# Spatial Distribution and Temporal Trends in the Daily Precipitation Concentration across the Yarlung Tsangpo River Basin: Eastern Himalaya of China

Authors: Mengtao Zhu; Meng Li; Chunyu Liu; Yinfei Wang; Jiqiu Li; Yungang Li
Journal: Advances in Meteorology
 (2020)

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## Abstract

Understanding the temporal inequality in precipitation is of great importance for water resource management, environmental risk management, and ecological conservation. This study investigated the spatial patterns and trends of the daily precipitation concentration over the Yarlung Tsangpo River Basin using the concentration index (CI) and the Lorentz asymmetric coefficient (LAC). A Mann–Kendall test and Hurst’s rescaled range analysis were used to detect the change in CI trends. The CI ranged from 0.58 to 0.65, suggesting that a quarter of the rainiest days contributed approximately 69–78% of the total precipitation. The LAC analysis indicated that the nonuniform distribution of precipitation was mainly attributed to a large proportion of days with light rainfall. Compared with that of the central region, the daily precipitation in the western and eastern regions was more irregular. At a seasonal scale, the dry season had a less homogeneous spatial distribution of CI compared to that of the wet season. Most areas exhibited no significant trends in CI from 1970 to 2017. A quarter of the stations presented a significant downward trend in CI, which were primarily found in the central and northern regions. In addition, the future trends of CI in most areas mostly agree with those of the current state; however, the majority of stations exhibited an uneven precipitation distribution in the dry season.


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## Body

## 1. Introduction

Precipitation is a fundamental process of the water cycle [1, 2] and shows high temporal and spatial variability [3, 4]. As the climate changes, the most notable variation in precipitation events will likely be observed in their intensity, frequency, and duration [5]. Numerous studies have reported that precipitation extremes appear to intensify with global warming [6–9]. Precipitation extremes are directly responsible for floods, droughts, landslides, and soil erosion, which have notable impacts on both the environment and society [10, 11]. Therefore, the analysis of the temporal inequality in precipitation is a subject of great interest [12].The precipitation concentration refers to the temporal heterogeneity of precipitation, which is applicable in research of water-related environmental risks [13, 14]. For instance, high precipitation concentrations, meaning a small number of rainy days with a large amount of total precipitation, could trigger floods and droughts [15, 16]. Many indices were introduced to quantify the temporal precipitation concentration. To quantify precipitation heterogeneity on a monthly scale, Oliver [17] developed the precipitation concentration index (PCI) using the monthly precipitation data within a given year. Zhang and Qian [18] proposed the precipitation concentration degree (PCD) and precipitation concentration period (PCP) to represent the intra-annual distribution of total precipitation based on vector analysis. To evaluate daily precipitation irregularity in a given year, Martin Vide [19] proposed the concentration index (CI) to determine the percentage of precipitation contributed by the days falling in each rainfall class. The CI has been widely applied to study rainfall on both global [12] and regional scales in multiple places, such as Spain [19], Iran [20], Malaysia [21], Italy [22], Algeria [23], India [24], Chile [25], Russia [26], Bangladesh [13], and China [27, 28].The Yarlung Tsangpo River Basin (YTRB) is in the eastern Himalaya of China, which contains great environmental diversity (e.g., high mountains, glaciers, permafrost, and seasonally frozen soil) and is sensitive to climate change as indicated by the observed retreat of glaciers, permafrost degradation, desertification, and land-use changes [29–31]. In the last three decades, natural disasters related to precipitation extremes, such as floods, droughts, glacier debris flows, and landslides, have become more severe and frequent [32]. Thus, it is crucial to understand the distribution and patterns of precipitation concentration because of the potential consequences of precipitation extremes and natural disasters in the YTRB.Climate change has been investigated in the YTRB with regard to diverse aspects. A remarkable warming trend was observed from 1970 to 2017 [33]. The warming trend was found to be up to 0.32°C/decade, while annual precipitation was found to increase by 6.32 mm/decade from 1961 to 2014 [34]. Fan et al. [35] found that annual rainfall amounts and the number of rainy days significantly increased from 1958 to 2010, indicating that the increasing number of rain days is one possible cause of the increases in annual rainfall amounts. Sang et al. [36] reported that the number of precipitation extremes and the amount of rainfall (25–50 mm/d) decreased from 1973 to 2011.Although previous studies have investigated the changes in mean precipitation and precipitation extremes, few studies have focused on temporal inequalities in precipitation, particularly with regard to the spatial patterns and trends of the daily precipitation concentration. The CI based on the Lorenz curve has been widely used in the studies on daily precipitation concentration in many regions around the world, which has also been applied to compare the precipitation concentration among different regions. In addition, the Lorenz asymmetry coefficient (LAC) is a supplementary indicator of the CI. It measures the contribution of different precipitation classes to the precipitation heterogeneity. Thus, the objectives of this study were to (1) analyze the spatial distribution of the daily precipitation concentration using the CI and the LAC, (2) detect trends in the CI using the Mann–Kendall trend test, and (3) predict the possible CI trend based on the Hurst’s rescaled range analysis.


