# Robust Response of Streamflow Drought to Different Timescales of Meteorological Drought in Xiangjiang River Basin of China

Authors: Lin Zhao; Jianjun Wu; Jian Fang
Journal: Advances in Meteorology
 (2016)

---

## Abstract

Meteorological drought can evolve into all aspects of hydrologic system such as soil layer, groundwater, and river discharge, leading to agricultural drought, groundwater drought, and streamflow drought, respectively. How does it propagate? Is there any strong relationship between meteorological drought and others? These issues need further understanding regarding different climate regions. In this paper, monthly SRI and SPEI at different timescales during 1976 and 2005 were utilized to understand how streamflow drought responded to meteorological drought in Xiangjiang river basin, a semihumid basin of Central China. Impressive findings included that strong correlations between SRI and SPEI were found. SPEI of 2-month timescale behaved best when correlating with SRI (R
=
0.79). Longer timescales of SPEI seemed not to be useful for streamflow drought identification. At seasonal scale, higher correlation coefficients were obtained during dry season, whereas lower coefficients were found in wet season. The maximum R reached up to 0.89 in November at 2-month timescale. Besides, robust response relation between streamflow drought and meteorological drought was also found. The average response rate (R
r) was considerably high (75.4%), with the maximum obtained at 2-month timescale (R
r
=
82.9%). Meanwhile, important seasonal difference of response rate has also been pointed out.


---

## Body

## 1. Introduction

Drought is a multifaceted phenomenon that occurs across a range of temporal and spatial scales [1], characterized by periods of more than normal water deficit. It is one of the most damaging natural disasters all over the world [2], causing significant damage to different sectors of natural environment, such as vegetation growth [3, 4], crop yield [5, 6], water supply [7], desertification [8], and forest fire [9]. Due to global warming, the dry land areas have increased significantly in the past fifty years [10] and widespread severe droughts in the next 30–90 years over many land areas were also simulated by most models [11].Four basic categories of drought have been identified by Wilhite and Glantz in 1985 [12], which are meteorological drought, agricultural drought, hydrological drought, and socioeconomic drought. Prolonged severe meteorological drought will gradually propagate into different sectors of water resources, such as soil moisture, groundwater, and river discharge, leading to soil drought, groundwater drought, and streamflow drought. The propagation of drought through hydrologic system is complex, which may be affected by underlying conditions such as land cover, vegetation, and topography [13–15]. Understanding of this propagation procedure and how it behaves in different area would not only be helpful for drought monitoring and early warning, but also provide further support in theory and practical implications for making regional drought plans.A few number of previous studies have reported on the relationship between hydrological drought and meteorological drought. Part of studies have paid attention to the evolution of drought characteristics when it propagated through different hydrologic systems. Hisdal and Tallaksen conducted a study on the comparison between regional characteristics of meteorological drought and hydrological drought in Denmark and found that hydrological droughts were less homogeneous over Denmark, less frequent, and lasted for longer time periods than meteorological drought [16]. Peters et al. have also provided an evidence that the propagation of meteorological drought to groundwater drought decreased the number of drought events and caused a shift in the drought severity distribution [17]. Major related researches have been devoted to how the response of hydrological drought to meteorological drought varied in different timescales and the time-lag of hydrological drought to meteorological drought. Vicente-Serrano and López-Moreno found that surface flows responded to short time scales of meteorological drought (1–4 months) in a mountainous Mediterranean Basin [18]. Tabrizi et al. found that annual time scale of meteorological drought in the upstream of the Doroodzan watershed in Iran was useful in investigating occurrence of streamflow drought in the downstream [19]. Good correlation between annual PDSI, SPI, and Percentage of Rainfall Anomaly was found in ten major basins across China [20]. Four-month timescale of Standardized Precipitation Index (SPI) was proved to be the most suitable indicator when relating with standardized runoff index (SRI) in a typical semiarid inland basin of China [21]. A time-lag of 127 days regarding comparison between streamflow drought and meteorological drought was also found in this area [21]. Similar time lag of 7 months was found in a study conducted in the Awash River basin of Ethiopia [22]. At a small drought-prone basin in Oklahoma of USA, there was a time-lag of 2 months between SRI and SPI in model projection [23].Considering limited related previous studies on the relationship between hydrological drought and meteorological drought in Asia, the scope of this research lies in the response of streamflow drought to meteorological drought in a humid basin in Southern China. As indicated in a recent study [24], PET, in the face of climate change, an important component in the hydrologic cycle, should not be ignored in drought monitoring. Different to SPI, PET has been integrated into the Standardized Precipitation Evapotranspiration Index (SPEI) calculation [25], making it more efficient than SPI in drought monitoring at humid and semihumid areas, in which both precipitation and temperature are vital for drought identification.The main purpose is to test the usefulness of different timescales of SPEI to indicate streamflow drought and how the relation between streamflow drought and meteorological drought behaves in different seasons at humid regions, especially under trend of global warming. The objective is to select the most suitable timescale of SPEI to identify drought in river discharge. Results will be helpful in regional water resources planning and drought management.


