Show in contextThe latter transition may well have continued into the Phanerozoic Eon, eventually resulting in near-present O2 (Berner, 2006; Dahl et al., 2010; Sperling et al., 2015). View in article
Brand, U., Veizer, J. (1980) Chemical diagenesis of a multicomponent carbonate system; 1, Trace elements. Journal of Sedimentary Research 50, 1219-1236.Show in contextBoth Zn and Fe partition coefficients (Kd) from fluid to carbonates increase with increasing diagenesis as shown by earlier work of Brand and Veizer (1980). View in article
Canfield, D.E. (1998) A new model for Proterozoic ocean chemistry. Nature 396, 450-453.Show in contextThis value is substantially lower than traditional estimates based on palaeosol work (Canfield, 1998; Rye and Holland, 1998), but consistent with recent estimates based on an independent tracer, a kinetic model for Cr-Mn oxidation and Cr isotopes in ironstones (Planavsky et al., 2014). View in article
Canfield, D.E. (2005) The early history of atmospheric oxygen: Homage to Robert A. Garrels. Annual Review of Earth and Planetary Sciences 33, 1-36.Show in contextAtmospheric O2 was extremely low in the Archean Eon (>2.5 Ga), and while multiple lines of evidence suggest that Earth’s oxygenation was protracted (Kah et al., 2004; Kah and Bartley, 2011; Lyons et al., 2014; Planavsky et al., 2014), pO2 may have risen abruptly at two different points in time: first during the “Great Oxygenation Event” (GOE) at ~2.4 Ga (Canfield, 2005; Holland, 2006; Guo et al., 2009; Farquhar et al., 2011), when atmospheric O2 rose from <0.001 % to an intermediate value commonly estimated as 1 to 10 % of the current level (Farquhar et al., 2000; Pavlov and Kasting, 2002), and again during a “Neoproterozoic Oxygenation Event” (NOE) at ~800 to 542 million years ago (Canfield and Teske, 1996; Fike et al., 2006; Frei et al., 2009; Och and Shields-Zhou, 2012). View in article
Canfield, D.E., Teske, A. (1996) Late Proterozoic rise in atmospheric oxygen concentration inferred from phylogenetic and sulphur-isotope studies. Nature 382, 127-132.Show in contextAtmospheric O2 was extremely low in the Archean Eon (>2.5 Ga), and while multiple lines of evidence suggest that Earth’s oxygenation was protracted (Kah et al., 2004; Kah and Bartley, 2011; Lyons et al., 2014; Planavsky et al., 2014), pO2 may have risen abruptly at two different points in time: first during the “Great Oxygenation Event” (GOE) at ~2.4 Ga (Canfield, 2005; Holland, 2006; Guo et al., 2009; Farquhar et al., 2011), when atmospheric O2 rose from <0.001 % to an intermediate value commonly estimated as 1 to 10 % of the current level (Farquhar et al., 2000; Pavlov and Kasting, 2002), and again during a “Neoproterozoic Oxygenation Event” (NOE) at ~800 to 542 million years ago (Canfield and Teske, 1996; Fike et al., 2006; Frei et al., 2009; Och and Shields-Zhou, 2012). View in article
Catling, D.C., Claire, M.W. (2005) How Earth's atmosphere evolved to an oxic state: A status report. Earth and Planetary Science Letters 237, 1-20.Show in contextThis pO2 curve provides a more continuous coverage of atmospheric O2 levels compared to compilations derived from multiple geochemical tracers, such as mass-independent S isotopes and palaeosol records (Rye and Holland, 1998; Catling and Claire, 2005). View in article
Dahl, T.W., Hammarlund, E.U., Anbar, A.D., Bond, D.P.G., Gill, B.C., Gordon, G.W., Knoll, A.H., Nielsen, A.T., Schovsbo, N.H., Canfield, D.E. (2010) Devonian rise in atmospheric oxygen correlated to the radiations of terrestrial plants and large predatory fish. Proceedings of the National Academy of Sciences of the United States of America 107, 17911-17915.Show in contextThe latter transition may well have continued into the Phanerozoic Eon, eventually resulting in near-present O2 (Berner, 2006; Dahl et al., 2010; Sperling et al., 2015). View in article