## 2. Data and Methods

### 2.1. Study Area

The YTRB is in the Qinghai–Tibet Plateau and is one of the highest major river basins in the world, with a mean elevation of over 4000 m. The YTRB is roughly 2229 km long and covers an area of 2.4 × 105 km2 [37] (Figure 1). The geographical location and topographic characteristics of the YTRB play a major role in the climate diversity of the upper, middle, and lower reaches of the basin. The surrounding vegetation in the basin changes from alpine meadow in the upstream region to alpine grassland in the midstream region to alpine forest in the downstream region [30]. Annual precipitation in the downstream region is more than 2000 mm and decreases to less than 300 mm in the upper stream region. The moisture from Bengal Bay is transported by Indian monsoons and is the primary source of precipitation in the region [38]. The climate is characterized by a distinct rainy season (June to September) in which approximately 60–80% of the annual precipitation occurs [37]. The Yarlung Tsangpo River has numerous tributaries and is an abundant freshwater resource that is important for Tibet and other downstream countries [39, 40].Figure 1
The location and distribution of meteorological stations in the YTRB.


### 2.2. Precipitation Data

Daily precipitation data at 16 meteorological stations across the YTRB were provided by the National Meteorological Information Center (NMIC;http://data.cma.cn). The quality of the dataset was verified by the NMIC when it was released, and quality control and homogeneity assessments were subsequently performed [33]. To make the best use of available data and obtain the best spatial coverage, 14 stations within the YTRB and 2 stations outside the basin were selected for subsequent analysis. The locations of the 16 meteorological stations are shown in Figure 1. The recording periods of the stations varied in duration; however, most stations had data available from 1970 to 2017. The specific information of the 16 stations is shown in Table 1.Table 1
Geographical coordinates, annual mean precipitation (P), coefficient of variation (VC), and mean number of rainy days (N) for the 16 stations considered in this study.
IDStationLat (°N)Long (°E)Elevation (m)Study periodP (mm)VC (%)N (day)55437Pulan30.2881.2549001973–2017156.0133.685255493Dangxiong30.4891.142001970–2017468.2720.2212155569Lazi29.0887.640001977–2017331.9428.477355578Rikeze29.2588.8838361970–2017428.6225.198055585Nimu29.4390.1638091973–2017343.1023.088255591Lasa29.6691.1336491970–2017445.3121.639355598Zedang29.2591.7635521970–2017387.8324.789255664Dingri28.6387.0843001970–2017291.8627.646055680Jiangzi28.9189.640401970–2017285.4322.757655690Cuona27.9891.9542801970–2017414.4615.7119455696Longzi28.4192.4638601970–2017284.7420.479255773Pali27.7389.0843001970–2017439.0817.3615956202Jiali30.6693.2844891970–2017729.4012.6717856227Bomi29.8695.7627361970–2017889.6115.6918956312Linzhi29.6694.3329921970–2017689.9417.1716856434Chayu28.6597.4623281970–2017796.9520.80173


### 2.3. Precipitation CI

The daily precipitation CI was computed using the approach proposed by [19], based on the Lorenz diagrams and the Gini index. The cumulative percentage of rainy days (X) was plotted against the associated cumulative percentage of rainfall (Y). The Lorenz curve was used to match the empirical pairs of values (X, Y) and had an exponential shape:(1)Y=a⋅X⋅expb⋅X,where a and b are constants that can be determined by using the least-squares method.(2)lna=∑xi2∑lnyi+∑xi∑xilnxi−∑xi2∑lnxi−∑xi∑xilnyiN∑xi2−∑xi2,b=N∑xilnyi+∑xi∑lnxi−N∑xilnxi−∑xi∑lnyiN∑xi2−∑xi2.Once the constants are obtained, the area under the Lorenz curve can be calculated as follows:(3)A=abebxx−1b0100.Finally, the CI is defined as follows:(4)CI=5000−A5000.The greater the CI value, the lower the uniformity, i.e., the more uneven the precipitation (mainly concentrated in a few rainy days).


