Studies of meteorological elements and climate change in the Uruçuí river basin/Brazil

The objective is to show the variability of meteorological elements in the hydrographic basin area of the hydrographic basin of the Uruçuí Preto River–PI/Brazil, aiming to contribute to sustainable development in the productive areas of agriculture, laser, and hydrology. The meteorological elements studied are air temperature and relative humidity and their fluctuations, thermal amplitude, wind (intensity and direction), total insolation, cloud cover, evaporation, evapotranspiration, and rainfall. The data were from the 1960-1990 series, acquired by the Superintendency of the Development of the Northeast and by the Technical Assistance and Rural Extension Company of Piauí. The maximum annual temperature is 32.1°C, its minimum 20.0°C, with an average annual temperature of 26.1°C. A climatic classification was used according to the KÖPPEN systems, where two climatic types are distinguished in the Uruçuí Preto/PI river basin, the Aw, tropical hot and humid, with rain in summer and dry in winter; Bsh, warm semi-arid, with summer rains and dry winter. The variation of the thermal amplitude is from 11.9 to 14.9ºC. The average relative humidity of the air was 47 to 79%; the average annual precipitation was 937.7 mm; it was observed that the annual march of relative humidity follows the annual distribution of precipitation because the precipitation was the feeding process from natural sources of water vapor and moisture. Total Sunstroke in the BHRUP area ranges from 2520 to 2750 hours. It is concluded that the maximum annual temperatures increased during the period, which can cause several socioeconomic problems, and human health.


Introduction
The conditions of the climatic and hydrological elements of a given region are the main parameters in the estimation of water availability in that territory and/or region. Thus, in hydro climatological studies, these are basic assumptions that will guide the development of work in defining the planning and management model of water resources to be implemented. In this way, the compatibility between water availability and demand can only be done when the climatic parameters, especially precipitation, evaporation and evapotranspiration, and hydrological parameters, such as the movement and quantification of surface and groundwater in time and space, are duly considered (Eguchi & Albino, 2021).
The climatic variety also influences the environment, acting as interactions between biotic and abiotic components.
The climate of any region, situated in the most diverse latitudes of the globe, does not present the same characteristics every year (Soriano, 1997;Sousa Silva & Suertegaray, 2018).). In a climate region of contrasting neighboring areas on one rainy side on the other semi-arid, such as the Northeast of Brazil (NEB) and especially the State of Piauí, the monitoring of precipitation, especially during the rainy season, is essential for decision making that will benefit the population. Good rainfall monitoring is an indispensable tool in mitigating droughts, and waterlogging (Paula, Brito & Braga, 2010). Among the elements of climate in tropical areas, rainfall is the one that most influences agricultural productivity (Ortolani & Camargo, 1987;Diaz, Pereira & Soares, 2017).), especially in the semi-arid region, where the rainfall regime is characterized by events of short duration and high intensity (Santana et al., 2007). as a result, rainfall (precipitation) seasonality concentrates almost all its volume during the five to six months in the rainy season (Silva, 2004).
Spatial and temporal variation are characteristics of weather and climate. The temporal variation is a characteristic that should be studied with greater particularity and on different chronological scales. Because these studies will allow the knowledge of the climate in the past, present, and even make prognoses and diagnoses for future climatic situations from the mathematical models used (Fernando, 2008).
Several studies have been prepared on climate variability and its characteristics, so it is still far from reaching a consensus, especially concerning the local influence on global trends. However, studies of local climate variability, especially on temperature, relative humidity, and precipitation, are essential to understand the impacts of these variations on the population in general. Suppose the fluctuations are significant at the local level. In that case, these changes can cause socioeconomic impacts, on agricultural and livestock production, environmental impacts, changes in ecosystems, and social impacts, proliferation of disease vectors (Maluf & Rosa., 2011).
