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Article

Determining the Distribution and Interaction of Soil Organic Carbon, Nitrogen, pH and Texture in Soil Profiles: A Case Study in the Lancangjiang River Basin, Southwest China

by
Wenxiang Zhou
,
Guilin Han
*,
Man Liu
,
Jie Zeng
,
Bin Liang
,
Jinke Liu
and
Rui Qu
Institute of Earth Sciences, China University of Geosciences (Beijing), Beijing 100083, China
*
Author to whom correspondence should be addressed.
Forests 2020, 11(5), 532; https://doi.org/10.3390/f11050532
Submission received: 5 April 2020 / Revised: 7 May 2020 / Accepted: 8 May 2020 / Published: 10 May 2020
(This article belongs to the Special Issue Organic Carbon Pools and Storage in Forest Soil)
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Abstract

:
The profile distributions of soil organic carbon (SOC), soil organic nitrogen (SON), soil pH and soil texture were rarely investigated in the Lancangjiang River Basin. This study aims to present the vertical distributions of these soil properties and provide some insights about how they interact with each other in the two typical soil profiles. A total of 56 soil samples were collected from two soil profiles (LCJ S-1, LCJ S-2) in the Lancangjiang River Basin to analyze the profile distributions of SOC and SON and to determine the effects of soil pH and soil texture. Generally, the contents of SOC and SON decreased with increasing soil depth and SOC contents were higher than SON contents (average SOC vs. SON content: 3.87 g kg−1 vs. 1.92 g kg−1 in LCJ S-1 and 5.19 g kg−1 vs. 0.96 g kg−1 in LCJ S-2). Soil pH ranged from 4.50 to 5.74 in the two soil profiles and generally increased with increasing soil depth. According to the percentages of clay, silt, and sand, most soil samples can be categorized as silty loam. Soil pH values were negatively correlated with C/N ratios (r = −0.66, p < 0.01) and SOC contents (r = −0.52, p < 0.01). Clay contents were positively correlated with C/N ratios (r = 0.43, p < 0.05) and SOC contents (r = 0.42, p < 0.01). The results indicate that soil pH and clay are essential factors influencing the SOC spatial distributions in the two soil profiles.

1. Introduction

Soil that is the largest carbon pool in the terrestrial ecosystem owns a strong ability to store organic carbon, which is critical for mitigating global warming caused by increasing atmospheric CO2 [1,2]. Soil strongly interacts with atmosphere and plant which makes soil an important role in regulating the global carbon cycle [3]. Against the background of global warming, learning about the distribution characteristics of soil organic carbon (SOC) in soils helps to determine the response of SOC on climate change. Moreover, soil C/N ratio (SOC to SON ratio) is an important indicator for the decomposition of SOM and often adopted to assess the quality of SOM: SOM that owns low C/N ratio is more easily to be decomposed and utilized by microorganisms [4]. It’s accepted that soil C/N ratio can significantly influence rice yield by changing the utilization efficiency of SON, thus it has been more concerned in agricultural management [5]. Therefore, studying the distribution characteristics and influencing factors of SOC and SON is essential in providing a reference for the development of soil management strategies.
The distributions of SOC and SON are influenced by many factors, including soil pH and soil texture. Although soil pH was generally thought not to influence the mineralization processes of SOM, the decomposition and nitrification processes of SOM are quite sensitive to soil pH [6,7]. Soil pH was reported to regulate a series of soil processes, such as SOM turnover, nutrient bioavailability and microbial activity, through which soil pH greatly affects the decomposition of SOM [8]. Soil texture refers to the soil particle size distributions (including clay, silt and sand) and is believed to be essential for understanding soil physicochemical properties in the terrestrial ecosystems [9,10]. Generally, clay and fine silt particles can protect SOM from being decomposed by a physical or chemical way due to their high surface activity and large specific surface area [11]. However, the effects of these fine particles on the accumulation and decomposition of SOM are different in different ecosystems, making it necessary to explore the specific influence of clay on SOM in different regions [10,11].
Lancangjiang River Basin is an undeveloped region where the intensity of human interference is quite low, making it a great area for exploring the correlations between different soil properties [12]. However, previous studies mainly focused on dam construction and soil erosion in the local area without identifying the spatial distribution of soil properties (e.g., soil pH, soil texture) [12,13]. Considering that little research on soil properties (including soil pH and soil texture), SOC, and SON is carried out in the Lancangjiang River Basin, this study aims to: (1) learn about the vertical distribution characteristics of SOC and SON in soil profiles of Lancangjiang River Basin, (2) learn about the vertical distribution characteristics soil pH and soil texture in these soil profiles, and (3) explore the influence of soil pH and soil texture on the distributions of SOC and SON.

