the Creative Commons Attribution 4.0 License.

the Creative Commons Attribution 4.0 License.

# High-spatial-resolution probability maps of drought duration and magnitude across Spain

### Fernando Domínguez-Castro

### Sergio M. Vicente-Serrano

### Miquel Tomás-Burguera

### Marina Peña-Gallardo

### Santiago Beguería

### Ahmed El Kenawy

### Yolanda Luna

### Ana Morata

Assessing the probability of occurrence of drought is important for improving current drought assessment, management and mitigation measures, and strategies across Spain. This study employed two well-established drought indices, the Standardized Precipitation Index (SPI) and the Standardized Precipitation Evapotranspiration Index (SPEI), to characterize drought duration and magnitude at different timescales over Spain. In order to map the drought hazard probability, we applied the extreme value theory and tested different thresholds to generate peak-over-threshold (POT) drought duration and magnitude series. Our results demonstrate that the generalized Pareto (GP) distribution performs well in estimating the frequencies of drought magnitude and duration. Specifically, we found a good agreement between the observed and modelled data when using upper percentiles to generate the POT series. Spatially, our estimations suggest a higher probability of extreme drought events in southern and central Spain compared to the northern and eastern regions. Also, our study found spatial differences in drought probability estimations as a function of the selected drought index (i.e. SPI vs. SPEI) and timescale (i.e. 1, 3, 6, and 12 months). Drought hazard probability maps can contribute to the better management of different sectors (e.g. agriculture, water resources management, urban water supply, and tourism) at national, regional, and even local scale in Spain.

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Drought is one of the main hydroclimatic hazards in Spain, with adverse impacts on natural and human environments (Pérez and Barreiro-Hurlé, 2009; UNEP, 2006). Numerous studies have analysed drought characteristics in Spain, suggesting a strong variability over both space and time (e.g. Domínguez-Castro et al., 2019a; González-Hidalgo et al., 2018). In Spain, drought management measures are usually based on insurance and government subsidies to diminish their impacts, particularly those related to the agricultural sector (Fernández, 2006). Alongside the existing systems for monitoring hydrological drought conditions across Spain (Maia and Vicente-Serrano, 2017), there are various pieces of national legislation (e.g. special drought plans) that aim at improving drought adaptation strategies and practices (Garrick et al., 2017).

Although current national measures are quite useful to diminish drought risk, other improved approaches are still desired to reduce drought risk, particularly for real-time drought monitoring (e.g. Svoboda et al., 2002) and forecasting (e.g. Mishra et al., 2009; Mishra and Singh, 2011). In this context, drought probability maps can be a promising tool to characterize drought risk at a detailed spatial scale. In particular, it is possible to determine the probability of drought episodes of a certain severity, allowing for better sectorial management strategies. Due to the availability of dense spatial climate data, there is a possibility to map drought probability at a fine spatial scale. This detailed scale can be useful for different socioeconomic sectors and for natural ecosystems. The utility of probabilistic approaches for enhancing drought monitoring and adaptation was evidenced in many regions worldwide (e.g. Engeland et al., 2005; Hussain et al., 2018; She et al., 2014; Tosunoglu and Can, 2016; Zamani et al., 2015).

