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  • The influence of terrigenous particulate Material Dissolution on ocean chemistry and global element cycles
    Chemical Geology, 2015
    Co-Authors: Catherine Jeandel, Eric H. Oelkers
    Abstract:

    Land to ocean transfer of Material largely controls the chemical composition of seawater and the global element cycles. Overall this transfer is dominated by the riverine transport of particulate Material to the oceans. A large number of isotopic tracers including 143Nd/144Nd, 87Sr/86Sr, 30Si/28Si, 56Fe/54Fe, and 232Th/230Th, demonstrate that a significant fraction of this particulate Material dissolves in seawater after its arrival to the oceans. Laboratory experiments confirm that these particles dissolve readily in seawater; 0.5 to 10% of the Sr and Nd in riverine transported particulate Material is found to dissolve in seawater over time scales ranging from weeks to months. Noting that the mass of most elements arriving to the oceans via particulates exceeds that of the elements arriving via dissolved transport by at least a factor of 50, it follows that 1) particulate Material Dissolution in the ocean may be the dominant mechanism contributing numerous elements to the oceans, and 2) estimates based on dissolved riverine transport alone may significantly underestimate the global element fluxes to the oceans. The role of particulate Material Dissolution in seawater may be most significant in the cycles of sparingly soluble elements, which are far more concentrated in particulate Material than more soluble elements. As such, particulate Material Dissolution and transport likely play a major role in the availability of those elements limiting marine primary productivity. This effect will be most significant at the ocean margins, as a large fraction of the products of particulate Material Dissolution are re-precipitated locally via reversible scavenging. The major effect of particulate Dissolution in the open-ocean will be on element isotope compositions. Moreover, as the transport of particulates to the oceans is far more sensitive to temperature and runoff than dissolved transport, the Dissolution of particulate in seawater and subsequent reactions may provide a strong yet underappreciated link between continental weathering and climate.

  • Riverine particulate Material Dissolution in seawater and its implications for the global cycles of the elements
    Comptes Rendus Geoscience, 2012
    Co-Authors: Eric H. Oelkers, Catherine Jeandel, Morgan T. Jones, Christopher R. Pearce, Eydis S. Eiriksdottir, Sigurður R. Gislason
    Abstract:

    Abstract The total mass of Material globally transported to the oceans as particulate Material is as much as 30 times greater that transported to the oceans in dissolved form. The degree to which riverine transported particles impact ocean chemistry and influence global elemental cycles depends on the reactivity of this particulate Material in seawater and the relative concentration of each element. The concentrations of elements in particulate Material relative to those of seawater range from less than 1 for soluble elements such as Na, to more than 10 7 for insoluble elements such as Al, Fe, and the Rare Earths. The reactivity of particulate Material in seawater is difficult to assess directly because this fluid is saturated or supersaturated with respect to numerous elements. As such, element release from the particulate Material is commonly matched by precipitation of secondary phases. The rates of element release can, however, be quantified by monitoring the isotopic evolution of seawater during its reaction with a variety of particulate Material samples collected from rivers throughout the world. This research focuses on the behavior of Sr and Nd, representative of the most and least soluble elements transported to the oceans. Batch experiments demonstrate that between 0.15 and 27% of Sr is liberated from volcanic and continental particulates when interacted with seawater over 6 months. Similarly, from 1.5 to 8.5% of Nd is liberated from volcanic sediments over this timespan. This observed elemental release rate from riverine particulate Material has important consequences for: (1) chemical and isotopic mass balances in the ocean; and (2) the application of the isotopic weathering proxies to the geological record.

  • Riverine particulate Material Dissolution as a significant flux of strontium to the oceans
    Earth and Planetary Science Letters, 2012
    Co-Authors: Morgan T. Jones, Catherine Jeandel, Christopher R. Pearce, Sigurður R. Gislason, Eydis S. Eiriksdottir, Vasileios Mavromatis, Eric H. Oelkers
    Abstract:

    The ratio of strontium isotopes, 87Sr/86Sr, in seawater is homogenous at any given time, yet varies considerably throughout the geological record. This variation is thought to stem from changes in the balance of predominantly radiogenic Sr entering the oceans via dissolved riverine transport, and unradiogenic Sr sourced from mid-ocean ridge hydrothermal activity. Recent evidence suggests, however, that hydrothermal exchange at mid-ocean ridges is a factor of 3 too low to balance Sr added to the oceans from dissolved continental riverine fluxes. Here we present evidence that the arrival and subsequent Dissolution of riverine particulate Material in seawater is a significant contributor of both radiogenic and unradiogenic Sr to the oceans. Batch experiments demonstrate that between 0.15% and 27.36% of Sr is liberated from riverine particulates to seawater within 6 months. The rates of release are dependent on surface area and particulate composition, with volcanic riverine Material more reactive than continental riverine particulates. The observed rapid Sr release rate from riverine particulate Material has important consequences for both chemical and isotopic mass balances in the ocean and the application of the 87Sr/86Sr weathering proxy to the geological record. The Dissolution of riverine particulate Material is likely, based on these findings, to at least partially account for the imbalance between Sr sources to the oceans.

