Runoff Characteristics and Soil Loss Mechanism in the Weathered Granite Area under Simulated Rainfall

Soils developed from the parent materials of highly weathered granite are particularly susceptible to soil erosion. Therefore, it is of great significance to conduct in-depth research on runoff characteristics and soil loss mechanisms in weathered granite areas. Using the weathered granite area in the hilly region of southeastern China as the research object, we conducted indoor artificial rainfall simulation experiments involving three slope steepnesses (SSs), 8°, 15°, and 25°, and five rainfall intensities (RIs), 0.5, 1.0, 1.5, 2.0, and 2.5 mm/min. The results showed that sediment load (SL) has positively linear relationships with mean runoff velocity (V), Reynolds number (Re), Froude number (Fr), shear stress (τ), and stream power (w). The eroded sediment was principally composed of silt and clay that accounted for 65.41–73.41% of the total SL. There was a boundary point at 0.02 mm for the particle size distribution (PSD) of the eroded sediment. The enrichment ratio (Er) of sand-grained particles (0.02–2 mm) ranged from approximately 0.45 to 0.65, while the Er of fine-grained particles (<0.02 mm) ranged from approximately 1.37 to 1.80. These results increase our understanding of the relationships among RI, SS, runoff, and soil losses from weathered granite hillslopes, particularly the relationships between different hydraulic parameters and sediment size characteristics.


Introduction
Soil erosion is one of the most important global environmental problems [1,2]; however, the sensitive weathered granite regions of southeastern China are particularly vulnerable [3,4]. Determining the mechanism of soil loss still remains a challenge due to the physical complexity of the erosion process [5]. The nature of eroded sediment, such as its size and density, has a great impact on the process of sediment yield [6]. Severe soil erosion not only reduces the productivity of the land but also causes pollution in aquatic environments [7,8]. The sediment caused by water erosion can act as a carrier of soil-bound nutrients and contaminants that are unevenly distributed in the sediment surface because of the varying surface areas [9][10][11][12]. The characterization of eroded sediment particle size distribution (PSD) is important for understanding erosion estimation and modeling [13,14]. Therefore, prerequisite knowledge about sediment sorting and dynamics is of great significance for studying the transportation of different kinds of nutrients and contaminants from sloping farmlands to aquatic environments [15,16].
Soil erosion involves the detachment of original soil materials by rainfall runoff and the subsequent transportation and deposition of the activated mobile particles [17]. The process of soil erosion is influenced by various factors including rainfall characteristics [18][19][20], topographic conditions [21,22], soil properties [23][24][25], farming methods [8,26], and vegetation cover [27,28], among which rainfall intensity (RI) and slope steepness (SS) have been widely studied and are still the focus of research [29][30][31]. For example, Sobol et al. [32] investigated the effects of rainfall intensity and slope steepness on the development of soil erosion in the southern Cis-Ural region, finding that soil loss linearly depended on these two factors, and that the clay content was higher in eroded material than in the original soils. Dai et al. [33] conducted field runoff plot-monitoring tests to reveal the plot-scale characteristics of surface soil erosion in the karst rocky desertification regions. They found that rainfall intensity had significant effects on runoff depth and soil loss rates, and slope steepness had a greater effect on soil loss than slope length. Guo et al. [34] investigated the combined impacts of rainfall and surface runoff on soil erosion, finally identifying the relationships between soil erosion and different hydraulic parameters. The effects of sample collection time intervals and rain peak morphology on the analysis results of runoff yield and soil erosion have also been studied [1,35,36].
The mechanism of soil erosion has been extensively studied over recent years around the world with different methods, including experimental monitoring and model simulation [37][38][39][40]. The current models of erosion forecasting can generally be divided into two categories: the physical model and the empirical model [13,41]. For example, a structural equation modeling method was employed by [42] to study the interactive effects of precipitation and vegetation on soil erosion. Kiani-Harchegani, Sadeghi, Singh, Asadi, and Abedi [29] found that partial eta-squared is an effective novel technique for improving the interpretation of complex hydrological processes and erosion evolution. Chen et al. [43] employed a meta-analysis of field plot data to identify the effects of soil-water conservation measures on the mitigation of land degradation. In addition, significant efforts have been made to investigate the process of soil erosion in different condition scales [44,45], particularly to explore the erosion mechanisms concerning the different hydraulic parameters on the sloping farmland. The hydraulic characteristics of runoff depth (h), mean runoff velocity (V), Reynolds number (Re), Froude number (Fr), hydraulic shear stress (τ), and stream power (w) have been applied to evaluate soil erosion in prediction models [34,46,47]. It has been commonly reported that sediment yield presents good linear relationships with τ, w, V, Re, and Fr [48,49].
However, the current studies about soil erosion in China mainly focus on slopes with loess, red and purple soils [9,43,50] and relatively little information is available regarding the slopes of weathered granite in SE China. The soils developed from the parent materials of highly weathered granite are notably susceptible to soil erosion [51]. The high intensity, frequency, and centralized distribution of rainstorms caused by fluent typhoons easily cause soil erosion and ultimately affect the sustainability of local socioeconomic development [52]. Authors recently attempted to explore the loss mechanisms of runoff, soil, and nutrients from weathered granite slopes with different underlying layers [51,53]. Research about the relationships between different hydraulic parameters and sediment size characteristics has not yet been conducted and the erosion mechanism is not well understood. Therefore, it is of great significance to conduct in-depth research to study the runoff characteristics and soil loss mechanisms in weathered granite areas. The objectives of this study are (1) to quantitatively highlight the characteristics of runoff and sediment yields from the weathered granite slopes, and (2) to identify the relationships between different hydraulic parameters and sediment size characteristics.

