Research Article  Open Access
Linlin Fan, Hongrui Wang, Cheng Wang, Wenli Lai, Yong Zhao, "Exploration of Use of Copulas in Analysing the Relationship between Precipitation and Meteorological Drought in Beijing, China", Advances in Meteorology, vol. 2017, Article ID 4650284, 11 pages, 2017. https://doi.org/10.1155/2017/4650284
Exploration of Use of Copulas in Analysing the Relationship between Precipitation and Meteorological Drought in Beijing, China
Abstract
Drought risk analysis is essential for regional water resource management. In this study, the probabilistic relationship between precipitation and meteorological drought in Beijing, China, was calculated under three different precipitation conditions (precipitation equal to, greater than, or less than a threshold) based on copulas. The Standardized Precipitation Evapotranspiration Index (SPEI) was calculated based on monthly total precipitation and monthly mean temperature data. The trends and variations in the SPEI were analysed using HilbertHuang Transform (HHT) and MannKendall (MK) trend tests with a running approach. The results of the HHT and MK test indicated a significant decreasing trend in the SPEI. The copulabased conditional probability indicated that the probability of meteorological drought decreased as monthly precipitation increased and that 10 mm can be regarded as the threshold for triggering extreme drought. From a quantitative perspective, when mm, the probabilities of moderate drought, severe drought, and extreme drought were 22.1%, 18%, and 13.6%, respectively. This conditional probability distribution not only revealed the occurrence of meteorological drought in Beijing but also provided a quantitative way to analyse the probability of drought under different precipitation conditions. Thus, the results provide a useful reference for future drought prediction.
1. Introduction
Drought is a recurrent extreme climate event that affects every aspect of the natural environment, as well as human lives [1]. It is defined as a natural temporary imbalance in water availability, which may be related to persistently lowerthanaverage precipitation. Droughts have uncertain frequencies, durations, and severities, and their occurrence is difficult to predict. Additionally, the water resource availability and carrying capacity of an ecosystem are diminished [2, 3]. Based on these factors, drought analysis has been a challenging topic in water resource management.
A variety of studies have examined the different aspects of drought phenomena by developing different drought indices [4–9], analysing the spatiotemporal patterns of drought [10–12], and predicting future drought risks [13, 14]. Regarded as a complex hydrologic event, drought is a type of multivariate event that is characterized by a few correlated random variables. Thus, a number of studies have focused on constructing multivariate distributions of drought characteristics, such as the intensity, duration, frequency, and recurrence [15–18]. Copulas are effective tools in multivariate distribution construction. They use a nonlinear approach to establish the joint probability distribution of two or more related variables and are able to model the dependence structure between random variables independent of their marginal distributions. Since Sklar [19] first introduced copulas, they have been widely used in waterrelated research fields. When using copulas for drought analysis, a joint probability distribution has commonly been used between different characteristics of drought. Shiau [20] used twodimensional copulas to construct a joint drought duration and severity distribution for the first time. Song and Singh [21] used threedimensional metaelliptical copulas to construct a joint drought duration, severity, and interarrival time distribution. Similar studies [22–27] have shown that copulas are useful in exploring the associations among correlated drought variables.
Apart from the joint probability distribution, copulas are also able to establish conditional probability distributions. Unlike joint probability, conditional properties can provide the probability distributions of drought under different conditions. Saghafian and Mehdikhani [28] investigated the conditional return periods of drought severity, peak, and duration based on a conditional probability distribution established by copulas. Additionally, Madadgar and Moradkhani [29] applied conditional probability for drought prediction. By incorporating copulas into a Bayesian framework, they developed a probabilistic forecasting model for predicting future spring drought status given the drought conditions in the previous season. Hao et al. [30] proposed a hydrological drought prediction method based on a metaGaussian model of conditional probability. The model considered the drought persistence and the prior meteorological drought conditions.
Since climate change and the increasing global warming trend have affected hydrological events in recent years, it is important to consider climatic variables when analysing drought. Generally, drought originates from a precipitation deficit, which first causes meteorological drought. Zhang et al. [31] studied how precipitation and temperature affect drought occurrence. They concluded that the similarity coefficient between the drought probability and low precipitation probability in China was 0.9732, reflecting a strong relationship between drought and precipitation. Copulas can be used to combine precipitation and drought indexes and to provide conditional probability distributions (with precipitation as the condition) between them. From this conditional probability distribution, we can quantify the probability of drought occurrence under different precipitation conditions.
