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State-of-the-art on Fe Precipitation in Porous Media: Hydrogeochemical Processes and Evolving Parameters

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Submitted:

11 March 2024

Posted:

14 March 2024

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Abstract
The mixing of terrestrial groundwater and seawater creates dynamic reaction zones in intertidal areas, where land-derived Fe(II) is oxidized to Fe(III) and then precipitates as Fe hydroxides at groundwater-seawater interface. These hydrogeochemical processes contribute to the formation of iron curtains beneath soil surface, which in turn influences the evolution of coastal aquifers. This paper provides a comprehensive review of physical and geochemical processes at field scale in coastal areas, explores the impact of mineral precipitation on pore structure at pore scale, and synthesizes reactive transport modeling (RTM) approaches for illustrating continuum-scale soil physio-chemical parameters during the evolution of porous media. Upon this review, knowledge gaps and research needs are identified. Additionally, challenges and opportunities are presented. Therefore, the incorporation of observational data into a comprehensive physico-mathematical model becomes imperative for capturing the pore-scale processes in porous media and their influence on groundwater flow and solute transport at large scales. Furthermore, a synergistic approach integrating pore-scale modeling and non-invasive imaging can provide detailed insights into intricate fluid-pore-solid interactions for future studies, as well as facilitate the development of regional engineering-scale models and physio-chemical coupled models with diverse applications in submarine science and engineering.
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Subject: Engineering  -   Civil Engineering

1. Introduction

Iron (Fe) is the fourth in abundance among the elements in the Earth’s crust [1], and Australia has the largest reserves of Fe ore in the world [2]. Consequently, Fe-containing minerals, such as hematite, magnetite, and goethite, are omnipresent in sedimentary rocks, weathering rinds, mine drainage, and oceanic sands [3]. Fe ions can easily find their way into local groundwater systems either naturally (e.g., rainwater infiltration) or via human activities (e.g., industrial effluent and landfill leachate) [4]. In water, Fe is typically present as divalent Fe(II) (i.e., Fe2+ ions) and trivalent Fe(III) (i.e., Fe3+ ions) [5]. As illustrated in Figure 1, when the water also contains dissolved oxygen (DO), Fe(II) is swiftly oxidized to Fe(III), which then precipitates as iron oxides beneath the soil surface. The precipitation of mineral phases can significantly affect the seepage properties of porous media [6], changing seepage parameters, including porosity, permeability, tortuosity, etc. These changes subsequently influence solute transport and chemical reactions within pore matrix. Therefore, determining the evolution of these parameters and their interdependencies is crucial in various environmental, agricultural, and industrial applications [7,8,9,10].
With a focus on coastal aquifers (see Figure 2), the mixing of fresh groundwater and seawater creates two dynamic zones: saltwater wedge (SW) and upper saline plume (USP) [11]. A confined freshwater discharge tube (FDT) between these zones intersects the beach near the low tide (LT) mark. Around this FDT, there is a geochemical transition from a reduced state to an oxygenated condition, which indicates an oxidizing environment for dissolved Fe(II) and leads to the oxidative precipitation of Fe(II) at the groundwater-seawater interface. Such zones with Fe precipitates were observed in the intertidal area of Waquoit Bay, Massachusetts, USA [12], and additional research revealed that the accumulation of these precipitates can act as a geochemical barrier to retain dissolved chemicals transported to the ocean [13,14,15,16,17]. Thenceforth, the term “iron curtain” was proposed and has since gained widespread use to describe its environmental functionalities in coastal groundwater systems. While numerous studies have focused on the response of groundwater to physical processes, such as inland hydraulic head [18,19], sea level rise [20,21], wave and tide [22,23,24,25], there has been limited attention directed toward geochemical processes associated with redox-sensitive Fe and iron curtain-like features. Despite significant research efforts providing valuable insights into Fe speciation, phosphate (PO43–) removal, and sulfate (SO42–) reduction in intertidal areas [11,17,21,26,27,28,29,30], our understanding of hydrogeochemical processes and spatiotemporal variations of the “iron curtain” remains incomplete. Additionally, the scarcity of field and experimental datasets has left many challenges to the representativeness of numerical model results. These result in a restricted comprehension of how an “iron curtain” forms and its influence on subsurface flow.
In subsurface groundwater-seawater mixing zone, such hydrogeochemical processes, i.e., reactive transport and oxidative precipitation of Fe(II), are significantly influenced by groundwater flow, solute transport, and geochemical reactions. Several parameters can dynamically respond to these processes, particularly porosity (n), permeability (k), tortuosity (τ), and specific surface area (S). Figure 3 illustrates the interactive mechanisms between the flow, transport, and reaction domains. Notably, permeability is a vital seepage property governing the reactive flow transmission through porous media [32,33]. During the oxidative precipitation of Fe(II) within pore matrix, the precipitated solid phase occupies interstitial spaces between particles, leading to a decrease in porosity, a subsequent reduction in permeability, and a corresponding increase in tortuosity at Darcy scale [34]. Moreover, Fe precipitates can reshape the surface of solid particles at pore scale, which provides direct response to the reaction rates and progress [35,36]. These changes, thereby, slow down groundwater flow and solute transport through the subsurface [37]. Through this analysis, it becomes evident that hydrogeochemical processes have the potential to induce multiple interactive mechanisms in reactive flow and transport. However, some parameters (e.g., τ and S) have often been treated as constant over time in most studies because hydrogeochemical reactions typically occur at pore scale, and Fe precipitation can modify the pore structure in multiple ways, such as narrowing existing flow channels and reducing the size of pore throats. Due to the inherent complexity and heterogeneity of pore structure, it remains difficult to couple all these effects in a precipitation-dominated regime, thereby making it challenging to achieve a representative evolution of the continuum-scale properties of porous media when the pore matrix evolves—for example, determining how permeability varies at any given instant [38,39]. To predict the variations of these parameters at continuum scale, it is essential to gain a more profound understanding of how hydrogeochemical processes control the evolution of porous matrix at pore scale.
Here, we summarized previous studies (e.g., field investigation, laboratory experiments, and numerical simulations) focused on the physical and geochemical processes in coastal aquifers. Then, we explored the impact of mineral precipitations on pore structure and provided a review of general approaches used to describe evolving parameters, including porosity, permeability, tortuosity, and specific surface area. Subsequently, we presented an outlook on opportunities to enhance modeling approaches for reactive transport through porous media. Finally, we addressed the challenges associated with bridging knowledge gaps between pore scale and continuum scale.

2. Hydrogeochemical Processes in Coastal Aquifers

The existing literature on hydrogeochemical processes in coastal aquifers was analyzed and categorized based on their applied methodology. These methodologies include (1) field investigations that study the porewater and sediment chemistry influenced by oceanic forces; (2) laboratory experiments that investigate the oxidative precipitation of Fe(II) or the interface between freshwater and seawater; and (3) numerical simulations that combine groundwater flow and solute transport in field or laboratory scale.