## 2. Materials and Methods

### 2.1. Study Area and Data

Xiangjiang River basin is one of the largest subbasins of Yangtze River Basin. It is located in the southcentral China and most of the basin is within Hunan Province (Figure1). As a main tributary of the Yangtze River, the Xiangjiang River originates from the mountainous area in the southwest and flows into the Dongting Lake in the northeast. It has a total length of 844 km and forms a basin of 94,660 km2. The streamflow in this basin is mainly charged by precipitation. Robust linear relationship between monthly mean runoff and monthly precipitation during 1976 and 2005 was found in Figure 2. The elevation in the basin varies from 2098 m to 0 m, with high mountains in the south and southwest part and flat plains in the north. The basin is characterized as a humid subtropical monsoon climate by averaging monthly temperature and monthly rainfall during 1976 and 2005 (Figure 3). The annual average temperature is about 17.1°C and annual average evaporation is around 1200 mm. The annual rainfall ranges from 1170 mm to 2160 mm and it is unevenly distributed, making it prone to frequent flood and drought.Figure 1
Study area and the location of all gauging stations.Figure 2
Scatter diagram of monthly mean runoff and monthly precipitation during 1976 and 2005.Figure 3
Intra-annual variation of monthly average temperature and monthly rainfall during 1976 and 2005.There are six meteorological stations in this basin (see black dots in Figure1). They provide the meteorological information used in this study. The monthly precipitation and mean temperature data covering the period between 1960 and 2014 were provided by the China Meteorological Administration. The daily discharge data were obtained in Xiangtan station (green dot in Figure 1) which is the key hydrological station in the downstream of Xiangjiang River, covering the period between 1976 and 2005. The hydrological data were provided by the Changjiang Water Resources Commission (CWRC) of China. Quality test of meteorological data and discharge data has been conducted before calculation of SPEI and SRI.To avoid inhomogeneity in the meteorological data, we tested its homogeneity by correlating data series of each meteorological station with the regional average. Table1 shows the coefficients of Pearson correlation among the monthly precipitation and mean temperature series in each station and the regional average series. Correlation coefficients are very high and significant (P
<
0.01) in all meteorological stations (R
≥
0.87).Table 1
Pearson correlation between the average data series and the series of each meteorological station.
Station
Precipitation
Temperature
Shuangfeng
0.8731
0.9986
Nanyue
0.8852
0.9977
Yongzhou
0.8962
0.9996
Hengyang
0.8895
0.9991
Daoxian
0.8783
0.9989
Chenzhou
0.8583
0.9988