Beijing is located in the dry northern part of China, which experienced water crises caused by drought from 1980 to 1985 and from 1999 to 2007 [32]. Cai et al. [33] evaluated the spatiotemporal characteristics of drought in the BeijingTianjinHebei metropolitan region. Liu et al. [34] proposed a vegetationdependent temperaturevegetation dryness index model for analysing regional drought disasters in the BeijingTianjinHebei metropolitan region. Li et al. [35] analysed the joint probability and return period of the drought severity and duration during the growth period of winter wheat in Beijing. Such studies have focused more on the spatiotemporal characteristics of drought and drought variables. They found that Beijing experienced quite frequent moderate and severe droughts, especially during the periods of 1965–1973 and 1997–2002. In addition, the risk of drought during winter was very high, and the area affected by drought was >70,000 ha. However, similar studies have focused less on how the climatic variables can affect drought conditions.
In this study, a conditional probability distribution was applied for meteorological drought analysis based on copulas. Monthly total precipitation and monthly mean temperature data from 1951 to 2013 were collected from one meteorological station to calculate the Standardized Precipitation Evapotranspiration Index (SPEI). After a temporal analysis of the SPEI based on the HilbertHuang Transform (HHT) and MannKendall (MK) trend test, the meteorological drought probability was analysed under three different precipitation conditions (precipitation equal to, greater than, or less than a threshold).
2. Materials and Methods
2.1. Data and SPEI Calculation
The SPEI was used to represent meteorological drought. A meteorological station in Beijing (latitude 39.80°N, longitude 116.47°E) was chosen as the study site. The monthly total precipitation (mm) and monthly mean air temperature (°C) data from 1951 to 2013 were collected from the National Climate Center of the China Meteorological Administration (http://data.cma.cn/). The SPEI describes the effects of drought on vegetation and agricultural practices on shortterm scales and represents a broad proxy for water resource management on longterm scales [36]. In this study, we calculated both shortterm (1 month) and longterm (12 months) SPEI values for meteorological drought analysis. According to the definition of the SPEI, the month SPEI is based on precipitation and evapotranspiration total for the previous months. Thus, a 12month SPEI represents conditions over the full calendar year, while a 1month SPEI represents conditions within a single month. The aim of analysing the temporal characteristics of the SPEI is to explore the changing patterns in meteorological drought conditions between different years and provide a holistic view. Thus, we chose the 12month SPEI for this part of the analysis. Meanwhile, the goal of the copulabased analysis of precipitation and SPEI is to obtain the conditional probability distributions of meteorological drought given different precipitation conditions. Conditional probability distributions can be used for meteorological drought prediction in the future. Because shortterm drought prediction is more practical than longterm prediction, we used the 1month SPEI for the copulasbased analysis.
The calculation process can be divided into the following three steps [8].
Calculate the water balance for month according to the following equation:where is monthly total precipitation and is potential evapotranspiration, which was calculated using the Thornthwaite method [37]. The calculated values are aggregated at different time scales. The difference in month and year depends on the chosen time scale . For example, the accumulated difference for one month in a particular year with a 12month time scale is calculated as follows:where is the difference in month and year i, in millimetres.
Use a threeparameter loglogistic probability density function to fit the established series. Then, obtain the cumulative probability function as follows:where is the probability density function of series; is the probability distribution function of series; and α, β, and γ are scale, shape, and origin parameters, respectively, for values, which can be obtained using an Lmoments approach.
Obtain the SPEI as the standardized values of :where is the probability of exceeding a determined value and . If , then is replaced by , and the sign of the resultant SPEI is reversed. The constants are as follows: = 2.515517, = 0802853, = 0.010328, = 1.432788, = 0.189269, and = 0.001308.
The SPEI follows the same classification criteria as the Standardized Precipitation Index (SPI) because of the similarity in the calculation principles of SPEI and SPI [11]. Table 1 reports the climate classification according to the SPEI [5].

2.2. Methods of Analysing Temporal Characteristics
2.2.1. HilbertHuang Transform
The HHT method was used to analyse the periodic features of the SPEI. The HHT comprises two algorithms: empirical mode decomposition (EMD) and Hilbert transform. After the EMD application, the original time series can be divided into several intrinsic mode functions (IMF) and one residual (RES). Each IMF represents a period, and RES represents the overall trend of the original time series. A Hilbert transform is then performed on each IMF to find its instantaneous frequency and amplitude. Thus, it provides the timefrequencyamplitude relationship of all the IMFs together. The calculation process is based on that presented in [38].