  • Riverine particulate Material Dissolution as a significant flux of strontium to the oceans
    Earth and Planetary Science Letters, 2012
    Co-Authors: Morgan T. Jones, Catherine Jeandel, Christopher R. Pearce, Sigurður R. Gislason, Eydis S. Eiriksdottir, Vasileios Mavromatis, Eric H. Oelkers
    Abstract:

    ISI Document Delivery No.: 078DQ Times Cited: 2 Cited Reference Count: 62 Cited References: ALBAREDE F, 1981, EARTH PLANET SC LETT, V55, P229, DOI 10.1016/0012-821X(81)90102-3 Allegre CJ, 2010, EARTH PLANET SC LETT, V292, P51, DOI 10.1016/j.epsl.2010.01.019 Aller R.C, 2008, J GEOPHYS RES, P113 Aller RC, 1998, MAR CHEM, V61, P143, DOI 10.1016/S0304-4203(98)00024-3 Arsouze T., 2009, BIOGEOSCIENCES, V6, P1 BERNER RA, 1992, GEOCHIM COSMOCHIM AC, V56, P3225, DOI 10.1016/0016-7037(92)90300-8 BLUTH GJS, 1994, GEOCHIM COSMOCHIM AC, V58, P2341, DOI 10.1016/0016-7037(94)90015-9 Brass G, 1976, GEOCHIM COSMOCHIM AC, V40, P720 Broecker W. S., 1982, TRACERS SEA Brunauer S, 1938, J AM CHEM SOC, V60, P309, DOI 10.1021/ja01269a023 Butterfield DA, 2001, GEOCHIM COSMOCHIM AC, V65, P4141, DOI 10.1016/S0016-7037(01)00712-8 Compton JS, 2007, S AFR J GEOL, V110, P339, DOI 10.2113/gssajg.110.2-3.339 Davis AC, 2003, EARTH PLANET SC LETT, V211, P173, DOI 10.1016/S0012-821X(03)00191-2 Durant AJ, 2010, ELEMENTS, V6, P235, DOI 10.2113/gselements.6.4.235 Egholm DL, 2009, NATURE, V460, P884, DOI 10.1038/nature08263 Eiriksdottir ES, 2008, EARTH PLANET SC LETT, V272, P78, DOI 10.1016/j.epsl.2008.04.005 Elderfield H, 1999, EARTH PLANET SC LETT, V172, P151, DOI 10.1016/S0012-821X(99)00191-0 ELDERFIELD H, 1982, NATURE, V300, P493, DOI 10.1038/300493a0 Elderfield H, 1996, ANNU REV EARTH PL SC, V24, P191, DOI 10.1146/annurev.earth.24.1.191 Gaillardet J, 1999, GEOCHIM COSMOCHIM AC, V63, P4037, DOI 10.1016/S0016-7037(99)00307-5 Gaillardet J., 2003, TREATISE GEOCHEMISTR, V5 Galy A, 1999, GEOCHIM COSMOCHIM AC, V63, P1905, DOI 10.1016/S0016-7037(99)00081-2 Gislason S.R, 2008, EARTH PLANET SC LETT, V277, P213 Gislason SR, 2006, GEOLOGY, V34, P49, DOI 10.1130/G22045.1 Gislason SR, 2011, P NATL ACAD SCI USA, V108, P7307, DOI 10.1073/pnas.1015053108 GOLDSTEIN SJ, 1987, CHEM GEOL, V66, P245, DOI 10.1016/0168-9622(87)90045-5 HODELL DA, 1989, EARTH PLANET SC LETT, V92, P165, DOI 10.1016/0012-821X(89)90044-7 Holland HD, 2005, AM J SCI, V305, P220, DOI 10.2475/ajs.305.3.220 Hsieh YT, 2011, EARTH PLANET SC LETT, V312, P280, DOI 10.1016/j.epsl.2011.10.022 Jeandel C., 2011, EOS T AM GEOPHYS UN, V92, P217 Jones MT, 2012, GEOCHIM COSMOCHIM AC, V77, P108, DOI 10.1016/j.gca.2011.10.044 Jones MT, 2011, B VOLCANOL, V73, P207, DOI 10.1007/s00445-010-0397-0 Jones MT, 2008, GEOCHIM COSMOCHIM AC, V72, P3661, DOI 10.1016/j.gca.2008.05.030 Krabbenhoft A, 2010, GEOCHIM COSMOCHIM AC, V74, P4097, DOI 10.1016/j.gca.2010.04.009 Lacan F, 2005, EARTH PLANET SC LETT, V232, P245, DOI 10.1016/j.epsl.2005.01.004 Louvat P, 2008, AM J SCI, V308, P679, DOI 10.2475/05.2008.02 MACKENZI.FT, 1966, AM J SCI, V264, P507 MARTIN JM, 1979, MAR CHEM, V7, P173, DOI 10.1016/0304-4203(79)90039-2 McArthur JM, 2001, J GEOL, V109, P155, DOI 10.1086/319243 Meybeck M, 2003, GLOBAL PLANET CHANGE, V39, P65, DOI 10.1016/S0921-8181(03)00018-3 MICHALOPOULOS P, 1995, SCIENCE, V270, P614, DOI 10.1126/science.270.5236.614 Milliman J.D., 2011, RIVER DISCHARGE COAS MILLIMAN JD, 1992, J GEOL, V100, P525 Milliman J.D, 2001, ENCY OCEAN SCI MOTTL MJ, 1994, GEOCHIM COSMOCHIM AC, V58, P2225, DOI 10.1016/0016-7037(94)90007-8 Oelkers EH, 2011, APPL GEOCHEM, V26, pS365, DOI 10.1016/j.apgeochem.2011.03.062 PALMER MR, 1989, EARTH PLANET SC