Experimental Equipment
The rainfall experiments were completed at the Research Center for Agricultural Non-point Source Pollution and Soil Erosion Control of Zhejiang University (Changxing County, China) from September to December 2018. The equipment used included the rainfall simulator (Figure 1a) as well as runoff flumes (Figure 1b). The portable QYJY-502 rainfall simulator (Qingyuan Xi'an Measurement and Control Technology Co., Ltd., Long Island City, NY, USA) could be adjusted precisely to any expected RI between 0.25 and 3.33 mm/min by combining different kinds of nozzles and water pressures. The nozzles were Water 2021, 13, 3453 3 of 16 uniformly placed above the runoff flumes at a height of 6 m with a rainfall coverage of 4 × 4 m, and 20 rainfall-calibrating gauges were placed around the runoff flumes. Before starting each rainfall test, the runoff plots were covered with waterproof cloth. Data of the rainfall calibrating gauges were verified for the Christiansen's uniformity coefficient of rainfall, which were all above 85% and considerably acceptable. Then, the tests started after the waterproof cloths were taken away.
Water 2021, 13, x FOR PEER REVIEW 3 of 17 rainfall simulator (Figure 1a) as well as runoff flumes (Figure 1b). The portable QYJY-502 rainfall simulator (Qingyuan Xi'an Measurement and Control Technology Co., Ltd.) could be adjusted precisely to any expected RI between 0.25 and 3.33 mm/min by combining different kinds of nozzles and water pressures. The nozzles were uniformly placed above the runoff flumes at a height of 6 m with a rainfall coverage of 4 × 4 m, and 20 rainfallcalibrating gauges were placed around the runoff flumes. Before starting each rainfall test, the runoff plots were covered with waterproof cloth. Data of the rainfall calibrating gauges were verified for the Christiansen's uniformity coefficient of rainfall, which were all above 85% and considerably acceptable. Then, the tests started after the waterproof cloths were taken away.

Materials
The experimental soil was taken from the weathered granite hillslopes in Anji County (30°34′ N, 119°23′ E) of northwestern Zhejiang Province, a mid-subtropical monsoon region characterized by abundant rainfall and a mild climate [54]. Torrential precipitation, caused by frequent typhoons, and slopes with an SS higher than 25° are dominant in the study area, with an SS of 8° considered a key threshold for soil erosion according to local data. In this area, soil thickness reduces due to the topsoil removal caused by severe hydraulic damage, exposing different underlying soil horizons (Figure 1c). Based on the parent material horizons and the outcrop of the different soil layers, soils from the tillage layer with slight water erosion were chosen as the simulated rainfall study objects to further explore the runoff characteristics and soil loss mechanisms of SE China's hilly region. Another reason why soils from the tillage layer were chosen was that the surface runoff on the slopes of sand and laterite layers was too thin to measure the runoff velocity. With a pH of 5.72, the experimental soils are weakly acidic and classed as clay loam, composed of 56.36% sand, 22.02% silt, and 21.62% clay. The bulk density is 1.65 g/cm 3 with a mean weight diameter (MWD) of 0.31 mm. The contents of soil organic matter, total nitrogen and total phosphorus are, respectively, 2.65, 0.74, and 1.90 g/kg.

Experimental Design and Measurements
Field soil was collected at 5 cm intervals from the top to downward layers and the physico-chemical properties were analyzed in an indoor laboratory. The test methods and results of the basic physical and chemical properties of the three soil layers can be found in published research papers [54]. All the measurements were conducted in triplicate. Then, runoff flumes were filled with original soil with the corresponding layers based on the original state method of removal, maintaining a consistent bulk density. The experimental soils were set aside for some time to naturally settle before the rainfall experiments. Three SSs, 8°, 15°, and 25°, and five RIs, 0.5, 1.0, 1.5, 2.0, and 2.5 mm/min, were adopted

Materials
The experimental soil was taken from the weathered granite hillslopes in Anji County (30 • 34 N, 119 • 23 E) of northwestern Zhejiang Province, a mid-subtropical monsoon region characterized by abundant rainfall and a mild climate [54]. Torrential precipitation, caused by frequent typhoons, and slopes with an SS higher than 25 • are dominant in the study area, with an SS of 8 • considered a key threshold for soil erosion according to local data. In this area, soil thickness reduces due to the topsoil removal caused by severe hydraulic damage, exposing different underlying soil horizons (Figure 1c). Based on the parent material horizons and the outcrop of the different soil layers, soils from the tillage layer with slight water erosion were chosen as the simulated rainfall study objects to further explore the runoff characteristics and soil loss mechanisms of SE China's hilly region. Another reason why soils from the tillage layer were chosen was that the surface runoff on the slopes of sand and laterite layers was too thin to measure the runoff velocity. With a pH of 5.72, the experimental soils are weakly acidic and classed as clay loam, composed of 56.36% sand, 22.02% silt, and 21.62% clay. The bulk density is 1.65 g/cm 3 with a mean weight diameter (MWD) of 0.31 mm. The contents of soil organic matter, total nitrogen and total phosphorus are, respectively, 2.65, 0.74, and 1.90 g/kg.

