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10 -2 hydrothermal fluid 10 -3 10 -4 sample/PAAS 10 -5 10 -6 10 -7 10 -8 10 -9 river water marine pore water estuaries world seawater La Ce Pr Nd PmSm Eu Gd Tb Dy Y Ho Er Tm Yb Lu Figure 5. Average REE and REY distributions in natural waters. Seawater and hydrothermal fluid data are the same as in Fig. 4. River water is an average of 155 filtered (0.2-0.45 μm) samples with pH between 5-9, and represents complete REY datasets for rivers in Venezuela, Australia, USA, and Sardinia (Tosiani et al., 2004; Lawrence et al., 2006; Bau et al. 2006; Cidu and Biddau, 2007), as well as complete REE data for rivers in France and Argentina (Tricca et al., 1999; Gammons et al., 2005b; Stille et al., 2006). The marine pore water REE pattern is the average of 89 filtered (0.2-0.45 μm) samples compiled from isotope dilution REE data for the eastern and western margins of North America (Elderfield and Sholkovitz, 1987; German and Elderfield, 1989; Sholkovitz et al., 1989; Sholkovitz et al., 1992), as well as complete REE datasets for pore waters from the western margins of North and South America (Haley and Klinkhammer, 2003; Haley et al., 2004). Estuary water is an average of 134 filtered (0.2-0.45 μm) samples with salinities between 1-30 ‰ (mean= 13.8 ‰, median= 14.2 ‰) and represents instrument neutron activation analysis data for samples from France (Martin et al., 1976), as well as isotope dilution REE data from estuaries along the margins of North America (Sholkovitz and Elderfeld, 1988; Goldstein and Jacobsen, 1988; Elderfeld et al., 1990; Sholkovitz et al., 1992), Great Britain (Elderfeld et al., 1990), South America (Sholkovitz, 1993), and Papua New Guinea (Sholkovitz and Szymczak, 2000). Additionally, estuarine water average incorporates complete REY data for estuaries from Australia (Lawrence and Kamber, 2006) and Germany (Kulaksız and Bau, 2007). modern seawater. Therefore, some process or processes must exist that effectively remove REY from these source solutions upon mixing with ambient seawater. The distinctly lower REY concentrations found in estuaries relative to river water (Fig. 5) indicate that significant REY removal occurs during the mixing of freshwater and seawater. This phenomenon has been noted in previous experimental studies (Hoyle et al., 1984), as well studies of natural systems (e.g., Elderfield et al., 1990). The removal of REY in estuaries is due to the coagulation and ‘salting-out’ of the major REY-carrying phases present in river water, which are Fe-organic colloids smaller than 10
~0.2 μm (Sholkovitz, 1995). The result of this process is that more than ~70% of the 10 3 times more REY than ambient seawater, the metal-oxides that precipitate from them ultimately act as sinks for seawater REY (German et al., 1990; German et al., 1991a). Pore waters within marine sediments are less well studied than either river or estuarine waters, and REE data are available for only a handful of sites worldwide (see Fig. 5 caption for details). Pore waters within marine sediments display strong variations in both REE concentrations and normalized REE patterns as a function of depth below the seawater-sediment interface (Elderfield and Sholkovitz, 1987; Haley et al., 2004). Though data are few, it appears that increased REE concentrations in pore waters are related to redox cycling of Fe in the upper few centimeters of the sediment (Elderfield and Sholkovitz, 1987), as well the degradation of organic matter (Haley et al., 2004). It also appears that pore water fluxes may be a significant source of REE to seawater; however, the variability in REE patterns and higher concentrations found in pore waters are generally not observed in seawater sampled a few meters above the seawater-sediment interface (Elderfield and Sholkovitz, 1987; Haley et al., 2004), implying that REE sourced from pore waters may be rapidly scavenged from oxic 11
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
Page 10 and 11: viii
Page 12 and 13: goal of the research is to discern
Page 14 and 15: Figure 1. Map of southern Africa sh
Page 16 and 17: appropriate to briefly discuss: 1)
Page 18 and 19: 100 10 MORB 1 0.1 raw data (mg/kg)
Page 22 and 23: seawater and returned to the sedime
Page 24 and 25: 100 MCO + 3 + M(CO 3 )- 2 rare eart
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Page 30 and 31: sound geochemical basis for anomalo
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Page 34 and 35: available, it should be possible to
Page 36 and 37: modern and Archean oceans, as well
Page 38 and 39: Bau M., Möller P., and Dulski P. (
Page 40 and 41: Elderfield H. and Greaves M.J. (198
Page 42 and 43: Haley B.A., Klinkhammer G.P. (2003)
Page 44 and 45: Lee J.H. and Byrne R.H. (1993) Comp
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Page 48 and 49: Tosiani T., Loubet M., Viers J., Va
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Page 52 and 53: Abstract The benefits of inductivel
Page 54 and 55: List of Figures Figure 1. Sample de
Page 56 and 57: 1. Introduction The advent of induc
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Page 60 and 61: during decomposition (SiF 4 and CO
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0.90, corresponding to an anomalous
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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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