### 2.4. Lorenz Asymmetric Coefficient

The CI cannot fully represent the Lorenz Curve as different Lorenz Curves may have the same CI [41, 42]. Therefore, the LAC was introduced to quantitatively define the contribution of different groups to the total heterogeneity [43]. For the ordered sequence, x1≤x2≤…xm≤…≤xn the LAC can be calculated according to the following equations:(5)LAC=Fμ+Lμ,δ=μ−xmxm+1−xm,Fμ=m+δn,Lμ=x1+x2+⋯+xm+δxm+1x1+x2+⋯+xn,where μ is the mean daily precipitation over all rainy days, n is the total number of rainy days, and m is the number of daily precipitation less than μ [42]. If LAC <1, the inequality is attributed to a large number of light rainfall events. Correspondingly, if LAC > 1, the inequality is attributed to a small number of very large rainfall events.


### 2.5. Trend Analysis

The nonparametric Mann–Kendall test has been widely applied to identify trends in hydrometeorological time series [44]. A positive value of the statistical eigenvalue, Z, will represent an upward trend, while a negative value will represent a downward trend. The null hypothesis of no trend should be rejected if |Z| > Z1–α/2, where α is the significance level. Significance levels of 0.1, 0.05, and 0.01 were considered in this study. In addition, the Hurst exponent (H) is used as part of a classical test to detect long memory in time series [45]. A well-known method to estimate H is a rescaled range (R/S) analysis [46]. Hurst’s rescaled range (R/S) analysis has been widely used in the study of climate change [47–49]. The value of H ranges from 0 to 1. When H = 0.5, the time series is considered to be random. When 0.5 < H < 1, a dynamic persistence or trend enhancement series is present. When 0 < H < 0.5, resistance to persistence or average recovery is present [50].


## 2.1. Study Area

The YTRB is in the Qinghai–Tibet Plateau and is one of the highest major river basins in the world, with a mean elevation of over 4000 m. The YTRB is roughly 2229 km long and covers an area of 2.4 × 105 km2 [37] (Figure 1). The geographical location and topographic characteristics of the YTRB play a major role in the climate diversity of the upper, middle, and lower reaches of the basin. The surrounding vegetation in the basin changes from alpine meadow in the upstream region to alpine grassland in the midstream region to alpine forest in the downstream region [30]. Annual precipitation in the downstream region is more than 2000 mm and decreases to less than 300 mm in the upper stream region. The moisture from Bengal Bay is transported by Indian monsoons and is the primary source of precipitation in the region [38]. The climate is characterized by a distinct rainy season (June to September) in which approximately 60–80% of the annual precipitation occurs [37]. The Yarlung Tsangpo River has numerous tributaries and is an abundant freshwater resource that is important for Tibet and other downstream countries [39, 40].Figure 1
The location and distribution of meteorological stations in the YTRB.


## 2.2. Precipitation Data

Daily precipitation data at 16 meteorological stations across the YTRB were provided by the National Meteorological Information Center (NMIC;http://data.cma.cn). The quality of the dataset was verified by the NMIC when it was released, and quality control and homogeneity assessments were subsequently performed [33]. To make the best use of available data and obtain the best spatial coverage, 14 stations within the YTRB and 2 stations outside the basin were selected for subsequent analysis. The locations of the 16 meteorological stations are shown in Figure 1. The recording periods of the stations varied in duration; however, most stations had data available from 1970 to 2017. The specific information of the 16 stations is shown in Table 1.Table 1
Geographical coordinates, annual mean precipitation (P), coefficient of variation (VC), and mean number of rainy days (N) for the 16 stations considered in this study.
IDStationLat (°N)Long (°E)Elevation (m)Study periodP (mm)VC (%)N (day)55437Pulan30.2881.2549001973–2017156.0133.685255493Dangxiong30.4891.142001970–2017468.2720.2212155569Lazi29.0887.640001977–2017331.9428.477355578Rikeze29.2588.8838361970–2017428.6225.198055585Nimu29.4390.1638091973–2017343.1023.088255591Lasa29.6691.1336491970–2017445.3121.639355598Zedang29.2591.7635521970–2017387.8324.789255664Dingri28.6387.0843001970–2017291.8627.646055680Jiangzi28.9189.640401970–2017285.4322.757655690Cuona27.9891.9542801970–2017414.4615.7119455696Longzi28.4192.4638601970–2017284.7420.479255773Pali27.7389.0843001970–2017439.0817.3615956202Jiali30.6693.2844891970–2017729.4012.6717856227Bomi29.8695.7627361970–2017889.6115.6918956312Linzhi29.6694.3329921970–2017689.9417.1716856434Chayu28.6597.4623281970–2017796.9520.80173


