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28 pages, 26490 KiB  
Article
Vertical Accelerations and Convection Initiation in an Extreme Precipitation Event in the Western Arid Areas of Southern Xinjiang
by Na Li, Lingkun Ran, Daoyong Yang, Baofeng Jiao, Cha Yang, Wenhao Hu, Qilong Sun and Peng Tang
Atmosphere 2024, 15(12), 1406; https://doi.org/10.3390/atmos15121406 - 22 Nov 2024
Viewed by 205
Abstract
A simulation of an extreme precipitation event in southern Xinjiang, which is the driest area in China, seizes the whole initiation process of the intense convective cell responsible for the high hourly rainfall amount. Considering the inner connection between convection and vertical motions, [...] Read more.
A simulation of an extreme precipitation event in southern Xinjiang, which is the driest area in China, seizes the whole initiation process of the intense convective cell responsible for the high hourly rainfall amount. Considering the inner connection between convection and vertical motions, the characteristics and mechanisms of the vertical accelerations during this initial development of the deep convection are studied. It is shown that three key accelerations are responsible for the development from the nascent cumuli to a precipitating deep cumulonimbus, including sub-cloud boundary-layer acceleration, in-cloud deceleration, and cloud-top acceleration. By analyzing the right-hand terms of the vertical velocity equation in the framework of the WRF model, together with a diagnosed relation of perturbation pressure to perturbation potential temperature, perturbation-specific volume (or density), and moisture, the physical processes associated with the corresponding accelerations are revealed. It is found that sub-cloud acceleration is associated with three-dimensional divergence, indicating that the amount of upward transported air must be larger than that of horizontally convergent air. This is favorable for the persistent accumulation of water vapor into the accelerated area. In-cloud deceleration is caused by the intrusion or entrainment of mid-level cold air, which cools down the developing cloud and delays the deep convection formation. Cloud-top acceleration is responsible for the rapid upward extension of the cloud top, which is highly correlated with the convergence and upward transport of moisture. Full article
(This article belongs to the Section Meteorology)
Show Figures

Figure 1

Figure 1
<p>(<b>a</b>) Accumulated 24 h precipitation on 15 June 2021. (<b>b</b>) Bar chart of hourly precipitation over several automatic observation stations in southern Xinjiang.</p>
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<p>(<b>a</b>–<b>i</b>) Observed composite radar reflectivity from the C-band radar in Hoton in southern Xinjiang. The stations indicated by the black stars are, respectively, Sampoulu (“1”), Lop (“2”), Hoton (“3”), and Moyu (“4”). The black box and the red circle indicate the focused convective areas.</p>
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<p>The weather pattern at 1100 UTC on 15 June 2021. (<b>a</b>) Geopotential height (black contours, unit: 1 gpm), wind speed (color shaded, unit: m s<sup>−1</sup>) and horizontal divergence regions (red contours, unit: 10<sup>−5</sup> s<sup>−1</sup>, 4 interval) at 200 hPa; (<b>b</b>) geopotential height (black contours, unit: 10 gpm) at 500 hPa, and wind speed (color shaded) and water vapor flux (red arrows, unit:) at 800 hPa. The symbol “H” means the high-pressure system and “L” means the low-pressure system, which is denoted by geopotential height in the figures. The black dotted short lines are trough regions. The black boxes indicate the focused precipitation region. The yellow arrow box indicates the flow from the east–west-oriented shallow trough, the pink arrow box indicates the flow from the north–south-oriented shallow trough and the green arrow indicates the flow from the east–west-oriented shallow trough over the mountain. The black thick arrows indicate the main directions of the moisture transportation.</p>
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<p>Simulated maximum radar reflectivities at (<b>a</b>) 0700 UTC, (<b>b</b>) 0800 UTC, (<b>c</b>) 0900 UTC, (<b>d</b>) 1000 UTC, (<b>e</b>) 1100 UTC, (<b>f</b>) 1200 UTC on 15 June 2021. Boxes enclosed the convective cell that the paper concerned. (<b>g</b>) The bar chart is the 10-min precipitation during this period.</p>
Full article ">Figure 4 Cont.
<p>Simulated maximum radar reflectivities at (<b>a</b>) 0700 UTC, (<b>b</b>) 0800 UTC, (<b>c</b>) 0900 UTC, (<b>d</b>) 1000 UTC, (<b>e</b>) 1100 UTC, (<b>f</b>) 1200 UTC on 15 June 2021. Boxes enclosed the convective cell that the paper concerned. (<b>g</b>) The bar chart is the 10-min precipitation during this period.</p>
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<p>(<b>a</b>,<b>b</b>) Maximum radar reflectivity (shaded, unit: dBz); (<b>c</b>,<b>d</b>) radar reflectivity (shaded, unit: dBz) and vertical velocity (contour, unit: m s<sup>−1</sup>); and (<b>e</b>,<b>f</b>) vertical accelerations denoted by Net_WAη (shaded, unit: 10<sup>−3</sup> s<sup>−1</sup>) and sum of mixing ratios of ice and cloud particles (0.05, 0.1, 0.2, 0.3, 0.4 black contours, unit: g/kg) at 0750 UTC along 78.5° E (left column) and 0820 UTC along 78.6° E (right column). The purple contour in (<b>f</b>) is 35 dBz radar reflectivity. The thick black line is 0 °C isotherm contour.</p>
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<p>(<b>a</b>–<b>c</b>) Maximum radar reflectivity (shaded, unit: dBz); (<b>d</b>–<b>f</b>) radar reflectivity (shaded, unit: dBz) and vertical velocity (contour, unit: m s<sup>−1</sup>); and (<b>g</b>–<b>i</b>) vertical accelerations denoted by Net_WAη (shaded, unit: 10<sup>−3</sup> s<sup>−1</sup>) and the sum of mixing ratios of ice and cloud particles (0.05, 0.1, 0.2, 0.3, 0.4 values, unit: g/kg) at 0910 UTC (left column), 0920 (middle column) and 0930 UTC (right column) along 78.8° E. The purple contour in (<b>g</b>–<b>i</b>) is 35 dBz radar reflectivity. The thick black line is the 0 °C isotherm contour. The green lines in (<b>d</b>–<b>f</b>) indicate 1 h precipitation (unit: mm) with magnitude on the right side of the y-axis.</p>
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<p>(<b>a</b>) PGF_WRF, (<b>b</b>) B_WRF and (<b>c</b>) Net_WAη at 0710 UTC along 78.5° N (contours, unit: 10<sup>−3</sup> s<sup>−1</sup>); (<b>d</b>–<b>f</b>) same as (<b>a</b>–<b>c</b>) but for 0750 UTC; (<b>g</b>) PGF_WRF difference, (<b>h</b>) B_WRF difference, and (<b>i</b>) Net_WAη difference between 0750 UTC and 0710 UTC along 78.5° N. The shaded areas are radar reflectivities. The red contours are the sum of mixing ratios of ice and cloud particles (0.05, 0.1, 0.2, 0.3, 0.4 values, unit: g/kg) to indicate the cloud. The “difference” means the fields at 0750 UTC minus those at 0710 UTC. The colored boxes indicate the areas with evident differences between 0710 and 0750 UTC. The areas enclosed by the orange box, blue box and green box are, respectively, the in-cloud area, the sub-cloud area and the boundary-layer area in front of the convection.</p>
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<p>(<b>a</b>) Difference of perturbation pressure between 0710 UTC and 0750 UTC (contours, unit: hPa) along 78.5° N; (<b>b</b>) same as (<b>a</b>) but for <math display="inline"><semantics> <mrow> <msubsup> <mi>p</mi> <mi>θ</mi> <mo>′</mo> </msubsup> </mrow> </semantics></math>; (<b>c</b>) same as (<b>a</b>) but for <math display="inline"><semantics> <mrow> <msubsup> <mi>p</mi> <mi>ρ</mi> <mo>′</mo> </msubsup> </mrow> </semantics></math>; (<b>d</b>) same as (<b>a</b>) but for <math display="inline"><semantics> <mrow> <msubsup> <mi>p</mi> <mi>ρ</mi> <mo>′</mo> </msubsup> <mo>+</mo> <msubsup> <mi>p</mi> <mi>θ</mi> <mo>′</mo> </msubsup> </mrow> </semantics></math>; (<b>e</b>) same as (<b>a</b>) but for <math display="inline"><semantics> <mrow> <msubsup> <mi>p</mi> <mi>m</mi> <mo>′</mo> </msubsup> </mrow> </semantics></math>. The shaded areas are radar reflectivities. The red contours are the sum of mixing ratios of ice and cloud particles (0.05, 0.1, 0.2, 0.3, 0.4 values, unit: g/kg) to indicate the cloud area. The “difference” means the fields at 0750 UTC minus those at 0710 UTC. The red thick arrows indicate the direction of PGF due to the change in the corresponding perturbation pressure.</p>
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<p>(<b>a</b>,<b>b</b>) Water vapor mixing ratio (shaded and black contours, unit: g/kg); (<b>c</b>,<b>d</b>) magnitude of water vapor flux (shaded) and wind vectors of (v, w) (unit: m/s); (<b>e</b>,<b>f</b>) horizontal wind speed; (<b>g</b>,<b>h</b>) 2D horizontal divergence (shaded, unit: 10<sup>−4</sup> s<sup>−1</sup>) and wind vectors of (v, w) (unit: m/s); and (<b>i</b>,<b>j</b>) 3D horizontal divergence (shaded, unit: 10<sup>−4</sup> s<sup>−1</sup>) and wind vectors of (v, w) (unit: m/s) in the section at 0710 UTC (left column) and 0750 UTC (right column) along 78.5° N. The red contours are the sum of mixing ratios of ice and cloud particles (0.05, 0.1, 0.2, 0.3, 0.4 values, unit: g/kg) to indicate the cloud. The blue line in (<b>e</b>,<b>f</b>) is the free convection level, and the orange line is the condensation level. The green line in (<b>j</b>) is the minus of the mass in column at 0750 and 0710 UTC (<math display="inline"><semantics> <mrow> <msub> <mrow> <mfenced close="|" open=""> <mrow> <msubsup> <mi>μ</mi> <mi>d</mi> <mo>′</mo> </msubsup> </mrow> </mfenced> </mrow> <mrow> <mn>0750</mn> <mi>U</mi> <mi>T</mi> <mi>C</mi> </mrow> </msub> <mo>−</mo> <msub> <mrow> <mfenced close="|" open=""> <mrow> <msubsup> <mi>μ</mi> <mi>d</mi> <mo>′</mo> </msubsup> </mrow> </mfenced> </mrow> <mrow> <mn>0710</mn> <mi>U</mi> <mi>T</mi> <mi>C</mi> </mrow> </msub> </mrow> </semantics></math>).</p>
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<p>(<b>a</b>) PGF_WRF, (<b>b</b>) B_WRF and (<b>c</b>) their sum for Net_WAη at 0820 UTC (contours, unit: 10<sup>−3</sup> s<sup>−1</sup>) along 78.6° N. The shaded areas are radar reflectivities. The red contours are the sum of mixing ratios of ice and cloud particles (0.05, 0.1, 0.2, 0.3, 0.4 values, unit: g/kg) to indicate the cloud.</p>
