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Dry and Wet Events in Andean Populations of Northern Peru: A Case Study of Chachapoyas, Peru

Climate change and population growth have heavily impacted the ecosystem’s water resources, essential for anthropogenic activities. These also apply to the Andean city of Chachapoyas, located in the north of Peru, which has gone through a substantial population increase in recent years, therefore increasing its water demand. This research aimed to assess dry and wet events from 1981 to 2019 that have taken place in Chachapoyas, by applying the Standardized Precipitation Index (SPI), and the Standardized Precipitation Evapotranspiration Index (SPEI). These events were periodically characterized, and the index relationship was determined at different timescales. The SPI and SPEI indices were calculated at the city’s only weather station for timescales of 3, 6, 12, and 24 months using climatic data. The indices showed a remarkably consistent behavior for timescales of 12 and 24 months detecting an extreme drought event in 1993, while for timescales of 3 and 6 months a severe drought event was detected in the same year. Contrastingly, there has been an increase in extreme wet events in the last decade, hence Chachapoyas is categorized between "moderate drought" and “moderate wet”. It should be noted that the indices have a high correlation between them when calculated for the same timescale. The results were statistically significant (p < 0.05). Considering the results obtained related to dry and wet events and their relation with economic activities such as environmental management, we can conclude that the SPI and SPEI indices are useful and valuable tools for local and regional governments.


INTRODUCTION
Climate change, a potentially destructive event with catastrophic consequences for humanity and ecosystems (Lin and Chan, 2015), affects precipitation, temperature, humidity, and winds. Thus, strongly impacting agriculture, agricultural communities, food sovereignty, and the sustainability of the world's population at risk, especially in developing countries (Nicholls and Altieri, 2019). Several studies carried out in Latin America, demonstrate that crop yields will significantly decrease, hence severely affecting the availability of food (Jones and Thornton, 2003;Jat et al., 2016;Altieri and Nicholls, 2017;Sá et al., 2017).
Rainfall variability in dry and wet events is entirely subjective depending on where in the world they happen. (Van Loon and Laaha, 2015). For example, extreme droughts in sub-Saharan countries are not the same as in the tropical Andes. Nevertheless, droughts are defined as natural weather events, where there is a significant precipitation deficit over a relatively long period of time (Cerón et al., 2015). The prediction of these events is complex as they depend on the study area (Sánchez-Montoya et al., 2018). Furthermore, these events are usually poorly characterized, due to the difficulty of quantifying their severity, magnitude, and extent (Quintana-Seguí et al., 2016).
Droughts can be classified into four categories: meteorological, agricultural, hydrological, and socioeconomic. Meteorological drought is a consequence of a rainfall deficit. Agricultural drought implies low soil moisture that causes a decline in crop growth and production. Hydrological drought refers to low levels of surface and groundwater. Socioeconomic drought is associated with the supply and demand of water needed for economic good and is affected by the combination with some of the other droughts (Wilhite and Glantz, 1985;Dai, 2011;Van Loon and Laaha, 2015;Zarei, 2019). However, meteorological drought can be considered the leading cause of a drought. In contrast, other droughts represent the impacts generated by a prolonged deficit of precipitation in certain compartments, such as soil moisture, surface water levels, or economic sectors (Stojanovic et al., 2017). Meteorological droughts are defined as intervals of time during which a specific area's humidity consistently drops below what is climatologically expected . Droughts are characterized by indices, which are indirect indicators that rely on meteorological information to quantify these phenomena and assess their effects (Hao et al., 2016). In recent decades, several indices have been developed for drought characterization . The most superficial indices use only precipitation data, while the most complex use parameters such as temperature, evapotranspiration or loss of soil humidity, etc. (Liu et al., 2018). The most recognized indices are the Standardized Precipitation Index (SPI), the Palmer Drought Severity Index (PDSI), the Standardized Precipitation Evapotranspiration Index (SPEI), the Crop Moisture Index (CMI), the Rainfall Anomaly Index (RAI), and the Effective Drought Index (EDI) (Bohn et al., 2007;Ahmad et al., 2016;Aybar-Camacho et al., 2017;Balbo et al., 2019). The most used indices are SPI and SPEI due to their lower complexity (Anshuka et al., 2019), however, they exhibit advantages and disadvantages for their application in the characterization of dry and wet events (Hayes et al., 1996;Tsakiris and Vangelis, 2004;Zhang Y. et al., 2017). Among their advantages are straightforward calculations, and the ability to identify different types of dry or wet events by having multiscale criteria. Being the scales of 1, 3, and 6 months relevant for agricultural drought impacts; the 12 months scale is especially relevant for hydrological drought impacts; the 24 months scale is relevant for socioeconomic drought impacts (Tan et al., 2015). Conversely, their major disadvantage is the tendency to underestimate or overestimate dry and wet events when applied to shorter timescales (Anshuka et al., 2019).
Droughts in South America are of particular interest due to their effects on agriculture, livestock, soil degradation, water management, economy, and society. The study of dry events in this area, whether by evaluating the variables implicated or by applying indices, has been carried out to find out their relationship with the El Niño phenomenon (Espinoza et al., 2011;Sobral et al., 2019;Mohammadi et al., 2020), their connection with climate change (Vicente-Serrano et al., 2015) or their effect on vegetation (Feldpausch et al., 2016).
The city of Chachapoyas is located in the northern Andes of Peru. It is an area of great importance, not only because it is the Amazonas region's capital, but because it is a city that economically depends on livestock and agriculture. The effects of dry and wet events have been thoroughly studied in central and south Ecuador, a predominately Andean region. Studies in this area have concluded that Quito is a good indicator of drought in this region. It was also found that climate change will affect the drought's characteristics, such as magnitude and duration, with a drastic decrease in future scenarios in this area (Domínguez-Castro et al., 2017;Zhiña et al., 2019). However, there are very few studies that report reliable data from remote areas of the Peruvian Andes. In Peru's Central Andes, it has been found that there is a 2% decrease in rainfall per decade. Meanwhile, in the southern Andes of Peru, the most intense droughts between 1981 and 2016 occurred during the El Niño events of that period. It is worth mentioning the elaboration of a precipitation danger map for the Peruvian Andes in terms of the intensity and duration of droughts, being entirely satisfactory considering that it is based on a low-density meteorological network (Silva et al., 2008;Domínguez-Castro et al., 2018;Imfeld et al., 2019).
Most of the antecedents mentioned earlier are at medium or large scale, without having a regional scale. Therefore, it is necessary to study dry and wet events at a local scale, especially in an Andean city in northern Peru, to increase and improve water resources management knowledge. Therefore, the dry and wet events that occurred from 1981 to 2019 in the city of Chachapoyas are analyzed. At the same time, the main climatological parameters were analyzed descriptively. In addition, the SPI and SPEI indices were applied and compared, to identify temporarily dry and wet events. Finally, the relation of the indices throughout different time scales was analyzed. All this will help to have a better understanding of water availability in the area.

