# Exploring the Occurrence of Clogging in Highly Permeable Coarse Soils of Dam Foundations

Authors: Jianquan Ma; Hao Peng; Shibo Li; Zhao Duan; Xinshe Zhang; Donghe Ma
Journal: Advances in Civil Engineering
 (2020)

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## Abstract

Leakage through the permeable coarse soils of dam foundations in Tibet, China, lessened over time without any additional antiseepage measures. In fact, clogging generated during the infiltration process is recognized as the major factor in reducing leakage. A laboratory study was conducted to understand clogging in highly permeable coarse soil of a dam foundation with the primary aim of determining the clogging patterns and optimum clogging particle size (PS). Seven replicate experiments were constructed using soil media with PS ranges of 32–64 mm, 16–32 mm, 8–16 mm, 4–8 mm, 2–4 mm, 1-2 mm, and 0.5–1 mm to observe clogging after feeding the soil media with sediments of different PSs. The experimental results showed that four clogging patterns were formed in different PSs of the coarse foundation soil. The ratio of the effective aperture of the soilDea and the equivalent clogging particle size dede/Dea had a dominant effect on the four clogging patterns (surface clogging, de/Dea>1; surface-internal clogging, 0.5<de/Dea≤1; internal partial pore blockage, 0.25<de/Dea≤0.5; and unclogging, de/Dea≤0.25). The assessment criterion of the optimum clogging pattern was determined by 0.5<de/Dea≤1, and from that, the optimum clogging PS do was calculated.


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## Body

## 1. Introduction

Leakage is a major safety issue that influences the economic value of dams and threatens dam stability [1–4]. It was reported that the sediments of the reservoir dam foundation in Shannan, located in the south of Tibet Province, China, were deep and overlain by coarse-grained soils originating from glacial deposits and characterized by physical weathering and high permeability [5, 6], creating a risk of leakage [7, 8]. Due to continuing seepage and erosion of the dam’s foundation, the flow rate in the soil foundation increased gradually. This increased the seepage through the dam foundation and caused concentrated erosion of the fine-grained material at the soil interface with the dam foundation, finally leading to failure of the dam’s foundation [9, 10]. A decades-long survey of five reservoirs (Daranduo Reservoir, Jiangxiong Reservoir, Jiaripu Reservoir, Qiongguo Reservoir, and Awoduo Reservoir, as shown in Figure 1(a)) in the Shannan area found that the state of leakage in the dam foundations at these sites lessened with time without any additional antiseepage measures [11–13]. The reason for this phenomenon was verified under seepage conditions in the dam foundation and was attributed to fine soil particles that were transported and retained in the pores, thus reducing leakage [6]. Therefore, placing fine sediments into foundation soil pores can serve as a recovery technology approach for leakage in foundation soil, similar to using geomembranes, as an effective method of clogging.Figure 1
The study site, located on Shannan of Tibet, China. (a) Five typical water reservoirs with leakage in strong infiltrating coarse soil of dam foundation. (b) Location of sample selected and Yarlung Zangbo Jiang river system. (c) Location for sampling site. (d) Status of field soil sediments of the sample.Sedimentation of fine particles can influence the permeability of soil [14], which has been verified in soil filters in geotechnical engineering. By preventing the erosion of base soils and building up pore pressure, clogging provided an effective method to obtain internal stability [9, 15]. It is evident from research in porous media that physical clogging may be more likely to occur under constant head conditions than under constant flow rates [16], similar to the highly permeable coarse soils of the dam foundations in Qiongguo reservoir and Jiangxiong reservoir [12]. The study on the permeability and mechanical properties of saturated cohesionless soil by laboratory tests shows that hydraulic gradient would drop and flow velocity would increase under long-term infiltration and large amounts of fine particles are eroded away, which finally caused the reduction of the soil strength at the major stage of drained shearing [7, 17].In surveys of clogging events in the disciplines of environmental engineering, geotechnical engineering, and biological engineering, clogging particles were mostly fine particles, such as sandy-silt [18], suspended solids [19–22], clay [23], or even colloid deposits [24]. For filter media, particle size includes two types: fine media, such as sandy loam [25], fine sand [26, 27], compost, and peat [19]; and coarse media, such as sand or mulch soil [20, 21] and even gravel beds [28, 29]. Unfortunately, highly permeable dam foundation media are always nonuniform and contain larger-sized particles, such as boulders, pebbles, or gravel deposits, which differ from the aforementioned filter media. In high constant head conditions, the clogging particles are always gravelly sands; silt, clay, or suspended solids could not clog or be trapped in the pores of the particles [12]. McIsaac and Rowe [30] have found that significant differences exist in permeability because of the difference in the media particle size and even found a hydraulic conductivity that was twice as high in a coarse gravel bed (38 mm) as in a 19 mm gravel. In particular, in coarse soil of spreading gradation as our study media, different particle size distributions will determine different suitable equivalent particle sizes, which affect clogging and permeability performance [31]. In addition, the hydraulic characteristics of soil media are very sensitive to the soil media particle size [32].Schälchli [33] indicated that flow conditions, such as the hydraulic conductivity of the soil filter, the shape, and size of suspended particles, the hydraulic gradient of the seepage flow, and the concentrations of suspended solids, have a dominant influence on physical clogging. Both sediment grains and suspended particles can cause clogging. The evolution of hydraulic characteristics over time and a reduction in permeability are evidence of clogging [34, 35]. The experimental observation shows that the hydraulic gradient is the most influential parameter in the clogging of sands and gravels [36]. Therefore, this article focuses on the changes to hydraulic characteristics (hydraulic gradient and flow velocity) caused by clogging and the influence of particle size (both of clogging sediments and soil media) on clogging. We also focus on building a relationship in clogging behavior, filter media particle size, and incoming particle size. A series of laboratory physical clogging experiments were conducted for this study.


## 2. Experimental Works

### 2.1. Materials

The materials used in this study were natural materials similar to the real dam foundation media obtained upstream of Zhuo Yu Gou in the middle of the Qiongguo and Jiangxiong Reservoirs, Shannan, Tibet (Figure1). The materials were divided into two parts, soil media (as skeleton particles in the experiments) and incoming sediments (the particles added in the column to checking clogging or not in the experiments). To assess the impact of particle size on clogging, the particle size distributions (PSDs) of all the materials are in accordance with the Udden-Wentworth scale [37, 38].In the research of foundation leakage in Shannan, the dam foundation soil mainly included boulders, pebbles, gravel, and sand and contained cohesive soil, rounded but poorly sorted with particle sizes mainly larger than 0.5 mm [5, 39]. In this study, the soil media particle size (PS) was sieved into 32–64 mm, 16–32 mm, 8–16 mm, 4–8 mm, 2–4 mm, 1-2 mm, and 0.5–1 mm ranges. Similar to particle migration and erosion processes, these media cover a range of gravel and sand sizes [40]. The dry density and porosity of the soil media and the PSs of the incoming sediments are shown in Table 1. To obtain soils that were inert to each other, all soil particles were sieved by soaking in water.Table 1
Basic properties of soil media and corresponding PSs of incoming sediment.
Incoming PS (mm)Dry density (ρd/g/cm3)Porosity (ns)Soil media PS (mm)32–6416–328–164–82–41–20.5–14–81.630.326T1T82–41.630.310T2T9T151–21.650.290T3T10T16T210.5–11.660.307T4T11T17T22T260.25–0.51.690.347T5T12T18T23T27T300.125–0.251.730.332T6T13T19T24T28T31T330.063–0.1251.790.341T7T14T20T25T29T32T34Note. Ti denotes the experiments’ serial number of different incoming sediments in different soil media PSs.