DePaolo, D.J. (2011) Surface kinetic model for isotopic and trace element fractionation during precipitation of calcite from aqueous solutions. Geochimica et Cosmochimica Acta 75, 1039-1056.Show in contextIn addition, theoretical calculations suggest that kinetic effects on trace element partitioning in carbonate may contribute to Zn/Fe variability in samples from the same locality (Watson, 2004; DePaolo, 2011). View in article
Farquhar, J., Bao, H.M., Thiemens, M. (2000) Atmospheric influence of Earth's earliest sulfur cycle. Science 289, 756-758.Show in contextAtmospheric O2 was extremely low in the Archean Eon (>2.5 Ga), and while multiple lines of evidence suggest that Earth’s oxygenation was protracted (Kah et al., 2004; Kah and Bartley, 2011; Lyons et al., 2014; Planavsky et al., 2014), pO2 may have risen abruptly at two different points in time: first during the “Great Oxygenation Event” (GOE) at ~2.4 Ga (Canfield, 2005; Holland, 2006; Guo et al., 2009; Farquhar et al., 2011), when atmospheric O2 rose from <0.001 % to an intermediate value commonly estimated as 1 to 10 % of the current level (Farquhar et al., 2000; Pavlov and Kasting, 2002), and again during a “Neoproterozoic Oxygenation Event” (NOE) at ~800 to 542 million years ago (Canfield and Teske, 1996; Fike et al., 2006; Frei et al., 2009; Och and Shields-Zhou, 2012). View in article
Farquhar, J., Zerkle, A., Bekker, A. (2011) Geological constraints on the origin of oxygenic photosynthesis. Photosynthesis Research 107, 11-36.Show in contextAtmospheric O2 was extremely low in the Archean Eon (>2.5 Ga), and while multiple lines of evidence suggest that Earth’s oxygenation was protracted (Kah et al., 2004; Kah and Bartley, 2011; Lyons et al., 2014; Planavsky et al., 2014), pO2 may have risen abruptly at two different points in time: first during the “Great Oxygenation Event” (GOE) at ~2.4 Ga (Canfield, 2005; Holland, 2006; Guo et al., 2009; Farquhar et al., 2011), when atmospheric O2 rose from <0.001 % to an intermediate value commonly estimated as 1 to 10 % of the current level (Farquhar et al., 2000; Pavlov and Kasting, 2002), and again during a “Neoproterozoic Oxygenation Event” (NOE) at ~800 to 542 million years ago (Canfield and Teske, 1996; Fike et al., 2006; Frei et al., 2009; Och and Shields-Zhou, 2012). View in article
Fike, D.A., Grotzinger, J.P., Pratt, L.M., Summons, R.E. (2006) Oxidation of the Ediacaran Ocean. Nature 444, 744-747.Show in contextAtmospheric O2 was extremely low in the Archean Eon (>2.5 Ga), and while multiple lines of evidence suggest that Earth’s oxygenation was protracted (Kah et al., 2004; Kah and Bartley, 2011; Lyons et al., 2014; Planavsky et al., 2014), pO2 may have risen abruptly at two different points in time: first during the “Great Oxygenation Event” (GOE) at ~2.4 Ga (Canfield, 2005; Holland, 2006; Guo et al., 2009; Farquhar et al., 2011), when atmospheric O2 rose from <0.001 % to an intermediate value commonly estimated as 1 to 10 % of the current level (Farquhar et al., 2000; Pavlov and Kasting, 2002), and again during a “Neoproterozoic Oxygenation Event” (NOE) at ~800 to 542 million years ago (Canfield and Teske, 1996; Fike et al., 2006; Frei et al., 2009; Och and Shields-Zhou, 2012). View in article