Precipitation is fundamental for climate characterization (Marinho & Rivera, 2021).). Its monitoring is important for managing and maintaining water resources because it provides data that contribute to public planning and studies that seek the sustainable use of water. Rainfall data, for example, are essential for studies like those of D' Almeida et al. (2006), Costa et al., (2007), Sampaio et al. (2007), and Coe, Costa & Soares-Filho (2009), who concluded that the deforestation of the Amazon Forest is directly the imbalance in the environment, especially in the hydrological cycle, wherein simulations showed a significant decrease in evapotranspiration and precipitation.
According to Silva et al. (2013), the State of Piauí has differentiated climatic conditions, with oscillation in rainfall rates whose origin is quite individualized, also presenting relatively variable average annual temperatures. Rainfall presents great spatial and temporal variability (Costa et al., 1998), showing two rainy regimes: in the south of the State, it rains from November to March; in the center and north, the rainy season begins in December, extending until May. Rainfall rates vary between 700 and 1,300 mm in the southern region, between 500 and 1,450 mm in the central region, and between 800 and 1,680 mm in the north of the State. In the North region, rainfall indices have a more regular distribution than in the Central and South areas, evidencing the physiographic aspects, relief, fauna, flora, and distance from the sea. Due to the large variation in rainfall over the years, it can be observed that the phenomena of macro, medium, and micro scales are of great importance for the rainfall regimes in the State of Piauí, which follow the chronological time of their activities and duration. Medeiros et al. (2013) refers to variability as one of the best-known elements of climate dynamics, and the impact produced by this phenomenon, even within the expected range, can have significant reflections on human activities. We used data on maximum air temperature and relative humidity and monthly and annual rainfall totals from 1960 to 1990. As a result of this work, it can be affirmed that the maximum annual temperatures increased during the analyzed period, which can cause several socioeconomic problems and problems for human health. From the data, it was also verified that the relative humidity of the air is decreasing throughout the series studied, which may be related to the increase in temperature and, consequently, to greater water evaporation. Regarding the total annual rainfall, it was noted that the values are gradually increasing, and this increase may be related to the increase in temperature, which causes greater evaporation and consequently more significant precipitation.
According to Marengo & Camargo (2007), the thermal amplitude for southern Brazil showed sharp negative trends in the period 1960-2002, indicating that the minimum temperatures were more intense than the maximum temperatures, especially in summer. For Rusticucci & Barrucand (2004), negative trends in diurnal thermal amplitude are due to positive variations in minimum temperature trends. According to the analyses by Marengo & Camargo (2007), the observed warming seems to be more intense in winter than in summer, which is probably related to the increase in the number of warm days in winter (Campos, 2010).
Air temperature expresses in a simple way the energy contained in the medium. During a day, the energy available in the environment oscillates between two extreme values, between the minimum and maximum temperature. As this energy goes from one extreme to the other, it continuously stimulates vital physiological processes in living beings such as the development and growth of plant species, such as transpiration, respiration, germination, growth, flowering, and fruiting. At each stage of plant development, there are suitable temperature ranges for its perfect development (Costa, Costa Filho & Brandão, 2011).
Moreover, the daily temperature cycle predominates in thermal comfort and the adequacy of human and animal beings in certain places. Rodrigues et al. (2016) showed that the minimum temperature variability for the municipality of Lavras / MG has been changing minimum values. Medeiros et al. (2014) analyzed the predominant monthly wind directions over the Uruçuí Preto river basin. The predominant wind direction was described from the frequency of occurrence in a given direction, the methodology adopted from Galvani et al. (1999). The predominant wind directions for the basin and the referred predominant contributions for the rainy and dry periods were represented. Medeiros (2010) clarified that the possibilities of mobile dune barrages should be worked on in the largest entrances of the predominance of winds and their intensities. A counter was performed to calculate the predominant wind input frequency for the studied area. The predominant directions with the highest input frequencies were: northeast-southeast with 19 times, east-southeast with 13 times, and northeast with 5 times around the basin.
