Experimental investigation of the mechanism of supercritical CO₂ interaction with tight sandstone

Abstract

One of the important technologies for combating global climate change is CCUS (Carbon Capture, Utilization, and Storage), which aims to address the issue of “greenhouse effect” generated by a significant amount of greenhouse gas emissions. Supercritical CO₂, a new type of anhydrous fracturing fluid with broad application prospects in low-pressure tight sandstone gas reservoirs, has several advantages over traditional water-based fracturing fluids, including quick flowback, minimal damage to the reservoir, and the ability to realize in-situ storage of greenhouse gases. The tight sandstone cores from the Jinqiu Gas field in the Sichuan Basin were used in an experimental investigation on the interaction mechanism between supercritical CO₂ and tight sandstone to examine the viability of supercritical CO₂ fracturing with tight sandstone, and analysis of the samples’ post-reaction samples’ mineral composition, microstructure, mass change, and total salinity change. The interaction of tight sandstone with supercritical CO₂ results in an increase in quartz content, a decrease in clay mineral content, the formation of new minerals, and partial mineral dissolution on the surface of the sample. Since the degree of mineral dissolution of sandstone samples increases with time, CO₂ can be stored in tight sandstone as carbonate minerals. This study evaluates how supercritical CO₂ interacts with tight sandstone and can offer a solid theoretical foundation and experimental evidence in favor of CO₂in-situ storage in tight sandstone gas reservoir.

1 Introduction

The “greenhouse effect,” which is brought on by a significant quantity of greenhouse gas emissions, has sparked widespread worry as social economy continues to advance and global industrialisation picks up speed. The average CO₂ concentration in the atmosphere has risen to its greatest level in almost a million years since the globe started the industrialization era, and temperatures are increasing (Grainger and Smith, 2021). Both the ecosystem of the world and the advancement of human society are in grave danger. Future climate change will cause a number of chain reactions that will get worse as time goes on, including an increase in extreme weather occurrences, a rise in sea level, and the extinction of marine and terrestrial ecosystems (Zou et al., 2021). If CO₂ emissions continue to climb, the world’s temperature will rise by 2°C by the end of the century, the sea level will rise by almost 1 m, most coral reefs will vanish, 13% of terrestrial ecosystems will be lost, and many plants and animals may be in danger (Umar et al., 2022). Although the industrial age has brought about great advancement and ease, it has also led to major environmental issues and unsustainable expansion.

The Paris Climate Agreement, which proposed achieving the goal of “net zero emissions” of CO₂ around 2050, or carbon neutrality, was adopted at the 21st United Nations Climate Change Conference in order to address global climate change (Zhao et al., 2022), realize the advancement of human civilization, and ensure the sustainable development of the earth’s ecosystem (Tapia et al., 2018). As a result, countries have adopted policies that reflect the significance of lowering greenhouse gases, particularly CO₂ emissions.

The geological storage method of CO₂ is currently the best efficient way to deal with CO₂, a greenhouse gas. It involves gathering the CO₂ gas produced by fixed point sources (industrial point sources or power plants) and storing it in a reasonably closed geological structure (Hasan et al., 2015). All deep salt water bearing strata, oil and gas reservoirs, barren coal seams, and deep ocean have the perfect storage location. Their individual CO₂ storage mechanisms, however, differ as a result of the various storage sites.

Researchers proposed three pathways for CO₂ disposal in deep saline water layer in the CO₂ storage in deep saline water layer study (Wang et al., 2021). First, in a process known as dissolution landfill technology, CO₂ is directly dissolved in formation water. This approach is expected to raise the acidity of the formation water, which will increase the solubility of minerals in the parent rock because the formation water with CO₂ dissolved is already mildly acidic (Zhou et al., 2019); Second, after CO₂ injection, it directly or indirectly reacts with minerals in the formation to produce secondary carbonate minerals, which are precipitated in the form of new minerals (Zhou et al., 2018). Third, CO₂ is stored under the cover of low permeability rock in the form of gas or supercritical fluid, that is, CO₂ is loaded into “sealed tank,” which is typically referred to as liquid landfill technology (Yue et al., 2022). Mineral landfill technique is the name given to this process. This process has a good chance of success since it can solidify CO₂ into a component of solid minerals over an extended period of time.