Study Area
The city of Chachapoyas is located in the northern Peruvian Andes (Figure 1), at 2,338 m.a.s.l. with an average annual precipitation of about 800 mm and an average temperature of 15.6°C. The annual temperature oscillation is very low, with 1°C on average monthly temperatures. The lowest minimum monthly temperature values are reported between June and August ( Figure 2A), while the highest maximum monthly temperature values happen from August to December ( Figure 2B). As in other Andean regions, rainfall is seasonal, with a wet season from October to March, and a dry season from April to September ( Figure 2C) (Rascón et al., 2020). In respect to the water resources of the city of Chachapoyas, they are in the form of rainwater and surface water. Within the superficial waters, emphasizing the Tialacancha River, that supplies potable water to the city, and lops Santa Lucia, Villohuayco, and Jatunsacha streams, which serve to supply to the cattle ranch and agriculture of the zone (Chávez Ortiz et al., 2016;Salas et al., 2018). Although, as in most Andean cities, very few climate studies are available due to the absence of reliable weather station networks. Chachapoyas possesses only one meteorological station (LAT -6.2083, LONG -77.8671, ELEV 2442, which belongs to the meteorological stations's network of the National Meteorology and Hydrology Service of Peru (SENAMHI). However, this station presents substantial gaps in its data, especially in past readings. That is why the PISCO (Peruvian Interpolated data of the SENAMHI'S Climatological and hydrological Observation) data grid was used.