2. Materials and Methods

2.1. Study Area

The Lancangjiang River Basin (94°40′~102°19′ E, 21°08′~33°81′ N) is located in Southwest China, with an area of 167,400 km2 [14,15]. The Lancangjiang River Basin has various kinds of climate types, varying from subtropical and temperate to cold climate zones [16]. There are two distinctive seasons within the basin all year round, a dry season (November to April) and a rainy season (May to October) [17,18]. It’s reported that 80% of the annual precipitation is concentrated in the rainy season so the Lancangjiang River Basin is mostly dominated by dry air in the dry season [19]. With huge changes of elevation (upper reach: >4500 m; middle reach: 2500 to 5000 m; lower reach: 500–3000 m) (Figure 1), the geomorphology of the basin is mainly characterized by deep valleys and high mountains [14,20]. The unique climatic and geographical characteristics determine that most areas of this region cannot be used for agricultural production and have kept virgin vegetation coverage over these years, including coniferous forests, evergreen broad-leaved forests, and miscellaneous grass meadow [12]. According to the remote sensing maps, the main land uses in the Lancangjiang River Basin are forest lands and grasslands that are estimated to account for 47% and 44% of the total area, respectively [12,21]. Therefore, the two soil profiles in this study were dug in forestland and grassland.
Surficial lithology is an important descriptor of the earth’s surface although only partial information can be obtained due to the occupation of sediments [22]. The main surficial rock types in the study area are carbonates, metamorphic rocks of low-grade, volcanic rocks, and Paleozoic clastic rocks [14].

