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Sampling Methods at Sea:<\/strong> Analytical Methods at LDEO:<\/strong> Concentrations of Th-232, Th-230 and Pa-231 were calculated by isotope dilution, relative to the calibrated tracers Th-229 and Pa-233 added at the beginning of sample processing. Analyses were carried out on a Thermo-Finnigan ELEMENT XR Single Collector Magnetic Sector ICP-MS, equipped with a high-performance Interface pump (Jet Pump Aridus I\u2122), and specially designed sample (Jet) and skimmer (X) cones to ensure the highest possible sensitivity. All measurements were made in low resolution mode (\u2206m\/M\u2248300), peak jumping in Escan mode across the central 5% of the flat-topped peaks. Measurements were made on a MasCom\u2122 SEM; Th-229, Th-230, Pa-231, and Pa-233 were measured in Counting mode, while the Th-232 signals were large enough that they were measured in Analog mode. Two solutions of SRM129, a natural U standard, were run multiple times throughout each run. One solution was in a concentration range where U-238 and U-235 were both measured in Counting mode, allowing us to determine the mass bias\/amu (typical values varied from -0.5%\/amu to 0.2%\/amu). In the other, more concentrated solution, U-238 was measured in Analog mode and U-235 was measured in Counting mode, yielding a measurement of the Analog\/Counting Correction Factor (typical values varied from 0.9 to 1.1). These corrections assume that the mass bias and Analog\/Counting Correction Factor measured on U isotopes can be applied to Th and Pa isotope measurements. Each sample measurement was bracketed by measurement of an aliquot of the run solution (0.16 M HNO3\/0.026 M HF), which was used to correct for the instrumental background count rates. To correct for tailing of Th-232 into the minor Th and Pa isotopes, a series of Th-232 standards were run at concentrations bracketing the expected Th-232 concentrations in the samples. The analysis routine for these standards was identical to the analysis routine for samples, so we could see the changing beam intensities at the minor masses as we increased the concentration of the Th-232 standards. The Th-232 count rates in our Pa fractions were quite low after separation of Pa from Th during anion-exchange chromatography, reflecting mainly reagent blanks, compared to the Th-232 signal intensity in the Th fraction. The regressions of Th-229, Th-230, Pa-231, and Pa-233 signals as a function of the Th-232 signal in the standards was used to correct for tailing of Th-232 in samples. Only in rare cases was a tail correction of Th-232 on Pa-231 and Pa-233 necessary, while it was always the case that tail corrections of Th-232 on Th-229 and Th-230 were performed.<\/p>\n Water samples were analyzed in batches of 15. Procedural blanks were determined by processing 4-5 L of Milli-Q H2O in an acid-cleaned cubitainer acidified to pH ~2 with 6 M HCl (Fisher Scientific OPTIMA grade) as a sample in each batch. Two procedural blanks were processed with each batch, with about half of the procedural blanks acidified at sea during HLY1502 and the other half acidified in the on-shore laboratory before sample processing. The difference in the procedural blank values for Th-232, Th-230, and Pa-231 between acidifying procedural blanks at sea or in the on-shore laboratory was statistically insignificant. An aliquot of two intercalibrated working standard solutions of Th-232, Th-230, and Pa-231, SW STD 2010-1 referred to by Anderson et al. (2012) and SW STD 2015-1 which has ~6 times lower Th-232 activity, were added to separate acid-cleaned Teflon beakers along with weighed aliquots of Th-229 and Pa-233 spike. Spikes and SW STD were equilibrated for at least 1 day. They were then dried down and dissolved in concentrated (12 M) HCl (Fisher Scientific OPTIMA grade) for