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<p>(<b>a</b>) Perturbation pressure, (<b>b</b>) <math display="inline"><semantics> <mrow> <msubsup> <mi>p</mi> <mi>θ</mi> <mo>′</mo> </msubsup> </mrow> </semantics></math>, (<b>c</b>) <math display="inline"><semantics> <mrow> <msubsup> <mi>p</mi> <mi>ρ</mi> <mo>′</mo> </msubsup> </mrow> </semantics></math>, (<b>d</b>) <math display="inline"><semantics> <mrow> <msubsup> <mi>p</mi> <mi>ρ</mi> <mo>′</mo> </msubsup> <mo>+</mo> <msubsup> <mi>p</mi> <mi>θ</mi> <mo>′</mo> </msubsup> </mrow> </semantics></math>; (<b>e</b>) <math display="inline"><semantics> <mrow> <msubsup> <mi>p</mi> <mi>m</mi> <mo>′</mo> </msubsup> </mrow> </semantics></math> at 0820 UTC along 78.6° N (contours, unit: hPa). The shaded areas are radar reflectivities. The red contours are the sum of mixing ratios of ice and cloud particles (0.05, 0.1, 0.2, 0.3, 0.4 values, unit: g/kg) to indicate the cloud.</p>
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<p>(<b>a</b>) Perturbation temperature at 0750 UTC (shaded and contours, unit: K), (<b>b</b>) perturbation temperature at 0820 UTC (shaded and contours, unit: K), (<b>c</b>) diabatic heating and cooling associated with the microphysical process at 0820 UTC (shaded, unit: 10<sup>−3</sup> K s<sup>−1</sup>), (<b>d</b>) the 2D divergence field at 0820 UTC (shaded, unit: 10<sup>−4</sup> s<sup>−1</sup>) along 78.6° N. The red contours in (<b>a</b>,<b>b</b>) and black contours in (<b>c</b>,<b>d</b>) are the sum of mixing ratios of ice and cloud particles (0.05, 0.1, 0.2, 0.3, 0.4 values, unit: g/kg) to indicate the cloud. The vectors are the wind vectors of (v, w) (unit: m/s) in the current section.</p>
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<p>(<b>a</b>) The 2D divergence fields (shaded, unit: 10<sup>−4</sup> s<sup>−1</sup>) and horizontal wind vectors (arrows, unit: m/s) at 7 km height at 0750 UTC, (<b>b</b>) 0820 UTC, (<b>c</b>) 0910 UTC and (<b>d</b>) 0930 UTC. The purple contours are 35 dBz radar reflectivity.</p>
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<p>Same as <a href="#atmosphere-15-01406-f007" class="html-fig">Figure 7</a> except for the time of 0850 UTC and 0910 UTC. The “difference” means the fields at 0910 UTC minus those at 0850 UTC. The area enclosed by the thick black line is the positive Net_WAη area, while that enclosed by the rose red line is the negative Net_WAη area. “PGF” is the pressure gradient force, and “B” is buoyancy.</p>
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<p>Same as <a href="#atmosphere-15-01406-f008" class="html-fig">Figure 8</a> except for the time of 0850 UTC and 0910 UTC. The “difference” means the fields at 0910 UTC minus those at 0850 UTC. The red thick arrows indicate the direction of PGF due to the change in the corresponding perturbation pressure.</p>
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<p>(<b>a</b>,<b>b</b>) Diabatic heating and cooling associated with the microphysical process (shaded, unit: 10<sup>−3</sup> K s<sup>−1</sup>); (<b>c</b>,<b>d</b>) water vapor mixing ratio (shaded and black contours, unit: g/kg) in the section at 0850 UTC (left column) and 0910 UTC (right column) along 78.8° N. The black contours in (<b>a</b>,<b>b</b>) and red contours in (<b>c</b>,<b>d</b>) are the sum of the mixing ratios of ice and cloud particles (0.05, 0.1, 0.2, 0.3, 0.4 values, unit: g/kg) to indicate the cloud. The purple contours are 35 dBz radar reflectivity.</p>
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<p>Horizontal wind speed (left column, shaded, unit: m/s) and water vapor mixing ratio (right column, shaded and contours, unit: 10<sup>−3</sup> g Kg<sup>−1</sup>) at 2 km height at (<b>a</b>,<b>b</b>) 0610 UTC, (<b>c</b>,<b>d</b>) 0700 UTC, (<b>e</b>,<b>f</b>) 0800 UTC, (<b>g</b>,<b>h</b>) 0850 UTC, and (<b>i</b>,<b>j</b>) 0930 UTC. The white, purple and red contours, respectively, represent the 10, 35 and 50 dBz radar reflectivity. The arrows are wind vectors. The black box indicates the location of the focused convection. The colored tringles indicate the small-scale ridges. The thick arrow in (<b>a</b>,<b>b</b>) indicates the moving direction of the topographic clouds.</p>
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17 pages, 10342 KiB  
Article
Study on the Water Mechanism of Sparse Grassland Decline of Ulmus pumila L.
by Tianbo Xia, Ping Zhang, Jinluo Ma, Yuan Zhao, Xiaohui Yang, Hao Wu, Xuejuan Feng, Lei Jin and Kaifang Zhang
Forests 2024, 15(12), 2061; https://doi.org/10.3390/f15122061 - 22 Nov 2024
Viewed by 242
Abstract
Ulmus pumila L. occupies an important niche in arid ecosystems. This study aimed to investigate the sap flow characteristics of declining Ulmus pumila L. in arid regions and its relationship with environmental factors. During the 2023 growing season (June to October), continuous sap [...] Read more.
Ulmus pumila L. occupies an important niche in arid ecosystems. This study aimed to investigate the sap flow characteristics of declining Ulmus pumila L. in arid regions and its relationship with environmental factors. During the 2023 growing season (June to October), continuous sap flow monitoring was conducted using thermal dissipation probes (TDPs) on Ulmus pumila L., along with measurements of soil moisture, air temperature, relative humidity, solar radiation, wind speed, and vapor pressure deficit (VPD). The results showed that when the sap flow rate of elm individuals reached 0.92 mL/cm2/h, the trees entered an extremely severe decline stage. Sap flow rates were significantly positively correlated with net solar radiation, relative humidity, VPD, and soil moisture, but negatively correlated with wind speed and real-time rainfall. VPD was identified as the key factor influencing sap flow across different decline stages, while solar radiation was critical in assessing the severity of decline. A weakened correlation between sap flow and solar radiation marked the onset of severe decline. Additionally, soil moisture exhibited a significant positive effect on sap flow rates overall. These findings not only advance our theoretical understanding of plant ecology in arid areas but also offer practical insights for managing Ulmus pumila L. decline, thus contributing to more sustainable resource management and environmental protection strategies. Full article
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Figure 1

Figure 1
<p>The study area in the Mu Us sandy land: (<b>a</b>) the location of the sample area in the Mu Us Desert; (<b>b</b>) satellite image of sample area location; (<b>c</b>) brief introduction of test point layout.</p>
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<p><span class="html-italic">Ulmus pumila</span> L. trees with different degrees of decline.</p>
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<p>TY-TDP needle-inserted plant stem flow measurement system.</p>
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<p>Soil moisture model and monthly variation of soil moisture: (<b>a</b>) the structural relationship between soil layers; (<b>b</b>) soil-water content.</p>
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<p>Changes of soil moisture at different depths after rainfall.</p>
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<p>Changes of daytime sap flow velocity of <span class="html-italic">Ulmus pumila</span> L. trees in four decay degrees.</p>
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<p>The fitting relationship between the sap flow velocity of the four decaying <span class="html-italic">Ulmus pumila</span> L. in the daytime after rain (<span class="html-italic">p</span> &lt; 0.05).</p>
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<p>The nighttime sap flow rate of <span class="html-italic">Ulmus pumila</span> L. in four decay stages.</p>
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<p>Fitting relationship of nocturnal liquid flow rate in four decay stages after rainfall.</p>
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<p>Diurnal variation characteristics of sap flow rate of <span class="html-italic">Ulmus pumila</span> L. in four decline stages: (<b>a</b>) diurnal variation of sap flow of <span class="html-italic">Ulmus pumila</span> L. trees with different decay degrees; (<b>b</b>) diurnal difference of sap flow of <span class="html-italic">Ulmus pumila</span> L. trees with different decay degrees.</p>
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<p>Diurnal variation characteristics of cumulative flow of <span class="html-italic">Ulmus pumila</span> L. in four decay stages: (<b>a</b>) diurnal variation of cumulative sap flow of <span class="html-italic">Ulmus pumila</span> L. with different decay degrees; (<b>b</b>) diurnal difference of cumulative sap flow of <span class="html-italic">Ulmus pumila</span> L. trees with different decay degrees.</p>
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<p>The cumulative flow and the proportion of night flow in the four decay stages: (<b>a</b>) the difference of cumulative flow of <span class="html-italic">Ulmus pumila</span> L. trees with different decay degrees under different weather conditions; (<b>b</b>) ratio of night sap flow to daytime sap flow of <span class="html-italic">Ulmus pumila</span> L. trees with different decay degrees.</p>
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<p>Path analysis of <span class="html-italic">Ulmus pumila</span> L. sap flow and meteorological factors.</p>
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<p>SEM equations of sap flow and meteorological conditions in four decay stages.</p>
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21 pages, 7514 KiB  
Article
Research on Challenges and Strategies for Reservoir Flood Risk Prevention and Control Under Extreme Climate Conditions
by Wenang Hou, Shichen Zhang, Jiangshan Yin and Jianfeng Huang
Water 2024, 16(23), 3351; https://doi.org/10.3390/w16233351 - 22 Nov 2024
Viewed by 268
Abstract
In recent years, reservoir flood control and dam safety have faced severe challenges due to changing environmental conditions and intense human activities. There has been a significant increase in the proportion of dam breaks caused by floods exceeding reservoir design levels. Dam breaks [...] Read more.