### 2.2. Methods

#### 2.2.1. Evaluation of Meteorological Drought

Meteorological drought events were evaluated based on the newly developed Standardized Precipitation Evapotranspiration Index (SPEI) [25]. The robustness of multiscale characteristics of time for SPEI is similar to the SPI [26]. And it also combines temperature into the model, which is used for calculating potential evapotranspiration (PET). We followed the Thornthwaite approach to calculate PET [27], which proved to be reliable in SPEI calculation [28].Computation of the SPEI requires long-term monthly meteorological data, which were arranged to appropriate time scales based on different goals, for example, 3 months, 6 months, 9 months, and 12 months. The different timescales (i-month) mean the different time lengths for accumulating precipitation data and averaging temperature data by backtracking. In this study, i-month timescale of SPEI was written in SPEIi by short. More detailed calculation procedures could be found in related references [25]. Input monthly precipitation and mean temperature for calculating SPEI were obtained by averaging the data from six meteorological stations, covering the period between 1960 and 2014. In this study, 1- to 12-month timescales of SPEI during 1976 and 2005 were extracted to coincide with the time span of SRI.The classification of meteorological drought based on SPEI value was given in Table2 [25]. Four major drought intensities were classified by the different values of SPEI.Table 2
Classification of drought intensity.
SPEI/SRI value
Drought intensity
(−1.00, −0.00]
Mild drought
(−1.50, −1.00]
Moderate drought
(−2.00, −1.50]
Severe drought
(−∞, −2.00]
Extreme drought


#### 2.2.2. Evaluation of Streamflow Drought

The SRI [29] was utilized to identify streamflow drought in this study. It was calculated in a manner similar to normal standardization procedure, which was given as(1)
S
R
I
i
j
=
R
i
j
-
R
j
-
σ
j
,where i and j were the year and month of the year, respectively (i
=
1976,1977
,
…
,
2005; j
=
1,2
,
3
,
…
,
12);R
j
- and σ
j were the mean and the standard deviation of R
i
j, respectively. R
i
j was the natural logarithm of the monthly mean discharge for the given ith year and the jth month. The timescale of SRI was one month.The classification of streamflow drought based on SRI value was given in Table2. Four major drought intensities were classified by the different values of SRI.


#### 2.2.3. The Response Rate of Streamflow Drought to Meteorological Drought

In this study, we used the response rate (R
r) to indicate the percentage of streamflow drought when meteorological drought occurred. It stands for how streamflow drought responds to different timescales of meteorological drought. The higher R
r means this response is more sensitive and vice versa. The specific algorithm for R
r was given below:(2)
R
r
=
n
m
×
100
%
,where m was the occurrence times of meteorological drought (SPEI < 0) during 1976 and 2005 and n was the occurrence times of streamflow drought (SRI < 0) under the condition that SPEI was less than 0.


## 2.1. Study Area and Data

Xiangjiang River basin is one of the largest subbasins of Yangtze River Basin. It is located in the southcentral China and most of the basin is within Hunan Province (Figure1). As a main tributary of the Yangtze River, the Xiangjiang River originates from the mountainous area in the southwest and flows into the Dongting Lake in the northeast. It has a total length of 844 km and forms a basin of 94,660 km2. The streamflow in this basin is mainly charged by precipitation. Robust linear relationship between monthly mean runoff and monthly precipitation during 1976 and 2005 was found in Figure 2. The elevation in the basin varies from 2098 m to 0 m, with high mountains in the south and southwest part and flat plains in the north. The basin is characterized as a humid subtropical monsoon climate by averaging monthly temperature and monthly rainfall during 1976 and 2005 (Figure 3). The annual average temperature is about 17.1°C and annual average evaporation is around 1200 mm. The annual rainfall ranges from 1170 mm to 2160 mm and it is unevenly distributed, making it prone to frequent flood and drought.Figure 1
Study area and the location of all gauging stations.Figure 2
Scatter diagram of monthly mean runoff and monthly precipitation during 1976 and 2005.Figure 3
Intra-annual variation of monthly average temperature and monthly rainfall during 1976 and 2005.There are six meteorological stations in this basin (see black dots in Figure1). They provide the meteorological information used in this study. The monthly precipitation and mean temperature data covering the period between 1960 and 2014 were provided by the China Meteorological Administration. The daily discharge data were obtained in Xiangtan station (green dot in Figure 1) which is the key hydrological station in the downstream of Xiangjiang River, covering the period between 1976 and 2005. The hydrological data were provided by the Changjiang Water Resources Commission (CWRC) of China. Quality test of meteorological data and discharge data has been conducted before calculation of SPEI and SRI.To avoid inhomogeneity in the meteorological data, we tested its homogeneity by correlating data series of each meteorological station with the regional average. Table1 shows the coefficients of Pearson correlation among the monthly precipitation and mean temperature series in each station and the regional average series. Correlation coefficients are very high and significant (P
<
0.01) in all meteorological stations (R
≥
0.87).Table 1
Pearson correlation between the average data series and the series of each meteorological station.
Station
Precipitation
Temperature
Shuangfeng
0.8731
0.9986
Nanyue
0.8852
0.9977
Yongzhou
0.8962
0.9996
Hengyang
0.8895
0.9991
Daoxian
0.8783
0.9989
Chenzhou
0.8583
0.9988