a series of anion-exchange chromatography and processed like samples with each batch. Samples were corrected using the pooled average of all procedural blanks analyzed during processing of HLY1502 dissolved samples. The average procedural blanks for Th-232, Th-230, and Pa-231 were 5.72 \u00b1 3.22 pg, 0.14 \u00b1 0.08 fg, and 0.07 \u00b1 0.08 fg, respectively. The limit of detection (LOD) is the smallest quantity of each isotope in samples that can reliably be detected or that can be statistically distinguished from a procedural blank. The LOD was considered to be 2 standard deviations above the average of the procedural blanks. Our LOD for Th-232, Th-230, and Pa-231 were 12.15 pg, 0.29 fg, and 0.23 fg, respectively, or about 2.1x, 2.1x, and 3.1x greater than the blank amount, respectively.<\/p>\n Further details on analysis of seawater dissolved radionuclides are given by Anderson et al. (2012).<\/p>\n Analytical Methods at UMN:<\/strong> Concentrations of Th-232, Th-230, and Pa-231 were calculated by isotope dilution using nuclide ratios determined on a Thermo-Finnigan Neptune Multicollector ICP-MS. All measurements were done using a peak jumping routine in ion Counting mode on the discreet dynode multiplier behind the retarding potential quadrupole. A solution of U-233-U-236 tracer 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 (weak nitric acid), which was used to correct for the instrument background count rates on the masses measured.<\/p>\n Water samples were analyzed in batches of 28-56. Procedural blanks were determined by performing a complete chemical procedure on 1 L of Milli-Q water with each batch of samples. An aliquot of one of two intercalibrated working standard solutions of Th-232, Th-230, and Pa-231, SW STD 2010-1 referred to by Anderson et al. (2012) and SW STD 2015-1 which has ~6 times lower Th-232 activity, was added to a separate acid-cleaned Teflon beaker along with weighed aliquots of Th-229 and Pa-233 spike. Spikes and SW STD were equilibrated for 3 days. They were then dried down and taken up in 7 M HNO3 for anion-exchange chromatography and processed like a sample with each batch. HLY1502 dissolved samples were corrected using the procedural blank analyzed during the same sample batch. The average procedural blanks for Th-232, Th-230, and Pa-231 were 0.83 \u00b1 0.80 pg, 0.03 \u00b1 0.03 fg, and 0.02 \u00b1 0.03 fg, respectively. The limit of detection (LOD) is the smallest quantity of each isotope in samples that can reliably be detected or that can be statistically distinguished from a procedural blank. The LOD was considered to be 2 standard deviations above the average of the procedural blanks. Our LOD for Th-232, Th-230, and Pa-231 were 2.44 pg, 0.09 fg, and 0.08 fg, respectively, or about 2.9x, 2.5x, and 3.1x greater than the blank amount, respectively.<\/p>\n Further details on Pa and Th analysis at University of Minnesota are given in Shen et al. (2002, 2003, 2012), and Cheng et al. (2000, 2013).<\/p>\n Notes on Derived Parameters:<\/strong> Th_230_D_XS_CONC_BOTTLE = Th_230_D_CONC_BOTTLE \u2013 4.0e-6 * 1.7473e5 * Th_232_D_CONC_BOTTLE<\/p>\n Pa_231_D_XS_CONC_BOTTLE: <\/strong> Pa_231_D_XS_CONC_BOTTLE = Pa_231_D_CONC_BOTTLE \u2013 8.8e-8 * 4.0370e5 * Th_232_D_CONC_BOTTLE<\/p>\n Th_230_D_XS_CONC_BOAT_PUMP:<\/strong> Th_230_D_XS_CONC_BOAT_PUMP = Th_230_D_CONC_BOAT_PUMP \u2013 4.0e-6 * 1.7473e5 * Th_232_D_CONC_BOAT_PUMP<\/p>\n Pa_231_D_XS_CONC_BOAT_PUMP:<\/strong> Pa_231_D_XS_CONC_BOAT_PUMP = Pa_231_D_CONC_BOAT_PUMP \u2013 8.8e-8 * 4.0370e5 * Th_232_D_CONC_BOAT_PUMP<\/p>\n Th_230_D_XS_CONC_SUBICE_PUMP:<\/strong> Th_230_D_XS_CONC_SUBICE_PUMP = Th_230_D_CONC_SUBICE_PUMP \u2013 4.0e-6 * 1.7473e5 * Th_232_D_CONC_SUBICE_PUMP<\/p>\n Pa_231_D_XS_CONC_SUBICE_PUMP<\/strong>: Pa_231_D_XS_CONC_SUBICE_PUMP = Pa_231_D_CONC_SUBICE_PUMP \u2013 8.8e-8 * 