In recent years, reservoir flood control and dam safety have faced severe challenges due to changing environmental conditions and intense human activities. There has been a significant increase in the proportion of dam breaks caused by floods exceeding reservoir design levels. Dam breaks have periodically occurred due to flood overtopping, threatening people’s lives and properties. This highlights the importance of describing the challenges encountered in reservoir flood risk prevention and control under extreme climatic conditions and proposing strategies to safeguard reservoirs against floods and to protect downstream communities. This study conducts a statistical analysis of dam breaks resulting from floods exceeding reservoir design levels, revealing new risk indicators in these settings. The study examines recent representative engineering cases involving flood risks and reviews research findings pertaining to reservoir flood risks under extreme climatic conditions. By comparing flood prevention standards at typical reservoirs and investigating the problems and challenges associated with current standards, the study presents the challenges and strategies associated with managing flood risks in reservoirs under extreme climatic conditions. The findings show that the driving forces and their effects shaping flood risk characteristics in specific regions are influenced by atmospheric circulation and vegetative changes in underlying surfaces or land use. There is a clear increasing probability of dam breaks or accidents caused by floods exceeding design levels. Most dam breaks or accidents occur in small and medium-sized reservoirs, due to low flood control standards and poor management. Therefore, this paper recommends measures for improving the flood prevention capacity of these specific types of reservoirs. This paper proposes key measures to cope with floods exceeding reservoir design levels, to supplement the existing standard system. This includes implementing an improved flood standard based on dam risk level and the rapid reduction in the reservoir water level. To prevent breaks associated with overtopping, earth–rock dams should be designed to consider extreme rainfall events. More clarity is needed in the execution principles of flood prevention standards, and the effectiveness of flood calculations should be studied, adjusted, and validated. The research results provide better descriptions of flood risks in reservoirs under extreme climatic conditions, and the proposed strategies have both theoretical and practical implications for building resilience against flood risks and protecting people’s lives and properties. Full article
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<p>Aerial image of the Edenville Dam break [<a href="#B47-water-16-03351" class="html-bibr">47</a>].</p>
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<p>Aerial image of the Sanford Gate Dam.</p>
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<p>Scene of Steinbach Reservoir in Germany after overtopping.</p>
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<p>Downstream dam slope after overtopping of Steinbach Reservoir in Germany.</p>
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<p>Layout of Saddle Dam D.</p>
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<p>Jussiape Dam before break.</p>
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<p>Breaking Jussiape Dam.</p>
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<p>Overtopping and break of Sheyuegou Reservoir.</p>
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<p>Post-break scene of Sheyuegou Reservoir.</p>
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<p>Schematic diagram of typical spatial distribution patterns of cascade reservoir groups.</p>
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<p>Crest hardening ensures “overtopping without breaking”.</p>
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<p>Insufficient downstream dam surface drainage.</p>
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<p>Schematic diagram of reservoir risk classification based on dam height and capacity.</p>
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19 pages, 3805 KiB  
Article
The Impact of Extreme Precipitation on Soil Moisture Transport in Apple Orchards of Varying Ages on the Loess Plateau
by Jialiang Huang, Yi Hua, Yuqing Zhang, Wei Xu, Linyun Gu, Yu Tian, Yi Wu, Quan Long, Haoyan Wei and Min Li
Water 2024, 16(22), 3322; https://doi.org/10.3390/w16223322 - 19 Nov 2024
Viewed by 331
Abstract
The long-term cultivation of apple trees with deep root systems can significantly deplete moisture from the deep soil layers, while extreme rainfall events can rapidly replenish this moisture. Therefore, it is of great academic significance to investigate the influence of extreme precipitation on [...] Read more.
The long-term cultivation of apple trees with deep root systems can significantly deplete moisture from the deep soil layers, while extreme rainfall events can rapidly replenish this moisture. Therefore, it is of great academic significance to investigate the influence of extreme precipitation on soil water dynamics in apple orchards of varying ages. This study was conducted on agricultural land and apple orchards of 12 years, 15 years, 19 years and 22 years (12 y, 15 y, 19 y and 22 y) to examine the impact of extreme precipitation on soil moisture transport. Soil moisture content and hydrogen and oxygen isotope (2H, 18O and 3H) data were collected before (October 2020 and May 2021) and after the extreme precipitation event (May 2022). This comprehensive analysis focuses on two aspects: soil moisture distribution and soil water recharge. The following main conclusions were drawn: (1) Extreme precipitation significantly enhanced deep soil water recharge in apple orchards: the depths of soil water supply for apple orchards of 12 y, 15 y, 19 y and 22 y were recorded as 282 mm, 180 mm, 448 mm and 269 mm, respectively. Correspondingly, the recharge depths were measured at approximately 12, 10, 10 and 7 m, respectively. It was observed that the recharge depth decreased with increasing age of the orchard. (2) Extreme precipitation did not have a significant impact on the values of δ2H and δ18O of deep soil moisture due to a limited infiltration depth through the piston flow mechanism (the maximum infiltration depth being around 3 m). (3) In agricultural land as well as apple orchards of 12 y, 15 y and 22 y in 2020, the tritium peak occurred at soil depths of 7.2, 6.9, 6.7 and 5.7 mm, respectively; in 2022, the corresponding values increased to 7.9, 8.7, 6.7 and 5.9 mm, respectively. This indicates that planting apple trees hindered the transport of soil moisture. The peak concentration of tritium in both agricultural land and different-aged apple orchards decreased after experiencing extreme precipitation. The findings will provide a scientific basis for water resource management and efforts toward ecological restoration on the Loess Plateau. Full article
(This article belongs to the Section Soil and Water)
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Figure 1
<p>Geographical location of the study area and distribution of each sampling point.</p>
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<p>Liquid water laser isotope analyzer.</p>
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<p>Low background liquid scintillation counter.</p>
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<p>The monthly precipitation from 2015 to 2021.</p>
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<p>Autumn rainfall, annual rainfall and proportion from 2015 to 2021.</p>
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<p>Distribution of soil moisture content with depth in agricultural land and orchards of varying ages in 2020, 2021 and 2022.</p>
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<p>Distribution characteristics of δ<sup>2</sup>H of soil moisture with depth in agricultural land and apple orchards of varying ages in 2020, 2021 and 2022.</p>
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<p>Distribution characteristics of soil water isotope δ<sup>18</sup>O with depth in agricultural land and apple orchards of varying ages in 2020, 2021 and 2022.</p>
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<p>Maximum soil water storage and recharge depth in agricultural land and apple orchards of varying ages in 2020 and 2022.</p>
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<p>Differences in soil moisture content of agricultural land and apple orchards of varying ages in 2022 compared with replenishment and consumption in 2020.</p>
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<p>Distribution characteristics of soil water tritium peak with depth in agricultural land and apple orchards of varying ages in 2020 and 2022.</p>
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<p>Distribution characteristics of soil water lc-excess with depth in agricultural land and apple orchards of varying ages in 2020, 2021 and 2022.</p>
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17 pages, 7867 KiB  
Article
The Response of Cloud Precipitation Efficiency to Warming in a Rainfall Corridor Simulated by WRF
by Qi Guo, Yixuan Chen, Xiongyi Miao and Yupei Hao
Atmosphere 2024, 15(11), 1381; https://doi.org/10.3390/atmos15111381 - 16 Nov 2024
Viewed by 260
Abstract
Due to model errors caused by local variations in cloud precipitation processes, there are still significant uncertainties in current predictions and simulations of short-duration heavy rainfall. To tackle this problem, the effects of warming on cloud-precipitation efficiency was analyzed utilizing a weather research [...] Read more.