## 2.3. Precipitation CI

The daily precipitation CI was computed using the approach proposed by [19], based on the Lorenz diagrams and the Gini index. The cumulative percentage of rainy days (X) was plotted against the associated cumulative percentage of rainfall (Y). The Lorenz curve was used to match the empirical pairs of values (X, Y) and had an exponential shape:(1)Y=a⋅X⋅expb⋅X,where a and b are constants that can be determined by using the least-squares method.(2)lna=∑xi2∑lnyi+∑xi∑xilnxi−∑xi2∑lnxi−∑xi∑xilnyiN∑xi2−∑xi2,b=N∑xilnyi+∑xi∑lnxi−N∑xilnxi−∑xi∑lnyiN∑xi2−∑xi2.Once the constants are obtained, the area under the Lorenz curve can be calculated as follows:(3)A=abebxx−1b0100.Finally, the CI is defined as follows:(4)CI=5000−A5000.The greater the CI value, the lower the uniformity, i.e., the more uneven the precipitation (mainly concentrated in a few rainy days).


## 2.4. Lorenz Asymmetric Coefficient

The CI cannot fully represent the Lorenz Curve as different Lorenz Curves may have the same CI [41, 42]. Therefore, the LAC was introduced to quantitatively define the contribution of different groups to the total heterogeneity [43]. For the ordered sequence, x1≤x2≤…xm≤…≤xn the LAC can be calculated according to the following equations:(5)LAC=Fμ+Lμ,δ=μ−xmxm+1−xm,Fμ=m+δn,Lμ=x1+x2+⋯+xm+δxm+1x1+x2+⋯+xn,where μ is the mean daily precipitation over all rainy days, n is the total number of rainy days, and m is the number of daily precipitation less than μ [42]. If LAC <1, the inequality is attributed to a large number of light rainfall events. Correspondingly, if LAC > 1, the inequality is attributed to a small number of very large rainfall events.


## 2.5. Trend Analysis

The nonparametric Mann–Kendall test has been widely applied to identify trends in hydrometeorological time series [44]. A positive value of the statistical eigenvalue, Z, will represent an upward trend, while a negative value will represent a downward trend. The null hypothesis of no trend should be rejected if |Z| > Z1–α/2, where α is the significance level. Significance levels of 0.1, 0.05, and 0.01 were considered in this study. In addition, the Hurst exponent (H) is used as part of a classical test to detect long memory in time series [45]. A well-known method to estimate H is a rescaled range (R/S) analysis [46]. Hurst’s rescaled range (R/S) analysis has been widely used in the study of climate change [47–49]. The value of H ranges from 0 to 1. When H = 0.5, the time series is considered to be random. When 0.5 < H < 1, a dynamic persistence or trend enhancement series is present. When 0 < H < 0.5, resistance to persistence or average recovery is present [50].