In Spain, several studies have developed dry spell probability maps (e.g. Lana et al., 2006; Martin-Vide and Gomez, 1999; Pérez-Sánchez and Senent-Aparicio, 2018). However, given that the probability of occurrence of dry spells is higher in arid regions than in humid regions, these studies did not account for the different drought hazard probabilities across Spain. It is well-recognized that the frequency and duration of dry spells are largely driven by the climatology of the studied area. Accordingly, the spatial variability of climate aridity can show similar spatial patterns to those of dry spell probability. However, drought probability cannot necessarily be related to the spatial patterns of climate aridity, as it can be associated more with the intrinsic characteristics of drought events. This is simply because, irrespective of the climatology, drought can occur in any world region when there is a negative anomaly with respect to the long-term average moisture conditions (Wilhite and Pulwarty, 2017). This highlights the importance of data standardization to make drought characteristics (e.g. duration, intensity, severity) comparable among regions with different climatic conditions. Several drought indices (e.g. Standardized Precipitation Index (SPI), Standardized Precipitation Evapotranspiration Index (SPEI), Palmer Drought Severity Index, Self-calibrated Palmer Drought Severity Index) have been developed to characterize drought conditions across regions with different climatic conditions (Redmond, 2002). Also, irrespective of climatic conditions, these indices can identify drought episodes according to their duration and magnitude (Dracup et al., 1980) Overall, based on these drought indices, the probability of occurrence of drought duration and magnitude can be characterized at a detailed spatial resolution. In their assessment of drought characteristics in Serbia, Tošić and Unkašević (2014) analysed the probability of occurrence of drought using the SPI between 1949 and 2011, concluding that the generalized Pareto (GP) distribution fits well with the series at 1- and 12- month timescales. Similarly, Yusof et al. (2013) analysed the probability of drought duration and magnitude using the SPI and rainfall data from 30 rain gauges distributed across peninsular Malaysia. Also, Zin et al. (2013) assessed the return period of drought severity over peninsular Malaysia by means of the SPI. An inspection of these studies reveals that they employed only an individual drought index in most cases, with few attempts to explore the possible differences in drought hazard probability as a function of different drought indices (e.g. Yan et al., 2018) or different drought timescales (Moradi et al., 2011; Tošić and Unkašević, 2014). Due to the varying response of the different hydrological subsystems, socioeconomic sectors, and natural ecosystems to drought, the impacts of droughts should be assessed at various drought timescales (McKee et al., 1993; Vicente-Serrano, 2013). Moreover, the spatial patterns of drought and hazard probability maps can differ largely in response to timescale (Vicente-Serrano, 2006). Taken together, it is important to assess drought hazard probability at different drought timescales to meet the specific needs of different socioeconomic sectors and natural systems.

The overall objective of this study is to employ a newly developed
high-resolution spatial (1.21 km^{2}) and temporal (weekly) gridded
dataset of drought indices (Vicente-Serrano et al., 2017) to characterize
drought events in Spain. Specifically, this study aims to (i) apply the
extreme value theory to determine the best threshold and statistical
distribution to fit the probability of drought duration and magnitude,
(ii) explore spatial variations in this probability as a function of two common
drought indices, with different underlying calculations (i.e. SPI vs. SPEI),
and (iii) assess whether there are spatial differences in drought hazard
probability in response to the different drought timescales. In Spain, this
detailed spatial assessment is still lacking, limiting the possibility to
provide guidance on the use of drought hazard probability to manage and
mitigate drought risks at the national, regional, and even local scale.

## 2.1 Dataset

Based on gridded datasets of maximum and minimum air temperatures
(1304 observatories), precipitation (2269 observatories), wind speed
(82 observatories), relative humidity (179 observatories), and sunshine duration
(112 observatories), Vicente-Serrano et al. (2017) developed a
high-resolution spatial (1.21 km^{2}) and temporal (weekly) drought
dataset for Spain (412 178 pixels). This dataset spans the period from 1961
to 2014. This drought dataset was developed after a rigorous procedure to
check the quality and homogeneity of the input climatic data. The grid of
each variable was computed by a universal kriging method (Borrough and
McDonnell, 1998; Pebesma, 2004) using the latitude, longitude, and elevation
of each grid cell as auxiliary variables. The grid layers were validated
with a jackknife resampling procedure (Phillips et al., 1992), indicating
low differences between the predicted and the observed values for each grid.
A detailed description of this dataset can be found in Vicente-Serrano et
al. (2017). Overall, these gridded climatic data were employed to compute
the SPI (McKee et al.,
1993) and the SPEI
(Vicente-Serrano et al., 2010) at different timescales ranging from 1 to 48
months
(http://monitordesequia.csic.es, last access: 6 March 2019). While the SPI accounts only for
precipitation data, the SPEI is based on a normalization of the difference
between precipitation and atmospheric evaporative demand (AED). In this
study, we employed these two drought indices to characterize the possible
impacts of the AED on drought hazard probability. Drought characteristics
were assessed for the period 1961–2014 using the SPI and SPEI at timescales
of 1, 3, 6, and 12 months.