Frei, R., Gaucher, C., Poulton, S.W., Canfield, D.E. (2009) Fluctuations in Precambrian atmospheric oxygenation recorded by chromium isotopes. Nature 461, 250-U125.Show in contextAtmospheric O2 was extremely low in the Archean Eon (>2.5 Ga), and while multiple lines of evidence suggest that Earth’s oxygenation was protracted (Kah et al., 2004; Kah and Bartley, 2011; Lyons et al., 2014; Planavsky et al., 2014), pO2 may have risen abruptly at two different points in time: first during the “Great Oxygenation Event” (GOE) at ~2.4 Ga (Canfield, 2005; Holland, 2006; Guo et al., 2009; Farquhar et al., 2011), when atmospheric O2 rose from <0.001 % to an intermediate value commonly estimated as 1 to 10 % of the current level (Farquhar et al., 2000; Pavlov and Kasting, 2002), and again during a “Neoproterozoic Oxygenation Event” (NOE) at ~800 to 542 million years ago (Canfield and Teske, 1996; Fike et al., 2006; Frei et al., 2009; Och and Shields-Zhou, 2012). View in article
Guo, Q.J., Strauss, H., Kaufman, A.J., Schroder, S., Gutzmer, J., Wing, B., Baker, M.A., Bekker, A., Jin, Q.S., Kim, S.T., Farquhar, J. (2009) Reconstructing Earth's surface oxidation across the Archean-Proterozoic transition. Geology 37, 399-402.Show in contextAtmospheric O2 was extremely low in the Archean Eon (>2.5 Ga), and while multiple lines of evidence suggest that Earth’s oxygenation was protracted (Kah et al., 2004; Kah and Bartley, 2011; Lyons et al., 2014; Planavsky et al., 2014), pO2 may have risen abruptly at two different points in time: first during the “Great Oxygenation Event” (GOE) at ~2.4 Ga (Canfield, 2005; Holland, 2006; Guo et al., 2009; Farquhar et al., 2011), when atmospheric O2 rose from <0.001 % to an intermediate value commonly estimated as 1 to 10 % of the current level (Farquhar et al., 2000; Pavlov and Kasting, 2002), and again during a “Neoproterozoic Oxygenation Event” (NOE) at ~800 to 542 million years ago (Canfield and Teske, 1996; Fike et al., 2006; Frei et al., 2009; Och and Shields-Zhou, 2012). View in article
Hardisty, D.S., Lu, Z., Planavsky, N.J., Bekker, A., Philippot, P., Zhou, X., Lyons, T.W. (2014) An iodine record of Paleoproterozoic surface ocean oxygenation. Geology doi: 10.1130/G35439.1.Show in contextHere we provide evidence for the hypothesis that carbonate-based redox proxies can provide an independent estimate of past pO2, expanding the palaeoredox record in time and space (Hardisty et al., 2014). View in article
Holland, H.D. (2006) The oxygenation of the atmosphere and oceans. Philosophical Transactions of the Royal Society B: Biological Sciences 361, 903-915.Show in contextAtmospheric O2 was extremely low in the Archean Eon (>2.5 Ga), and while multiple lines of evidence suggest that Earth’s oxygenation was protracted (Kah et al., 2004; Kah and Bartley, 2011; Lyons et al., 2014; Planavsky et al., 2014), pO2 may have risen abruptly at two different points in time: first during the “Great Oxygenation Event” (GOE) at ~2.4 Ga (Canfield, 2005; Holland, 2006; Guo et al., 2009; Farquhar et al., 2011), when atmospheric O2 rose from <0.001 % to an intermediate value commonly estimated as 1 to 10 % of the current level (Farquhar et al., 2000; Pavlov and Kasting, 2002), and again during a “Neoproterozoic Oxygenation Event” (NOE) at ~800 to 542 million years ago (Canfield and Teske, 1996; Fike et al., 2006; Frei et al., 2009; Och and Shields-Zhou, 2012). View in article
