Kaolinite dissolution and precipitation kinetics at 22°C and pH 4

Yang, Li; Steefel, Carl I.

doi:10.1016/j.gca.2007.10.011

Cited by 123 publications

(76 citation statements)

References 40 publications

(72 reference statements)

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“…For instance, the rate laws governing saponite precipitation are unknown and must be guessed through comparison with other clay minerals that differ in terms of chemistry and crystal structure (e.g., ref. 30). Moreover, order-of-magnitude differences between kinetic rate laws determined in the laboratory and observed in natural systems are a well-documented challenge for reaction-transport models.…”

Section: Model Summarymentioning

confidence: 99%

Low HesperianP_CO2constrained from in situ mineralogical analysis at Gale Crater, Mars

Bristow

Haberle

Blake

et al. 2017

Proc. Natl. Acad. Sci. U.S.A.

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Carbon dioxide is an essential atmospheric component in martian climate models that attempt to reconcile a faint young sun with planetwide evidence of liquid water in the Noachian and Early Hesperian. In this study, we use mineral and contextual sedimentary environmental data measured by the Mars Science Laboratory (MSL) Rover Curiosity to estimate the atmospheric partial pressure of CO 2 (P CO2 ) coinciding with a long-lived lake system in Gale Crater at ∼3.5 Ga.A reaction-transport model that simulates mineralogy observed within the Sheepbed member at Yellowknife Bay (YKB), by coupling mineral equilibria with carbonate precipitation kinetics and rates of sedimentation, indicates atmospheric P CO2 levels in the 10s mbar range. At such low P CO2 levels, existing climate models are unable to warm Hesperian Mars anywhere near the freezing point of water, and other gases are required to raise atmospheric pressure to prevent lake waters from being lost to the atmosphere. Thus, either lacustrine features of Gale formed in a cold environment by a mechanism yet to be determined, or the climate models still lack an essential component that would serve to elevate surface temperatures, at least locally, on Hesperian Mars. Our results also impose restrictions on the potential role of atmospheric CO 2 in inferred warmer conditions and valley network formation of the late Noachian.Hesperian Mars | martian atmosphere | Mars Science Laboratory | Gale Crater | carbon dioxide M ore than four decades of orbital imaging of Mars provide geomorphological evidence of a more active hydrological cycle and larger inventory of water during the Noachian and Early Hesperian (1, 2). The widespread distribution of hydrous clay minerals in martian terrains of this age and their subsequent demise provide pivotal supporting evidence (3, 4), but the clay mineral-bearing deposits also present a paradox in that carbonate minerals, expected coprecipitates in surficial settings in communication with a CO 2 -bearing atmosphere, are typically absent (5). Atmospheric reconstructions using carbon isotopic measurements and global inventories of martian carbon also indicate 100s mbar CO 2 levels (5, 6). This leads to the question of how the surface of ancient Mars, faintly heated by a young sun, was kept warm enough to allow an active hydrological cycle, without substantial amounts of a key greenhouse gas in the atmosphere. However, the breadth of available constraints on carbon sinks (6) and potential clay mineral formation in subsurface settings uninfluenced by the atmosphere (7) introduce uncertainties to estimates and the periods to which they apply. In this work we use mineralogical and sedimentological data from ∼3.5 Ga martian lake sediments to obtain a reference point for the evolution of martian P CO2 .During its traverse to the lower slopes of Aeolis Mons (informally known as Mt. Sharp), the MSL team documented a ∼70 m sedimentary section of mudstones, siltstones, sandstones, and conglomerates deposited by lakes and rivers on the floor of Gale c...

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Section: Model Summarymentioning

confidence: 99%

Low HesperianP_CO2constrained from in situ mineralogical analysis at Gale Crater, Mars

Bristow

Haberle

Blake

et al. 2017

Proc. Natl. Acad. Sci. U.S.A.