## 2.2 Selection of drought events

There are several criteria (thresholds) to identify independent drought events (e.g. Fleig et al., 2006; Lee et al., 1986). These thresholds are generally arbitrary, with no clear objective metrics to relate a certain value of a drought index with specific sectorial impacts. Indeed, this is a challenging task, given the large number of economic sectors and environmental systems impacted by droughts (Pérez and Barreiro-Hurlé, 2009). Furthermore, regions and sectors can respond differently to various drought timescales (Lorenzo-Lacruz et al., 2013; Pasho et al., 2012). In this work, we obtained series of drought events from weekly gridded series of SPEI and SPI at four selected timescales (1, 3, 6, and 12 months). We used a zero threshold to define drought events. Although this threshold allows for the inclusion of less severe drought events, it can secure a sufficient sampling size to conduct the probabilistic analysis. Importantly, the retention of drought events in this manner will not bias the obtained results, considering that high values of the series will be retained following the peak-over-threshold approach.

Overall, each drought event was defined as the period of consecutive weeks with SPI or SPEI values lower than zero. Likewise, the series of drought duration and magnitude were created based on the consecutive weeks of SPEI–SPI values below zero. The drought magnitude was calculated following the classical approach of Dracup et al. (1980). However, for operational purposes, the total magnitude of drought was transformed to positive values.

## 2.3 Probabilistic analysis

The peak-over-threshold (POT) series were obtained using series of
drought duration and magnitude calculated at 1-, 3-, 6-, and 12-month
timescales. These series are stationary and do not show any trend
(Domínguez-Castro et al., 2019a), which is a
prerequisite for the application of extreme value theory. The POT series
were obtained according to a threshold (*x*_{0}) as

In order to assess the role of the selected threshold in fitting the probability distribution of the series, we tested different thresholds defined according to the percentiles of the series (i.e. 0th, 10th, 20th, …, 90th, and 95th). Following this procedure, we selected the optimal percentile threshold to define the exceedance series of drought duration and magnitude for the different indices and timescales.

Numerous studies employed the GP distribution to model meteorological and hydrological droughts (e.g. Fleig et al., 2006; Nadarajah, 2008; Nadarajah and Kotz, 2008; Chen et al., 2011; Yusof et al., 2013; Tošić and Unkašević, 2014; Trenberth et al., 2014; Zamani et al., 2015; Liu et al., 2016). This is mainly because the probability distribution of a POT series, with random occurrence times, fits well with GP distribution (e.g. Hosking and Wallis, 1987; Pham et al., 2014; Wang, 1991). The GP distribution is a flexible, long-tailed distribution, whose distribution function is formulated as

where *κ*, *α*, and *ε* are the shape, scale, and
location parameters of the distribution origin that correspond to the lower
bound *x*_{0}. The GP parameters were obtained using
L-moment statistics following Hosking (1990).

Hosking (1990) proposed a procedure to provide parametric
approximations to the relationships between L skewness and L kurtosis. This
procedure allows for the determination of the suitability of the GP distribution to
fit the exceedance obtained from different *x*_{0} values. Herein, we plotted the
different L-moment diagrams with the statistics obtained from drought
duration and magnitude series. The aim was to assess the suitability of the
different *x*_{0} thresholds to obtain POT series with a good fit to the GP distribution.

We applied the Anderson–Darling test to check the goodness of fit of the
POT series obtained from different x0 thresholds. To define the most
suitable threshold, we paid attention to securing a sample of sufficient
length to obtain solutions for the GP parameters. This is important to
obtain reliable probability estimations. For this purpose, we compared the
observed maximum drought duration and magnitude obtained for the whole study
period (1961–2014) with those estimated using GP distribution and POT for
the different thresholds. Then, we calculated the probability that an event
of magnitude *X*_{T} in a period of *T*=54 years (expressed in the
original scale) will occur at least once in a period of *T* years. This is formulated as

where *λ* is a frequency parameter equalling the average number of
occurrences of *X* per year in the original sample. The performance of each
threshold was assessed using different accuracy statistics, including the
mean absolute error (MAE), the Willmott *D* agreement index
(Willmott, 1981), and the Pearson's *r* correlation
coefficient. Comparisons were made for the observed maximum drought
duration and magnitude and the GP estimations for the same sample length.