Kah, L.C., Bartley, J.K. (2011) Protracted oxygenation of the Proterozoic biosphere. International Geology Review 53, 1424-1442.Show in contextAtmospheric O2 was extremely low in the Archean Eon (>2.5 Ga), and while multiple lines of evidence suggest that Earth’s oxygenation was protracted (Kah et al., 2004; Kah and Bartley, 2011; Lyons et al., 2014; Planavsky et al., 2014), pO2 may have risen abruptly at two different points in time: first during the “Great Oxygenation Event” (GOE) at ~2.4 Ga (Canfield, 2005; Holland, 2006; Guo et al., 2009; Farquhar et al., 2011), when atmospheric O2 rose from <0.001 % to an intermediate value commonly estimated as 1 to 10 % of the current level (Farquhar et al., 2000; Pavlov and Kasting, 2002), and again during a “Neoproterozoic Oxygenation Event” (NOE) at ~800 to 542 million years ago (Canfield and Teske, 1996; Fike et al., 2006; Frei et al., 2009; Och and Shields-Zhou, 2012). View in article
Kah, L.C., Lyons, T.W., Frank, T.D. (2004) Low marine sulphate and protracted oxygenation of the proterozoic biosphere. Nature 431, 834-838.Show in contextAtmospheric O2 was extremely low in the Archean Eon (>2.5 Ga), and while multiple lines of evidence suggest that Earth’s oxygenation was protracted (Kah et al., 2004; Kah and Bartley, 2011; Lyons et al., 2014; Planavsky et al., 2014), pO2 may have risen abruptly at two different points in time: first during the “Great Oxygenation Event” (GOE) at ~2.4 Ga (Canfield, 2005; Holland, 2006; Guo et al., 2009; Farquhar et al., 2011), when atmospheric O2 rose from <0.001 % to an intermediate value commonly estimated as 1 to 10 % of the current level (Farquhar et al., 2000; Pavlov and Kasting, 2002), and again during a “Neoproterozoic Oxygenation Event” (NOE) at ~800 to 542 million years ago (Canfield and Teske, 1996; Fike et al., 2006; Frei et al., 2009; Och and Shields-Zhou, 2012). View in article
Konhauser, K.O., Pecoits, E., Lalonde, S.V., Papineau, D., Nisbet, E.G., Barley, M.E., Arndt, N.T., Zahnle, K., Kamber, B.S. (2009) Oceanic nickel depletion and a methanogen famine before the Great Oxidation Event. Nature 458, 750-753.Show in contextRedox-sensitive major and trace elements in iron formations and black shales deposited beneath euxinic waters have been developed as proxies to reconstruct palaeoenvironmental history in deep time (Scott et al., 2008; Konhauser et al., 2009; Sahoo et al., 2012). View in article
Lee, C.T.A., Luffi, P., Le Roux, V., Dasgupta, R., Albarede, F., Leeman, W.P. (2010) The redox state of arc mantle using Zn/Fe systematics. Nature 468, 681-685.Show in contextIn addition, because both Fe and Zn behave as incompatible elements during mantle partial melting, Zn/Fe has been developed as a tracer of mantle redox, revealing that the oxygen fugacity of the upper mantle has remained relatively constant through Earth history (Lee et al., 2010). View in article
Lyons, T.W., Reinhard, C.T., Planavsky, N.J. (2014) The rise of oxygen in Earth's early ocean and atmosphere. Nature 506, 307-315.Show in contextAtmospheric O2 was extremely low in the Archean Eon (>2.5 Ga), and while multiple lines of evidence suggest that Earth’s oxygenation was protracted (Kah et al., 2004; Kah and Bartley, 2011; Lyons et al., 2014; Planavsky et al., 2014), pO2 may have risen abruptly at two different points in time: first during the “Great Oxygenation Event” (GOE) at ~2.4 Ga (Canfield, 2005; Holland, 2006; Guo et al., 2009; Farquhar et al., 2011), when atmospheric O2 rose from <0.001 % to an intermediate value commonly estimated as 1 to 10 % of the current level (Farquhar et al., 2000; Pavlov and Kasting, 2002), and again during a “Neoproterozoic Oxygenation Event” (NOE) at ~800 to 542 million years ago (Canfield and Teske, 1996; Fike et al., 2006; Frei et al., 2009; Och and Shields-Zhou, 2012). View in article Our Palaeoproterozoic data are also consistent with earlier suggestions that pO2 may have risen substantially during the GOE and then declined again to persistent Proterozoic values (Lyons et al., 2014). View in article Figure 3 [...] The blue field indicates semi-quantitative interpretation from current understanding of the atmospheric O2 curve (modified from Lyons et al., 2014). View in article Moreover, the estimates match our current understanding (Lyons et al., 2014) of a general two-step increase of atmospheric O2 around the GOE and the NOE. View in article