### 2.2. Experimental Apparatus

For the purpose of the experimental works, a special infiltration-clogging monitoring system was built. The infiltration-clogging monitoring system comprised four parts: sample column, feeding column connected to a feeding pipe, monitoring equipment, and water supply tank with circulation function. Both the sample column and feeding column were 500 mm in height and 370 mm in diameter and made of Plexiglas (Figure1). As recommended for seepage studies in coarse-particle soils [41], the ratio of the sample column diameter to the soil media particle diameter was more than 5 to 6, appropriate for media particles smaller than 64 mm. Hydraulic head distributions along the soil media were measured by pore water pressure sensors, which were connected to a computer and laterally buried to the sample column. To avoid a preferential flow path between the soil and the Plexiglas cell wall, the monitoring point of hydraulic head change was selected at the center of the sample.From the feeding pipe, incoming sediments filled in, and the damping plates in the feeding column ensured even distribution of the incoming particles. Reddi et al. [42] and Alem et al. [16] indicated that clogging appeared to be greater under the condition of a constant head than under a constant flow rate. During the operation period, a submersible pump was used to continuously supply water to the constant head controller using a pressure tank and to circulate water in the water supply tank. In the experiment, a 6 m water head was provided by a pressure tank and was stabilized by the top sensor. Figure 2 shows a schematic and photograph of the system.Figure 2
Infiltration-clogging monitor system. (a) Schematic diagram. (b) Photograph.
(a)(b)


### 2.3. Experimental Procedure and Data Analysis

After placing the fully compacted soil media layer by layer, the sample column was checked for leakage before each test. To release air bubbles in the soil media, after one layer of soil media was fully saturated, another was placed. After the device was installed and after setting a constant hydraulic head, the experiment started. Before feeding sediment particles, the hydraulic head and flow velocity were first stabilized. Then, incoming sediments were slowly and uniformly fed into the apparatus. For soil media in the same PS, the same stable time was selected for feeding in each experiment. The clogging phenomenon was monitored by the flow velocity and hydraulic gradient. The hydraulic gradient was calculated by monitoring the hydraulic head, which is the rate of change in hydraulic head per unit of distance of flow.A 6 m stable head height was set in the test. The hydraulic gradient for different soil media PSs should be approximately 12 for a specimen height of 0.5 m. However, to ensure hydraulic head stability, the hydrovalve (Figure2) was adjusted to change the flow velocity. Thus, the flow velocity varied with time and was different than the hydraulic gradient for the 34 experiments. However, for the flow velocity obtained in the 34 experiments, Darcy’s law does not apply. The hydraulic conductivity was not selected to illustrate the results, and instead, a discussion of the experimental hydraulic characteristics based on the hydraulic gradient and flow velocity is provided.After feeding the particles for a period of time, the monitoring data reach the secondary stable state, and the experiment was deemed finished. The lost particles under the drainage pipe were collected, and the soil media in the sample column were layered and sieved after the experiment.


## 2.1. Materials

The materials used in this study were natural materials similar to the real dam foundation media obtained upstream of Zhuo Yu Gou in the middle of the Qiongguo and Jiangxiong Reservoirs, Shannan, Tibet (Figure1). The materials were divided into two parts, soil media (as skeleton particles in the experiments) and incoming sediments (the particles added in the column to checking clogging or not in the experiments). To assess the impact of particle size on clogging, the particle size distributions (PSDs) of all the materials are in accordance with the Udden-Wentworth scale [37, 38].In the research of foundation leakage in Shannan, the dam foundation soil mainly included boulders, pebbles, gravel, and sand and contained cohesive soil, rounded but poorly sorted with particle sizes mainly larger than 0.5 mm [5, 39]. In this study, the soil media particle size (PS) was sieved into 32–64 mm, 16–32 mm, 8–16 mm, 4–8 mm, 2–4 mm, 1-2 mm, and 0.5–1 mm ranges. Similar to particle migration and erosion processes, these media cover a range of gravel and sand sizes [40]. The dry density and porosity of the soil media and the PSs of the incoming sediments are shown in Table 1. To obtain soils that were inert to each other, all soil particles were sieved by soaking in water.Table 1
Basic properties of soil media and corresponding PSs of incoming sediment.
Incoming PS (mm)Dry density (ρd/g/cm3)Porosity (ns)Soil media PS (mm)32–6416–328–164–82–41–20.5–14–81.630.326T1T82–41.630.310T2T9T151–21.650.290T3T10T16T210.5–11.660.307T4T11T17T22T260.25–0.51.690.347T5T12T18T23T27T300.125–0.251.730.332T6T13T19T24T28T31T330.063–0.1251.790.341T7T14T20T25T29T32T34Note. Ti denotes the experiments’ serial number of different incoming sediments in different soil media PSs.


## 2.2. Experimental Apparatus

For the purpose of the experimental works, a special infiltration-clogging monitoring system was built. The infiltration-clogging monitoring system comprised four parts: sample column, feeding column connected to a feeding pipe, monitoring equipment, and water supply tank with circulation function. Both the sample column and feeding column were 500 mm in height and 370 mm in diameter and made of Plexiglas (Figure1). As recommended for seepage studies in coarse-particle soils [41], the ratio of the sample column diameter to the soil media particle diameter was more than 5 to 6, appropriate for media particles smaller than 64 mm. Hydraulic head distributions along the soil media were measured by pore water pressure sensors, which were connected to a computer and laterally buried to the sample column. To avoid a preferential flow path between the soil and the Plexiglas cell wall, the monitoring point of hydraulic head change was selected at the center of the sample.From the feeding pipe, incoming sediments filled in, and the damping plates in the feeding column ensured even distribution of the incoming particles. Reddi et al. [42] and Alem et al. [16] indicated that clogging appeared to be greater under the condition of a constant head than under a constant flow rate. During the operation period, a submersible pump was used to continuously supply water to the constant head controller using a pressure tank and to circulate water in the water supply tank. In the experiment, a 6 m water head was provided by a pressure tank and was stabilized by the top sensor. Figure 2 shows a schematic and photograph of the system.Figure 2
Infiltration-clogging monitor system. (a) Schematic diagram. (b) Photograph.
(a)(b)


## 2.3. Experimental Procedure and Data Analysis

After placing the fully compacted soil media layer by layer, the sample column was checked for leakage before each test. To release air bubbles in the soil media, after one layer of soil media was fully saturated, another was placed. After the device was installed and after setting a constant hydraulic head, the experiment started. Before feeding sediment particles, the hydraulic head and flow velocity were first stabilized. Then, incoming sediments were slowly and uniformly fed into the apparatus. For soil media in the same PS, the same stable time was selected for feeding in each experiment. The clogging phenomenon was monitored by the flow velocity and hydraulic gradient. The hydraulic gradient was calculated by monitoring the hydraulic head, which is the rate of change in hydraulic head per unit of distance of flow.A 6 m stable head height was set in the test. The hydraulic gradient for different soil media PSs should be approximately 12 for a specimen height of 0.5 m. However, to ensure hydraulic head stability, the hydrovalve (Figure2) was adjusted to change the flow velocity. Thus, the flow velocity varied with time and was different than the hydraulic gradient for the 34 experiments. However, for the flow velocity obtained in the 34 experiments, Darcy’s law does not apply. The hydraulic conductivity was not selected to illustrate the results, and instead, a discussion of the experimental hydraulic characteristics based on the hydraulic gradient and flow velocity is provided.After feeding the particles for a period of time, the monitoring data reach the secondary stable state, and the experiment was deemed finished. The lost particles under the drainage pipe were collected, and the soil media in the sample column were layered and sieved after the experiment.


## 3. Results and Discussion

### 3.1. Laboratory Experiment Results

#### 3.1.1. Hydraulic Characteristics

According to Figure3, it can be seen that the hydraulic gradient remained relatively constant at first (approximately 12) and increased significantly with time after some particle sizes were introduced before it dropped with time and finally became stable at the initial value (approximately 12).Figure 3
Evolution of the hydraulic gradient and the flow velocity in six groups of soil media samples. (a) Soil media PS of 32–64 mm. (b) Soil media PS of 16–32 mm. (c) Soil media PS of 8–16 mm. (d) Soil media PS of 4–8 mm. (e) Soil media PS of 2–4 mm. (f) Soil media PS pf 1–2 mm. (g) Soil media PS of 0.5–1 mm.
(a)(b)(c)(d)(e)(f)(g)Under the same hydraulic head and for a fixed sample column, clogging in a smaller PS of the soil media resulted in a higher increase in the amplitude of the hydraulic gradient. Moreover, for the same PS of the soil media, the increased amplitude of the hydraulic gradient was different after introducing different sizes of incoming particles. For instance, the hydraulic gradient increased to its highest point after incoming PSs of 0.063–0.125 mm were introduced following soil media particles sizes of 0.5–1 mm, as shown in Figure3(g), and the same was observed for soil media PSs of 1-2 mm following incoming PSs of 0.125–0.25 mm in Figure 3(f), soil media PSs of 2–4 mm following incoming PSs of 0.25–0.5 mm in Figure 3(e), soil media PSs of 4–8 mm following incoming PSs of 0.5–1 mm in Figure 3(d), soil media PSs of 8–16 mm following incoming PSs of 1-2 mm in Figure 3(c), soil media PSs of 16–32 mm following incoming PSs of 2–4 mm in Figure 3(b), and soil media PSs of 32–64 mm following incoming PSs of 4–8 mm in Figure 3(a), respectively.In addition to the above variation, the hydraulic gradient curve shows exhibited fluctuations. This does not necessarily represent variations in the hydraulic gradient because when the water pump feeds the water circulated from the column, some air is entrained into the sample column, which might cause fluctuations in the hydraulic gradient.The initial flow velocity in the experimental columns of different soil media was found to vary around 25% within replicates (Figure3). This can be attributed to the natural variability in media, and these observed variations were within the ranges reported in the literature, e.g., Sébastien et al. [43] around 49% and Kandra et al. [20] around 30% for different sand media.The flow velocity remained relatively constant initially. It is logical that the larger the PS of the soil media is, the higher the initial stable flow velocity is. However, there were distinct differences in flow velocity after introducing incoming particles. For soil media of 2–4 mm (Figure3(e)), the flow velocity decreased significantly after introducing particles of 0.125–0.25 mm, 0.25–0.5 mm, and 0.5–1 mm, especially 0.25–0.5 mm. However, no changes were observed after introducing PSs of 0.063–0.125 mm. A similar evolution of the flow velocity for the other six soil media is shown in Figure 3. This suggests that there is a clogging of particles in the sample column due to introducing different particle sizes.A comparison of the flow velocity at the start and end of these experiments shows that the smaller the PS of the soil media is, the more obvious the variations in the flow velocity are; conversely, the variations in the flow velocity become more stable. A maximum decline was observed in the experiments of soil media PSs of 0.5–1 mm (Figure3(g)), which results in an order of magnitude difference. This indicates that the particle size of soil media influences the properties of permeability and clogging.