Experimental Design and Measurements
Field soil was collected at 5 cm intervals from the top to downward layers and the physico-chemical properties were analyzed in an indoor laboratory. The test methods and results of the basic physical and chemical properties of the three soil layers can be found in published research papers [54]. All the measurements were conducted in triplicate. Then, runoff flumes were filled with original soil with the corresponding layers based on the original state method of removal, maintaining a consistent bulk density. The experimental soils were set aside for some time to naturally settle before the rainfall experiments. Three SSs, 8 • , 15 • , and 25 • , and five RIs, 0.5, 1.0, 1.5, 2.0, and 2.5 mm/min, were adopted according to the data from the local meteorological station to simulate the corresponding hydrological and terrain conditions. Two runoff flumes were simultaneously used for the experimental research replications. The 5 cm topsoil layer was disturbed by rainfall splashes and the test soil was replaced with original soil after each rainfall test.
The time of rainfall initiation was recorded using stopwatches and the rainfall lasted 90 min after surface runoff occurred for convenient runoff and sediment collection. The runoff sediment samples were collected from the top "V-shape" outlet at every 3 min and the runoff volumes (Rv) were measured using the volume method. The amounts of eroded sediment were measured using the dry weighing method and then the sediment was further analyzed using the pipette method to determine the PSD, MWD, and enrichment ratio (Er) of different particles. The velocity of surface runoff was measured by the dyeracing method after the rainfall runoff became relatively stable. The time taken for the dye tracer to travel a given distance along the slopes was recorded with stopwatches, which was conducted in triplicate to get the average values for determining the measured runoff velocity (V 0 ).

Data Calculation and Analysis
V 0 was determined as the travelling distance per unit time and was then used to estimate the mean runoff velocity (V) via the following formula: where V 0 is the measured runoff velocity, m/s; V is the mean runoff velocity, m/s; k is a coefficient equal to 0.67 as the runoff is laminar flow. h was calculated via the following formula: where h is the runoff depth, m; Q is the accumulative Rv during sampling time t (s), m 3 ; B is the width of water-crossing section, m. Re and Fr were determined to reflect the flow regime and were calculated as follows: where v is the kinematic viscosity, m 2 /s; g is the gravitational acceleration, m/s 2 . τ was calculated via the following formula: where τ is the shear stress, N/m 2 ; ρ is the mass density of the runoff-sediment mixture assuming the sediment volume to be negligible, g/L; J is the friction slope, m/m. w was calculated via the following formula: where w is the stream power, N/m/s. The runoff rate (Rr), sediment rate (Sr), sediment concentration (Sc), Er and MWD of the eroded sediment were determined according to the methods reported in the previous studies [6,10,53].
where I is the runoff coefficient; T is the time of runoff, min; Rv is runoff volume, L; RI is rainfall intensity, mm/min; SS is slope steepness, • ; S is runoff tank area, m 2 . The figures were drawn using Origin 9.0, and statistical analysis was performed using Microsoft Excel 2016, SPSS 20.0 and CANOCO 5.0. The correlation tests and multiple regression analyses between Rv, S L and SS, RI and the hydraulic parameters were finally conducted to determine their relationships. A redundancy analysis (RDA) was employed to determine the relationships between sediment size characteristics and different hydraulic parameters by analyzing the Er and MWD of the eroded sediment. Table 1 shows that the values of T 0 are negatively correlated to RI and SS. T 0 on the slopes with an SS of 25 • , 15 • , and 8 • decreased 83.15%, 88.86%, and 93.89%, respectively, as RI increased from 0.5 to 2.5 mm/min. The dropping ratios of T 0 under the uniform RI were, respectively, 85.61%, 63.00%, 61.27%, 64.55%, and 60.29% when SS was increased from 8 • to 25 • . RI presents a much greater correlation to T 0 compared to SS. It has been reported that the process of runoff generation is affected by multiple factors such as the soil properties, the underlying surface, and topographic and rainfall characteristics [8,27,37]. As for the rainfall characteristics, the intensity and duration of every rainfall event are the most important factors affecting runoff generation [55,56]. T 0 significantly decreased as slope steepness increased (SS), most likely due to the pre-saturation process of the experimental soil. The soil was saturated and the soil pores were full of infiltrated water at the initial stage. Surface runoff originates when the infiltration rate is less than the rainfall intensity (Hortonian flow). This decrease in infiltration happens when the soil begins to become saturated. The experimental soil contained very little organic matter and was weakly aggregated with poor stability. The surface roughness caused the rainfall runoff to infiltrate the soil more easily; the infiltration rate is related to the rate of water supply [57]. The runoff pattern transformed into saturation excess after the experimental soil was entirely saturated with the prolonged rainfall duration. Additionally, the experimental soil was more likely to be saturated in heavy rainfall, and the runoff velocity became faster on the steeper slopes, with an accelerated horizontal component of gravity, thereby shortening T 0 [58,59]. Note: SS is slope steepness; RI is rainfall intensity; T 0 is the occurring time of surface runoff and sediment yield; Rv is runoff volume; S L is sediment load; Sc is average sediment concentration; I is the runoff coefficient.