LETT, V92, P11, DOI 10.1016/0012-821X(89)90017-4 Pearce CR, 2010, EARTH PLANET SC LETT, V295, P104, DOI 10.1016/j.epsl.2010.03.032 Pedersen VK, 2010, GEOMORPHOLOGY, V122, P129, DOI 10.1016/j.geomorph.2010.06.005 Peucker-Ehrenbrink B, 2010, GEOCHEM GEOPHY GEOSY, V11, DOI 10.1029/2009GC002869 von Strandmann Philip A E Pogge, 2008, Earth and Planetary Science Letters, V274, DOI 10.1016/j.epsl.2008.07.041 Stein M, 1997, GEOCHIM COSMOCHIM AC, V61, P3975, DOI 10.1016/S0016-7037(97)00191-9 Syvitski JPM, 2003, SEDIMENT GEOL, V162, P5, DOI 10.1016/S0037-0738(03)00232-X Tipper ET, 2006, EARTH PLANET SC LETT, V250, P241, DOI 10.1016/j.epsl.2006.07.037 Vance D, 2009, NATURE, V458, P493, DOI 10.1038/nature07828 VEIZER J, 1974, GEOCHIM COSMOCHIM AC, V38, P1461, DOI 10.1016/0016-7037(74)90099-4 Viers J, 2009, SCI TOTAL ENVIRON, V407, P853, DOI 10.1016/j.scitotenv.2008.09.053 Walling DE, 2006, GEOMORPHOLOGY, V79, P192, DOI 10.1016/j.geomorph.2006.06.019 Wallmann K, 2008, GEOCHIM COSMOCHIM AC, V72, P2895, DOI 10.1016/j.gca.2008.03.026 Wall-Palmer D, 2011, MAR GEOL, V282, P231, DOI 10.1016/j.margeo.2011.03.001 Wolff-Boenisch D, 2004, GEOCHIM COSMOCHIM AC, V68, P4843, DOI 10.1016/j.gca.2004.05.027 Wolff-Boenisch D, 2006, GEOCHIM COSMOCHIM AC, V70, P858, DOI 10.1016/j.gca.2005.10.016 Jones, Morgan T. Pearce, Christopher R. Jeandel, Catherine Gislason, Sigurour R. Eiriksdottir, Eydis S. Mavromatis, Vasileios Oelkers, Eric H. Pearce, Christopher/A-5599-2010 Pearce, Christopher/0000-0002-4382-2341 EC Marie Curie 'MIN-GRO' Research and Training Network [MRTN-CT-2006-035488]; Marie Curie Intra-European Fellowship [PIEF-GA-2009-254495] We thank Jerome Gaillardet and John Compton for the provision of samples. Derek Vance and an anonymous reviewer provided constructive and insightful comments and criticisms on this manuscript. M. T. Jones and C. R. Pearce were supported by the EC Marie Curie 'MIN-GRO' Research and Training Network (MRTN-CT-2006-035488). M. T. Jones is currently supported by a Marie Curie Intra-European Fellowship (PIEF-GA-2009-254495). 2 ELSEVIER SCIENCE BV AMSTERDAM EARTH PLANET SC LETTThe ratio of strontium isotopes, Sr-87/Sr-86, in seawater is homogenous at any given time, yet varies considerably throughout the geological record. This variation is thought to stem from changes in the balance of predominantly radiogenic Sr entering the oceans via dissolved riverine transport, and unradiogenic Sr sourced from mid-ocean ridge hydrothermal activity. Recent evidence suggests, however, that hydrothermal exchange at mid-ocean ridges is a factor of 3 too low to balance Sr added to the oceans from dissolved continental riverine fluxes. Here we present evidence that the arrival and subsequent Dissolution of riverine particulate Material in seawater is a significant contributor of both radiogenic and unradiogenic Sr to the oceans. Batch experiments demonstrate that between 0.15% and 27.36% of Sr is liberated from riverine particulates to seawater within 6 months. The rates of release are dependent on surface area and particulate composition, with volcanic riverine Material more reactive than continental riverine particulates. The observed rapid Sr release rate from riverine particulate Material has important consequences for both chemical and isotopic mass balances in the ocean and the application of the Sr-87/Sr-86 weathering proxy to the geological record. The Dissolution of riverine particulate Material is likely, based on these findings, to at least partially account for the imbalance between Sr sources to the oceans. (C) 2012 Elsevier B.V. All rights reserved

