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seawater and returned to the sediment column. In consideration of the above observations, river waters are the dominant source of the REY to modern seawater. It should be noted that aeolian dust also delivers REY to the oceans, but the magnitude of this flux to dissolved REY in seawater is debated (e.g., Nakai et al., 1993; Tachikawa et al., 1999; Greaves et al., 1999; Bayon et al., 2004), and regardless, the REY distribution in the aeolian flux will generally reflect continental REY sources. It should be noted that the Pacific Ocean seems atypical in this regard, as volcanic particles derived from intraplate and circum-Pacific volcanism appear to be a significant REY source, and the reader is referred to Goldstein and Hemming (2003) for a more thorough discussion. Within seawater itself, the REY display consistent behavior. Figure 6 shows rare earth element abundances and distributions from the Atlantic, Pacific, and Indian oceans. All of the major world oceans have been sampled, with exceptions being the Southern Ocean (south of 60° latitude) and the central Arctic Ocean. The available rare earth element dataset for seawater is extensive, and approximately 900 samples worldwide have been analyzed, with the Pacific Ocean providing the most samples (47%), followed by the Indian (29%), Atlantic (15%), Arctic (8%), and Mediterranean (
sample/PAAS 10 -6 10 -7 deep water >2000 m NW Pacific NE Indian SW Pacific S Atlantic 10 -8 shallow water 2000 m) possesses an indistinguishable rare earth element pattern and very similar concentrations regardless of the ocean basin sampled. and concentrations observed in modern seawater are very similar regardless of location (Fig. 6). The consistent REY patterns in modern seawater regardless of location or depth reflect the interplay between solution complexation effects and particle surface adsorption processes. The REY are lithophilic and generally insoluble elements, and precipitation of REY mineral phases in equilibrium with seawater does not control REY concentrations or distributions, as all of the lanthanides are undersaturated in seawater (Brookins, 1989). Dissolved REE in seawater do not generally exist as hydrated free metal ions, but are predominantly complexed by carbonate anions (CO 2- 3 ) as illustrated in Figure 7 using the data of Cantrell and Byrne (1987). 13
Page 1: Iron sedimentation and the neodymiu
Page 4 and 5: The process(es) by which IFs were d
Page 7: This thesis represents original and
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Page 12 and 13: goal of the research is to discern
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Page 18 and 19: 100 10 MORB 1 0.1 raw data (mg/kg)
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Page 52 and 53: Abstract The benefits of inductivel
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10 2 JDo-1 reference values 10 1 IF
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Figure 5. Diagram depicting various
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20 18 basalt BHVO-2 (n=5) run preci
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The method precision for elements p
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Two approaches may be utilized to d
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For the more recent, full 32 elemen
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isotopic data for geologic CRMs, av
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Table 4. Interferences observed for
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value uncertainty (as %RSD) is repr
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1.50 FeR-4 (n=2) 1.25 JUB / referen
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1 IF-G/shale 0.1 0.01 La Ce Pr Nd P
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consistent (App. 1), and similar to
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1.50 SGR-1b (n=3) 1.25 JUB / refere
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1.50 JCh-1 (n=3) 1.25 JUB / referen
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1.50 JDo-1 (n=5) 1.25 JUB / referen
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determinations in carbonate rocks r
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1.50 JMn-1 (n=4) 1.25 JUB / referen
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eference value. The result is that
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eference value and the measured JUB
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the 32 analyzed elements, with Ti b
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Govindaraju K. (1995) 1995 working
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Appendix 1. Analytical data Appendi
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Appendix 1. Literature reference va
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Appendix 1 continued. Data in mg/kg
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the concentration of the major elem
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Potential interferences on monoisot
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1500 0.5 M HCl 4.0 interference on
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4000 0.40 0.20 3500 0.17 mg/kg 0.18
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interference on 95 Mo in sample sol
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Nd isotopes in 2.9 Ga Archean surfa
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Table 2 Trace element concentration
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Author's personal copy B.W. Alexand
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and preservation of oxide-facies IF
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TOP relative stratigraphic position
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The mechanism by which the alkali m
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6. Widdel, F. et al. Ferrous iron o
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82 PRESERVATION OF PRIMARY REE PATT
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ulk, open ocean seawater tended to
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