Characteristics of Runoff Generation
Rr first increased with rainfall duration and then reached a relatively stable dynamic state until the end of the rainfall ( Figure 2). As the rainfall duration reduced to a stable state, the RI increased and the SS decreased with a range around 3-45 min. There is a clear positive correlation between Rr and RI, while Rr tended to be negatively correlated with SS under the uniform RI. The accumulative Rv had a positive correlation with increasing RI (R 2 > 0.99) and decreased as the SS increased because of the declining rainfall-bearing area (Table 1), similar to the trends of Rr. Rr increased with the increasing RI in the uncovered runoff flumes as a consequence of the increased water supply per unit of time of heavier rainfalls [34]. Rain splash will cause the soil surface structure to be gradually compacted, and then form a crust on the soil surface, which is conducive to the generation of runoff [60]. The runoff coefficient (I) is significantly positively correlated with RI, but not significantly correlated with SS. This shows the positive impact of RI on runoff. The size and velocity of raindrops were larger under heavier rainfalls, making it more likely that soil aggregates are broken down into smaller parts; this can cause pore clogging and soil sealing [61]. The formation of crust reduced surface roughness and limited the soil infiltration rate after the soil structure was broken by the beating action of the raindrops, resulting in greater runoff generation and a higher Rr [62]. There are two crust modes on the soil surface: the physically structural crust and the depositional crust [63]. The structural crust forms first and is caused by raindrop impacts and then the depositional crust occurs due to the formations of puddles and surface runoff [64]. Crusts on the soil surface are an important symbol of soil spoilage by rainfall runoff. Raindrop impacts the soil's physical properties, and soil losses have been found to gradually decrease with the increasing RI. This occurs because raindrops with a low Ri have lower levels of kinetic energy [5].
Rr first increased with rainfall duration and then reached a relatively stable dynamic state until the end of the rainfall ( Figure 2). As the rainfall duration reduced to a stable state, the RI increased and the SS decreased with a range around 3-45 min. There is a clear positive correlation between Rr and RI, while Rr tended to be negatively correlated with SS under the uniform RI. The accumulative Rv had a positive correlation with increasing RI (R 2 > 0.99) and decreased as the SS increased because of the declining rainfall-bearing area (Table 1), similar to the trends of Rr. Rr increased with the increasing RI in the uncovered runoff flumes as a consequence of the increased water supply per unit of time of heavier rainfalls [34]. Rain splash will cause the soil surface structure to be gradually compacted, and then form a crust on the soil surface, which is conducive to the generation of runoff [60]. The runoff coefficient (I) is significantly positively correlated with RI, but not significantly correlated with SS. This shows the positive impact of RI on runoff. The size and velocity of raindrops were larger under heavier rainfalls, making it more likely that soil aggregates are broken down into smaller parts; this can cause pore clogging and soil sealing [61]. The formation of crust reduced surface roughness and limited the soil infiltration rate after the soil structure was broken by the beating action of the raindrops, resulting in greater runoff generation and a higher Rr [62]. There are two crust modes on the soil surface: the physically structural crust and the depositional crust [63]. The structural crust forms first and is caused by raindrop impacts and then the depositional crust occurs due to the formations of puddles and surface runoff [64]. Crusts on the soil surface are an important symbol of soil spoilage by rainfall runoff. Raindrop impacts the soil's physical properties, and soil losses have been found to gradually decrease with the increasing RI. This occurs because raindrops with a low Ri have lower levels of kinetic energy [5].  Table 2. V ranges from 0.83 × 10 −2 to 4.99 × 10 −2 m/s and h ranges from 1.35 to 2.31 mm. The trends of increasing h and V caused by eliminating the raindrops' impact are similar to the results of An et al. [65], while Beuselinck et al. [66] found that raindrop impact slows down V. In agreement with these findings, Lu, Zheng, Li, Bian, and An [61] reported that raindrop impact increases with increasing RI among 0.53 and 1.67 mm/min, which results in heavy soil compaction and crust followed by low soil infiltration and more runoff generation. With regard to Re, the values generally increased with the increasing RI, varying from 12.   Table 2. V ranges from 0.83 × 10 −2 to 4.99 × 10 −2 m/s and h ranges from 1.35 to 2.31 mm. The trends of increasing h and V caused by eliminating the raindrops' impact are similar to the results of An et al. [65], while Beuselinck et al. [66] found that raindrop impact slows down V. In agreement with these findings, Lu, Zheng, Li, Bian, and An [61] reported that raindrop impact increases with increasing RI among 0.53 and 1.67 mm/min, which results in heavy soil compaction and crust followed by low soil infiltration and more runoff generation. With regard to Re, the values generally increased with the increasing RI, varying from 12.70 to 72.76, indicating that the surface runoff is a type of laminar tranquil flow according to the criterion of open channel flow, because all the values are less than 500. Fr also increased with the increasing RI, ranging from 0.06 to 0.42, indicating that the surface runoff belongs to slow flow as all the values are smaller than the critical threshold of 1. The values of τ show trends that increased with the increasing RI from 0.47 × 10 −2 to 10.83 × 10 −2 N/m. In the case of w, the values increased with both increasing RI and SS with a range of 0.04 × 10 −4 to 5.29 × 10 −4 N/m/s, and the values are far lower than the results of Guo, Ma, Cai, and Wu [34] and Sajjadi and Mahmoodabadi [49] due to the difference in soil types and the experimental setup. with both increasing RI and SS with a range of 0.04 × 10 −4 to 5.29 × 10 −4 N/m/s, and the values are far lower than the results of Guo, Ma, Cai, and Wu [34] and Sajjadi and Mahmoodabadi [49] due to the difference in soil types and the experimental setup.

