Viscosity of Aqueous NaCl Solutions with Dissolved CO<sub>2</sub> at (30 to 60) °C and (10 to 20) MPa

Bando, Shigeru; Takemura, Fumio; Nishio, Makoto; Hihara, Eiji; Akai, Makoto

doi:10.1021/je049940f

Cited by 72 publications

(74 citation statements)

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“…However for most CO 2 -oil systems the viscosity decreases with increasing concentration of CO 2 and hence R < 0 and S > 0. The values for CO 2 -water system are estimated from Gmelin 1 and Bando et al 33 as R = 0.13, S = 0.02, which means that R is below the value for which velocity effects on the diffusion coefficient have to be taken into account. 22 Notice that ρ =ρ c=1 −ρ c=0 = ρ 0 S, which implies…”

Section: Dimensionless Form Of the Equationsmentioning

confidence: 99%

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The effect of interface movement and viscosity variation on the stability of a diffusive interface between aqueous and gaseous CO2

2013

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Carbon dioxide injected in an aquifer rises quickly to the top of the reservoir and forms a gas cap from where it diffuses into the underlying water layer. Transfer of the CO 2 to the aqueous phase below is enhanced due to the high density of the carbon dioxide containing aqueous phase. This paper investigates the behavior of the diffusive interface in an enclosed space in which initially the upper part is filled with pure carbon dioxide and the lower part with liquid. Our analysis differs from a conventional analysis as we take the movement of the diffusive interface due to mass transfer and the composition dependent viscosity in the aqueous phase into account. The same formalism can also be used to describe the situation when an oil layer is underlying the gas cap. Therefore we prefer to call the lower phase the liquid phase. In this paper we include these two effects into the stability analysis of a diffusive interface between CO 2 and a liquid in the gravity field. We identify the relevant bifurcation parameter as q = Ra, where is the width of the interface. This implies the (well known) scaling of the critical time ∼Ra −2 and wavelength ∼Ra −1 (The critical time t c and critical wavelength k c are defined as follows: σ (k) ≤ 0 ∀t ≤ t c ; equality only holds for t = t c and k = k c ). Inclusion of the interface upward movement leads to earlier destabilization of the system. Increasing viscosity for increasing CO 2 concentration stabilizes the system. The theoretical results are compared to bulk flow visual experiments using the Schlieren technique to follow finger development in aquifer sequestration of CO 2 . In the appendix, we include a detailed derivation of the dispersion relation σ (k) in the Hele-Shaw case [C. T. Tan and G. M. Homsy, Phys. Fluids 29, 3549-3556 (1986)] which is nowhere explicitly given. C 2013 AIP Publishing LLC. [http://dx

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Section: Dimensionless Form Of the Equationsmentioning

confidence: 99%

“…Those analytical solutions yield two boundary conditions at z = . The eigenvalue problem (33) and (34) is solved numerically in R 1 . We have to solve two second order equations, which means that four initial conditions are required.…”

Section: Splitting the Domain In Two Partsmentioning

confidence: 99%

The effect of interface movement and viscosity variation on the stability of a diffusive interface between aqueous and gaseous CO2

2013

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“…Subscripts m and w denote the CO 2 + water mixture and the initial water, respectively. Both viscosity [1,29] and density [9,25] are functions of the CO 2 concentration and increase with increasing carbon dioxide concentration. The pressure in both phases is the same as we ignore the capillary forces and therefore p m = p w = p. The saturated density difference between an aqueous solution of CO 2 and pure water is given by c ρ p g , where the value of the c ρ = 0.261 kg/m 3 /bar for pure water (see [21], p. 72); c ρ will be less for formation brines, because the solubility of CO 2 in water decreases with increasing salinity.…”