Due to model errors caused by local variations in cloud precipitation processes, there are still significant uncertainties in current predictions and simulations of short-duration heavy rainfall. To tackle this problem, the effects of warming on cloud-precipitation efficiency was analyzed utilizing a weather research and forecasting (WRF) model. The analysis focused on a rainstorm corridor event that took place in July 2020. Rainstorm events from 4–6 July formed a narrow rain belt with precipitation exceeded 300 mm in the middle and lower reaches of the Yangtze River. Temperature sensitivity tests revealed that warming intensified the potential temperature gradient between north and south, leading to stronger upward motion on the front. It also strengthened the southwest wind, which resulted in more pronounced precipitation peaks. Warming led to a stronger accumulation and release of convective instability energy. Convective available potential energy (CAPE) and convective inhibition (CIN) both increased correspondingly with the temperature. The precipitation efficiency increased sequentially with 2 °C warming to 27.4%, 31.2%, and 33.1%. Warming can affect the cloud precipitation efficiency by both promoting and suppressing convective activity, which may be one of the reasons for the enhancement of extreme precipitation under global warming. The diagnostic relationship between upward moisture flux and lower atmospheric stability during precipitation evolution was also revealed. Full article
(This article belongs to the Section Meteorology)
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<p>Extent of the model’s inner and outer simulation area, topographic height (in m) distribution (<b>a</b>), and observed cumulative precipitation (in mm) for the 4–7 July 2020 precipitation process (<b>b</b>). The black boxes d01 and d02 in the figure indicate the first and second layers of the nested grid areas, respectively. The blue lines represent the Yellow River and the Yangtze River respectively.</p>
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<p>Cumulative precipitation distribution of the observed (OBS_MERG) and WRF simulations (Wrfout_CTL) from 4 July 2020 06:00 to 6 July 2020 18:00 (UTC) (<b>a</b>,<b>b</b>) and the zonal evolution of meridional mean precipitation (<b>c</b>,<b>d</b>), all in mm. The blue lines represent the Yellow River and the Yangtze River respectively.</p>
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<p>Temporal evolution of the mean precipitation (in mm) in the simulated domain of the inner grid d02, black lines are observations, and red lines are WRF simulations. The error bars indicate the regional mean standard deviation.</p>
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<p>Temporal evolution of the 850 hPa meteorological field during the two heavy precipitation events. The brown and blue areas are the ranges of equivalent potential temperatures (in K) exceeding 355 K and below 345 K, respectively. The contours in the figure are the radar reflectivity (in dBZ), and vectors with arrows indicate the horizontal wind field.</p>
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<p>The evolution of meridional vertical profiles for equivalent potential temperature (in K) is depicted by filled colors, and vertical velocity outlined by red contours (intervals of 5 m/s), along with zonal wind speed indicated by black contours with numbers (in m/s), in relation to the precipitation processes during two distinct precipitation events.</p>
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<p>Temporal evolution of mean precipitation (in mm) (<b>a</b>), CAPE (in J/kg) (<b>b</b>), CIN (in J/kg) (<b>c</b>), LCL (in m) (<b>d</b>) and LFC (in m) (<b>e</b>) in the d02 simulated domain for the three sets of temperature sensitivity tests from 4–7 July.</p>
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<p>Temporal evolution of the mean CAPE and CIN vertical profiles in the d02 simulation domain for three sets of temperature sensitivity tests. The filled color represents CAPE, the contour denotes CIN, and the units are all J/kg.</p>
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<p>Same as <a href="#atmosphere-15-01381-f005" class="html-fig">Figure 5</a>, but for the difference between the warming test and the cooling test (T + 2)—(CTL).</p>
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<p>Box chart of precipitation (in mm) (<b>a</b>), total water condensate (in g/kg) (<b>b</b>) and precipitation efficiency (in %) (<b>c</b>) with temperature sensitivity tests in the d02 simulation domain during the first precipitation.</p>
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<p>The box chart of CAPE (in J/kg) (<b>a</b>), CIN (in J/kg) (<b>b</b>), LTS (in K) (<b>c</b>), UMF (in g/m<sup>2</sup>/h) (<b>d</b>), LCL (in m) (<b>e</b>), and LFC (in m) (<b>f</b>) with temperature sensitivity test changes in the inner d02 simulation domain.</p>
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21 pages, 16910 KiB  
Article
Extreme Precipitation Events During the Wet Season of the South America Monsoon: A Historical Analysis over Three Major Brazilian Watersheds
by Aline Araújo de Freitas, Vanessa Silveira Barreto Carvalho and Michelle Simões Reboita
Climate 2024, 12(11), 188; https://doi.org/10.3390/cli12110188 - 15 Nov 2024
Viewed by 432
Abstract
Most of South America, particularly the region between the southern Amazon and southeastern Brazil, as well as a large part of the La Plata Basin, has its climate regulated by the South American Monsoon System. Extreme weather and climate events in these areas [...] Read more.
Most of South America, particularly the region between the southern Amazon and southeastern Brazil, as well as a large part of the La Plata Basin, has its climate regulated by the South American Monsoon System. Extreme weather and climate events in these areas have significant socioeconomic impacts. The Madeira, São Francisco, and Paraná river basins, three major watersheds in Brazil, are especially vulnerable to wet and drought periods due to their importance as freshwater ecosystems and sources of water for consumption, energy generation, and agriculture. The scarcity of surface meteorological stations in these basins makes meteorological studies challenging, often using reanalysis and satellite data. This study aims to identify extreme weather (wet) and climate (wet and drought) events during the extended wet season (October to March) from 1980 to 2022 and evaluate the performance of two gridded datasets (CPC and ERA5) to determine which best captures the observed patterns in the Madeira, São Francisco, and Paraná river basins. Wet weather events were identified using the 95th percentile, and wet and drought periods were identified using the Standardized Precipitation Index (SPI) on a 6-month scale. In general, CPC data showed slightly superior performance compared to ERA5 in reproducing statistical measures. For extreme day precipitation, both datasets captured the time series pattern, but CPC better reproduced extreme values and trends. The results also indicate a decrease in wet periods and an increase in drought events. Both datasets performed well, showing they can be used in the absence of station data. Full article
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<p>Representation of the study area with a zoom on the basins that were analyzed and the locations of the pluviometric stations used. The number of stations in each basin is also indicated in the figure in parentheses.</p>
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<p>Flowchart summarizing the steps of the analyses performed in this article.</p>
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<p>Analysis for the MRB: climatology of accumulated precipitation for the rainy season (October to March) for (<b>a</b>) CPC and (<b>b</b>) ERA5; (<b>c</b>) statistical analysis based on daily data; (<b>d</b>) monthly climatology; and (<b>e</b>) annual accumulation. In (<b>d</b>,<b>e</b>), the ERA5 database is indicated in green, the CPC is indicated in blue, and the observations are shown in black. Regions I, II and III indicate the Upper, Middle and Lower Madeira regions, respectively.</p>
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<p>Statistical analysis based on daily data, monthly climatology, and annual accumulation for 2 stations in Upper Madeira: (<b>a</b>) 1559000 and (<b>b</b>) 1560000. The ERA5 database is indicated in green, the CPC is indicated in blue, and the observations are shown in black.</p>
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<p>Analysis for the PRB: climatology of accumulated precipitation for the rainy season (October to March) for (<b>a</b>) CPC and (<b>b</b>) ERA5; (<b>c</b>) statistical analysis based on daily data; (<b>d</b>) monthly climatology; and (<b>e</b>) annual accumulation. In (<b>d</b>,<b>e</b>), the ERA5 database is indicated in green, the CPC is indicated in blue, and the observations are shown in black. Regions I, II, III, IV, V, and VI indicate the Paranaíba, Grande, Tietê, Paraná, Paranapanema, and Iguaçu regions.</p>
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<p>Analysis for the SFRB: climatology of accumulated precipitation for the rainy season (October to March) for (<b>a</b>) CPC and (<b>b</b>) ERA5; (<b>c</b>) statistical analysis based on daily data; (<b>d</b>) monthly climatology; and (<b>e</b>) annual accumulation. In (<b>d</b>,<b>e</b>), the ERA5 database is indicated in green, the CPC is indicated in blue, and the observations are shown in black. Regions I, II, III, and IV indicate the Upper, Middle, Sub-Middle, and Lower São Francisco regions.</p>
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<p>P95 values (precipitation in mm) identified by the ANA, CPC, and ERA5 datasets considering the average in the basins and for each of the subregions. The ERA5 database is indicated in green, the CPC in blue and the observations are shown in red.</p>
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<p>Number of days with extreme precipitation higher than P95 identified by the ANA, CPC, and ERA5 datasets in the MRB regions between 1980 and 2022: (<b>a</b>) entire basin; (<b>b</b>) Upper; (<b>c</b>) Middle; and (<b>d</b>) Lower. In some figures, the means of the datasets are quite close, which causes the black line representing the average to appear as a single line. The ERA5 database is indicated in green, the CPC is indicated in blue, and the observations are shown in red.</p>
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<p>Number of days with extreme precipitation higher than P95 identified by the ANA, CPC, and ERA5 datasets in the PRB regions between 1980 and 2022: (<b>a</b>) entire basin; (<b>b</b>) Paranaíba; (<b>c</b>) Grande; (<b>d</b>) Tietê; (<b>e</b>) Paraná; (<b>f</b>) Paranapanema; (<b>g</b>) and Iguaçu. In some figures, the means of the datasets are quite close, which causes the black line representing the average to appear as a single line. The ERA5 database is indicated in green, the CPC is indicated in blue, and the observations are shown in red.</p>
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<p>Number of days with extreme precipitation higher than P95 identified by the ANA, CPC, and ERA5 datasets in the SFRB regions between 1980 and 2022: (<b>a</b>) entire basin; (<b>b</b>) Upper; (<b>c</b>) Middle; (<b>d</b>) Sub-Middle; and (<b>e</b>) Lower. In some figures, the means of the datasets are quite close, which causes the black line representing the average to appear as a single line. The ERA5 database is indicated in green, the CPC is indicated in blue, and the observations are shown in red.</p>
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<p>March SPI-6 for the MRB considering the datasets (<b>a</b>) ANA, (<b>b</b>) CPC, and (<b>c</b>) ERA5.</p>
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<p>March SPI-6 for the PRB considering the datasets (<b>a</b>) ANA, (<b>b</b>) CPC, and (<b>c</b>) ERA5.</p>
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<p>March SPI-6 for the SFRB considering the datasets (<b>a</b>) ANA, (<b>b</b>) CPC, and (<b>c</b>) ERA5.</p>
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<p>Summary of all analyses performed and which database presented the best results, considering the basin as a whole and the subregions of MRB, PRB, and SFRB.</p>
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22 pages, 3255 KiB  
Article
Classification Importance of Seed Morphology and Insights on Large-Scale Climate-Driven Strophiole Size Changes in the Iberian Endemic Chasmophytic Genus Petrocoptis (Caryophyllaceae)
by Jorge Calvo-Yuste, Ángela Lis Ruiz-Rodríguez, Brais Hermosilla, Agustí Agut, María Montserrat Martínez-Ortega and Pablo Tejero
Plants 2024, 13(22), 3208; https://doi.org/10.3390/plants13223208 - 15 Nov 2024
Viewed by 351
Abstract
Recruitment poses significant challenges for narrow endemic plant species inhabiting extreme environments like vertical cliffs. Investigating seed traits in these plants is crucial for understanding the adaptive properties of chasmophytes. Focusing on the Iberian endemic genus Petrocoptis A. Braun ex Endl., a strophiole-bearing [...] Read more.
