# Research on Quantitative Evaluation of Remote Sensing and Statistics Based on Wireless Sensors and Farmland Soil Nutrient Variability

Authors: Weishuai Ji; Yaqiu Liu
Journal: Computational Intelligence and Neuroscience
 (2022)

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## Abstract

The combination of wireless sensor networks and radio technology can form a new type of communication network. The emergence of wireless sensor networks has effectively solved the problems existing in radio technology, but traditional wireless sensor networks and radio technology networks cannot be directly applied to wireless sensors. On this basis, this paper studies the remote sensing of soil nutrient variability in agricultural land using wireless sensors. Due to traditional farmland management and agricultural systems, farmland soil nutrient variability has led to polarization: fertile soil has excess nutrients, reducing the use rate of chemical fertilizers and polluting high-quality farmland. Traditional farming methods can no longer meet the requirements, and modern technology must be used to comprehensively understand the spatiotemporal variability of soil nutrients during plant growth. Remote sensing technology has the advantages of accuracy, speed, economy, and regular monitoring. It provides new ideas and technical guarantees for soil quality evaluation in land development and consolidation projects. This paper also studies the use of statistical quantitative evaluation technology to carry out multidimensional statistical quantification of soil protection function evaluation at a given location. Finally, wireless sensor networks are used to analyze the relationship between several natural factors and quantitative estimation of soil protection. Based on wireless sensor technology, this paper studies the variability of farmland soil nutrients and statistical quantitative evaluation, hoping to lay a foundation for the development of agriculture and statistics.


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## Body

## 1. Introduction

In the past few decades, wireless sensor networks have received great attention from academia and industry. Sensor nodes communicate over a short distance through a wireless network and communicate with each other to perform tasks. For soil detection, hundreds or even thousands of sensor nodes can be used to collect data [1]. Due to the low cost of sensor nodes, constant changes in availability, and limited sensor energy, the development of routing protocols suitable for soil detection, extending the life of the network, and increasing the utilization rate are of great significance to the promotion of agricultural development [2]. On this basis, this article investigates the variability of farmland soil nutrients. China still mainly adopts traditional farmland management measures; that is, the same fertilization measures are adopted instead of considering the spatial distribution of farmland soil nutrient variability, which results in fertility [3]. The oversupply of nutrients in the plots caused unnecessary waste, while also reducing fertilizer utilization and causing large-scale agricultural nonpoint source pollution [4]. On the barren land, the supply of nutrients was limited and could not meet the growth needs of crops [5]. In view of the complex soil types and extensive soil information, traditional farmland management methods can no longer meet the requirements [6]. To achieve effective fertilization and production management, it is necessary to use modern science and technology to understand the variable characteristics of farmland nutrients. The successful application of remote sensing technology in soil organic matter monitoring, soil moisture monitoring, vegetation index, and other aspects has brought new ideas and technical guarantees for soil evaluation [7]. According to the quality of development and land consolidation and remote sensing based on the variability of soil nutrients in farmland, this paper also conducts research on statistical quantitative evaluation [8]. China continues to implement land development and consolidation projects and carries out acceptance evaluation of real estate development and consolidation projects [9]. Quantitative assessment of soil quality after completion becomes more and more important. At present, it is necessary to strengthen the research on soil quality evaluation after land consolidation. On the one hand, soil quality evaluation requires a lot of manpower, material resources, and financial resources [10]. On the other hand, the standards for soil quality evaluation are not standardized, so this work is rarely carried out [11]. At present, the evaluation of development and land consolidation mainly adopts artificial field analysis and statistical quantitative evaluation methods [12]. This kind of evaluation method cannot be comprehensively evaluated, and it is time-consuming, laborious, and costly and lacks objective comparison and the macroscopic nature of evaluation [13]. The above research can contribute to further in-depth research on quantitative science and remote sensing technology [14]. It can also enrich China’s land development and consolidation theories, accelerate the development of land development theoretical systems and the adoption and evaluation of consolidation, and promote the development of precision agriculture and digital agriculture [15].


## 2. Related Work

The literature proposes that the application of remote sensing technology to wireless sensors creates a wireless sensor network, which overcomes the limitations of traditional wireless sensor networks. The sensor node evaluates the conditions independently or in cooperation with other nodes and uses the allowed channel to complete data transmission [16]. If nutrient activity is detected in the main user’s soil, the remote sensing technology immediately leaves the current channel [17]. The literature states that agricultural land is an extremely precious natural resource, with a slow origin time, a small amount, and uneven spatial distribution [18]. From a natural point of view, its formation is affected by the five elements of parent material, biology, climate, topography, and time [19]. These five factors have their own characteristics and properties, but they collectively control the formation of soil development and characteristics from different angles [20]. The literature discusses the scheme of combining wireless sensor network technology and remote sensing technology for environmental geological monitoring of mining areas, and in view of the problems and difficulties faced by the scheme, it proposes the use of these two technologies to establish a dynamic model of vegetation net initial value productivity (NPP) in the mining area. The literature shows that the soil protection module of the remote sensing technology model conducts quantitative research on soil protection in a certain area, so that its spatial attributes are visible in three dimensions, and uses soil-based detectors to reveal the relationship between soil protection and various natural functions [21]. The literature introduces the research on the temporal and spatial variability of nutrients in the soil, which is an urgent problem to be solved in agronomy, forestry, horticulture, ecology, and other disciplines [22]. Research has also developed from qualitative research to quantitative research and expanded from the original classical statistical methods to quantitative methods. Compared with classical statistical research, variables should be purely random and statistical research should involve regional variables. The literature shows that the spatial variability of soil nutrients has a large-scale effect, and soil sampling at different scales demonstrates the corresponding spatial structure characteristics and changing laws. The spatial variability of the same trait varies greatly at different scales, and large-scale studies will examine the structural characteristics of small-scale soils. In order to accurately and systematically record soil variability, soil scholars gradually try to study the variability of soil nutrients from different perspectives.


## 3. Principles of Wireless Sensors and Remote Sensing Technology

### 3.1. Wireless Sensor

Wireless sensor networks use independent sensor nodes and wireless technology to communicate with other nodes to relay information to appropriate destinations. After the sensor node processes the data through its internal processor, it sends the integrated data to the next hop node. Research on wireless sensor networks has been conducted for more than 30 years and is rapidly expanding and improving to meet the needs of military applications.The basic idea of WSN is that the capacity of each individual sensor node is limited, but the overall performance of the entire network is sufficient to perform the required tasks. The network topology of traditional WSN is shown in Figure1.Figure 1
WSN topology.Some characteristics of wireless sensor networks are as follows: First, compared with some deterministic networks, the nodes of sensor networks are used randomly. Second, wireless sensor networks are designed for specific scenarios, so the types and numbers of sensors equipped in different scenarios are also different. For example, building monitoring requires only a small number of sensors, which can be placed separately.


### 3.2. Remote Sensing Image Processing

#### 3.2.1. Geometric Precision Correction of Images

The point selection technology provided by image registration, that is, geometric correction, includes “(image to image)” and “(image to reference map).” In this experiment, the ground control point coordinates are measured on the spot and the examples are the first two methods of selecting points.The polynomial correction model is as follows:(1)x=Fxu,v=∑i=0n∑j=0n−iaijuivj,where aij and bij are undefined coefficients, n is the polynomial order, and Fx and Fy are thedistortion correction function.


#### 3.2.2. Jurisdiction Calibration

Radiometric calibration refers to quantifying the relationship between the brightness value in the corresponding field of view of the remote sensing sensor and the digital quantitative output. Therefore, the following relationship exists between the received radiation intensity and its data value:(2)Lλ=LMAXλ−LMINλQcalmaxQcal+LMINλ,where Lλ is the radiation intensity received by the sensor (W/(m2·μm·sr)), Qcal is the gray value of the pixel, and Qcalmax is the maximum DN value.Spectral reflectivityr outside the atmosphere at each band is as follows:(3)r=πLd2Ecosθ.Here,E is the average spectral irradiance outside the atmosphere of the corresponding area (unit: W·m−2·μm−1·sr−1), d is the astronomical unit of the distance between the sun and the Earth, and ɵ is the zenith angle of the sun (unit: Rad).Atmospheric external albedoαtoa is as follows:(4)atoa=∑cirii=1,2,3,4,5,6,7.Here,ci is the weight coefficient of the i-th band.Ground albedoa is as follows:(5)a=atoa−apathτ2sw.Here, sw is the one-way transmission of the atmosphere andapath is the radiation range (value between 0.025 and 0.04).