#### 3.1.2. Image Analysis

For porous media, like soil, physical clogging can be influenced by not only hydraulic characteristics but also porosity, size, type, and percent of fines [44]. For different PSs of soil media, due to smaller pore sizes of soil media than the size of the incoming particles, some incoming particles could not penetrate the pores; instead, they were mainly retained on the top of the soil media, forming a surface mat (Figure 4(a)). The particles could be transported by infiltration; however, some of them were trapped in the soil media (Figures 4(b) and 4(c)), while others were lost. Therefore, different PSs of incoming sediments can induce clogging of the soil column for different PSs of the soil media.Figure 4
Images of soil media at different layers after experiment and soil media particles of size in 2–4 mm using USB DIGITAL MICROSCOPE. (a) Surface of the soil media. (b) Surface of layer 2. (c) Surface of layer 3. (d) Surface of layer 4.


#### 3.1.3. Sieve Analysis

For the same size of soil media particles, with incoming particles of different sizes, clogging changes with depth and thickness. To quantify the changes in the behavior of physical clogging due to incoming particles, relationships in the size of the soil media particles, the weight of the clogging particles, and accurate positions of the clogging were constructed, as shown in Figure5. From top to bottom, the soil media in the sample column were divided into four layers by sieve analysis. The term α1 indicates the mass percentage of some incoming particle size in layer i, β indicates the mass percentage of some incoming particle size in the collection column, and the total is ∑αi+β=100%. Values of ∑αi+β ranging from 96.3 to 99.1% are attributed to measurement errors in Table 2.Figure 5
Mass percentage of clogging particles in four layers and loss in the collection column in six groups of soil media samples. (a) Soil media PSs of 32–64 mm. (b) Soil media PSs of 16–32 mm. (c) Soil media PSs of 8–16 mm. (d) Soil media PSs of 4–8 mm. (e) Soil media PSs of 2–4 mm. (f) Soil media PSs of 1–2 mm. (g) Soil media PSs of 0.5–1 mm.αi=mi/m0×100%; mi is the mass of the incoming particles of some size in layer I, kg; m0 is the total mass of incoming particles of some size, kg; β=mm/m0×100%; and mm is the mass of incoming particles of some size in the collection column, kg.
(a)(b)(c)(d)(e)(f)(g)Table 2
Mass percentage of incoming particle size in different soil media particles.
Incoming particle size (mm)Mass percentage of incoming PSs in soil media particles (%) and clogging patterns32–64 mm16–32 mm8–16 mm4–8 mm2–4 mm1–2 mm0.5–1 mmα1α1+α2∑αiβCPα1α1+α2∑αiβCPα1α1+α2∑αiβCPα1α1+α2∑αiβCPα1α1+α2∑αiβCPα1α1+α2∑αiβCPα1α1+α2∑αiβCP4–875.285.997.40S8794.498.70S————————————————————2–410.849.490.26.7I46.183.698.80S–I92.195.698.30S————————————————1–200.314.584.4N135.38316.1I4886.198.60S–I84.191.897.70S————————————0.5–1001187.7N1.14.617.981N7.740.676.522.1I4782.197.30S–I93.595.796.40S————————0.25–0.5006.191.5N01.110.688.1N1.55.613.983.7N2.635.77721.1I6184.596.80S–I85.792.4970S————0.125–0.25001.995.1N006.492.1N00692.4N04.723.175N1.737.677.120.4I57.879.4970S–I90.293.996.50S0.063–0.125002.196.3N001.795.7N003.894.7N0019.577.5N0.62.720.975.5N3.440.3942.3I59.785.596.30S–INote. CP denotes clogging patterns. S denotes surface clogging. S–I denotes the surface-internal clogging. I denotes the internal partial pore blockage. N denotes unclogging.From Figure5, for different soil media particles, incoming sediments of the same PSs were trapped in different layers. For instance, sediments of PSs of 0.125–0.25 mm were concentrated on top of the soil media of PSs of 0.5–1 mm as in Figure 3(g), were clogged in layer 1 and layer 2 in the soil media of PSs of 1-2 mm shown in Figure 3(f), accumulated in layer 2, layer 3, and layer 4 in the soil media of PSs of 2–4 mm in Figure 3(e), and were lost from the soil media of PSs of 32–64 mm, 16–32 mm, 8–16 mm, and 4–8 mm shown in Figures 3(a)–3(d). Again, the mass percentage of incoming sediment clogging in different PSs of soil media was different. For instance, the mass percentage of sediments of PSs of 0.125–0.25 mm in layer 1 was 90.2% for soil media 0.5–1 mm, the mass percentage in layer 1 and layer 2 was 79.4% for soil media 1-2 mm, and the mass percentage for the sum or layer 1, layer 2, layer 3, and layer 4 was 77.1% for soil media 2–4 mm. However, the mass percentage loss was 75%, 92.4%, 92.1%, and 95.1% for soil media of 4–8 mm, 8–16 mm, 16–32 mm, and 32–64 mm, respectively. Clogging for different PSs of incoming sediments in different soil media particles also suggests similar regularity, as shown in Table 2.


### 3.2. Division of Clogging Patterns and Determination of the Dominant Clogging Pattern

According to the sieve analysis, two results were found. First, four kinds of proportion characteristics of the mass percentage for different incoming sediment PSs clogging in different PSs of soil media were identified (Table3-left). The mass percentage was determined by observations from Kandra et al. [20]. Clogging occurred if the incoming sediment mass percentage was more than 75%. Second, four different clogging patterns were observed in different layers in the laboratory experiments, corresponding to the aforementioned mass percentage characteristics (Table 3). The idealized clogging was indicative of pure size exclusion, where clogging events occur only if particles enter a pore that is equal to their own diameter. However, soil pores were always inhomogeneous and anisotropic. We can, therefore, conclude that four different patterns were formed, which have been described in the image analysis results.Table 3
Mass percentage of incoming PSs in different soil media particles.
Proportion characteristics of mass percentage for different incoming sediments in size cloggingfor different soil skeletons in sizeClogging patternsα1 is greater than 75%Sα1 is less than 75% and the sum of α1 and α2 is greater than 75%S–ISum ofα1 and α2 is less than 75% and the sum of α1, α2, α3, and α4 is greater than 75%Iβ is greater than 75%NNote. S denotes surface clogging. S–I denotes surface-internal clogging. I denotes internal partial pore blockage. N denotes unclogging.A comparison of the clogging patterns in the above seven experiments indicated that the mass percentage of incoming sediments forming surface clogging and surface-internal clogging patterns wasα1>α2>α3>α4, and the mass percentage of incoming sediments forming an internal partial pore blockage pattern was α2>α3>α4. However, the mass percentage of incoming sediments forming an unclogging pattern was β>α4>α3>α2>α1. As expected, each clogging pattern developed a dominant layer. For the surface clogging and surface-internal clogging patterns, the dominant layer was layer 1, and layer 2 was dominant for the internal partial pore blockage pattern. Moreover, incoming sediments were lost for the unclogging pattern.In addition, the flow velocity varied much for incoming sediments forming patterns of surface clogging, surface-internal clogging, and internal partial pore blockage, and the velocity was lower and variable for surface-internal clogging (Figure3). At the same time, the hydraulic gradient for incoming sediments forming surface-internal clogging was slightly higher than that of the other two patterns (Figure 3). This indicates that the particles causing a lower flow velocity than the other size particles represented the dominant clogging particles, and the pattern of surface-internal clogging was the dominant clogging pattern. The dominant clogging PS for the soil media PSs of 16–32 mm was 2–4 mm, for 8–16 mm, it was 1-2 mm, for 4–8 mm, it was 0.5–1 mm, for 2–4 mm, it was 0.25–0.5 mm, for 1-2 mm, it was 0.125–0.25 mm, and for 0.5–1 mm, it was 0.063–0.125 mm (Table 2). Moreover, the 34 groups of experiments formed four patterns after being induced to incoming sediments of continuously graded soil, with only the soil media PSs of 32–64 mm not being representative of the surface-internal clogging pattern (Table 2). However, the clogging results showed that the flow velocity dropped and formed a surface clogging pattern. This is due to the lower head height and weaker carrying capacity of the water, while for incoming sediment PSs of 4–8 mm, sediment particles that were not transported accumulated on the surface of soil media PSs of 32–64 mm.


