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dc.contributor.authorMurray, James W.  Concept link
dc.contributor.authorRoberts, Emily  Concept link
dc.contributor.authorHoward, Evan M.  Concept link
dc.contributor.authorO'Donnell, Michael  Concept link
dc.contributor.authorBantam, Cory  Concept link
dc.contributor.authorCarrington, Emily  Concept link
dc.contributor.authorFoy, Mike  Concept link
dc.contributor.authorPaul, Barbara  Concept link
dc.contributor.authorFay, Amanda  Concept link
dc.date.accessioned2015-06-22T18:04:57Z
dc.date.available2015-06-22T18:04:57Z
dc.date.issued2015-02-19
dc.identifier.citationLimnology and Oceanography 60 (2015): 957–966en_US
dc.identifier.urihttps://hdl.handle.net/1912/7356
dc.description© The Author(s), 2015. This article is distributed under the terms of the Creative Commons Attribution License. The definitive version was published in Limnology and Oceanography 60 (2015): 957–966, doi:10.1002/lno.10062.en_US
dc.description.abstractWe present a time series of data for temperature, salinity, nitrate, and carbonate chemistry from September 2011 to July 2013 at the University of Washington's Friday Harbor Laboratories. Samples were collected at the Friday Harbor dock and pump house. Seawater conditions at Friday Harbor were high nitrate-low chlorophyll, with average nitrate and pCO2 concentrations of ∼ 25 ± 5 μmol L−1 and ∼ 700 ± 103 μatm (pH 7.80 ± 0.06). Transient decreases in surface water nitrate and pCO2 corresponded with the timing of a spring bloom (April through June). The high nitrate and pCO2 originate from the high values for these parameters in the source waters to the Salish Sea from the California Undercurrent (CU). These properties are due to natural aerobic respiration in the region where the CU originates, which is the oxygen minimum zone in the eastern tropical North Pacific. Alkalinity varies little so the increase in pCO2 is due to inputs of dissolved inorganic carbon (DIC). This increase in DIC can come from both natural aerobic respiration within the ocean and input of anthropogenic CO2 from the atmosphere when the water was last at the sea surface. We calculated that the anthropogenic “ocean acidification” contribution to DIC in the source waters of the CU was 36 μmol L−1. This contribution ranged from 13% to 22% of the total increase in DIC, depending on which stoichiometry was used for C/O2 ratio (Redfield vs. Hedges). The remaining increase in DIC was due to natural aerobic respiration.en_US
dc.description.sponsorshipWe thank The Educational Foundation of America (EFA) and National Science Foundation Field Station Marine Lab Program (FSML) (NSF DBI 0829486) for essential initial funding to JWM to develop the Ocean Acidification Experimental Lab (OAEL). Additional support was provided by NSF award EF1041213 to E. Carrington Ken Sebens for encouragement to involve students in this research as part of a FHL mini-apprenticeship course.en_US
dc.format.mimetypeapplication/pdf
dc.language.isoen_USen_US
dc.publisherJohn Wiley & Sonsen_US
dc.relation.urihttps://doi.org/10.1002/lno.10062
dc.rightsAttribution-NonCommercial-NoDerivatives 4.0 International*
dc.rights.urihttp://creativecommons.org/licenses/by-nc-nd/4.0/
dc.titleAn inland sea high nitrate-low chlorophyll (HNLC) region with naturally high pCO2en_US
dc.typeArticleen_US
dc.identifier.doi10.1002/lno.10062


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