The objective was to demonstrate that the meteorological elements studied such as maximum air temperature, minimum air temperature, average air temperature, and their maximum and minimum fluctuations, temperature range, relative air humidity, wind (intensity and direction), insolation total, cloud cover, evaporation, evapotranspiration, and rainfall have their contributions to climate variability and its oscillations targeting climate change in the area of the hydrographic basin of the Uruçuí Preto-PI (BHRUP)/Brazil river. As well as analyzing the municipal rainfall variability between the different rainfall regimes for the state of Piauí (North, Central and South regions), it was proven that they have common areas of rainfall Research, Society andDevelopment, v. 10, n. 11, e554101120055, 2021 (CC BY 4.0) | ISSN 2525-3409 | DOI: http://dx.doi.org/10.33448/rsd-v10i11.20055 5 occurrences with their respective provocative and inhibitory systems. Finally, we sought to analyze the climate variability of relative air humidity and maximum air temperature in the Uruçuí Preto River basin -PI, focusing on such variations as a means to understand future changes. Data on maximum air temperature and relative humidity and monthly and annual rainfall totals from 1960 to 1990 were used.

Methodology
The area of interest of the study has a reduced and spatially poorly distributed network of meteorological stations, which hinders a good characterization of the climatic conditions. Thus, we used interpolated data, estimated and generated by straight lines of multiple linear regressions, through the software estima_T (Cavalcanti & Silva, 1994;Cavalcanti, Silva & De Souza, 2006). To analyze the inter-municipal climatic behavior of the Uruçuí Preto river basin, precipitation data acquired through the Superintendence for the Development of the Northeast -SUDENE, and the Company for Technical Assistance and Rural Extension of the State of Piauí -EMATER/PI, for the period from 1960 to 1990 were used, comprising 49 rainfall posts located in the study area.
The region is drained by the Uruçuí Preto River and its tributaries Ribeirão dos Paulos, Castros, Colheres and Morro da Água, and by the Estiva and Corrente creeks, both perennial. The Uruçuí Preto river basin is preponderantly located in the sedimentary basin of the Parnaíba river, constituting one of the main tributaries on the right margin. It has a total area of approximately 15,777 km2, representing 5% of the territory of Piauí. It covers part of the southwest region, projecting from south to north in a spear (Comdepi, 2002).
The Uruçuí Preto river basin comprises 25 municipalities and 24 farms containing rainfall data with a 30-year series (1960-1990 period). The maximum annual temperature is 32.1 ºC, the minimum annual temperature is 20.0 ºC, and the average annual temperature is 26.1 ºC. We used the Climatic Classification according to the KÖPPEN systems, where two climatic types are distinguished in the basin of the Uruçui Preto river -PI, the Aw, tropical hot and humid, with summer rains and dry winter; is the Bsh, semi-arid hot, with summer rains and dry winter (Medeiros, 2013;Medeiros, de Holanda & Alexandre, 2018;Medeiros, Cavalcanti, & Medeiros Duarte, 2020).
The precipitation regime that comprises the study area begins with the pre-season rains, starting in the second half of October. The characterization of the rainy season begins in the first days of November and extends until March, with December, January, and February as the rainiest quarters.
The predominant rainfall factors for Uruçuí the Preto river basin are the formation of instability lines carried by the Southeast-Northeast trade winds, heat exchanges, traces of cold fronts when their most active penetrations convective cluster formations, orography, cyclonic vortex formation contributions, conveyor belt, orography, and local effects, are factors that increase the transport of water vapor and moisture and consequently the cloud cover. Usually, the rains have moderate intensity, fregular weather and around seven to eight hours of discontinuous daily rainfall, followed by irregularity due to the failures of the acting meteorological systems. It is emphasized that summer periods, occurrences of several consecutive days without rain during the rainy season, in the four months (December, January, February, March) are expected. Its magnitude varies depending on the season and the meteorological factors that are off. It has been recorded occurrences with summers longer than nineteen (19) days in the time interval within the four months. Medeiros (2013).

Results and Discussion
In this section, the results are presented using figures from the meteorological elements in the area of the hydrographic basin of the Uruçuí Preto-PI -BHRUP/Brazil river from the 1960-1990 series, acquired by the Superintendence for the Development of the Northeast -SUDENE, and by the Piauí Technical Assistance and Rural Extension Company -EMATERPI.