Weather Data
Climatological data was obtained from the National Meteorological and Hydrological Service of Peru (SENAMHI), specifically, from the spatial database for monthly precipitation at a grid resolution of 0.05°for a series starting in January 1981 to the present, called PISCO, both for monthly precipitation, minimum and maximum monthly temperature. This grid was created using terrestrial observations from the SENAMHI meteorological stations' network, together with data from the global base of the CHIRPS project (Climate Hazards InfraRed Precipitation with Station data) (Aybar et al., 2019).
The generation of the PISCO climate data grid encountered several limitations, such as the low-density of stations in areas with complex geography, the low quality of the station data, and the biases inherent in satellite data. Therefore, PISCO was generated based on the integration of CHIRP data, serially complete gauge datasets, radar-based climatologies, and geostatistical and deterministic interpolation methods (Aybar et al., 2019). For the quality control of the grid, automatic control was applied, evaluating the data of each station, the god ranges, the temporal and spatial coherence. In this way, they eliminated outliers in the data that exceeded the established limits. Later, through data visualization they inspected the breaks evident in the time series and eliminated the non-homogeneous segments, filling in the gaps by using the modified CUTOFF algorithm and quantum maps. As a result, there is a high correlation between the grid data and the stations (0.75-0.99), with the higher the correlation, when there is a station closer (Aybar-Camacho et al., 2017). PISCO data are available free of charge on the following website: http://iridl.ldeo.columbia.edu/ SOURCES/.SENAMHI/.HSR/.PISCO/. Therefore, they were processed with the statistical software R version 3.6.3, Frontiers in Environmental Science | www.frontiersin.org March 2021 | Volume 9 | Article 614438 through the "raster" and "ncdf4" libraries (Pierce, 2019;Hijmans, 2020;R Core Team, 2020). Monthly data from the Chachapoya's weather station were obtained for the 1981-2019 period for precipitation, minimum and maximum temperatures.

Drought Indices
Drought indices were developed to provide a quantitative assessment of the characteristics of each drought event. The most simple indices solely use average rainfall data, while other more sophisticated indices use other parameters such as temperature, evapotranspiration, loss of soil moisture, and prior soil moisture (Zhang et al., 2019).
The SPI, developed by Mckee et al. (1993) quantifies precipitation deficit to evaluate droughts. This method is highly recommended by the World Meteorological Organization (WMO) for drought characterization (Kostopoulou et al., 2017). SPI is calculated by adjusting a gamma probability distribution to a standardized normal distribution (with a mean equal to zero and variance equal to one), thus calculating the final SPI value (Mineo et al., 2019). It was determined that the gamma distribution was the distribution that best fitted the precipitation data, because of its good adjustment. This distribution provides good models to describe precipitation events, and besides, it has been frequently used in previous investigations carried out in Andean zones (González and Dominguez, 2012;González, 2015;Zambrano et al., 2017;Endara et al., 2019;Cerón et al., 2020). First, the SPI adjusts the gamma probability density function (PDF) of the precipitation record for each weather station. Then, the adjusted values are transformed to the normal PDF, which represents the SPI value. For periods of time greater than 1 month, the initial basic procedure for SPI estimation is to use moving sums. By having a long and reliable series (30 years or more) it is possible to calculate the SPI for any previously registered month (i months). The SPI enables researchers to determine the rareness of a drought or an anomalous wet event at a particular timescale for any place in the world. It is important to mention that, for this study, the SPI was carried out for timescales of 3, 6, 12, and 24 months.
In contrast to the SPI, which solely uses precipitation data; the SPEI, developed by Vicente-Serrano et al. (2010), is a new and more comprehensive multiscale index. This index integrates precipitation data, temperature data, and variables like evapotranspiration. It is noted that several formulae, such as the Thornthwaite, Hargreaves, and Penman-Monteith equations are utilized to determine evapotranspiration values in order to calculate SPEI (Stagge et al., 2014). Furthermore, tools that provide objective and quantitative assessments of drought severity can be developed from the aforementioned indices (Vicente-Serrano et al., 2012). Hence, generating a valid and accurate database that enables constant monitoring of event conditions through early warnings (Avilés et al., 2015). From these, adaptation and mitigation strategies can be formulated or implemented in order to alleviate the impacts of these hazards (Cortez et al., 2018). The calculation procedure is similar to that of the SPI; however, the SPEI uses the differences between monthly precipitation and evapotranspiration values, which represents a simple climate water balance. This difference is then adjusted to a logistic distribution, which is then transformed to a standard normal distribution with a zero mean and one variance (Vicente-Serrano et al., 2010).
It should be emphasized that for their estimation, SPI and SPEI when using distributions adjusted to a normal distribution, will make the mean value of SPI and SPEI close to zero (Mckee et al., 1993;Vicente-Serrano et al., 2010).
The SPI and SPEI indices use the same classification for drought or humidity events. This classification divides the events into different categories, determined by index values ( Table 1). To determine the occurrence of dry and wet events, a threshold was established between 1 and −1. These thresholds are those recommended by the WMO guidelines for SPI droughts (Zargar et al., 2011;World Meteorological Organization, 2012). They also correspond to a probability of occurrence of 0.159 (Agnew, 2000).