2.2.2. MannKendall Trend Test with a Running Approach
The MK nonparametric test is widely used in the hydrological field for trend analysis [39, 40]. The related equations for calculating the MK test statistic and the standardized test statistic are as follows:where and are the sequential data values of the time series in years and , respectively, and is the length of the time series. Positive values of indicate increasing trends, while negative values indicate decreasing trends. When , a significant trend exists in the time series. is the critical value of from the standard normal table, and at the 5% significance level, the value of is 1.96.
In this paper, the MK test was employed for SPEI trend analysis using a running approach, which was conducted as shown in Figure 1 [36].
When applying the approach shown in Figure 1 in this paper, the minimum window width was 10 years. The maximum window width was 63 years.
2.3. Copula Theory
2.3.1. Copula Definition and Selection
Copulas offer a flexible way of describing the dependence structure of multivariate data independent of their marginal probability distributions. Additionally, copulas are powerful tools for modelling and sampling multivariate data that are nonlinearly interrelated. Gumbel, Frank, and Clayton copulas are all Archimedean copulas, which have been widely used in drought analysis. In this paper, these three types of copulas are chosen to match the two variables (precipitation and SPEI). The cumulative distribution functions (CDF) of the Gumbel, Frank, and Clayton copulas are described in (6) to (8):
Gumbel is
Frank is
Clayton iswhere and are two variables and is the copula parameter. is the Kendall rank correlation coefficient, which can be calculated using (7):where sgn is the sign function, is the number of samples, and is the actual data.
Ordinary least squares (OLS), mean square error (MSE) [41], Akaike information criterion (AIC) [42], and Bayesian information criterion (BIC) [43] were used to assess the fitting results of different copulas and to identify the bestperforming one. The minimum value reflects the bestfitting result. The OLS, MSE, AIC, and BIC measures were defined as follows: where is the empirical frequency, is the theoretical frequency, is the number of copula parameters, and is the number of samples.
2.3.2. Conditional Probability Distribution
To distinguish between the abbreviations of precipitation and probability (both capital letter P), we use R (short for rainfall) as the abbreviation for precipitation and as the abbreviation for SPEI. With the joint probability distribution of precipitation and SPEI, the conditional probability can be calculated in three ways.
Given a certain precipitation threshold , the conditional CDF of the SPEI is given as follows [44]:
If precipitation exceeds a certain threshold , the probability that the SPEI is less than a certain threshold or exceeds a certain threshold is given as follows [45]:where and are the marginal CDFs of precipitation and the SPEI, respectively; is the joint CDF of precipitation and SPEI, which is derived using copulas; and is the unique copula function that links and to form the joint CDF.
When applying copulas, five steps should be followed.
Step 1. Determine the marginal distributions of two variables based on the collected data.
Step 2. Determine the Kendall rank correlation coefficient to establish whether the two variables are related.
Step 3. According to , calculate the parameter for the Gumbel, Frank, and Clayton copulas to obtain the expressions of different copula functions.
Step 4. Choose the bestfitting copula function based on OLS, MSE, AIC, and BIC criteria.
Step 5. Calculate the conditional probability distribution according to the corresponding functions.
All the methods used in this paper, such as HHT, the MK trend test, and copulas, were executed using MATLAB® software.
3. Results and Discussion
3.1. SPEI Calculation Results
The SPEI was calculated at both the 1month (shortterm) and 12month (longterm) scales from 1951 to 2013 (Figure 2). Both the 1month SPEI and 12month SPEI exhibited fluctuating patterns. The 12month SPEI (Figure 2(a)) was used for trend and period analysis, while the 1month SPEI (Figure 2(b)) was used for establishing copula functions between monthly precipitation and the SPEI.