Recruitment poses significant challenges for narrow endemic plant species inhabiting extreme environments like vertical cliffs. Investigating seed traits in these plants is crucial for understanding the adaptive properties of chasmophytes. Focusing on the Iberian endemic genus Petrocoptis A. Braun ex Endl., a strophiole-bearing Caryophyllaceae, this study explored the relationships between seed traits and climatic variables, aiming to shed light on the strophiole’s biological role and assess its classificatory power. We analysed 2773 seeds (557 individuals) from 84 populations spanning the genus’ entire distribution range. Employing cluster and machine learning algorithms, we delineated well-defined morphogroups based on seed traits and evaluated their recognizability. Linear mixed-effects models were utilized to investigate the relationship between climate predictors and strophiole area, seed area and the ratio between both. The combination of seed morphometric traits allows the division of the genus into three well-defined morphogroups. The subsequent validation of the algorithm allowed 87% of the seeds to be correctly classified. Part of the intra- and interpopulation variability found in strophiole raw and relative size could be explained by average annual rainfall and average annual maximum temperature. Strophiole size in Petrocoptis could have been potentially driven by adaptation to local climates through the investment of more resources in the production of bigger strophioles to increase the hydration ability of the seed in dry and warm climates. This reinforces the idea of the strophiole being involved in seed water uptake and germination regulation in Petrocoptis. Similar relationships have not been previously reported for strophioles or other analogous structures in Angiosperms. Full article
(This article belongs to the Section Plant Ecology)
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<p>Cluster grouping of 84 populations of <span class="html-italic">Petrocoptis</span> A. Braun ex Endl. following k-means algorithm based on 9 morphological seed traits. Colours depict prior identification following the taxonomic proposal by Montserrat &amp; Fernández-Casas [<a href="#B39-plants-13-03208" class="html-bibr">39</a>], and symbol shapes indicate seed morphogroups: circles, cluster a; triangles, cluster b; squares, cluster c.</p>
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<p>Comparison among the three k-means morphogroups (a, b and c), indicating the distribution, mean values and standard deviation of seed area (<b>left</b>), strophiole area (<b>center</b>) and strophiole relative size (<b>right</b>). Red dots indicate mean values and grey bars indicate median values. Every Games–Howell pairwise test showed significant differences.</p>
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<p>Partial dependence plots of the three morphogroups (a, b and c), based on seed area, strophiole area and strophiole relative size for the seed morphology data, derived from support vector machine (svm) algorithm. Colours depict the predicted classification probabilities of a <span class="html-italic">Petrocoptis</span> seed within a given group based on its morphological traits of interest. C and gamma hyperparameters were set as default: C = 1; γ = 1/(data dimension). Values are restricted to lie within the convex hull of their training values in order to avoid extrapolation.</p>
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<p>Distribution of observed data values and best-fitted linear mixed-effects models (lme) between climate variables and strophiole area (<b>up</b>) and strophiole relative size (<b>down</b>). Coloured X-axis is adjusted to show its original scale (prior standardization) for illustrative purposes.</p>
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<p>Mean variable importance of best-fitted linear mixed-effects models of strophiole area (<b>up</b>) and strophiole relative size (<b>down</b>). Dotted lines indicate RMSE value of the full models, and bars depict RMSE loss when removing one variable at a time. RMSE loss was calculated after 50 permutations. Variables included: nested population and individual levels (pop:ind), average annual rainfall (rainfall) and average annual maximum temperature (tmax).</p>
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<p>Geographic distribution of the <span class="html-italic">Petrocoptis</span> sampled populations. Symbol shapes indicate seed morphogroups (see <a href="#sec2-plants-13-03208" class="html-sec">Section 2</a> and <a href="#plants-13-03208-f001" class="html-fig">Figure 1</a>: circles, cluster a; triangles, cluster b; squares, cluster c) and colours depict prior identification following the taxonomic proposal by Montserrat &amp; Fernández Casas [<a href="#B39-plants-13-03208" class="html-bibr">39</a>]. Population codes follow <a href="#app1-plants-13-03208" class="html-app">Table S1</a>.</p>
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<p><span class="html-italic">Petrocoptis</span> seed traits of interest.</p>
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20 pages, 7069 KiB  
Article
The Development of a Hydrological Method for Computing Extreme Hydrographs in Engineering Dam Projects
by Oscar E. Coronado-Hernández, Vicente S. Fuertes-Miquel and Alfonso Arrieta-Pastrana
Hydrology 2024, 11(11), 194; https://doi.org/10.3390/hydrology11110194 - 15 Nov 2024
Viewed by 384
Abstract
Engineering dam projects benefit society, including hydropower, water supply, agriculture, and flood control. During the planning stage, it is crucial to calculate extreme hydrographs associated with different return periods for spillways and diversion structures (such as tunnels, conduits, temporary diversions, multiple-stage diversions, and [...] Read more.
Engineering dam projects benefit society, including hydropower, water supply, agriculture, and flood control. During the planning stage, it is crucial to calculate extreme hydrographs associated with different return periods for spillways and diversion structures (such as tunnels, conduits, temporary diversions, multiple-stage diversions, and cofferdams). In many countries, spillways have return periods ranging from 1000 to 10,000 years, while diversion structures are designed with shorter return periods. This study introduces a hydrological method based on data from large rivers which can be used to compute extreme hydrographs for different return periods in engineering dam projects. The proposed model relies solely on frequency analysis data of peak flow, base flow, and water volume for various return periods, along with recorded maximum hydrographs, to compute design hydrographs associated with different return periods. The proposed method is applied to the El Quimbo Hydropower Plant in Colombia, which has a drainage area of 6832 km2. The results demonstrate that this method effectively captures peak flows and evaluates hydrograph volumes and base flows associated with different return periods, as a Root Mean Square Error of 11.9% of the maximum volume for various return periods was achieved during the validation stage of the proposed model. A comprehensive comparison with the rainfall–runoff method is also provided to evaluate the relative magnitudes of the various variables analysed, ensuring a thorough and reliable assessment of the proposed method. Full article
(This article belongs to the Special Issue Hydrological Modeling and Sustainable Water Resources Management)
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<p>Location of case study.</p>
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<p>Methodology used in research.</p>
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<p>Used variables for proposed model.</p>
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<p>Proposed dimensionless hydrograph.</p>
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<p>Rainfall–runoff models employed in research.</p>
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<p>Computation of extreme variables for various return periods: (<b>a</b>) peak flow, (<b>b</b>) 48 h volume, (<b>c</b>) and base flow.</p>
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<p>The results of the proposed model: (<b>a</b>) recorded and average hydrographs; (<b>b</b>) design hydrographs for various return periods.</p>
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<p>Comparison between modelled and recorded hydrograph volumes using hydrometric models.</p>
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<p>Isohyetal maps of daily maximum precipitation for return periods: (<b>a</b>) 10,000 years; (<b>b</b>) 2000 years; (<b>c</b>) 1000 years; (<b>d</b>) 200 years; (<b>e</b>) 100 years; (<b>f</b>) 50 years; (<b>g</b>) 20 years; (<b>h</b>) 10 years; and (<b>i</b>) 5 years.</p>
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<p>Comparison of shapes of design hydrographs for different hydrological methods.</p>
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<p>Sensitivity analysis of peak time for proposed model.</p>
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23 pages, 22588 KiB  
Article
Monitoring Dissolved Organic Carbon Concentration and Flux in the Qiantang Riverine System Using Sentinel-2 Satellite Images
by Yujia Yan, Xianqiang He, Yan Bai, Jinsong Liu, Palanisamy Shanmugame, Yaqi Zhao, Xuan Zhang, Zhihong Wang, Yifan Zhang and Fang Gong
Remote Sens. 2024, 16(22), 4254; https://doi.org/10.3390/rs16224254 - 15 Nov 2024
Viewed by 576
Abstract
Real-time monitoring of riverine-dissolved organic carbon (DOC) and its controlling factors is critical for formulating strategies regarding the river basin and marginal seas pollution prevention and control. In this study, we established a linear regression formulation that relates the permanganate index (CODMn [...] Read more.
