depositional environments, water depths, and stratigraphic ages. delta(202) Hg (MDF) ranges from -2.34% to -0.78%; Delta(199) Hg (MIF) from -0.18% to +0.12%; and Delta(201) Hg (MIF) from -0.29% to + 0.05% for the complete data set (n = 33). Holocene sediments from the Chukchi Sea and Morris Jesup Rise record the most negative Delta(199) Hg values, while Pleistocene sediments from the Central Arctic Ocean record the most positive Delta(199) Hg values. The most negative delta(202) Hg values are recorded in Pleistocene sediments. Eocene sediments (Lomonosov Ridge) show some overlap in their Hg isotopic compositions with Quaternary sediments, with a sample of the Arctic Ocean PETM (56 Ma) most closely matching the average Hg isotopic composition of Holocene Arctic marine sediments. Collectively, these data support a terrestrially-dominated Hg source input for Arctic Ocean sediment through time, although other sources, as well as influences of sea ice, atmospheric mercury depletion events (AMDEs), and anthropogenic Hg (in core top samples) on Hg isotopic signatures must also be considered.

sted, utgiver, år, opplag, sider
2017. Vol. 197, s. 245-262
Emneord [en]
Mercury isotopes, Marine sediments, Central Arctic Ocean, Cenozoic, PETM
HSV kategori
Identifikatorer
URN: urn:nbn:se:su:diva-139362DOI: 10.1016/j.gca.2016.10.033ISI: 000390987700015OAI: oai:DiVA.org:su-139362DiVA, id: diva2:1072718
Tilgjengelig fra: 2017-02-08 Laget: 2017-02-06 Sist oppdatert: 2017-11-29bibliografisk kontrollert

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