(a)
(b)
3.2. SPEI Trend and Period
The HHT method was applied to analyse the periodic features of the 12month SPEI. After the EMD application, the original SPEI was decomposed into four IMFs and one RES (Figure 3). Hilbert transform was conducted on four IMFs and one RES to obtain the timefrequencyamplitude Hilbert spectrum (Figure 4). From the EMD results in Figure 3, the average periods of IMF1, IMF2, IMF3, and IMF4 were 2.7 years, 5 years, 10 years, and 18 years, respectively. In particular, the RES exhibited a decreasing trend. The Hilbert spectrum (Figure 4) offers a different method of analysing IMF and RES values from the point of view of energy variations. The colours of lines and dots represent the energy. The period is the reciprocal of the frequency. Thus, a lower frequency reflects a longer period. The two lines near the horizontal ordinate can be described as lowfrequency and highenergy lines. The periods of these two lines were larger than those of others, indicating that RES and IMF4 had periods longer than 18 years. This phenomenon indicates that large periods, especially periods over 18 years, were the major SPEI periods, and they significantly influenced the variations in SPEI. In the upper part of Figure 3, the highfrequency IMFs appear as vaguely scattered dots. These scattered dots also displayed high energy, indicating that short 2–5year periods can significantly influence the variations in SPEI.
The MK trend test with a running approach was applied to analyse the trend characteristics of different start times and durations. The trends were plotted for better visualization. The axis indicates the window width, and the axis is the first year of the window to which the trend refers (Figure 5). The value of the trend is characterized by the coloured triangle symbols. An increasing or decreasing trend is significant when . This figure captures the entire spectrum of significant trends present in the series; thus, it provides all detailed subseries information. The frequency of each symbol in Figure 5 is summarized in Table 2.

From Table 2, 80% of the subseries displayed a general decrease, half of which were significant. Most blue inverted triangle symbols appeared in the upperright portion of Figure 5, indicating a significant decreasing trend for the entire SPEI series. For the largest window widths, a significant decreasing pattern was detected (the blue inverted triangle in the upperleft portion of the figure). In the first years of the observation period, for temporal window widths of less than 15 years, an insignificant increasing trend was detected (yellow triangles in the bottomleft portion of the figure). This phenomenon is consistent with the RES result, with a slight increasing trend from 1951 to 1965. A significant increasing trend was also detected in recent years from 1998 to 2013 (red triangles in the bottomright portion of the figure).
3.3. Conditional Probability between Precipitation and SPEI
Figure 6 illustrates the marginal distributions of and the SPEI. The CDF of precipitation fit an exponential distribution, while the SPEI values fit a normal distribution.
(a)
(b)
The statistical dependencies between and SPEI were estimated using statistical measures. Kendall’s τ was calculated to be 0.734, indicating a strong positive dependence between and SPEI. Initially, the Gumbel, Frank, and Clayton copulas were established to jointly describe the two variables. The OLS, MSE, AIC, and BIC criteria were used to compare the fits of the different copula models and to select the model that best described the dependency between the two variables. The results, which are presented in Table 3, show that the bestfitting model was the Clayton copula; therefore, it was chosen for use in this study.

When precipitation equals a threshold, that is, , the probability of SPEI can be calculated based on (12). Figure 7(a) illustrates the conditional probabilities in three ways: SPEI , SPEI , and SPEI . According to the classification of SPEI in Table 1, SPEI ≤ −2 represents the conditions of extreme drought and worse, SPEI represents the conditions of severe drought and worse, and SPEI represents the conditions of moderate drought and worse. In Figure 7(a), all three curves exhibit decreasing trends, which suggests that the probability of drought decreases as monthly precipitation increases. Additionally, the slopes of the three curves display the same decreasing pattern. The curve of SPEI is above the other two curves, indicating a higher probability.
(a)
(b)
(c)
When precipitation exceeds a threshold, that is, , the probability of SPEI can be calculated based on (13). Figure 7(b) illustrates the conditional probabilities of five conditions: R ≥ 10 mm, R ≥ 20 mm, R ≥ 50 mm, R ≥ 100 mm, and R ≥ 200 mm. The axis represents the values of SPEI, while the axis represents the probability that SPEI is less than the corresponding value. In other words, these curves can be regarded as the CDF of the SPEI. The shape of the five curves is similar to a normal distribution, in which the probability that SPEI = 0 is approximately 0.5. The curve of R ≥ 200 mm plots lowest in the figure, while the curve of R ≥ 10 mm is at the top. This result suggests that the probability of drought decreases as the precipitation threshold increases.
When precipitation is equal to or less than a threshold, that is, , the probability of SPEI can be calculated based on (14). Figure 7(c) illustrates the conditional probabilities of five conditions: R ≤ 10 mm, R ≤ 20 mm, R ≤ 50 mm, R ≤ 100 mm, and R ≤ 200 mm. In this sense, Figure 7(c) also illustrates the CDF of SPEI for precipitation greater than a threshold. The shapes of the five curves in Figure 7(c) are similar to a normal distribution. Similar to the curves in Figure 7(b), the curve of R ≤ 200 mm plots at the bottom, while the curve of R ≤ 10 mm is at the top. This result suggests that the probability of drought decreases as the threshold of precipitation increases.
