<div><p><strong>Sampling and Analytical Methodology: </strong><br />
Water samples were collected with a Sea-Bird Electronics CTD carousel fitted with 24 10-liter PVC Niskin bottles. The carousel was lowered from the ship with steel wire. Niskin bottles caps were held together with rubber tubing. After collection seawater was drained with Teflon-lined TygonTM tubing and filtered through Pall AcropakTM 500 filters on deck (gravity filtration, 0.8/0.45 µm pore size) into Fisher I-Chem series 300 LDPE cubitainers. Approximately 9-10 L was collected per desired depth. Prior to the cruise, the tubing, filters and cubitainers were cleaned by immersion in 1.2 M HCl (Fisher Scientific Trace Metal Grade) for 4-5 days. Once filtered, samples were adjusted to a pH ~2 with ultra-clean 6 M HCl (Tama Chemicals, TAMAPURE-AA-100 grade), double-bagged and stored at room temperature as packaged until analysis.</p>
<p>In the on-shore laboratory, samples were weighed to determine sample size, taking into account the weight of the cubitainer and of the acid added at sea. Four to five liters of the original sample was used for Th/Pa analysis, the remaining sample kept as archive. Then weighed aliquots of the artificial isotope yield monitors 229Th (20 pg) and 233Pa (0.5 pg) and 15 mg dissolved Fe were added to each sample. After allowing 1 day for spike equilibration, the pH of each sample was raised to 8-8.5 by adding ~10 mL of concentrated NH4OH (Fisher Scientific OPTIMA grade) which caused iron (oxy)hydroxide precipitates to form. This precipitate was allowed to settle for 1-2 days before the overlaying seawater was siphoned off. The Fe precipitate was transferred to centrifuge tubes for centrifugation and rinsing with Milli-Q H2O (>18 MO) to remove the major seawater ions. The precipitate was then dissolved in 16 M HNO3 (Fisher Scientific OPTIMA grade) and transferred to a Teflon beaker for a high-temperature (180-200°C) digestion with HClO4 and HF (Fisher Scientific OPTIMA grade) on a hotplate in a HEPA-filtered laminar flow hood. After total dissolution of the sample, another precipitation of iron (oxy)hydroxide followed and the precipitate was washed with Mill-Q H2O, centrifuged, and dissolved in 12 M HCl for a series of anion-exchange chromatography using 6 mL polypropylene columns each containing a 1 mL bed of Bio-rad resin (AG1-X8, 100-200 mesh size) and a 45 µm porous polyethylene frit. The final column elutions were dried down at 180°C in the presence of 2 drops of HClO4 and taken up in approximately 1 mL of 0.16 M HNO3/0.026 M HF for mass spectrometric analysis. </p>
<p>Concentrations of 232Th, 230Th and 231Pa were calculated by isotope dilution using nuclide ratios determined on a VG Elemental AXIOM Single Collector Magnetic Sector ICP-MS with a Resolving Power of ~400 to ensure the highest sensitivity. All measurements were done using a peak jumping routine in ion counting mode. A solution of SRM129, a natural U standard, was run to determine the mass bias correction (assuming that the mass fractionation for Th and Pa are the same as for U). Each sample measurement was bracketed by measurement of an aliquot of the run solution, used to correct for the instrument background count rates on the masses measured. To correct for potential tailing of 232Th into the minor Th and Pa isotopes, beam intensities were measured at the half masses above and below each mass for 230Th, 231Pa, and 233Pa. Tailing under each minor isotope was estimated as the log mean intensity of the half masses on either side of each minor isotope.</p>
<p>Water samples were analyzed in batches of 10-12. Procedural blanks were determined by processing 4-5 L of Milli-Q water in an acid-cleaned cubitainer acidified to pH ~2 with 6 M HCl as a sample in each batch. An aliquot of an intercalibrated working standard solution of 232Th, 230Th and 231Pa, SW STD 2010-1 referred to by Anderson et al. (2012), was added to a separate cubitainer with 5 L of Milli-Q water (acidified to pH 2) and also processed like a sample in each batch. Total procedural blanks for 232Th, 230Th, and 231Pa ranged from 7.1-24.3 pg, 0.8-1.6 fg, and 0.02-0.2 fg respectively. One batch had an anomalously high 232Th blank of 140 pg (with 230Th and 231Pa in the reported range). Application of this blank correction to the analyzed SW STD caused an anomalously low estimate of its 232Th concentration (approximately 990 ± 15 pg/g). From this we concluded the blank was due to random contamination of the procedural blank and it should not be used to blank-correct samples. Instead, we determined what magnitude of blank correction would be necessary for the analyzed SW STD to achieve the intercalibrated concentration. This was 12 pg 232Th, which is close to the average blank value measured throughout the course of this project. </p>
<p>Further details on sampling and analysis are given by Anderson et al. (2012).</p></div>