Data Analysis
Firstly, a descriptive variable analysis was made from box plots, followed by a graphical comparison of indices for each timescale. Hence, defining the intensity, duration, and timescales of the most important dry and wet events. Subsequently, SPI and SPEI values were obtained through the use of the R software (version 3.6.3), the "SPEI" package for equivalent timescale (3, 6, 12, and 24 months), using precipitation data, minimum and maximum temperature, and the station's latitude (Beguería and Vicente-Serrano, 2017;R Core Team, 2020). Although the best method for calculating evapotranspiration is the Penman-Monteith, there are several limitations to it due to the difficulty of obtaining meteorological parameters such as air humidity, wind speed, radiation, and atmospheric pressure. For this reason, the method proposed by Hargreaves (1994) was selected. In addition, some studies show a great correlation between the Penman-Monteith method and the Hargreaves method .
Then, with SPI and SPEI values in different scales, the temporal analysis was made to know the evolution of the dry and wet events. For this, moderate, severe, and extreme dry and wet events were identified, comparing the index values with the classification determined in Table 1. On the other hand, using the indices as indicators, a drought or wet event for a time scale i, is defined as the period during which the index reaches values below -1 (drought) or above 1 (wet), ending when it reaches values between −1 and 1. With this, the duration and approximate timescale of such events is determined, being the intensity the value given by the indices. Simultaneously, using data previously obtained through descriptive statistics (average, maximum, minimum SPI and SPEI values at different scales, as well as their standard deviation), a temporal analysis was carried out in order to assess the behavior of the dry and wet events. Finally, because the higher timescales of the indices did not comply with the Smirnov-Kolmogorov assumption of normality (Wei and Simko, 2017; R Core Team, 2020), the Spearman rank-order correlation coefficient (p < 0.05) was calculated using the R software (version 3.6.3) with the "corrplot" package, to measure the level of correlation and direction that exists between the SPI and SPEI indices across timescales. Figure 3 shows that the highest average monthly precipitation data were collected from 1990 to 1999, followed by a decrease in 2000-2009, however recuperating in the current decade. Nevertheless, in the period 2010-2019, there was a drop in these temperatures. The climate water balance remained more or less constant during the first three decades, while in the last decade there were the conditions of lower deficit of the period

