Pore-scale imaging of geological carbon dioxide storage under in situ conditions
Qatar Carbonates and Carbon Storage Research Centre, Department of Earth Science and Engineering, Imperial College London, London, UK
Corresponding author: M. Andrew, Qatar Carbonates and Carbon Storage Research Centre, Department of Earth Science and Engineering, South Kensington Campus, Imperial College London, London SW7 2AZ, UK. (firstname.lastname@example.org)
 While geological carbon dioxide (CO2) storage could contribute to reducing global emissions, it must be designed such that the CO2 cannot escape from the porous rock into which it is injected. An important mechanism to immobilize the CO2, preventing escape, is capillary trapping, where CO2 is stranded as disconnected pore-scale droplets (ganglia) in the rock, surrounded by water. We used X-Ray microtomography to image, at a resolution of 6.4 µm, the pore-scale arrangement and distribution of trapped CO2 clusters in a limestone. We applied high pressures and temperatures typical of a storage formation, while maintaining chemical equilibrium between the CO2, brine, and rock. Substantial amounts of CO2 were trapped, with an average saturation of 0.18. The cluster sizes obeyed a power law distribution, with an exponent of approximately −2.1, consistent with predictions from percolation theory. This work confirms that residual trapping could aid storage security in carbonate aquifers.
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 The original work on 3-D X-ray microtomography (μCT) by Flannery et al.  states in conclusion: “we believe that it will be possible to study contained systems under conditions of temperature, pressure, and environment representative of process conditions.” Since this seminal work, there has been an explosion in the use of μCT with the rapid development of bench-top scanners and huge interest in the study of porous rocks—as in the original paper—with application to hydrocarbon production and carbon dioxide storage. μCT is now the foremost method for the noninvasive imaging of rock cores at ambient conditions, applied to modeling and experimental interpretation [Berg et al., 2013; Blunt et al., 2013; Dann et al., 2011; Feali et al., 2012; Wildenschild and Sheppard, 2013]; however, imaging under conditions representative of flow and transport deep underground, including effects due to chemical equilibrium, has remained a challenge [Silin et al., 2011]. In this paper, we present the first in situ images of multiple phases in the pore space at elevated temperatures and pressures, representative of an aquifer at around 1 km depth, while maintaining mutual chemical equilibrium between the fluid phases and the rock.
 The application of this study is for geological carbon dioxide (CO2) storage, where the concern is to design injection such that the CO2 remains underground for hundreds to thousands of years. Sedimentary basins that are potentially suitable carbon storage sites include deep carbonate aquifers [Bachu, 2003]. An important mechanism that limits the spread and potential escape of CO2 is capillary trapping, where CO2, displaced by aquifer brine, is stranded as pore-scale droplets (ganglia) [Juanes et al., 2006]. Under favorable conditions, this process can, in theory, render the vast majority of the CO2 immobile [Ennis-King and Paterson, 2002; Golding et al., 2011; Qi et al., 2009]. The average amount of trapping can be measured in core flood (cm scale) experiments [Akbarabadi and Piri, 2013; Bennion and Bachu, 2010; El-Maghraby, 2013; El-Maghraby and Blunt, 2013; Okabe and Tsuchiya, 2008; Pentland et al., 2011] and has been imaged at the pore scale in a sandstone [Iglauer et al., 2011]. However, in typical deep storage sites, the CO2 will be in a supercritical (sc) phase in mutual chemical equilibrium with the host brine and the rock: dissolved CO2 forms an acid that can react with many rock minerals, including carbonates. We demonstrate that, locally, substantial quantities of scCO2 can be trapped in the pore space of the limestone studied, at representative in situ conditions where the scCO2, brine, and rock are in mutual chemical equilibrium. We demonstrate that the trapped clusters have an approximately power law distribution of size, consistent with the predictions of percolation theory assuming that CO2 is the nonwetting phase [Blunt and Scher, 1995; Dias and Wilkinson, 1986]. It is also consistent with measurements of trapping on analogue systems at ambient conditions [Iglauer et al., 2012; Iglauer et al., 2010].
2 Materials and Methods
 We imaged scCO2 and brine phases in a homogenous limestone, Ketton Oolite, from the Upper Lincolnshire Limestone Member (deposited 169–176 million years ago) using an X-ray transparent flow apparatus and the Versa XRM-500 X-Ray Microscope (www.xradia.com). Four separate experiments were conducted. For details on the experimental apparatus and procedure, please refer to the supporting information. Ketton limestone has a bimodal pore structure, with a simple, cemented bead-pack like macropores and a micritic intragranular microporous structure.
 The raw reconstructed μCT scans were filtered using a nonlocal means edge preserving filter [Buades et al., 2005; 2008] (Figures 1a–1b) to reduce noise. The images were then segmented using a seeded watershed algorithm (Figures 1c–1e), based on the 3-D gradient magnitude and grey-scale value of each voxel. This eliminates much of the voxel misidentification present in simple grey-scale segmentation, as well as the arbitrary nature of the thresholds taken. It also eliminates partial volume artefacts. All image processing was conducted within the Avizo Fire 7.0 program (Visualization Sciences Group, www.vsg3d.com).
 The separated phases were analyzed to compute the average saturation and the 3-D distribution of trapped CO2, which resides in the pore space as isolated ganglia, surrounded by brine—see Figure 2.