#### 3.2.3. Correction of Radiation Errors Caused by the Sun’s Altitude

Generally, the following relationship can be used to solve the radiation error correction caused by the sun’s altitude:(6)fx,y=gx,ysinθ.In this equation,ɵ is the angle of the sun’s height, gx,y is the pixel coordinate of the sun’s image at the elevation angle, and f (x, y) is the pixel coordinate of the image obtained under direct sunlight.


#### 3.2.4. Atmospheric Correction

The goal of atmospheric correction is to eliminate these effects caused by the atmosphere and light in remote sensing images and to obtain true reflectance data of ground objects.(7)Lλ=XλA+B,(8)PTOA=πLλd2ESUNλcosθs,where Xλ is the DN value of each band, parameter A is the absolute calibration gain of the image product after radiation correction, Lλ is the brightness of each band, d is the astronomical distance between the sun and the Earth, parameter B is the calibration offset of the image product, θs is the zenith angle of the sun, and ESUN is the average solar illuminance of the outer atmosphere at wavelength λ.


## 3.1. Wireless Sensor

Wireless sensor networks use independent sensor nodes and wireless technology to communicate with other nodes to relay information to appropriate destinations. After the sensor node processes the data through its internal processor, it sends the integrated data to the next hop node. Research on wireless sensor networks has been conducted for more than 30 years and is rapidly expanding and improving to meet the needs of military applications.The basic idea of WSN is that the capacity of each individual sensor node is limited, but the overall performance of the entire network is sufficient to perform the required tasks. The network topology of traditional WSN is shown in Figure1.Figure 1
WSN topology.Some characteristics of wireless sensor networks are as follows: First, compared with some deterministic networks, the nodes of sensor networks are used randomly. Second, wireless sensor networks are designed for specific scenarios, so the types and numbers of sensors equipped in different scenarios are also different. For example, building monitoring requires only a small number of sensors, which can be placed separately.


## 3.2. Remote Sensing Image Processing

### 3.2.1. Geometric Precision Correction of Images

The point selection technology provided by image registration, that is, geometric correction, includes “(image to image)” and “(image to reference map).” In this experiment, the ground control point coordinates are measured on the spot and the examples are the first two methods of selecting points.The polynomial correction model is as follows:(1)x=Fxu,v=∑i=0n∑j=0n−iaijuivj,where aij and bij are undefined coefficients, n is the polynomial order, and Fx and Fy are thedistortion correction function.


### 3.2.2. Jurisdiction Calibration

Radiometric calibration refers to quantifying the relationship between the brightness value in the corresponding field of view of the remote sensing sensor and the digital quantitative output. Therefore, the following relationship exists between the received radiation intensity and its data value:(2)Lλ=LMAXλ−LMINλQcalmaxQcal+LMINλ,where Lλ is the radiation intensity received by the sensor (W/(m2·μm·sr)), Qcal is the gray value of the pixel, and Qcalmax is the maximum DN value.Spectral reflectivityr outside the atmosphere at each band is as follows:(3)r=πLd2Ecosθ.Here,E is the average spectral irradiance outside the atmosphere of the corresponding area (unit: W·m−2·μm−1·sr−1), d is the astronomical unit of the distance between the sun and the Earth, and ɵ is the zenith angle of the sun (unit: Rad).Atmospheric external albedoαtoa is as follows:(4)atoa=∑cirii=1,2,3,4,5,6,7.Here,ci is the weight coefficient of the i-th band.Ground albedoa is as follows:(5)a=atoa−apathτ2sw.Here, sw is the one-way transmission of the atmosphere andapath is the radiation range (value between 0.025 and 0.04).


### 3.2.3. Correction of Radiation Errors Caused by the Sun’s Altitude

Generally, the following relationship can be used to solve the radiation error correction caused by the sun’s altitude:(6)fx,y=gx,ysinθ.In this equation,ɵ is the angle of the sun’s height, gx,y is the pixel coordinate of the sun’s image at the elevation angle, and f (x, y) is the pixel coordinate of the image obtained under direct sunlight.


### 3.2.4. Atmospheric Correction

The goal of atmospheric correction is to eliminate these effects caused by the atmosphere and light in remote sensing images and to obtain true reflectance data of ground objects.(7)Lλ=XλA+B,(8)PTOA=πLλd2ESUNλcosθs,where Xλ is the DN value of each band, parameter A is the absolute calibration gain of the image product after radiation correction, Lλ is the brightness of each band, d is the astronomical distance between the sun and the Earth, parameter B is the calibration offset of the image product, θs is the zenith angle of the sun, and ESUN is the average solar illuminance of the outer atmosphere at wavelength λ.


## 3.2.1. Geometric Precision Correction of Images

The point selection technology provided by image registration, that is, geometric correction, includes “(image to image)” and “(image to reference map).” In this experiment, the ground control point coordinates are measured on the spot and the examples are the first two methods of selecting points.The polynomial correction model is as follows:(1)x=Fxu,v=∑i=0n∑j=0n−iaijuivj,where aij and bij are undefined coefficients, n is the polynomial order, and Fx and Fy are thedistortion correction function.


## 3.2.2. Jurisdiction Calibration

Radiometric calibration refers to quantifying the relationship between the brightness value in the corresponding field of view of the remote sensing sensor and the digital quantitative output. Therefore, the following relationship exists between the received radiation intensity and its data value:(2)Lλ=LMAXλ−LMINλQcalmaxQcal+LMINλ,where Lλ is the radiation intensity received by the sensor (W/(m2·μm·sr)), Qcal is the gray value of the pixel, and Qcalmax is the maximum DN value.Spectral reflectivityr outside the atmosphere at each band is as follows:(3)r=πLd2Ecosθ.Here,E is the average spectral irradiance outside the atmosphere of the corresponding area (unit: W·m−2·μm−1·sr−1), d is the astronomical unit of the distance between the sun and the Earth, and ɵ is the zenith angle of the sun (unit: Rad).Atmospheric external albedoαtoa is as follows:(4)atoa=∑cirii=1,2,3,4,5,6,7.Here,ci is the weight coefficient of the i-th band.Ground albedoa is as follows:(5)a=atoa−apathτ2sw.Here, sw is the one-way transmission of the atmosphere andapath is the radiation range (value between 0.025 and 0.04).


## 3.2.3. Correction of Radiation Errors Caused by the Sun’s Altitude

Generally, the following relationship can be used to solve the radiation error correction caused by the sun’s altitude:(6)fx,y=gx,ysinθ.In this equation,ɵ is the angle of the sun’s height, gx,y is the pixel coordinate of the sun’s image at the elevation angle, and f (x, y) is the pixel coordinate of the image obtained under direct sunlight.


## 3.2.4. Atmospheric Correction

The goal of atmospheric correction is to eliminate these effects caused by the atmosphere and light in remote sensing images and to obtain true reflectance data of ground objects.(7)Lλ=XλA+B,(8)PTOA=πLλd2ESUNλcosθs,where Xλ is the DN value of each band, parameter A is the absolute calibration gain of the image product after radiation correction, Lλ is the brightness of each band, d is the astronomical distance between the sun and the Earth, parameter B is the calibration offset of the image product, θs is the zenith angle of the sun, and ESUN is the average solar illuminance of the outer atmosphere at wavelength λ.