2.1. Field Investigations

As illustrated in Figure 4, significant research revealed the elevated concentration of dissolved Fe(II) in the streams flowing into Deception Bay (northwest end of Moreton Bay), Queensland, Australia [40]. It has been identified as a key factor contributing to the occurrence of Lynbya blooms in the nearshore [41]. Subsequent field studies on the Deception Bay catchment and Caboolture River sub-catchment discovered that the outcropping sediments contained ironstone and Fe minerals (up to 8.5%). Moreover, discrepancies in the chemical compositions of leachate and shallow groundwater indicated that the groundwater flowing through this region had another source [42,43]. Meanwhile, the report on samples from the intertidal area off Sandstone Point, Queensland, Australia, showed that the soil had an acidic pH level ranging from 4.6 to 5.2 at a depth of 0.2 m, and it was highly acidic with a pH below 3.4 at depths between 1 m and 1.2 m [42,44]. These findings indicate the presence of acid sulfate soils (ASS), which are widespread in the coastal regions of Queensland. As illustrated in Figure 2, when these soils undergo hydromechanically disturbances, such as in agriculture and construction, the exposed sulfides react with oxygen in the air to form sulfuric acid, which leads to the decomposition of Fe minerals [43], and the subsequent release of Fe(II) into groundwater systems [4]. As a result, soil samples from the top layer (up to 0.3 m) contained a moderate content of extractable Fe, with levels reaching 91 mg/kg, while the groundwater had a high Fe(II) concentration of up to 1.6 mg/L. This implies that significant amounts of fresh groundwater through the soil at depth delivered Fe(II) to the neighboring intertidal area of Deception Bay [44]. Furthermore, detailed measurements of Fe(II) concentrations obtained by incubating sediment cores from northern Deception Bay provided evidence of the benthic release of Fe(II) at the sediment-seawater interface in an intertidal area [45]. In comparison, on the east side of Moreton Bay, field measurements of porewater salinity and DO profiles on the west coast of Moreton Island (Mulgumpin) presented a conceptual model of the coastal unconfined aquifer (CUA) driven by oceanic oscillations, particularly tides and waves [23,46]. The results revealed significant geochemical zonations that strongly influenced the fate and distribution of reactive chemicals at the groundwater-seawater interface, as well as their subsequent discharge to coastal waters. Furthermore, chemical analysis of porewater samples from an offshore site of Eastern Banks in North Stradbroke Island (Minjerribah) indicated that dissolved Fe in groundwater primarily existed in the form of Fe(II), and it also demonstrated the presence of a higher Fe(II) concentration compared to that in seawater [47]. As a supplement, an in-depth assessment of phosphorus (P) cycling in the sediments of Peel-Harvey Estuary, Western Australia, suggested that P was adsorbed onto micro-scale enrichments of Fe(III) oxyhydroxide due to Fe redox chemistry [48].
On a global scale shown in Figure 4, zones with Fe precipitation or Fe-oxides-coated sand have been discovered in many field-based studies. For instance, in the tidal freshwater marshes of Chickahomiy River in Virginia, USA [49], and on the beaches of the North Sea, Germany [50]. Sediment cores collected from the intertidal zone of Waquoit Bay, Massachusetts, USA, revealed Fe-oxides-coated sand with dark red-yellow and orange colors [12]. In addition, porewater samples extracted from this area showed a high concentration of dissolved Fe(II), and more than 95% of the total Fe were in ferrous form, which could be traced to the Fe(II) in the submarine groundwater. Subsequently, the findings from the study of Patos Lagoon Barrie, Brazil, indicated that phosphate was immobilized as a result of Fe precipitation, and there was also an enrichment of Fe in coastal surface waters [51,52]. Moreover, porewater and sediment samples from the freshwater discharge zone of the Indian River Lagoon in Florida, USA, substantiated the Fe release into surface waters along coastlines [21]. Additionally, McAllister et al. [53] observed that seasonal variations in freshwater gradients induced the iron curtain to contract and expand at Cape Shores, Lewes, Delaware. Specifically, the iron curtain moves toward the ocean in summer and toward land in winter. Sawyer et al. [54] summarized that the configuration of an “iron curtain” could be significantly influenced by hydrodynamic variability across several timescales related to waves, tides, storms, sea-level rise, seasons, annual precipitation patterns, and climate change. Furthermore, Trezzi et al. [30] observed that Fe ions in groundwater underwent chemical reactions upon contact with seawater in the Mediterranean. Also, chemical analysis of dissolved Fe in beach porewaters on Spiekeroog Island, Germany, provided further evidence that Fe oxides formed in the transition zone between anaerobic freshwater and aerobic seawater [15,28]. Meanwhile, intensive measurements of nutrient content at Tolo Harbour, Hong Kong, China, successfully captured the temporal variation of nutrients at a sandy beach. The results exhibited the absorption of PO43- onto Fe oxides in the deep transition zone [55]. Subsequently, the field study conducted on the Baltic Sea unraveled that the physio-chemical variables could be modified as a result of Fe precipitation and PO43- adsorption. This resulted in the formation of an iron curtain, serving as a temporal sink for P in coastal sediments [56].

2.2. Laboratory Experiments

Since the 1990s, research into Fe transformation in aqueous systems has begun to receive much attention. Organic substances, e.g., dissolved organic matter (DOM) or dissolved organic carbon (DOC), have been reported to accelerate, retard, or have no effect on the rate of Fe(II) oxidation under a variety of pH and DO conditions [57,58,59]. Rose and Waite [60,61] initially constructed a kinetic model to describe the redox cycling of Fe in seawater. This model specifically focused on the oxidation of Fe(II) in the presence and absence of natural organic substances obtained from Moreton Bay, Australia. The experimental results showed that the processes of Fe oxidation and precipitation were mainly accelerated by DO concentration and were significantly influenced by the presence of DOM. Furthermore, the hydrolysis of Fe(III) rapidly occurred in seawater, and the corresponding solid precipitates were initially labile. Subsequently, the research by Spiteri et al. [13] illustrated how pH and redox transitions determined the geochemical zonations in the intertidal area. These zonations had a substantial impact on the distribution of metals, as well as their discharge into the ocean. Further research by Garg et al. [62] investigated the effect of water pH on pathways that contributed to Fe transformation in freshwater systems with natural organic matter (NOM). The findings revealed that the Fe(II) oxidation rate was controlled by its interaction with DO. The steady state of Fe(II) concentrations was greatly affected by pH changes, whereas the Fe(II) concentration in surface waters may not be significantly impacted.
In addition to such studies concerning chemical reactions, flow tank or sand flume experiments (see Figure 5a) are commonly employed to investigate pathways and mechanisms under various predetermined forcing circumstances, such as different tidal ranges and net groundwater flow rates. For example, with a focus on the effects of saltwater diffusion zone and tidal fluctuation, a laboratory-scale investigation on the contaminant transport was conducted in a flow tank (1.65 m long, 0.6 m high, and 0.1 m wide) with glass beads, which served as a porous media in a CUA [63]. Their results indicated that the contaminant source traveled seaward with groundwater flow and exited as a concentrated plume in a restricted discharge area at the simulated coastline. The saltwater interface substantially affected the migration pattern of contaminant plumes. In recent years, a combination of sand flume (3.5 m long, 0.8 m high, and 0.02 m wide) experiments and field-scale numerical simulation was successfully conducted to investigate porewater dynamics across the aquifer-ocean interface in response to tidal fluctuations and different inland hydraulic heads [64]. One of the new findings was that tides can create shallow circulations and enhance density-driven circulations, thereby increasing the seasonal exchange of aquifer-sea porewater under varying inland freshwater input. Subsequently, a further experiment was undertaken in conjunction with laboratory-scale modeling to study the combined impact of inland groundwater and tidal oscillations on the subsurface flow of a coastal reservoir and adjacent aquifer. The findings revealed a considerable impact of tides on porewater exchange between the reservoir and aquifer. The resulting increase in density-driven flow and tide-induced flow was identified as the major source of solutes in the coastal reservoir [65]. Nevertheless, there is still a limited availability of such laboratory research that specifically investigates hydrogeochemical processes in coastal aquifers.
Instead, column experiments (see Figure 5b) are typically utilized to explore the migration of certain compounds in a particular substrate [66]. A wide range of applications can be implemented to effectively tackle more specialized research issues. For example, the impact of varying water tables on redox conditions [67], preferential flow affecting solute transport [68], pharmaceutical substance transport under saturated conditions [69], pesticides leaching under unsaturated conditions [70], the remediation of acidic mine drainage [71], or the mobility of nanoparticles for soil remediation [72]. The basic concept of a column experiment is to pump water containing a desired solute through a column filled with substrates of interest. Such column tests generally employ three experimental setups: (a) a column with a downward flow to replicate percolation across unsaturated zones [73], (b) a column with an upward flow to simulate saturated conditions [69], and (c) a series of columns to analyze the changes of hydrochemical parameters along the flow path [74]. In published studies, columns are often built of stainless steel to avoid solute interactions [75,76,77], acrylic glass for better visualization of wetting front and dye tracer migration [78,79,80], and other materials such as aluminium [81], glass [82], polyvinyl chloride (PVC) [83] and polyethylene [84]. Although the slenderness ratio (i.e., height to diameter) has a profound impact on hydraulic conditions and solute transport in the column, broad research has reported a wide range of column dimensions, with heights ranging from 0.5 m [85] to 2.4 m [86], and diameters from 0.02 m [85] to 0.36 m [84]. However, Lewis and Sjöstrom [87] suggested an appropriate ratio of 4.0 to minimize scaling effects. Additionally, peristaltic pumps are widely used in researching fluid transport in saturated columns due to their ability to provide uniform flow rates [88,89,90], and other pumps include syringe pumps [91], pulsating pumps [92], piston pumps [93], gear pumps [75] and suction pumps [94]. Furthermore, a wide variety of substrates have been reported as column infill, e.g., site-specific aquifer sediment [75], natural or artificial soils [88,95], model quartz sand [96], and Fe-coated sand [79].