The three diagrams in Figure 7 all correspond to the same trend: the probability of drought decreases as precipitation increases. This rule is logical, as precipitation can alleviate drought. However, the diagrams in Figure 7 can further provide a quantitative relationship between precipitation and meteorological drought. In Figure 7(a), when precipitation ranges from 0 to 20 mm, the curves of SPEI and SPEI exhibit large decreasing trends; however, when precipitation increases above 20 mm, the curves are concave. For the curve of SPEI , the inflection point occurs when precipitation is approximately 10 mm. Thus, 10 mm can be regarded as the monthly precipitation threshold for triggering extreme drought phenomena, while 20 mm can be considered the threshold value for lesser droughts. Within the threshold value, even 1 mm of precipitation can effectively reduce the incidence of drought. Quantitatively, when monthly precipitation in Beijing is less than 20 mm, the probability of moderate drought occurrence is 8%, the probability of severe drought occurrence is 15%, and the probability of extreme drought occurrence is 5%.
Figures 7(b) and 7(c) are two types of cumulative probability distributions for the SPEI. The probability of each type of drought (or level of wetness) classified in Table 1 can be calculated based on these cumulative probability distributions, as shown in the diagrams in Figure 8. The axis indicates the SPEI class in Table 1 divided by the SPEI value (going from dry to wet conditions from Class 7 to Class 1). For instance, Class 7 represents extreme drought, Class 4 represents normal conditions, and Class 2 represents very wet conditions. The axis indicates the probability of meteorological drought. Figure 8(a) was calculated from Figure 7(b) for precipitation exceeding a threshold . The upper diagram in Figure 8(a) demonstrates the probabilities of all seven classes. The probability of a normal situation is the largest at approximately 70% for all five conditions, and this probability is far higher than those of the other six classes. The probabilities of wet conditions are higher than those of drought conditions. To obtain a clear view of the probability of drought, we magnified the diagram to obtain the bottom plot in Figure 8(a). The probabilities of extreme drought, severe drought, and moderate drought are all below 10% for the five conditions. Figure 8(b) was calculated from Figure 7(c) for precipitation equal to or less than a threshold . The probability of each scenario is listed in Table 4. The probability of normal conditions (Class 4) is the highest, but different situations vary. The probabilities of drought conditions are higher than those of wet conditions. When R ≤ 10 mm, the probabilities of moderate drought, severe drought, and extreme drought are 22.1%, 18%, and 13.6%, respectively. When increases above 20 mm, the probability of each class does not vary considerably.

(a)
(b)
This copulabased conditional probability between and SPEI not only reveals the occurrence of drought in Beijing but also provides a probability distribution of drought under different precipitation conditions. This quantitative distribution is based on a comprehensive analysis of historical data, and it can be used for future drought prediction. For instance, if we know how much precipitation will occur in the next month, then we can refer to this probability distribution and obtain the risk associated with each type of drought. Copula functions are effective tools for establishing relationships between related variables based on a nonlinear approach. However, in this study, we used data from only one station and analysed only the relationship between precipitation and meteorological drought. In future studies, these analysis methods can be expanded for similar fields, and other meteorological variables that affect drought conditions (temperature, wind speed, sun exposure, etc.) can be considered.
4. Conclusions
In this paper, copulas were applied to analyse the probabilistic relationship between monthly precipitation and SPEI (representing the situations of meteorological drought) based on three conditions (, , and ) in Beijing, China. The HHT and MK trend tests with a running approach were also applied to analyse the temporal variations in the SPEI.
Results from HHT method indicated that the SPEI varied in four periods: 18 years, 10 years, 5 years, and 3 years. The results from MK test with a running approach showed a significant decreasing trend for the entire SPEI series and insignificant increasing trends from 1951 to 1965 and 1998 to 2013, respectively.