Theoretical study and practical experience demonstrate that oil and gas reservoirs can store CO₂ for a long period because of their effective capping. The chance of CO₂ stored there leaking out is the smallest compared to other geological entities such deep salt water layers, basalt, and non-minable coal seams. Additionally, it is easier to store CO₂ and has higher economic benefits now that production wells and injection wells have been constructed in the oil and gas reservoirs. A long-term technique of storing CO₂ is in oil and gas reservoirs. One of the primary methods for storing CO₂ is to inject supercritical CO₂ into oil and gas reservoirs using oil field injection wells or production wells (Bachu, 2016). Therefore, increased oil recovery is paired with CO₂ reservoir storage as the primary method. Oil and gas reservoir storage uses CO₂ to force crude oil to flow to production wells, similar to how water drive enhance oil recovery. The main mechanism of CO₂ oil displacement involves interphase mass transfer, crude oil volume expansion, viscosity reduction, lowering of oil-gas interfacial tension, and oil-gas mixing, all of which occur during the contact between CO₂ and crude oil (Mouahid et al., 2022).

Supercritical CO₂ has been employed as a working fluid in various theoretical and experimental studies in petroleum engineering (Nikolai et al., 2019; Peng et al., 2019), and it can be used to displace oil. Supercritical CO₂ hydraulic fracturing is regarded as one of the most environmentally benign fracturing technologies since it has several benefits in reservoirs (Zhao et al., 2017; Hazarika and Boruah, 2022), particularly for water-sensitive formations (Liu et al., 2014), low pressure reservoirs, and water-stressed regions (Cao et al., 2017). Although it is well known that supercritical CO₂ has many advantages over water-based fracturing fluid, the majority of the work is still done on shale (Jiang et al., 2016; Jia et al., 2018; Memon et al., 2022). For example, the matrix minerals dissolve (Ao et al., 2017), the dissolved minerals precipitate (Chen et al., 2022), the rock breakdown pressure is lowered (Gathitu et al., 2009; Wang et al., 2018; Peng et al., 2020), the rock matrix swells (Day et al., 2008), and so on. Uncertainty exists regarding the exact mechanism of action between supercritical CO₂ and tight sandstone. Tight sandstone and supercritical CO₂ will interact physicochemically during supercritical CO₂ fracturing (Peng et al., 2016). The flow condition of subsurface oil and gas will be impacted by changes in tight sandstone’s pore characteristics, porosity, permeability, and other physical qualities (Lin et al., 2008; Lin et al., 2022). The evaluation of the mineral composition, microstructure, mass change, and total salinity change of supercritical CO₂ fracturing in low pressure tight sandstone reservoirs is therefore critical; nevertheless, there have only been a few publications in the literature up to this point.

This study examines the feasibility of fracturing supercritical CO₂ with tight, low-pressure sandstone. We investigate how tight sandstone and supercritical CO₂ interact. Different tight sandstone samples were treated with supercritical CO₂ using the tight sandstone cores from the Jinqiu Gas field in the Sichuan Basin, and the results were evaluated for changes in mineral composition, microstructure, mass change, and total salinity under various time, pressure, and temperature conditions. To further enhance the interaction mechanism between supercritical CO₂ and low pressure tight sandstone, quantify the impact of supercritical CO₂ on the mineral composition, microstructure, mass change, and total salinity of tight sandstone. This discovery evaluates the mechanism of supercritical CO₂’s interaction with tight sandstone, and it can offer a theoretical foundation and experimental support for CO₂in-situ storage in tight sandstone gas reservoirs.

2 Materials and methods

2.1 Core sample

The channel sand bodies in the Shaximiao Formation in the Sichuan Basin are found to be very developed longitudinally, widely dispersed on the plane, with good reservoir physical properties, and to have great exploration potential, according to recent comprehensive geological research on the Shaximiao Formation System. The three-dimensional carving stereogram of river sand body is shown in Figure 1 (Zhang and Yang, 2022).

FIGURE 1

The Shaximiao formation’s natural gas has the advantages of shallow burial, low cost, short cycle, and quick effect. At the moment, it is one of the important practical fields of benefit development under low oil prices, and has drawn a lot of attention. Major natural gas exploration breakthroughs have been made in Qiulin, Jinhua, Yanting, and other locations in the central and western Sichuan region. As a result, Shaximiao formation has emerged as the Sichuan Basin’s newest focus for oil and gas exploration (Zhang et al., 2022).

The reservoir temperature is 1.9–2.5°C/100 m, the reservoir depth is 1,500–2800 m, the cumulative thickness of the reservoir is 20–70 m, the reservoir porosity is mainly 8%–15%, the permeability is mainly 0.01–1.00 mD, and the pressure coefficient of the seven# sand body is only 0.47, belonging to the normal temperature and low pressure tight sandstone gas reservoir (Zheng et al., 2021).