  • Riverine particulate Material Dissolution in seawater and its implications for the global cycles of the elements
    Comptes Rendus Geoscience, 2012
    Co-Authors: Eric H. Oelkers, Catherine Jeandel, Morgan T. Jones, Christopher R. Pearce, Eydis S. Eiriksdottir, Sigurður R. Gislason
    Abstract:

    ISI Document Delivery No.: 062NH Times Cited: 1 Cited Reference Count: 41 Cited References: Allegre CJ, 2010, EARTH PLANET SC LETT, V292, P51, DOI 10.1016/j.epsl.2010.01.019 Aller RC, 1996, CONT SHELF RES, V16, P753, DOI 10.1016/0278-4343(95)00046-1 Arsouze T., 2009, BIOGEOSCIENCES, V6, P1 Blum AE, 1995, REV MINERAL, V31, P291 Brady PV, 1997, GEOCHIM COSMOCHIM AC, V61, P965, DOI 10.1016/S0016-7037(96)00385-7 Burton KW, 1997, NATURE, V386, P382, DOI 10.1038/386382a0 Chairat C, 2007, GEOCHIM COSMOCHIM AC, V71, P5901, DOI 10.1016/j.gca.2007.08.031 Davis AC, 2003, EARTH PLANET SC LETT, V211, P173, DOI 10.1016/S0012-821X(03)00191-2 Frank M, 2002, REV GEOPHYS, V40, DOI 10.1029/2000RG000094 Fripiat F, 2011, MAR CHEM, V123, P11, DOI 10.1016/j.marchem.2010.08.005 Gaillardet J., 2003, TREATISE GEOCHEMISTR, V5 Gherbi C, 2010, CR GEOSCI, V342, P126, DOI 10.1016/j.crte.2009.11.002 Gislason SR, 2006, GEOLOGY, V34, P49, DOI 10.1130/G22045.1 Gislason SR, 2009, EARTH PLANET SC LETT, V277, P213, DOI 10.1016/j.epsl.2008.10.018 Hatje V, 2003, ENVIRON INT, V29, P619, DOI 10.1016/S0160-4120(03)00049-7 Jeandel C., 2011, EOS T AM GEOPHYS UN, V92, P217 Jeandel C, 1998, GEOCHIM COSMOCHIM AC, V62, P2597, DOI 10.1016/S0016-7037(98)00169-0 Jickells TD, 2005, SCIENCE, V308, P67, DOI 10.1126/science.1105959 Jones MT, 2012, GEOCHIM COSMOCHIM AC, V77, P108, DOI 10.1016/j.gca.2011.10.044 Jones M.T., EARTH PLANET S UNPUB Kohler SJ, 2005, CHEM GEOL, V222, P168, DOI 10.1016/j.chemgeo.2005.07.011 Lacan F, 2001, EARTH PLANET SC LETT, V186, P497, DOI 10.1016/S0012-821X(01)00263-1 Lacan F, 2005, EARTH PLANET SC LETT, V232, P245, DOI 10.1016/j.epsl.2005.01.004 Mavromatis V., 2012, EARTH PLANET SCI LET McKee BA, 2004, CONT SHELF RES, V24, P899, DOI 10.1016/j.csr.2004.02.009 Oelkers EH, 2011, APPL GEOCHEM, V26, pS365, DOI 10.1016/j.apgeochem.2011.03.062 Oelkers EH, 2009, GEOCHIM COSMOCHIM AC, V73, P4617, DOI 10.1016/j.gca.2009.05.028 Oelkers EH, 2002, CHEM GEOL, V191, P73, DOI 10.1016/S0009-2541(02)00149-3 PALMER MR, 1989, EARTH PLANET SC LETT, V92, P11, DOI 10.1016/0012-821X(89)90017-4 PARKS GA, 1990, REV MINERAL, V23, P133 Peucker-Ehrenbrink B, 2010, GEOCHEM GEOPHY GEOSY, V11, DOI 10.1029/2009GC002869 SCHOTT J, 1995, PURE APPL CHEM, V67, P903, DOI 10.1351/pac199567060903 Schott J, 2009, REV MINERAL GEOCHEM, V70, P207, DOI 10.2138/rmg.2009.70.6 Stefansdottir MB, 2005, EARTH PLANET SC LETT, V237, P433, DOI 10.1016/j.epsl.2005.07.002 Syvitski JPM, 2005, SCIENCE, V308, P376, DOI 10.1126/science.1109454 Turekian K.K., 1968, OCEANS Vance D, 2009, NATURE, V458, P493, DOI 10.1038/nature07828 Viers J, 2009, SCI TOTAL ENVIRON, V407, P853, DOI 10.1016/j.scitotenv.2008.09.053 Walling DE, 2006, GEOMORPHOLOGY, V79, P192, DOI 10.1016/j.geomorph.2006.06.019 Wimpenny J, 2010, GEOCHIM COSMOCHIM AC, V74, P5259, DOI 10.1016/j.gca.2010.06.028 Wolff-Boenisch D, 2006, GEOCHIM COSMOCHIM AC, V70, P858, DOI 10.1016/j.gca.2005.10.016 Oelkers, Eric H. Jones, Morgan T. Pearce, Christopher R. Jeandel, Catherine Eiriksdottir, Eydis Salome Gislason, Sigurdur R. Pearce, Christopher/A-5599-2010 Pearce, Christopher/0000-0002-4382-2341 EC Marie Curie "MIN-GRO" Research and Training Network [MRTN-CT-2006-035488]; Marie Curie Intra-European Fellowship [PIEF-GA-2009-254495] We thank Jerome Gaillardet, Derek Vance, Jacques Schott, and Oleg Pokrovsky for insightful discussions and encouragement. M.T.Jones and C.R. Pearce were supported by the EC Marie Curie "MIN-GRO" Research and Training Network (MRTN-CT-2006-035488). M.T.Jones is currently supported by a Marie Curie Intra-European Fellowship (PIEF-GA-2009-254495). 1 ELSEVIER FRANCE-EDITIONS SCIENTIFIQUES MEDICALES ELSEVIER PARIS CR GEOSCIThe total mass of Material globally transported to the oceans as particulate Material is as much as 30 times greater that transported to the oceans in dissolved form. The degree to which riverine transported particles impact ocean chemistry and influence global elemental cycles depends on the reactivity of this particulate Material in seawater and the relative concentration of each element. The concentrations of elements in particulate Material relative to those of seawater range from less than 1 for soluble elements such as Na, to more than 10(7) for insoluble elements such as Al, Fe, and the Rare Earths. The reactivity of particulate Material in seawater is difficult to assess directly because this fluid is saturated or supersaturated with respect to numerous elements. As such, element release from the particulate Material is commonly matched by precipitation of secondary phases. The rates of element release can, however, be quantified by monitoring the isotopic evolution of seawater during its reaction with a variety of particulate Material samples collected from rivers throughout the world. This research focuses on the behavior of Sr and Nd, representative of the most and least soluble elements transported to the oceans. Batch experiments demonstrate that between 0.15 and 27% of Sr is liberated from volcanic and continental particulates when interacted with seawater over 6 months. Similarly, from 1.5 to 8.5% of Nd is liberated from volcanic sediments over this timespan. This observed elemental release rate from riverine particulate Material has important consequences for: (1) chemical and isotopic mass balances in the ocean; and (2) the application of the isotopic weathering proxies to the geological record. (c) 2012 Academie des sciences. Published by Elsevier Masson SAS. All rights reserved