Real-time monitoring of riverine-dissolved organic carbon (DOC) and its controlling factors is critical for formulating strategies regarding the river basin and marginal seas pollution prevention and control. In this study, we established a linear regression formulation that relates the permanganate index (CODMn) to the DOC concentration based on in situ measurements collected on five field surveys in 2023–2024. This regression formulation was used on a large number of data collected from automatic monitoring stations in the Qiantang River area to construct a daily quasi-in situ database of DOC concentration. By combining the quasi-in situ DOC data and Sentinel-2 measurements, an enhanced algorithm for empirical DOC estimation was developed (R2 = 0.66) using the extreme gradient boosting (XGBoost) method and its spatial and temporal variations in the Qiantang River were analyzed from 2016 to 2023. Spatially, the main stream of the Qiantang River exhibited an overall decreasing and increasing trend influenced by population density, economic development, and pollutant discharge in the basin area, and the temporal distribution of DOC was controlled by meteorological conditions. The DOC contents had the highest in summer, primarily due to high rainfall and leaching. The inter-annual variation in DOC concentration was influenced by the total annual runoff volumes, with a minimum level of 2.24 mg L−1 in 2023 and a maximum level of 2.45 mg L−1 in 2019. The monthly DOC fluxes ranged from 6.3 to 13.8 × 104 t, with the highest values coinciding with the maximum river discharge volumes in June and July. The DOC levels in the Qiantang River remained relatively high in recent years (2016–2023). This study enables the concerned stakeholders and researchers to better understand carbon transportation and its dynamics in the Qiantang River and its coastal areas. Full article
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<p>The spatial distribution of the Qiantang River, monitoring stations, and Zhijiang station. (<b>a</b>) Spatial distribution of the Qiantang River in Zhejiang Province, China. The pink area represents the Zhejiang Province. (<b>b</b>) Four sections of the Qiantang River. (<b>c</b>) Spatial distribution and the number of monitoring stations. (<b>d</b>) Spatial distribution of Zhijiang station and nearby field sampling stations (the pinkish-red point represents the sampling station in December 2023 and the green point represents the sampling station in March 2024). The digital elevation model (DEM) data were derived from the Geospatial Data Cloud site, Computer Network Information Center, Chinese Academy of Sciences (<a href="http://www.gscloud.cn" target="_blank">http://www.gscloud.cn</a>, assessed on 30 May 2024).</p>
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<p>The spatial distribution of the field sampling stations.</p>
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<p>Flowchart of the methodology for estimating DOC concentration and flux.</p>
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<p>The relationship between the measured permanganate index and dissolved organic carbon based on in situ measurement data.</p>
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<p>Ranks of feature importance for XGBoost model.</p>
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<p>Scatterplots of the dataset. (<b>a</b>) training dataset, (<b>b</b>) validation dataset, and (<b>c</b>) test dataset.</p>
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<p>Comparison of time series DOC concentrations from the retrieval model and quasi-realistic datasets at six monitoring stations. The red points represent the modeled data, and the green points represent the independent test data. (<b>a</b>) Station2; (<b>b</b>) Station9; (<b>c</b>) Station13; (<b>d</b>) Station14; (<b>e</b>) Station18; and (<b>f</b>) Station23.</p>
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<p>The dynamic range and mean values of DOC concentration obtained from quasi-in situ data and the retrieval model at 31 monitoring stations.</p>
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<p>The spatial distribution of DOC concentration in the main stream and some tributaries of the Qiantang River. (<b>a</b>) Annual average; (<b>b</b>) the changes of DOC along Zone 1, Zone 2, and Zone 4; (<b>c</b>) spring (March to May); (<b>d</b>) summer (June to August); (<b>e</b>) autumn (September to November); and (<b>f</b>) winter (December to February).</p>
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<p>(<b>a</b>) Districts boundaries, (<b>b</b>) population density, GDP, COD<sub>Cr</sub> emissions, farmland area, and fertilizer application as the percentage of the sum of all districts. Data are derived from the Zhejiang Provincial Bureau of Statistics 2023.</p>
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<p>Temporal changes in DOC concentration. (<b>a</b>) Mean values of DOC concentrations in the whole Qiantang River and four zones in each season; (<b>b</b>) annual variation in DOC concentration during 2016–2023.</p>
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<p>(<b>a</b>) Annual DOC levels and total annual runoff volumes from 2016 to 2022; (<b>b</b>) a relationship between DOC flux and discharge data.</p>
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<p>Temporal changes in DOC flux. (<b>a</b>) Monthly change; (<b>b</b>) annual change; and (<b>c</b>) seasonal change.</p>
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24 pages, 4650 KiB  
Article
Passenger Flow Prediction for Rail Transit Stations Based on an Improved SSA-LSTM Model
by Xing Zhao, Chenxi Li, Xueting Zou, Xiwang Du and Ahmed Ismail
Mathematics 2024, 12(22), 3556; https://doi.org/10.3390/math12223556 - 14 Nov 2024
Viewed by 365
Abstract
Accurate and timely passenger flow prediction is important for the successful deployment of rail transit intelligent operation. The Sparrow Search Algorithm (SSA) has been applied to the parameter optimization of a Long-Short-Term Memory (LSTM) model. To solve the inherent weaknesses of SSA, this [...] Read more.
Accurate and timely passenger flow prediction is important for the successful deployment of rail transit intelligent operation. The Sparrow Search Algorithm (SSA) has been applied to the parameter optimization of a Long-Short-Term Memory (LSTM) model. To solve the inherent weaknesses of SSA, this paper proposes an improved SSA-LSTM model with optimization strategies including Tent Map and Levy Flight to practice the short-term prediction of boarding passenger flow at rail transit stations. Aimed at the passenger flow at four rail transit stations in Nanjing, China, it is found that the day of a week and rainfall are the influencing factors with the highest correlation. On this basis, we apply the proposed SSA-LSTM and four baseline models to realize the short-term prediction, and carry out the prediction experiments with different time granularities. According to the experimental results, the proposed SSA-LSTM model has a more effective performance than the Support Vector Regression (SVR) method, the eXtreme Gradient Boosting (XGBoost) model, the traditional LSTM model, and the improved LSTM model with the Whale Optimization Algorithm (WOA-LSTM) in the passenger flow prediction. In addition, for most stations, the prediction accuracy of the proposed SSA-LSTM model is greater at a larger time granularity, but there are still exceptions. Full article
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<p>Architecture of an LSTM cell.</p>
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<p>Framework of the proposed SSA-LSTM model.</p>
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<p>Example of the optimization procedure for Tent-Levy-SSA.</p>
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<p>Nanjing rail system and passenger flow thermodynamic diagram (In 2017).</p>
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<p>Daily boarding passenger flow at the stations in October 2017.</p>
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<p>Temporal patterns of boarding passenger flow on different days at the stations.</p>
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<p>Temporal patterns of boarding passenger flow on different days at the stations.</p>
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<p>Temporal patterns of boarding passenger flow on different days at the stations.</p>
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<p>Temporal patterns of boarding passenger flow on different days at the stations.</p>
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<p>Prediction results of boarding passenger flow at stations with 10 min time granularity.</p>
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<p>Prediction results of boarding passenger flow at stations with 10 min time granularity.</p>
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13 pages, 2987 KiB  
Article
Evaluation of the Hydrological Response to Land Use Change Scenarios in Urban and Non-Urban Mountain Basins in Ecuador
by Diego Mejía-Veintimilla, Pablo Ochoa-Cueva and Juan Arteaga-Marín
Land 2024, 13(11), 1907; https://doi.org/10.3390/land13111907 - 14 Nov 2024
Viewed by 330
Abstract
Land cover is a crucial factor in controlling rainfall–runoff processes in mountain basins. However, various anthropogenic activities, such as converting natural vegetation to agricultural or urban areas, can affect this cover, thereby increasing the risk of flooding in cities. This study evaluates the [...] Read more.