SPI and SPEI Indices
SPI and SPEI results for the city of Chachapoyas were calculated for the time scales of 3, 6, 12, and 24 months. On a three month scale, the series shows high frequency oscillation (Figure 4), due to the short time in which the variables are taken into account, thus changes are assimilated at great speed (Kimaru et al., 2019). The behavior of both indices is quite similar. In general, values range from −3.0 to 2.0, with severe to moderate wet events being more frequent in the SPEI ( Figure 4B). On the contrary, according to the SPI ( Figure 4A), severe dry events intersperse with moderately wet events. In particular and according to the SPI values, the city of Chachapoyas experienced four extreme droughts (2001, 2005, 2010, and 2018). However, only one extreme event was reported by the SPEI (2010). Most of these detected dry events coincided with the years with the highest number of forest fires in the area of Chachapoyas, being the years of 2005, 2010, and 2018, the ones with more fires (Manríquez Zapata, 2019;Castillo et al., 2020). Therefore, the occurrence of fires could be associated with extreme dry events. Moreover, the SPI (2006SPI ( , 2012SPI ( , and 2018 reported, three extremely wet events although only one was noted by the SPEI (2018). It should be noted that there is a disparity between SPI and SPEI results from 2017 to 2019, where the SPEI indicates the occurrence of only wet events This disparity between the indices occurs because of the increase in precipitation, the only variable that the SPI index takes into account, occurs before the decrease in temperature, a variable that the SPEI requires to calculate the climate water balance (Stojanovic et al., 2020). The SPI and SPEI values on a 6-month time scale oscillate between −2.5 and 2.0 ( Figure 5). Both dry and wet events were of lower intensity and longer duration, which is normal when the time scale is increased (Vicente-Serrano et al., 2010;Kimaru et al., 2019). In this scale, the SPI ( Figure 5A), is the only one that indicated that two extreme droughts took place in 2001 and 2005, in contrast to SPEI ( Figure 5B), which classifies the same droughts as severe. On this scale, both indices continue to show disparity from 2017 to 2019.
According to the three and six-month, SPI and SPEI timescales dry and wet events intensify from the middle of the 1981-2019 period, specifically in the year 2017 for wet events. At the same time, the SPI classified wet events as more intensive than the SPEI. It is important to highlight, that indices at small time scales have greater variability, causing dry or wet events to be very frequent and of very short duration. On the other hand, on larger time scales, this variability decreases, and as a result, dry or wet events are less frequent but have a longer duration (Mckee et al., 1993;Avilés et al., 2015).
The 12-months SPI and SPEI indices are more stable ( Figure 6). As previously mentioned, dry and wet events are less frequent but of more duration due to slower index value fluctuation. Both the SPI and SPEI, show greater intensity in dry events at the initial phase and greater intensity towards the final phase in wet events. Overall, both indices oscillate between −2.5 and 2.0, evidencing an extreme drought in 1993, and an extremely wet event in 2017. It is to be noted that the extreme drought event of 1993, is detected by the 3 and 6 months SPI and the SPEI, as a severe drought event. This is mainly due to the indices' behavior. In small timescales (3 or 6-months), the indices behavior is very variable due to their fast response to precipitation and temperature changes. In contrast, when the timescales are longer (12 or 24 months), the indices respond more slowly to changes in climate variables. This makes the events less frequent but more long-lasting and, in some cases, more intense (Castillo-Castillo et al., 2017).
Finally, according to the 24-months scale, both SPI and SPEI show more considerable differences regarding the intensity and occurrence of dry and wet events (Figure 7). The time disparity towards the end of both indices is now less than in short time scales. The SPEI values indicate more significant humidity surplus than the SPI, not only because of an increase in precipitation over the last decade but also because of a reduction in maximum and minimum temperatures ( Figure 3). As a result, severe and extreme wet events have occurred since 2011. Additionally, the 12-and 24-months SPI and SPEI indices indicate a drought of great duration and intensity from 1991 to 1994, as well as two wet events of equivalent duration and intensity from 2012-2016 to 2017-2019. This variation in intensity is due to the fact that precipitation data has a seasonal component since both SPI and SPEI depend on the area's rainfall (Ahmad et al., 2016). It should be noted that although the SPEI values generally oscillated between −3.0 and 2.0, the 24-months SPEI is the only one that has presented values close to −3.0 ( Figure 7A), in comparison to other SPEI values at smaller scales. This may suggest that the importance of temperature and evapotranspiration is greater for longer time scales (Stojanovic et al., 2020). The highest occurrence of wet events started in 1999. This can be observed on all time scales for both indices. Specifically, from 1999Specifically, from -2001Specifically, from , 2012Specifically, from -2016Specifically, from , to 2017Specifically, from -2019 where three intense periods of wet events were identified.
These results coincide with those reported by Imfeld et al. Studies in other parts of the world report on different behaviors. In several locations within the interior valleys of the central Cordillera de la Costa in Venezuela, several droughts were determined using the SPI for a 1 month time scale (1973-1974, 1982-1983, 1997-1998, 2002-2003, 2009-2010, 2013-2014), some of which coincide with the wet events in Chachapoyas (Cortez et al., 2018). Furthermore, Cunha et al. (2019), in their study on extreme droughts in Brazil from 1964 to 2019, registered an increase in extreme droughts during the last two decades in central and northern Brazil by using the 12-months SPI metric. Similarly, results reported by Stojanovic et al. (2018), from their assessment of droughts from 1980 to 2015 in Central Europe and their association with the moisture contribution from the Mediterranean Sea, indicate an increasing trend of extreme droughts, identified with the one-month SPEI index.