## 2.2. Methods

### 2.2.1. Evaluation of Meteorological Drought

Meteorological drought events were evaluated based on the newly developed Standardized Precipitation Evapotranspiration Index (SPEI) [25]. The robustness of multiscale characteristics of time for SPEI is similar to the SPI [26]. And it also combines temperature into the model, which is used for calculating potential evapotranspiration (PET). We followed the Thornthwaite approach to calculate PET [27], which proved to be reliable in SPEI calculation [28].Computation of the SPEI requires long-term monthly meteorological data, which were arranged to appropriate time scales based on different goals, for example, 3 months, 6 months, 9 months, and 12 months. The different timescales (i-month) mean the different time lengths for accumulating precipitation data and averaging temperature data by backtracking. In this study, i-month timescale of SPEI was written in SPEIi by short. More detailed calculation procedures could be found in related references [25]. Input monthly precipitation and mean temperature for calculating SPEI were obtained by averaging the data from six meteorological stations, covering the period between 1960 and 2014. In this study, 1- to 12-month timescales of SPEI during 1976 and 2005 were extracted to coincide with the time span of SRI.The classification of meteorological drought based on SPEI value was given in Table2 [25]. Four major drought intensities were classified by the different values of SPEI.Table 2
Classification of drought intensity.
SPEI/SRI value
Drought intensity
(−1.00, −0.00]
Mild drought
(−1.50, −1.00]
Moderate drought
(−2.00, −1.50]
Severe drought
(−∞, −2.00]
Extreme drought


### 2.2.2. Evaluation of Streamflow Drought

The SRI [29] was utilized to identify streamflow drought in this study. It was calculated in a manner similar to normal standardization procedure, which was given as(1)
S
R
I
i
j
=
R
i
j
-
R
j
-
σ
j
,where i and j were the year and month of the year, respectively (i
=
1976,1977
,
…
,
2005; j
=
1,2
,
3
,
…
,
12);R
j
- and σ
j were the mean and the standard deviation of R
i
j, respectively. R
i
j was the natural logarithm of the monthly mean discharge for the given ith year and the jth month. The timescale of SRI was one month.The classification of streamflow drought based on SRI value was given in Table2. Four major drought intensities were classified by the different values of SRI.


### 2.2.3. The Response Rate of Streamflow Drought to Meteorological Drought

In this study, we used the response rate (R
r) to indicate the percentage of streamflow drought when meteorological drought occurred. It stands for how streamflow drought responds to different timescales of meteorological drought. The higher R
r means this response is more sensitive and vice versa. The specific algorithm for R
r was given below:(2)
R
r
=
n
m
×
100
%
,where m was the occurrence times of meteorological drought (SPEI < 0) during 1976 and 2005 and n was the occurrence times of streamflow drought (SRI < 0) under the condition that SPEI was less than 0.


## 2.2.1. Evaluation of Meteorological Drought

Meteorological drought events were evaluated based on the newly developed Standardized Precipitation Evapotranspiration Index (SPEI) [25]. The robustness of multiscale characteristics of time for SPEI is similar to the SPI [26]. And it also combines temperature into the model, which is used for calculating potential evapotranspiration (PET). We followed the Thornthwaite approach to calculate PET [27], which proved to be reliable in SPEI calculation [28].Computation of the SPEI requires long-term monthly meteorological data, which were arranged to appropriate time scales based on different goals, for example, 3 months, 6 months, 9 months, and 12 months. The different timescales (i-month) mean the different time lengths for accumulating precipitation data and averaging temperature data by backtracking. In this study, i-month timescale of SPEI was written in SPEIi by short. More detailed calculation procedures could be found in related references [25]. Input monthly precipitation and mean temperature for calculating SPEI were obtained by averaging the data from six meteorological stations, covering the period between 1960 and 2014. In this study, 1- to 12-month timescales of SPEI during 1976 and 2005 were extracted to coincide with the time span of SRI.The classification of meteorological drought based on SPEI value was given in Table2 [25]. Four major drought intensities were classified by the different values of SPEI.Table 2
Classification of drought intensity.
SPEI/SRI value
Drought intensity
(−1.00, −0.00]
Mild drought
(−1.50, −1.00]
Moderate drought
(−2.00, −1.50]
Severe drought
(−∞, −2.00]
Extreme drought