## 3. Results

### 3.1. Spatial Pattern of the Daily Precipitation Concentration

The annual CI and LAC were calculated for 16 meteorological stations in the YTRB for the period 1970–2017. The values of the regression coefficients (a and b) and the CI and LAC are presented in Table 2. The annual CI value ranged between 0.58 and 0.65, suggesting that the lowest values observed are related to regions where 25% of the rainiest days accounted for 69% of the total precipitation, while the highest values are associated with places where 25% of the rainiest days contribute to 78% of the total precipitation (Table 2). According to the proposed classifications for the CI [11], the averaged value of the CI (0.60) over the YTRB is within high concentration categories, which implied that 25% of the rainiest days could concentrate more than 70% of the total precipitation. The annual LAC value ranged between 0.86 and 0.95, with a median value of 0.89, which illustrates a high precipitation concentration attributed to a large number of light rainfall events. Figure 2 shows an example of the concentration curves for three stations: Pulan station in the western region (CI: 0.65, LAC: 0.95), Lasa station in the central region (CI: 0.59, LAC: 0.86), and Chayu station in the eastern region (CI: 0.62, LAC: 0.92). Pulan station is located in a frigid zone with an annual rainfall of less than 300 mm. The intra-annual distribution of precipitation is characterized by a few rainy days in the winter season. The Lasa station is located in the valley of a tributary and is found in a semiarid plateau climate with a small amount of annual precipitation (300–600 mm). Chayu station is located in a subtropical humid zone and has relatively abundant precipitation. The spatial difference in CI indicated that the inequality in precipitation is closely associated with the frequency and intensity of rainfall and not with the amount of precipitation.Table 2
Values for the constants,a and b, of the exponential curves, coefficients of determination (R2), CI, LAC, and percentage of precipitation contributed by 25% of the rainiest days (P 25%).
StationabR2CILACP 25%Pulan0.0230.0360.960.6460.94678Dangxiong0.0430.0310.990.5810.89369Lazi0.0370.0330.990.5940.89471Rikeze0.0360.0331.000.5900.86169Nimu0.0400.0320.990.5860.88470Lasa0.0390.0321.000.5860.86469Zedang0.0340.0340.990.5990.87672Dingri0.0300.0350.990.6080.88072Jiangzi0.0330.0340.990.6020.89172Cuona0.0460.0300.960.5840.94672Longzi0.0460.0300.990.5820.91371Pali0.0460.0300.980.5850.92571Jiali0.0400.0320.990.5860.88470Bomi0.0290.0350.990.6120.90773Linzhi0.0290.0350.990.6110.90073Chayu0.0270.0350.980.6200.92174Figure 2
Concentration curve for the Pulan (a), Lasa (b), and Chayu stations (c) from 1970 to 2017.
(a)(b)(c)The CI and LAC values from 1970 to 2017 of the individual stations were spatially interpolated throughout the YTRB based on the Inverse Distance Weighted technique. The high CI values (0.60–0.64) were primarily found in the eastern and western regions, while in the central region, the majority of values fell within 0.58–0.60 (Figure3(a)). In the eastern region, the high rainfall intensity observed agreed with the high precipitation concentrations recorded in the area. However, in the western region, high precipitation concentrations were not attributed to remarkably high precipitation but rather to a few rainy days. In the central region, less precipitation and a few days of precipitation contributed to low precipitation concentrations. The values of LAC were less than 1 across the basin, which indicated the nonuniform distribution of precipitation, which was mainly attributed to a large proportion of days with light rainfall (Figure 3(b)).Figure 3
Spatial distribution of annual CI (a) and LAC (b) values.
(a)(b)


### 3.2. Seasonal Distribution of the Daily Precipitation Concentration

Affected by the warm and humid Indian Summer monsoon, the rainy season usually begins in May or June and ends at the end of September or October [51]. Therefore, we divided May to September as the wet season and October to April as the dry season [52]. Figure 4 demonstrates the spatial pattern of the CI and LAC during the wet season (May to September) and dry season (October to April), respectively. The CI values of the wet season ranged from 0.55 (Pali and Jiali stations) to 0.65 (Pulan station), while it varied between 0.57 (Dangxiong station) and 0.65 (Pulan, Pali, and Chayu stations) during the dry season (Figures 4(a) and 4(b)). The spatial pattern of CI in the wet and dry seasons was very similar to that of the annual pattern. However, the median CI value in the dry season (0.61) was larger than that of the wet season (0.58), which indicated that the heterogeneity of the precipitation distribution was more pronounced in the dry season. The LAC values of the wet season ranged from 0.85 (Rikeze and Zedang station) to 0.94 (Cuona station), while these varied between 0.89 (Rikeze and Bomi stations) and 0.97 (Pali and Lasa stations) in the dry season (Figures 4(c) and 4(d)). Higher LAC values in the dry season were observed when compared with those of the wet season, and the median values in the dry season and wet seasons were 0.94 and 0.89, respectively.Figure 4
The spatial distribution of the CI and LAC in the wet season and dry season. (a) CI in the wet season; (b) CI in the dry season; (c) LAC in the wet season; (d) LAC in the dry season.
(a)(b)(c)(d)


### 3.3. Observed Trends of the Daily Precipitation Concentration

Figure5 shows the variation in annual CI, rainy days, and precipitation at the Pulan, Lasa, and Chayu stations, which represent the upper, middle, and lower YTRB, respectively. At Pulan station in the upper region (Figure 5(a)), the CI presented a positive trend; however, the number of rainy days and precipitation showed negative trends, implying that more precipitation fell over a few rainy days. At Lasa station, both the CI and the number of rainy days decreased while precipitation increased, which was attributed to the increases in the precipitation intensity (Figure 5(b)). At Chayu station, the CI, the number of rainy days, and precipitation decreased, suggesting that the decrease in heavy rainfall events was greater than that of the light rainfall events (Figure 5(c)).Figure 5
Time series of annual CI, rainy days, and total precipitation amount at the Pulan (a), Lasa (b), and Chayu stations (c). The solid red lines are the corresponding linear trend and the solid green line is 9-year smooth line.
(a)(b)(c)Figure6 shows the number of meteorological stations that presented trends (positive and negative) at different significant levels. On an annual scale and during the wet season, three-quarters of the stations showed no significant trends during the study period. Four stations showed a significant negative trend with confidence levels greater than 90%, which indicated that the intra-annual distribution of precipitation presented a more uniform pattern. These stations are mainly found in the central and northern regions of the basin. However, in the dry season, the number of stations with positive CI trends was greater than that of stations with negative CI trends, although only one station had a significantly positive trend at the 95% confidence level.Figure 6
Observed CI trends for different ranges of the significance level.