Once a general threshold was established to define the POT series of drought duration and magnitude, we determined the goodness of the GP modelling for each drought index and timescale. For this purpose, we used probability–probability (P–P) plots, which define the extent to which the empirical and modelled GP cumulative distribution functions (CDFs) closely match. This procedure was applied to a total of 412 178 gridded series of drought magnitude and duration covering the four selected timescales of the SPI and SPEI. The empirical CDFs were obtained using the plotting position formula proposed by Hosking (1990) for highly skewed data, according to

where *i* is the rank of the observations arranged in descending order, and
*N* is the number of observations. The goodness of agreement between the
empirical and modelled CDFs was tested using a weighted correlation
coefficient. This procedure gives more weight to the highest and less
frequent observations in the sample, which are more relevant to extreme
value analysis. The weight was defined using the empirical CDF as

where CDF is the cumulative distribution function, and *j* refers to the
observations in the series of exceedance sorted in ascending order.

## 3.1 Selection of the distribution and threshold to define the POT series

Figure 1 illustrates some examples of L-moment diagrams, considering the
1-month SPEI duration series over peninsular Spain. The series for each
diagram were obtained considering POT at different percentiles. Each line
represents a theoretical curve distribution: the generalized logistic (GLO,
blue), generalized extreme value (GEV, green), generalized Pareto (GPA,
red), generalized normal (GNO, black), and Pearson type III (PE3, light
blue). As noted, irrespective of the selected threshold, the drought
duration series tend to closely approximate to the GP distribution. Notably,
there is a higher dispersion of points around the theoretical curve at
higher percentiles, which can simply be seen in the context of lower
sampling size. Figure 2 depicts the L-moment diagrams corresponding to the
12-month SPEI magnitude series. The plots show high dispersion considering
the different percentile thresholds. Nevertheless, at low percentiles, the
points do not approximate to the theoretical curve of the GP distribution,
but they conversely tend to approximate to the GP curve at percentiles
between 60th and 80th. Again, the points exhibited high dispersion at upper
percentiles (mostly above the 85th). An inspection of Figs. S1 to S14
in the Supplement suggests similar patterns for other timescales and for the drought
duration and magnitude series obtained using the SPI. Table 1 summarizes the
percentage of the POT series that fit well with the GP distribution
following Anderson–Darling statistics. As listed, the series of drought
magnitude show a better fit to GP distribution than those of drought duration,
but with no considerable differences between SPI and SPEI. In contrast, we
noted remarkable differences amongst the different timescales. For example,
we noted that a high percentage of the series obtained for low percentiles
did not fit well to the GP distribution. In contrast, for all drought
duration and magnitude series, this fitting improved markedly when
considering higher percentiles (mostly above the 40th percentile). The only
exceptions were found for the duration series obtained at a 1-month timescale, but considering thresholds higher than the
80th percentile either for SPI
or SPEI. The total percentage of these series is close to 100 %.
Overall, although the results suggest that high percentiles (e.g. 90th or 95th)
were more appropriate to define the series of drought duration and
magnitude, our decision was to define the series using a more relaxed
threshold (80th percentile). This decision was motivated mainly by the
notion that L-moment statistics showed high dispersion at the uppermost
percentiles. Furthermore, it was quite difficult to secure a sufficient sampling
size using these upper percentiles. Figure 3 shows the number of drought
events corresponding to the different percentiles and timescales (i.e. 1,
3, 6, and 12 months). It can be noted that the number of events using the
90th and 95th percentile thresholds was very low for all timescales. This
low number of events was statistically insufficient for the reliable estimation
of L-moment and GP parameters (Table 2). Accordingly, we considered lower
percentiles to get more reliable probabilistic estimations. In this context,
our results indicated that the series of drought duration and magnitude
obtained using the 80th percentile as a threshold mostly fit to the
GP distribution, and the majority of these series (≈99 %) showed
solutions for GP parameters. Figure 4 depicts the accuracy metrics
(i.e. Willmott's *D*, MAE, and Pearson's *r* coefficient), which compare the maximum
observed and modelled drought duration and magnitude for each grid. It can
be noted that the agreement between the maximum observed and modelled values
is higher for drought magnitude series than for drought duration series.
However, for drought magnitude and duration series, this agreement improved
when considering higher percentiles, especially the 80th percentile. These
findings were clearly evident for the SPI and SPEI and for all timescales.