2.3. Numerical Simulations

Conducting field-scale tests is challenging because of restricted access to the groundwater-seawater interface and spatiotemporal scale, both of which are required to observe an in-situ iron curtain. Hence, numerical models offer an efficient way to quantify the hydrogeochemical process of Fe(II) and its driving mechanisms in real-world scenarios. For example, by implementing a simple reaction network in a one-dimensional (1-D) reactive transport model (RTM) (see Figure 6a), Spiteri et al. [13] discovered that the pH gradient instead of the DO gradient was the primary factor influencing the oxidative precipitation of land-derived Fe(II) in the mixing zone, and determining the location and the amount of Fe oxides in Waquoit Bay, USA. Later, based on a two-dimensional (2-D) RTM (Figure 6b) coupled groundwater flow and biogeochemical reactions, the findings further indicated an important link between the accumulation of Fe oxides and the binding of P compounds [97]. Coincidentally, Pham et al. [98] successfully calculated the precipitation rate throughout a pH range that could be predicted in laboratory conditions. This study concluded that the kinetics of water exchange may govern the kinetics of Fe precipitation. Subsequently, Roy et al. [21] developed an RTM to study the diagenesis of Fe linked to DOC under field conditions in Florida, USA, and the findings revealed that the dissolution of Fe was influenced by both the evolving reactivity of DOC and the reduced velocity of groundwater flow as the distance from the shore increased. Furthermore, by integrating SEAWAT and PHT3D programs, Anwar et al. [26] numerically studied the formation of Fe(OH)3 in an intertidal zone and presented the accumulation of Fe(OH)3 over a simulation period of 300 days. However, the spatial distribution along the SW did not stabilize, and the amount of Fe(OH)3 did not reach a quasi-steady state after 300 days. Additionally, Zhang et al. [99] combined field investigations and three-dimensional (3-D) numerical modeling to analyze how alongshore morphology impacted nearshore porewater flow and chemical input to the coastal sea. However, the use of 3-D models (Figure 6c) is still rare in published studies to date. Recently, Wang et al. [100] employed TOUGHREACT to investigate the formation and distribution of iron curtains due to freshwater-seawater mixing. Their results indicated that Fe(OH)3 tended to accumulate on the freshwater side of the mixing zone, which extended from surface layers to deeper layers. The amount of Fe(OH)3 was influenced by the groundwater flux and the ratio of DO to Fe(II) concentrations.

3. Impact of Fe Precipitation on Pore Structure

3.1. Evolution of Pore Structure at Pore Scale

The oxidative precipitation of Fe(II) can modify the pore structure of porous media, thereby influencing the connectivity between pores. Under such a precipitation process, Figure 7 provides a visual representation illustrating the evolution of a porous media at pore scale. The initial pore structure has three different zones: (a), (b), and (c). Zone (a) is significant because of its good connectivity, which serves as a key channel for fluid and solute transport. Zone (b) shows a tortuous pathway for advection and diffusion. Zone (c) is defined by large pores with restricted connections to the major channel. With a focus on the regime dominated by precipitation, Fe precipitation can (1) reduce the size of pore throats, (2) clog the initial pore space, and (3) increase the solid surface area, henceforth increasing hydraulic energy loss by friction between seeping fluid and surface of soil particles. In any of these scenarios, the accumulation of Fe precipitates at pore scale has a major impact on the seepage properties of porous media at continuum scale.
With the utilization of non-invasive imaging techniques, it has become a reality to visualize the pore structure with high resolutions, which provides an in-depth insight into the complex nature of porous media. Werth et al. [101] summarized the pros and cons of four non-invasive imaging techniques, including optical imaging using UV or visible light, dual-energy gamma radiation, X-ray microtomography, and magnetic resonance imaging (MRI). In particular, the X-ray approach was recommended in the field of hydrogeology and geochemistry because of its great resolution and flexibility for the three-dimensional (3-D) characterization of natural porous media. Theoretically, it is possible to numerically investigate reactive transport and develop predictive models based on 2-D or 3-D images of pore geometry. Figure 8a illustrates a 3-D micro-computed tomography (micro-CT) image of a sample porous media with interconnected pores, facilitating the construction of a pore network model (PNM) by representing pores as spheres and pore throats as cylinders [102]. An analysis of the PNM indicates that the fluid flow through this media is considerably affected by the size of pores, the width of the pore throats, and the connection between pores. The decrease in pore size and pore throats, as well as limited connectivity in three dimensions, suggests a high value of tortuosity, which makes both advective and diffusive transport challenging.
Furthermore, a recent study by Zhao et al. [103] provided several images of Fe-oxide-coated sand samples under scanning electron microscope (SEM) and optic microscopes. Figure 8b exhibits the alternations in pore space caused by Fe precipitation in sand, where Fe precipitates can either increase the size of existing particles or form new structures. Based on such observations, Fe precipitation has a minor effect on the connectivity between pores if precipitated Fe coats particles without clogging pore throats. However, accumulated precipitation can reshape existing pathways for seepage flow and solute transport, thereby leading to changes in tortuosity and permeability. Additionally, the reaction rates of oxidation and precipitation processes are generally controlled by surface area, which is determined by several factors, such as particle size [104], surface roughness, and the presence of imperfections or etch-pits [105]. Also, fluid dynamics can result in the formation of extra reactive zones, which could be the explanation for the observed discrepancies between reactive and geometric surface areas [34]. Consequently, the combination of these factors determines the effective surface area during hydrogeochemical processes [106]. However, any of these factors can temporally evolve as porous matrix undergoes chemical reactions.