## 4. Statistical Quantitative Evaluation Analysis and Application Research on the Variability of Farmland Soil Nutrients

### 4.1. Principles of the Quantitative Evaluation of Soil Quality

The InVEST model is a model for evaluating ecosystem service functions. It includes three main modules and several submodules of terrestrial, freshwater, and marine ecosystems. The results of the work are visually presented in the form of a map, which helps to better understand the nature of ecosystem services. The difference between erosion and actual erosion reflects the reduction in potential erosion in each block. The latter means that the product of the amount of sand and the degree of sediment retention indicates the ability of the grid block to intercept the sediment or other sediments on the slope. The USLE equation ignores this important hydrological process. It is calculated as follows:(9)SEDRETx=RKLSx−USLEx+SEDRx,(10)PKLSx=Rx⋅Kx⋅LSx,(11)USLEx=Rx⋅Kx⋅LSx⋅Cx⋅Px,(12)SDREx=SEx∑y=0x−1,where SEx is the sediment retention efficiency in the x grid, SEDRETx and SEDRx are the soil retention and sediment retention in the x grid, and SEz is the sediment retention efficiency in the z grid. RKLSx is the potential soil loss in grid x based on terrain and climatic conditions, and USLEx and USLEy are the actual erosion values of grid x and its upstream grid y.Geographic detectors are divided into four types: factor, ecology, risk, and interaction. The factor detector is designed to detect the spatial differentiation of the dependent variable and the degree of interpretation of the spatial differentiationY, expressed by the q value, and its expression is as follows:(13)q=1−∑a=1BMncd2Mc2=1−DDEDDR,(14)DDE=∑a=1BMncd2,(15)DDR=MC2.Here,a = 1, …, B is the division of variable Y or factor X and DDE and DDR are the sum of the intralayer variance and the total variance of the entire region, respectively.Ecological detector: it is used to judge whether there are significant differences in the influence of two factors,b1 and b2, on the spatial distribution of Y attributes, which is characterized by the S statistic:(16)S=Ax1Ax2−1DDEx1Ax2Ax1−1DDEx2,(17)DDEx1=∑a=1B1Mncd2,(18)DDEx2=∑a=1B2Mncd2,where AXO and An represent the sample sizes of factors X1 and X2, respectively, and DDEn1 and DDE2 are the sum of the intralayer variances of the layer formed by X1 and X2, respectively. The null hypothesis H0 is DDEn = DDEX2. If H0 deviates from the significance level c, this means that X1 and X2 are significantly different in the spatial distribution of Y.Risk detector: it is used to determine whether there is a significant difference in the attribute mean of the two subregions and uses thet statistic to test(19)tT¯g=1−T¯g=2=T¯g=1−T¯g=2CsvT¯g=1/mg=1+CsvT¯g=2/mg=21/2,where Te is the average value of the attributes in the subdomain g, m is the number of samples in the subrange g, and Csv is the variance.


### 4.2. Soil Data Processing

#### 4.2.1. Rainfall ErosivityR Factor

The greater the precipitation erosion coefficient, the greater the intensity of soil erosion. The methods to obtain this coefficient are listed:(1)
The classic algorithm is as follows:(20)R=E×I30,whereR is the erosion activity of rain, E is the total kinetic energy of rain, and I30 is the rainfall intensity within 30 minutes.This model has extremely high requirements for data sources and must be based on a large amount of precipitation data. It has limitations in the complexity of obtaining kinetic energy and precipitation rate data, and its relatively narrow scope limits further applications.The modified formula for the calculatedR factor formula is as follows:(21)R=∑i=1121.735×101.5lgTi2/T−0.8188×17.02,whereT is the annual average rainfall (mm) and Ti is the monthly rainfall (mm).(2)
We established a power index structure daily rainfall erosivity model:(22)Rds=R∑i=1kTiλ.k represents the number of days, Ti represents the precipitation of the i-th day, Ti ≥ 12 mm is required; otherwise, the value is 0, Ty12 is the annual average rainfall with a daily rainfall ≥12 mm, and Td12 is the daily average rainfall with a daily rainfall ≥12 mm.(3)
We established the national daily replacement model (half-month rainfall erosivity model):(23)Mi=α∑j=1kDjβ.Here, Mi is the erosion activity value in thei-th half-month period (MJ·mm·hm−2·h−1), α and β are the model parameters, k represents the number of days in a half-month, and Dj represents the j-th day of the first half-month. The daily precipitation requires precipitation ≥12 mm.The numbersα and β represent model parameters reflecting the characteristics of precipitation in the area. According to the daily precipitation data, the values of α and β in the station are estimated according to(24)β=0.8363+18.144Pd12+24.455Py12,(25)∝=21.586β−7.1891.This method uses long-term continuous daily rainfall as the main unit of data. It is generally considered to be the most accurate and most representative method of the actual rainfall erosion rate, and long-term continuous data are required.According to the applicability of the model, combined with the existing meteorological and precipitation data, the final method of calculating theR factor is as follows:(26)R=∑i=11273.989×Pi2Pa0.7387.Here,R is the erosion activity value (MJ·mm·hm−2·h−1), Pi is the precipitation of the i-th month (mm), and Pa is the average annual precipitation (mm).The latitude and longitude of a certain area and its 6 surrounding counties and cities and theR value of precipitation erosion are shown in Table 1.Table 1
Information on latitude and longitude and rainfall erosivityR value of a certain area and its 6 surrounding counties and cities.
AreaLongitude (E)Dimensions (N)R factor valueArea A102.82435423.2255964834Area B102.38019623.3670384094Area C102.82344723.6313943944Area D103.23414722.7872528784Area E102.40330622.9955327806Area F103.15672823.3777924987This paper uses the monthly precipitation data of a certain region and 6 counties and cities over 35 years from 1986 to 2020 to calculate the annual value of precipitation erosivity and the value of the annual average rainfall erosivity factor.On this basis, the Kriging interpolation method was used on the GIS platform to generate anR layer based on the 6 counties from 1986 to 2020, and then, the mask was extracted to obtain the spatial distribution of the R factor of the A district and counties, as shown in Figure 2.Figure 2
Spatial distribution of theR factor of rainfall erosivity.Figure2 shows that the R value gradually decreases from south to north. There are high-value areas adjacent to the southwest and southeast of area A and high-precipitation areas D and E; a low value area appears in the dry hot area adjacent to the northwest of the valley.


#### 4.2.2. Soil ErodibilityK Factor

The soil erodibilityK factor reflects the difficulty of separating and transporting soil with different particle sizes, and the difference in the K factor reflects the sensitivity of different types of soil to erosion. The K value can be obtained by querying data, actual measurement, and calculation. The most common method for querying data is the Vischmeier nomogram. This method requires more data on soil structure coefficients and permeability levels. At present, China’s soil data are mainly based on the results of the national soil census, which is far from the data requirements. At the same time, reclamation and plowing will change the nature of the soil, so it is impractical to directly use this method. The actual measurement includes the standard battery measurement method and physical and chemical properties measurement with the highest accuracy, but time-consumption, cumbersome procedures, equipment limitations, rainfall, and other unforeseen factors are drawbacks.The spatial distribution of the soil erosionK factor in a certain area is shown in Figure 3.Figure 3
Spatial distribution of the soil erodibilityK factor in a certain area.The soil erosion factor of Zone A ranges from 0.0375116 to 0.0410254, with an average of 0.0392685. From the macrodistribution of the soil erosionK value in China’s water erosion area, it can be seen that the soil erosion coefficient K in a certain area is 0.0484–0.0091, with an average value of 0.0292; compared with this value, the calculation result of the soil erosion rate coefficient K in circle A is slightly higher than the provincial average. The north and northeast are bordered by the Yuanjiang River, with large dry heat evaporation and little precipitation. The conditions of erosion (precipitation) are not perfect, resulting in small and uniform K.


#### 4.2.3. P Factor of Soil and Water Conservation Measures

Common soil and water protection measures include reducing the slope, transforming the subsoil, and building ponds and dams. These measures mainly control soil erosion by affecting speed and flow. Among them, reducing the slope can effectively reduce water flow, and the construction of ponds and dams can adjust and reduce the flow. These measures are effective in reducing soil erosion and promoting soil protection.The calculation and verification of the soil conservation function of county A based on the InVEST model are shown in Table2.Table 2
Calculation and verification of the soil conservation function in a certain area and county based on the InVEST model.
Land use typeC valueP valuePaddy field0.060.06Dry land0.050.31Woodland0.030.99Bush0.030.99Other woodlands0.020.99High coverage grassland0.050.99Low coverage grassland0.180.99Canal0.150.01Reservoir pond0.210.01Beach0.020.06Urban land0.080.01Rural settlement0.070.01Other construction lands0.060.01The current research on theP value is mainly based on different land use types; due to the different actual conditions in the study area, the P value of the same land use type in different areas is different. When calculating the P factor, it is necessary to make extensive reference to related disciplines or similar research topics and then combine actual research to determine it. Due to its particularity, the P factor has a high degree of subjective flexibility when assigning values, so it is considered to be the most difficult to determine in the InVEST model. Area A is a mountainous area in southwest China, with a lot of deep and steep slopes, heavy rainfall, and excessive soil erosion. Soil protection measures such as afforestation, terrace construction, contour farming, and improvement of irrigation and drainage systems are adopted locally.