Also, we compared the empirical and modelled cumulative distribution
functions using the GP distribution considering the 80th percentile
POT series. Comparisons were made at the pixel scale considering the
two drought indices (SPI vs. SPEI) and the different timescales. A
representative example is shown in Fig. 5 for the grid point located at
40^{∘} N and 3^{∘} W. As illustrated, we noted a
high agreement between the empirical and modelled CDFs, irrespective of the
drought index and the timescale. However, a lower agreement was observed for
longer timescales (i.e. 6 and 12 months). This can be expected given the low
sampling size at long timescales in comparison to shorter timescales.
Overall, the weighted correlations between the empirical and the modelled
CDFs showed high values (>0.98) in all cases, which was
reflected in the general observed pattern for the whole of Spain. Figure 6
depicts the spatial distribution of the weighted correlations between the
empirical and the GP-distribution-modelled CDFs using the 80th percentile
POT series. At the 1- and 3-month timescales, the correlations were
close to 1 for all of Spain. The magnitude of correlation decreased for
the 6- and 12-month timescales, despite being above 0.97 in most areas.
Overall, these findings support our decision to select the 80th percentile
and the GP distribution to statistically model drought duration and
magnitude in our study domain.

## 3.2 Mapping drought duration and magnitude

Figures 7 and 8 illustrate the spatial distribution of GP parameters
calculated for drought duration series obtained using the SPI and SPEI,
respectively. The GP parameters showed very similar distributions for SPI
and SPEI. However, we found considerable spatial variations in the
distribution of these parameters as a function of the drought timescale,
with higher values of the location (*X*_{o}) and scale (*α*) parameters for
longer timescales. This can be explained by the increase in drought
duration at longer timescales. The shape (*k*) parameter exhibited similar
range values for all timescales. Herein, it is difficult to interpret the
geographical distribution of the shape (*k*), as there is large uncertainty in
estimating this parameter (Rosbjerg et al., 1992). As illustrated in
Figs. S15 and S16, all parameters showed similar spatial patterns for the drought magnitude series.

We mapped drought probability for the drought duration and magnitude series using parameter maps and Eq. (3). Figure 9 shows the estimated drought duration (in weeks) obtained from the 1-, 3-, 6-, and 12-month SPEI series for periods of 50 and 100 years. The results suggest important spatial differences among drought timescales. For example, at the 1-month timescale, the maximum duration was found in the central areas of Spain, with more than 40 weeks of consecutive negative SPEI values. A similar pattern can also be noted for the 3-month timescale, as central and southern Spain experience a longer duration. In northern Spain, the estimated maximum drought duration is almost half that in central Spain. Nevertheless, the spatial patterns of drought probability differ markedly at the timescales of 6 and 12 months, with the maximum duration recorded in south-eastern and south-western regions and parts of northern and north-eastern Spain. The spatial patterns found at the 12-month timescale closely resemble those observed at the 6-month timescale, suggesting a maximum drought duration (>180 weeks) in a period of 50 years over some regions in the south-west and along the eastern Mediterranean coast. On the other hand, considering the maximum drought duration for a period of 100 years, drought events are expected to extend spatially, especially in southern Spain. Figure 10 reveals that drought probability maps obtained using SPI are similar to those obtained using SPEI, although with some spatial differences that can mainly be linked to drought timescale. Figure 11 summarizes the relationship between the maximum drought duration of SPEI and SPI, considering 1-, 3-, 6-, and 12-month timescales and periods of 50 and 100 years. For drought duration, the agreement between SPI and SPEI is stronger considering long timescales. For timescales between 1 and 6 months, the SPEI tends to record higher quantile estimates than SPI. Nevertheless, at the 12-month timescale, the differences in the quantile estimates between the two indices are clearly minimized. For drought magnitude, the quantile estimates show more consistent spatial patterns for the two indices compared to those identified for drought duration series (Figs. S17 to S19).