Characteristics of Sediment Yield
The trends of Sr changing with rainfall duration under different experimental conditions are depicted in Figure 4. Sr increased sharply at the initial stage and then displayed a rapid decreasing trend with the prolongation of rainfall duration with some minor fluctuations under most of the rainfall occurrences, which is mainly due to the first flushing effect [4]. There was strong splashing erosion in the runoff flumes during the initial presaturation stage of the experimental soil before the generation of surface runoff. Surface runoff gradually formed with the prolongation of rainfall duration and migrated to the bottom outlet, transporting the mobile particles that have been activated in the earlier stage. The soil erosion induced by rainfall commonly consists of the rill and interrill components according to the source of the eroded sediment [9,67]. The pattern of soil erosion in this study belongs to interrill erosion due to the relatively short slope length (2.0 m) of the experimental runoff flumes [2]; there was almost no rill erosion. Interrill erosion is

Characteristics of Sediment Yield
The trends of Sr changing with rainfall duration under different experimental conditions are depicted in Figure 4. Sr increased sharply at the initial stage and then displayed a rapid decreasing trend with the prolongation of rainfall duration with some minor fluctuations under most of the rainfall occurrences, which is mainly due to the first flushing effect [4]. There was strong splashing erosion in the runoff flumes during the initial presaturation stage of the experimental soil before the generation of surface runoff. Surface runoff gradually formed with the prolongation of rainfall duration and migrated to the bottom outlet, transporting the mobile particles that have been activated in the earlier stage. The soil erosion induced by rainfall commonly consists of the rill and interrill components according to the source of the eroded sediment [9,67]. The pattern of soil erosion in this study belongs to interrill erosion due to the relatively short slope length (2.0 m) of the experimental runoff flumes [2]; there was almost no rill erosion. Interrill erosion is more likely to transport fine sediment, because the coarse sediment is hard to activate and transport down the slopes. Surface runoff has been reported to be a key factor in controlling soil erosion on hillslopes due to its ability to detach and transport soil materials [68]. There are two erosion mechanisms: raindrop splashes and runoff washes [69]. Soil aggregates in the topsoil are destroyed by raindrop kinetic energy and then the fine-grained particles are peeled off and carried away [70]. The soil aggregates can be disrupted by quick wetting and mechanical breakdown due to raindrop hammering [71]. The strong disruption of soil materials and fast formation of crusts on the surface are related to the increasing RI. Sr has a positive correlation to RI, and the average Sc is positively interrelated to both RI and SS (Table 1). The accumulative S L also positively correlates with the increasing RI and SS, with a range of 74.50-5857.25 g. The increasing times of total S L on the slopes with SS of 8 • , 15 • , and 25 • were, respectively, 15.93, 28.17, and 13.85 when RI increased from 0.5 to 2.5 mm/min (Table 1). Figure 5 shows that the sediment yield is positively linearly related to total the Rv on various slopes (R 2 > 0.93). The average Sc also positively correlates with RI (R 2 > 0.83) and the order of the average Sc under different slopes is 25 • > 15 • > 8 • when RI is uniform, indicating that the increasing sediment rate is faster than that of runoff generation. These results are similar to the findings of Tuset et al. [72], who found that the fluctuations of suspended Sc are strongly correlated to runoff magnitude and the amounts of eroded sediment correlate to Rv. The average Sc increased about 2.10, 4.26, and 1.62 times, respectively, for the slopes with SS of 8 • , 15 • , and 25 • when RI increased from 0.5 to 2.5 mm/min. The erosion form changed from a transporting limitation to a detaching limitation when RI increased, to some extent because of the soil's inherent susceptibility to form seals [67]. more likely to transport fine sediment, because the coarse sediment is hard to activate and transport down the slopes. Surface runoff has been reported to be a key factor in controlling soil erosion on hillslopes due to its ability to detach and transport soil materials [68]. There are two erosion mechanisms: raindrop splashes and runoff washes [69]. Soil aggregates in the topsoil are destroyed by raindrop kinetic energy and then the fine-grained particles are peeled off and carried away [70]. The soil aggregates can be disrupted by quick wetting and mechanical breakdown due to raindrop hammering [71]. The strong disruption of soil materials and fast formation of crusts on the surface are related to the increasing RI. Sr has a positive