Land cover is a crucial factor in controlling rainfall–runoff processes in mountain basins. However, various anthropogenic activities, such as converting natural vegetation to agricultural or urban areas, can affect this cover, thereby increasing the risk of flooding in cities. This study evaluates the hydrological behavior of two mountain basins in Loja, Ecuador, under varying land use scenarios. El Carmen small basin (B1), located outside the urban perimeter, and Las Pavas small basin (B2), within the urban area, were modeled using HEC-HMS 4.3 software. The results highlight the significant influence of vegetation degradation and restoration on hydrological processes. In degraded vegetation scenarios, peak flows increase due to reduced soil infiltration capacity, while baseflows decrease. Conversely, the conserved and restored vegetation scenarios show lower peak flows and higher baseflows, which are attributed to enhanced evapotranspiration, interception, and soil water storage. The study underscores the importance of ecosystem management and restoration in mitigating extreme hydrological events and improving water resilience. These findings provide a foundation for decision-making in urban planning and basin management, emphasizing the need for comprehensive and multidisciplinary approaches to develop effective public policies. Full article
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<p>Location map and average monthly distribution of temperature and precipitation of the study area.</p>
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<p>Selected precipitation events and hydrographs for hydrological modeling of the B1.</p>
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<p>Current and future hypothetical land cover scenarios. (<b>a</b>,<b>b</b>) El Carmen (B1). (<b>c</b>,<b>d</b>) Las Pavas (B2).</p>
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<p>Gauged and simulated flows under the LULC scenarios for basins B1 and B2.</p>
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<p>Box plot for scenario-specific flow rates.</p>
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19 pages, 4217 KiB  
Article
Midge Paleo-Communities (Diptera Chironomidae) as Indicators of Flood Regime Variations in a High-Mountain Lake (Italian Western Alps): Implications for Global Change
by Marco Bertoli, Gianguido Salvi, Rachele Morsanuto, Elena Pavoni, Paolo Pastorino, Giuseppe Esposito, Damià Barceló, Marino Prearo and Elisabetta Pizzul
Diversity 2024, 16(11), 693; https://doi.org/10.3390/d16110693 - 12 Nov 2024
Viewed by 381
Abstract
Sediments of alpine lakes serve as crucial records that reveal the history of lacustrine basins, offering valuable insights into the effects of global changes. One significant effect is the variation in rainfall regimes, which can substantially influence nutrient loads and sedimentation rates in [...] Read more.
Sediments of alpine lakes serve as crucial records that reveal the history of lacustrine basins, offering valuable insights into the effects of global changes. One significant effect is the variation in rainfall regimes, which can substantially influence nutrient loads and sedimentation rates in lacustrine ecosystems, thereby playing a pivotal role in shaping biotic communities. In this study, we analyze subfossil chironomid assemblages within a sediment core from an alpine lake (western Italian Alps) to investigate the effects of rainfall and flood regime variations over the past 1200 years. Sediment characterization results highlight changes in sediment textures and C/N ratio values, indicating phases of major material influx from the surrounding landscape into the lake basin. These influxes are likely associated with intense flooding events linked to heavy rainfall periods over time. Flooding events are reflected in changes in chironomid assemblages, which in our samples are primarily related to variations in sediment texture and nutrient loads from the surrounding landscape. Increased abundances of certain taxa (i.e., Brillia, Chaetocladius, Cricotopus, Psectrocladius, Cricotopus/Orthocladius Parorthocladius) may be linked to higher organic matter and vegetation inputs from the surrounding landscape. Biodiversity decreased during certain periods along the core profile due to intense flood regimes and extreme events. These results contribute to our understanding of alpine lake system dynamics, particularly those associated with intense flooding events, which are still understudied. Full article
(This article belongs to the Section Biodiversity Loss & Dynamics)
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<p>(<b>a</b>) Study area and (<b>b</b>) location of the sampling site in Upper Balma Lake.</p>
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<p>Stratigraphic diagram of the sedimentological and geochemical parameters measured in core sections sampled in the Upper Balma Lake. Results of the element analysis in light blue color are also reported.</p>
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<p>Bayesian age-depth model calculated for the Upper Balma Lake, based on 4000 interactions Markov Chain Monte Carlo. The dark gray areas represent the more precise dates, those in light gray the less precise dates; the red line indicates the best estimate of age for each level, and the black dashed lines the 95% confidence intervals.</p>
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<p>Relative abundances of the chironomid taxa observed in the Upper Balma Lake core sections and trends of the main community indices calculated along the core. Time periods with high flood regimes are indicated by the light blue bands superimposed on the graphs; identification of these periods is based on Giguet-Covex et al. [<a href="#B8-diversity-16-00693" class="html-bibr">8</a>] and Wilhelm et al. [<a href="#B55-diversity-16-00693" class="html-bibr">55</a>]. Group colors highlighted by cluster analysis and used in the RDA are reported (see <a href="#diversity-16-00693-f005" class="html-fig">Figure 5</a> and <a href="#diversity-16-00693-f006" class="html-fig">Figure 6</a>a).</p>
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<p>Cluster analysis defining stratigraphic zones (groups of sections) along the core based on the chironomid assemblages in the Upper Balma Lake (<b>a</b>) and broken sticks analysis defining the proper number of groups (<b>b</b>) (<span class="html-italic">n</span> = 6). Obtained stratigraphic zones are indicated with the same colors used for RDA analysis (see <a href="#diversity-16-00693-f006" class="html-fig">Figure 6</a>a).</p>
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<p>(<b>a</b>) Redundancy Analyses (RDA) illustrate the associations between chironomid taxa and the variables under consideration and (<b>b</b>) Venn diagrams depict the results of variance partitioning analysis (VPA) for the four variable groups: nutrients (TOC and C/N ratio), trace elements (Pb, Mo), sediment characteristics (first percentile Cμ and median diameter Mμ), and the presence of fish in relation to chironomid taxa. Variance that is unexplained or accounts for less than 1% is omitted. The group colors used in the RDA analysis correspond to those in the cluster analysis (refer to <a href="#diversity-16-00693-f005" class="html-fig">Figure 5</a>).</p>
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25 pages, 11175 KiB  
Article
Performance Evaluation of Satellite Precipitation Products During Extreme Events—The Case of the Medicane Daniel in Thessaly, Greece
by Dimitrios Katsanos, Adrianos Retalis, John Kalogiros, Basil E. Psiloglou, Nikolaos Roukounakis and Marios Anagnostou
Remote Sens. 2024, 16(22), 4216; https://doi.org/10.3390/rs16224216 - 12 Nov 2024
Viewed by 330
Abstract
Mediterranean tropical-like cyclones, or Medicanes, present unique challenges for precipitation estimations due to their rapid development and localized impacts. This study evaluates the performance of satellite precipitation products in capturing the precipitation associated with Medicane Daniel that struck Greece in early September 2023. [...] Read more.
Mediterranean tropical-like cyclones, or Medicanes, present unique challenges for precipitation estimations due to their rapid development and localized impacts. This study evaluates the performance of satellite precipitation products in capturing the precipitation associated with Medicane Daniel that struck Greece in early September 2023. Utilizing a combination of ground-based observations, reanalysis, and satellite-derived precipitation data, we assess the accuracy and spatial distribution of the satellite precipitation products GPM IMERG, GSMaP, and CMOPRH during the cyclone event, which formed in the Eastern Mediterranean from 4 to 7 September 2023, hitting with unprecedented, enormous amounts of rainfall, especially in the region of Thessaly in central Greece. The results indicate that, while satellite precipitation products demonstrate overall skill in capturing the broad-scale precipitation patterns associated with Medicane Daniel, discrepancies exist in estimating localized intense rainfall rates, particularly in convective cells within the cyclone’s core. Indeed, most of the satellite precipitation products studied in this work showed a misplacement of the highest amounts of associated rainfall, a significant underestimation of the event, and large unbiased root mean square error in the areas of heavy precipitation. The total precipitation field from IMERG Late Run and CMORPH showed the smallest bias (but significant) and good temporal correlation against rain gauges and ERA5-Land reanalysis data as a reference, while IMERG Final Run and GSMaP showed the largest underestimation and overestimation, respectively. Further investigation is needed to improve the representation of extreme precipitation events associated with tropical-like cyclones in satellite precipitation products. Full article
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<p>Global Forecast System (GFS) reanalysis of 500 hpa geopotential height during 4–7 September 2023 (dates are shown in images), available at <a href="https://www.wetterzentrale.de/de/reanalysis.php?model=cfsr" target="_blank">https://www.wetterzentrale.de/de/reanalysis.php?model=cfsr</a> (accessed on 12 March 2024).</p>
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<p>Satellite images of the evolution (4 and 5 September 2023, upper left and right; 6 and 7 September 2023, lower left and right) of Medicane Daniel (Meteosat SEVIRI), available at <a href="https://pics.eumetsat.int/viewer/index.html" target="_blank">https://pics.eumetsat.int/viewer/index.html</a> (accessed on 21 July 2024).</p>
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<p>Sea surface temperature from 3 to 6 September 2023 according to Copernicus Marine Data, available at <a href="https://data.marine.copernicus.eu/product/SST_MED_SST_L3S_NRT_OBSERVATIONS_010_012" target="_blank">https://data.marine.copernicus.eu/product/SST_MED_SST_L3S_NRT_OBSERVATIONS_010_012</a> (accessed on 12 March 2024).</p>
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<p>Comparison of total accumulated rainfall from (<b>a</b>) ERA5-Land and (<b>b</b>) XPOL radar for the time period and the area of radar operation, and (<b>c</b>) scatter plot of daily accumulated rainfall from ERA5-Land and XPOL radar. The red line is the equality line.</p>
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<p>Accumulated rainfall from (<b>a</b>) ERA5-Land and (<b>b</b>) ERA5 in the region of Thessaly in the time period of operation of the XPOL radar.</p>
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<p>(<b>a</b>) Observed flood extent and (<b>b</b>) water extent on 10 September 2023 in the region of Thessaly. Data are from Copernicus Emergency Management Service (©2024 European Union), event EMSR962, based on GeoEye-1/VHR2 satellite data (accessed on 24 April 2024).</p>
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<p>Location of weather stations used in the study and cities/areas affected by Medicane Daniel (water extent on 10 September 2023 shown with light blue line).</p>
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<p>Cumulative rainfall and 10 min precipitation rate recorded by NOA stations during the event, calculated from high-resolution 1 min measurements.</p>
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<p>Cumulative rainfall and 30 min precipitation rate of TOEV stations during the event.</p>
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<p>Spatial distribution of IMERG (version 07B), GSMaP (version 8), CMOPRH (version 2.0), and ERA5-Land total accumulated precipitation during the event.</p>
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<p>Spatial distribution of IMERG (version 07B), GSMaP (version 8), CMOPRH (version 2.0), and ERA5-Land total accumulated precipitation during the event.</p>
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<p>Same as <a href="#remotesensing-16-04216-f010" class="html-fig">Figure 10</a>, but for IMERG L version 06D and CMORPH version 1.0.</p>
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<p>Thirty-minute cumulative precipitation for the Klokotos, Larissa, and Stavros stations, CMORPH, GSMap, IMERG, and ERA5-Land, during the event. The results for the rest of TOEV stations are similar to those obtained by Stavros station (see <a href="#remotesensing-16-04216-f009" class="html-fig">Figure 9</a>).</p>
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<p>Spatial distribution of relative bias between the satellite precipitation products and ERA5-Land.</p>
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<p>Spatial distribution of unbiased RMSE between the satellite precipitation products and ERA5-Land.</p>
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<p>Spatial distribution of unbiased RMSE between the satellite precipitation products and ERA5-Land.</p>
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<p>Spatial distribution of temporal correlation between the satellite precipitation products and ERA5-Land.</p>
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<p>Spatial distribution of temporal correlation between the satellite precipitation products and ERA5-Land.</p>
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18 pages, 3729 KiB  
Article
Wildlife Tourism and Climate Change: Perspectives on Maasai Mara National Reserve
by Catherine Muyama Kifworo and Kaitano Dube
Climate 2024, 12(11), 185; https://doi.org/10.3390/cli12110185 - 11 Nov 2024
Viewed by 732
Abstract
The impact of climate change on nature-based tourism is gaining significance. This study evaluated the impacts of climate change and tourism stakeholders’ perspectives on the subject in the Maasai Mara National Reserve and World Heritage Site. Surveys and interviews were used to collect [...] Read more.
