Initial pore structure of compacted loess
Figure 3a–c presents the PSDs of compacted loess specimens with the same compaction energy and different molding water contents, and the curves of compacted loess specimens with the same molding water content and different compaction degrees are presented in Fig. 3d–f. The pores in compacted loess are divided into three groups according to the pore diameter, i.e., micropores (d ≤ 200 nm), mesopores (200 nm < d ≤ 3000 nm) and macropores (d > 3000 nm). This classification is adopted to facilitate the description of the PSD variation due to changes in molding water content or compaction energy. The boundary between micropores and mesopores is 200 nm, which is identical to the boundary diameter between intra-aggregate pores and inter-aggregate pores (Xiao et al. 2022).
It is worth noting that the bimodal characteristic of the PSD is not modified no matter whether the specimen was molded at dry side or wet side of the optimum water content, all curves have two peaks. In Fig. 3a–c, at the same molding water content, the PSD of macropores varies a lot while that of micropores or mesopores changes a little with the increase of compaction energy. It can be seen that as compaction energy increases from 85 to 90% or 94%, not only the peak density decreases, the corresponding pore diameter in the range of macropores (i.e., the dominant diameter of inter-aggregate pores) reduces from 6000 nm to approximately 4000 nm or 3000 nm (see Fig. 3a). Moreover, the PSD variation of compacted loess due to changes in compaction energy is similar to that during consolidation and shearing, as reported by Li et al. (2020b); that is, the PSD of inter-aggregate pores is compressed to the left, while that of intra-aggregate pores maintains unchanged. As shown in Fig. 3d–f, at the same compaction energy, the density of macropores decreases with the increase of molding water content, meanwhile the density of mesopores increases significantly; however, there is no remarkable change in the dominant diameter of inter-aggregate pores.
Figure 4 summarizes the void ratios of micropores, mesopores and macropores (emicro, emeso, emacro) of all compacted loess specimens. It can be seen that emicro rarely changes as compaction condition varies, being consistent with that described above. At a given compaction energy, emacro decreases and emeso increases with the increasing molding water content. At a given molding water content, only emacro decreases with the increase of compaction energy. As shown in Fig. 4, at the compaction degree of 85%, as molding water content increases from 16 to 20%, emacro decreases from 0.372 to 0.343 and emeso increases from 0.230 to 0.242. At the molding water content of 16%, as compaction degree increases from 85 to 94%, emacro decreases from 0.372 to 0.168.
It is widely acknowledged that different compaction conditions (mainly refer to molding water content and compaction energy for static compaction) produce different soil microstructures (Romero et al. 1999; Alonso et al. 2013; Li et al. 2016; Cheng et al. 2020b). A microstructural state variable, ξm, introduced by Alonso et al. (2013) can be used to further analyze the microstructural variation of compacted loess; ξm = em/etotal, where, etotal is the total void ratio, and etotal is the sum of the void ratio of intra-aggregate pores (em) and the void ratio of inter-aggregate pores (eM) (Alonso et al. 2013). Since the micropores defined in this study are actually intra-aggregate pores, the boundary diameter between micropores and mesopores is identical to that between intra-aggregate pores and inter-aggregate pores, the microstructural state variable of each specimen can be obtained from its PSD. The ξm values of nine compacted loess specimens are summarized in Fig. 5. It can be observed that ξm increases with the increase of compaction energy at any molding water content. While ξm does not have a clear trend in response to the increase of molding water content. For example, at the compaction degree of 85%, ξm is almost unchanged; while at the compaction degree of 90%, ξm increases first and then decreases with the increase of molding water content. That is different from the observation of Cheng et al. (2020b) on a compacted silt; they found that ξm increases with the increasing molding water content, indicating that intra-aggregate pores are increased.
SWCC
The SWCCs of compacted loess specimens are depicted in Fig. 6. The curves are shown in terms of gravimetric water content. According to Vanapalli et al. (1996), the desaturation of a soil is commonly divided into three stages, which can be delineated by three zones on the drying SWCC, i.e., boundary effect zone, transition zone and residual zone. It shows in Fig. 6a–c that compaction energy has significant influence on the boundary effect zone. An increase in compaction energy means a decrease in void ratio. Hence, at the same molding water content, the greater the compaction degree of compacted loess specimen, the smaller the saturated gravimetric water content and air-entry value (AEV). This observation is consistent with the viewpoints of many scholars (e.g., Vanapalli et al. 1996; Birle et al. 2008). At the same molding water content, the SWCCs of compacted loess specimens with different compaction degrees tend to converge together when suction is higher than 30 kPa (see Fig. 6a–c). It suggests that compaction energy has little effect on the water retention capacity of compacted loess when suction exceeds 30 kPa. This result is similar to that obtained by Romero et al. (1999), Sreedeep and However (2006); they suggested that the water retention property of compacted soil is not affected by compaction energy and molding water content when suction exceeds a certain value. In addition, it is shown in many studies that compaction condition, wetting–drying action, freezing–thawing action, etc., only affect the SWCC in the low suction range, while the SWCC in the high suction range depends on the soil nature (such as the GSD and mineral composition) (Birle et al. 2008; Hou et al. 2020).
