Revisiting the dissolution of biogenic Si in marine sediments: a key term in the ocean Si budget

Frings, Patrick J.

doi:10.1007/s11631-017-0183-1

Cited by 31 publications

(40 citation statements)

References 16 publications

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“…7 and 9). Compared to the slight increases in benthic fluxes withtemperature at clay-dominated sites, the exponential trend of increased benthic fluxes with temperature for carbonate sites is related to the higher rates of silicic acid production in pore waters that are highly undersaturated with respect to biosilica.The function of bottom temperature during silica early diagenesis through influencing the undersaturation status with biogenic opal in pore water focused in this study seems to be in contrast with the results of comparable research byFrings (2017) which, based on doi.org/10.5194/os-2019-121 Preprint. Discussion started: 3 January 2020 c Author(s) 2020.…”

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confidence: 99%

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Bottom-water temperature controls on biogenic silica dissolution and recycling in surficial deep-sea sediments

Varkouhi

Wells

2020

Preprint

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Abstract. This study calculated the dissolution rates of biogenic silica deposited on the seafloor and the silicic acid benthic flux for 22 Ocean Drilling Program sites. Simple models developed for two host sediment types – detrital and carbonate – were used to explain the variability of biogenic opal dissolution and recycling under present-day low (−0.3 to 2.14 °C) bottom-water temperatures. The kinetic constants describing silicic acid release and silica saturation concentration increased systematically with increasing bottom-water temperatures. When these temperature effects were incorporated into the diagenetic models, the prediction of dissolution rates and diffusive fluxes was more robust. This demonstrates that temperature acts as a primary control that decreases the relative degree of pore-water saturation with opal while increasing the silica concentration. The correlation between the dissolution rate and benthic flux with temperature was pronounced at sites where biogenic opal is accommodated in surficial sediments mostly comprised of biogenic carbonates. This is because the dissolution of carbonates provides the alkalinity necessary for both silica dissolution and clay formation; thus strongly reducing the retarding influence of clays on opal dissolution. Conversely, the silica exchange rates were modified by presence of aluminosilicates, which led to a higher burial efficiency for opal in detrital- than in carbonate-dominated benthic layers. Though model prediction of first-order silica early transformation suggests likely effects from surface temperatures (0–4 °C) on opal-CT precipitation over short geological times (

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contrasting

confidence: 99%

“…Therefore, unsurprisingly no relationship is observed between the silica exchange rates and the warmer bottom-water temperatures. Excluding the warmer temperatures, flux-temperature diagram of Frings (2017) illustrates a good correlation between these parameters.…”

Section: Dissolution Rate and Benthic Efflux: Empirical Modelsmentioning

confidence: 80%

Bottom-water temperature controls on biogenic silica dissolution and recycling in surficial deep-sea sediments

Varkouhi

Wells

2020

Preprint

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“…Submarine groundwater discharge (SGD) was also reported as being a contributor to DSi in the coastal water of the ECS. Tan et al () estimated that the SGD‐derived DSi flux to the ECS ranged from 47 × 10 10 to 139 × 10 10 mol/year (including both terrestrial SGD and recirculated seawater), far exceeding the DSi flux discharged by Changjiang (10 × 10 10 mol year; Ding et al, ), of which the terrestrial SGD contribute only <1% of the total SGD flux in this zone (Tan et al, ), with the rest originates from the circulated seawater as well as extra DSi addition from dissolution of deposited biogenic silica (Frings, ) and Si‐bearing minerals (Fabre et al, ; Rahman et al, ) during its circulation pathways. The degree of DSi enrichment and δ 30 Si(OH) 4 alteration during this circulation process will vary with subsurface residence time and mineral type (Georg, Zhu, et al, , Georg, West, et al, ).…”

Section: Discussionmentioning

confidence: 99%

Evaluation of Silicic Acid Sources for Spring Diatom Blooms on the Continental Shelf: Insights FromStable Silicon Isotopes in the East China Sea