3.2. Distribution of Precipitation in Pore Matrix

Given the considerable effect of Fe precipitation on the evolution of porous media, it is crucial to highlight the relationships between flow transport rates and chemical reaction processes within porous matrix. Numerous studies indicate that the relationships can be characterized by Péclet (Pe) number and Damköhler (Da) number, which determines the transport regime based on timescales of advection, diffusion, and reaction. Pe number reveals the significance of advective and diffusive transport [107], while Da number reflects the relationship between reaction rate and transport rate [108]. They are defined as follows:
P e = a d v e c t i v e   t r a n s p o r t   r a t e d i f f u s i v e   t r a n s p o r t   r a t e = ν L D
D a = r e a c t i o n   r a t e a d v e c t i v e   o r   d i f f u s i v e   t r a n s p o r t   r a t e
where v is the flow velocity, L is the characteristic length of porous media, and D is the diffusion coefficient.
The precipitation of solid-phase minerals (e.g., Fe oxides) can cause an extreme case of pore-clogging, which changes the groundwater flow and solute transport through porous media. Hence, it is of significance to understand how hydrogeochemical reactions influence transport properties and to include the evolution of these parameters in modeling studies. Kang et al. [109] numerically studied the impact of Pe and diffusive Da numbers on mineral precipitation and the resulting decrease in permeability. The simulation results revealed that Da determined the time duration to clog the pore space when Pe was kept constant at a high value. Increasing Da (with a constant Pe) led to a more concentrated precipitation zone and more efficient pore-clogging near the inlet, whereas increasing Pe (with a constant Da) yields a wider precipitation front, requiring more time and reactants to clog all the pores. It was concluded that the combination of moderate Da (3.24 < Da < 32.4) and small Pe numbers (Pe < 0.628) can contribute to rapid pore-clogging, resulting in impermeable pore structures even with a small amount of precipitation. Further research by Tartakovsky et al. [110,111] presented consistent findings on mixing-induced precipitation with various solutes. Precipitation occurred throughout porous media in the case of high Pe (Pe > 6) and low Da numbers (Da < 0.4), while precipitation formed along the main flow pathway (i.e., dendrite-like pattern) in the case of low Pe (Pe < 1) and high Da numbers (Da > 17). Besides, low Pe (Pe < 1) and high Da (Da > 17) numbers led to localized precipitation near the inlet, resulting in rapid pore-clogging and a substantial reduction in flow rates. In summary, high Da numbers (Da > 17) produce a narrow precipitation zone near the inlet where reactants contact, whereas low Da numbers (Da < 0.4) cause a wide zone due to diffusion dominance. While these studies provided a detailed insight into the coupling of physical and geochemical processes, it is difficult to predict the temporal changes of transport parameters because they are determined by the spatial distribution of precipitates rather than their total amount, particularly in the pore-clogging case.
A few studies indicated other factors influencing the distribution of mineral precipitation. For example, Chagneau et al. [8] studied celestite precipitation in a diffusion-reaction cell and observed that precipitates primarily presented in large pores as a result of the differential transport of anions and cations. Further research has shown that spatial heterogeneities play an important role in determining how precipitation is distributed, subsequently governing the evolution of continuum-scale parameters, such as tortuosity, permeability, and reactivity of porous media [112,113]. Additionally, Rajyaguru et al. [114] compared the precipitation patterns between barite and gypsum in chalk samples, and micro-CT images revealed that barite precipitation showed a thin continuous disk, while gypsum precipitation appeared as large isolated spheres. Moreover, barite had a more profound effect on diffusivity despite a comparable 2% decrease in total porosity when compared to gypsum. The outcome suggested that barite precipitated through uniform and non-uniform nucleation, while the precipitation pattern of gypsum was dominated by heterogeneities of the local pore structure. These experiments highlighted that even when the flow and solute transport were only subject to diffusion, mineral precipitation in pore structures remained highly complicated.

4. Parameterization of Evolving Porous Media

4.1. Evolution of Porosity at REV Scale

A porous media has significant heterogeneity at multiple scales. Statistically, the concept of a representative elementary volume (REV) can be utilized to determine stable packing conditions (such as void ratio and porosity) in a matrix of solid particles and void spaces. According to Figure 9, the porosity at REV scale is defined as
n = V v V t = V w V s + V w
where Vt is the total volume of porous media, Vv is the void volume, which equals the water volume Vw under fully saturated conditions, and Vs is the volume of solid particles.
Even though the concept of total porosity is straightforward, it is difficult to obtain the value of n directly. Some laboratory methods can be used to achieve the accurate n. Using the volumetric saturation method, Missimer and Lopez [115] investigated a total of 100 well-sorted beach and dune sands and conducted five separate measurements to evaluate the accuracy. The results revealed that the standard deviation for this method approached 0.004 (viz., ±0.4%). In addition, 91 out of 100 samples were within the highest allowable error of ±3%, and the average deviation was ±0.064%, proving that the volumetric saturation method is quite reliable.
During the oxidative precipitation of Fe(II) in porous media, solid-phase Fe occupies void spaces and reduces the porosity. The change in porosity can be derived by considering the volume fraction of Fe precipitates in a porous matrix. It is expressed as
n = n 0 − φ i
where n0 is the initial porosity, and φi is the volume fraction of the mineral i.
As a result, the temporal evolution of porosity can be calculated by defining the mass balance equations for reactive minerals [116].
d n d t = − d φ i d t = − V i R i
where Vi is the molar volume fraction of the mineral i, and Ri is the precipitation rate of the mineral i.

4.2. Permeability-Porosity Relationships

Permeability is a REV-scale seepage property that reflects the ability of fluid to transport through porous media [32,33]. As illustrated in Figure 10, the intrinsic permeability k can be calculated using Darcy’s law (see Equation (6)), which quantifies a linear relationship between discharge rate and hydraulic gradient in a porous-media-filled column during constant laminar flow [117]:
k = Q A · ∆ L ∆ h · μ ρ g
where Q is the volume flux, A is the cross-sectional area, ΔL is the length between inlet and outlet, Δh is the height difference between inlet and outlet, µ is the fluid viscosity, ρ is the fluid density, and g is the gravitational acceleration.
Based on factors such as void ratio, saturation, and heterogeneities, the permeability of geomaterials greatly varies, ranging from coarse to very fine-grained soils by up to ten orders of magnitude. The statistics reveal that the k values of clean sand range from 10–9 to 10–12 m2, while marine clay has a k range of 10–16 to 10–19 m2 [118]. Accurate permeability can be determined by analyzing pore geometry obtained from pore-scale imaging, which is regarded as the only reliable way [36]. However, most studies have employed seepage tests to investigate permeability under various conditions [119]. For example, Sandoval et al. [120] studied the measuring accuracies of constant-head and falling-head methods and found that the constant-head method is more effective for distinguishing the permeabilities of different materials.
From a theoretical perspective, a wide range of equations have been proposed and validated for estimating permeability in many types of soil [121,122], which enables permeability to be predicted based on experimentally obtained parameters such as particle size and porosity. One of the early attempts is the Hazen–Williams (H–W) equation (see Equation (7)), which was established in the 1890s and remains a significant empirical relationship in America and the Middle East. This equation is frequently used to calculate the pressure drop of water flow within a pipe. Additionally, it finds application in predicting the permeability of uniform sand, provided that the uniformity coefficient is below 5.0 and the effective particle size ranges from 0.1 mm to 3 mm [123]. In other cases, it presents substantial discrepancies as this equation is only valid for water [124].
k = c H d 10 2
where d10 is the effective particle diameter that represents the 10% of particles smaller than this size, and cH is a coefficient from 1 to 1000 [125].
One of the most renowned equations is the Kozeny–Carman (K–C) equation, which was initially proposed by Kozeny in 1927 and later modified by Carman in 1937. The equation facilitates the estimation of permeability of porous media, such as homogeneously packed glass beads, sand, and gravel, through porosity and effective diameter [119,126]. Typically, it is expressed as follows:
k = c k n 3 1 − n 2 d 10 2
where ck is a shape factor ranging from 180 to 270 (e.g., 180 corresponding to perfectly spherical particles) [127].
Extensive research indicated that the K–C equation provided accurate results for coarse soils when d10 is less than 3 mm. However, it can not be reliably applied to clay soils [128]. Additionally, the research by Pomès et al. [129] suggested the disparity between the permeability predicted by the K–C equation and that obtained from volume averaging can increase with the injection rate. Mostaghimi et al. [130] also demonstrated that the K–C equation can lead to considerable overestimation of permeability for heterogeneous or poorly connected porous media.
Furthermore, there are several semi-analytical equations, such as the Terzaghi equation (see Equation (9)), the Breyer equation (see Equation (10)), and the Slitcher equation (see Equation (11)).
k = 0.0084 n − 0.13 1 − n 1 / 3 2 d 10 2
k = 0.06 l o g 500 C u d 10 2
k = n 3.287 d 10 2
where Cu is the uniformity coefficient defined as the ratio of d60 to d10.
In the Terzaghi equation, the particular value of 0.0084 represents a classification coefficient from 0.0061 to 0.00107. Although the applicability of the Breyer equation is limited by specific porosities, it is considered most useful for granular materials with heterogeneous distributions and poorly sorted grains, particularly when Cu ranges from 1 to 20, and d10 is from 0.06–0.6 mm [131]. Moreover, Marschalko et al. [132] demonstrated a good agreement between the permeability calculated by the Slitcher equation and that obtained from the constant head method for various sand. This equation is most suitable when soil particles are uniformly distributed within a range of 0.01–5 mm in particle size [133].
When the pore matrix evolves with the oxidative precipitation of Fe(II), it becomes challenging to determine how its permeability varies at any given instant during this hydrogeochemical process [38,39]. Under such conditions, seepage flow and solute transport are not only dependent on changes in permeability and porosity but also affected by changes in other parameters related to pore geometry, such as tortuosity and specific surface area [37,134].