Shinichi Shimizu - One of the best experts on this subject based on the ideXlab platform.

Hideaki Hamada - One of the best experts on this subject based on the ideXlab platform.

Andrey P. Jivkov - One of the best experts on this subject based on the ideXlab platform.

  • On Dissolution driven crack growth
    International Journal of Solids and Structures, 2007
    Co-Authors: Per Ståhle, Christina Bjerkén, Andrey P. Jivkov
    Abstract:

    The formation and growth of a crack in a body subjected to stress driven Material Dissolution is studied. The rate of Material Dissolution is proportional to strain energy and curvature of the body surface. The formation of a crack from a plane surface is preceded by an evolving surface roughness. The continued Dissolution enhances roughness amplitude resulting in pit formation. As the pit grows deeper into the Material, it assumes the shape of a crack. The sharpness of the crack reaches its maximum during this transition from a pit to a crack. As the crack grows, a self-similar state is gradually assumed. During this phase characteristic lengths of the crack shape scale with the crack length. In line with this the crack progressively becomes blunt. The widest part of the crack when unloaded is in the vicinity of the crack tip. A consequence of the model is that no criterion is needed for crack growth. Neither is a criterion needed for determination of the crack path. It also follows that the crack growth rate is almost independent of the remote load. Further, spontaneous crack branching is anticipated. A motivation for this is given.

  • On Dissolution driven crack growth
    2006
    Co-Authors: Per Ståhle, Andrey P. Jivkov, Christina Bjerkén, T Nakamura
    Abstract:

    The formation and growth of a crack in a body subjected to stress driven Material Dissolution is studied. The rate of Material Dissolution is proportional to strain energy and curvature of the body surface. The evolution of a crack from a plane surface is via a developed waviness of the surface. The continued Dissolution makes waves grow to become pits. As a pit grows deeperinto the Material it assumes the shape of a crack. The sharpness of the crack reaches its maximum during this transition from a pit to a crack. As the crack grows, a self-similar state is gradually assumed. During this phase characteristic lengths of the crack shape scale with the crack length. In line with this the crack is progressively blunting. The widest part of the crack when unloaded is in the vicinity of the crack tip. A consequence of the model is that no criterion is needed for crack growth. It also follows that crack growth rate is almost independent of the remote load. The crack grows with a nearly constant rate. Neither is a criterion needed for determination of the crack path. When a certain width is reached at the crack tip the crack spontaneously branches. Both branches grow with the same rate as the original crack. The width of the branches is around half of the width of the crack immediately before branching.

  • Selfsimilar solutions for stress driven Material Dissolution
    2004
    Co-Authors: Per Ståhle, Andrey P. Jivkov
    Abstract:

    ECF 15 - The 15th European Conference of Fracture - advanced fracture mechanics for life and safety assessments, Stockholm, August 11-13, 2004

  • Selfsimilar solutions for stress driven Material Dissolution : Advanced Fracture Mechanics for Life and Safety Assessments
    2004
    Co-Authors: Per Ståhle, Andrey P. Jivkov
    Abstract:

    During corrosive Dissolution of metal ions from a body surface, an oxide compound isproduced. This compound forms a protective film that reduces the Dissolution rate. When afraction of a millimetre depth is dissolved the Dissolution rate become insignificant. However,repeated loading will damage the film with continued Dissolution as a result. In connectionwith this a threshold strain is assumed to exist. This paper proposes a model where electrochemical processes and the mechanical load work together in forming a corrosion pit. Theratio between the threshold strain and the remotely applied strain is shown to control theshape of the pit. For small applied strains cracks are formed. A crack evolving from a surfaceirregularity is studied. The growth rate of the crack is determined by the Dissolution rate atthe crack tip. No crack growth criterion is needed. The growing crack is itself creatingconditions for strain concentration, which leads to a high crack growth rate. The modelsimulates how Dissolution forms a pit that grows to become a crack in a single continuousprocess. For small loads the crack growth rate is independent of applied load. (Less)

  • Surface irregularities as sources for corrosion fatigue
    2003
    Co-Authors: Andrey P. Jivkov
    Abstract:

    Corrosion fatigue crack nucleation from surface irregularity is modelled as a mov-ing boundary value problem. The model is based on Material Dissolution proportional to the surface stretch. Dissolution and re-passivation processes are forming the ge-ometry of the crack tip, thus creating con-ditions for strain concentration. No crack growth criterion is used. The interaction between the electrochemical processes and the deformation of the crack tip region is incorporated in continuum mechanical theory. Elastic-perfectly plastic Materials under low frequency cyclic load are con-sidered. The model simulates how cracks form and grow in a single continuous process. The resulting natural variation of lengths of the formed cracks makes them grow with different rates. One crack after another falls into a wake behind a larger crack and the crack tip load of the smaller decreases leading to its arrest.