In Figure 2 (a, b, c, d, e) represents the temperature range (a) of the coldest month; (b) hottest month; (c) coldest four months; (d) hottest four months; (e) and annual, for the Uruçuí Preto river basin area -PI.
In Figure 2a shows the temperature range of the coldest month (January) for the area of the BHRUP; it is observed that the west and the extreme southwest predominate the area of the lowest ranges, the range of average ranges predominates throughout the area (north, central and south) with its fluctuation ranging from 9.58 to 9.78 °C, it was also observed a small area of temperature range greater than 9.78 °C in the eastern sector of the study area.
In Figure 2b represents the temperature range of the hottest month (September) for the area of the BHRUP; it is observed a range of temperature range in the extreme south of the study area greater than 15°C, a area in the southeast and southwest sectors as amplitude ranging between 14.7 to 15.2 °C and part of the southern region, part of the central region with temperature range ranging between 14.5 to 15.2 °C, the predominant temperature range in the central part and throughout the Research, Society andDevelopment, v. 10, n. 11, e554101120055, 2021 (CC BY 4.0) | ISSN 2525-3409 | DOI: http://dx.doi.org/10.33448/rsd-v10i11.20055 7 northern area is 15.3 °C. In Figure 2c shows the thermal behavior of the coldest four months (December to March), which follows the characteristics of Figure 2a.
In Figure 2d shows the behavior of the variability of the temperature range for the warmest four months (June to September), it is observed a small area of maximum amplitude in the extreme southwest and an area of minimum amplitude in the north and northeast and a small area near the city of Gilbués. In the south, central and north regions, there is a variability of the thermal amplitude oscillating between 14.3 and 14.7 °C.
In Figure 2e an increase is observed in the north-south direction; it is highlighted that the areas of lower amplitudes are located in the north and northeast and a small range in the southwest, in the central region, south, and part of the south of the northern region it is seen the variability of the temperature range fluctuating between 12 and 12.3 °C it is noted that the range of southeast to the southwest is characterized by the largest annual temperature ranges. In Figure 3a a gradual increase in the south-north direction is observed, noticing that the greatest fluctuations of the maximum and minimum temperatures occur north of the central region and in the entire area of the north and northeast region.
In Figure 3b shows the persistence of the gradual increase of the maximum temperature in the direction from south to north, a small area in the southwestern sector with maximum temperature, it is observed that in the southern region occurs reductions of maximum temperatures and in other areas predominate high temperatures of maximums. Research, Society andDevelopment, v. 10, n. 11, e554101120055, 2021 (CC BY 4.0) | ISSN 2525-3409 | DOI: http://dx.doi.org/10.33448/rsd-v10i11.20055 8 In Figure 3c, we have the variability of maximum temperature for the coldest four months (December to March), in which we highlight an increase in the south-north direction with its most intense oscillations in the central and northern sector and a small area in the southwestern sector, the southern and western sector of the central sector record the lowest values of the maximum temperature of the four months.   (c) four-month minimum of the minimum; (d) four-month minimum of the maximum; (e) and annual, for the Uruçuí Preto river basin area -PI.
In Figure 4a, we can see the minimum temperature variability that occurs in June, where a gradual increase in the south-north direction can be seen. A small area in the southwest with 19 °C and another in the northeast with an oscillation between 18.6 and 20 °C can be highlighted. Figure 4b has the behavior of the minimum temperature of the maximum for the area of the BHRUP that occurs between August and September, realize the gradual increase in the south-north direction. The minimum temperature variations Research, Society andDevelopment, v. 10, n. 11, e554101120055, 2021 (CC BY 4.0) | ISSN 2525-3409 | DOI: http://dx.doi.org/10.33448/rsd-v10i11.20055 9 are more significant in the southern sectors and part of the central region; the highest minimum-maximum temperature occurs north of the central region. Throughout the northern area of the BHRUP, there are small areas in the southwestern and eastnortheastern sectors with a high minimum temperature of the maximum. Figure 4c represents the four months of the occurrence of the minimum temperature of the minimum in which it highlights the areas with greater intensity located to the southwest and northeast of the figure with an oscillation ranging from 18.1 to 20.7 ° C is observed a gradual increase in that parameter in the south-north direction and a range of low minimum temperature in the southern sector.