### 3.3. Assessment Criterion of Clogging Patterns and Determination of the Optimum Clogging PS

Based on the above analysis, we found that the relationship between soil media PSs and incoming sediment PSs affected the accurate classification of the clogging patterns. According to the relationship between them, a theoretical model was established.


#### 3.3.1. Theoretical Analysis

The homogeneous soil is idealized as an ensemble of spheres of equal size, including various parallel capillary tubes (cylinders) of the same diameter that are equal to the natural soil pore. The pore is expressed as(1)n=NπD24×1,where D is the homogeneous soil pore size in the ideal state, N denotes the number of capillary tubes per unit area, and n is the porosity of natural soil. The number of capillary tubes per unit area, N, may be expressed as follows:(2)N=4nπD2.In an ideal state, the volume of homogeneous soil media is equal to the volume of natural soil media, written as follows:(3)Mπd36=1−n,where M is the number of homogeneous soil media particles per unit volume, and d is the size of homogeneous soil media particles in an ideal state.Based on the above results, the area of the capillary tube wall can be taken as the area of the soil particle surface:(4)NπD=Mπd2,(5)M=NDd2.By combining equations (2), (3), and (5), D is solved as(6)D=23n1−nd.Indeed, each soil particle is an inhomogeneous sphere, the pores formed by soil media particles are also uneven, and the incoming particles are inhomogeneous too. We can choose the equivalent size of soil particles and an effective aperture formed by soil particle pores to substitute inhomogeneous soil particles and their formed voids. For each PS range, the equivalent size was calculated by the particle geometric average:(7)De=DmaxDmin,where De denotes the equivalent size of the soil particles, Dmax is the maximum PS, and Dmin is the minimum PS.The effective aperture of soil is then calculated as follows:(8)Dea=23α1ns1−nsDe,where Dea denotes the effective aperture of the soil, ns is the porosity of the soil equal to n, and α1 is a particle shape correction factor equal to the ratio of soil particle surface area and sphere surface area in the same volume for ideal sand and gravel materials: α1 = 1.5–1.9 [45].


#### 3.3.2. Assessment Criterion of Clogging Patterns

The equivalent size of soil media particles and incoming particles was calculated using equation (7) to derive De and de, and the effective aperture Dea was calculated using equation (8). Then, the ratio of de and Dea was obtained. Assuming that the soil particles are spheres of equal size, it is logical that when the ratio of the incoming particle size and the pore size is greater than 1, a mat is formed on the surface of the soil media. Moreover, when the ratio is equal to 1, clogging occurs, and when the ratio is less than 1, incoming particles will penetrate the pores and be lost. However, as already discussed, the soil particles and pores were not uniform in shape or size, as shown in Table 3. Clogging was formed when the de/Dea ratio was less than 1, as shown in Table 4. A similar situation was previously observed in wetland tests by Hua et al. [46], where clogging was observed for particles entering pores of a smaller diameter.Table 4
Calculation results.
Ds (mm)De (mm)nsDea (mm)da (mm)de (mm)de/DeaClogging patterns from the experimental observations32∼6445.2550.3267.68–9.734–85.660.58–0.74S2–42.830.29–0.37I1–21.410.15–0.18N0.5–10.710.07–0.09N0.25–0.50.360.04–0.05N0.125–0.250.180.02–0.03N0.063–0.1250.090.01–0.02N16∼3222.6270.3103.57–4.524–85.661.25–1.59S2–42.830.63–0.79S–I1–21.410.31–0.40I0.5–10.710.15–0.20N0.25–0.50.360.07–0.10N0.125–0.250.180.03–0.05N0.063–0.1250.090.01–0.03N8∼1611.3140.2901.62–2.052–42.831.38–1.74S1–21.410.69–0.87S–I0.5–10.710.34–0.44I0.25–0.50.350.17–0.22N0.125–0.250.160.08–0.11N0.063–0.1250.080.04–0.06N4∼85.6570.3070.88–1.111–21.411.27–1.60S0.5–10.710.63–0.80S–I0.25–0.50.350.31–0.40I0.125–0.250.180.15–0.20N0.063–0.1250.090.07–0.10N2∼42.8280.3400.51–0.650.5–10.711.09–1.39S0.25–0.50.350.54–0.69S–I0.125–0.250.180.27–0.35I0.063–0.1250.0890.13–0.18N1∼21.4140.3320.25–0.310.25–0.50.351.13–1.40S0.125–0.250.180.58–0.72S–I0.063–0.1250.0890.29–0.36I0.5∼10.7070.3350.125–0.160.125–0.250.181.13–1.44S0.063–0.1250.0890.56–0.72S–INote. Ds denotes soil skeleton particle size. Da denotes incoming particle size. De is the equivalent size of soil skeleton particles. De denotes the equivalent size of incoming particles. ns is the porosity of the soil skeleton. α1 is the particle shape correction factor. Dea is the effective aperture of soil in different α1.According to the results of six groups of soil media PSs from 0.5 mm to 32 mm, if we hypothesized that the criteria of0.5<de/Dea≤1 were representative of the surface-internal clogging pattern, knowing the PS and porosity of the soil media and using equation (8), the clogging PS det could be obtained by calculating do as follows:(9)n3α11−nDe<do≤2n3α11−nDe,where do denotes the clogging PS that results in the surface-internal clogging pattern. The calculation results agree well with the dominant clogging PS of the surface-internal clogging pattern in the laboratory (Figure 6(a)).Figure 6
Clogging particle size for different soil media by calculation and experimental observation. (a) Surface-internal clogging pattern. (b) Surface clogging pattern. (c) Internal partial pore blockage pattern. (d) Unclogging pattern.
(a)(b)(c)(d)The other three criteria were assumed to be represented byde/Dea>1 for the surface clogging pattern, 0.25<de/Dea≤0.5 for the internal partial pore blockage pattern, and de/Dea≤0.25 for representing the unclogging pattern. The mathematical expressions for these relations are as follows:(10)dsc>2n3α11−nDe,(11)n6α11−nDe≤dic<n3α11−nDe,(12)duc<n6α11−nDe,where dsc denotes the PS forming the surface clogging pattern, dic denotes the PS forming the internal partial pore blockage pattern, and duc denotes the PS not resulting in clogging. The calculation results of the above four criteria confirmed the correspondence between the de/Dea ratio and the four clogging patterns (Figure 6). Therefore, the dependence of the clogging pattern on the de/Dea ratio is shown in Table 5.Table 5
Criteria for determining the clogging patterns of unisize-graded soils.
de/Dea＞10.5–10.25–0.5＜0.25Clogging patternsSurface cloggingSurface-internal cloggingInternal partial pore blockageUncloggingNote. de denotes the equivalent size of incoming particles. Dea denotes the effective aperture of soil.In addition, for soil media PSs of 32–64 mm and incoming PSs of 4–8 mm, the calculation result was consistent with the surface-internal clogging pattern, although the surface clogging pattern was observed in the laboratory. This difference may be explained by the lower head height and weaker carrying capacity of the water, as discussed in Section3.2. This implies that it is more difficult for larger pore structure media to form clogs, as observed by Hua et al. [46]. Furthermore, for soil media PSs of 0.5–1 mm and 1–2 mm, no unclogging pattern was observed after feeding the particles, which has also been reported in the literature, e.g., Wang [19] and Fetzer et al. [47]. The observations eventually resulted in the above criteria, which are more suitable for smaller PS pebbles and gravel and larger PS sand.


#### 3.3.3. Optimum Clogging PS

The calculated clogging PSs for different clogging patterns were compared with the data observed in the laboratory (Figure6). The calculated results using the inequalities in equation (9) showed the best agreement with the observed clogging PS in the laboratory, which can be adopted to estimate the optimum clogging PS. Ultimately, d was confirmed as the optimum clogging PS, and 0.5<de/Dea≤1 was used as the assessment criterion of the optimum clogging pattern.