Morel, F.M.M., Price, N.M. (2003) The Biogeochemical Cycles of Trace Metals in the Oceans. Science 300, 944-947.Show in contextAs an essential nutrient in many phytoplankton enzymes, especially those of eukaryotes (Williams and da Silva, 1996), zinc plays an important role in marine primary production, and for this reason, Zn is depleted in surface waters relative to the deep sea (Morel and Price, 2003). View in article
Morse, J.W., Luther III, G.W. (1999) Chemical influences on trace metal-sulfide interactions in anoxic sediments. Geochimica et Cosmochimica Acta 63, 3373-3378.Show in contextUnder sulphidic conditions, dissolved Zn2+ and Fe2+ behave similarly and are rapidly precipitated as sulphides (Morse and Luther III, 1999). View in article
Och, L.M., Shields-Zhou, G.A. (2012) The Neoproterozoic oxygenation event: Environmental perturbations and biogeochemical cycling. Earth-Science Reviews 110, 26-57.Show in contextAtmospheric O2 was extremely low in the Archean Eon (>2.5 Ga), and while multiple lines of evidence suggest that Earth’s oxygenation was protracted (Kah et al., 2004; Kah and Bartley, 2011; Lyons et al., 2014; Planavsky et al., 2014), pO2 may have risen abruptly at two different points in time: first during the “Great Oxygenation Event” (GOE) at ~2.4 Ga (Canfield, 2005; Holland, 2006; Guo et al., 2009; Farquhar et al., 2011), when atmospheric O2 rose from <0.001 % to an intermediate value commonly estimated as 1 to 10 % of the current level (Farquhar et al., 2000; Pavlov and Kasting, 2002), and again during a “Neoproterozoic Oxygenation Event” (NOE) at ~800 to 542 million years ago (Canfield and Teske, 1996; Fike et al., 2006; Frei et al., 2009; Och and Shields-Zhou, 2012). View in article
Pavlov, A.A., Kasting, J.F. (2002) Mass-independent fractionation of sulfur isotopes in Archean sediments: Strong evidence for an anoxic Archean atmosphere. Astrobiology 2, 27-41.Show in contextAtmospheric O2 was extremely low in the Archean Eon (>2.5 Ga), and while multiple lines of evidence suggest that Earth’s oxygenation was protracted (Kah et al., 2004; Kah and Bartley, 2011; Lyons et al., 2014; Planavsky et al., 2014), pO2 may have risen abruptly at two different points in time: first during the “Great Oxygenation Event” (GOE) at ~2.4 Ga (Canfield, 2005; Holland, 2006; Guo et al., 2009; Farquhar et al., 2011), when atmospheric O2 rose from <0.001 % to an intermediate value commonly estimated as 1 to 10 % of the current level (Farquhar et al., 2000; Pavlov and Kasting, 2002), and again during a “Neoproterozoic Oxygenation Event” (NOE) at ~800 to 542 million years ago (Canfield and Teske, 1996; Fike et al., 2006; Frei et al., 2009; Och and Shields-Zhou, 2012). View in article