correlation to RI, and the average Sc is positively interrelated to both RI and SS (Table 1). The accumulative SL also positively correlates with the increasing RI and SS, with a range of 74.50-5857.25 g. The increasing times of total SL on the slopes with SS of 8°, 15°, and 25° were, respectively, 15.93, 28.17, and 13.85 when RI increased from 0.5 to 2.5 mm/min (Table 1). Figure 5 shows that the sediment yield is positively linearly related to total the Rv on various slopes (R 2 > 0.93). The average Sc also positively correlates with RI (R 2 > 0.83) and the order of the average Sc under different slopes is 25° > 15° > 8° when RI is uniform, indicating that the increasing sediment rate is faster than that of runoff generation. These results are similar to the findings of Tuset et al. [72], who found that the fluctuations of suspended Sc are strongly correlated to runoff magnitude and the amounts of eroded sediment correlate to Rv. The average Sc increased about 2.10, 4.26, and 1.62 times, respectively, for the slopes with SS of 8°, 15°, and 25° when RI increased from 0.5 to 2.5 mm/min. The erosion form changed from a transporting limitation to a detaching limitation when RI increased, to some extent because of the soil's inherent susceptibility to form seals [67].  Both total Rv and SL present positively linear relationships with V, Re, Fr, τ, an ( Figure 6). However, the linear fitting effects between τ, w, and total Rv are not very h Specifically, the correlations between total Rv and V (R 2 = 0.88), Re (R 2 = 0.81) are be than that between total SL and V (R 2 = 0.75), Re (R 2 = 0.70). On the contrary, correlat between total SL and Fr (R 2 = 0.82), τ (R 2 = 0.74), w (R 2 = 0.91) are better than between t Rv and Fr (R 2 = 0.76), τ (R 2 = 0.14), w (R 2 = 0.30). These results indicate that these hydra Both total Rv and S L present positively linear relationships with V, Re, Fr, τ, and w ( Figure 6). However, the linear fitting effects between τ, w, and total Rv are not very high. Specifically, the correlations between total Rv and V (R 2 = 0.88), Re (R 2 = 0.81) are better Water 2021, 13, 3453 9 of 16 than that between total S L and V (R 2 = 0.75), Re (R 2 = 0.70). On the contrary, correlations between total S L and Fr (R 2 = 0.82), τ (R 2 = 0.74), w (R 2 = 0.91) are better than between total Rv and Fr (R 2 = 0.76), τ (R 2 = 0.14), w (R 2 = 0.30). These results indicate that these hydraulic parameters are good indicators of total S L . The soil particles are more easily transported by runoff with stronger τ and w and faster V under heavier rainfalls. Field simulation experiments by Tian et al. [73] stated that the most sensitive hydrodynamic parameters to S L are τ and w. Sajjadi and Mahmoodabadi [49] concluded that V is a better parameter to use when predicting Sc than w and τ. In this study, Re is the most highly correlated parameter with total S L , which is, in some respects, consistent with the findings of Guo, Ma, Cai, and Wu [34]. Taking the comprehensive effects of RI, SS, and surface runoff hydraulics on the erosion process into consideration, a multiple regression analysis was conducted to determine the relationships between S L and RI, SS, V, h, Re, Fr, τ, and w. The relationships can be expressed by the following formula: where S L is the sediment load, g; SS is the slope steepness, m/m; RI is the rainfall intensity, mm/min; V is the runoff velocity, 10 −2 m/s; h is the runoff depth, mm; Re is the Reynolds number; Fr is the Frounde number; τ is the hydraulic shear stress, 10 −2 N/m 2 ; w is the stream power, N/m/s; n is the number of the samples. Equation (8) shows that the relationships can be described by a linear equation with a determination coefficient (R 2 ) larger than 0.96.
Water 2021, 13, x FOR PEER REVIEW 10 of 17 Figure 6. Relationships between runoff volume, sediment load, and different hydraulic parameters.

Characteristics of Sediment Size
The PSD of eroded sediment is affected by many factors including soil properties, such as texture and clay content [23]; soil nature, e.g., soil aggregates, moisture, and particle size [17]; the rainfall nature, e.g., intensity and duration [60]; and runoff types, e.g., shallow flow and rill flow [27]. The soil texture has been reported to be one of the most predominant factors affecting the PSD of eroded sediment [24,74]. The temporal and spatial variability of eroded sediment PSD depends on the main factors impacting the erosion process. A better understanding of the process of sediment transportation and the characteristics of size selectivity can increase our understanding of the functions and interactions of these different factors. In this study, the percentages of PSD for eroded sediment present an order of clay (<0.002 mm) > silt (0.002-0.02 mm) > fine sand (0.02-0.25 mm) > coarse sand (0.25-2 mm) when RI and SS are determined, which is the opposite of the original Figure 6. Relationships between runoff volume, sediment load, and different hydraulic parameters.