### 3.4. Future Trends of the Daily Precipitation Concentration

Hurst’s rescaled range analysis was used to explore the future trends of CI. On an annual scale, the future CI trend was opposite (0 <H < 0.5) and consistent (0.5 < H < 1) to the current state accounting for 12.50% and 81.25% of all stations, respectively (Figure 7(a)). More concretely, upward trends of the CI continued at 4 stations, while downward trends continued at 9 stations. In addition, 2 other stations showed antipersistent trends, and one station presented an uncertain trend. The future trend of the wet season CI is similar to that of the annual CI (Figure 7(b)). Moreover, the future trend of the dry season CI, which was opposite and consistent to the current state, accounted for 43.75% and 56.25% of all stations, respectively (Figure 7(c)). Specifically, the upward CI trend was enhanced at 5 stations, while downward trends continued at 3 stations. The other 7 stations presented antipersistent trends. Figure 7 shows the spatial distribution of the future CI trend. The precipitation concentration in the western and southern regions of the basin will exhibit an increasing trend, while the precipitation concentration in the eastern and northern regions will decrease in the future (Figures 7(a) and 7(b)). It is worth noting that the majority of stations in the YTRB will exhibit irregular and nonuniform distribution in the dry season in the future (Figure 7(c)).Figure 7
Spatial distribution of future CI. (a) Year. (b) Wet season. (c) Dry season.
(a)(b)(c)


## 3.1. Spatial Pattern of the Daily Precipitation Concentration

The annual CI and LAC were calculated for 16 meteorological stations in the YTRB for the period 1970–2017. The values of the regression coefficients (a and b) and the CI and LAC are presented in Table 2. The annual CI value ranged between 0.58 and 0.65, suggesting that the lowest values observed are related to regions where 25% of the rainiest days accounted for 69% of the total precipitation, while the highest values are associated with places where 25% of the rainiest days contribute to 78% of the total precipitation (Table 2). According to the proposed classifications for the CI [11], the averaged value of the CI (0.60) over the YTRB is within high concentration categories, which implied that 25% of the rainiest days could concentrate more than 70% of the total precipitation. The annual LAC value ranged between 0.86 and 0.95, with a median value of 0.89, which illustrates a high precipitation concentration attributed to a large number of light rainfall events. Figure 2 shows an example of the concentration curves for three stations: Pulan station in the western region (CI: 0.65, LAC: 0.95), Lasa station in the central region (CI: 0.59, LAC: 0.86), and Chayu station in the eastern region (CI: 0.62, LAC: 0.92). Pulan station is located in a frigid zone with an annual rainfall of less than 300 mm. The intra-annual distribution of precipitation is characterized by a few rainy days in the winter season. The Lasa station is located in the valley of a tributary and is found in a semiarid plateau climate with a small amount of annual precipitation (300–600 mm). Chayu station is located in a subtropical humid zone and has relatively abundant precipitation. The spatial difference in CI indicated that the inequality in precipitation is closely associated with the frequency and intensity of rainfall and not with the amount of precipitation.Table 2
Values for the constants,a and b, of the exponential curves, coefficients of determination (R2), CI, LAC, and percentage of precipitation contributed by 25% of the rainiest days (P 25%).
StationabR2CILACP 25%Pulan0.0230.0360.960.6460.94678Dangxiong0.0430.0310.990.5810.89369Lazi0.0370.0330.990.5940.89471Rikeze0.0360.0331.000.5900.86169Nimu0.0400.0320.990.5860.88470Lasa0.0390.0321.000.5860.86469Zedang0.0340.0340.990.5990.87672Dingri0.0300.0350.990.6080.88072Jiangzi0.0330.0340.990.6020.89172Cuona0.0460.0300.960.5840.94672Longzi0.0460.0300.990.5820.91371Pali0.0460.0300.980.5850.92571Jiali0.0400.0320.990.5860.88470Bomi0.0290.0350.990.6120.90773Linzhi0.0290.0350.990.6110.90073Chayu0.0270.0350.980.6200.92174Figure 2
Concentration curve for the Pulan (a), Lasa (b), and Chayu stations (c) from 1970 to 2017.
(a)(b)(c)The CI and LAC values from 1970 to 2017 of the individual stations were spatially interpolated throughout the YTRB based on the Inverse Distance Weighted technique. The high CI values (0.60–0.64) were primarily found in the eastern and western regions, while in the central region, the majority of values fell within 0.58–0.60 (Figure3(a)). In the eastern region, the high rainfall intensity observed agreed with the high precipitation concentrations recorded in the area. However, in the western region, high precipitation concentrations were not attributed to remarkably high precipitation but rather to a few rainy days. In the central region, less precipitation and a few days of precipitation contributed to low precipitation concentrations. The values of LAC were less than 1 across the basin, which indicated the nonuniform distribution of precipitation, which was mainly attributed to a large proportion of days with light rainfall (Figure 3(b)).Figure 3
Spatial distribution of annual CI (a) and LAC (b) values.
(a)(b)