2.2. Soil Sampling and Analysis

A total of 56 soil samples were collected from two soil profiles (LCJ S-1, LCJ S-2) in the Lancangjiang River Basin. We selected these two soil profiles because they were derived from volcanic rock that was one of the main rock types in the study area [14]. The land covers of the soil profiles LCJ S-1 (21°56′9″ N, 100°53′24″ E) and LCJ S-2 (24°27′11″ N, 100°8′49″ E) were forest and grass, respectively. Soil profiles above 50 cm were sampled at 5 cm intervals, and below 50 cm were sampled at 10 cm intervals. The topsoil of the two soil profiles was collected from the soil layer of 0–3 cm. The specific descriptions of different horizons in the two soil profiles were shown in Table 1. The humus layer in the soil profile LCJ S-1 was around 3 cm thick while no obvious humus layer was found in the soil profile LCJ S-2. The soils in the two soil profiles have been severely weathered accompanied by the breakdown of minerals during soil forming processes. Therefore, large amounts of base cations (e.g., Ca2+, Mg2+) might be released from those minerals and leached along soil profiles, which would regulate the vertical distribution of soil pH [23,24]. On the other, the plant roots reached a depth of more than 160 cm in the soil profile LCJ S-1 (Table 1), which might exert an influence on the distributions of SOM in the soil profile. Microbes and soil fauna in subsoils were thought to participate in SOM dynamics by directly consuming SOM or indirectly changing the community compositions of soil microbes [25]. It was reported that the activities of microbes and soil fauna in the subsoil were strongly regulated by the labile organic carbon from roots which would further affect the SOM contents in subsoils [26]. Based on the field descriptions of the two soil profiles, soils in these soil profiles could be classified as Ferralsols that are mainly characterized by homogeneous texture, high weathering degree, and iron concentrations [27].
All samples are air dried sufficiently, after which plant residues and stones are picked out by passing these samples through a 2-mm sieve [29,30]. To make these dried samples homogenized for further analyses [31,32], they are ground to 200 mesh using a grinding machine (Retsch GmbH, Haan, Germany). To obtain SOC and SON contents, soil inorganic carbon and nitrogen should be eliminated with HCl and KCl solutions [33,34]. About 1 g soil powders are separately soaked in 20 mL of 0.5 M HCl and 1 M KCl solutions for 24 h. During these periods, they should be shaken frequently to make the reaction happen thoroughly. Subsequently, pure water is used to wash soil samples repeatedly to make them neutral for the benefit of the elemental analyzer. Finally, the SOC and SON contents of these soil samples are analyzed by the “Vario TOC cube” (Elementar, Langenselbold, Germany), an elemental analyzer with the precision of ±0.1% for C and ±0.02% for N. Soil pH is determined using the widely used method [35,36]: 25 mL pure water is added to 10 g soils and the mixture is stirred until they are fully mixed. Then they are left to stand for 30 min before being measured with a pH-meter whose precision was ±0.05. Before the soil particle sizes are measured, calcareous cements and organic bonding agents (e.g., carbonates, organic matter) in soils should be removed, for which 30% H2O2 and 10% HCl solutions are added to soil samples under heating condition. Finally, these soil samples are dispersed with ultrasounds and then measured with the laser particle analyzer “Mastersizer 2000” whose precision was ±1%.

2.3. Statistical Analysis

The correlation analyses between different soil properties were conducted by SPSS 20 (Statistical Package for Social Science, IBM, Armonk, NY, USA). Elevation map of the Lancangjiang River Basin were produced by ArcMap 10.0 software and other figures (including the vertical distributions of SOC, SON, soil pH, and soil texture, ternary diagram of soil texture and scatter plot between soil texture, pH and soil C/N ratio, SOC contents) were drawn by OriginPro 9.0 software.

3. Results and Discussion

3.1. Distribution Characteristics of SOC, SON, Soil pH and Soil Texture in Soil Profiles

3.1.1. Distribution of SOC, SON Contents

It was reported that the SOC and SON contents primarily depended on the compositions of parent materials, but the leaching and decomposition processes of SOM would also alter the SOC and SON contents [1,37], making it essential to explore the profile distributions of SOC, SON contents and various soil properties. As shown in Table 2, average SOC and SON contents were 3.87 g kg−1 and 1.92 g kg−1 in the soil profile LCJ S-1, 5.19 g kg−1 and 0.96 g kg−1 in the soil profile LCJ S-2, respectively. Based on the coefficient of variation, SOC contents were more variable than SON contents in the two soil profiles and both contents were distinctly variable at different depths (CV > 0.2).
Vertical distributions of SOC and SON contents in the two soil profiles were presented in Figure 2. Overall, SOC contents decreased with increasing soil depth in the two soil profiles although there was an obvious positive peak at the depth of about 100–140 cm in the soil profile LCJ S-2. Meanwhile, SON contents also showed positive peaks at the similar depths and obviously that the topsoil of LCJ S-2 had much higher SON contents. The positive peak of SOC and SON contents might result from the leaching and accumulation of organic matter along the soil profile, which was closely associated with the caly contents of soils. The SOC contents of soils above 40 cm in the two soil profiles were higher than those of deep soils, which might be attributed to the external input of organic matter. The topsoil of the two soil profiles would receive more organic matter from trees and grass because plant and soil microbe residues were the main raw materials of soil organic matter that was the main holder of SOC [38].