## 2.2.2. Evaluation of Streamflow Drought

The SRI [29] was utilized to identify streamflow drought in this study. It was calculated in a manner similar to normal standardization procedure, which was given as(1)
S
R
I
i
j
=
R
i
j
-
R
j
-
σ
j
,where i and j were the year and month of the year, respectively (i
=
1976,1977
,
…
,
2005; j
=
1,2
,
3
,
…
,
12);R
j
- and σ
j were the mean and the standard deviation of R
i
j, respectively. R
i
j was the natural logarithm of the monthly mean discharge for the given ith year and the jth month. The timescale of SRI was one month.The classification of streamflow drought based on SRI value was given in Table2. Four major drought intensities were classified by the different values of SRI.


## 2.2.3. The Response Rate of Streamflow Drought to Meteorological Drought

In this study, we used the response rate (R
r) to indicate the percentage of streamflow drought when meteorological drought occurred. It stands for how streamflow drought responds to different timescales of meteorological drought. The higher R
r means this response is more sensitive and vice versa. The specific algorithm for R
r was given below:(2)
R
r
=
n
m
×
100
%
,where m was the occurrence times of meteorological drought (SPEI < 0) during 1976 and 2005 and n was the occurrence times of streamflow drought (SRI < 0) under the condition that SPEI was less than 0.


## 3. Results

### 3.1. Temporal Variability of SRI and SPEI

Monthly SRI and different timescales of SPEI in this basin were depicted in Figure4, covering the period between 1976 and 2005. Four main streamflow drought periods were recognized from SRI series, which were AUG/1977-SEP/1981 (streamflow drought period 1 (SDP1)), JUL/1983-APR/1993 (SDP2), AUG/1998-JUN/1999 (SDP3), and JUN/2003-JUN/2004 (SDP4). SDP1 and SDP2 were also characterized by intermittent short wet periods. The other two periods were much shorter, covered by continuous streamflow drought. The most severe streamflow drought occurred in SDP3, which was characterized by extremely low SRI value of consecutive three months (SRI of FMA/1999 < −2).Figure 4
Time series of SRI and different timescales of SPEI during 1976 and 2005.From views of SPEI at different timescales (Figure4), evolution of meteorological drought at different timescales can be identified. Higher drought frequency was found at shorter timescales of SPEI. Drought occurrence time of longer timescales lagged that of shorter timescales, which was indicated by that the red vertical stripes (drought events) inclined towards right. In addition, dominant drought spells along with their magnitude and duration can also be clearly seen from Figure 4. The most severe meteorological drought occurred in 1998-1999. Furthermore, a good correspondence between streamflow drought and meteorological drought can be found from the comparative analysis of SRI and SPEI at different timescales. Two severe or extreme meteorological drought periods mentioned above (1998-1999, 2003-2004) characterized by SPEI at all timescales correspond with SDP3 and SDP4 very well. This result indicated that consecutive severe meteorological drought could lead to severe or consecutive streamflow drought in this basin.