### 4.3. Evaluation and Characteristics of Soil Organic Matter

#### 4.3.1. Descriptive Statistical Characteristics of the Spatial Variability of Soil Nutrients at Different Scales

The statistical characteristics of soil available nutrients at different sampling scales are shown in Table3.Table 3
Statistical characteristics of soil available nutrients at different sampling scales.
ScaleVariableMin (mg·kg−1)Max (mg·kg−1)Mean (mg·kg−1)SD (mg·kg−1)SkeKursigCoefficient of variation (%)Distribution typeCountyAN9.01169.0180.8321.330.440.830.0726.37NAP1.0193.0123.0814.211.382.530.0461.48LNAK24.01553.01177.3581.761.272.120.1246.11LNFieldAN16.83126.8856.1224.610.881.030.6643.85NAP19.58133.8655.4429.081 .050.370.0652.42NAK134.08373.17252.8570.59−0.13−1.280.3227.93NPlotAN15.28264.4788.1447.721.061.580.3754.12NAP15.33153.4463.3829.230.750.340.6346.12NAK170.12669.83308.8780.420.562.860.1726.04LNIt can be seen from Table3 that on the sampling scale, AP has the highest change intensity, followed by AK, and AN has the lowest change intensity; on the field scale, AP shows the largest change intensity, followed by AN, and AK shows the smallest change intensity; on the plot scale, AN has the largest change intensity, followed by AP, and AK has the smallest change intensity.


#### 4.3.2. Spatial Autocorrelation Characteristics of the Spatial Variability of Soil Nutrients at Different Scales

The model parameters of the semivariance function soil nutrient index are shown in Table4.Table 4
Parameters of the semivariance function model of the soil nutrient index.
ScaleVariableTheoretical modelNuggetCoSillCo + CNugget/Sill (%)Range (m)Decisive factorR2Residual (RSS)CountyANExponential0.002350.0154915.13410.010.4299.73 × 10−6APExponential0.008910.0785111.33320.010.6115.68 × 10−5AKExponential0.005820.0324517.92390.010.6381.96 × 10−5FieldANGaussian0.000110.118210.09118.310.4246.16 × 10−4APExponential0.000110.040610.2655.410.9582.41 × 10−7AKGaussian0.000020.015730.07112.210.5587.57 × 10−6PlotANExponential0.002410.058614.1118.610.263.75 × 10−5APExponential0.003510.046317.5743.310.7311.58 × 10−5AKExponential0.001540.0110713.8427.610.3628.15 × 10−7At the county level, the AN, AP, and AK regions are the largest; at the field scale, the range is reduced by 118.31 m, 55.41 m, and 112.21 m, respectively; at the block scale, the range further drops to 18.61 m, 43.31 m, and 27.61 m, leading to drastic changes in small-scale soils AN, AP, and AK and significantly reducing their scope.


#### 4.3.3. Scale Effect of Spatial Variability of Soil Nutrients

The fragmentation degree of the soil available nutrient map at different sampling scales is shown in Table5.Table 5
Fragmentation degree of soil available nutrient map at different sampling scales.
ScaleVariableNumber of plaques NP (pieces)Plaque density PD (pcs:hm−2)CountyAN750.16AP1160.22AK890.17FieldAN130.23AP180.36AK140.25PlotAN481.75AP331.18AK180.71The maximum effective phosphorus PD value is 1.18, and the distribution is relatively scattered. The main reason is that AP is more susceptible to random factors, which makes AP distributions disjoint, and has obvious local characteristics.The spatial distribution of available nutrients at different sampling scales is shown in Figure4.Figure 4
The spatial distribution of available nutrients at different sampling scales. (a) At the AN sampling scale of 0–180. (b) At the AP sampling scale of 0–120. (c) At the AK sampling scale of 0–600.It can be seen from the spatial distribution of nutrients that at the county level, except for a small part that is in a barren state, the alkali hydrolyzed nitrogen is continuously distributed in the soil, and most of the rest are at an average level.The corresponding curve diagram of the measured sample point of the soil organic matter content measured at the sampling point on November 2, 2020, is shown in Figure5.Figure 5
Fitting curve of soil organic matter content and measured sample point reflectivity on November 2, 2020.y = −0.0002x2 + 0.0019x + 0.2098 (fitness:0.835).It can be seen from the obtained data that this paper adopts the method of polynomial modeling, combined with comparative experiments for research, selects one of the sample points of polynomial fitting, and uses the sample point as the control point.The adjustment curve of soil organic matter content and reflectance at the image sampling point on November 2, 2020, is shown in Figure6.Figure 6
Fitting curve of soil organic matter content and image sample point reflectivity on November 2, 2020.y = 5E − 0.5x3 + 0.0017x2 − 0.0163x + 0.2202 (fitness:0.806).We select one of the sample points for polynomial fitting and check the sampling points, and the accuracy is similar, which proves that the model is very accurate and can be used to invert the soil organic matter in the entire area.The statistical comparison table of the percentage of organic matter in a certain area in the three periods is given in Table6.Table 6
Comparison table of the percentage of organic matter content in a certain area in three periods.
Organic matter content (%)/time<10[10–20)[20–30)[30–40]>40July 17, 201416.52332.59231.0878.95810.841November 2, 20193.4076.55414.05630.07245.912June 16, 20206.66613.30410.01140.26229.756Table6 shows the distribution of organic matter content in the test area during the three time periods. The results show that the results of remote sensing inversion of organic matter are consistent with those of the organic matter content measured by field sampling. After land consolidation, the organic matter content in the experimental area is mainly distributed in the plains and above.The statistical comparison table of the percentage of organic matter in a certain area in the three periods is given in Table7.Table 7
Comparison table of the percentage of organic matter content in a certain area in three periods.
Organic matter content (%)/time<10[10–20)[20–30)[30–40]>40July 2, 200376.52710.5926.824.9241.123November 27, 201937.40746.5528.9674.7152.356June 7, 202060.66617.33413.0115.9113.075Statistics for the distribution of organic matter over the three time periods in the study area show that the remote sensing inversion results of organic matter in the defined test area are consistent with the organic matter data obtained by field sampling. It can be seen from Table7 that after land development and consolidation in a certain experimental area, soil fertility has been greatly improved, soil quality has been significantly improved, and the effect of land development and consolidation has been significant.


#### 4.3.4. BP Neural Network Inversion Model

The BP neural network is composed of input layer, hidden layer, and output layer.The cumulative credibility of the first six principal components is shown in Table8.Table 8
Cumulative credibility of the first six principal components.
Main ingredientCumulative reliability of the prediction set (%)Cumulative credibility of the validation set (%)P0199.42799.961P0299.57699.937P0399.42499.566P0499.82199.347P0599.96799.522P0699.97899.431The 26 samples in a certain experimental area are divided into a prediction set and a verification set. There are 15 sets of predictions and 9 sets of verifications. The spectral band of the sample is calculated using the full spectrum, which requires a large amount of calculation and has nothing to do with the composition of the sample. The principal component analysis method can fully reflect the information of the original multiwavelength variables and perform principal component analysis of the prediction sample and the verification set.The statistical comparison table of organic matter content in a certain area in two periods is shown in Table9.Table 9
Statistical comparison table of organic matter content in a certain area in two periods.
Organic matter content (%)/time<10[10–20)[20–30)[30–40]>40July 17, 201516.72432.49730.1779.24611.357November 2, 20203.3366.67613.34830.03746.602The inversion results in Table9 are approximately equal to the inversion results of the polynomial inversion model. The results showed that the content of soil organic matter in this area increased significantly after land consolidation, which significantly improved soil fertility and quality.


### 4.4. Research on the Analysis Method of Soil Nutrient Variability in Farmland

Research in recent years has shown that the method of combining multisource satellite images and multitemporal images with laboratory spectral analysis and ground-based in situ research is the development trend of soil organic matter measurement.Remote sensing is obviously the preferred method for estimating the surface temperature, because the main feature of remote sensing technology is that it can provide a wide range of data and images and use satellite data to calculate the surface temperature. Sensor technology is the theory and method for detecting satellite hot air duct data. At present, the remote sensing algorithms for surface temperature mainly include single-channel and multichannel satellite sensor infrared channel methods, infrared thermometer to measure surface temperature, and microwave remote sensing to monitor the surface temperature. At present, the use of infrared thermal data to monitor surface temperature is widely higher level.Soil surface evapotranspiration is an important part of both surface heat balance and ecosystem water balance. The water balance determines the quantity and spatial distribution of water resources, and the heat balance between water and soil is very large. It determines the weather and climate change, which in turn determines the soil quality and the formation and development of ecosystems. Remote sensing technology is currently used to monitor surface evapotranspiration. There are mainly single-layer models and double-layer models, especially the SEBAL model based on the principle of energy balance equation. Its outstanding advantage is that it has a strong physical foundation and is suitable for different climates. The vegetation index is a simple and effective indicator to characterize the vegetation coverage and plant growth status. In recent years, with the rapid development of remote sensing technology, the use of remote sensing technology to extract the vegetation index has been relatively expanded. In the field of ecology, the vegetation index examines ecosystems on a global scale, and the results of patch-level ecosystem research are extended to the global space.