3.1.2. Distribution of pH and C/N Ratio

As one of the most important soil chemical properties, soil pH might influence the plant utilization of organic matter and the structure of the terrestrial ecosystem through regulating biogeochemical processes in soils and affecting other soil properties [39,40]. Overall, soil pH increased with soil depth in the two soil profiles, which was consistent with what many studies have found [38,41]. Soil pH values ranged from 4.65 to 5.56 in LCJ S-1 and 4.50 to 5.74 in LCJ S-2 (Table 2), indicating that the soils in the two soil profiles were acidic. As shown in Figure 3, soil pH values in the two soil profiles generally tended to increase with soil depth which was contrary to the distribution tendency of SOC contents. It was reported that large amounts of calcium and magnesium ions were released and leached down soil profiles during the weathering processes of bedrocks, which might lower soil pH values and attribute to the increasing pH values along soil profiles [24,42]. The opposite distribution tendency of SOC contents and pH values with soil depth denoted that there might be an interaction between them in the two soil profiles.
It has been widely reported that the materials with lower C/N ratio would be decomposed into the more mobile materials or nutrients that were easy to be utilized by plants or microorganisms [5,43]. Therefore, soil C/N ratio was an important parameter used to roughly evaluate the decomposition rates of soil organic matter [4]. Soil profiles LCJ S-1 and LCJ S-2 were covered by C3 plants and Goosegrass, whose C/N ratios were 21.52 and 30.07, respectively. The soil C/N ratios ranged from 0.40 to 14.84 in LCJ S-1, 3.36 to 16.78 in LCJ S-2 (Table 2), which were obviously lower than those of the surface plants. As shown in Figure 3, the C/N ratio in both soil profiles gradually decreased as soil depth increased, indicating that SOM in deep soils was more easily to be decomposed and utilized. The distribution tendency of soil pH values and soil C/N ratios in the two soil profiles was the opposite, which indicated a potential relationship between them in the two soil profiles.

3.1.3. Soil Texture

According to the American soil classification system, all soil particles could be classified into clay (<0.002 mm), silt (0.002–0.05 mm) and sand (>0.05 mm). The average percentages of these components were 15%, 68% and 17% in LCJ S-1, 12%, 63% and 25% in LCJ S-2, respectively (Table 2). The CV values (Coefficient of variation) of clay and sand percentages were much higher than those of silt percentages (Table 2), suggesting that the variation degree of clay and sand was much higher than that of silt in the two soil profiles. According to the percentages of clay, silt and sand (Figure 4), nearly all soil samples could be categorized as silty loam, indicating that most soil samples in the soil profiles were rich in silt.
The vertical distributions of clay, silt and sand percentages in the two soil profiles were shown in Figure 5. Overall, the percentages of clay and silt decreased with soil depth while sand percentages showed the opposite distribution tendency in the two soil profiles. Soil texture of topsoil was influenced by many external factors, such as the soil pedogenesis caused by low rainfall and soil erosion [3]. The weathering degree of topsoil was greater than that of deep soils (Table 1), which might be an important reason for the decreasing percentages of clay and silt along soil profiles [44]. On the other hand, soil erosion triggered by water could be considered as the other reason for the phenomenon that the clay percentages in topsoil were higher than those in deep soil layers. It was reported that silt and clay were little influenced by soil erosion processes triggered by rainfall due to their aggregate structures [45]. Moreover, soil particles whose particle sizes ranged from 0.25 to 0.5 mm and from 0.2 to 0.25 mm might be the most and the second most erodible components in soils [9].