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“…0.019T (Smith and Ehrenberg 1989). Our simulation results showed that the (2005); Yang and Steefel (2008) chemical reaction processes at work in the reservoirs can be roughly divided into two stages. Stage 1: Fast calcite precipitation-slow analcite dissolution (Fig.…”

Section: Analcite-calcite-co 2 -H 2 O Systemmentioning

confidence: 78%

“…For this study, the specific surface areas of 2000 cm 2 /g for calcite and 1800 cm 2 /g for analcite are used. Kaolinite has a much larger specific surface area, up to approximately 10 9 10 4 cm 2 /g (Yang and Steefel 2008) (Table 1). …”

Section: Kinetic Datamentioning

confidence: 99%

Selective dissolution of eodiagenesis cements and its impact on the quality evolution of reservoirs in the Xing’anling Group, Suderte Oil Field, Hailar Basin, China

et al. 2016

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Reservoirs in the Xing'anling Group in the Suderte Oil Field, Hailar Basin exhibit ultra-low to low permeability and high tuffaceous material content. This study comprehensively analyzed diagenesis and quality evolution of these low-permeability reservoirs using thin sections, SEM samples, rock physical properties, pore water data, as well as geochemical numerical simulations. Calcite and analcite are the two main types of cements precipitated in the eodiagenetic stage at shallow burial depths in the reservoirs. These two cements occupied significant primary intergranular pores and effectively retarded deep burial compaction. Petrography textures suggest selective dissolution of massive analcite and little dissolution of calcite in the mesodiagenetic stage. Chemical calculations utilizing the Geochemist's Workbench 9.0 indicated that the equilibrium constant of the calcite leaching reaction is significantly smaller than that of the analcite leaching reaction, resulting in extensive dissolution of analcite rather than calcite in the geochemical system with both minerals present. Numerical simulations with constraints of kinetics and pore water chemistry demonstrated that the pore water in the Xing'anling group is saturated with respect to calcite, but undersaturated with analcite, leading to dissolution of large amounts of analcite and no dissolution of calcite. Significant secondary intergranular pores have formed in analcite-cemented reservoirs from selective dissolution of analcite in the mesodiagenetic stage; the analcite dissolution formed preferential flow paths in the reservoirs, which promoted feldspar dissolution; and dissolution of such minerals led to the present reservoirs with medium porosity and low permeability. Calcite-cemented tight reservoirs have not experienced extensive dissolution of cements, so they exhibit ultra-low porosity and permeability.

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“…For example, the dissolution rate R 0 varies from 5.0 × 10 −19 cm s −1 for quartz into pure water, to 2.3 × 10 −8 cm s −1 for vitreous silica into 1.0 M HF (Iler, 1979). The dissolution rate of kaolinite is on the order of ∼ 10 −15 cm s −1 (Yang and Steefel, 2008). The dissolution rate of olivine (Fo 100 ) at 25…”

Section: Timescale For Settlingmentioning

confidence: 99%

Differentiation of silicates from H2O ice in an icy body induced by ripening

Sirono

2013

Earth Planet Sp

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One of the probable scenarios of differentiation between silicate-ice in an icy object is the settling of a silicate particle in water after the melting of the object. In order for settling to proceed or occur, the size of the particle should be sufficiently large such that the settling velocity of the particle exceeds the background flow velocity induced by thermal convection. The sizes of the particles change because of dissolution and precipitation. This process is called ripening. In this study, the critical particle sizes required for settling, and the timescales for the growth of the particles to these sizes through ripening, are analytically derived. It is observed that settling is possible if the silicate particles coagulate with each other to form a network in water. If the particles do not coagulate, the probability of the occurrence of settling is low, because the time duration required for the particle growth to the critical size is large. The coagulation of silicate particles strongly depends on the pH of the water.

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Kaolinite dissolution and precipitation kinetics at 22°C and pH 4

Cited by 123 publications

References 40 publications

Low HesperianP_CO2constrained from in situ mineralogical analysis at Gale Crater, Mars

Low HesperianP_CO2constrained from in situ mineralogical analysis at Gale Crater, Mars

Selective dissolution of eodiagenesis cements and its impact on the quality evolution of reservoirs in the Xing’anling Group, Suderte Oil Field, Hailar Basin, China

Differentiation of silicates from H2O ice in an icy body induced by ripening

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Kaolinite dissolution and precipitation kinetics at 22°C and pH 4

Cited by 123 publications

References 40 publications

Low HesperianPCO2constrained from in situ mineralogical analysis at Gale Crater, Mars

Low HesperianPCO2constrained from in situ mineralogical analysis at Gale Crater, Mars

Selective dissolution of eodiagenesis cements and its impact on the quality evolution of reservoirs in the Xing’anling Group, Suderte Oil Field, Hailar Basin, China

Differentiation of silicates from H2O ice in an icy body induced by ripening

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Low HesperianP_CO2constrained from in situ mineralogical analysis at Gale Crater, Mars

Low HesperianP_CO2constrained from in situ mineralogical analysis at Gale Crater, Mars