4.3. Tortuosity-Porosity Relationships

Due to the complex pore space morphology, the flow channel often has a longer length than a straight pathway between the source and destination [135]. Hence, Carman [136] proposed the concept of tortuosity to match the estimated permeability with the experimental data. As illustrated in Figure 11, tortuosity is defined as the ratio of the effective length of a flow channel (Le) to the straight-line distance (Ls) through a porous media:
τ = L e L s
However, it is frequently used as a variable in practical applications [137], suggesting a lack of understanding of its physical characteristics. Consequently, multiple forms of tortuosity have been identified and utilized in the literature on porous media. For instance, the tortuosity was defined as Ls/Le, which is the inverse of Equation (12) [138]. Bear [139] introduced tortuosity as (Ls/Le)2, the square of the inversed Equation (12), while Holzer et al. [140] documented it as (Le/Ls)2, the square of Equation (12). Precisely, the concept of tortuosity shall be restricted to its geometric meaning related to flow channels. For this purpose, this study adopts Equation (12).
Koponen et al. [141] used a lattice-gas approach to model the tortuosity of incompressible fluid flow in a 2-D porous media with a critical porosity of 0.33 (nt = 0.33). Upon this, Equation (13) was proposed to define tortuosity as a function of porosity:
τ = 1 + 0.65 1 − n n − n t 0.19
Subsequently, Mota et al. [142] presented a semi-analytical relationship between tortuosity and porosity, particularly for spherical particles:
τ = n − β
where β is an exponent to be determined experimentally or numerically. The proposed value was 0.4, while Millington and Quirk [143] suggested 4/3 for saturated soils.
Another popular equation is a logarithmic function of porosity, given as:
τ = 1 − P l n n
where P is a constant with specific values, e.g., 0.49 for highly porous beds [144], 0.41 for monosized and polydisperse spheres [145], and 0.77 for laminar fluid flow in 2-D porous media consisting of freely overlapping solid squares [146].
In addition, Li and Yu [147] also developed a tortuosity model for flow paths in a Sierpinski Carpet, a pore fractal model composed of particles of various sizes and uniform pores. The model takes the form:
τ = 19 18 l n n / l n 8 / 9
Meanwhile, Ahmadi et al. [148] provided an analytical derivation of tortuosity for monosized spheres using a volume-averaging method:
τ = 2 n 3 1 − B 1 − n 2 / 3 + 1 3
where B is a fixed value of 1.209 for cubic packings, while 1.108 for tetrahedral, and Equation (17) becomes infinite when n reaches 0.248 and 0.143, respectively.
Figure 12 compares tortuosity predictions as a porosity function based on Equations (13)–(17) for saturated porous media. Under theoretical conditions, tortuosity is 1 when porosity is 1, and it approaches infinite when porosity is zero. It can be observed that tortuosities obtained from these equations yield 1.0 for a porosity of 1.0, and all display similar results for porosities over 0.4, except for Equation (14). However, they exhibit substantial differences for porosities lower than 0.3. In particular, for porosities below 0.1, the calculated tortuosities can differ by several orders of magnitude. This implies that these tortuosity–porosity relationships are unique to porous materials and may become invalid as the pores approach complete clogging. The fact could be that these studies started with an initial porosity and tortuosity specific to investigated materials and relied on semi-theoretical laws to estimate how tortuosity temporally evolved using early-time data. As a result, reasonable agreements with observational data were achieved by specifying different fitting factors or exponents. Furthermore, these relationships indicate that various materials can be influenced in distinct ways, which is mainly linked to their original pore structure. A porous media with high initial tortuosity and narrow pore throats is more sensitive to the impact of precipitation processes, as observed in both experimental and numerical studies [34].
Moreover, in a solute-mixing-induced precipitation regime, hydrodynamic dispersion typically has a more significant effect than molecular diffusion when the fluid travels through porous media at a low velocity (e.g., v < 1.0×10–5 m/s). In such cases, pore geometry can play a dramatic role. Specifically, tortuosity can decelerate the solute spreading, while dispersion can elongate the solute band in the flow direction. As a consequence of materials and conditions, it is not straightforward to illustrate the evolving tortuosity as a function of changing porosity. Additionally, obtaining a more accurate representation of changes in diffusion and dispersion presents challenges in reproducing observed mineral precipitation patterns. Thus, recent research proposed an effective diffusion D* to represent these combined effects [149,150]. It is calculated using a linear dispersion model:
D * = τ − 1 D 1 + α L D v
where D is the molecular diffusion coefficient, and αL is the lateral dispersion coefficient.

4.4. Evolving Reactivity and Surface Area

Characterizing the evolving reactivity in porous media is also important when porous media evolves, and reactivity is often quantified based on the surface area. The simplest assumption is that mineral precipitates uniformly coat solid particles. Hence, the specific surface area of a spherical particle (see Figure 13) is only related to its radius r:
S = 4 π r 2 4 3 π r 3 = 3 r
As a result, a power-law function can be developed to describe how surface area changes with the volume fraction of solid-phase minerals. The mineral dissolution-precipitation reactions are defined as surface-controlled reactions:
S = S 0 φ i t φ i 0 w
where S0 is a reference surface area, φ i 0 and φ i t define the volume fraction of mineral i at the initial stage (t = 0) and the instant time t, respectively, w is a fitting exponent. Steefel and Lichtner [151] proposed a constant value of 2/3, which was validated by subsequent research conducted by Xie et al. [152]. However, Andreani et al. [153] and Luhmann et al. [154] specified a value of 1 to accurately match the breakthrough curves in their experiments, which was supported by recent hydrogeochemical simulations by Pavuluri et al. [149].
However, later minerals precipitating on the surface of earlier minerals can cause surface passivation by heterogeneous nucleation [155]. Thenceforth, the reactivity of earlier minerals is related to the volume fraction of later minerals [34]. Therefore, Jeen et al. [156] employed an exponential model to illustrate the evolving reactivity of Fe in a permeable reactive barrier, and the results showed an improved agreement with observed data compared to that predicted by Equation (20).
S = S 0 e x p − a φ i
where a is an empirical constant linking Fe reactivity loss to mineral accumulation.
Moreover, Noiriel et al. [36] investigated the evolving surface area during carbonate precipitation through a combination of imaging techniques, Brunauer-Emmett-Teller (BET) analysis, and numerical modeling. The study showed that the local increase in surface area due to mineral precipitation notably influenced mineral concentrations. The corresponding model with a constant surface area failed to match the observed data, indicating the importance of accounting for the changes in surface area throughout precipitation processes. Further research has also revealed that mineralogical heterogeneity and surface area change significantly impacted the overall reactivity of rocks and the release of solutes [157,158].