Depth profiles of seawater dissolved 232Th, 230Th, and 231Pa, NW Pacific
<div><p>Depth profiles of seawater dissolved 232Th, 230Th, and 231Pa at seven sites in the NW Pacific.</p>
<p>This dataset is published:<br />
Hayes, C.T., Anderson, R.F., Jaccard, S.L., François, R., Fleisher, M.Q., Soon, M., Gersonde, R., 2013. A new perspective on boundary scavenging in the North Pacific Ocean. Earth Planet. Sci. Lett. 369-370, 86-97.<br /><a href="https://dx.doi.org/10.1016/j.epsl.2013.03.008">http://dx.doi.org/10.1016/j.epsl.2013.03.008</a><br /><a href="http://www.sciencedirect.com/science/article/pii/S0012821X13001295">http://www.sciencedirect.com/science/article/pii/S0012821X13001295</a></p>
<p>These data are also available through PANGAEA: <a href="/objectserver/f8709e93fd7dcdaba6ef43b34863a672/PANGAEA.811760?url=http%3A%2F%2Fdoi.pangaea.de%2F10.1594%2FPANGAEA.811760&f=3565373439386331363730363334306462323638363632623035386131616539687474703a2f2f646f692e70616e676165612e64652f31302e313539342f50414e474145412e383131373630">http://doi.pangaea.de/10.1594/PANGAEA.811760</a></p></div>
Dissolved Th/Pa - SO-202
<div><p><strong>Data Processing:</strong></p>
<p>The reported errors for radionuclide concentrations represent the propagation of one sigma errors based on the standard deviation of five sequences of isotope ratios collected by ICP-MS, estimated error in the 229Th or 233Pa spike concentration, and the blank correction of the individual isotopes for each sample batch.</p>
<p>Analysis of all samples was completed over the course of 2 years. A correction was made to account for the ingrowth of 230Th and 231Pa due to the decay of the natural 234U and 235U preserved in the acidified samples during the period of time between sample collection and U-Th/Pa separation during anion exchange chromatography. Thus, the reported 230Th and 231Pa concentrations have been corrected to represent their concentrations at the time of sampling. U concentrations in the samples were estimated using the bottle salinity (S) measured from the CTD and the U-Salinity relationship of North Pacific seawater (Chen et al., 1986), [U] = (0.1115*S – 0.6356) ng U (g seawater)-1. We used seawater U-isotopic compositions of 234U/238 U = 1.1468 activity ratio (Andersen et al., 2010), and 238U/235U = 137.824 mole ratio (Weyer et al., 2008), to calculate [234U] and [235U] respectively based on [U]. In our submitted manuscript (Hayes et al., submitted) we converted gravimetric concentration (fg/kg) into volumetric activities (dpm m-3) for easier comparison to historical data. The half-lives used were 75,690 yrs for 230Th (Cheng et al., 2000), 32,760 yrs for 231Pa (Robert et al., 1969), 245,250 yrs for 234U (Cheng et al., 2000), and 7.0381 x 108 yrs for 235U (Jaffey et al. 1971).</p>
<p><strong>Related files and references: </strong><br />
Anderson, R.F., Fleisher, M.Q., Robinson, L.F., Edwards, R.L., Hoff, J., Moran, S.B., Rutgers van der Loeff, M.M., Thomas, A.L., Roy-Barman, M., François, R., 2012. GEOTRACES intercalibration of 230Th, 232Th, 231Pa, and prospects for 10Be. Limnol. Oceanogr. Methods 10, 179-213.</p>
<p>Chen, J.H., Lawrence Edwards, R., Wasserburg, G.J., 1986. 238U, 234U and 232Th in seawater. Earth Planet. Sci. Lett. 80, 241-251.</p>
<p>Cheng, H., Edwards, R.L., Hoff, J., Gallup, C.D., Richards, D.A., Asmerom, Y., 2000. The half-lives of uranium-234 and thorium-230. Chem. Geol. 169, 17-33.</p>
<p>Hayes, C.T., Anderson, R.F., Jaccard, S.L., Fleisher, M.Q., Soon, M., Gersonde, R., submitted. The nature of boundary scavenging in the North Pacific Ocean. Earth Planet. Sci. Lett.</p>
<p>Jaffey, A.H., Flynn, K.F., Glendenin, L.E., Bentley, W.C., Essling, A.M., 1971. Precision Measurement of Half-Lives and Specific Activities of 235U and 238U. Physical Review C 4, 1889-1906.</p>
<p>Robert, J., Miranda, C.F., Muxart, R., 1969. Mesure de la periode du protactinium-231 par microcalorimetrie. Radiochim. Acta 11, 104-108.</p></div>
3856
Dissolved Th/Pa - SO-202
2013-01-16T09:58:56-05:00
2013-01-16T09:58:56-05:00
2023-07-07T16:10:26-04:00
urn:bcodmo:dataset:3856
Depth profiles of seawater dissolved 232Th, 230Th, and 231Pa, NW Pacific from R/V Sonne SO202 in the North Pacific and the Bering Sea from July 2009 (Sources-Sinks Th-Pa project)
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Anderson, R. F., Fleisher, M. Q. (2013) Depth profiles of seawater dissolved 232Th, 230Th, and 231Pa, NW Pacific from R/V Sonne SO202 in the North Pacific and the Bering Sea from July 2009 (Sources-Sinks Th-Pa project). Biological and Chemical Oceanography Data Management Office (BCO-DMO). Version Date 2013-01-16 [if applicable, indicate subset used]. http://lod.bco-dmo.org/id/dataset/3856 [access date]
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2013-01-16
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