We developed high-resolution drought probability maps for Spain using two widely recognized drought indices that are spatially and temporally comparable: the Standardized Precipitation Index (SPI) and the Standardized Precipitation Evapotranspiration Index (SPEI). Although they have similar conceptual backgrounds, these indices differ in their input variables. Specifically, while the SPI accounts only for precipitation data (McKee et al., 1993), the SPEI considers the atmospheric evaporative demand (AED) in its calculation (Vicente-Serrano et al., 2010). In this study, we computed these two drought indices at different timescales (1, 3, 6, and 12 months). The aim was to assess whether there are noticeable spatial differences in the obtained drought hazard probabilities as a function of the selected index and/or timescale.

We assessed the suitability of the GP distribution to model drought duration and magnitude events. The results demonstrate that drought magnitude and duration series mostly fit well with a GP distribution, a finding that was confirmed in earlier drought assessment investigations in many regions worldwide (e.g. Chen et al., 2011; Serra et al., 2016; Vicente-Serrano and Beguería-Portugués, 2003; Zamani et al., 2015). In this study, our decision to select the GP distribution was motivated by the need to achieve a balance between the goodness of the fit to the GP distribution on the one hand and the selection of a representative threshold to obtain the POT series on the other hand. Our exploratory analysis suggests the use of the 80th percentile as a threshold. This threshold is a good balance between the two requirements for the SPI and SPEI and for all timescales.

In earlier hydrologic and climatic hazards investigations, a regionalization approach has been employed to estimate the probability distribution, L-moment statistics, and distribution parameters (e.g. Durrans and Tomic, 1996; Serra et al., 2016; She et al., 2014). As opposed to these studies, our preference was given to analyse hazard probability locally. Specifically, to calculate the L-moment statistics and the distribution parameters, we considered each gridded cell as an independent series. While regionalization is advantageous in terms of spatial homogeneity and the reduction of parameter uncertainty (Hosking and Wallis, 1997), characterization of drought conditions in our study domain reveals noticeable spatial differences in response to drought timescale. This is clearly evident for probabilities of both drought duration and magnitude. Regionalization is usually based on the variables used for calculating drought indices (i.e. precipitation or the difference between precipitation and atmospheric evaporative demand) (Ghosh and Srinivasan, 2016; Habibi et al., 2018; Santos et al., 2011; Yuan et al., 2013; Zhang et al., 2015). Importantly, this study stresses that this kind of regionalization might not be useful when drought hazard differs strongly due to drought timescale. Previous studies indicated that the spatial patterns of drought may differ strongly as a function of drought timescale, especially with different temporal influences of local–regional precipitation events on drought index values (e.g. Vicente-Serrano, 2006). This is confirmed in our study for the whole of Spain, where the spatial patterns of the GP parameters and the maps of hazard probability strongly vary due to the different drought timescale. Again, this stresses the difficulty of applying regionalization approaches to obtain maps of drought probability. This difficulty is confirmed in this study, as our findings reveal differences in drought probability as a consequence of the selected drought index, which makes this kind of regionalization a challenging task. A possible solution could be establishing different regionalization schemes based on the different series of drought indices and timescales. However, this is practically disadvantageous, as it makes the use of probability estimations by end users more confusing (e.g. stakeholders, decision makers, and local communities). Also, with the spatial coherence and the observed gradients of GP parameters, a direct calculation of hazard probabilities at the local scale is highly recommended, particularly in regions with strong spatial and temporal climatic variability like Spain. Overall, taking all these limitations into consideration, this study stresses that employing regionalization approaches to determine drought hazard probabilities should be done with caution, especially when different drought indices and timescales are used.

Assessing the different spatial patterns of drought probabilities as a function of timescales has strong implications for drought impact assessment and drought mitigation. It is well-established that different hydrological, agricultural, and environmental systems respond differently to drought timescales (Pasho et al., 2012; Peña-Gallardo et al., 2018; Vicente-Serrano, 2013). As such, for more effective assessment and monitoring of drought hazard, drought timescales must be linked to specific drought impacts. This is basically because although drought probability can differ in response to drought timescale, the impacts of drought hazard may vary considerably from one region to another due to different environmental and socioeconomic factors. Correspondingly, the degree of vulnerability can differ according to drought timescale and region. For example, although with the high probability of occurrence of an extreme drought event at a certain timescale in a particular region, drought risk may be small if the sensitivity to drought timescale is low. This confirms that it is essential to obtain drought hazard probability maps at different timescales. Practically, the real hazard would be definitely derived from a drought timescale that triggers impacts in a given space and sector.