## 3.1. Laboratory Experiment Results

### 3.1.1. Hydraulic Characteristics

According to Figure3, it can be seen that the hydraulic gradient remained relatively constant at first (approximately 12) and increased significantly with time after some particle sizes were introduced before it dropped with time and finally became stable at the initial value (approximately 12).Figure 3
Evolution of the hydraulic gradient and the flow velocity in six groups of soil media samples. (a) Soil media PS of 32–64 mm. (b) Soil media PS of 16–32 mm. (c) Soil media PS of 8–16 mm. (d) Soil media PS of 4–8 mm. (e) Soil media PS of 2–4 mm. (f) Soil media PS pf 1–2 mm. (g) Soil media PS of 0.5–1 mm.
(a)(b)(c)(d)(e)(f)(g)Under the same hydraulic head and for a fixed sample column, clogging in a smaller PS of the soil media resulted in a higher increase in the amplitude of the hydraulic gradient. Moreover, for the same PS of the soil media, the increased amplitude of the hydraulic gradient was different after introducing different sizes of incoming particles. For instance, the hydraulic gradient increased to its highest point after incoming PSs of 0.063–0.125 mm were introduced following soil media particles sizes of 0.5–1 mm, as shown in Figure3(g), and the same was observed for soil media PSs of 1-2 mm following incoming PSs of 0.125–0.25 mm in Figure 3(f), soil media PSs of 2–4 mm following incoming PSs of 0.25–0.5 mm in Figure 3(e), soil media PSs of 4–8 mm following incoming PSs of 0.5–1 mm in Figure 3(d), soil media PSs of 8–16 mm following incoming PSs of 1-2 mm in Figure 3(c), soil media PSs of 16–32 mm following incoming PSs of 2–4 mm in Figure 3(b), and soil media PSs of 32–64 mm following incoming PSs of 4–8 mm in Figure 3(a), respectively.In addition to the above variation, the hydraulic gradient curve shows exhibited fluctuations. This does not necessarily represent variations in the hydraulic gradient because when the water pump feeds the water circulated from the column, some air is entrained into the sample column, which might cause fluctuations in the hydraulic gradient.The initial flow velocity in the experimental columns of different soil media was found to vary around 25% within replicates (Figure3). This can be attributed to the natural variability in media, and these observed variations were within the ranges reported in the literature, e.g., Sébastien et al. [43] around 49% and Kandra et al. [20] around 30% for different sand media.The flow velocity remained relatively constant initially. It is logical that the larger the PS of the soil media is, the higher the initial stable flow velocity is. However, there were distinct differences in flow velocity after introducing incoming particles. For soil media of 2–4 mm (Figure3(e)), the flow velocity decreased significantly after introducing particles of 0.125–0.25 mm, 0.25–0.5 mm, and 0.5–1 mm, especially 0.25–0.5 mm. However, no changes were observed after introducing PSs of 0.063–0.125 mm. A similar evolution of the flow velocity for the other six soil media is shown in Figure 3. This suggests that there is a clogging of particles in the sample column due to introducing different particle sizes.A comparison of the flow velocity at the start and end of these experiments shows that the smaller the PS of the soil media is, the more obvious the variations in the flow velocity are; conversely, the variations in the flow velocity become more stable. A maximum decline was observed in the experiments of soil media PSs of 0.5–1 mm (Figure3(g)), which results in an order of magnitude difference. This indicates that the particle size of soil media influences the properties of permeability and clogging.


### 3.1.2. Image Analysis

For porous media, like soil, physical clogging can be influenced by not only hydraulic characteristics but also porosity, size, type, and percent of fines [44]. For different PSs of soil media, due to smaller pore sizes of soil media than the size of the incoming particles, some incoming particles could not penetrate the pores; instead, they were mainly retained on the top of the soil media, forming a surface mat (Figure 4(a)). The particles could be transported by infiltration; however, some of them were trapped in the soil media (Figures 4(b) and 4(c)), while others were lost. Therefore, different PSs of incoming sediments can induce clogging of the soil column for different PSs of the soil media.Figure 4
Images of soil media at different layers after experiment and soil media particles of size in 2–4 mm using USB DIGITAL MICROSCOPE. (a) Surface of the soil media. (b) Surface of layer 2. (c) Surface of layer 3. (d) Surface of layer 4.


### 3.1.3. Sieve Analysis

For the same size of soil media particles, with incoming particles of different sizes, clogging changes with depth and thickness. To quantify the changes in the behavior of physical clogging due to incoming particles, relationships in the size of the soil media particles, the weight of the clogging particles, and accurate positions of the clogging were constructed, as shown in Figure5. From top to bottom, the soil media in the sample column were divided into four layers by sieve analysis. The term α1 indicates the mass percentage of some incoming particle size in layer i, β indicates the mass percentage of some incoming particle size in the collection column, and the total is ∑αi+β=100%. Values of ∑αi+β ranging from 96.3 to 99.1% are attributed to measurement errors in Table 2.Figure 5
Mass percentage of clogging particles in four layers and loss in the collection column in six groups of soil media samples. (a) Soil media PSs of 32–64 mm. (b) Soil media PSs of 16–32 mm. (c) Soil media PSs of 8–16 mm. (d) Soil media PSs of 4–8 mm. (e) Soil media PSs of 2–4 mm. (f) Soil media PSs of 1–2 mm. (g) Soil media PSs of 0.5–1 mm.αi=mi/m0×100%; mi is the mass of the incoming particles of some size in layer I, kg; m0 is the total mass of incoming particles of some size, kg; β=mm/m0×100%; and mm is the mass of incoming particles of some size in the collection column, kg.
(a)(b)(c)(d)(e)(f)(g)Table 2
Mass percentage of incoming particle size in different soil media particles.
Incoming particle size (mm)Mass percentage of incoming PSs in soil media particles (%) and clogging patterns32–64 mm16–32 mm8–16 mm4–8 mm2–4 mm1–2 mm0.5–1 mmα1α1+α2∑αiβCPα1α1+α2∑αiβCPα1α1+α2∑αiβCPα1α1+α2∑αiβCPα1α1+α2∑αiβCPα1α1+α2∑αiβCPα1α1+α2∑αiβCP4–875.285.997.40S8794.498.70S————————————————————2–410.849.490.26.7I46.183.698.80S–I92.195.698.30S————————————————1–200.314.584.4N135.38316.1I4886.198.60S–I84.191.897.70S————————————0.5–1001187.7N1.14.617.981N7.740.676.522.1I4782.197.30S–I93.595.796.40S————————0.25–0.5006.191.5N01.110.688.1N1.55.613.983.7N2.635.77721.1I6184.596.80S–I85.792.4970S————0.125–0.25001.995.1N006.492.1N00692.4N04.723.175N1.737.677.120.4I57.879.4970S–I90.293.996.50S0.063–0.125002.196.3N001.795.7N003.894.7N0019.577.5N0.62.720.975.5N3.440.3942.3I59.785.596.30S–INote. CP denotes clogging patterns. S denotes surface clogging. S–I denotes the surface-internal clogging. I denotes the internal partial pore blockage. N denotes unclogging.From Figure5, for different soil media particles, incoming sediments of the same PSs were trapped in different layers. For instance, sediments of PSs of 0.125–0.25 mm were concentrated on top of the soil media of PSs of 0.5–1 mm as in Figure 3(g), were clogged in layer 1 and layer 2 in the soil media of PSs of 1-2 mm shown in Figure 3(f), accumulated in layer 2, layer 3, and layer 4 in the soil media of PSs of 2–4 mm in Figure 3(e), and were lost from the soil media of PSs of 32–64 mm, 16–32 mm, 8–16 mm, and 4–8 mm shown in Figures 3(a)–3(d). Again, the mass percentage of incoming sediment clogging in different PSs of soil media was different. For instance, the mass percentage of sediments of PSs of 0.125–0.25 mm in layer 1 was 90.2% for soil media 0.5–1 mm, the mass percentage in layer 1 and layer 2 was 79.4% for soil media 1-2 mm, and the mass percentage for the sum or layer 1, layer 2, layer 3, and layer 4 was 77.1% for soil media 2–4 mm. However, the mass percentage loss was 75%, 92.4%, 92.1%, and 95.1% for soil media of 4–8 mm, 8–16 mm, 16–32 mm, and 32–64 mm, respectively. Clogging for different PSs of incoming sediments in different soil media particles also suggests similar regularity, as shown in Table 2.