4.0370e5 * Th_232_D_CONC_SUBICE_PUMP<\/p>\n Th_230_ICE_D_XS_CONC_CORER:<\/strong> Th_230_ICE_D_XS_CONC_CORER = Th_230_ICE_D_CONC_CORER \u2013 4.0e-6 * 1.7473e5 * Th_232_ICE_D_CONC_CORER<\/p>\n Pa_231_ICE_D_XS_CONC_CORER:<\/strong> Pa_231_ICE_D_XS_CONC_CORER = Pa_231_ICE_D_CONC_CORER \u2013 8.8e-8 * 4.0370e5 * Th_232_ICE_D_CONC_CORER<\/p>\n Th_230_D_XS_CONC_MELTPOND_PUMP:<\/strong> Th_230_D_XS_CONC_MELTPOND_PUMP = Th_230_D_CONC_MELTPOND_PUMP \u2013 4.0e-6 * 1.7473e5 * Th_232_D_CONC_MELTPOND_PUMP<\/p>\n Pa_231_D_XS_CONC_MELTPOND_PUMP:<\/strong> Pa_231_D_XS_CONC_MELTPOND_PUMP = Pa_231_D_CONC_MELTPOND_PUMP \u2013 8.8e-8 * 4.0370e5 * Th_232_D_CONC_MELTPOND_PUMP<\/p><\/div>","@type":"rdf:HTML"}],"http:\/\/ocean-data.org\/schema\/hasBriefDescription":[{"@value":"GN01 Dissolved Thorium and Protactinium","@language":"en-US"}],"http:\/\/purl.org\/dc\/terms\/description":[{"@value":" This dataset contains concentrations of dissolved thorium and protactinium isotopes (Th-232, Th-230, Pa-231) in seawater, sea ice, and melt ponds collected during the U.S. GEOTRACES Arctic cruise (HLY1502, GN01) on USCGC Healy from August to October 2015. This is compiled data produced by two laboratories with the following associations: Lamont-Doherty Earth Observatory of Columbia University (LDEO) and the University of Minnesota (UMN). All data have been deemed intercalibrated by the International GEOTRACES Standards and Intercalibration (S&I) Committee.<\/p>\n Naming Conventions:<\/strong> A GEOTRACES sample number (Sample_ID) appended with an \"A\" denotes the archive sample collected during the same cast and at the same depth as the sample that was originally analyzed.<\/p>\n \"Dissolved\" (D) here refers to that which passed through stacked 0.8\/0.45 \u00b5m Acropak\u2122 500 filter capsules sampled from conventional Niskin bottles on a CTD rosette (BOTTLE; NIS and GSNIS). This is true for all dissolved samples except for a select number that were collected using GO-FLO bottles on a CTD rosette (BOTTLE; GF), a pump from a small boat (BOAT_PUMP; SMBT), a pump through sea ice into seawater (SUBICE_PUMP), a trace metal clean ice corer (CORER), and a pump into a melt pond (MELTPOND_PUMP). Sampling system is indicated by the parameter name, and in some cases by Bottle_ID. For Bottle_ID, NIS represents Niskin bottles sampled from the 12-place 30 liter ODF rosette, GSNIS represents Niskin bottles sampled from the 36-place 10 liter GO-SHIP rosette, GF represents GO-FLO bottles sampled from the 24-place 12 liter GTC clean carousel, and SMBT represents surface (1 m) seawater samples collected from a small boat upstream of the ship using a battery-powered pump and Teflon-lined PVC tubing. SUBICE_PUMP represents seawater samples collected from under the ice (at approximately 1, 5, and 20 m) with the same pumping system used for BOAT_PUMP, MELTPOND_PUMP represents melt pond water samples that were collected using a battery-powered peristaltic pump and silicone tubing, and CORER represents sea ice samples that were collected using a trace metal clean ice corer. Bulk sea ice (CORER) samples were collected as ice cores about 1 m in length and melted overnight in LDPE melting chambers before they were subsampled into 5 liter cubitainers. BOAT_PUMP, SUBICE_PUMP, and MELTPOND_PUMP samples were each stored in 25 liter carboys during sample collection and then subsampled into 5 liter cubitainers aboard the ship. GF (BOTTLE), BOAT_PUMP, MELTPOND_PUMP, and CORER samples were passed through a 0.2 \u00b5m Acropak\u2122 200 filter capsule, unlike NIS (BOTTLE), GSNIS (BOTTLE), and SUBICE_PUMP samples, which were passed through stacked 0.8\/0.45 \u00b5m Acropak\u2122 500 filter capsules. All seawater, sea ice, and melt pond samples were weighed directly in the on-shore laboratory to determine sample size, taking into account acid added at sea.