3.2. Effects of Soil pH and Soil Texture on the C/N Ratio

The decomposition of SOM might have been influenced by many soil properties, such as soil texture, soil pH and soil moisture content [46]. Soil C/N ratio might be an essential parameter in denoting soil decomposition processes and generally, SOM with lower C/N ratio would be decomposed into more mobile materials or nutrients that were easy to be utilized [43]. As shown in Figure 6, soil pH values were significantly negatively correlated with soil C/N ratios (r = −0.66, p < 0.01) while clay contents were positively correlated with soil C/N ratios (r = 0.43, p < 0.05) in the soil profile LCJ S-1. Because the SON contents of most samples in the soil profile LCJ S-2 were quite low (near the detection limit of Vario TOC cube), the soil profile was not included to ensure the accuracy of data analyses. The mathematical analysis result showed that the C/N ratios of SOM were significantly correlated with soil pH and clay contents in these two soil profiles. The result revealed a potential relationship between soil pH and the decomposition of SOM, denoting that soil pH might play an important role in regulating the decomposition processes. It was reported that soil pH can apparently influence the bacterial community structures and the changes in soil pH might cause the variations of microorganism’s diversity [47,48]. In terrestrial ecosystems, the decomposition of SOM depended almost entirely on microorganisms [5,38,49]. Therefore, soil pH might exert an influence on C/N ratios by altering the utilization of carbon and nitrogen by microorganisms in the two soil profiles. Meanwhile, soil C/N ratio was also regarded as an important factor that influenced the structure of soil microorganisms [5]. It could be referred that soil pH influenced the decomposition of SOM by controlling the activities of soil microorganisms to affect the C/N ratio of SOM in the two soil profiles. On the other hand, soil pH was reported to affect soil C/N ratios directly through changing plant litter quality, which might be the main mechanism by which soil pH affected soil C/N ratios in deep soils because the activities of microorganisms were expected to be lower in deep soils [7]. Overall, relatively higher soil pH values might accelerate the depletion of SOM when soil pH ranged from 4.50 to 5.74 in the two soil profiles based on the relationship between soil pH and soil C/N ratio.
Soil texture was also considered as an important factor influencing the decomposition of organic matter. Generally, it was reported to be more difficult for SOM associated with clay fraction to be decomposed because finer particles had stronger surface adsorption [50,51]. In this study, clay contents were positively correlated with C/N ratios (r = 0.43, p < 0.05) in the soil profile LCJ S-1 (Figure 6), indicating that the existence of clay could make SOM less easy to be decomposed and increase the SOM contents in soil profiles. Soil texture (especially the content of clay) was thought to have great influences on the microbial biomass and stabilization of SOM [46,52]. Based on the correlation analysis between clay contents and soil C/N ratio, it can be concluded that clay might reduce the decomposition of SOM and enhance SOC contents in the soil profile LCJ S-1.

3.3. Effects of Soil pH and Soil Texture on SOC Contents

As shown in Figure 7, soil pH was significantly negatively correlated with SOC contents (r = −0.52, p < 0.01), indicating that relatively lower soil pH values might benefit the accumulation of SOC in the two soil profiles. According to the correlation between soil pH and soil C/N ratio, one potential mechanism by which soil pH affected SOC contents was to affect the decomposition processes of SOM. On the other hand, the accumulation of SOM would acidize soils which might also contribute to the negative correlation between SOC contents and soil pH values in the two soil profiles [38,53]. The positive correlation between SOC contents and clay contents showed that more clay in soils might benefit the accumulation of SOM in the two soil profiles. It was reported that clay might affect SOM contents by forming stable complexes with organic materials and these organo-mineral complexes might be decomposed in relatively low rates [54,55]. Therefore, the leaching processes of SOM along soil profiles might be reduced with higher clay contents due to the adsorption of SOM complexes by clay. Based on these statistical analyses and the distribution characteristics of SOC and SON contents, soil pH and clay contents were most likely to affect the distribution of SOC along with the two soil profiles by regulating the decomposition and leaching processes of SOM.