Select a sandstone core that is underground that has a complete exterior and no visible fractures. Drill, cut, and polish the two ends with an end grinder to make sure they are parallel and smooth. The core measures 15 mm in length and 25 mm in diameter, As shown in Figure 2. The end face of the core sample must be vertical to the circumference and the maximum deviation must not be greater than 0.05 mm. The height and diameter errors of the core sample must not be greater than 0.3 mm. The core must be processed in accordance with the standards of the International Society of Rock Mechanics (ISRM) to make the sample error within the following range. The sandstone sample must be wrapped and covered with fresh-keeping film after preparation in order to shield it from air reaction during following studies.

FIGURE 2

2.2 Apparatus

As shown in Figure 3, the visualization apparatus for the interaction of supercritical CO₂ with rock consists of a CO₂ gas cylinder, a CO₂ storage tank, a cold bath, a CO₂ booster pump, a visual reactor, a heating jacket, and control systems. Visual reactor is a crucial part of the experimental system. As seen in Figure 3, the sapphire glass window in the visual reactor allows for real-time observation of the interaction process between supercritical CO₂ and rock. The visual reactor has a volume of 500 ml, the CO₂ storage tank has a volume of 5 L, the temperature range is −5°C–150°C, and the pressure bearing capability of the entire unit is 50 MPa. The flow chart of the experimental device is shown in Figure 4. By using the control system and changing the settings of the heating jacket and CO₂ booster pump, the liquid CO₂ is converted to supercritical CO₂, as shown in Figure 5, which can be used for the interaction process between supercritical CO₂ and rock at different temperatures, pressures and times.

FIGURE 3

FIGURE 4

FIGURE 5

The scanning electron microscopy apparatus is represented in Figure 6, and it is primarily made up of an electron microscope, an electron gun filament, a vacuum system, and an automated system for acquiring and processing samples and images. With a maximum magnification of ×150000 and a resolution higher than 10 nm, it can swiftly produce images with rich surface features that can be used to measure samples that are smaller than a micron or even smaller than a nanometer in size. It is used to research how supercritical CO₂ interacts with rock and to track trends in reservoir physical qualities like permeability and porosity.

FIGURE 6

Figure 7 shows an X-ray diffractometer. A high stability X-ray source, a sample and sample position orientation adjustment mechanism system, a ray detector, and a system for processing and analyzing diffraction patterns make up its core parts. Equipment specifications: A common size light tube is used as the Cu target, and a theta/theta vertical goniometer is used. The theta angle range is 2–160, and the angle accuracy is 0.0001. The X-ray needed for measurement is produced by the high stability X-ray source. The X-ray tube’s anode target material can alter the wavelength of the radiation. The intensity of the X-ray source can be changed by adjusting the anode voltage. This allows for routine phase analysis and semi-quantitative analysis of polycrystalline powder, block, and liquid samples, as well as the determination and correction of unit cell parameters, the X-ray diffraction indexation of unidentified polycrystalline samples, and the determination of grain size and crystallinity.

FIGURE 7

The flow compatibilizer, high-pressure infusion pump, sampler, chromatographic column, detector, and data processing system are the key components of the ion chromatograph, as shown in Figure 8. The chromatographic pump has a maximum operating pressure of 50 MPa, a flow rate of 0.001–20 ml/min, a minimum graduation value of 0.001 ml/min, a concentration range of 0–100% for the ion chromatograph’s eluent, an effective injection volume of 0.5–11 ml, and a measurement range of 0–15000 us/cm without section switching. The plasma concentrations of K⁺, Na⁺, Ca²⁺, Mg²⁺, Cl⁻, F⁻, and SO₄²⁻ in aqueous solution are used in a liquid chromatography method for separation and detection that uses the ionic properties of the tested substances. This method is a powerful reference for the variation characteristics and laws of ion concentration in liquid.

FIGURE 8

2.3 Methods

3 Process of supercritical CO₂ reacting with tight sandstone

When supercritical CO₂ comes into contact with sandstone at the proper temperature and pressure, it first diffuses into the rock aquifer’s pores, interacts with formation water to form a weak acidic fluid, and then reacts with the rocks to produce a series of complicated chemical reactions that lead to the decomposition of brittle minerals like carbonate and feldspar in the sandstone and the precipitation of new minerals, altering the microstructure, weight, porosity, and permeability of sandstone.