It is observed the fluctuation of the minimum temperature for the four-month with the minimum occurrences of the maximums as shown in Figure 4d where it highlights the areas of maximum elevations in the southwestern position and the northern and northeastern part of the northern region, in the other areas, occur gradual increases with oscillations ranging from 19.9 to 21.7 °C, the lowest variability of this parameter occurs in the southern region.
In Figure 4e shows us the variability of minimum annual temperature in the area of the BHRUP; the highest minimum temperatures are located in the southwest and part of the north and northeast region; in the southern region, there are two areas where is located the lowest variability of minimum temperature.   In Figure 6a represents the maximum evaporative power that occurs between August and September with fluctuation from 120 to 162 mm; the northern, northeastern, southeastern, and southwestern sectors occur the highest evaporative rates, highlighting a gradual increase from south to north. Figure 6b shows the minimum evaporation that occurs in February with a monthly evaporative rate ranging from 84 to 118 mm. It can be seen that the highest evaporative rate is located in the part of the northern area, northeast, and southeast, and the lowest evaporative rates are in the extreme south and east of the central region.
In Figure 6c shows the variability of the evaporation of the minimum four months (December to March) that has its variability between 88 to 118 mm, highlighting the areas of lowest evaporation located in the extreme south and the eastern sector of the central region, areas with high evaporative power to the southeast, northeast and north of the BHRUP, the southern sectors of the southern region, the central area to the west and the western sector of the northern region with intermediate evaporations.
The evaporative variability of the four months of maximum evaporation can be seen in Figure 6d, which occurs in the range of 114 to 158 mm between June and September.
In Figure 6e shows an annual variability of evaporation ranging from 100 to 226 mm per year, the southernmost sector has the lowest evaporation rates, and there is an increase in the south-north direction, which gradually increases its evaporative power.  Research, Society andDevelopment, v. 10, n. 11, e554101120055, 2021 (CC BY 4.0) | ISSN 2525-3409 | DOI: http://dx.doi.org/10.33448/rsd-v10i11.20055 12 In Figure 7 (a, b, c, d, e) represents the variability of evapotranspiration -ETP: (a) minimum; (b) maximum; (c) minimum four months (d) maximum four months; (e) and annual, for the Uruçuí Preto river basin area -PI.
In Figure 7a we have the minimum evapotranspiration rates that occur in February with fluctuation from 84 to 118 mm; the areas with lower ETP rates are located in the extreme south and the eastern part of the central region, while the northern, northeastern, and southeastern sectors have high ETP rates.
In Figure 7b shows a south-north increase throughout the BHRUP, with its minimum values of maximum values located in the extreme south and a small strip to the east of the central area.
In Figure 7c is presented as an evaporative behavior of the four-month minimum ETP, where they are located in the extreme south and a band east of the central area; the other areas present values in gradual increases with variability ranging from 98 to 118 mm.
In Figure 7d is evidenced by the variability of evapotranspiration of the four months maximum between August and September; with its variability ranging from 114 to 158 mm, the lowest evapotranspiration rates occur in the extreme south, and in other areas is seen a gradual increase in maximum evapotranspiration.