## 3.1.1. Hydraulic Characteristics

According to Figure3, it can be seen that the hydraulic gradient remained relatively constant at first (approximately 12) and increased significantly with time after some particle sizes were introduced before it dropped with time and finally became stable at the initial value (approximately 12).Figure 3
Evolution of the hydraulic gradient and the flow velocity in six groups of soil media samples. (a) Soil media PS of 32–64 mm. (b) Soil media PS of 16–32 mm. (c) Soil media PS of 8–16 mm. (d) Soil media PS of 4–8 mm. (e) Soil media PS of 2–4 mm. (f) Soil media PS pf 1–2 mm. (g) Soil media PS of 0.5–1 mm.
(a)(b)(c)(d)(e)(f)(g)Under the same hydraulic head and for a fixed sample column, clogging in a smaller PS of the soil media resulted in a higher increase in the amplitude of the hydraulic gradient. Moreover, for the same PS of the soil media, the increased amplitude of the hydraulic gradient was different after introducing different sizes of incoming particles. For instance, the hydraulic gradient increased to its highest point after incoming PSs of 0.063–0.125 mm were introduced following soil media particles sizes of 0.5–1 mm, as shown in Figure3(g), and the same was observed for soil media PSs of 1-2 mm following incoming PSs of 0.125–0.25 mm in Figure 3(f), soil media PSs of 2–4 mm following incoming PSs of 0.25–0.5 mm in Figure 3(e), soil media PSs of 4–8 mm following incoming PSs of 0.5–1 mm in Figure 3(d), soil media PSs of 8–16 mm following incoming PSs of 1-2 mm in Figure 3(c), soil media PSs of 16–32 mm following incoming PSs of 2–4 mm in Figure 3(b), and soil media PSs of 32–64 mm following incoming PSs of 4–8 mm in Figure 3(a), respectively.In addition to the above variation, the hydraulic gradient curve shows exhibited fluctuations. This does not necessarily represent variations in the hydraulic gradient because when the water pump feeds the water circulated from the column, some air is entrained into the sample column, which might cause fluctuations in the hydraulic gradient.The initial flow velocity in the experimental columns of different soil media was found to vary around 25% within replicates (Figure3). This can be attributed to the natural variability in media, and these observed variations were within the ranges reported in the literature, e.g., Sébastien et al. [43] around 49% and Kandra et al. [20] around 30% for different sand media.The flow velocity remained relatively constant initially. It is logical that the larger the PS of the soil media is, the higher the initial stable flow velocity is. However, there were distinct differences in flow velocity after introducing incoming particles. For soil media of 2–4 mm (Figure3(e)), the flow velocity decreased significantly after introducing particles of 0.125–0.25 mm, 0.25–0.5 mm, and 0.5–1 mm, especially 0.25–0.5 mm. However, no changes were observed after introducing PSs of 0.063–0.125 mm. A similar evolution of the flow velocity for the other six soil media is shown in Figure 3. This suggests that there is a clogging of particles in the sample column due to introducing different particle sizes.A comparison of the flow velocity at the start and end of these experiments shows that the smaller the PS of the soil media is, the more obvious the variations in the flow velocity are; conversely, the variations in the flow velocity become more stable. A maximum decline was observed in the experiments of soil media PSs of 0.5–1 mm (Figure3(g)), which results in an order of magnitude difference. This indicates that the particle size of soil media influences the properties of permeability and clogging.


## 3.1.2. Image Analysis

For porous media, like soil, physical clogging can be influenced by not only hydraulic characteristics but also porosity, size, type, and percent of fines [44]. For different PSs of soil media, due to smaller pore sizes of soil media than the size of the incoming particles, some incoming particles could not penetrate the pores; instead, they were mainly retained on the top of the soil media, forming a surface mat (Figure 4(a)). The particles could be transported by infiltration; however, some of them were trapped in the soil media (Figures 4(b) and 4(c)), while others were lost. Therefore, different PSs of incoming sediments can induce clogging of the soil column for different PSs of the soil media.Figure 4
Images of soil media at different layers after experiment and soil media particles of size in 2–4 mm using USB DIGITAL MICROSCOPE. (a) Surface of the soil media. (b) Surface of layer 2. (c) Surface of layer 3. (d) Surface of layer 4.


## 3.1.3. Sieve Analysis

For the same size of soil media particles, with incoming particles of different sizes, clogging changes with depth and thickness. To quantify the changes in the behavior of physical clogging due to incoming particles, relationships in the size of the soil media particles, the weight of the clogging particles, and accurate positions of the clogging were constructed, as shown in Figure5. From top to bottom, the soil media in the sample column were divided into four layers by sieve analysis. The term α1 indicates the mass percentage of some incoming particle size in layer i, β indicates the mass percentage of some incoming particle size in the collection column, and the total is ∑αi+β=100%. Values of ∑αi+β ranging from 96.3 to 99.1% are attributed to measurement errors in Table 2.Figure 5
Mass percentage of clogging particles in four layers and loss in the collection column in six groups of soil media samples. (a) Soil media PSs of 32–64 mm. (b) Soil media PSs of 16–32 mm. (c) Soil media PSs of 8–16 mm. (d) Soil media PSs of 4–8 mm. (e) Soil media PSs of 2–4 mm. (f) Soil media PSs of 1–2 mm. (g) Soil media PSs of 0.5–1 mm.αi=mi/m0×100%; mi is the mass of the incoming particles of some size in layer I, kg; m0 is the total mass of incoming particles of some size, kg; β=mm/m0×100%; and mm is the mass of incoming particles of some size in the collection column, kg.
(a)(b)(c)(d)(e)(f)(g)Table 2
Mass percentage of incoming particle size in different soil media particles.
Incoming particle size (mm)Mass percentage of incoming PSs in soil media particles (%) and clogging patterns32–64 mm16–32 mm8–16 mm4–8 mm2–4 mm1–2 mm0.5–1 mmα1α1+α2∑αiβCPα1α1+α2∑αiβCPα1α1+α2∑αiβCPα1α1+α2∑αiβCPα1α1+α2∑αiβCPα1α1+α2∑αiβCPα1α1+α2∑αiβCP4–875.285.997.40S8794.498.70S————————————————————2–410.849.490.26.7I46.183.698.80S–I92.195.698.30S————————————————1–200.314.584.4N135.38316.1I4886.198.60S–I84.191.897.70S————————————0.5–1001187.7N1.14.617.981N7.740.676.522.1I4782.197.30S–I93.595.796.40S————————0.25–0.5006.191.5N01.110.688.1N1.55.613.983.7N2.635.77721.1I6184.596.80S–I85.792.4970S————0.125–0.25001.995.1N006.492.1N00692.4N04.723.175N1.737.677.120.4I57.879.4970S–I90.293.996.50S0.063–0.125002.196.3N001.795.7N003.894.7N0019.577.5N0.62.720.975.5N3.440.3942.3I59.785.596.30S–INote. CP denotes clogging patterns. S denotes surface clogging. S–I denotes the surface-internal clogging. I denotes the internal partial pore blockage. N denotes unclogging.From Figure5, for different soil media particles, incoming sediments of the same PSs were trapped in different layers. For instance, sediments of PSs of 0.125–0.25 mm were concentrated on top of the soil media of PSs of 0.5–1 mm as in Figure 3(g), were clogged in layer 1 and layer 2 in the soil media of PSs of 1-2 mm shown in Figure 3(f), accumulated in layer 2, layer 3, and layer 4 in the soil media of PSs of 2–4 mm in Figure 3(e), and were lost from the soil media of PSs of 32–64 mm, 16–32 mm, 8–16 mm, and 4–8 mm shown in Figures 3(a)–3(d). Again, the mass percentage of incoming sediment clogging in different PSs of soil media was different. For instance, the mass percentage of sediments of PSs of 0.125–0.25 mm in layer 1 was 90.2% for soil media 0.5–1 mm, the mass percentage in layer 1 and layer 2 was 79.4% for soil media 1-2 mm, and the mass percentage for the sum or layer 1, layer 2, layer 3, and layer 4 was 77.1% for soil media 2–4 mm. However, the mass percentage loss was 75%, 92.4%, 92.1%, and 95.1% for soil media of 4–8 mm, 8–16 mm, 16–32 mm, and 32–64 mm, respectively. Clogging for different PSs of incoming sediments in different soil media particles also suggests similar regularity, as shown in Table 2.


## 3.2. Division of Clogging Patterns and Determination of the Dominant Clogging Pattern

According to the sieve analysis, two results were found. First, four kinds of proportion characteristics of the mass percentage for different incoming sediment PSs clogging in different PSs of soil media were identified (Table3-left). The mass percentage was determined by observations from Kandra et al. [20]. Clogging occurred if the incoming sediment mass percentage was more than 75%. Second, four different clogging patterns were observed in different layers in the laboratory experiments, corresponding to the aforementioned mass percentage characteristics (Table 3). The idealized clogging was indicative of pure size exclusion, where clogging events occur only if particles enter a pore that is equal to their own diameter. However, soil pores were always inhomogeneous and anisotropic. We can, therefore, conclude that four different patterns were formed, which have been described in the image analysis results.Table 3
Mass percentage of incoming PSs in different soil media particles.
Proportion characteristics of mass percentage for different incoming sediments in size cloggingfor different soil skeletons in sizeClogging patternsα1 is greater than 75%Sα1 is less than 75% and the sum of α1 and α2 is greater than 75%S–ISum ofα1 and α2 is less than 75% and the sum of α1, α2, α3, and α4 is greater than 75%Iβ is greater than 75%NNote. S denotes surface clogging. S–I denotes surface-internal clogging. I denotes internal partial pore blockage. N denotes unclogging.A comparison of the clogging patterns in the above seven experiments indicated that the mass percentage of incoming sediments forming surface clogging and surface-internal clogging patterns wasα1>α2>α3>α4, and the mass percentage of incoming sediments forming an internal partial pore blockage pattern was α2>α3>α4. However, the mass percentage of incoming sediments forming an unclogging pattern was β>α4>α3>α2>α1. As expected, each clogging pattern developed a dominant layer. For the surface clogging and surface-internal clogging patterns, the dominant layer was layer 1, and layer 2 was dominant for the internal partial pore blockage pattern. Moreover, incoming sediments were lost for the unclogging pattern.In addition, the flow velocity varied much for incoming sediments forming patterns of surface clogging, surface-internal clogging, and internal partial pore blockage, and the velocity was lower and variable for surface-internal clogging (Figure3). At the same time, the hydraulic gradient for incoming sediments forming surface-internal clogging was slightly higher than that of the other two patterns (Figure 3). This indicates that the particles causing a lower flow velocity than the other size particles represented the dominant clogging particles, and the pattern of surface-internal clogging was the dominant clogging pattern. The dominant clogging PS for the soil media PSs of 16–32 mm was 2–4 mm, for 8–16 mm, it was 1-2 mm, for 4–8 mm, it was 0.5–1 mm, for 2–4 mm, it was 0.25–0.5 mm, for 1-2 mm, it was 0.125–0.25 mm, and for 0.5–1 mm, it was 0.063–0.125 mm (Table 2). Moreover, the 34 groups of experiments formed four patterns after being induced to incoming sediments of continuously graded soil, with only the soil media PSs of 32–64 mm not being representative of the surface-internal clogging pattern (Table 2). However, the clogging results showed that the flow velocity dropped and formed a surface clogging pattern. This is due to the lower head height and weaker carrying capacity of the water, while for incoming sediment PSs of 4–8 mm, sediment particles that were not transported accumulated on the surface of soil media PSs of 32–64 mm.