The fluid changes into a weak acidic fluid as a result of CO₂ first coming into touch with the water in the pores, followed by it dissolving in the water at the water-air interface and reacting with it to generate carbonic acid (Bierg and Banwart, 2000).The reaction formula is:

Carbonic acid quickly breaks down into bicarbonate ions:

The released hydrogen ions will result in the complexation of dissolved cations with bicarbonate ions and the disintegration of carbonate minerals and silicates in tight sandstone rocks, including:

Finally, the dissolved bicarbonate combines with cations to produce additional carbonate minerals such as calcite, magnesite, siderite, and dawsonite:

Therefore, soluble minerals in the rock are dissolved after CO₂ and tight sandstone come into contact, and new minerals are also generated, modifying the sandstone.

4 Results and discussion

4.1 Effect of supercritical CO₂ on the weight of tight sandstone

According to the formation conditions and the characteristic time stage after simulated fracturing treatment. Tight sandstone and supercritical CO₂ reaction for 48, 168, and 360 h, respectively, at 60°C under a test pressure of 10 MPa, the temperature is the formation temperature, the pressure is the difference between the minimum principal stress of the formation and the formation pore pressure, and the action time is selected as several characteristic time points after fracturing treatment. The samples of sandstone are weighed after the reaction. Table 1 shows the test results. The weight of the rocks decreases after the test. After supercritical CO₂ dissolves in water, the hydrogen ions decomposed by weak acidic fluid dissolve potassium feldspar, plagioclase and some clay minerals, resulting in rock weight changes. The weight of the tight sandstone samples reduces by 1.91% after 48 h, 2.88% after 168 h, and 4.85% after 360 h. More weight loss over time suggests that the supercritical CO₂ and rock primarily have a certain dissolving response during the experiment, and that the degree of dissolution gradually increases as time goes on.

4.2 Effect of supercritical CO₂ on microstructure of tight sandstone

Tight sandstone and supercritical CO₂ reacted at 60°C for 48 h, 168 h, and 360 h, respectively, under an experimental pressure of 10 MPa. After the reaction, sandstone samples were examined under a scanning electron microscope to reveal that after 48 h, the feldspar was only mildly corroded while the quartz and clay minerals remained comparatively stable, generating a few corrosion pits, as seen in Figure 9. As depicted in Figure 10, after 168 h of reaction, the degree of feldspar dissolution increased, quartz and clay minerals also started to undergo weak dissolution, and some deep holes developed on the visible surface; After 360 h of reaction, the feldspar’s degree of dissolution increased further, and quartz and clay minerals started to dissolve somewhat as well, resulting in a broken dissolution phenomena, as illustrated in Figure 11.

FIGURE 9

FIGURE 10

FIGURE 11

4.3 Effect of supercritical CO₂ on mineral composition of tight sandstone

When CO₂ is in a supercritical state, it reacts with tight sandstone. It initially diffuses into the tight sandstone aquifer pores at formation temperature and pressure, reacts with formation water to form weak acidic fluid, and then interacts with rocks to produce a series of intricate chemical processes.

The mineral compositions of sandstone before and after supercritical CO₂ and tight sandstone were qualitatively and quantitatively examined by XRD in order to further characterize the CO₂ water rock interaction mechanism.

In Figure 12 and Table 2, the results of the analysis and interpretation of the relative content test of mineral components of tight sandstone samples prior to the action of supercritical CO₂ are displayed. The examination of sandstone composition shows that Jinqiu tight sandstone has the highest concentrations of quartz and plagioclase, at 54.2% and 34.5%, respectively.

FIGURE 12

The tight sandstone reacts with supercritical CO₂ after 48 h, 168 h, and 360 h at 60°C under an experimental pressure of 10 MPa. The sandstone samples are analyzed by X-ray diffraction after the reaction. In Figure 13, the experimental results are displayed.

FIGURE 13

Following the experiment, the sandstone’s material composition was compared and examined. It can be seen that after 48 h of reaction with supercritical CO₂, the quartz content of Jinqiu tight sandstone increased by 1.5%, the potassium feldspar content decreased by 0.2%, the plagioclase content decreased by 1.2%, and the clay minerals content decreased by 0.4%. 0.3% of newly formed calcite was discovered at the same time. After 168 h of reaction, quartz’s content increased by 3.4%, potassium feldspar’s content dropped by 0.7%, plagioclase’s content dropped by 2.8%, the content of clay minerals dropped by 0.6%, and the content of newly formed calcite increased to 0.7%. After 360 h of reaction, there was a 5.3% increase in quartz content, a 1.1% decrease in potassium feldspar content, a 4.3% drop in plagioclase content, a 1.0% decrease in clay mineral content, and a 1.0% increase in newly created calcite content.