4. Conclusions

Average SOC and SON contents were 3.87 g kg–1 and 1.92 g kg−1 in the soil profile LCJ S-1 and 5.19 g kg−1 and 0.96 g kg−1 in the soil profile LCJ S-2. Generally, SOC contents tend to decrease with soil depth which may result from that the topsoil of soil profiles can receive organic matter from plant and animal residues. Soil pH values range from 4.50 to 5.74 in these two soil profiles and tend to increase with soil depth. The accumulation of SOM may lower soil pH which might result from that organic acids are produced during the decomposition processes of SOM. Soil C/N ratios tend to decrease with soil depth, indicating that the SOM in deep soils might be more mobile and easier to be utilized. The average percentages of clay, silt and sand are 15%, 68%, and 17% in LCJ S-1 and 12%, 63%, and 25% in LCJ S-2. According to the percentages of clay, silt and sand, these soil samples can be considered as silty loam. Clay percentages are higher in topsoil which might result from the greater weathering degree of topsoil and external soil erosion triggered by rainfall. The correlation analyses show that lower soil pH (4.50–5.74) and higher clay contents benefit the accumulation of SOM. Soil pH and clay mainly influence SOC contents by affecting the leaching and decomposition processes of SOM in the two soil profiles.

Author Contributions

Conceptualization, G.H. and W.Z.; methodology, G.H. and M.L.; software, M.L., J.Z., B.L. and W.Z.; validation, G.H., W.Z., M.L., J.L., and R.Q.; formal analysis, W.Z., M.L.; investigation, M.L., J.Z., B.L., J.L. and R.Q.; resources, G.H.; data curation, W.Z., M.L.; writing—original draft preparation, W.Z.; writing—review and editing, G.H., M.L.; supervision, G.H.; project administration, G.H.; funding acquisition, G.H. All authors have read and agreed to the published version of the manuscript.

Funding

This research was funded by the National Natural Science Foundation of China, grant number 41661144029 and 41325010.

Acknowledgments

The authors gratefully acknowledge Shuhao Zhang from China University of Geosciences (Beijing) for helping with the experiment treatment.

Conflicts of Interest

The authors declare no conflict of interest.