## 4.1. Principles of the Quantitative Evaluation of Soil Quality

The InVEST model is a model for evaluating ecosystem service functions. It includes three main modules and several submodules of terrestrial, freshwater, and marine ecosystems. The results of the work are visually presented in the form of a map, which helps to better understand the nature of ecosystem services. The difference between erosion and actual erosion reflects the reduction in potential erosion in each block. The latter means that the product of the amount of sand and the degree of sediment retention indicates the ability of the grid block to intercept the sediment or other sediments on the slope. The USLE equation ignores this important hydrological process. It is calculated as follows:(9)SEDRETx=RKLSx−USLEx+SEDRx,(10)PKLSx=Rx⋅Kx⋅LSx,(11)USLEx=Rx⋅Kx⋅LSx⋅Cx⋅Px,(12)SDREx=SEx∑y=0x−1,where SEx is the sediment retention efficiency in the x grid, SEDRETx and SEDRx are the soil retention and sediment retention in the x grid, and SEz is the sediment retention efficiency in the z grid. RKLSx is the potential soil loss in grid x based on terrain and climatic conditions, and USLEx and USLEy are the actual erosion values of grid x and its upstream grid y.Geographic detectors are divided into four types: factor, ecology, risk, and interaction. The factor detector is designed to detect the spatial differentiation of the dependent variable and the degree of interpretation of the spatial differentiationY, expressed by the q value, and its expression is as follows:(13)q=1−∑a=1BMncd2Mc2=1−DDEDDR,(14)DDE=∑a=1BMncd2,(15)DDR=MC2.Here,a = 1, …, B is the division of variable Y or factor X and DDE and DDR are the sum of the intralayer variance and the total variance of the entire region, respectively.Ecological detector: it is used to judge whether there are significant differences in the influence of two factors,b1 and b2, on the spatial distribution of Y attributes, which is characterized by the S statistic:(16)S=Ax1Ax2−1DDEx1Ax2Ax1−1DDEx2,(17)DDEx1=∑a=1B1Mncd2,(18)DDEx2=∑a=1B2Mncd2,where AXO and An represent the sample sizes of factors X1 and X2, respectively, and DDEn1 and DDE2 are the sum of the intralayer variances of the layer formed by X1 and X2, respectively. The null hypothesis H0 is DDEn = DDEX2. If H0 deviates from the significance level c, this means that X1 and X2 are significantly different in the spatial distribution of Y.Risk detector: it is used to determine whether there is a significant difference in the attribute mean of the two subregions and uses thet statistic to test(19)tT¯g=1−T¯g=2=T¯g=1−T¯g=2CsvT¯g=1/mg=1+CsvT¯g=2/mg=21/2,where Te is the average value of the attributes in the subdomain g, m is the number of samples in the subrange g, and Csv is the variance.


## 4.2. Soil Data Processing

### 4.2.1. Rainfall ErosivityR Factor

The greater the precipitation erosion coefficient, the greater the intensity of soil erosion. The methods to obtain this coefficient are listed:(1)
The classic algorithm is as follows:(20)R=E×I30,whereR is the erosion activity of rain, E is the total kinetic energy of rain, and I30 is the rainfall intensity within 30 minutes.This model has extremely high requirements for data sources and must be based on a large amount of precipitation data. It has limitations in the complexity of obtaining kinetic energy and precipitation rate data, and its relatively narrow scope limits further applications.The modified formula for the calculatedR factor formula is as follows:(21)R=∑i=1121.735×101.5lgTi2/T−0.8188×17.02,whereT is the annual average rainfall (mm) and Ti is the monthly rainfall (mm).(2)
We established a power index structure daily rainfall erosivity model:(22)Rds=R∑i=1kTiλ.k represents the number of days, Ti represents the precipitation of the i-th day, Ti ≥ 12 mm is required; otherwise, the value is 0, Ty12 is the annual average rainfall with a daily rainfall ≥12 mm, and Td12 is the daily average rainfall with a daily rainfall ≥12 mm.(3)
We established the national daily replacement model (half-month rainfall erosivity model):(23)Mi=α∑j=1kDjβ.Here, Mi is the erosion activity value in thei-th half-month period (MJ·mm·hm−2·h−1), α and β are the model parameters, k represents the number of days in a half-month, and Dj represents the j-th day of the first half-month. The daily precipitation requires precipitation ≥12 mm.The numbersα and β represent model parameters reflecting the characteristics of precipitation in the area. According to the daily precipitation data, the values of α and β in the station are estimated according to(24)β=0.8363+18.144Pd12+24.455Py12,(25)∝=21.586β−7.1891.This method uses long-term continuous daily rainfall as the main unit of data. It is generally considered to be the most accurate and most representative method of the actual rainfall erosion rate, and long-term continuous data are required.According to the applicability of the model, combined with the existing meteorological and precipitation data, the final method of calculating theR factor is as follows:(26)R=∑i=11273.989×Pi2Pa0.7387.Here,R is the erosion activity value (MJ·mm·hm−2·h−1), Pi is the precipitation of the i-th month (mm), and Pa is the average annual precipitation (mm).The latitude and longitude of a certain area and its 6 surrounding counties and cities and theR value of precipitation erosion are shown in Table 1.Table 1
Information on latitude and longitude and rainfall erosivityR value of a certain area and its 6 surrounding counties and cities.
AreaLongitude (E)Dimensions (N)R factor valueArea A102.82435423.2255964834Area B102.38019623.3670384094Area C102.82344723.6313943944Area D103.23414722.7872528784Area E102.40330622.9955327806Area F103.15672823.3777924987This paper uses the monthly precipitation data of a certain region and 6 counties and cities over 35 years from 1986 to 2020 to calculate the annual value of precipitation erosivity and the value of the annual average rainfall erosivity factor.On this basis, the Kriging interpolation method was used on the GIS platform to generate anR layer based on the 6 counties from 1986 to 2020, and then, the mask was extracted to obtain the spatial distribution of the R factor of the A district and counties, as shown in Figure 2.Figure 2
Spatial distribution of theR factor of rainfall erosivity.Figure2 shows that the R value gradually decreases from south to north. There are high-value areas adjacent to the southwest and southeast of area A and high-precipitation areas D and E; a low value area appears in the dry hot area adjacent to the northwest of the valley.


### 4.2.2. Soil ErodibilityK Factor

The soil erodibilityK factor reflects the difficulty of separating and transporting soil with different particle sizes, and the difference in the K factor reflects the sensitivity of different types of soil to erosion. The K value can be obtained by querying data, actual measurement, and calculation. The most common method for querying data is the Vischmeier nomogram. This method requires more data on soil structure coefficients and permeability levels. At present, China’s soil data are mainly based on the results of the national soil census, which is far from the data requirements. At the same time, reclamation and plowing will change the nature of the soil, so it is impractical to directly use this method. The actual measurement includes the standard battery measurement method and physical and chemical properties measurement with the highest accuracy, but time-consumption, cumbersome procedures, equipment limitations, rainfall, and other unforeseen factors are drawbacks.The spatial distribution of the soil erosionK factor in a certain area is shown in Figure 3.Figure 3
Spatial distribution of the soil erodibilityK factor in a certain area.The soil erosion factor of Zone A ranges from 0.0375116 to 0.0410254, with an average of 0.0392685. From the macrodistribution of the soil erosionK value in China’s water erosion area, it can be seen that the soil erosion coefficient K in a certain area is 0.0484–0.0091, with an average value of 0.0292; compared with this value, the calculation result of the soil erosion rate coefficient K in circle A is slightly higher than the provincial average. The north and northeast are bordered by the Yuanjiang River, with large dry heat evaporation and little precipitation. The conditions of erosion (precipitation) are not perfect, resulting in small and uniform K.