## 3.2. Seasonal Distribution of the Daily Precipitation Concentration

Affected by the warm and humid Indian Summer monsoon, the rainy season usually begins in May or June and ends at the end of September or October [51]. Therefore, we divided May to September as the wet season and October to April as the dry season [52]. Figure 4 demonstrates the spatial pattern of the CI and LAC during the wet season (May to September) and dry season (October to April), respectively. The CI values of the wet season ranged from 0.55 (Pali and Jiali stations) to 0.65 (Pulan station), while it varied between 0.57 (Dangxiong station) and 0.65 (Pulan, Pali, and Chayu stations) during the dry season (Figures 4(a) and 4(b)). The spatial pattern of CI in the wet and dry seasons was very similar to that of the annual pattern. However, the median CI value in the dry season (0.61) was larger than that of the wet season (0.58), which indicated that the heterogeneity of the precipitation distribution was more pronounced in the dry season. The LAC values of the wet season ranged from 0.85 (Rikeze and Zedang station) to 0.94 (Cuona station), while these varied between 0.89 (Rikeze and Bomi stations) and 0.97 (Pali and Lasa stations) in the dry season (Figures 4(c) and 4(d)). Higher LAC values in the dry season were observed when compared with those of the wet season, and the median values in the dry season and wet seasons were 0.94 and 0.89, respectively.Figure 4
The spatial distribution of the CI and LAC in the wet season and dry season. (a) CI in the wet season; (b) CI in the dry season; (c) LAC in the wet season; (d) LAC in the dry season.
(a)(b)(c)(d)


## 3.3. Observed Trends of the Daily Precipitation Concentration

Figure5 shows the variation in annual CI, rainy days, and precipitation at the Pulan, Lasa, and Chayu stations, which represent the upper, middle, and lower YTRB, respectively. At Pulan station in the upper region (Figure 5(a)), the CI presented a positive trend; however, the number of rainy days and precipitation showed negative trends, implying that more precipitation fell over a few rainy days. At Lasa station, both the CI and the number of rainy days decreased while precipitation increased, which was attributed to the increases in the precipitation intensity (Figure 5(b)). At Chayu station, the CI, the number of rainy days, and precipitation decreased, suggesting that the decrease in heavy rainfall events was greater than that of the light rainfall events (Figure 5(c)).Figure 5
Time series of annual CI, rainy days, and total precipitation amount at the Pulan (a), Lasa (b), and Chayu stations (c). The solid red lines are the corresponding linear trend and the solid green line is 9-year smooth line.
(a)(b)(c)Figure6 shows the number of meteorological stations that presented trends (positive and negative) at different significant levels. On an annual scale and during the wet season, three-quarters of the stations showed no significant trends during the study period. Four stations showed a significant negative trend with confidence levels greater than 90%, which indicated that the intra-annual distribution of precipitation presented a more uniform pattern. These stations are mainly found in the central and northern regions of the basin. However, in the dry season, the number of stations with positive CI trends was greater than that of stations with negative CI trends, although only one station had a significantly positive trend at the 95% confidence level.Figure 6
Observed CI trends for different ranges of the significance level.


## 3.4. Future Trends of the Daily Precipitation Concentration

Hurst’s rescaled range analysis was used to explore the future trends of CI. On an annual scale, the future CI trend was opposite (0 <H < 0.5) and consistent (0.5 < H < 1) to the current state accounting for 12.50% and 81.25% of all stations, respectively (Figure 7(a)). More concretely, upward trends of the CI continued at 4 stations, while downward trends continued at 9 stations. In addition, 2 other stations showed antipersistent trends, and one station presented an uncertain trend. The future trend of the wet season CI is similar to that of the annual CI (Figure 7(b)). Moreover, the future trend of the dry season CI, which was opposite and consistent to the current state, accounted for 43.75% and 56.25% of all stations, respectively (Figure 7(c)). Specifically, the upward CI trend was enhanced at 5 stations, while downward trends continued at 3 stations. The other 7 stations presented antipersistent trends. Figure 7 shows the spatial distribution of the future CI trend. The precipitation concentration in the western and southern regions of the basin will exhibit an increasing trend, while the precipitation concentration in the eastern and northern regions will decrease in the future (Figures 7(a) and 7(b)). It is worth noting that the majority of stations in the YTRB will exhibit irregular and nonuniform distribution in the dry season in the future (Figure 7(c)).Figure 7
Spatial distribution of future CI. (a) Year. (b) Wet season. (c) Dry season.
(a)(b)(c)