### 3.2. Relationship between SRI and Different Timescales of SPEI

The Pearson correlation coefficients between SRI and SPEI at different timescales were shown in Figure5. Correlation coefficients were high and significant at all timescales (R
>
0.55, P
<
0.01). There were significant differences with regard to timescales. The maximum correlation coefficient was obtained at 2-month timescale (R
=
0.79). The correlation decreased gradually along with the increasing timescales. It also indicated that the runoff of Xiangjiang River was mainly charged by rainfall of the current and previous months.Figure 5
Correlation between SRI and the SPEI at different time scales.A further analysis of the relationship between SRI and SPEI of different timescales at different months has been conducted. Significant seasonal difference regarding different timescales was found in Figure6. Higher correlation coefficients were found from October to March at all timescales (mean R
>
0.75, P
<
0.01). The lowest correlation coefficient was found in May, with most R at different timescales less than 0.5. Regarding timescales, the correlation at 1-month scale was low. It appeared much higher at 2-month scale and decreased gradually when timescale increased. The highest correlation was found at three parts in Figure 6 (the red region with R greater than 0.85). The top three high correlation coefficients were obtained in November at 2-month scale (R
=
0.89), August at 3-month scale (R
=
0.88), and March at 5-month scale (R
=
0.88). Figure 7 showed the SRI series and SPEI series at 2-month timescale in November. It can be clearly found that the fluctuation of SRI accorded with that of SPEI2 very well. Near all the peak and valley of SRI series corresponded to that of SPEI2.Figure 6
Monthly correlation coefficients between SRI and SPEI at different time scales.Figure 7
SRI and SPEI2 in November during 1976 and 2005.


### 3.3. Response of Streamflow Drought to Meteorological Drought

The response rate (R
r) of streamflow drought to meteorological drought at different timescales was shown in Figure 8. Strong response relationship was found between them. The R
r was considerably high at all timescales, with the average 75.4%. At short to medium timescales (1 to 8 months), the R
r remained at about 75% except that the peak value appeared at 2-month timescale (R
r
=
82.9
%). After 8-month scale, R
r declined gradually along with the increase of timescale and reached the minimum at 12-month scale (R
r
=
69.3
%). Results indicated that streamflow drought in Xiangjiang River basin responded to meteorological drought at 2-month timescale very well. When meteorological drought occurred (SPEI2 < 0), the probability of streamflow drought would reach up to 82.9%.Figure 8
Response rate of streamflow drought to meteorological drought at different timescales.Figure9 reflected the seasonal difference of response between streamflow drought and meteorological drought. Robust response relation was also found at monthly scale. A majority of response rate was larger than 70%. Moreover, remarkable monthly difference of R
r was shown clearly. The sensitivity of streamflow drought to meteorological drought differed in seasons and timescales. Shorter (1–4 months) timescales of SPEI could indicate streamflow drought (SRI < 0) better during January and July, whereas medium timescales (5–9 months) of SPEI perform better for indicating streamflow drought from August to December. Higher response rate was found during autumn and winter months (dry seasons). The possible reason is that streamflow responds to rainfall sensitively in dry seasons, while, in wet seasons, this relationship could be affected by other factors such as much more frequent heavy rainfall, stronger evapotranspiration associated with high temperature, and higher water demand such as agricultural irrigation and higher domestic water demands of urban and rural inhabitants. The top three high response rates were obtained in November at 7-month scale (R
r
=
93.8
%), February at 3-month scale (R
r
=
92.9
%), and July at 1-month scale (R
r
=
92.3
%). The lowest R
r appeared in May, with the minimum equal to 41.7%.Figure 9
Monthly response rate of streamflow drought to meteorological drought at different timescales.


## 3.1. Temporal Variability of SRI and SPEI

Monthly SRI and different timescales of SPEI in this basin were depicted in Figure4, covering the period between 1976 and 2005. Four main streamflow drought periods were recognized from SRI series, which were AUG/1977-SEP/1981 (streamflow drought period 1 (SDP1)), JUL/1983-APR/1993 (SDP2), AUG/1998-JUN/1999 (SDP3), and JUN/2003-JUN/2004 (SDP4). SDP1 and SDP2 were also characterized by intermittent short wet periods. The other two periods were much shorter, covered by continuous streamflow drought. The most severe streamflow drought occurred in SDP3, which was characterized by extremely low SRI value of consecutive three months (SRI of FMA/1999 < −2).Figure 4
Time series of SRI and different timescales of SPEI during 1976 and 2005.From views of SPEI at different timescales (Figure4), evolution of meteorological drought at different timescales can be identified. Higher drought frequency was found at shorter timescales of SPEI. Drought occurrence time of longer timescales lagged that of shorter timescales, which was indicated by that the red vertical stripes (drought events) inclined towards right. In addition, dominant drought spells along with their magnitude and duration can also be clearly seen from Figure 4. The most severe meteorological drought occurred in 1998-1999. Furthermore, a good correspondence between streamflow drought and meteorological drought can be found from the comparative analysis of SRI and SPEI at different timescales. Two severe or extreme meteorological drought periods mentioned above (1998-1999, 2003-2004) characterized by SPEI at all timescales correspond with SDP3 and SDP4 very well. This result indicated that consecutive severe meteorological drought could lead to severe or consecutive streamflow drought in this basin.