### 4.2.3. P Factor of Soil and Water Conservation Measures

Common soil and water protection measures include reducing the slope, transforming the subsoil, and building ponds and dams. These measures mainly control soil erosion by affecting speed and flow. Among them, reducing the slope can effectively reduce water flow, and the construction of ponds and dams can adjust and reduce the flow. These measures are effective in reducing soil erosion and promoting soil protection.The calculation and verification of the soil conservation function of county A based on the InVEST model are shown in Table2.Table 2
Calculation and verification of the soil conservation function in a certain area and county based on the InVEST model.
Land use typeC valueP valuePaddy field0.060.06Dry land0.050.31Woodland0.030.99Bush0.030.99Other woodlands0.020.99High coverage grassland0.050.99Low coverage grassland0.180.99Canal0.150.01Reservoir pond0.210.01Beach0.020.06Urban land0.080.01Rural settlement0.070.01Other construction lands0.060.01The current research on theP value is mainly based on different land use types; due to the different actual conditions in the study area, the P value of the same land use type in different areas is different. When calculating the P factor, it is necessary to make extensive reference to related disciplines or similar research topics and then combine actual research to determine it. Due to its particularity, the P factor has a high degree of subjective flexibility when assigning values, so it is considered to be the most difficult to determine in the InVEST model. Area A is a mountainous area in southwest China, with a lot of deep and steep slopes, heavy rainfall, and excessive soil erosion. Soil protection measures such as afforestation, terrace construction, contour farming, and improvement of irrigation and drainage systems are adopted locally.


## 4.2.1. Rainfall ErosivityR Factor

The greater the precipitation erosion coefficient, the greater the intensity of soil erosion. The methods to obtain this coefficient are listed:(1)
The classic algorithm is as follows:(20)R=E×I30,whereR is the erosion activity of rain, E is the total kinetic energy of rain, and I30 is the rainfall intensity within 30 minutes.This model has extremely high requirements for data sources and must be based on a large amount of precipitation data. It has limitations in the complexity of obtaining kinetic energy and precipitation rate data, and its relatively narrow scope limits further applications.The modified formula for the calculatedR factor formula is as follows:(21)R=∑i=1121.735×101.5lgTi2/T−0.8188×17.02,whereT is the annual average rainfall (mm) and Ti is the monthly rainfall (mm).(2)
We established a power index structure daily rainfall erosivity model:(22)Rds=R∑i=1kTiλ.k represents the number of days, Ti represents the precipitation of the i-th day, Ti ≥ 12 mm is required; otherwise, the value is 0, Ty12 is the annual average rainfall with a daily rainfall ≥12 mm, and Td12 is the daily average rainfall with a daily rainfall ≥12 mm.(3)
We established the national daily replacement model (half-month rainfall erosivity model):(23)Mi=α∑j=1kDjβ.Here, Mi is the erosion activity value in thei-th half-month period (MJ·mm·hm−2·h−1), α and β are the model parameters, k represents the number of days in a half-month, and Dj represents the j-th day of the first half-month. The daily precipitation requires precipitation ≥12 mm.The numbersα and β represent model parameters reflecting the characteristics of precipitation in the area. According to the daily precipitation data, the values of α and β in the station are estimated according to(24)β=0.8363+18.144Pd12+24.455Py12,(25)∝=21.586β−7.1891.This method uses long-term continuous daily rainfall as the main unit of data. It is generally considered to be the most accurate and most representative method of the actual rainfall erosion rate, and long-term continuous data are required.According to the applicability of the model, combined with the existing meteorological and precipitation data, the final method of calculating theR factor is as follows:(26)R=∑i=11273.989×Pi2Pa0.7387.Here,R is the erosion activity value (MJ·mm·hm−2·h−1), Pi is the precipitation of the i-th month (mm), and Pa is the average annual precipitation (mm).The latitude and longitude of a certain area and its 6 surrounding counties and cities and theR value of precipitation erosion are shown in Table 1.Table 1
Information on latitude and longitude and rainfall erosivityR value of a certain area and its 6 surrounding counties and cities.
AreaLongitude (E)Dimensions (N)R factor valueArea A102.82435423.2255964834Area B102.38019623.3670384094Area C102.82344723.6313943944Area D103.23414722.7872528784Area E102.40330622.9955327806Area F103.15672823.3777924987This paper uses the monthly precipitation data of a certain region and 6 counties and cities over 35 years from 1986 to 2020 to calculate the annual value of precipitation erosivity and the value of the annual average rainfall erosivity factor.On this basis, the Kriging interpolation method was used on the GIS platform to generate anR layer based on the 6 counties from 1986 to 2020, and then, the mask was extracted to obtain the spatial distribution of the R factor of the A district and counties, as shown in Figure 2.Figure 2
Spatial distribution of theR factor of rainfall erosivity.Figure2 shows that the R value gradually decreases from south to north. There are high-value areas adjacent to the southwest and southeast of area A and high-precipitation areas D and E; a low value area appears in the dry hot area adjacent to the northwest of the valley.


## 4.2.2. Soil ErodibilityK Factor

The soil erodibilityK factor reflects the difficulty of separating and transporting soil with different particle sizes, and the difference in the K factor reflects the sensitivity of different types of soil to erosion. The K value can be obtained by querying data, actual measurement, and calculation. The most common method for querying data is the Vischmeier nomogram. This method requires more data on soil structure coefficients and permeability levels. At present, China’s soil data are mainly based on the results of the national soil census, which is far from the data requirements. At the same time, reclamation and plowing will change the nature of the soil, so it is impractical to directly use this method. The actual measurement includes the standard battery measurement method and physical and chemical properties measurement with the highest accuracy, but time-consumption, cumbersome procedures, equipment limitations, rainfall, and other unforeseen factors are drawbacks.The spatial distribution of the soil erosionK factor in a certain area is shown in Figure 3.Figure 3
Spatial distribution of the soil erodibilityK factor in a certain area.The soil erosion factor of Zone A ranges from 0.0375116 to 0.0410254, with an average of 0.0392685. From the macrodistribution of the soil erosionK value in China’s water erosion area, it can be seen that the soil erosion coefficient K in a certain area is 0.0484–0.0091, with an average value of 0.0292; compared with this value, the calculation result of the soil erosion rate coefficient K in circle A is slightly higher than the provincial average. The north and northeast are bordered by the Yuanjiang River, with large dry heat evaporation and little precipitation. The conditions of erosion (precipitation) are not perfect, resulting in small and uniform K.


## 4.2.3. P Factor of Soil and Water Conservation Measures

Common soil and water protection measures include reducing the slope, transforming the subsoil, and building ponds and dams. These measures mainly control soil erosion by affecting speed and flow. Among them, reducing the slope can effectively reduce water flow, and the construction of ponds and dams can adjust and reduce the flow. These measures are effective in reducing soil erosion and promoting soil protection.The calculation and verification of the soil conservation function of county A based on the InVEST model are shown in Table2.Table 2
Calculation and verification of the soil conservation function in a certain area and county based on the InVEST model.
Land use typeC valueP valuePaddy field0.060.06Dry land0.050.31Woodland0.030.99Bush0.030.99Other woodlands0.020.99High coverage grassland0.050.99Low coverage grassland0.180.99Canal0.150.01Reservoir pond0.210.01Beach0.020.06Urban land0.080.01Rural settlement0.070.01Other construction lands0.060.01The current research on theP value is mainly based on different land use types; due to the different actual conditions in the study area, the P value of the same land use type in different areas is different. When calculating the P factor, it is necessary to make extensive reference to related disciplines or similar research topics and then combine actual research to determine it. Due to its particularity, the P factor has a high degree of subjective flexibility when assigning values, so it is considered to be the most difficult to determine in the InVEST model. Area A is a mountainous area in southwest China, with a lot of deep and steep slopes, heavy rainfall, and excessive soil erosion. Soil protection measures such as afforestation, terrace construction, contour farming, and improvement of irrigation and drainage systems are adopted locally.


## 4.3. Evaluation and Characteristics of Soil Organic Matter

### 4.3.1. Descriptive Statistical Characteristics of the Spatial Variability of Soil Nutrients at Different Scales

The statistical characteristics of soil available nutrients at different sampling scales are shown in Table3.Table 3
Statistical characteristics of soil available nutrients at different sampling scales.
ScaleVariableMin (mg·kg−1)Max (mg·kg−1)Mean (mg·kg−1)SD (mg·kg−1)SkeKursigCoefficient of variation (%)Distribution typeCountyAN9.01169.0180.8321.330.440.830.0726.37NAP1.0193.0123.0814.211.382.530.0461.48LNAK24.01553.01177.3581.761.272.120.1246.11LNFieldAN16.83126.8856.1224.610.881.030.6643.85NAP19.58133.8655.4429.081 .050.370.0652.42NAK134.08373.17252.8570.59−0.13−1.280.3227.93NPlotAN15.28264.4788.1447.721.061.580.3754.12NAP15.33153.4463.3829.230.750.340.6346.12NAK170.12669.83308.8780.420.562.860.1726.04LNIt can be seen from Table3 that on the sampling scale, AP has the highest change intensity, followed by AK, and AN has the lowest change intensity; on the field scale, AP shows the largest change intensity, followed by AN, and AK shows the smallest change intensity; on the plot scale, AN has the largest change intensity, followed by AP, and AK has the smallest change intensity.