<\/p>\n Units of Measurement:<\/strong> Results Publications:<\/strong> Data Processing:<\/strong> Analysis of all samples was completed over the course of several years. A correction was made to account for the ingrowth of Th-230 and Pa-231 due to the decay of the natural U-234 and U-235 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 Th-230 and Pa-231 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 in seawater (Owens et al., 2011), [U] = (0.100 * S \u2013 0.326) ng U (g seawater)-1. We used seawater U-isotopic compositions of U-234\/U-238 = 1.1468 activity ratio (Andersen et al., 2010), and U-238\/U-235 = 137.824 mole ratio (Weyer et al., 2008), to calculate [U-234] and [U-235] respectively based on [U].<\/p>\n Individual uncertainties for protactinium and thorium were calculated to include contributions from (a) blank correction using the variance of the blanks measured over the course of the analyses, (b) standard error of the ratios of the analysis (typically close to counting statistics) and (c) spike calibration. For protactinium we also included assessment of the correction from the yield correction, mass bias and instrument background. In order to assess the reproducibility of the procedure, repeat analyses were performed on the GEOTRACES 2010-1 and 2015-1 standards. For standards run alongside GN01 dissolved samples at LDEO, the reproducibility for each isotope was 0.87% for Th-232, 0.86% for Th-230, and 1.63% for Pa-231 on SW STD 2010-1, and was 4.78% for Th-232, 0.71% for Th-230, and 3.24% for Pa-231 on SW STD 2015-1. At UMN, the reproducibility for each isotope was 1.09% for Th-232, 0.86% for Th-230, and 1.44% for Pa-231 on SW STD 2010-1, and was 0.34% for Th-232, 0.35% for Th-230, and 1.17% for Pa-231 on SW STD 2015-1.<\/p>\n Quality Flags:<\/strong> 0 = no quality control; The SeaDataNet quality flags assigned to the derived parameters are based on the SeaDataNet quality flags assigned to the measured parameters and are defined as:<\/p>\n 1 = good value = both Th-230 (Pa-231) and Th-232 are flagged as good (1);<\/p>\n 2 = probably good value = either Th-230 (Pa-231) is flagged as good (1) and Th-232 is flagged as probably good (2), probably bad (3), or bad (4), or Th-230 (Pa-231) is flagged as probably good (2) and Th-232 is flagged as good (1), probably good (2), probably bad (3), or bad (4);<\/p>\n 3 = probably bad value = Th-230 (Pa-231) is flagged as probably bad (3) and Th-232 is flagged as good (1), probably good (2), probably bad (3), or bad (4);<\/p>\n 4 = bad value = Th-230 (Pa-231) is flagged as bad (4) and Th-232 is flagged as good (1), probably good (2), probably bad (3), or bad (4);<\/p>\n 6 = value below detection = either or both Th-230 (Pa-231) and Th-232 are flagged as below detection (6) and neither are flagged as missing (9);<\/p>\n 9 = missing value = either or both Th-230 (Pa-231) and Th-232 are flagged as missing (9).<\/p>\n Concentrations below the limit of detection (LOD) are indicated as \"nd\" and flagged with \"6\". The missing data identifier, \"nd\", also refers to no data available when flagged with \"9\" (i.e., no analysis).<\/p>\n BCO-DMO Processing:<\/strong> Version History:<\/strong> Start_ISO_DateTime_UTC<\/strong> for: End_Date_UTC<\/strong> for: End_Time_UTC&<\/strong> for: End_ISO_DateTime_UTC<\/strong> for: Start_Latitude<\/strong> for: Start_Longitude<\/strong> for: Cast_ID<\/strong> for: Sample_Depth<\/strong> for:
\nSampling methods at sea followed the GEOTRACES cookbook (Cutter et al., 2017). Water samples were collected with a Sea-Bird Electronics CTD carousel fitted with either 12 30-liter or 36 10-liter PVC Niskin bottles, managed and operated by Ship-based Science Technical Support in the Arctic and the Ocean Data Facility of Scripps Institution of Oceanography, or with a Sea-Bird Electronics CTD carousel fitted with 24 12-liter GO-FLO bottles (the GEOTRACES Clean carousel). The 12-place 30 L Niskin bottle rosette was used for stations 1-10 and 26, the 36-place 10 L Niskin bottle rosette was used for stations 12-19, 30-38, and 43-66, and the 24-place 12 L GO-FLO bottle rosette was used for station 41. Carousels were lowered from the ship with steel wire. Niskin bottles were equipped with nylon-coated closure springs and Viton O-rings. After collection, seawater was drained with Teflon-lined Tygon\u2122 tubing and filtered through Pall Acropak\u2122 500 filters on deck (gravity filtration, 0.8\/0.45 \u03bcm pore size) into Fisher I-Chem series 300 LDPE cubitainers. Ice hole seawater samples were collected from under the ice (at approximately 1, 5, and 20 m) using a battery-powered pump and Teflon-lined PVC tubing, then filtered and stored in the same manner as seawater samples collected from a rosette using a Niskin bottle. Surface (1 m) seawater samples were also collected from a small boat upstream of the ship using the same pumping system used to collect ice hole seawater samples, except they were passed through a 0.2 \u00b5m Acropak\u2122 200 filter capsule before being transferred to cubitainers. Melt pond samples were collected using a battery-powered peristaltic pump and silicone tubing, bulk sea ice samples were collected using a trace metal clean ice corer and melted overnight in LDPE melting chambers, and both were also passed through a 0.2 \u00b5m Acropak\u2122 200 filter capsule before cubitainer storage. Approximately 4-5 liters were collected per desired depth for each dissolved sample. Prior to the cruise, the tubing, filters, and cubitainers were cleaned by immersion in dilute (1.2 M) HCl (Fisher Scientific Trace Metal Grade) for 4-5 days. Once filtered, samples were adjusted to a pH of ~2 with ultra-clean 6 M HCl (Fisher Scientific OPTIMA grade), double-bagged, stored in pallet boxes on-deck until the end of the cruise, and then at room temperature once shipped to the participating laboratories for analysis.<\/p>\n
\nIn the on-shore laboratory, seawater, sea ice, and melt pond samples were weighed to determine sample size, taking into account the weight of the cubitainer and of the acid added at sea. Then, weighed aliquots of the artificial isotope yield monitors Th-229 (1 pg) and Pa-233 (0.05-0.17 pg) and 25 mg dissolved Fe were added to each sample. After allowing 1 day for spike equilibration, the pH of each sample was raised to 8.3-8.7 by adding ~12 mL of concentrated NH4OH (Fisher Scientific OPTIMA grade) which caused iron (oxy)hydroxide precipitates to form. Each sample cubitainer was fitted with a nozzle cap, inverted, and the Fe precipitate was allowed to settle for 2 days. After 2 days, the nozzle caps were opened and the pH~8.3-8.7 water was slowly drained, leaving only the iron oxyhydroxide precipitate and 250-500 mL of water. The Fe precipitate was transferred to centrifuge tubes for centrifugation and rinsing with Milli-Q H2O (>18 M\u03a9) to remove the major seawater ions. The precipitate was then dissolved in concentrated (16 M) HNO3 (Fisher Scientific OPTIMA grade) and transferred to a Teflon beaker for a high-temperature (180-200\u00b0C) digestion with concentrated 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 Milli-Q H2O, centrifuged, and dissolved in concentrated (16 M) HNO3 (Fisher Scientific OPTIMA grade) 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 \u03bcm porous polyethylene frit (Anderson et al., 2012). The final column elutions were dried down at 180-200\u00b0C in the presence of 2 drops of concentrated HClO4 (Fisher Scientific OPTIMA grade) and taken up in 0.5 mL of 0.16 M HNO3\/0.026 M HF (Fisher Scientific OPTIMA grade) for mass spectrometric analysis.<\/p>\n