In Figure 7e shows the lowest annual evapotranspiration rates in the extreme south and the eastern area of the central region, the other areas present evapotranspiration in elevations, and their maximum values occur in the northern, northeastern, and southwestern sectors. Its annual fluctuation occurs in the range of 1,160 to 1,600 mm.  Research, Society andDevelopment, v. 10, n. 11, e554101120055, 2021 (CC BY 4.0) | ISSN 2525-3409 | DOI: http://dx.doi.org/10.33448/rsd-v10i11.20055 13 In Figure 8a, we observe the minimum total insolation (February) behavior in the BHRUP, where its variability oscillates between 155 to 178 hours, with emphasis on the small area to the southwest with 157 hours of total insolation. In the total maximum insolation (September) (in Figure 8b)  In Figure 8d represents the total insolation for the four months of maximum insolation (June, July, August, and September). One can see small areas of low insolation in the southwestern, extreme northern, and northeastern sectors, extreme insolation in the southwestern, western, and eastern sectors of the central area, and a reduction in the southern-northern direction. The variability of the total insolation oscillates from 2520 to 2750 hours within the BHRUP; a reduced area in the southwest of the basin stands out, in which its insolation is the minimum 2520 h, according to Figure 8e. (d) four-month maximum; (e) and annual, for the Uruçuí Preto river basin area -PI. Figure 9a demonstrates the variability of the minimum cloud cover for the BHRUP, the lowest cloud coverages occur in the southern area of the central sector and northern area of the southern sector, and the eastern sector of the BHRUP, in the southern sector of the southern area and the northern sectors of the central and in almost the entire area of the northern sector the fluctuability of cloud cover oscillates between 2.5 to 2.9 tenths.
In Figure 9b, the variability of maximum cloud cover fluctuates between 6.6 to 7.1 tenths, and its increases occur in the east-northwest direction. Its smallest areas of cloud cover occur in the eastern position and the southern end of the BHRUP. Figure 9c represents the cloud cover in the four months of minimum cloud cover in the area of BHRUP (June to September); it highlights the area of lowest cloud cover located east-northeast; the other areas have a variability of coverage ranging from 6 to 6.9 tenths.
In Figure 9d represents the cloud cover in the four months of maximum cloud cover in the BHRUP area (October to March). We highlight the far south and east areas with low cloud cover and the coastal part of the western region, where there is maximum cloud cover.
In Figure 9e shows the annual variability of cloud cover for the BHRUP; there is a gradual increase in the northeastsouthwest direction, the largest areas with cloud cover are concentrated in the southwestern region and the coastal area of the western region ranging from 4.9 to 5.3 tenths and an area of low cloud cover in the northeastern sector with an oscillation between 4.7 and 4.9 tenths of coverage. In Figure 10 (a, b, c, d, e) represent the variability of relative humidity (a) minimum; (b) maximum; (c) four-month minimum; (d) four-month maximum; (e) and annual, for the Uruçuí Preto river basin area -PI. Research, Society andDevelopment, v. 10, n. 11, e554101120055, 2021 (CC BY 4.0) | ISSN 2525-3409 | DOI: http://dx.doi.org/10.33448/rsd-v10i11.20055 15 The variability of the minimum relative humidity (RH) (September) in the BHRUP area is represented in Figure 10a, which oscillates between 47.2 and 52.6%.
In Figure 10b shows the oscillations of maximum RH (February), highlighting the area to the east and the northern sectors of the central region and the southern sector of the northern region, and a small area in the southern sector with low RH concentrations.
In Figure 10c, we observe the fluctuations of RH in the four months of minimum humidity; it appears that in the northern region and northern part of the central region and the extreme south and southwest are concentrated the values of high humidity and in the southeast sector stands out the lowest values of RH for the minimum four-month period.
In Figure 10d has the representation of the four months of maximum RH of the area under study, the central region presents the lowest concentration of RH as well as a small area in the southern sector, in the northern sector of the central area, and throughout the northern sector and in isolated areas of the southern sector there are the highest rates of RH concentration.
In Figure 10e Figure 11a represents the minimum wind intensity in the BHRUP, and a reduction of intensity is observed in the eastwest direction and the areas with lower intensities located at the extreme south and west of the figure.
The maximum wind intensities are represented in Figure 11b, where their intensities flow between 1.71 to 1.98 ms-1. Figure 11c has the oscillations of wind intensity for the four months of minimum intensities; it is noteworthy the area in the extreme south as low intensity, in the southern region the high wind intensities are observed and also in the riverine strip of the eastern sector, in other areas, there are moderate intensities.