5. Approach for Reactive Transport Modelling

In recent decades, subsurface processes, including groundwater flow, solute transport, and geochemical reactions, have been extensively studied using Reactive Transport Modelling (RTM). According to Li et al. [159], the RTM approach allows for coupling physical and geochemical processes in spatiotemporal scales, bridging the fields of hydrogeology and geochemistry in porous media. As described in Figure 14, reactive transport in such porous media can be characterized using three distinct models: pore-scale, continuum-scale, and hybrid-scale that integrates pore and continuum scales.
As a conventional approach, the continuum model (see Figure 14c) considers porous media as an averaged REV, and the pore structure is characterized by REVs [139]. Upon this approach, a few software solutions have been developed to address reactive transport within the pore matrix at REV scale [160], which includes MIN3P [161], TOUGHREACT [162], HP1 [163], CrunchFlow [116], and PFlotran [164]. In these solutions, the equations describing fluid flow and mass transport are formulated using REV averages and coupled with geochemical reactions [116]. Henceforth, Darcy’s Law is frequently used to simulate the groundwater flow, and advection-diffusion-reaction (ADR) equations are used to model the transport of dissolved solutes in groundwater. Furthermore, geochemical processes such as Fe precipitation can have an effect on the flow field and REV-scale properties (e.g., tortuosity, permeability, and specific surface area) by reducing pore space [165]. As a result, changes in these parameters are typically considered constant or presented as a function of porosity in response to hydrogeochemical reactions. For example, most research works at continuum scale utilize Equations (8), (14), and (20) to define the relationships between porosity and evolving parameters [152]. However, the combination of advection, molecular diffusion, hydrodynamic dispersion, and geochemical reactions can produce high heterogeneity. Equations containing empirical constants are difficult to accurately present the combined effects, as these constants often lack a robust theoretical foundation and typically remain unchanged with the progress of hydrochemical processes [166]. Additionally, the REV-averaging method assumes the disregard of fluctuations in governing variables, making it unable to identify those areas in a computational domain when the continuum model is inadequate [167]. To overcome these difficulties, numerous recent studies have focused on using high computational resources to develop numerical models at pore scale [168,169,170,171].
In pore-scale models described in Figure 14a, each point in the pore space is occupied by either a fluid or solid phase [150], and the fluid-mineral interface moves with the surface reaction of mineral precipitation [172]. So far, pore-scale models have proven to be a mature tool for studying flow patterns, and the evolution of hydraulic properties during biogeochemical processes in the pores has also been simulated. For example, Liu et al. [173] and Yan et al. [174] conducted pore-scale simulations to investigate how porous media heterogeneity affected immiscible fluid displacement patterns. Xie et al. [168] developed an improved pore-scale model that incorporated viscous coupling to improve the prediction of relative permeability. Dashtian et al. [169] performed a pore-scale study on reactive transport in porous materials, and demonstrated the impact of Pe and Da number on dissolution and porosity. Molins et al. [175] conducted a pioneering study that focused on a first-order kinetic reaction between a single solute and a single mineral. The results demonstrated the capability of existing models to accurately predict mineral dissolution at the pore scale. Among these pore-scale models, a wide range of particle tracking approaches have been implemented, in addition to the Lattice Boltzmann method (LBM) (see Figure 15), and the smoothed particle hydrodynamics (SPH) method [175]. These methods typically necessitate high computational resources with parallel computation to accelerate pore-scale modeling and simulations. However, the continuum-scale concept is not directly applicable at pore scale. Therefore, REV-scale properties can be acquired from an average of pore-scale simulation results if the domain is sufficiently large to achieve a REV size [176]. To date, the majority of research in this field has been focused on solving the Navier-Stokes equations in single and two-phase flow conditions to calculate seepage properties [177,178]. Nevertheless, further efforts are still needed to improve and validate pore-scale modeling of multiphase solutions reacting with multiple minerals within heterogeneous pore networks [150].
Although the oxidative precipitation of Fe(II) occurs at the pore scale, the oxidation and precipitation processes have distinct time and length scales. Specifically, the oxidation of Fe(II) to Fe(III) is nearly instantaneous in an aqueous environment, while the formation of Fe precipitates is at significantly different rates. Consequently, the evolving porous media exhibits a variety of spatial scales in response to hydrogeochemical processes. To the author’s knowledge, continuum-scale models employ homogenizing flow, averaged parameters at a REV scale, and empirical equations based on specific experiments. Therefore, uncertainties may present when applying these to other cases. In contrast, pore-scale models have been proven reliable in providing accurate predictions of coupled physical-geochemical processes in the pore space and enhancing an in-depth understanding of continuum-scale transport properties by allowing variations in the parameters of pore structure. However, they require substantial computational resources and are typically applicable to computational domains smaller than 0.1 m. To address these concerns, hybrid-scale models have been suggested by combining pore-scale modeling for specific areas with continuum-scale modeling for others (see Figure 14b). Based on a root-finding method coupling the pore and continuum scales, such models comprise domain decomposition, selection and execution of different governing equations for each subdomain, and continuity verification at the interface of sub-domains [179]. On one hand, they do not require extra parameters except for REV-scale properties of porous media, physio-chemical properties of specified fluid and solute, as well as pore geometry. On the other hand, they succeed in addressing highly localized heterogeneities, providing a high level of accuracy in representing physics at the pore scale. Furthermore, these models have been valuable in distinguishing microscale features that are smaller than the resolution of imaging systems in image-based simulations [180,181]. The benchmarks by Pavuluri et al. [149] presented a groundbreaking study that demonstrates the feasibility of hybrid-scale modeling for 2-D advective-diffusive systems with complex interactions of geochemical reactions and porosity on permeability.