Section: Governing Equationsmentioning

confidence: 99%

An empirical theory for gravitationally unstable flow in porous media

et al. 2013

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In this paper, we follow a similar procedure as proposed by Koval (SPE J 3(2): [145][146][147][148][149][150][151][152][153][154] 1963) to analytically model CO 2 transfer between the overriding carbon dioxide layer and the brine layer below it. We show that a very thin diffusive layer on top separates the interface from a gravitationally unstable convective flow layer below it. Flow in the gravitationally unstable layer is described by the theory of Koval, a theory that is widely used and which describes miscible displacement as a pseudo two-phase flow problem. The pseudo two-phase flow problem provides the average concentration of CO 2 in the brine as a function of distance. We find that downstream of the diffusive layer, the solution of the convective part of the model, is a rarefaction solution that starts at the saturation corresponding to the highest value of the fractional-flow function. The model uses two free parameters, viz., a dilution factor and a gravity fingering index. A comparison of the Koval model with the horizontally averaged concentrations obtained from 2-D numerical simulations provides a correlation for the two parameters with the Rayleigh number. The obtained scaling relations can be used in numerical simulators to account for the density-driven natural convection, which cannot be currently captured because the grid cells are typically orders of magnitude

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“…An accurate experimental measurement of the flux for the actual CO 2 -brine system is difficult. For porous media, a large number of numerical studies (Ennis-King et al, 2005;Riaz et al, 2006) show that the onset time of convection is inversely proportional to the Rayleigh number, which can be expressed as, (Bando et al, 2004)  (Duan and Sun, 2003) D (Sell et al, 2012 The experimental onset times are presented in Table 2 and are compared to the theoretical relations, derived by Riaz et al (2006), Ennis-King et al (2005), Hassanzadeh et al (2007) , Xu et al (2006), Pau et al (2010) and Meulenbroek et al (2013). In order to quantify the time evolution of the flux, we describe the late time behavior when the plumes have not yet reached the bottom boundary.…”

Section: Discussionmentioning

confidence: 99%

Effect of Salinity and Pressure on the Rate of Mass Transfer in Aquifer Storage of CO2

Khosrokhavar¹,

Eftekhari²,

Farajzadeh³

et al. 2015

Proceedings

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SUMMARYThe growing concern about global warming has increased interest in improving the technology for the geological storage of CO2 in aquifers. One important aspect for aquifer storage is the rate of transfer between the overlying gas layer and the aquifer below. It is generally accepted that density driven natural convection is an important mechanism that enhances the mass Transfer rate.There is a lack of experimental work that study the transfer rate into water saturated porous medium at in-situ conditions, i.e., above critical temperatures and at pressures above 60 bar. Representative natural convection experiments require relatively large volumes (e.g., a diameter 8.5 cm and a length of 23 cm). We studied the transfer rate experimentally for both fresh water and brine (2.5, 5 and 10 w/w %). The experiment uses a high pressure ISCO pump to keep the pressure constant. A log-log plot reveals that the mass transfer rate is proportional to t^0.8, and thus much faster than the predicted by Fick's law. Moreover, the experiments show that natural convection currents are weakest in highly concentrated brine and strongest in pure water.

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Viscosity of Aqueous NaCl Solutions with Dissolved CO₂ at (30 to 60) °C and (10 to 20) MPa

Cited by 72 publications

References 10 publications

The effect of interface movement and viscosity variation on the stability of a diffusive interface between aqueous and gaseous CO2

The effect of interface movement and viscosity variation on the stability of a diffusive interface between aqueous and gaseous CO2

An empirical theory for gravitationally unstable flow in porous media

Effect of Salinity and Pressure on the Rate of Mass Transfer in Aquifer Storage of CO2

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Viscosity of Aqueous NaCl Solutions with Dissolved CO2 at (30 to 60) °C and (10 to 20) MPa

Cited by 72 publications

References 10 publications

The effect of interface movement and viscosity variation on the stability of a diffusive interface between aqueous and gaseous CO2

The effect of interface movement and viscosity variation on the stability of a diffusive interface between aqueous and gaseous CO2

An empirical theory for gravitationally unstable flow in porous media

Effect of Salinity and Pressure on the Rate of Mass Transfer in Aquifer Storage of CO2

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Viscosity of Aqueous NaCl Solutions with Dissolved CO₂ at (30 to 60) °C and (10 to 20) MPa