Characteristics of Sediment Size
The PSD of eroded sediment is affected by many factors including soil properties, such as texture and clay content [23]; soil nature, e.g., soil aggregates, moisture, and particle size [17]; the rainfall nature, e.g., intensity and duration [60]; and runoff types, e.g., shallow flow and rill flow [27]. The soil texture has been reported to be one of the most predominant factors affecting the PSD of eroded sediment [24,74]. The temporal and spatial variability of eroded sediment PSD depends on the main factors impacting the erosion process. A better understanding of the process of sediment transportation and the characteristics of size selectivity can increase our understanding of the functions and interactions of these different factors. In this study, the percentages of PSD for eroded sediment present an order of clay (<0.002 mm) > silt (0.002-0.02 mm) > fine sand (0.02-0.25 mm) > coarse sand (0.25-2 mm) when RI and SS are determined, which is the opposite of the original soil order (Figure 7). The eroded sediment is principally composed of silt-and clay-grained particles that account for about 65.41-73.41% of the total S L . There is a boundary point at 0.02 mm for the PSD of eroded sediment because the percentages of sand-grained particles (0.02-2 mm) generally increased with the increasing RI, while that of clay-and silt-grained particles regularly decreased. However, there is no notable regularity of PSD among slopes with different SSs under the uniform RI. The Er of various sediment particles under different experimental conditions can prove the existence of a grading limitation of 0.02 mm for sediment transportation (Figure 8). The Er of sand-grained particles are all <1 with a range of 0.45-0.65, while that of clay-and silt-grained particles are >1 with a range of 1.37-1.80. The Er of clay and silt particles are negatively related to SS, whereas the Er of sand-grained particles present no notable regularity related to SS. The results of Er for siltand clay-grained particles are similar to the findings of Lin et al. [75] with a range of 1.1-1.4, indicating a more severe depletion for silt-and clay-grained particles in the original soil. However, the Er of sand-grained particles is inconsistent with their corresponding results and the main interpretation might be due to the difference in experimental conditions and setup. Other studies have found that eroded sediment presents bimodal distributions in that particles with both large and small grains are easily transported, while the particles with intermediate-sized grains are not migrated [10,58]. In theory, fine-grained particles mostly gather in aggregates because of soil cohesion, while coarser particles are large enough to be moved without forming aggregates [6]. To some extent, the clay-and silt-grained particles are difficult to peel away and transport due to their agglomerate structure. Fine-grained particles become available for transportation and enrichment when the rainfall energy is high enough to break soil aggregates; however, coarse particles with high resistance are not easily displaced and transported during the erosion process [23]. The increasing RI and level of raindrop energy led to an increase in the proportions of sand-grained particles; this phenomenon is more pronounced on the steeper slopes. Large raindrops increased the detachment of soil particles and the transporting capacity of the surface runoff. This demonstrates that soil aggregates can be broken down into smaller masses and transported in a suspension, accounting for the notably higher proportion of fine-grained particles in the eroded sediment than the original soil. In contrast with the results of this study, some research has shown that the particles in the eroded sediment are mostly consistent with the original soil, or even coarser [58]. The process of sediment transportation is not only determined by the amount of raindrop energy, but also by the physico-chemical properties of the original soil [76]. The sand-grained particles may be relocated on the downward slopes during the transporting process even after they have been dragged and are unable to migrate significant distances. Raindrop splashes induced a particle cloud in the surface runoff, and the suspended particles might have been relocated on the slopes when the sedimentation velocity was faster than the flow velocity. The moving distance of the transported particles is determined by the runoff velocity, the sedimentation rate, and flowing height of the particles [53]. Overall, the transporting capacity of the rainfall runoff in this study is very strong due to the weak cohesive force between soil particles and the combination of heavy rainfalls and steep slopes in the weathered granite area, making the eroded sediment easy to transport. pended particles might have been relocated on the slopes when the sedimentation velocity was faster than the flow velocity. The moving distance of the transported particles is determined by the runoff velocity, the sedimentation rate, and flowing height of the particles [53]. Overall, the transporting capacity of the rainfall runoff in this study is very strong due to the weak cohesive force between soil particles and the combination of heavy rainfalls and steep slopes in the weathered granite area, making the eroded sediment easy to transport.  The MWD is calculated in order to reconsider PSD, reflecting the stability of the original soil [10]. The MWD of the eroded sediment shows positively linear relationships with distances. Raindrop splashes induced a particle cloud in the surface runoff, and the suspended particles might have been relocated on the slopes when the sedimentation velocity was faster than the flow velocity. The moving distance of the transported particles is determined by the runoff velocity, the sedimentation rate, and flowing height of the particles [53]. Overall, the transporting capacity of the rainfall runoff in this study is very strong due to the weak cohesive force between soil particles and the combination of heavy rainfalls and steep slopes in the weathered granite area, making the eroded sediment easy to transport.  