When establishing the copula functions, Clayton copula was selected as the bestfitting copula. Based on the conditional probability method, the probability of drought was calculated based on three conditions (, , and ). For all three conditions, the probability of meteorological drought decreased as monthly precipitation increased, and 10 mm can be regarded as the threshold for triggering extreme drought, while 20 mm can be regarded as the threshold for lesser droughts. From a quantitative perspective, when precipitation is equal to 20 mm, the probability of moderate drought, severe drought, and extreme drought is 8%, 15%, and 5%, respectively. For , the probability of normal conditions is approximately 70%, which is the largest among all 7 classes. The probabilities of wet conditions are larger than those of drought conditions. Notably, the probabilities of extreme drought, severe drought, and moderate drought are all below 10%. When , the probabilities of drought conditions are higher than those of wet conditions. The probabilities of moderate drought, severe drought, and extreme drought are 22.1%, 18%, and 13.6%, respectively, when ≤ 10 mm.
Conflicts of Interest
The authors declare no conflicts of interest.
Acknowledgments
This work was supported by the National Natural Science Foundation of China (Grants nos. 51479003, 51279006, and 51309016) and National Key R&D Program of China (Grant no. 2016YFC0401407).
References
 S. Madadgar and H. Moradkhani, “Drought analysis under climate change using copula,” Journal of Hydrologic Engineering, vol. 18, no. 7, pp. 746–759, 2013. View at: Publisher Site  Google Scholar
 L. S. Pereira, I. Cordery, and I. Iacovides, Coping with Water Scarcity: Addressing the Challenges, Springer, Netherlands, 2009. View at: Publisher Site
 T. Raziei, B. Saghafian, A. A. Paulo, L. S. Pereira, and I. Bordi, “Spatial patterns and temporal variability of drought in Western Iran,” Water Resources Management, vol. 23, no. 3, pp. 439–455, 2009. View at: Publisher Site  Google Scholar
 A. Zargar, R. Sadiq, B. Naser, and F. I. Khan, “A review of drought indices,” Environmental Reviews, vol. 19, no. 1, pp. 333–349, 2011. View at: Publisher Site  Google Scholar
 T. B. McKee, N. J. Doesken, and J. Kleist, “The relationship of drought frequency and duration to time scale,” in Procceding of the 8th Conference on Applied Climatology, pp. 179–186, American Meteorological Society, Anaheim, Calif, USA, January 1993. View at: Google Scholar
 T. B. McKee, N. J. Doesken, and J. Kleist, “Drought monitoring with multiple time scales,” in Proceeding of the 9th Conference on Applied Climatology, pp. 233–236, Boston, Mass, USA, 1995. View at: Google Scholar
 W. C. Palmer, “Meteorological drought,” Research Paper 45, U.S. Dept. of Commerce, Office of Climatology, U.S. Weather Bureau, Washington, DC, USA, 1965. View at: Google Scholar
 S. M. VicenteSerrano, S. Beguería, and J. I. LópezMoreno, “A multiscalar drought index sensitive to global warming: the standardized precipitation evapotranspiration index,” Journal of Climate, vol. 23, no. 7, pp. 1696–1718, 2010. View at: Publisher Site  Google Scholar
 S. Beguería, S. M. VicenteSerrano, F. Reig, and B. Latorre, “Standardized precipitation evapotranspiration index (SPEI) revisited: parameter fitting, evapotranspiration models, tools, datasets and drought monitoring,” International Journal of Climatology, vol. 34, no. 10, pp. 3001–3023, 2014. View at: Publisher Site  Google Scholar
 G. Tsakiris, D. Pangalou, and H. Vangelis, “Regional drought assessment based on the reconnaissance drought index (RDI),” Water Resources Management, vol. 21, no. 5, pp. 821–833, 2007. View at: Publisher Site  Google Scholar
 C. Tan, J. Yang, and M. Li, “Temporalspatial variation of drought indicated by SPI and SPEI in Ningxia Hui Autonomous Region, China,” Atmosphere, vol. 6, no. 10, pp. 1399–1421, 2015. View at: Publisher Site  Google Scholar
 S. Ghosh and K. Srinivasan, “Analysis of spatiotemporal characteristics and regional frequency of droughts in the southern peninsula of india,” Water Resources Management, vol. 30, pp. 1–20, 2016. View at: Google Scholar