6. Knowledge Gaps and Research Needs

Hydrogeochemical reactions in porous media, such as the oxidative precipitation of Fe(II) commonly observed in Australia, can induce substantial changes in pore structure and dramatically alter soil properties in various natural and engineered systems. RTM is a valuable approach for analyzing these coupled nonlinear effects. Yet, achieving an accurate illustration of phenomena like iron curtains necessitates an in-depth comprehension of their dynamics and kinetics at the pore scale. Over the past three decades, pore-scale imaging has seen dramatic improvements, enabling the visualization of detailed pore geometry and its response to chemical reactions. Additionally, pore-scale simulations using 3-D images offer valuable datasets to enhance our comprehension of how a porous media evolves under multiple mineral reactions. Despite these significant research efforts, there are still major limitations regarding the pore-clogging phenomenon. Therefore, the following knowledge gaps and research needs were identified:
(1) Driving mechanism for Fe transformation in coastal groundwater systems
The conceptual model of CUA systems has been in existence for 20 years, with the FDT recognized as an important pathway for delivering land-derived chemicals (e.g., N, P, Fe, and DOM) to nearshore environments [11]. This potentially contributes to coastal pollution, as Lyngbya blooms were reported in many parts of Queensland, Australia [41], which threatens coral populations and marine ecosystems. To date, most research efforts have been devoted to addressing physical processes in intertidal areas, with little emphasis on their coupling with geochemical processes (e.g., oxidative precipitation of Fe(II)). As these processes are of the utmost importance for indicating the role of FDT in determining the chemical speciation and solubility of elements along the flow path, it is essential to conduct field measurements of these coupling processes together and subsequently combine these collected data with field-scale RTM for calibration and validation, which may require a strong multi-disciplinary background in hydrogeology and geochemistry. Furthermore, many field studies employ the methodology of transient distributions of physio-chemical variables and chemical concentrations in the intertidal area, which may result in uncertainties regarding the effects of historical conditions. Note that coastal geochemical zonations are affected by present oceanic forces and chemical behaviors and are regulated by historic driving mechanisms. Despite the challenge of acquiring initial and past conditions in the field, there is a pressing need to include temporal effects by collecting field data over more extended monitoring periods. Upon such investigation, the outcomes may assist in establishing a useful database and a unique opportunity to unravel the driving mechanisms behind Lyngbya blooms and their link with Fe(II) in coastal waters, as well as iron curtains and their environmental functionalities in coastal aquifers.
(2) Physico-mathematical model linking porosity, tortuosity, and permeability
Multiple interactive mechanisms have indicated intrinsic correlations between seepage properties and porosity. When the pore matrix evolves with the oxidative precipitation of Fe(II), solid-phase precipitation can slowly reshape the pore structure and reduce the pore volume. Such change in porosity can decrease permeability and increase tortuosity, thereby slowing down groundwater flow and solute transport through porous media [37]. However, the relationships between these parameters are commonly considered independent [141], and empirical relationships (such as the best-known K–C equation) have proven valuable in interpreting observational data under unique evolving conditions. Due to hydrogeochemical reactions at the pore scale and the non-uniform distribution of minerals in pore space, these equations are inadequate for physically representing these pore-scale processes. In addition, it is not practical to rely on these equations for a process-oriented evaluation of experimental data. Taking the K–C equation as an example, its ability to predict the evolution of porosity, tortuosity, and permeability is restricted in a precipitation-dominated regime. First, its derivation was intended for a solid media with hydraulic conduits rather than natural geomaterials [34]. Second, the consideration of geometric tortuosity is not completely resolved when it evolves with porosity changes [141]. Third, it remains uncertain whether the shape factor, with its relatively wide range, is suitable for predicting the permeability of evolving porous media [158]. Because of these limitations in addressing the evolution of porous media corresponding to hydrogeochemical processes [134,182], there is an urgent need to develop a theoretical model for accurately characterizing the permeability–tortuosity–porosity relationship in a form that is both straightforward and geophysically meaningful.
(3) Integrated numerical approach for complete pore-clogging phenomena
The accumulation of Fe precipitation can induce complete pore-clogging in porous media, leading to a porosity value of zero and a complete disappearance of the aqueous phase. Such extreme cases are challenging to resolve in numerical simulations because most RTM codes set a specific porosity threshold value, below which fluid flow and solute transport are assumed not to exist [34]. In the published literature, Xie et al. [152] successfully implemented the K–C equation and Archie’s Law to address clogging-dominated problems associated with mineral dissolution-precipitation using RTM codes CrunchFlow, HP1, Pflotran and TOUGHREACT, in which groundwater flow and reactive transport are sequentially solved. Such decoupled treatment demands minimal steps to prevent any mass balance errors at each time step. Furthermore, Pavuluri et al. [149] and Soulaine et al. [150] developed a coupled OpenFOAM-PHREEQC platform to model hydrogeochemical processes in evolving porous media at both pore-scale and Darcy-scale. Simulation results were compared with those obtained from MIN3P and TOUGHREACT, demonstrating the feasibility of combining multiphase flow and reactive transport with evolving porosity through a hybrid-scale method.
Simulations of cement carbonation clogging revealed a failure to replicate the outcomes observed experimentally, highlighting the necessity for a more integrated approach to refine evolving parameters [34]. Although accurate mathematical models for such phenomena are yet to be determined, it is reasonable that a methodology based on porosity alone is inadequate for fully capturing the complexities of processes occurring at both pore and continuum scales. Alternatively, it may be more appropriate to consider the surface area at pore scale. On one hand, there exists an inherent correlation between reactivity and surface area, with the latter dictating how solid particles interact with the fluid and solute [178]. On the other hand, Saripalli et al. [183] have revealed that a higher surface area results in more tortuous pathways with reduced transport properties. These factors emphasize the importance of integrating surface area onto models, rather than depending on porosity alone, to achieve improved agreement between simulation results and experimental findings.
(4) Opportunities associated with non-invasive imaging techniques
In the last decade, non-invasive imaging techniques such as micro-CT and SEM have provided detailed images of pore structures without invading samples, which allows researchers to capture the intricate details of pore networks in various materials. With high-performance computing (HPC) resources, these images can serve as valuable input data for pore-scale modeling and simulation studies and can be analyzed to extract quantitative information about pore size distribution, pore connectivity, tortuosity, and other important parameters that influence fluid flow and transport processes. For example, Blunt et al. [102] illustrated the potential of pore-scale modeling based on the PNM derived from micro-CT images. Pereira Nunes et al. [184] introduced a particle-based approach for simulating the dissolution of carbonate at pore scale using micro-CT image voxels. Roslin et al. [185] implemented micro-CT and SEM techniques for structure analysis and permeability estimation of coal samples. Wang et al. [186] conducted steady-state multiphase flow experiments on continuum-scale samples with a pore-scale resolution using micro-CT. The insights gained from these studies not only contribute to a scientific understanding of porous media at the pore scale but also provide practical solutions for addressing limitations in the continuum scale, particularly when applied to evolving porous media [34]. However, present imaging techniques lack the resolution needed to adequately visualize the pore structure of fine-grained materials, particularly clays and cement with nanometric pores. Moreover, hydrogeochemical processes in porous media occur at small scales (nm~μm), while engineered RTMs are generally at large scales (m~km). As a result, continuum approaches remain promising for engineering applications in the study of groundwater flow and solute transport. Shortly, a strategy integrating micro-scale imaging and hybrid-scale modeling will offer high-resolution insights into pore-scale processes in porous media.
In conclusion, the oxidative precipitation of Fe(II) can indeed trigger multiple interactive mechanisms at the pore scale, which in turn increases the interdependencies of parameters governing groundwater flow and solute transport at the continuum scale. This complexity highlights the importance of constraining a physico-mathematical model that effectively links porosity, tortuosity, and permeability while incorporating observational data from both field and laboratory studies. Such an integrated model can facilitate predictive capabilities of the behavior of porous media under different conditions, and this is essential for researchers and engineers to make informed decisions in various applications ranging from environmental remediation to subsurface energy resource management. Through this literature review, hydrogeochemical processes in coastal aquifers revealed the spatiotemporal variability of these systems corresponding to oceanic oscillations and geochemical transitions at the field scale. The subsequent analysis of Fe(II) precipitation within pore matrix provided an instructive review of how hydrogeochemical reactions at pore scale govern the evolution of porous media. It illustrated the challenges of parametrizing evolving porous media at continuum scale. RTM can act as a valuable tool for bridging the gap between local observations and regional-scale phenomena, so that it enables the extrapolation of specific and discrete measurements onto large scales. Nevertheless, combining the pore-scale modeling approach with non-invasive imaging techniques has offered a powerful and versatile strategy for studying the processes in porous media. This synergistic approach can provide detailed insights into complicated fluid-pore-solid interactions for future studies, as well as facilitate the development of regional engineering-scale models and physio-chemical coupled models with diverse applications in science and engineering, particularly in disciplines involving complex systems like porous media, fluid dynamics, and environmental science.