\nIn the on-shore laboratory, 1-liter aliquots of the seawater, sea ice, and melt pond samples were weighed to determine sample size, taking into account the weight of the subsample container and of the acid added at sea. Then, weighed aliquots of the artificial isotope yield monitors Th-229 (1 pg) and Pa-233 (0.2-0.6 pg) and 3 mg dissolved Fe were added to each sample. After allowing 3 days for spike equilibration (at a temperature of about 40\u00b0C), the pH of each sample was raised to 8.0-8.5 by adding concentrated NH4OH 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 deionized H2O (>18 M\u03a9) to remove the major seawater ions. The precipitate was then dissolved in 14 M HNO3 and transferred to a Teflon beaker. It was then dried down and taken up in 7 M HNO3 for anion-exchange chromatography using Bio-rad resin (AG1-X8, 100-200 mesh size) and a polyethylene frit. Initial separation was done on Teflon columns with a 0.75 mL column volume (CV). The sample was loaded in 0.75 mL (1 CV) of 7 M HNO3, followed by 1.125 mL (1.5 CV) of 7 M HNO3 (to wash Fe and other undesired elements off the resin), 2.25 mL (3 CV) of 8 M HCl (to collect Th fraction), and 2.25 mL (3 CV) of 8 M HCl\/0.015 M HF (to collect Pa fraction). The Pa and Th fractions were then dried down in the presence of 2 drops of concentrated HClO4 and taken up in 7 M HNO3. They were each passed through second and third columns (each with 0.5 mL column volumes) using similar elution schemes. The final Pa and Th fractions were then dried down in the presence of 2 drops of concentrated HClO4 and dissolved in weak nitric acid for analysis on the mass spectrometer.<\/p>\n
Th_230_D_XS_CONC_BOTTLE: <\/strong>
\nThe dissolved excess Th-230 concentration refers to the measured dissolved Th-230 corrected for a contribution of Th-230 due to the partial dissolution of uranium-bearing minerals, or lithogenics. Thereby the dissolved excess represents solely the fraction of Th-230 produced in the water by decay of dissolved uranium-234. We estimate the lithogenic Th-230 using measured dissolved Th-232 and a lithogenic Th-230\/Th-232 ratio of 4.0e-6 (atom ratio) as determined by Roy-Barman et al. (2002) and a conversion factor to convert picomoles to micro-Becquerels.<\/p>\n
\nThe dissolved excess Pa-231 concentration refers to the measured dissolved Pa-231 corrected for a contribution of Pa-231 due to the partial dissolution of uranium-bearing minerals, or lithogenics. Thereby the dissolved excess represents solely the fraction of Pa-231 produced in the water by decay of dissolved uranium-235. We estimate the lithogenic Pa-231 using measured dissolved Th-232 and a lithogenic Pa-231\/Th-232 ratio of 8.8e-8 (atom ratio) which is derived from assuming an average upper continental crustal U\/Th ratio (Taylor and McClennan, 1995) and secular equilibrium between Pa-231 and U-235 in the lithogenic material. An additional conversion factor is needed to convert picomoles to micro-Becquerels.<\/p>\n
\nThe dissolved excess Th-230 concentration refers to the measured dissolved Th-230 corrected for a contribution of Th-230 due to the partial dissolution of uranium-bearing minerals, or lithogenics. Thereby the dissolved excess represents solely the fraction of Th-230 produced in the water by decay of dissolved uranium-234. We estimate the lithogenic Th-230 using measured dissolved Th-232 and a lithogenic Th-230\/Th-232 ratio of 4.0e-6 (atom ratio) as determined by Roy-Barman et al. (2002) and a conversion factor to convert picomoles to micro-Becquerels.<\/p>\n
\nThe dissolved excess Pa-231 concentration refers to the measured dissolved Pa-231 corrected for a contribution of Pa-231 due to the partial dissolution of uranium-bearing minerals, or lithogenics. Thereby the dissolved excess represents solely the fraction of Pa-231 produced in the water by decay of dissolved uranium-235. We estimate the lithogenic Pa-231 using measured dissolved Th-232 and a lithogenic Pa-231\/Th-232 ratio of 8.8e-8 (atom ratio) which is derived from assuming an average upper continental crustal U\/Th ratio (Taylor and McClennan, 1995) and secular equilibrium between Pa-231 and U-235 in the lithogenic material. An additional conversion factor is needed to convert picomoles to micro-Becquerels.<\/p>\n