 A. Belayneh, J. Adamowski, and B. Khalil, “Shortterm SPI drought forecasting in the awash river basin in Ethiopia using wavelet transforms and machine learning methods,” Sustainable Water Resour Manag, vol. 2, pp. 87–101, 2016. View at: Publisher Site  Google Scholar
 E. E. Moreira, C. L. Pires, and L. S. Pereira, “SPI drought class predictions driven by the north atlantic oscillation index using loglinear modeling,” Water, vol. 8, no. 43, 2016. View at: Google Scholar
 S. Huang, J. Chang, Q. Huang, and Y. Chen, “Spatiotemporal changes and frequency analysis of drought in the Wei River Basin, China,” Water Resources Management, vol. 28, no. 10, pp. 3095–3110, 2014. View at: Publisher Site  Google Scholar
 M. B. Masud, M. N. Khaliq, and H. S. Wheater, “Analysis of meteorological droughts for the Saskatchewan River Basin using univariate and bivariate approaches,” Journal of Hydrology, vol. 522, pp. 452–466, 2015. View at: Publisher Site  Google Scholar
 M. Yang, D. Yan, Y. Yu, and Z. Yang, “SPEIbased spatiotemporal analysis of drought in Haihe River basin from 1961 to 2010,” Advances in Meteorology, vol. 2016, Article ID 7658015, 10 pages, 2016. View at: Publisher Site  Google Scholar
 M. X. Yu, Q. F. Li, M. J. Hayes, M. D. Svoboda, and R. R. Heim, “Are droughts becoming more frequent or severe in China based on the standardized precipitation evapotranspiration index: 1951–2010?” International Journal of Climatology, vol. 34, no. 3, pp. 545–558, 2014. View at: Publisher Site  Google Scholar
 A. Sklar, Ndimensional distribution functions and their margins, vol. 8, L'Institut de statistique de l'université de Paris, Paris, France, 1959. View at: MathSciNet
 J. T. Shiau, “Fitting drought duration and severity with twodimensional copulas,” Water Resources Management, vol. 20, no. 5, pp. 795–815, 2006. View at: Publisher Site  Google Scholar
 S. Song and V. P. Singh, “Metaelliptical copulas for drought frequency analysis of periodic hydrologic data,” Stoch Environ Res Risk Assess, vol. 24, pp. 425–444, 2010. View at: Publisher Site  Google Scholar
 A. Favre, S. El Adlouni, L. Perreault, N. Thiémonge, and B. Bobée, “Multivariate hydrological frequency analysis using copulas,” Water Resources Research, vol. 40, no. 1, pp. 290–294, 2004. View at: Publisher Site  Google Scholar
 S. Grimaldi and F. Serinaldi, “Asymmetric copula in multivariate flood frequency analysis,” Advances in Water Resources, vol. 29, no. 8, pp. 1155–1167, 2006. View at: Publisher Site  Google Scholar
 A. AghaKouchak, A. Bárdossy, and E. Habib, “Copulabased uncertainty modelling: Application to multisensor precipitation estimates,” Hydrological Processes, vol. 24, no. 15, pp. 2111–2124, 2010. View at: Publisher Site  Google Scholar
 Q. Wang, P. Shi, T. Lei et al., “The alleviating trend of drought in the HuangHuaiHai Plain of China based on the daily SPEI,” International Journal of Climatology, vol. 35, pp. 3760–3769, 2015. View at: Publisher Site  Google Scholar
 J. H. Stagge, L. M. Tallaksen, L. Gudmundsson, A. F. Van Loon, and K. Stahl, “Candidate distributions for climatological drought indices (SPI and SPEI),” International Journal of Climatology, vol. 35, no. 13, pp. 4027–4040, 2015. View at: Publisher Site  Google Scholar
 H. Wang, S. M. Vicenteserrano, F. Tao et al., “Monitoring winter wheat drought threat in Northern China using multiple climatebased drought indices and soil moisture during 2000–2013,” Agricultural and Forest Meteorology, vol. 228229, pp. 1–12, 2016. View at: Publisher Site  Google Scholar
 B. Saghafian and H. Mehdikhani, “Drought characterization using a new copulabased trivariate approach,” Natural Hazards, vol. 72, no. 3, pp. 1391–1407, 2014. View at: Publisher Site  Google Scholar
 S. Madadgar and H. Moradkhani, “A bayesian framework for probabilistic seasonal drought forecasting,” Journal of Hydrometeorology, vol. 14, no. 6, pp. 1685–1705, 2013. View at: Publisher Site  Google Scholar