Figure 6e–f compares the SWCCs of compacted loess specimens with different molding water contents. It is observed that at the same compaction degree, compacted loess specimens have the same saturated gravimetric water content, that is understandable since they have the same void ratio. As molding water content increases, the AEV of compacted loess reduces slightly; for example, at the compaction degree of 85%, as molding water content increases, the AEV decreases from 10 to 8 kPa or 5 kPa (see Fig. 6e). This coincides with the results of Romero et al. (1999), Vanapalli et al. (1999) and Jiang et al. (2017). They thought it could be because the specimen with a higher molding water content has more macropores among aggregates since it has more aggregates. However, the pore structure measurement results show that macropores do not increase with the increase of molding water content (see Fig. 4). For this reason, it should be recognized that the AEV is related to the maximum diameter of pores in the specimen, which may not be accurately determined by MIP since too large pores (greater than 360 μm theoretically) can not be detected by MIP (Vanapalli et al. 1996). Moreover, the SWCCs of compacted loess specimens with the same compaction degree intersect at a suction, above which the curve of the specimen with a lower molding water content is below that of the specimen with a higher molding water content. It suggests that the latter has a smaller desorption rate and a higher water retention capacity than the former at the same suction.
The relationship between SWCC and initial pore structure
The equation proposed by van Genutchen (1980) was used to fit the SWCC data obtained in this study:
$$\begin{array}{*{20}c} {\theta = \theta_{r} + \frac{{\theta_{s} - \theta_{r} }}{{\left[ {1 + \left( {\alpha s} \right)^{n} } \right]^{m} }}} \\ \end{array}$$
(1)
where, θ is the volumetric water content; θs is the saturated volumetric water content; θr is the residual volumetric water content; s is the suction; α, m and n are fitting parameters, α relates to the inverse of AEV; that is to say, α increases with the decrease of AEV.
Figure 7 presents the correlations between the SWCC fitting parameters (α, m, n), microstructural parameters (etotal, emacro, emeso, emicro, ξm) and compaction condition (dry density, molding water content) obtained on the basis of multivariate statistical analysis. The closer the correlation coefficient to 1, the stronger the correlation. On the one hand, it can be observed that, α is negatively correlated with dry density while the coefficient is only −0.40. On the other hand, α is positively correlated with molding water content, with a correlation coefficient of 0.86. That is consistent with the observation that the AEV reduces slightly with the increase of molding water content. The fitting parameter m is negatively correlated with molding water content, with a correlation coefficient of −0.87. These suggest that the AEV and the shape of SWCC of compacted loess depend mainly on molding water content. That is different from the result of Zhao et al. (2017), they showed that void ratio or dry density has more significant effect on the shape of SWCC. It is worth noting that dry density is negatively correlated with etotal and emacro, and there is a close relationship between molding water content and emeso, and there is no significant connection found between emicro and molding water content or dry density.
Microstructural evolution of compacted loess during drying
The PSDs of compacted loess specimens with different compaction degrees or molding water contents dried to six suctions (i.e., 3, 6, 50, 100, 200 and 400 kPa) are presented in Fig. 8. Similarly, drying or suction increase does not modify the bimodal characteristic of the PSD of compacted loess. The densities of mesopores and micropores in compacted loess specimens are little varied, and changes in the density of macropores are notable. This is similar to the observation of Cai et al. (2020) on a compacted red soil. Their results showed that intra-aggregate pores are almost unchanged during drying, while the density of inter-aggregate pores is affected evidently; the dominant diameter of inter-aggregate pores increases gradually with the increase of suction, meanwhile, the peak density corresponding to the dominant diameter of inter-aggregate pores grows during drying. In comparison, a clear trend could not be identified for the density of macropores from the results of this study, see Fig. 8. That is to say, the effect of drying or suction increase on the PSD of compacted loess under null pressure condition is weak and uncertain. This difference might be due to the difference in soil type. Red soil is a clayey soil, while the loess studied in this paper is a silt, the former soil is more sensitive to suction change. The study carried out by Fu et al. (2011) showed that during drying or wetting, the volumetric change of soil was very small in the low suction range, about 0.5% of the total volume. In addition, Hou et al. (2020) and Li (2021) reported that under the null pressure condition, the volume change of compacted loess is very small during either drying or wetting.