Catherine Jeandel - One of the best experts on this subject based on the ideXlab platform.

  • The influence of terrigenous particulate Material Dissolution on ocean chemistry and global element cycles
    Chemical Geology, 2015
    Co-Authors: Catherine Jeandel, Eric H. Oelkers
    Abstract:

    Land to ocean transfer of Material largely controls the chemical composition of seawater and the global element cycles. Overall this transfer is dominated by the riverine transport of particulate Material to the oceans. A large number of isotopic tracers including 143Nd/144Nd, 87Sr/86Sr, 30Si/28Si, 56Fe/54Fe, and 232Th/230Th, demonstrate that a significant fraction of this particulate Material dissolves in seawater after its arrival to the oceans. Laboratory experiments confirm that these particles dissolve readily in seawater; 0.5 to 10% of the Sr and Nd in riverine transported particulate Material is found to dissolve in seawater over time scales ranging from weeks to months. Noting that the mass of most elements arriving to the oceans via particulates exceeds that of the elements arriving via dissolved transport by at least a factor of 50, it follows that 1) particulate Material Dissolution in the ocean may be the dominant mechanism contributing numerous elements to the oceans, and 2) estimates based on dissolved riverine transport alone may significantly underestimate the global element fluxes to the oceans. The role of particulate Material Dissolution in seawater may be most significant in the cycles of sparingly soluble elements, which are far more concentrated in particulate Material than more soluble elements. As such, particulate Material Dissolution and transport likely play a major role in the availability of those elements limiting marine primary productivity. This effect will be most significant at the ocean margins, as a large fraction of the products of particulate Material Dissolution are re-precipitated locally via reversible scavenging. The major effect of particulate Dissolution in the open-ocean will be on element isotope compositions. Moreover, as the transport of particulates to the oceans is far more sensitive to temperature and runoff than dissolved transport, the Dissolution of particulate in seawater and subsequent reactions may provide a strong yet underappreciated link between continental weathering and climate.

  • Riverine particulate Material Dissolution in seawater and its implications for the global cycles of the elements
    Comptes Rendus Geoscience, 2012
    Co-Authors: Eric H. Oelkers, Catherine Jeandel, Morgan T. Jones, Christopher R. Pearce, Eydis S. Eiriksdottir, Sigurður R. Gislason
    Abstract:

    Abstract The total mass of Material globally transported to the oceans as particulate Material is as much as 30 times greater that transported to the oceans in dissolved form. The degree to which riverine transported particles impact ocean chemistry and influence global elemental cycles depends on the reactivity of this particulate Material in seawater and the relative concentration of each element. The concentrations of elements in particulate Material relative to those of seawater range from less than 1 for soluble elements such as Na, to more than 10 7 for insoluble elements such as Al, Fe, and the Rare Earths. The reactivity of particulate Material in seawater is difficult to assess directly because this fluid is saturated or supersaturated with respect to numerous elements. As such, element release from the particulate Material is commonly matched by precipitation of secondary phases. The rates of element release can, however, be quantified by monitoring the isotopic evolution of seawater during its reaction with a variety of particulate Material samples collected from rivers throughout the world. This research focuses on the behavior of Sr and Nd, representative of the most and least soluble elements transported to the oceans. Batch experiments demonstrate that between 0.15 and 27% of Sr is liberated from volcanic and continental particulates when interacted with seawater over 6 months. Similarly, from 1.5 to 8.5% of Nd is liberated from volcanic sediments over this timespan. This observed elemental release rate from riverine particulate Material has important consequences for: (1) chemical and isotopic mass balances in the ocean; and (2) the application of the isotopic weathering proxies to the geological record.

  • Riverine particulate Material Dissolution as a significant flux of strontium to the oceans
    Earth and Planetary Science Letters, 2012
    Co-Authors: Morgan T. Jones, Catherine Jeandel, Christopher R. Pearce, Sigurður R. Gislason, Eydis S. Eiriksdottir, Vasileios Mavromatis, Eric H. Oelkers
    Abstract:

    The ratio of strontium isotopes, 87Sr/86Sr, in seawater is homogenous at any given time, yet varies considerably throughout the geological record. This variation is thought to stem from changes in the balance of predominantly radiogenic Sr entering the oceans via dissolved riverine transport, and unradiogenic Sr sourced from mid-ocean ridge hydrothermal activity. Recent evidence suggests, however, that hydrothermal exchange at mid-ocean ridges is a factor of 3 too low to balance Sr added to the oceans from dissolved continental riverine fluxes. Here we present evidence that the arrival and subsequent Dissolution of riverine particulate Material in seawater is a significant contributor of both radiogenic and unradiogenic Sr to the oceans. Batch experiments demonstrate that between 0.15% and 27.36% of Sr is liberated from riverine particulates to seawater within 6 months. The rates of release are dependent on surface area and particulate composition, with volcanic riverine Material more reactive than continental riverine particulates. The observed rapid Sr release rate from riverine particulate Material has important consequences for both chemical and isotopic mass balances in the ocean and the application of the 87Sr/86Sr weathering proxy to the geological record. The Dissolution of riverine particulate Material is likely, based on these findings, to at least partially account for the imbalance between Sr sources to the oceans.