### 4.3.2. Spatial Autocorrelation Characteristics of the Spatial Variability of Soil Nutrients at Different Scales

The model parameters of the semivariance function soil nutrient index are shown in Table4.Table 4
Parameters of the semivariance function model of the soil nutrient index.
ScaleVariableTheoretical modelNuggetCoSillCo + CNugget/Sill (%)Range (m)Decisive factorR2Residual (RSS)CountyANExponential0.002350.0154915.13410.010.4299.73 × 10−6APExponential0.008910.0785111.33320.010.6115.68 × 10−5AKExponential0.005820.0324517.92390.010.6381.96 × 10−5FieldANGaussian0.000110.118210.09118.310.4246.16 × 10−4APExponential0.000110.040610.2655.410.9582.41 × 10−7AKGaussian0.000020.015730.07112.210.5587.57 × 10−6PlotANExponential0.002410.058614.1118.610.263.75 × 10−5APExponential0.003510.046317.5743.310.7311.58 × 10−5AKExponential0.001540.0110713.8427.610.3628.15 × 10−7At the county level, the AN, AP, and AK regions are the largest; at the field scale, the range is reduced by 118.31 m, 55.41 m, and 112.21 m, respectively; at the block scale, the range further drops to 18.61 m, 43.31 m, and 27.61 m, leading to drastic changes in small-scale soils AN, AP, and AK and significantly reducing their scope.


### 4.3.3. Scale Effect of Spatial Variability of Soil Nutrients

The fragmentation degree of the soil available nutrient map at different sampling scales is shown in Table5.Table 5
Fragmentation degree of soil available nutrient map at different sampling scales.
ScaleVariableNumber of plaques NP (pieces)Plaque density PD (pcs:hm−2)CountyAN750.16AP1160.22AK890.17FieldAN130.23AP180.36AK140.25PlotAN481.75AP331.18AK180.71The maximum effective phosphorus PD value is 1.18, and the distribution is relatively scattered. The main reason is that AP is more susceptible to random factors, which makes AP distributions disjoint, and has obvious local characteristics.The spatial distribution of available nutrients at different sampling scales is shown in Figure4.Figure 4
The spatial distribution of available nutrients at different sampling scales. (a) At the AN sampling scale of 0–180. (b) At the AP sampling scale of 0–120. (c) At the AK sampling scale of 0–600.It can be seen from the spatial distribution of nutrients that at the county level, except for a small part that is in a barren state, the alkali hydrolyzed nitrogen is continuously distributed in the soil, and most of the rest are at an average level.The corresponding curve diagram of the measured sample point of the soil organic matter content measured at the sampling point on November 2, 2020, is shown in Figure5.Figure 5
Fitting curve of soil organic matter content and measured sample point reflectivity on November 2, 2020.y = −0.0002x2 + 0.0019x + 0.2098 (fitness:0.835).It can be seen from the obtained data that this paper adopts the method of polynomial modeling, combined with comparative experiments for research, selects one of the sample points of polynomial fitting, and uses the sample point as the control point.The adjustment curve of soil organic matter content and reflectance at the image sampling point on November 2, 2020, is shown in Figure6.Figure 6
Fitting curve of soil organic matter content and image sample point reflectivity on November 2, 2020.y = 5E − 0.5x3 + 0.0017x2 − 0.0163x + 0.2202 (fitness:0.806).We select one of the sample points for polynomial fitting and check the sampling points, and the accuracy is similar, which proves that the model is very accurate and can be used to invert the soil organic matter in the entire area.The statistical comparison table of the percentage of organic matter in a certain area in the three periods is given in Table6.Table 6
Comparison table of the percentage of organic matter content in a certain area in three periods.
Organic matter content (%)/time<10[10–20)[20–30)[30–40]>40July 17, 201416.52332.59231.0878.95810.841November 2, 20193.4076.55414.05630.07245.912June 16, 20206.66613.30410.01140.26229.756Table6 shows the distribution of organic matter content in the test area during the three time periods. The results show that the results of remote sensing inversion of organic matter are consistent with those of the organic matter content measured by field sampling. After land consolidation, the organic matter content in the experimental area is mainly distributed in the plains and above.The statistical comparison table of the percentage of organic matter in a certain area in the three periods is given in Table7.Table 7
Comparison table of the percentage of organic matter content in a certain area in three periods.
Organic matter content (%)/time<10[10–20)[20–30)[30–40]>40July 2, 200376.52710.5926.824.9241.123November 27, 201937.40746.5528.9674.7152.356June 7, 202060.66617.33413.0115.9113.075Statistics for the distribution of organic matter over the three time periods in the study area show that the remote sensing inversion results of organic matter in the defined test area are consistent with the organic matter data obtained by field sampling. It can be seen from Table7 that after land development and consolidation in a certain experimental area, soil fertility has been greatly improved, soil quality has been significantly improved, and the effect of land development and consolidation has been significant.


### 4.3.4. BP Neural Network Inversion Model

The BP neural network is composed of input layer, hidden layer, and output layer.The cumulative credibility of the first six principal components is shown in Table8.Table 8
Cumulative credibility of the first six principal components.
Main ingredientCumulative reliability of the prediction set (%)Cumulative credibility of the validation set (%)P0199.42799.961P0299.57699.937P0399.42499.566P0499.82199.347P0599.96799.522P0699.97899.431The 26 samples in a certain experimental area are divided into a prediction set and a verification set. There are 15 sets of predictions and 9 sets of verifications. The spectral band of the sample is calculated using the full spectrum, which requires a large amount of calculation and has nothing to do with the composition of the sample. The principal component analysis method can fully reflect the information of the original multiwavelength variables and perform principal component analysis of the prediction sample and the verification set.The statistical comparison table of organic matter content in a certain area in two periods is shown in Table9.Table 9
Statistical comparison table of organic matter content in a certain area in two periods.
Organic matter content (%)/time<10[10–20)[20–30)[30–40]>40July 17, 201516.72432.49730.1779.24611.357November 2, 20203.3366.67613.34830.03746.602The inversion results in Table9 are approximately equal to the inversion results of the polynomial inversion model. The results showed that the content of soil organic matter in this area increased significantly after land consolidation, which significantly improved soil fertility and quality.


## 4.3.1. Descriptive Statistical Characteristics of the Spatial Variability of Soil Nutrients at Different Scales

The statistical characteristics of soil available nutrients at different sampling scales are shown in Table3.Table 3
Statistical characteristics of soil available nutrients at different sampling scales.
ScaleVariableMin (mg·kg−1)Max (mg·kg−1)Mean (mg·kg−1)SD (mg·kg−1)SkeKursigCoefficient of variation (%)Distribution typeCountyAN9.01169.0180.8321.330.440.830.0726.37NAP1.0193.0123.0814.211.382.530.0461.48LNAK24.01553.01177.3581.761.272.120.1246.11LNFieldAN16.83126.8856.1224.610.881.030.6643.85NAP19.58133.8655.4429.081 .050.370.0652.42NAK134.08373.17252.8570.59−0.13−1.280.3227.93NPlotAN15.28264.4788.1447.721.061.580.3754.12NAP15.33153.4463.3829.230.750.340.6346.12NAK170.12669.83308.8780.420.562.860.1726.04LNIt can be seen from Table3 that on the sampling scale, AP has the highest change intensity, followed by AK, and AN has the lowest change intensity; on the field scale, AP shows the largest change intensity, followed by AN, and AK shows the smallest change intensity; on the plot scale, AN has the largest change intensity, followed by AP, and AK has the smallest change intensity.