Generally speaking, when supercritical CO₂ interacts with Jinqiu tight sandstone, quartz content rises, potassium feldspar and plagioclase content fall, and new calcite minerals form. Thus, it is clear how the ionic reaction Ca²⁺ + CO₃^2- ⇋ CaCO₃ (calcite) in the solution and the deposition of the resulting calcite on the sample surface occur during the experiment as a result of the interaction between CO₂ and the sandstone samples. It is possible to implement the underground storage of CO₂ using material traps, as evidenced by the development of calcite, which shows that CO₂ can be stored in the solution as insoluble carbonate and precipitated as calcite and other CO₂ capture minerals.

4.4 Effect of supercritical CO₂ on solution composition

Feldspar, quartz, and other soluble minerals in the reservoir sandstone can dissolve in the acidic fluid created when CO₂ dissolves in water, creating new carbonate minerals. The formation temperature and pressure of the reservoir are simulated in accordance with the detection results of the formation water quality of the reservoir in order to further study the dissolution of feldspar, quartz, clay minerals, and other soluble minerals, combined with the change of ion concentration in the reaction solution. The production of CO₂ fluid and the interaction of water and sandstone are further discussed.

After completely soaking the dense sandstone samples, Table 3 displays the formation water data of the sha1-2 sub member of the Shaximiao Formation in the Jinqiu gas field. CaCl₂ type formation water is used. According to the salt formed by the final combination of Na⁺, Cl⁻ and other ions, the name of this kind of salt is water type. It mainly includes NaHCO₃ type, Na₂SO₄ type, MgCl₂ type and CaCl₂ type. CaCl₂ type formation water represents the water formed under the deep closed structural environment, with good sealing property, which is conducive to the accumulation and preservation of oil and gas, and is a sign of good oil and gas.

The tight sandstone reacts with supercritical CO₂ over 48 h, 168 h, and 360 h at 60°C under a test pressure of 10 MPa. Following the reaction, the water quality of the solution containing the samples of sandstone is examined and evaluated. Figure 14 displays the examination results.

FIGURE 14

In cations, the mass concentrations of K⁺, Na⁺, Ca²⁺ increased with reaction time. K⁺ mainly came from the dissolution of potassium feldspar, and the K⁺ concentration increased from 5,133 mg/L to 5,339 mg/L, an increase of 206 mg/L. Na⁺ and Ca²⁺ are mainly from the dissolution of plagioclase, indicating that the dissolution degree of potassium feldspar and plagioclase is gradually increasing. The concentration of Na⁺ increases from 6,227 mg/L to 6,401 mg/L, an increase of 174 mg/L, and the concentration of Ca²⁺ increases from 18,000 mg/L to 18,200 mg/L, an increase of 200 mg/L. The mass concentration of Mg²⁺ and Ba²⁺ changed slightly with time. The concentration of Mg²⁺ increased from 233 mg/L to 272 mg/L, increased by 39 mg/L, the concentration of Ba²⁺ increased from 1815 mg/L to 1821 mg/L, increased by 6 mg/L, and Al³⁺ also increased from nothing, but the content was low. Al³⁺ concentration increased from 0 mg/L to 12 mg/L, an increase of 12 mg/L.

In anions, a small amount of clay minerals dissolved, resulting in a slow increase in anionic Cl⁻ concentration, which increased from 51,323 mg/L to 51,569 mg/L, an increase of 246 mg/L. The mass concentration of SO₄^2- changed little, and the concentration of SO₄^2- increased from 5 mg/L to 12 mg/L, an increase of 7 mg/L. The concentrations of HCO₃⁻ and CO₃^2- in the solution first increased rapidly, and then the growth rate gradually decreased. HCO₃⁻ concentration increased from 123 mg/L to 733 mg/L, an increase of 610 mg/L. The concentration of CO₃²⁻ increased from 0 mg/L to 69 mg/L, an increase of 69 mg/L. The two reactions H₂CO₃ = H⁺ + HCO₃⁻ and HCO₃⁻ = H⁺ + CO₃²⁻ can be used to illustrate the changing process. The CO₃²⁻ is consumed by the reaction equation (HCO₃⁻ = H⁺ + CO₃²⁻), which causes the divalent cations dispersed in the solution and CO₃²⁻ to form insoluble carbonate. As the minerals dissolve, the divalent cations dissolve and produce carbonate precipitation, which slows the pace at which HCO₃⁻ and CO₃²⁻ concentrations develop in the solution.

5 Summary and conclusions

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