\nThe dissolved excess Th-230 concentration refers to the measured dissolved Th-230 corrected for a contribution of Th-230 due to the partial dissolution of uranium-bearing minerals, or lithogenics. Thereby the dissolved excess represents solely the fraction of Th-230 produced in the water by decay of dissolved uranium-234. We estimate the lithogenic Th-230 using measured dissolved Th-232 and a lithogenic Th-230\/Th-232 ratio of 4.0e-6 (atom ratio) as determined by Roy-Barman et al. (2002) and a conversion factor to convert picomoles to micro-Becquerels.<\/p>\n
\nThe dissolved excess Pa-231 concentration refers to the measured dissolved Pa-231 corrected for a contribution of Pa-231 due to the partial dissolution of uranium-bearing minerals, or lithogenics. Thereby the dissolved excess represents solely the fraction of Pa-231 produced in the water by decay of dissolved uranium-235. We estimate the lithogenic Pa-231 using measured dissolved Th-232 and a lithogenic Pa-231\/Th-232 ratio of 8.8e-8 (atom ratio) which is derived from assuming an average upper continental crustal U\/Th ratio (Taylor and McClennan, 1995) and secular equilibrium between Pa-231 and U-235 in the lithogenic material. An additional conversion factor is needed to convert picomoles to micro-Becquerels.<\/p>\n
\nThe dissolved excess Th-230 concentration refers to the measured dissolved Th-230 corrected for a contribution of Th-230 due to the partial dissolution of uranium-bearing minerals, or lithogenics. Thereby the dissolved excess represents solely the fraction of Th-230 produced in the water by decay of dissolved uranium-234. We estimate the lithogenic Th-230 using measured dissolved Th-232 and a lithogenic Th-230\/Th-232 ratio of 4.0e-6 (atom ratio) as determined by Roy-Barman et al. (2002) and a conversion factor to convert picomoles to micro-Becquerels.<\/p>\n
\nThe dissolved excess Pa-231 concentration refers to the measured dissolved Pa-231 corrected for a contribution of Pa-231 due to the partial dissolution of uranium-bearing minerals, or lithogenics. Thereby the dissolved excess represents solely the fraction of Pa-231 produced in the water by decay of dissolved uranium-235. We estimate the lithogenic Pa-231 using measured dissolved Th-232 and a lithogenic Pa-231\/Th-232 ratio of 8.8e-8 (atom ratio) which is derived from assuming an average upper continental crustal U\/Th ratio (Taylor and McClennan, 1995) and secular equilibrium between Pa-231 and U-235 in the lithogenic material. An additional conversion factor is needed to convert picomoles to micro-Becquerels.<\/p>\n
\nThe dissolved excess Th-230 concentration refers to the measured dissolved Th-230 corrected for a contribution of Th-230 due to the partial dissolution of uranium-bearing minerals, or lithogenics. Thereby the dissolved excess represents solely the fraction of Th-230 produced in the water by decay of dissolved uranium-234. We estimate the lithogenic Th-230 using measured dissolved Th-232 and a lithogenic Th-230\/Th-232 ratio of 4.0e-6 (atom ratio) as determined by Roy-Barman et al. (2002) and a conversion factor to convert picomoles to micro-Becquerels.<\/p>\n