 The apparent porosity evaluated from the μCT image (ϕ = 0.1373) was lower than that measured using helium porosimetry (0.2337); μCT will only image pores larger than the image resolution and does not capture the microporosity within the oolite grains. From the image analysis, we compute the total number of voxels containing trapped CO2: knowing the total volume of the image, we can compute the fraction of the rock volume containing CO2—this is the capillary trapping capacity. The saturation values were found by dividing by the total porosity of the sample. The oolite grains—and hence the microporosity—remained brine-saturated throughout the experiment; CO2 was prevented from entering these regions because of its high capillary entry pressure (>0.1 MPa, from mercury injection analysis) compared to the maximum capillary pressures generated during the experiment (<0.01 MPa).
 The volume-averaged residual (trapped) CO2 saturation was 0.19 ± 0.03, representing a capillary trapping capacity of 0.045 ± 0.006: some 30–40% of the macroporosity contained trapped CO2. Similar experiments were performed on a larger cm-sized Ketton core [El-Maghraby, 2013]: averaged over five experiments, the residual saturation was 0.137 ± 0.012, with a capillary trapping capacity of 0.032 ± 0.003. While the values are comparable, we see more trapping in the microflow cell. This could be due to finite size effects and the confined flow domain that prevents the displacement of some CO2 that might be mobile in a larger system.
4 Ganglia Size Analysis
 At the pore scale, brine injection is an imbibition process, where a wetting fluid displaces a nonwetting phase. The wetting phase fills regions of the pore space in order of size, occupying the smallest pores first [Roof, 1970]. The nonwetting phase (scCO2) is trapped as a result of a percolation-like process [Dias and Wilkinson, 1986]. If this is the case, then we expect to see trapped clusters of all size with a power law distribution: the number N of clusters of volume s (measured in voxels) should scale as N(s) ~ s− τ, with an exponent τ = 2.189 [Lorenz and Ziff, 1998]. There is a lower cutoff, since we do not expect to see clusters smaller than a typical pore size, and an upper cutoff, since the trapped clusters cannot be larger than the system size. To quantify this, the distribution of pore radii was computed from a topological analysis of the pore space that identifies the largest voids [Dong and Blunt, 2009]. A typical pore radius is around 40 µm—consistent with the images shown in Figure 1—giving a lower cutoff for N(s) of around 2000 voxels.
 Figure 3 shows for the different experiments. The ganglion size distribution gives information about the dynamic processes which created the residual ganglia and also the scale range relevant to the length scale of ganglia contributing to the residual saturation. The best fit to a power law for s > 2000 is shown obtained using the maximum likelihood estimator which helps to remove biases due to a small number of very large ganglia [Clauset et al., 2009]: the exponents obtained are shown in Table 2. In these experiments, the single largest ganglion did not contribute substantially to the overall trapped volume—indeed, since τ > 2, the residual saturation was dominated by the smallest clusters (those extending over just one or a few pores). This result is consistent with other studies on sandstones [Iglauer et al., 2011], but not simplified systems such as sintered glass splinters [Georgiadis et al., 2011], where, possibly, the displacement is not a percolation-like process. Our average exponent is 2.10 ± 0.14, which is close to the theoretical value from percolation theory (2.189) and the results of pore-scale modeling for a strongly water-wet system (2.05) [Blunt and Scher, 1995]. This indicates that in the displacement process, CO2 behaves as a nonwetting phase, while the brine is the wetting phase. This confirms the conclusions of larger core floods on carbonates [El-Maghraby, 2013; El-Maghraby and Blunt, 2013], while contradicting some contact angle measurements of scCO2-brine-mineral systems that have suggested that under supercritical conditions, scCO2 may no longer be nonwetting [Espinoza and Santamarina, 2010; Jung and Wan, 2008; Kim et al., 2012; Yang et al., 2008], implying little opportunity for capillary trapping and—potentially—reduced storage security [Chaulbaud et al., 2010].
 We have used a high-pressure high-temperature apparatus to image trapped supercritical CO2 in a carbonate system with a voxel size of 6.4 µm. The experiments employed a carbon fiber core holder to maintain pressure, while remaining largely X-ray transparent. The fluids and rock were preequilibrated to preserve conditions of chemical equilibrium throughout the experiments. The trapped clusters ranged in volume over 3 orders of magnitude, with an approximately power law distribution consistent with percolation theory, leading to a large surface area for dissolution and reaction. We suggest that the CO2 acts as the nonwetting phase, with a substantial fraction of the CO2 contained as isolated ganglia suggesting, locally, good storage security.
 This technique for high-resolution in situ imaging is easily applicable to other systems, and further work could extend this apparatus to study a wide variety of multiphase flow problems in porous media at conditions of temperature and pressure and geochemical equilibrium typical of storage aquifers, oil fields, or other deep geological systems.
 We gratefully acknowledge funding from the Qatar Carbonates and Carbon Storage Research Centre (QCCSRC), provided jointly by Qatar Petroleum, Shell, and Qatar Science & Technology Park. We also thank the Imperial College Consortium on Pore-Scale Modeling for their support.
 The Editor thanks an anonymous reviewer for assisting in the evaluation of this paper.