The MWD is calculated in order to reconsider PSD, reflecting the stability of the original soil [10]. The MWD of the eroded sediment shows positively linear relationships with The MWD is calculated in order to reconsider PSD, reflecting the stability of the original soil [10]. The MWD of the eroded sediment shows positively linear relationships with RI (R 2 > 0.95) with a range of 0.15-0.20 mm (Figure 9). The differences between the maximum and minimum values of MWD on slopes with SS of 8 • , 15 • , and 25 • become smaller and are, respectively, 0.045, 0.026, and 0.014 mm. The MWD of the eroded sediment is far less than that of the original soil (0.31 mm), indicating that a greater number of fine-grained particles are enriched in the eroded sediment by interrrill erosion. The correlations between the Er of various sediment particles, MWD, and different hydraulic parameters were analyzed (Table 3). There are positive correlations among Er1 (0.25-2 mm), Er2 (0.02-0.25 mm), MWD, and different hydraulic parameters, while negative correlations are observed for Er3 (0.002-0.02 mm) and Er4 (<0.002 mm). The MWD correlations are extremely significant among RI, V, Re, Fr, and Er. For τ, the correlation is only significant for Er3. Regarding h and SS, the correlations are not significant. The MWD is also found to positively correlate with the different hydraulic parameters; the correlation between h and SS is the weakest. Some studies analyzed the Er3 and Er4 of eroded sediment by comparing to the undisturbed soil, concluding that that the eroded sediment becomes coarser and more stable as rainfall duration increases [10]. It is commonly speculated that clay-and silt-grained particles accumulate at the beginning of rainfall. The approximate threshold of transportation between suspension/saltation and bed loading can be identified by the size classification and minimum transporting rate [9,69]. Hao, Wang, Guo, and Hua [19] found that the aggregates <0.05 mm are preferentially moved by suspension/saltation while those between 0.105 and 0.25 mm are usually resistant to runoff transportation. Loch and Donnollan [77] also concluded the transitional size variation of 0.125-0.25 mm from suspension/saltation to bed loading. Leguedois et al. [78] reported that particles ≥0.05 mm are carried away in the form of individual airborne particles, while those <0.05 mm are moved in aggregates. The research performed by Asadi, Moussavi, Ghadiri, and Rose [58] indicated that the critical range of size classes for bed loading is 0.18-0.38 mm in the fluvial sand, while it is 0.5-1.0 mm in the forest soil. Studies by Harchegani, Sadeghi, and Asadi [1] and Wang and Shi [79] reached findings that were similar to the critical point of 0.063 mm for the depletion/enrichment of sediment particles by interrill erosion. The differences between these results may be attributed to varying soil textures, causing different erodibility and rainfall characteristics with different hydraulic parameters [74]. Another interpretation is that the grading criteria and operating methods are different. Altogether, the actual grading limitation of the transporting mechanisms between suspension/saltation and bed loading depends on both the soil properties and hydraulic characteristics. Further tests that investigate sediment size characteristics with more detailed classifications should be conducted to specifically discover the accurate grading limitation. Furthermore, effective conservation practices should be taken into consideration to mitigate soil and water losses from the bare hillslopes of weathered granite, since heavy rainfalls mostly have a high probability of occurrence in these areas, particularly those with intensive agricultural practices. and silt-grained particles accumulate at the beginning of rainfall. The approximate threshold of transportation between suspension/saltation and bed loading can be identified by the size classification and minimum transporting rate [9,69]. Hao, Wang, Guo, and Hua [19] found that the aggregates <0.05 mm are preferentially moved by suspension/saltation while those between 0.105 and 0.25 mm are usually resistant to runoff transportation. Loch and Donnollan [77] also concluded the transitional size variation of 0.125-0.25 mm from suspension/saltation to bed loading. Leguedois et al. [78] reported that particles ≥0.05 mm are carried away in the form of individual airborne particles, while those <0.05 mm are moved in aggregates. The research performed by Asadi, Moussavi, Ghadiri, and Rose [58] indicated that the critical range of size classes for bed loading is 0.18-0.38 mm in the fluvial sand, while it is 0.5-1.0 mm in the forest soil. Studies by Harchegani, Sadeghi, and Asadi [1] and Wang and Shi [79] reached findings that were similar to the critical point of 0.063 mm for the depletion/enrichment of sediment particles by interrill erosion. The differences between these results may be attributed to varying soil textures, causing different erodibility and rainfall characteristics with different hydraulic parameters [74]. Another interpretation is that the grading criteria and operating methods are different. Altogether, the actual grading limitation of the transporting mechanisms between suspension/saltation and bed loading depends on both the soil properties and hydraulic characteristics. Further tests that investigate sediment size characteristics with more detailed classifications should be conducted to specifically discover the accurate grading limitation. Furthermore, effective conservation practices should be taken into consideration to mitigate soil and water losses from the bare hillslopes of weathered granite, since heavy rainfalls mostly have a high probability of occurrence in these areas, particularly those with intensive agricultural practices.   Note: SS is slope steepness; RI is rainfall intensity; V is mean flow velocity; h is mean runoff depth; Re is Reynolds number; Fr is Frounde number; τ is hydraulic shear stress; w is stream power. Er1 to Er4 are the Enrichment ratio of sediment particles, respectively, for 0.25-2, 0.02-0.25, 0.002-0.02, <0.002 mm; T 0 is the occurring time of surface runoff and sediment yield; Sc is sediment concentration; I is the runoff coefficient; MWD is mean weight diameter. *, the correlation is significant at a confidence level of 0.05, n = 15; **, the correlation is significant at a confidence level of 0.01, n = 15.

Conclusions
The characteristics of runoff and sediment yield in relation to different hydraulic parameters were analyzed based on the method of artificial rainfall simulation. The results suggested that the impact of RI on runoff and sediment yield was stronger than that of SS. T 0 was shortened because the experimental soil was more quickly pre-saturated and V became faster in heavier rainfalls on steep slopes. All the hydraulic parameters