Author Contributions

Conceptualization, W.C. and G.Y.; methodology, W.C., A.S. and H.H.; formal analysis, W.C. and G.Y.; writing—original draft preparation, W.C.; writing—review and editing, G.Y., H.H. and A.S.; visualization, W.C. and G.Y.; supervision, A.S. and H.H; project administration, A.S. All authors have read and agreed to the published version of the manuscript.

Funding

This research was funded by the Australian Research Council through its Discovery Project (grant number: DP190103782).

Institutional Review Board Statement

Not applicable.

Informed Consent Statement

Not applicable.

Data Availability Statement

The original contributions presented in the study are included in the article. Further inquiries can be directed to the corresponding author.

Acknowledgments

The authors thank the School of Civil Engineering, the School of the Environment, and the Center for Advanced Imaging at the University of Queensland for their support and the reviewers and editor for constructive comments on this paper.

Conflicts of Interest

The authors declare no conflicts of interest.

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Figure 1. An overview of the mechanisms of Fe(II) oxidative precipitation, as well as the impact of precipitated Fe on porous media.
Figure 1. An overview of the mechanisms of Fe(II) oxidative precipitation, as well as the impact of precipitated Fe on porous media.
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Figure 2. Conceptual model illustrating the hydrological and geochemical processes in the intertidal area [31]. The colored areas indicate different geochemical zonations, and black dashed arrows represent groundwater flow. In between the saltwater wedge (SW) and the upper saline plume (USP) lies a freshwater discharge tube (FDT).
Figure 2. Conceptual model illustrating the hydrological and geochemical processes in the intertidal area [31]. The colored areas indicate different geochemical zonations, and black dashed arrows represent groundwater flow. In between the saltwater wedge (SW) and the upper saline plume (USP) lies a freshwater discharge tube (FDT).
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Figure 3. Schematic diagram illustrating the interactive mechanisms between the flow, transport, and reaction domains, where n is porosity, S is specific surface area, k is permeability, h is hydraulic head, τ is tortuosity, q is volumetric flow rate, c is molar concentration.
Figure 3. Schematic diagram illustrating the interactive mechanisms between the flow, transport, and reaction domains, where n is porosity, S is specific surface area, k is permeability, h is hydraulic head, τ is tortuosity, q is volumetric flow rate, c is molar concentration.
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Figure 4. Illustration of representative field investigation in Australia and worldwide. The red rectangles outline significant research related to Fe speciation and Fe oxides in Australia, with the majority focused on Deception Bay (northwest end of Moreton Bay), Queensland, Australia. The purple rectangles list important field studies in the USA, Germany, China and Brazil, with a focus on intertidal zones with Fe precipitation or Fe-oxides-coated sand.
Figure 4. Illustration of representative field investigation in Australia and worldwide. The red rectangles outline significant research related to Fe speciation and Fe oxides in Australia, with the majority focused on Deception Bay (northwest end of Moreton Bay), Queensland, Australia. The purple rectangles list important field studies in the USA, Germany, China and Brazil, with a focus on intertidal zones with Fe precipitation or Fe-oxides-coated sand.
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Figure 5. Schematic illustration of (a) sand flume and (b) sand column. A sand flume test can be used to investigate pathways and mechanisms under various predetermined forcing circumstances, such as different tidal ranges and net groundwater flow rates, while a sand column test can be typically utilized to explore the migration of certain compounds in a particular substrate. .
Figure 5. Schematic illustration of (a) sand flume and (b) sand column. A sand flume test can be used to investigate pathways and mechanisms under various predetermined forcing circumstances, such as different tidal ranges and net groundwater flow rates, while a sand column test can be typically utilized to explore the migration of certain compounds in a particular substrate. .
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Figure 6. Illustration of numerical simulations using (a) 1-D model, (b) 2-D model, and (c) 3-D model. The 1-D model features a simple reaction network along the flow path. The 2-D model can be utilized to investigate groundwater flow and biogeochemical reactions in the cross-shore direction of intertidal areas. Meanwhile, the 3-D model is suitable for investigating the variation of groundwater flow and solute transport in the alongshore direction of coastal aquifers. .
Figure 6. Illustration of numerical simulations using (a) 1-D model, (b) 2-D model, and (c) 3-D model. The 1-D model features a simple reaction network along the flow path. The 2-D model can be utilized to investigate groundwater flow and biogeochemical reactions in the cross-shore direction of intertidal areas. Meanwhile, the 3-D model is suitable for investigating the variation of groundwater flow and solute transport in the alongshore direction of coastal aquifers. .
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Figure 7. Schematic illustration of the effect of precipitation process on pore structure. Brown area represents solid particles (e.g., quartz sand), while green coatings are solid-phase precipitation.
Figure 7. Schematic illustration of the effect of precipitation process on pore structure. Brown area represents solid particles (e.g., quartz sand), while green coatings are solid-phase precipitation.
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Figure 8. a) 3-D micro-CT image of solid particles, and (b) SEM image of sand grains and pore space changes due to Fe precipitation.
Figure 8. a) 3-D micro-CT image of solid particles, and (b) SEM image of sand grains and pore space changes due to Fe precipitation.
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Figure 9. Phase relationship diagram in a cross section of REV-scale porous media, where Vt is the total volume, Vv is the void volume, which equals the water volume Vw under fully saturated conditions, and Vs is the volume of solid particles and precipiated minerals.
Figure 9. Phase relationship diagram in a cross section of REV-scale porous media, where Vt is the total volume, Vv is the void volume, which equals the water volume Vw under fully saturated conditions, and Vs is the volume of solid particles and precipiated minerals.
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Figure 10. Diagram of seepage test using a constant-head approach, where the Marriot bottle maintains a constant hydraulic head Δh, allowing for the measurement of water passing through the porous media (total length ΔL) within a specific time interval t.
Figure 10. Diagram of seepage test using a constant-head approach, where the Marriot bottle maintains a constant hydraulic head Δh, allowing for the measurement of water passing through the porous media (total length ΔL) within a specific time interval t.
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Figure 11. Schematic illustrating the concept of tortuosity in a REV, where Le is the effective length of a flow channel, and Ls is the straight-line distance through a porous media. Note that grey circles represent solid particles in the graphical representation.
Figure 11. Schematic illustrating the concept of tortuosity in a REV, where Le is the effective length of a flow channel, and Ls is the straight-line distance through a porous media. Note that grey circles represent solid particles in the graphical representation.
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Figure 12. Comparison of predicted tortuosity as a function of porosity using Equations (13)–(17).
Figure 12. Comparison of predicted tortuosity as a function of porosity using Equations (13)–(17).
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Figure 13. Diagram illustrating the surface area and volume of an idealized spherical particle, where r is the radius of the particle, and Δr is the increase in radius as a result of Fe precipitation uniformly coating the solid particle.
Figure 13. Diagram illustrating the surface area and volume of an idealized spherical particle, where r is the radius of the particle, and Δr is the increase in radius as a result of Fe precipitation uniformly coating the solid particle.
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Figure 14. a) pore-scale approach for which porosity is completely addressed. The grey area indicates solid particles, while the orange area indicates pore space. (b) hybrid-scale approach that manages the solid and porous areas in a framework, (c) continuum-scale approach for all REVs with a mixture of fluid and solid.
Figure 14. a) pore-scale approach for which porosity is completely addressed. The grey area indicates solid particles, while the orange area indicates pore space. (b) hybrid-scale approach that manages the solid and porous areas in a framework, (c) continuum-scale approach for all REVs with a mixture of fluid and solid.
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Figure 15. A demonstration of CFD using LBM coupled with DEM: (a) CFD carried out using LBM and (b) soil particle package set inside a REV using DEM.
Figure 15. A demonstration of CFD using LBM coupled with DEM: (a) CFD carried out using LBM and (b) soil particle package set inside a REV using DEM.
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