## 3.3. Assessment Criterion of Clogging Patterns and Determination of the Optimum Clogging PS

Based on the above analysis, we found that the relationship between soil media PSs and incoming sediment PSs affected the accurate classification of the clogging patterns. According to the relationship between them, a theoretical model was established.


### 3.3.1. Theoretical Analysis

The homogeneous soil is idealized as an ensemble of spheres of equal size, including various parallel capillary tubes (cylinders) of the same diameter that are equal to the natural soil pore. The pore is expressed as(1)n=NπD24×1,where D is the homogeneous soil pore size in the ideal state, N denotes the number of capillary tubes per unit area, and n is the porosity of natural soil. The number of capillary tubes per unit area, N, may be expressed as follows:(2)N=4nπD2.In an ideal state, the volume of homogeneous soil media is equal to the volume of natural soil media, written as follows:(3)Mπd36=1−n,where M is the number of homogeneous soil media particles per unit volume, and d is the size of homogeneous soil media particles in an ideal state.Based on the above results, the area of the capillary tube wall can be taken as the area of the soil particle surface:(4)NπD=Mπd2,(5)M=NDd2.By combining equations (2), (3), and (5), D is solved as(6)D=23n1−nd.Indeed, each soil particle is an inhomogeneous sphere, the pores formed by soil media particles are also uneven, and the incoming particles are inhomogeneous too. We can choose the equivalent size of soil particles and an effective aperture formed by soil particle pores to substitute inhomogeneous soil particles and their formed voids. For each PS range, the equivalent size was calculated by the particle geometric average:(7)De=DmaxDmin,where De denotes the equivalent size of the soil particles, Dmax is the maximum PS, and Dmin is the minimum PS.The effective aperture of soil is then calculated as follows:(8)Dea=23α1ns1−nsDe,where Dea denotes the effective aperture of the soil, ns is the porosity of the soil equal to n, and α1 is a particle shape correction factor equal to the ratio of soil particle surface area and sphere surface area in the same volume for ideal sand and gravel materials: α1 = 1.5–1.9 [45].


### 3.3.2. Assessment Criterion of Clogging Patterns

The equivalent size of soil media particles and incoming particles was calculated using equation (7) to derive De and de, and the effective aperture Dea was calculated using equation (8). Then, the ratio of de and Dea was obtained. Assuming that the soil particles are spheres of equal size, it is logical that when the ratio of the incoming particle size and the pore size is greater than 1, a mat is formed on the surface of the soil media. Moreover, when the ratio is equal to 1, clogging occurs, and when the ratio is less than 1, incoming particles will penetrate the pores and be lost. However, as already discussed, the soil particles and pores were not uniform in shape or size, as shown in Table 3. Clogging was formed when the de/Dea ratio was less than 1, as shown in Table 4. A similar situation was previously observed in wetland tests by Hua et al. [46], where clogging was observed for particles entering pores of a smaller diameter.Table 4
Calculation results.
Ds (mm)De (mm)nsDea (mm)da (mm)de (mm)de/DeaClogging patterns from the experimental observations32∼6445.2550.3267.68–9.734–85.660.58–0.74S2–42.830.29–0.37I1–21.410.15–0.18N0.5–10.710.07–0.09N0.25–0.50.360.04–0.05N0.125–0.250.180.02–0.03N0.063–0.1250.090.01–0.02N16∼3222.6270.3103.57–4.524–85.661.25–1.59S2–42.830.63–0.79S–I1–21.410.31–0.40I0.5–10.710.15–0.20N0.25–0.50.360.07–0.10N0.125–0.250.180.03–0.05N0.063–0.1250.090.01–0.03N8∼1611.3140.2901.62–2.052–42.831.38–1.74S1–21.410.69–0.87S–I0.5–10.710.34–0.44I0.25–0.50.350.17–0.22N0.125–0.250.160.08–0.11N0.063–0.1250.080.04–0.06N4∼85.6570.3070.88–1.111–21.411.27–1.60S0.5–10.710.63–0.80S–I0.25–0.50.350.31–0.40I0.125–0.250.180.15–0.20N0.063–0.1250.090.07–0.10N2∼42.8280.3400.51–0.650.5–10.711.09–1.39S0.25–0.50.350.54–0.69S–I0.125–0.250.180.27–0.35I0.063–0.1250.0890.13–0.18N1∼21.4140.3320.25–0.310.25–0.50.351.13–1.40S0.125–0.250.180.58–0.72S–I0.063–0.1250.0890.29–0.36I0.5∼10.7070.3350.125–0.160.125–0.250.181.13–1.44S0.063–0.1250.0890.56–0.72S–INote. Ds denotes soil skeleton particle size. Da denotes incoming particle size. De is the equivalent size of soil skeleton particles. De denotes the equivalent size of incoming particles. ns is the porosity of the soil skeleton. α1 is the particle shape correction factor. Dea is the effective aperture of soil in different α1.According to the results of six groups of soil media PSs from 0.5 mm to 32 mm, if we hypothesized that the criteria of0.5<de/Dea≤1 were representative of the surface-internal clogging pattern, knowing the PS and porosity of the soil media and using equation (8), the clogging PS det could be obtained by calculating do as follows:(9)n3α11−nDe<do≤2n3α11−nDe,where do denotes the clogging PS that results in the surface-internal clogging pattern. The calculation results agree well with the dominant clogging PS of the surface-internal clogging pattern in the laboratory (Figure 6(a)).Figure 6
Clogging particle size for different soil media by calculation and experimental observation. (a) Surface-internal clogging pattern. (b) Surface clogging pattern. (c) Internal partial pore blockage pattern. (d) Unclogging pattern.
(a)(b)(c)(d)The other three criteria were assumed to be represented byde/Dea>1 for the surface clogging pattern, 0.25<de/Dea≤0.5 for the internal partial pore blockage pattern, and de/Dea≤0.25 for representing the unclogging pattern. The mathematical expressions for these relations are as follows:(10)dsc>2n3α11−nDe,(11)n6α11−nDe≤dic<n3α11−nDe,(12)duc<n6α11−nDe,where dsc denotes the PS forming the surface clogging pattern, dic denotes the PS forming the internal partial pore blockage pattern, and duc denotes the PS not resulting in clogging. The calculation results of the above four criteria confirmed the correspondence between the de/Dea ratio and the four clogging patterns (Figure 6). Therefore, the dependence of the clogging pattern on the de/Dea ratio is shown in Table 5.Table 5
Criteria for determining the clogging patterns of unisize-graded soils.
de/Dea＞10.5–10.25–0.5＜0.25Clogging patternsSurface cloggingSurface-internal cloggingInternal partial pore blockageUncloggingNote. de denotes the equivalent size of incoming particles. Dea denotes the effective aperture of soil.In addition, for soil media PSs of 32–64 mm and incoming PSs of 4–8 mm, the calculation result was consistent with the surface-internal clogging pattern, although the surface clogging pattern was observed in the laboratory. This difference may be explained by the lower head height and weaker carrying capacity of the water, as discussed in Section3.2. This implies that it is more difficult for larger pore structure media to form clogs, as observed by Hua et al. [46]. Furthermore, for soil media PSs of 0.5–1 mm and 1–2 mm, no unclogging pattern was observed after feeding the particles, which has also been reported in the literature, e.g., Wang [19] and Fetzer et al. [47]. The observations eventually resulted in the above criteria, which are more suitable for smaller PS pebbles and gravel and larger PS sand.


### 3.3.3. Optimum Clogging PS

The calculated clogging PSs for different clogging patterns were compared with the data observed in the laboratory (Figure6). The calculated results using the inequalities in equation (9) showed the best agreement with the observed clogging PS in the laboratory, which can be adopted to estimate the optimum clogging PS. Ultimately, d was confirmed as the optimum clogging PS, and 0.5<de/Dea≤1 was used as the assessment criterion of the optimum clogging pattern.