  • Riverine particulate Material Dissolution as a significant flux of strontium to the oceans
    Earth and Planetary Science Letters, 2012
    Co-Authors: Morgan T. Jones, Catherine Jeandel, Christopher R. Pearce, Sigurður R. Gislason, Eydis S. Eiriksdottir, Vasileios Mavromatis, Eric H. Oelkers
    Abstract:

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Pearce, Christopher R. Jeandel, Catherine Gislason, Sigurour R. Eiriksdottir, Eydis S. Mavromatis, Vasileios Oelkers, Eric H. Pearce, Christopher/A-5599-2010 Pearce, Christopher/0000-0002-4382-2341 EC Marie Curie 'MIN-GRO' Research and Training Network [MRTN-CT-2006-035488]; Marie Curie Intra-European Fellowship [PIEF-GA-2009-254495] We thank Jerome Gaillardet and John Compton for the provision of samples. Derek Vance and an anonymous reviewer provided constructive and insightful comments and criticisms on this manuscript. M. T. Jones and C. R. Pearce were supported by the EC Marie Curie 'MIN-GRO' Research and Training Network (MRTN-CT-2006-035488). M. T. Jones is currently supported by a Marie Curie Intra-European Fellowship (PIEF-GA-2009-254495). 2 ELSEVIER SCIENCE BV AMSTERDAM EARTH PLANET SC LETTThe ratio of strontium isotopes, Sr-87/Sr-86, in seawater is homogenous at any given time, yet varies considerably throughout the geological record. This variation is thought to stem from changes in the balance of predominantly radiogenic Sr entering the oceans via dissolved riverine transport, and unradiogenic Sr sourced from mid-ocean ridge hydrothermal activity. Recent evidence suggests, however, that hydrothermal exchange at mid-ocean ridges is a factor of 3 too low to balance Sr added to the oceans from dissolved continental riverine fluxes. Here we present evidence that the arrival and subsequent Dissolution of riverine particulate Material in seawater is a significant contributor of both radiogenic and unradiogenic Sr to the oceans. Batch experiments demonstrate that between 0.15% and 27.36% of Sr is liberated from riverine particulates to seawater within 6 months. The rates of release are dependent on surface area and particulate composition, with volcanic riverine Material more reactive than continental riverine particulates. The observed rapid Sr release rate from riverine particulate Material has important consequences for both chemical and isotopic mass balances in the ocean and the application of the Sr-87/Sr-86 weathering proxy to the geological record. The Dissolution of riverine particulate Material is likely, based on these findings, to at least partially account for the imbalance between Sr sources to the oceans. (C) 2012 Elsevier B.V. All rights reserved

  • Riverine particulate Material Dissolution in seawater and its implications for the global cycles of the elements
    Comptes Rendus Geoscience, 2012
    Co-Authors: Eric H. Oelkers, Catherine Jeandel, Morgan T. Jones, Christopher R. Pearce, Eydis S. Eiriksdottir, Sigurður R. Gislason
    Abstract:

    ISI Document Delivery No.: 062NH Times Cited: 1 Cited Reference Count: 41 Cited References: Allegre CJ, 2010, EARTH PLANET SC LETT, V292, P51, DOI 10.1016/j.epsl.2010.01.019 Aller RC, 1996, CONT SHELF RES, V16, P753, DOI 10.1016/0278-4343(95)00046-1 Arsouze T., 2009, BIOGEOSCIENCES, V6, P1 Blum AE, 1995, REV MINERAL, V31, P291 Brady PV, 1997, GEOCHIM COSMOCHIM AC, V61, P965, DOI 10.1016/S0016-7037(96)00385-7 Burton KW, 1997, NATURE, V386, P382, DOI 10.1038/386382a0 Chairat C, 2007, GEOCHIM COSMOCHIM AC, V71, P5901, DOI 10.1016/j.gca.2007.08.031 Davis AC, 2003, EARTH PLANET SC LETT, V211, P173, DOI 10.1016/S0012-821X(03)00191-2 Frank M, 2002, REV GEOPHYS, V40, DOI 10.1029/2000RG000094 Fripiat F, 2011, MAR CHEM, V123, P11, DOI 10.1016/j.marchem.2010.08.005 Gaillardet J., 2003, TREATISE GEOCHEMISTR, V5 Gherbi C, 2010, CR GEOSCI, V342, P126, DOI 10.1016/j.crte.2009.11.002 Gislason SR, 2006, GEOLOGY, V34, P49, DOI 10.1130/G22045.1 Gislason SR, 2009, EARTH PLANET SC LETT, V277, P213, DOI 10.1016/j.epsl.2008.10.018 Hatje V, 2003, ENVIRON INT, V29, P619, DOI 10.1016/S0160-4120(03)00049-7 Jeandel C., 2011, EOS T AM GEOPHYS UN, V92, P217 Jeandel C, 1998, GEOCHIM COSMOCHIM AC, V62, P2597, DOI 10.1016/S0016-7037(98)00169-0 Jickells TD, 2005, SCIENCE, V308, P67, DOI 10.1126/science.1105959 Jones MT, 2012, GEOCHIM COSMOCHIM AC, V77, P108, DOI 10.1016/j.gca.2011.10.044 Jones M.T., EARTH PLANET S UNPUB Kohler SJ, 2005, CHEM GEOL, V222, P168, DOI 10.1016/j.chemgeo.2005.07.011 Lacan F, 2001, EARTH PLANET SC LETT, V186, P497, DOI 10.1016/S0012-821X(01)00263-1 Lacan F, 2005, EARTH PLANET SC LETT, V232, P245, DOI 10.1016/j.epsl.2005.01.004 Mavromatis V., 2012, EARTH PLANET SCI LET McKee BA, 2004, CONT SHELF RES, V24, P899, DOI 10.1016/j.csr.2004.02.009 Oelkers EH, 2011, APPL GEOCHEM, V26, pS365, DOI 10.1016/j.apgeochem.2011.03.062 Oelkers EH, 2009, GEOCHIM COSMOCHIM AC, V73, P4617, DOI 10.1016/j.gca.2009.05.028 Oelkers EH, 2002, CHEM GEOL, V191, P73, DOI 10.1016/S0009-2541(02)00149-3 PALMER MR, 1989, EARTH PLANET SC LETT, V92, P11, DOI 10.1016/0012-821X(89)90017-4 PARKS GA, 1990, REV MINERAL, V23, P133 Peucker-Ehrenbrink B, 2010, GEOCHEM GEOPHY GEOSY, V11, DOI 10.1029/2009GC002869 SCHOTT J, 1995, PURE APPL CHEM, V67, P903, DOI 10.1351/pac199567060903 Schott J, 2009, REV MINERAL GEOCHEM, V70, P207, DOI 10.2138/rmg.2009.70.6 Stefansdottir MB, 2005, EARTH PLANET SC LETT, V237, P433, DOI 10.1016/j.epsl.2005.07.002 Syvitski JPM, 2005, SCIENCE, V308, P376, DOI 10.1126/science.1109454 Turekian K.K., 1968, OCEANS Vance D, 2009, NATURE, V458, P493, DOI 10.1038/nature07828 Viers J, 2009, SCI TOTAL ENVIRON, V407, P853, DOI 10.1016/j.scitotenv.2008.09.053 Walling DE, 2006, GEOMORPHOLOGY, V79, P192, DOI 10.1016/j.geomorph.2006.06.019 Wimpenny J, 2010, GEOCHIM COSMOCHIM AC, V74, P5259, DOI 10.1016/j.gca.2010.06.028 Wolff-Boenisch D, 2006, GEOCHIM COSMOCHIM AC, V70, P858, DOI 10.1016/j.gca.2005.10.016 Oelkers, Eric H. Jones, Morgan T. Pearce, Christopher R. Jeandel, Catherine Eiriksdottir, Eydis Salome Gislason, Sigurdur R. Pearce, Christopher/A-5599-2010 Pearce, Christopher/0000-0002-4382-2341 EC Marie Curie "MIN-GRO" Research and Training Network [MRTN-CT-2006-035488]; Marie Curie Intra-European Fellowship [PIEF-GA-2009-254495] We thank Jerome Gaillardet, Derek Vance, Jacques Schott, and Oleg Pokrovsky for insightful discussions and encouragement. M.T.Jones and C.R. Pearce were supported by the EC Marie Curie "MIN-GRO" Research and Training Network (MRTN-CT-2006-035488). M.T.Jones is currently supported by a Marie Curie Intra-European Fellowship (PIEF-GA-2009-254495). 1 ELSEVIER FRANCE-EDITIONS SCIENTIFIQUES MEDICALES ELSEVIER PARIS CR GEOSCIThe total mass of Material globally transported to the oceans as particulate Material is as much as 30 times greater that transported to the oceans in dissolved form. The degree to which riverine transported particles impact ocean chemistry and influence global elemental cycles depends on the reactivity of this particulate Material in seawater and the relative concentration of each element. The concentrations of elements in particulate Material relative to those of seawater range from less than 1 for soluble elements such as Na, to more than 10(7) for insoluble elements such as Al, Fe, and the Rare Earths. The reactivity of particulate Material in seawater is difficult to assess directly because this fluid is saturated or supersaturated with respect to numerous elements. As such, element release from the particulate Material is commonly matched by precipitation of secondary phases. The rates of element release can, however, be quantified by monitoring the isotopic evolution of seawater during its reaction with a variety of particulate Material samples collected from rivers throughout the world. This research focuses on the behavior of Sr and Nd, representative of the most and least soluble elements transported to the oceans. Batch experiments demonstrate that between 0.15 and 27% of Sr is liberated from volcanic and continental particulates when interacted with seawater over 6 months. Similarly, from 1.5 to 8.5% of Nd is liberated from volcanic sediments over this timespan. This observed elemental release rate from riverine particulate Material has important consequences for: (1) chemical and isotopic mass balances in the ocean; and (2) the application of the isotopic weathering proxies to the geological record. (c) 2012 Academie des sciences. Published by Elsevier Masson SAS. All rights reserved