## 3.2. Relationship between SRI and Different Timescales of SPEI

The Pearson correlation coefficients between SRI and SPEI at different timescales were shown in Figure5. Correlation coefficients were high and significant at all timescales (R
>
0.55, P
<
0.01). There were significant differences with regard to timescales. The maximum correlation coefficient was obtained at 2-month timescale (R
=
0.79). The correlation decreased gradually along with the increasing timescales. It also indicated that the runoff of Xiangjiang River was mainly charged by rainfall of the current and previous months.Figure 5
Correlation between SRI and the SPEI at different time scales.A further analysis of the relationship between SRI and SPEI of different timescales at different months has been conducted. Significant seasonal difference regarding different timescales was found in Figure6. Higher correlation coefficients were found from October to March at all timescales (mean R
>
0.75, P
<
0.01). The lowest correlation coefficient was found in May, with most R at different timescales less than 0.5. Regarding timescales, the correlation at 1-month scale was low. It appeared much higher at 2-month scale and decreased gradually when timescale increased. The highest correlation was found at three parts in Figure 6 (the red region with R greater than 0.85). The top three high correlation coefficients were obtained in November at 2-month scale (R
=
0.89), August at 3-month scale (R
=
0.88), and March at 5-month scale (R
=
0.88). Figure 7 showed the SRI series and SPEI series at 2-month timescale in November. It can be clearly found that the fluctuation of SRI accorded with that of SPEI2 very well. Near all the peak and valley of SRI series corresponded to that of SPEI2.Figure 6
Monthly correlation coefficients between SRI and SPEI at different time scales.Figure 7
SRI and SPEI2 in November during 1976 and 2005.


## 3.3. Response of Streamflow Drought to Meteorological Drought

The response rate (R
r) of streamflow drought to meteorological drought at different timescales was shown in Figure 8. Strong response relationship was found between them. The R
r was considerably high at all timescales, with the average 75.4%. At short to medium timescales (1 to 8 months), the R
r remained at about 75% except that the peak value appeared at 2-month timescale (R
r
=
82.9
%). After 8-month scale, R
r declined gradually along with the increase of timescale and reached the minimum at 12-month scale (R
r
=
69.3
%). Results indicated that streamflow drought in Xiangjiang River basin responded to meteorological drought at 2-month timescale very well. When meteorological drought occurred (SPEI2 < 0), the probability of streamflow drought would reach up to 82.9%.Figure 8
Response rate of streamflow drought to meteorological drought at different timescales.Figure9 reflected the seasonal difference of response between streamflow drought and meteorological drought. Robust response relation was also found at monthly scale. A majority of response rate was larger than 70%. Moreover, remarkable monthly difference of R
r was shown clearly. The sensitivity of streamflow drought to meteorological drought differed in seasons and timescales. Shorter (1–4 months) timescales of SPEI could indicate streamflow drought (SRI < 0) better during January and July, whereas medium timescales (5–9 months) of SPEI perform better for indicating streamflow drought from August to December. Higher response rate was found during autumn and winter months (dry seasons). The possible reason is that streamflow responds to rainfall sensitively in dry seasons, while, in wet seasons, this relationship could be affected by other factors such as much more frequent heavy rainfall, stronger evapotranspiration associated with high temperature, and higher water demand such as agricultural irrigation and higher domestic water demands of urban and rural inhabitants. The top three high response rates were obtained in November at 7-month scale (R
r
=
93.8
%), February at 3-month scale (R
r
=
92.9
%), and July at 1-month scale (R
r
=
92.3
%). The lowest R
r appeared in May, with the minimum equal to 41.7%.Figure 9
Monthly response rate of streamflow drought to meteorological drought at different timescales.