Planavsky, N.J., Reinhard, C.T., Wang, X., Thomson, D., McGoldrick, P., Rainbird, R.H., Johnson, T., Fischer, W.W., Lyons, T.W. (2014) Low Mid-Proterozoic atmospheric oxygen levels and the delayed rise of animals. Science 346, 635-638.Show in contextAtmospheric O2 was extremely low in the Archean Eon (>2.5 Ga), and while multiple lines of evidence suggest that Earth’s oxygenation was protracted (Kah et al., 2004; Kah and Bartley, 2011; Lyons et al., 2014; Planavsky et al., 2014), pO2 may have risen abruptly at two different points in time: first during the “Great Oxygenation Event” (GOE) at ~2.4 Ga (Canfield, 2005; Holland, 2006; Guo et al., 2009; Farquhar et al., 2011), when atmospheric O2 rose from <0.001 % to an intermediate value commonly estimated as 1 to 10 % of the current level (Farquhar et al., 2000; Pavlov and Kasting, 2002), and again during a “Neoproterozoic Oxygenation Event” (NOE) at ~800 to 542 million years ago (Canfield and Teske, 1996; Fike et al., 2006; Frei et al., 2009; Och and Shields-Zhou, 2012). View in article This value is substantially lower than traditional estimates based on palaeosol work (Canfield, 1998; Rye and Holland, 1998), but consistent with recent estimates based on an independent tracer, a kinetic model for Cr-Mn oxidation and Cr isotopes in ironstones (Planavsky et al., 2014). View in article
Raiswell, R., Tranter, M., Benning, L.G., Siegert, M., De’ath, R., Huybrechts, P., Payne, T. (2006) Contributions from glacially derived sediment to the global iron (oxyhydr)oxide cycle: Implications for iron delivery to the oceans. Geochimica et Cosmochimica Acta 70, 2765-2780.Show in contextAlso, local primary production differences may contribute to Zn/Fe variability of different formations from the same interval. In the modern oxidised shallow ocean, particulate Fe sourced from eroding continents remains biogeochemically labile and may be cycled back to a dissolved phase during diagenesis in reducing continental margin sediments (Raiswell et al., 2006). View in article
Robbins, L.J., Lalonde, S.V., Saito, M.A., Planavsky, N.J., Mloszewska, A.M., Pecoits, E., Scott, C., Dupont, C.L., Kappler, A., Konhauser, K.O. (2013) Authigenic iron oxide proxies for marine zinc over geological time and implications for eukaryotic metallome evolution. Geobiology 11, 295-306.Show in contextIn the modern ocean, zinc input from hydrothermal ridge systems (~4.4 x 109 mol yr-1) is an order of magnitude greater than riverine fluxes (~3.4 x 108 mol yr-1; Robbins et al., 2013). View in article Zn concentrations in euxinic black shale and iron formations (Robbins et al., 2013; Scott et al., 2013), however, suggest that the bioavailability of Zn has not changed dramatically through Earth history. View in article
Rye, R., Holland, H.D. (1998) Paleosols and the evolution of atmospheric oxygen: A critical review. American Journal of Science 298, 621-672.Show in contextThis pO2 curve provides a more continuous coverage of atmospheric O2 levels compared to compilations derived from multiple geochemical tracers, such as mass-independent S isotopes and palaeosol records (Rye and Holland, 1998; Catling and Claire, 2005). View in article This value is substantially lower than traditional estimates based on palaeosol work (Canfield, 1998; Rye and Holland, 1998), but consistent with recent estimates based on an independent tracer, a kinetic model for Cr-Mn oxidation and Cr isotopes in ironstones (Planavsky et al., 2014). View in article
Sahoo, S.K., Planavsky, N.J., Kendall, B., Wang, X., Shi, X., Scott, C., Anbar, A.D., Lyons, T.W., Jiang, G. (2012) Ocean oxygenation in the wake of the Marinoan glaciation. Nature 489, 546-549.Show in contextRedox-sensitive major and trace elements in iron formations and black shales deposited beneath euxinic waters have been developed as proxies to reconstruct palaeoenvironmental history in deep time (Scott et al., 2008; Konhauser et al., 2009; Sahoo et al., 2012). View in article