Zhang

Liu

et al. 2020

JGR Oceans

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The concentration of dissolved silicic acid (DSi) and its isotopic composition (δ30Si(OH)4) were determined for the East China Sea (ECS) shelf in the spring season with high spatial resolution. DSi concentrations and δ30Si(OH)4 values ranged from 1.3 to 116.5 μM and +0.85‰ to +2.53‰, respectively. An enrichment of 30Si was observed in most surface‐water samples compared with bottom waters. Several shallow‐water stations at water depths of <20 m reflected the overall control of biological utilization of DSi and regeneration of DSi from biogenic silica (BSi) on the distribution of δ30Si(OH)4 values. A seasonal difference in δ30Si(OH)4 values was observed in the euphotic zone of shelf waters, which is attributed mainly to continuous consumption of DSi in enhanced diatom blooms. The major water masses influencing the ECS shelf were characterized with distinct DSi concentrations and isotopic compositions. Using Si isotopic constraints, modeling of δ30Si(OH)4 values implied that utilization of DSi in the ECS occurred as if in a steady‐state mode. Riverine input was the major DSi source for the surface waters of inner‐shelf areas, as well as part of the middle‐ and outer‐shelf surface waters near the Changjiang River estuary. Upwelled Kuroshio Subsurface Water from the shelf break supported diatom growth in middle‐shelf surface waters. Taiwan Strait Warm Water and Kuroshio Surface Water were relatively oligotrophic, and their influence was confined to waters near the Taiwan Strait and the outer shelf and slope areas.

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“…Additionally, a comprehensive review of silicon isotope geochemistry was given by Poitrasson et al [59], covering elemental and isotopic abundances in extraterrestrial and terrestrial reservoirs, as well as the elemental and isotopic behaviors during major geological processes and relevant implications. The continental Si cycle and its impact on the ocean Si isotope budget have been well stressed by Frings et al [60]. The influence of the evolution of biosilicifying organisms on oceanic dissolved Si (i.e., DSi) inventory since the beginning of oxygenic photosynthesis and its implication for the cycling of carbon and other key nutrients in the ocean were demonstrated by Conley et al [61].…”

Section: Introductionmentioning

confidence: 99%

Silicon Isotope Geochemistry: Fractionation Linked to Silicon Complexations and Its Geological Applications

et al. 2019

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The fundamental advances in silicon isotope geochemistry have been systematically demonstrated in this work. Firstly, the continuous modifications in analytical approaches and the silicon isotope variations in major reservoirs and geological processes have been briefly introduced. Secondly, the silicon isotope fractionation linked to silicon complexation/coordination and thermodynamic conditions have been extensively stressed, including silicate minerals with variable structures and chemical compositions, silica precipitation and diagenesis, chemical weathering of crustal surface silicate rocks, biological uptake, global oceanic Si cycle, etc. Finally, the relevant geological implications for meteorites and planetary core formation, ore deposits formation, hydrothermal fluids activities, and silicon cycling in hydrosphere have been summarized. Compared to the thermodynamic isotope fractionation of silicon associated with high-temperature processes, that in low-temperature geological processes is much more significant (e.g., chemical weathering, biogenic/non-biogenic precipitation, biological uptake, adsorption, etc.). The equilibrium silicon isotope fractionation during the mantle-core differentiation resulted in the observed heavy isotope composition of the bulk silicate Earth (BSE). The equilibrium fractionation of silicon isotopes among silicate minerals are sensitive to the Si–O bond length, Si coordination numbers (CN), the polymerization degrees of silicate unites, and the electronegativity of cations in minerals. The preferential enrichment of different speciation of dissoluble Si (DSi) (e.g., silicic acid H4SiO40 (H4) and H3SiO4− (H3)) in silica precipitation and diagenesis, and chemical weathering, lead to predominately positive Si isotope signatures in continental surface waters, in which the dynamic fractionation of silicon isotope could be well described by the Rayleigh fractionation model. The role of complexation in biological fractionations of silicon isotopes is more complicated, likely involving several enzymatic processes and active transport proteins. The integrated understanding greatly strengthens the potential of δ30Si proxy for reconstructing the paleo terrestrial and oceanic environments, and exploring the meteorites and planetary core formation, as well as constraining ore deposits and hydrothermal fluid activity.

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Revisiting the dissolution of biogenic Si in marine sediments: a key term in the ocean Si budget

Cited by 31 publications

References 16 publications

Bottom-water temperature controls on biogenic silica dissolution and recycling in surficial deep-sea sediments

Bottom-water temperature controls on biogenic silica dissolution and recycling in surficial deep-sea sediments

Evaluation of Silicic Acid Sources for Spring Diatom Blooms on the Continental Shelf: Insights FromStable Silicon Isotopes in the East China Sea

Silicon Isotope Geochemistry: Fractionation Linked to Silicon Complexations and Its Geological Applications

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