The variations of the void ratios of three pore families (micropores, mesopores and macropores) due to suction increase are presented in Fig. 9. It can be seen that as suction increases, the void ratios of micropores and mesopores are almost unchanged, and changes in the void ratio of macropores are obvious relatively. This further illustrates that larger pores are more sensitive to suction change. In addition, the total intrusion void ratios of specimens at different suctions are close (see Fig. 8d, 9b). Ying et al. (2021) also found that the variation of the void ratio of macropores in a lime-treated silt was relatively obvious while the total intrusion void ratio is basically unchanged with the increasing suction during drying.
Effect of drying on the fractal dimension of compacted loess
The fractal dimension is an important parameter that can be used to quantitatively characterize the complexity or roughness of the pore surfaces in porous media (Zhang et al. 1995). Several models have been proposed to determine the fractal dimension of soil as its PSD is known. One of the models, proposed by Zhang et al. (1995), assumes that in the process of mercury intrusion, the work done by the applied pressure on mercury is equal to the increase in the surface energy of mercury. The fractal dimension can be determined following the equations below:
$$\begin{array}{*{20}c} {\ln \left( {W_{n} /r_{n}^{2} } \right) = D_{f} lnQ_{n} + C} \\ \end{array}$$
(2)
$$\begin{array}{*{20}c} {W_{n} = \mathop \sum \limits_{i = 1}^{n} P_{i} \Delta V_{i} } \\ \end{array}$$
(3)
$$\begin{array}{*{20}c} {Q_{n} = V_{n}^{1/3} /r_{n} } \\ \end{array}$$
(4)
where, Wn is the cumulative surface energy; Vn is the cumulative intrusion volume of the nth intrusion; Qn is the function of pore radius (rn) and Vn; Pi and Vi are the intrusion pressure and the corresponding volume during the ith intrusion; C is a constant associated with the surface tension and contact angle between soil particle and mercury; Df is the fractal dimension.
Figure 10 presents how the fractal dimensions of specimens at different suctions were determined. It can be seen that the relationship between ln(Qn) and ln(Wn/rn2) is linear, with a slope basically unchanged in the whole measurable range of pore diameter. The ln(Qn)−ln(Wn/rn2) curve can be well fitted by a straight line, with the deviation parameter greater than 0.99; the slope of the straight line is the fractal dimension of compacted loess specimen according to Eq. 1. It means that there is only one fractal interval in the whole measurable range of pore diameter; in other words, there is only one fractal dimension. It can be found in Fig. 10 that the slope of the straight line increases gradually with the increase of suction. That is to say, the fractal dimension of compacted loess is increasing in response to suction increase, the roughness of the pore surfaces is increasing during drying (Zhang et al. 1995; Sun et al. 2020). As shown in Fig. 8, changes in the PSD of compacted loess are not significant. However, when using the fractal dimension to quantitatively characterize the microstructural evolution of compacted loess, it is evidently shown that the roughness of the pore surfaces or complexity of the pore structure increases with the increase of suction during drying. From this point of view, the fractal dimension can be a supplement to the PSD; upon the analysis of both of them, the microstructural evolution of compacted loess could be interpreted comprehensively. It also suggests that although the suction increase or drying has a little effect on the pore size in compacted loess, the pore surfaces are significantly influenced. The larger the suction, the greater the roughness of the pore surfaces.
The relationship between fractal dimension and suction of compacted loess is illustrated in Fig. 10. It can be observed that the fractal dimension of compacted loess shows a good linear relationship with the logarithm of suction, and the deviation parameter is greater than 0.91. It is similar to the fractal dimension variation of compacted loess during shearing (Xiao et al. 2022). The difference is that the fractal dimension increases linearly with the increase of axial strain during shearing; while during drying, the fractal dimension increases linearly with the logarithm of suction. Sun et al. (2020) also found that the fractal dimension of compacted bentonite increases with the increase of suction. In addition, they observed from the ESEM images with large magnifications that the roughness of the pore surfaces exactly increases with the increase of suction. However, Sun et al. (2020) did not provide the relationship between suction and fractal dimension due to the limited data. However, Gao et al. (2020) investigated the variation of fractal dimension of Zhaotong lignite during drying and drew an opposite conclusion; they reported that the fractal dimension decreases with the increase of suction. It might be because they dried the specimens under 200 ℃ and 280 ℃; the high temperature may lead to a variety of physical and chemical reactions in the Zhaotong lignite studied, so that the molecules are arranged directionally, hence reducing the roughness of the pore surfaces, i.e., the fractal dimension decreases with the increase of suction.
By comparing Fig. 11b, d, it can be found that under the same level of suction, the larger the compaction degree of compacted loess, the larger the fractal dimension. This is similar to the fractal dimension variation of compacted loess with axial strain during shearing. For the shear shrinkage situation, it is known that the increase in axial strain is similar to the increase in dry density. Hence, it could be inferred that the fractal dimension increases with the shrinkage of specimens.