## 4. Discussion and Conclusion

In order to understand how streamflow drought responded to meteorological drought in the Xiangjiang River basin, monthly SRI and SPEI of different timescales during 1976 and 2005 were calculated to identify streamflow drought and meteorological drought, respectively. Correlation and response relationship have been investigated. Robust relation between streamflow drought and meteorological drought was found in this basin. The main conclusions were summarized as below:(1)
Relationship between streamflow drought and meteorological drought can be investigated well by the comparative analysis of SRI and SPEI at different timescales. Continuous severe meteorological drought would propagate to severe or consecutive streamflow drought in this basin, whereas intermittent or moderate meteorological drought may lead to separate streamflow drought.
(2)
Robust correlation between SRI and SPEI was found. SPEI of 2-month timescale behaved best in correlating with SRI (R
=
0.79, P
<
0.01). The longer the timescale of SPEI was, the weaker the correlation was. At seasonal scale, significant difference of correlation was found. Higher correlation coefficients were obtained during dry season (October to March), with the maximum R reaching up to 0.89, whereas the minimum was found in wet season (April to June). These findings agreed with the results carried out in the Aragon River basin of the central Spanish Pyrenees [18].
(3)
Remarkable results were also found regarding to the response rate of streamflow drought to meteorological drought. The average response rate was considerably high (75.4%). MaximumR
r was obtained at 2-month timescale (R
r
=
82.9
%). It stated again that SPEI2 could be used as a good indicator in streamflow drought identification. Besides, R
r differed greatly in different seasons. Shorter timescales of meteorological drought could indicate streamflow drought better during winter and spring, whereas streamflow drought in late summer to autumn responded to meteorological drought at medium timescales.In this study, important relationship between streamflow drought and meteorological drought has been pointed out. This relation would provide scientific support in drought mitigation and regional water resources management. It is also necessary to test the most suitable timescale of meteorological drought index before drought monitoring of different hydrologic variables. Generally, shorter timescales of meteorological drought indices proved to be better when relating to streamflow. Vicente-Serrano and López-Moreno have indicated that 1–4 months of SPI could relate to the surface flows quite well in a mountainous Mediterranean Basin [18]. A case study conducted in two reservoirs in central Spain has shown that very high correlations (>0.9) were found between hydrological and climatic droughts for timescales between 3 and 5 months, by relating SPI, SPEI to the z-standardized inflows [30]. In a plain basin surrounded by high mountains in Greece, higher correlations have also been obtained with the 3-month SPI and 6-month SPI when relating to a standardized runoff index [31]. In another case study conducted in a semiarid basin of China, similar results had indicated that SPI of 4-month timescale correlated with SRI better [21].In addition, seasonality must also be investigated carefully. Different timescales of meteorological drought indices may behave totally different in various seasons. Streamflow response to climatic droughts may be very different as a function of the river regimes [32]. So, the selection of the most suitable timescale regarding different months before utilizing SPEI to indicates that streamflow drought is of great importance. In this study, SPEI2 was proved to be the most suitable index when relating to SRI generally, whereas SPEI1 and SPEI7 behaved best in July and November, respectively. In central Spain, very high correlations were found between hydrological and climatic droughts from January to March for timescales between 3 and 5 months. In contrast, correlations during summer months were very low at the shortest timescales [30]. However, in some high-latitude Asian basins that drain to the Arctic Ocean, correlations between SPEI and SSI were much higher in July than in January [32].The noticeable timescale issue and seasonality may depend on the basin characteristics, elevation, terrain, climate zone, vegetation cover, and water resources regulation. How do these factors affect the sensitivity of streamflow drought to meteorological drought? Maybe it can be explained by comparison among similar basins in the future research. Besides, interannual variability of the propagation procedure under global warming could be obtained if there is long-term hydrologic and climatic data. Furthermore, how meteorological drought propagate through the hydrologic system quantitatively and the time lag between meteorological drought and other types of drought are also interesting issues that should be addressed in a future study.



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*Source: 1634787-2015-12-30.xml*