 Z. Hao, F. Hao, V. P. Singh, A. Y. Sun, and Y. Xia, “Probabilistic prediction of hydrologic drought using a conditional probability approach based on the metagaussian model,” Journal of Hydrology, vol. 542, pp. 772–780, 2016. View at: Publisher Site  Google Scholar
 D. Zhang, L. Zhang, J. Yang, and G. Feng, “The impact of temperature and precipitation variation on drought in china in last 50 years,” Acta Physica Sinica, vol. 59, pp. 655–663, 2010. View at: Google Scholar
 L. Fan, H. Wang, W. Lai, and C. Wang, “Administration of water resources in beijing: problems and countermeasures,” Water Policy, vol. 17, no. article 563, 2015. View at: Publisher Site  Google Scholar
 W. Cai, Y. Zhang, Q. Chen, and Y. Yao, “Spatial patterns and temporal variability of drought in BeijingTianjinHebei metropolitan areas in China,” Advances in Meteorology, vol. 2015, Article ID 289471, 14 pages, 2015. View at: Publisher Site  Google Scholar
 H. Liu, A. Zhang, T. Jiang, H. Lv, X. Liu, and H. Wang, “The spatiotemporal variation of drought in the BeijingTianjinHebei metropolitan region (BTHMR) based on the modified TVDI,” Sustainability, vol. 8, no. article 1327, 2016. View at: Publisher Site  Google Scholar
 Y. Li, W. Gu, W. Cui, Z. Chang, and Y. Xu, “Exploration of copula function use in crop meteorological drought risk analysis: a case study of winter wheat in Beijing, China,” Natural Hazards, vol. 77, no. 2, pp. 1289–1303, 2015. View at: Publisher Site  Google Scholar
 G. Buttafuoco, T. Caloiero, and R. Coscarelli, “Analyses of drought events in calabria (Southern Italy) using standardized precipitation index,” Water Resources Management, vol. 29, no. 2, pp. 557–573, 2015. View at: Publisher Site  Google Scholar
 C. W. Thornthwaite, “An approach toward a rational classification of climate,” Geographical Review, vol. 38, pp. 55–89, 1948. View at: Publisher Site  Google Scholar
 N. E. Huang, Z. Shen, S. R. Long et al., “The empirical mode decomposition and the Hilbert spectrum for nonlinear and nonstationary time series analysis,” Proceedings of the Royal Society A: Mathematical, Physical and Engineering Sciences, vol. 454, pp. 903–995, 1998. View at: Publisher Site  Google Scholar  MathSciNet
 D. Zuo, Z. Xu, H. Yang, and X. Liu, “Spatiotemporal variations and abrupt changes of potential evapotranspiration and its sensitivity to key meteorological variables in the Wei River basin, China,” Hydrological Processes, vol. 26, no. 8, pp. 1149–1160, 2012. View at: Publisher Site  Google Scholar
 J. Zhao, Z.X. Xu, D.P. Zuo, and X.M. Wang, “Temporal variations of reference evapotranspiration and its sensitivity to meteorological factors in Heihe River Basin, China,” Water Science and Engineering, vol. 8, pp. 1–8, 2015. View at: Google Scholar
 S. Moazami, S. Golian, M. R. Kavianpour, and Y. Hong, “Uncertainty analysis of bias from satellite rainfall estimates using copula method,” Atmospheric Research, vol. 137, pp. 145–166, 2014. View at: Publisher Site  Google Scholar
 L. A. Jordanger and D. Tjøstheim, “Model selection of copulas: AIC versus a cross validation copula information criterion,” Statistics and Probability Letters, vol. 92, pp. 249–255, 2014. View at: Publisher Site  Google Scholar
 G. Schwarz, “Estimating the dimension of a model,” The Annals of Statistics, vol. 6, no. 2, pp. 461–464, 1978. View at: Publisher Site  Google Scholar  MathSciNet
 J. T. Shiau and R. Modarres, “Copulabased drought severitydurationfrequency analysis in Iran,” Meteorological Applications, vol. 16, no. 4, pp. 481–489, 2009. View at: Publisher Site  Google Scholar
 F. Yuan, M. Ma, L. Ren et al., “Possible future climate change impacts on the hydrological drought events in the weihe river basin, China,” Advances in Meteorology, vol. 2016, Article ID 2905198, 14 pages, 2016. View at: Publisher Site  Google Scholar
Copyright
Copyright © 2017 Linlin Fan et al. This is an open access article distributed under the Creative Commons Attribution License, which permits unrestricted use, distribution, and reproduction in any medium, provided the original work is properly cited.