In Figure 11d, it is observed the predominance of the intensity of the four-month maximum wind in the southwestern sector and the areas of the southern and central regions, in the northern and eastern regions of the central area have the lowest wind intensities representative of the four months.
In Figure 11e represents the annual wind intensity, with the following highlights in the area of small wind intensity in the far south and the central part to the north of the southern region is the highest intensities and moderate winds in the northern sector of the central region and throughout the area of the northern region.] In Figure 12 (a, b, c, d, e) represents the variability of rainfall (a) maximum; (b) minimum; (c) rainy four months; (d) dry four months; € and annual, for the Uruçuí Preto river basin area -PI.
In Figure 12a highlights the southern area in its center, which recorded the highest rainfall intensities, while in the southwestern and southeastern sectors occurred the lowest rainfall indices, while in the other areas of the basin, the rainfall indices are insignificant for farming and water storage.
In Figure 12b represents the maximum rainfall occurring in the BHRUP, observing that the rainfall occurs in an eastwest direction and its maximum values occur in the extreme southwest and the coastal area of the basin.
In Figure 12c shows the behavior of the dry four-month period in which the highest rainfall indices are observed in the southern region and its gradual reduction until the northern region where the lowest rainfall indices are observed.
In Figure 12d, it is highlighted that the occurrences of rainfall for the dry four months occur with greater significance in the central part of the basin towards the west, in the eastern sector until the middle of the basin, the lowest rainfall indexes are concentrated, these rains are of low magnitudes and short time interval.   (2016) Relative humidity can be an active or passive contributor to soil degradation and desertification because with other meteorological elements benefiting or disfavoring soil drying and defragmentation, it can contribute to the increase or reduction of fire outbreaks and air quality (Medeiros, de Medeiros & LIMA, 2011).
In a climate analysis, it is worth considering the periods where the intermittence of rain, even in summer, can present long daily periods without rain. That is because there are irregularities in meteorological systems. As well as the temporal and spatial variability of rainfall, it is a climate attribute in tropical climate regions, as it is understood as a system of relationships between atmospheric attributes, such as wind, temperature, and humidity, with geographic factors such as relief, land use, latitude, continentality, among others, related (Moura & Jardim, 2017).

Conclusion
The results presented indicate possible climatic variations in air temperature, relative humidity, and precipitation, pointing to a trend towards warmer and rainier conditions.
An anomalous effect of precipitation distribution is observed during the January summers. The variability of fluctuations in maximum air temperature increases, the reduction in relative humidity, and the increases in rainfall indices may be related to local changes.
The annual maximum air temperature showed great variation among the studied period, the absolute maximum temperature was increased by 10.8%, and the absolute minimum temperature suffered an increase of 9.5%.
The total annual precipitation showed a gradual increase in its indices since the 1980s, which may be related to the increase in temperature; it is observed that since the 1990s, a gradual reduction may be related to the increase in temperature and consequently with greater water evaporation. It can be observed that the relative humidity in the dry months reached critical levels below 15%.
The extreme, maximum and minimum, and average temperature can contribute to desertification and soil degradation because it causes the drying up and defragmentation of the soil and makes the withering point in the vegetation.
The wind directions and speeds are responsible for the transport of dust, smoke, and grain, in addition to causing the drying out of the soil and causing erosion, plant lodging, the spread of pests and diseases; it contributes to a better rate of evaporation and evapotranspiration, increases the intensities of the flames in hotspots and fires, reduces the thermal sensation.
Thus, through the data inferred in this work, we can have subsidies to plan future actions in projects for the recovery of degraded areas and urban development, both as an aid in clean and renewable energy generation projects (wind power, for example), in large agricultural projects, minimizing the chances of occurrence of lodging through wind barriers that can be deployed, in addition to contributing to the planning of cities, industrial parks, and leisure.
The meteorological variables analyzed can be contributing factors to the agricultural sustainability process.
Considering consecutive years, in which the extremes seen occur systematically, one can have factors that added together, would induce sustainability, causing problems directly related to flora and consequently the fauna of the place under study.