## 3.3.1. Theoretical Analysis

The homogeneous soil is idealized as an ensemble of spheres of equal size, including various parallel capillary tubes (cylinders) of the same diameter that are equal to the natural soil pore. The pore is expressed as(1)n=NπD24×1,where D is the homogeneous soil pore size in the ideal state, N denotes the number of capillary tubes per unit area, and n is the porosity of natural soil. The number of capillary tubes per unit area, N, may be expressed as follows:(2)N=4nπD2.In an ideal state, the volume of homogeneous soil media is equal to the volume of natural soil media, written as follows:(3)Mπd36=1−n,where M is the number of homogeneous soil media particles per unit volume, and d is the size of homogeneous soil media particles in an ideal state.Based on the above results, the area of the capillary tube wall can be taken as the area of the soil particle surface:(4)NπD=Mπd2,(5)M=NDd2.By combining equations (2), (3), and (5), D is solved as(6)D=23n1−nd.Indeed, each soil particle is an inhomogeneous sphere, the pores formed by soil media particles are also uneven, and the incoming particles are inhomogeneous too. We can choose the equivalent size of soil particles and an effective aperture formed by soil particle pores to substitute inhomogeneous soil particles and their formed voids. For each PS range, the equivalent size was calculated by the particle geometric average:(7)De=DmaxDmin,where De denotes the equivalent size of the soil particles, Dmax is the maximum PS, and Dmin is the minimum PS.The effective aperture of soil is then calculated as follows:(8)Dea=23α1ns1−nsDe,where Dea denotes the effective aperture of the soil, ns is the porosity of the soil equal to n, and α1 is a particle shape correction factor equal to the ratio of soil particle surface area and sphere surface area in the same volume for ideal sand and gravel materials: α1 = 1.5–1.9 [45].


## 3.3.2. Assessment Criterion of Clogging Patterns

The equivalent size of soil media particles and incoming particles was calculated using equation (7) to derive De and de, and the effective aperture Dea was calculated using equation (8). Then, the ratio of de and Dea was obtained. Assuming that the soil particles are spheres of equal size, it is logical that when the ratio of the incoming particle size and the pore size is greater than 1, a mat is formed on the surface of the soil media. Moreover, when the ratio is equal to 1, clogging occurs, and when the ratio is less than 1, incoming particles will penetrate the pores and be lost. However, as already discussed, the soil particles and pores were not uniform in shape or size, as shown in Table 3. Clogging was formed when the de/Dea ratio was less than 1, as shown in Table 4. A similar situation was previously observed in wetland tests by Hua et al. [46], where clogging was observed for particles entering pores of a smaller diameter.Table 4
Calculation results.
Ds (mm)De (mm)nsDea (mm)da (mm)de (mm)de/DeaClogging patterns from the experimental observations32∼6445.2550.3267.68–9.734–85.660.58–0.74S2–42.830.29–0.37I1–21.410.15–0.18N0.5–10.710.07–0.09N0.25–0.50.360.04–0.05N0.125–0.250.180.02–0.03N0.063–0.1250.090.01–0.02N16∼3222.6270.3103.57–4.524–85.661.25–1.59S2–42.830.63–0.79S–I1–21.410.31–0.40I0.5–10.710.15–0.20N0.25–0.50.360.07–0.10N0.125–0.250.180.03–0.05N0.063–0.1250.090.01–0.03N8∼1611.3140.2901.62–2.052–42.831.38–1.74S1–21.410.69–0.87S–I0.5–10.710.34–0.44I0.25–0.50.350.17–0.22N0.125–0.250.160.08–0.11N0.063–0.1250.080.04–0.06N4∼85.6570.3070.88–1.111–21.411.27–1.60S0.5–10.710.63–0.80S–I0.25–0.50.350.31–0.40I0.125–0.250.180.15–0.20N0.063–0.1250.090.07–0.10N2∼42.8280.3400.51–0.650.5–10.711.09–1.39S0.25–0.50.350.54–0.69S–I0.125–0.250.180.27–0.35I0.063–0.1250.0890.13–0.18N1∼21.4140.3320.25–0.310.25–0.50.351.13–1.40S0.125–0.250.180.58–0.72S–I0.063–0.1250.0890.29–0.36I0.5∼10.7070.3350.125–0.160.125–0.250.181.13–1.44S0.063–0.1250.0890.56–0.72S–INote. Ds denotes soil skeleton particle size. Da denotes incoming particle size. De is the equivalent size of soil skeleton particles. De denotes the equivalent size of incoming particles. ns is the porosity of the soil skeleton. α1 is the particle shape correction factor. Dea is the effective aperture of soil in different α1.According to the results of six groups of soil media PSs from 0.5 mm to 32 mm, if we hypothesized that the criteria of0.5<de/Dea≤1 were representative of the surface-internal clogging pattern, knowing the PS and porosity of the soil media and using equation (8), the clogging PS det could be obtained by calculating do as follows:(9)n3α11−nDe<do≤2n3α11−nDe,where do denotes the clogging PS that results in the surface-internal clogging pattern. The calculation results agree well with the dominant clogging PS of the surface-internal clogging pattern in the laboratory (Figure 6(a)).Figure 6
Clogging particle size for different soil media by calculation and experimental observation. (a) Surface-internal clogging pattern. (b) Surface clogging pattern. (c) Internal partial pore blockage pattern. (d) Unclogging pattern.
(a)(b)(c)(d)The other three criteria were assumed to be represented byde/Dea>1 for the surface clogging pattern, 0.25<de/Dea≤0.5 for the internal partial pore blockage pattern, and de/Dea≤0.25 for representing the unclogging pattern. The mathematical expressions for these relations are as follows:(10)dsc>2n3α11−nDe,(11)n6α11−nDe≤dic<n3α11−nDe,(12)duc<n6α11−nDe,where dsc denotes the PS forming the surface clogging pattern, dic denotes the PS forming the internal partial pore blockage pattern, and duc denotes the PS not resulting in clogging. The calculation results of the above four criteria confirmed the correspondence between the de/Dea ratio and the four clogging patterns (Figure 6). Therefore, the dependence of the clogging pattern on the de/Dea ratio is shown in Table 5.Table 5
Criteria for determining the clogging patterns of unisize-graded soils.
de/Dea＞10.5–10.25–0.5＜0.25Clogging patternsSurface cloggingSurface-internal cloggingInternal partial pore blockageUncloggingNote. de denotes the equivalent size of incoming particles. Dea denotes the effective aperture of soil.In addition, for soil media PSs of 32–64 mm and incoming PSs of 4–8 mm, the calculation result was consistent with the surface-internal clogging pattern, although the surface clogging pattern was observed in the laboratory. This difference may be explained by the lower head height and weaker carrying capacity of the water, as discussed in Section3.2. This implies that it is more difficult for larger pore structure media to form clogs, as observed by Hua et al. [46]. Furthermore, for soil media PSs of 0.5–1 mm and 1–2 mm, no unclogging pattern was observed after feeding the particles, which has also been reported in the literature, e.g., Wang [19] and Fetzer et al. [47]. The observations eventually resulted in the above criteria, which are more suitable for smaller PS pebbles and gravel and larger PS sand.


## 3.3.3. Optimum Clogging PS

The calculated clogging PSs for different clogging patterns were compared with the data observed in the laboratory (Figure6). The calculated results using the inequalities in equation (9) showed the best agreement with the observed clogging PS in the laboratory, which can be adopted to estimate the optimum clogging PS. Ultimately, d was confirmed as the optimum clogging PS, and 0.5<de/Dea≤1 was used as the assessment criterion of the optimum clogging pattern.


## 4. Conclusions

A lab-based approach was carried out by studying the effects of the PS and the effective aperture of soil on the clogging performance in highly permeable coarse soil of dam foundations. The results showed that due to the soil particles and pores being inhomogeneous in shape or size, four different clogging patterns were formed in the studied coarse soil. The assessment criterion of clogging patterns can be depicted through thede/Dea ratio as follows:(i)
de/Dea> for surface clogging(ii)
0.5<de/Dea≤1 for surface-internal clogging(iii)
0.25<de/Dea≤0.5 for internal partial pore blockage(iv)
de/Dea≤0.25 for uncloggingDue to the lower head height and weaker carrying capacity of the water, leading to the above criteria being more suitable for pebbles and gravels of smaller PSs and sand of larger PSs, for the soil media larger than 32 mm, most of the incoming particles were lost.Moreover, from the results of experiments and formula calculations, surface-internal clogging was the optimum clogging pattern. The optimum clogging particle in the pattern of surface-internal clogging was confirmed by the following:(13)n3α11−nDe<do≤2n3α11−nDe.The classification of clogging patterns, the calculation of the optimum clogging PS, and the determination of the equivalent PS can provide an effective way to study shrinking leakage problems in highly permeable coarse soil of dam foundations.



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