Scott, C., Lyons, T.W., Bekker, A., Shen, Y., Poulton, S.W., Chu, X., Anbar, A.D. (2008) Tracing the stepwise oxygenation of the Proterozoic ocean. Nature 452, 456-U5.Show in contextRedox-sensitive major and trace elements in iron formations and black shales deposited beneath euxinic waters have been developed as proxies to reconstruct palaeoenvironmental history in deep time (Scott et al., 2008; Konhauser et al., 2009; Sahoo et al., 2012). View in article
Scott, C., Planavsky, N.J., Dupont, C.L., Kendall, B., Gill, B.C., Robbins, L.J., Husband, K.F., Arnold, G.L., Wing, B.A., Poulton, S.W., Bekker, A., Anbar, A.D., Konhauser, K.O., Lyons, T.W. (2013) Bioavailability of zinc in marine systems through time. Nature Geoscience 6, 125-128.Show in contextZn concentrations in euxinic black shale and iron formations (Robbins et al., 2013; Scott et al., 2013), however, suggest that the bioavailability of Zn has not changed dramatically through Earth history. View in article
Sperling, E.A., Wolock, C.J., Morgan, A.S., Gill, B.C., Kunzmann, M., Halverson, G.P., Macdonald, F.A., Knoll, A.H., Johnston, D.T. (2015) Statistical analysis of iron geochemical data suggests limited late Proterozoic oxygenation. Nature 523, 451-454.Show in contextThe latter transition may well have continued into the Phanerozoic Eon, eventually resulting in near-present O2 (Berner, 2006; Dahl et al., 2010; Sperling et al., 2015). View in article Palaeoenvironmental research on carbonate rocks commonly focuses on individual stratigraphic successions; here we adopt a complementary strategy, analysing a large suite of Phanerozoic, Proterozoic, and Archean samples that enables us to make statistical statements (Sperling et al., 2015) about Zn/Fe in the global surface ocean through geologic time. View in article
Watson, E.B. (2004) A conceptual model for near-surface kinetic controls on the trace-element and stable isotope composition of abiogenic calcite crystals. Geochimica et Cosmochimica Acta 68, 1473-1488.Show in contextIn addition, theoretical calculations suggest that kinetic effects on trace element partitioning in carbonate may contribute to Zn/Fe variability in samples from the same locality (Watson, 2004; DePaolo, 2011). View in article
Wheat, C.G., Mottl, M.J., Rudnicki, M. (2002) Trace element and REE composition of a low-temperature ridge-flank hydrothermal spring. Geochimica et Cosmochimica Acta 66, 3693-3705.Show in contextThe Fe budget is similar to that of Zn, wherein hydrothermal input dominates over riverine fluxes by a factor of ~9 (Wheat et al., 2002). View in article
Williams, R.J.P., da Silva, J.J.R.F. (1996) The natural selection of the chemical elements. Great Britian, Bath Press Ltd.Show in contextAs an essential nutrient in many phytoplankton enzymes, especially those of eukaryotes (Williams and da Silva, 1996), zinc plays an important role in marine primary production, and for this reason, Zn is depleted in surface waters relative to the deep sea (Morel and Price, 2003). View in article
Wilson, J.P., Fischer, W.W., Johnston, D.T., Knoll, A.H., Grotzinger, J.P., Walter, M.R., McNaughton, N.J., Simon, M., Abelson, J., Schrag, D.P., Summons, R., Allwood, A., Andres, M., Gammon, C., Garvin, J., Rashby, S., Schweizer, M., Watters, W.A. (2010) Geobiology of the late Paleoproterozoic Duck Creek Formation, Western Australia. Precambrian Research 179, 135-149.Show in contextLimestone and penecontemporaneous dolomites that retain depositional signatures well (Wilson et al., 2010) are abundant in the geologic record, typically recording shallow marine environments that would have been in open communication with the overlying atmosphere. View in article