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Figure 1. Map of elevation in the Lancangjiang River Basin, Southwest China. (Data of elevation from Geospatial Data Cloud).
Figure 1. Map of elevation in the Lancangjiang River Basin, Southwest China. (Data of elevation from Geospatial Data Cloud).
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Figure 2. Vertical distribution of SOC (a) and SON (b) in soil profiles. (SON contents of soil samples below 150 cm in soil profile LCJ S-2 were lower than the instrument detection limit).
Figure 2. Vertical distribution of SOC (a) and SON (b) in soil profiles. (SON contents of soil samples below 150 cm in soil profile LCJ S-2 were lower than the instrument detection limit).
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Figure 3. Vertical distribution of soil pH (a) and C/N ratios (b) in soil profiles. (SON contents of some soil samples were lower than the instrument detection limit, so some C/N ratios weren’t obtained).
Figure 3. Vertical distribution of soil pH (a) and C/N ratios (b) in soil profiles. (SON contents of some soil samples were lower than the instrument detection limit, so some C/N ratios weren’t obtained).
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Figure 4. Ternary diagram of soil texture.
Figure 4. Ternary diagram of soil texture.
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Figure 5. Vertical distributions of clay (a), silt (b) and sand (c) percentages in soil profiles.
Figure 5. Vertical distributions of clay (a), silt (b) and sand (c) percentages in soil profiles.
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Figure 6. Liner correlation between soil pH (a), clay contents (b) and soil C/N ratio in soil profile LCJ S-1.
Figure 6. Liner correlation between soil pH (a), clay contents (b) and soil C/N ratio in soil profile LCJ S-1.
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Figure 7. Liner correlation between soil pH (a), clay contents (b) and SOC contents.
Figure 7. Liner correlation between soil pH (a), clay contents (b) and SOC contents.
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Table
Table 1. The descriptions of the two soil profiles in the Lancangjiang River Basin.
Table 1. The descriptions of the two soil profiles in the Lancangjiang River Basin.
HorizonDepth (cm)Colour 1Structure 2 TextureRoots 3Thickness (cm)Boundary 4Other Observation 5
Soil profile LCJ S-1
A0–207.5 YR 4/6Granularsilty loamM&C20A&WRich in black organic matter
B120–905 YR 6/5SBsilty loamC&M70A&WMottles (F&F&F); Fe minerals
B290–1205 YR 7/5SBsilty loamF&F30A&WMottles (F&F&F); Fe minerals
B3120–1602.5 YR 6/4SBsilty loamF&F40A&WFe minerals
B/C160–2402.5 Y 8/1SBsilty loamN80--Mottles (C&A&D)
Soil profile LCJ S-2
A0–82.5 Y 8/3Granularsilty loamM&F8C&WMottles (F&M&D)
B8–1105 YR 6/6SBsilty loamN102C&SMottles (C&A&D); Fe minerals
B/C110–2007.5 YR 5/6SBsilty loamN90--Mottles (M&A&D); granite fragments
1 The descriptions of soil color were following the Munsell Soil Color Charts [28]; 2 Code for types of soil structure was used: SB—Subangular blocky; 3 Codes for descriptions of roots were used: M&C—Many and coarse; C&M—Common and medium; F&F—Few and fine; N—None; M&F—Many and fine; 4 Codes for descriptions of boundaries were used: A&W—Abrupt and wavy; C&W—Clear and wavy; C&S—Clear and smooth; 5 Codes for descriptions of mottles were used: F&F&F—Few and fine and faint; C&A&D—Common and coarse and distinct; F&M&D—Few and medium and distinct; M&A&D—Many and coarse and distinct.
Table
Table 2. Data description for SOC, SON and other soil properties in soil profiles LCJ S-1 and LCJ S-2.
Table 2. Data description for SOC, SON and other soil properties in soil profiles LCJ S-1 and LCJ S-2.
NMinMaxMean (SD)Coefficient of Variation (CV)
SOC g kg−1300.7710.133.87 (2.94)0.76
SON g kg−1300.462.671.92 (0.42)0.22
pH304.655.565.08 (0.28)0.06
LCJ S-1C/N300.4014.842.36 (2.82)1.19
Clay %3062415 (6.06)0.41
Silt %30617468 (4.01)0.06
Sand %3043317 (9.43)0.55
SOC g kg−1261.3723.785.19 (4.27)0.82
SON g kg−1260.292.850.96 (0.67)0.70
pH264.505.744.93 (0.39)0.08
LCJ S-2C/N263.3616.787.91 (4.37)0.55
Clay %2631912 (4.88)0.40
Silt %26297963 (10.40)0.16
Sand %2646825 (14.30)0.58

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Zhou, W.; Han, G.; Liu, M.; Zeng, J.; Liang, B.; Liu, J.; Qu, R. Determining the Distribution and Interaction of Soil Organic Carbon, Nitrogen, pH and Texture in Soil Profiles: A Case Study in the Lancangjiang River Basin, Southwest China. Forests 2020, 11, 532. https://doi.org/10.3390/f11050532

AMA Style

Zhou W, Han G, Liu M, Zeng J, Liang B, Liu J, Qu R. Determining the Distribution and Interaction of Soil Organic Carbon, Nitrogen, pH and Texture in Soil Profiles: A Case Study in the Lancangjiang River Basin, Southwest China. Forests. 2020; 11(5):532. https://doi.org/10.3390/f11050532

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Zhou, Wenxiang, Guilin Han, Man Liu, Jie Zeng, Bin Liang, Jinke Liu, and Rui Qu. 2020. "Determining the Distribution and Interaction of Soil Organic Carbon, Nitrogen, pH and Texture in Soil Profiles: A Case Study in the Lancangjiang River Basin, Southwest China" Forests 11, no. 5: 532. https://doi.org/10.3390/f11050532

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