## 4. Discussion

The precipitation concentrations of the YTRB ranged between 0.58 and 0.65, indicating that a quarter of the rainiest days accounted for approximately 69–78% of the total precipitation. Compared to those reported for different parts of China [16, 28, 42, 48, 53] and other regions in the world [14, 21, 23, 25, 54–57], the amount of annual rainfall could not accurately reveal the time compression of precipitation, given that similar annual rainfall patterns could present varying daily distributions [26, 58].The spatial pattern of the CI across the YTRB was impacted by water vapor transport, topography, and climate zone. Precipitation is mainly controlled by the South Asian Monsoon (SAM), which weakens from east to west along the Himalayas [59]. Therefore, the intensity, duration, and amount of monsoon rainfall vary from east to west [60]. In addition, the distribution of precipitation in the YTRB is largely influenced by topography [61]. The Himalaya acts as a barrier to the SAM, which brings abundant precipitation that concentrates windward and causes a distinct dry-belt in the leeward side [62]. Therefore, the low CI values were found in the central region that receives less rainfall. Moreover, high CI values were found in the southeast region, which was mainly due to the influence of the topography on local atmospheric circulation. Water vapor is transported along the river canyon from south to north, resulting in relatively abundant precipitation in the southeastern region. In addition, solid precipitation is an important component of the precipitation over the western area at high altitude [59]. The high precipitation concentration was mainly attributed to a few rainy days with large precipitation in the cold season.The CI of most areas over the YTRB showed no significant trend during the study period, which agrees with the results of previous studies that were carried out in the adjacent regions. For example, most of the area of Xinjiang showed no significant trends in CI from 1961 to 2008 [15]. The decreasing trends in the CI of the Yangtze River Basin were not significant in most parts from 1960 to 2008 [63]. Overall, daily precipitation was generally more homogeneous in western China from 1961 to 2017 [28]. In the future, it is worth noting that the majority of stations in the YTRB will exhibit irregular and nonuniform distribution in precipitation during the dry season, which implies that the risk of environmental problems, such as flooding, soil erosion, and landslides, is likely to increase.Some limitations and uncertainties inevitably exist due to the meteorological data and methods used in this study. The CI analysis using 16 stations in the basin was not fully representative of the spatial distribution of precipitation in the region. Precipitation data with a high spatiotemporal resolution is the basis for analyzing extreme climate events [57]. For instance, satellite-based precipitation is an alternative source of precipitation data [64]. Therefore, gridded precipitation data derived from merging gauge, satellite, and reanalysis data should be considered to promote thorough precipitation concentration research in the YTRB. In addition, the Hurst exponent was used to predict future trends of the CI. However, this method failed to predict how long the anticipated CI trend will continue. Given this, a climate model is a feasible and effective tool to study future precipitation concentration. Multimodel ensemble prediction may improve our understanding of future changes in precipitation extremes [9].


## 5. Conclusions

This study investigated the spatial distribution and changing trends of the daily precipitation concentration over the YTRB from 1970 to 2017. The CI values ranged from 0.58 to 0.65, suggesting that a quarter of the rainiest days contributed approximately 69–78% of the total precipitation. Higher CI values were found in the western and eastern regions, while lower CI values were observed in the central region. The nonuniform distribution of rainfall was attributed to a large proportion of days with light rainfall. At a seasonal scale, the dry season was found to have a less homogeneous spatial distribution of CI. Most areas exhibited no significant trends in CI from 1970 to 2017. A quarter of the stations presented a significant downward trend of the CI, which were primarily found in the central and northern regions. The Hurst index analysis demonstrated that the precipitation concentration in the eastern and northern regions would decrease in the future, while the precipitation concentration in the southern and western regions will increase. The majority of stations in the YTRB exhibited an uneven precipitation distribution in the dry season, which implied that the risks of environmental problems, such as flooding, soil erosion, and landslides, are likely to increase. These results could provide useful information for water resource management, environmental risk management, and ecological conservation.



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*Source: 8813394-2020-12-15.xml*