Temporal Characterization
The indices descriptive statistics on different time scales in the city of Chachapoyas have averages close to zero, something expected by the way they are calculated. (Table 2).
After assessing results for each index and time scale, the maximum intensity of a wet event, with a value of 2.565, was obtained from the 12-months SPI, while the maximum intensity of a drought was obtained from the 3-months SPI, with a value of −3,869. Likewise, the standard deviation oscillates between 0.966 and 1.027. Hence, the values mentioned above indicate that the city of Chachapoyas stays between the "moderate drought" and "moderately wet" categories. As previously noted, the intensity of dry and wet events is higher within shorter time scales. The SPI is an index that only takes into account rainfall, which is why the events of dry and moisture are more intense . Likewise, the SPEI, also takes into account the evapotranspiration, which generates that this index does not show the same intensities as the SPI for the same dry and wet events (Lee et al., 2017). In the case of Chachapoyas, there are several differences in the number of dry and wet events according to both indices, generally finding more events with the SPI than with the SPEI. This difference is mainly due to the evapotranspiration parameter, which depends on temperature (Vicente-Serrano et al., 2010. Therefore, including this parameter causes differences in the intensity and quantity of dry and wet events detected by indices Vicente-Serrano et al., 2015;Lee et al., 2017;Páscoa et al., 2017). In addition, SPEI usually represents dry and wet events better than SPI in both arid and humid climates , something which is not happening in the city of Chachapoyas, which stands out for its seasonal rainfall and mild temperatures (Rascón et al., 2020).

Relationship Between Indices at Different Time Scales
Precipitation is the parameter that regulates dry and wet events, either its deficit or surplus in a given period. At the same time, it is the main parameter used for the elaboration of both indices. That is why the correlation between the SPI and the SPEI is so high on the same timescale. However, the indices' correlation decreases when the timescales differ and more when comparing short and long timescales. This difference may be due to the decrease in temperatures, affecting evapotranspiration during the entire time series studied (Vicente-Serrano et al., 2010;Stagge et al., 2014). It must also be taken into account that evapotranspiration is a very important parameter in this area of the Andes, due to its relationship with climate water balance and the high seasonality of rainfall in this Andean region.  A correlation coefficient of 0.98 and 0.99 indicates that the periodic evolution of SPI and SPEI at the same temporal scale is similar. These results coincide with those obtained by Stojanovic et al. (2018), who determined a correlation value of 0.96 between the SPI and the SPEI at a 1 month scale when assessing droughts in central Europe. It should be noted that verifying if the inclusion of evapotranspiration data causes significant variations in SPEI values with respect to SPI values is important (Stagge et al., 2015). In the case of the city of Chachapoyas, the range of correlation between SPEI and SPI values varies from 0.54 to 0.99. These results are slightly lower, however akin to those reported by Stagge et al. (2014) for SPI and SPEI values in Europe.

CONCLUSION
This study analyzed the dry and humid events, as well as the main climatological parameters of the city of Chachapoyas in the period from 1981 to 2019, through the application of the drought indices SPI and SPEI and simple statistical analysis. After applying the SPI and SPEI indices in the city of Chachapoyas, it can be stated that wet events are predominant, compared to droughts. The most critical drought took place in the 1990s, while the most crucial wet events have occurred in the last 10 years. This finding is astounding because other studies that have been mentioned above found an inverse behavior to that of Chachapoyas. The SPEI, when including temperatures, shows an upward trend in the intensity, severity, and duration of wet events concerning the SPI. Considering that the SPEI is linked to changes in temperature, it allows researchers to assess better the beginning and end of dry and wet events at any time scale in comparison to the SPI. In the case of Chachapoyas, the indices have a high correlation between them regarding the same timescale.
Considering the tremendous impact of dry and wet events in production processes such as agriculture or livestock, or their relationship with forest fires or water availability for the  population, both the SPI, based exclusively on precipitation and the SPEI, sensitive to temperature changes, are positioned as a valuable analysis tool. Therefore, local and regional governments can use this tool to develop prevention, monitoring and mitigation plans for dry and wet events or to improve impact management plans.

DATA AVAILABILITY STATEMENT
The original contributions presented in the study are included in the article/Supplementary Material, further inquiries can be directed to the corresponding author.

AUTHOR CONTRIBUTIONS
JR, WA, MO, and MB conceived the ideas. JR and LQ collected the data. JR and LQ analysed the data. JR, WA, MO, and MB wrote the manuscript. All authors contributed to the article and approved the submitted version.

FUNDING
This work was funded by the SNIP project Nor. 352431 "Creation of the services of the research center in climatology and alternative energies at the Toribio Rodríguez de Mendoza National University, Amazonas region" -PROCICEA, which was financed by the Peruvian Economy and Finance Ministry's (MEF's) National System of Public Investment (SNIP).