\nThe dissolved excess Pa-231 concentration refers to the measured dissolved Pa-231 corrected for a contribution of Pa-231 due to the partial dissolution of uranium-bearing minerals, or lithogenics. Thereby the dissolved excess represents solely the fraction of Pa-231 produced in the water by decay of dissolved uranium-235. We estimate the lithogenic Pa-231 using measured dissolved Th-232 and a lithogenic Pa-231\/Th-232 ratio of 8.8e-8 (atom ratio) which is derived from assuming an average upper continental crustal U\/Th ratio (Taylor and McClennan, 1995) and secular equilibrium between Pa-231 and U-235 in the lithogenic material. An additional conversion factor is needed to convert picomoles to micro-Becquerels.<\/p>\n
\nParameter names in the form such as \"Th_232_D_CONC_BOTTLE\" are adopted based on a recommendation from the GEOTRACES community (https:\/\/www.geotraces.org\/parameter-naming-conventions\/<\/a>).<\/p>\n
\nRadionuclide concentrations are given as micro-Becquerel (10e-6 Bq, \u00b5Bq or micro-Bq) per kilogram water for Th-230 and Pa-231, and picomole (10e-12 mol, pmol) per kilogram water for Th-232. A Becquerel is the SI unit for radioactivity and is defined as 1 disintegration per second. These units are recommended by the GEOTRACES community.<\/p>\n
\nThese data have been published in the following:
\nCharette et al., 2020 \u2013 Dissolved Th-232 concentrations in upper ocean waters (Th_232_D_CONC_BOTTLE_dan73c)<\/p><\/div>","@type":"rdf:HTML"}],"http:\/\/www.w3.org\/2000\/01\/rdf-schema#label":[{"@value":"GN01 Dissolved Thorium and Protactinium","@type":"xsd:string"}],"http:\/\/ocean-data.org\/schema\/hasProcessingDescription":[{"@value":"
\nThe reported errors for radionuclide concentrations represent the propagation of one sigma errors based on the standard isotope ratios collected by ICP-MS, estimated error in the Th-229 or Pa-233 spike concentration, and the blank correction of the individual isotopes. For LDEO, samples were corrected for blanks using the pooled average of all procedural blanks analyzed during processing of HLY1502 dissolved samples, while for UMN, samples were corrected for blanks using the procedural blank analyzed during the same sample batch.<\/p>\n
\nSeaDataNet quality flags have been assigned to all measured and derived parameters. More information on SeaDataNet quality flags is available from GEOTRACES at https:\/\/www.geotraces.org\/geotraces-quality-flag-policy\/<\/a> and from SeaDataNet at https:\/\/www.seadatanet.org\/Standards\/Data-Quality-Control<\/a>. In summary:<\/p>\n
\n1 = good value;
\n2 = probably good value;
\n3 = probably bad value;
\n4 = bad value;
\n5 = changed value;
\n6 = value below detection;
\n7 = value in excess;
\n8 = interpolated value;
\n9 = missing value;
\nA = value phenomenon uncertain.<\/p>\n
\n- modified parameter names to conform with BCO-DMO naming conventions (replaced \"::\" with an underscore and changed \"1SD\" to \"SD1\").<\/p>\n
\n-2020-12-29: version 1 published.
\n- 2021-02-23: replaced with data file received 2021-01-28 (version 2); includes changes to some data values.
\n- 2021-08-25: replaced with data file receive 2021-08-01 (version 3); includes the following changes:
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This is compiled data produced by two laboratories with the following associations: Lamont-Doherty Earth Observatory of Columbia University (LDEO) and the University of Minnesota (UMN). All data have been deemed intercalibrated by the International GEOTRACES Standards and Intercalibration (S&I) Committee.","@language":"en-US"}],"http:\/\/purl.org\/dc\/terms\/rights":[{"@id":"https:\/\/creativecommons.org\/licenses\/by\/4.0\/"}],"http:\/\/ocean-data.org\/schema\/deprecated":[{"@value":"false","@type":"xsd:boolean"}],"http:\/\/ocean-data.org\/schema\/temporalExtent":[{"@value":"_:temporalExtent833887"}],"http:\/\/ocean-data.org\/schema\/spatialCoverage":[{"@value":"_:spatialCoverage833887"}],"http:\/\/purl.org\/dc\/terms\/bibliographicCitation":[{"@value":"Vivancos, S. M., Anderson, R. F., Fleisher, M. Q., Zhang, P., Li, X., Edwards, R. L., Cheng, H. 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