## 4.3.2. Spatial Autocorrelation Characteristics of the Spatial Variability of Soil Nutrients at Different Scales

The model parameters of the semivariance function soil nutrient index are shown in Table4.Table 4
Parameters of the semivariance function model of the soil nutrient index.
ScaleVariableTheoretical modelNuggetCoSillCo + CNugget/Sill (%)Range (m)Decisive factorR2Residual (RSS)CountyANExponential0.002350.0154915.13410.010.4299.73 × 10−6APExponential0.008910.0785111.33320.010.6115.68 × 10−5AKExponential0.005820.0324517.92390.010.6381.96 × 10−5FieldANGaussian0.000110.118210.09118.310.4246.16 × 10−4APExponential0.000110.040610.2655.410.9582.41 × 10−7AKGaussian0.000020.015730.07112.210.5587.57 × 10−6PlotANExponential0.002410.058614.1118.610.263.75 × 10−5APExponential0.003510.046317.5743.310.7311.58 × 10−5AKExponential0.001540.0110713.8427.610.3628.15 × 10−7At the county level, the AN, AP, and AK regions are the largest; at the field scale, the range is reduced by 118.31 m, 55.41 m, and 112.21 m, respectively; at the block scale, the range further drops to 18.61 m, 43.31 m, and 27.61 m, leading to drastic changes in small-scale soils AN, AP, and AK and significantly reducing their scope.


## 4.3.3. Scale Effect of Spatial Variability of Soil Nutrients

The fragmentation degree of the soil available nutrient map at different sampling scales is shown in Table5.Table 5
Fragmentation degree of soil available nutrient map at different sampling scales.
ScaleVariableNumber of plaques NP (pieces)Plaque density PD (pcs:hm−2)CountyAN750.16AP1160.22AK890.17FieldAN130.23AP180.36AK140.25PlotAN481.75AP331.18AK180.71The maximum effective phosphorus PD value is 1.18, and the distribution is relatively scattered. The main reason is that AP is more susceptible to random factors, which makes AP distributions disjoint, and has obvious local characteristics.The spatial distribution of available nutrients at different sampling scales is shown in Figure4.Figure 4
The spatial distribution of available nutrients at different sampling scales. (a) At the AN sampling scale of 0–180. (b) At the AP sampling scale of 0–120. (c) At the AK sampling scale of 0–600.It can be seen from the spatial distribution of nutrients that at the county level, except for a small part that is in a barren state, the alkali hydrolyzed nitrogen is continuously distributed in the soil, and most of the rest are at an average level.The corresponding curve diagram of the measured sample point of the soil organic matter content measured at the sampling point on November 2, 2020, is shown in Figure5.Figure 5
Fitting curve of soil organic matter content and measured sample point reflectivity on November 2, 2020.y = −0.0002x2 + 0.0019x + 0.2098 (fitness:0.835).It can be seen from the obtained data that this paper adopts the method of polynomial modeling, combined with comparative experiments for research, selects one of the sample points of polynomial fitting, and uses the sample point as the control point.The adjustment curve of soil organic matter content and reflectance at the image sampling point on November 2, 2020, is shown in Figure6.Figure 6
Fitting curve of soil organic matter content and image sample point reflectivity on November 2, 2020.y = 5E − 0.5x3 + 0.0017x2 − 0.0163x + 0.2202 (fitness:0.806).We select one of the sample points for polynomial fitting and check the sampling points, and the accuracy is similar, which proves that the model is very accurate and can be used to invert the soil organic matter in the entire area.The statistical comparison table of the percentage of organic matter in a certain area in the three periods is given in Table6.Table 6
Comparison table of the percentage of organic matter content in a certain area in three periods.
Organic matter content (%)/time<10[10–20)[20–30)[30–40]>40July 17, 201416.52332.59231.0878.95810.841November 2, 20193.4076.55414.05630.07245.912June 16, 20206.66613.30410.01140.26229.756Table6 shows the distribution of organic matter content in the test area during the three time periods. The results show that the results of remote sensing inversion of organic matter are consistent with those of the organic matter content measured by field sampling. After land consolidation, the organic matter content in the experimental area is mainly distributed in the plains and above.The statistical comparison table of the percentage of organic matter in a certain area in the three periods is given in Table7.Table 7
Comparison table of the percentage of organic matter content in a certain area in three periods.
Organic matter content (%)/time<10[10–20)[20–30)[30–40]>40July 2, 200376.52710.5926.824.9241.123November 27, 201937.40746.5528.9674.7152.356June 7, 202060.66617.33413.0115.9113.075Statistics for the distribution of organic matter over the three time periods in the study area show that the remote sensing inversion results of organic matter in the defined test area are consistent with the organic matter data obtained by field sampling. It can be seen from Table7 that after land development and consolidation in a certain experimental area, soil fertility has been greatly improved, soil quality has been significantly improved, and the effect of land development and consolidation has been significant.


## 4.3.4. BP Neural Network Inversion Model

The BP neural network is composed of input layer, hidden layer, and output layer.The cumulative credibility of the first six principal components is shown in Table8.Table 8
Cumulative credibility of the first six principal components.
Main ingredientCumulative reliability of the prediction set (%)Cumulative credibility of the validation set (%)P0199.42799.961P0299.57699.937P0399.42499.566P0499.82199.347P0599.96799.522P0699.97899.431The 26 samples in a certain experimental area are divided into a prediction set and a verification set. There are 15 sets of predictions and 9 sets of verifications. The spectral band of the sample is calculated using the full spectrum, which requires a large amount of calculation and has nothing to do with the composition of the sample. The principal component analysis method can fully reflect the information of the original multiwavelength variables and perform principal component analysis of the prediction sample and the verification set.The statistical comparison table of organic matter content in a certain area in two periods is shown in Table9.Table 9
Statistical comparison table of organic matter content in a certain area in two periods.
Organic matter content (%)/time<10[10–20)[20–30)[30–40]>40July 17, 201516.72432.49730.1779.24611.357November 2, 20203.3366.67613.34830.03746.602The inversion results in Table9 are approximately equal to the inversion results of the polynomial inversion model. The results showed that the content of soil organic matter in this area increased significantly after land consolidation, which significantly improved soil fertility and quality.


## 4.4. Research on the Analysis Method of Soil Nutrient Variability in Farmland

Research in recent years has shown that the method of combining multisource satellite images and multitemporal images with laboratory spectral analysis and ground-based in situ research is the development trend of soil organic matter measurement.Remote sensing is obviously the preferred method for estimating the surface temperature, because the main feature of remote sensing technology is that it can provide a wide range of data and images and use satellite data to calculate the surface temperature. Sensor technology is the theory and method for detecting satellite hot air duct data. At present, the remote sensing algorithms for surface temperature mainly include single-channel and multichannel satellite sensor infrared channel methods, infrared thermometer to measure surface temperature, and microwave remote sensing to monitor the surface temperature. At present, the use of infrared thermal data to monitor surface temperature is widely higher level.Soil surface evapotranspiration is an important part of both surface heat balance and ecosystem water balance. The water balance determines the quantity and spatial distribution of water resources, and the heat balance between water and soil is very large. It determines the weather and climate change, which in turn determines the soil quality and the formation and development of ecosystems. Remote sensing technology is currently used to monitor surface evapotranspiration. There are mainly single-layer models and double-layer models, especially the SEBAL model based on the principle of energy balance equation. Its outstanding advantage is that it has a strong physical foundation and is suitable for different climates. The vegetation index is a simple and effective indicator to characterize the vegetation coverage and plant growth status. In recent years, with the rapid development of remote sensing technology, the use of remote sensing technology to extract the vegetation index has been relatively expanded. In the field of ecology, the vegetation index examines ecosystems on a global scale, and the results of patch-level ecosystem research are extended to the global space.


## 5. Conclusion

A wireless sensor network consists of sensor nodes with radio functions and is a very promising solution in the era of the Internet of Things. Although remote sensing technology eliminates the drawbacks of using it, there are still energy and equipment problems. Therefore, it is necessary to find new ways to solve the problems of energy and remote sensing technology. Through the development of related algorithms, this paper mainly solves the problems of power consumption, interference, intercluster communication, and channel stability in wireless sensor networks. The soil conservation module calculates and analyzes the functional strength of soil protection in a certain area in 2020, obtains the spatial distribution of soil environmental resistance, and compares the obtained results with the coefficient of determination to test the accuracy of the research. In terms of quantitative statistics, this article uses a combination of classical statistics and geostatistics, in addition to a geostatistical analysis model of remote sensing technology to examine specific areas. Obviously, after land consolidation, the fertility of the soil in the rectified area has increased, the content of related organic matter has also increased significantly, and the fertility and quality of the soil have been improved.



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*Source: 3646264-2022-01-19.xml*