Recently, there has been a great debate on the influence of climate change processes on drought severity (Dai, 2013; Sheffield et al., 2012; Trenberth et al., 2014). This debate is largely motivated by the role of warming processes and the atmospheric evaporative demand in drought severity. Numerous studies have shown a noticeable increase in the AED across the Mediterranean region, which could enhance the severity of drought events in comparison to events driven mainly by precipitation deficit (Stagge et al., 2017; Vicente-Serrano et al., 2014). Here, we indicated that, mainly at timescales from 1 to 6 months, SPEI duration and magnitude values are higher than those of the SPI. This finding suggests that the increased AED due to warming processes may have a certain role in increasing drought duration and magnitude hazard probabilities in Spain. When a drought event occurs as a consequence of a precipitation deficit, high values of the AED can increase the magnitude and duration of drought events. However, this pattern was not observed for long drought timescales (i.e. 12 months), which showed small differences between the SPI and SPEI drought duration and magnitude quantile maps. This could be explained by the strong seasonality that characterizes the climate of Spain. This can be seen for the 12-month timescale, which summarizes the annual climate conditions. As indicated by Vicente-Serrano et al. (2014), the role of increased AED (mostly recorded during summer months) would be diminished in comparison to the role of precipitation. In contrast, the role of the AED would be more highlighted at shorter timescales that record stronger seasonal variability.

Assessing drought hazard probability by means of joint probabilities of drought duration and magnitude has been applied in more depth through the use of copulas (e.g. Ganguli and Reddy, 2012; Liu et al., 2011; Zhang et al., 2015). Nevertheless, given the nature of drought indices, the time series exhibit strong temporal autocorrelation, and accordingly the duration and magnitude of particular drought events can show high agreement. Here, we found a strong correlation between the magnitude and the duration of drought events for the selected drought indices and timescales. This indicates that – as expected – the total magnitude of an event is proportional to drought duration. Therefore, although copulas could give some additional information for particular events, we still believe that an accurate evaluation of drought hazard probability in Spain using a univariate approach is more advantageous.

Recalling the strong spatial differences in the drought hazard probability over Spain, the maps obtained in this study can contribute to better management practices for different sectors, including agriculture, water resources management, urban water supply, tourism, and environmental management. The spatial quantile probabilities developed in this study, combined with those estimated for 50 and 100 years, are fully accessible to the research community and end users via the web repository of the Spanish National Research Council (CSIC) (Domínguez-Castro et al., 2019b).

The Generalized Pareto parameters and drought risk maps developed in this study are accessible at http://digital.csic.es/handle/10261/178150 (Domínguez-Castro et al., 2019b).

The supplement related to this article is available online at: https://doi.org/10.5194/nhess-19-611-2019-supplement.

All the authors contributed equally to the paper.

The authors declare that they have no conflict of interest.

This article is part of the special issue “Hydroclimatic extremes and impacts at catchment to regional scales”. It is not associated with a conference.

This work was supported by the following research projects: CGL2014-52135-C03-01
and PCIN-2015-220 financed by the Spanish Commission of Science and Technology
and FEDER, 1560/2015; Herramientas de monitorización de la
vegetación mediante modelización ecohidrológica en parques
continentales financed by the Red de Parques Nacionales; IMDROFLOOD financed
by Water Works 2014; a co-funded call of the European Commission and
INDECIS, which is part of ERA4CS; and an ERA-NET initiated by JPI Climate,
funded by MINECO with co-funding by the European Union (grant 690462).
Marina Peña-Gallardo was funded by the Spanish Ministry of Economy and
Competitiveness, Miquel Tomas-Burguera was supported by a doctoral grant by
the Spanish Ministry of Education, Culture and Sport, and Ahmed El Kenawy was
supported by a postdoctoral Juan de la Cierva contract.

Edited by: Chris Reason

Reviewed by: two anonymous referees

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