The impact of climate change on nature-based tourism is gaining significance. This study evaluated the impacts of climate change and tourism stakeholders’ perspectives on the subject in the Maasai Mara National Reserve and World Heritage Site. Surveys and interviews were used to collect data. The main climate-related threats to tourism were heavy rain, floods, and extreme droughts. These events adversely impacted infrastructure, such as roads, bridges, and accommodation facilities, and outdoor tourism activities, such as game viewing, cultural tours, birdwatching, and hot air ballooning. They also exacerbated human–wildlife conflicts. The key challenges identified in dealing with impacts were poor planning, non-prioritizing climate change as a threat, a lack of expertise, inadequate research, and a lack of internal early warning systems. The key recommendations included prioritization of climate change planning, development of internal early warning systems, and building resilience toward climate-related disasters. This study contributes to practice by making recommendations for management and other stakeholders. It also extends the discussions of climate change and tourism to wildlife tourism destinations in Africa. Full article
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<p>Map location of Maasai Mara Game Reserve.</p>
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<p>Stakeholders’ familiarity with climate change: data from questionnaire survey.</p>
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<p>Rainfall trend for Maasai Mara between 1981 and 2022.</p>
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<p>Monthly rainfall pattern for the Maasai Mara Nature Reserve in 1981–2020.</p>
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<p>Time series analysis of daily precipitation for Maasai Mara corrected from 1982 to 2023.</p>
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<p>Time series analysis of daily temperature for Maasai Mara corrected in the period of 1982–2023.</p>
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<p>Potential risks of Maasai Mara to various extreme weather events: data from questionnaire surveys.</p>
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<p>Infrastructure damage by extreme weather events: data from questionnaire surveys.</p>
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<p>Activities interrupted by extreme weather events: data from questionnaire surveys.</p>
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<p>Socio-economic impacts of extreme weather events.</p>
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29 pages, 17765 KiB  
Article
Trends of Climate Extremes and Their Relationships with Tropical Ocean Temperatures in South America
by Luiz Octávio Fabrício dos Santos, Nadja Gomes Machado, Carlos Alexandre Santos Querino and Marcelo Sacardi Biudes
Earth 2024, 5(4), 844-872; https://doi.org/10.3390/earth5040043 - 11 Nov 2024
Viewed by 398
Abstract
South America has experienced significant changes in climate patterns over recent decades, particularly in terms of precipitation and temperature extremes. This study analyzes trends in climate extremes from 1979 to 2020 across South America, focusing on their relationships with sea surface temperature (SST) [...] Read more.
South America has experienced significant changes in climate patterns over recent decades, particularly in terms of precipitation and temperature extremes. This study analyzes trends in climate extremes from 1979 to 2020 across South America, focusing on their relationships with sea surface temperature (SST) anomalies in the Pacific and Atlantic Oceans. The analysis uses precipitation and temperature indices, such as the number of heavy rainfall days (R10mm, R20mm, R30mm), total annual precipitation (PRCPTOT), hottest day (TXx), and heatwave duration (WSDI), to assess changes over time. The results show a widespread decline in total annual precipitation across the continent, although some regions, particularly in the northeast and southeast, experienced an increase in the intensity and frequency of extreme precipitation events. Extreme temperatures have also risen consistently across South America, with an increase in both the frequency and duration of heat extremes, indicating an ongoing warming trend. The study also highlights the significant role of SST anomalies in both the Pacific and Atlantic Oceans in driving these climate extremes. Strong correlations were found between Pacific SST anomalies (Niño 3.4 region) and extreme precipitation events in the northern and southern regions of South America. Similarly, Atlantic SST anomalies, especially in the Northern Atlantic (TNA), exhibited notable impacts on temperature extremes, particularly heatwaves. These findings underscore the complex interactions between SST anomalies and climate variability in South America, providing crucial insights into the dynamics of climate extremes in the region. Understanding these relationships is essential for developing effective adaptation and mitigation strategies in response to the increasing frequency and intensity of climate extremes. Full article
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<p>Climate normal for precipitation and air temperature and location of the climate reference regions from the Sixth Assessment Report of the Intergovernmental Panel on Climate Change (IPCC AR6) for South America from 1979 to 2020.</p>
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<p>Location of the ENSO (Niño 1 + 2, Niño 3, Niño 3.4, and Niño 4) and Atlantic Dipole (TNA and TSA) regions in the equatorial Pacific and tropical Atlantic, respectively.</p>
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<p>Spatial distribution of trends from 1979 to 2020: number of heavy precipitation days (R10mm) (<b>a</b>); number of very heavy precipitation days (R20mm) (<b>b</b>); number of days above 30 mm (R30mm) (<b>c</b>); max 1-day precipitation amount (Rx1day) (<b>d</b>); max 5-day precipitation amount (Rx5day) (<b>e</b>); annual total wet day precipitation (PRCPTOT) (<b>f</b>); simple daily intensity index (SDII) (<b>g</b>); precipitation on very wet days (R95p) (<b>h</b>); precipitation on extremely wet days (R99p) (<b>i</b>); consecutive wet days (CWD) (<b>j</b>); and consecutive dry days (CDD) (<b>k</b>) over the climate reference regions of the Sixth Assessment Report of the Intergovernmental Panel on Climate Change (IPCC—AR6) on South America. Only values with statistical significance at the 5% level are presented in the maps.</p>
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<p>Spatial distribution of trends from 1979 to 2020: warmest day (TXx) (<b>a</b>); warmest night (TNx) (<b>b</b>); coldest day (TXn) (<b>c</b>); coldest night (TNn) (<b>d</b>); diurnal temperature Range (DTR) (<b>e</b>); warm spell duration (WSDI) (<b>f</b>); cold spell duration (CSDI) (<b>g</b>); warm days (TX90p) (<b>h</b>); warm nights (TN90p) (<b>i</b>); cool days (TX10p) (<b>j</b>); cool nights (TN10p) (<b>k</b>); and frost days (FD) (<b>l</b>) over the climate reference regions of the Sixth Assessment Report of the Intergovernmental Panel on Climate Change (IPCC—AR6) on South America. Only values with statistical significance at the 5% level are presented in the maps.</p>
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<p>Probability density function (PDF) of the annual frequency of the following extreme precipitation indices over South America from 1979 to 2020: number of heavy precipitation days (R10mm) (<b>a</b>); number of very heavy precipitation days (R20mm) (<b>b</b>); number of days with precipitation above 50 mm (R50mm) (<b>c</b>); maximum 1-day precipitation amount (Rx1day) (<b>d</b>); maximum 5-day precipitation amount (Rx5day) (<b>e</b>); annual total wet-day precipitation (PRCPTOT) (<b>f</b>); simple daily intensity index (SDII) (<b>g</b>); precipitation on very wet days (R95p) (<b>h</b>); precipitation on extremely wet days (R99p) (<b>i</b>); consecutive wet days (CWD) (<b>j</b>); consecutive dry days (CDD) (<b>k</b>).</p>
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<p>Probability density function (PDF) of the annual frequency of the following extreme temperature indices over South America from 1979 to 2020: warmest day (TXx) (<b>a</b>); warmest night (TNx) (<b>b</b>); coldest day (TXn) (<b>c</b>); coldest night (TNn) (<b>d</b>); diurnal temperature range (DTR) (<b>e</b>); warm spell duration (WSDI) (<b>f</b>); cold spell duration (CSDI) (<b>g</b>); warm days (TX90p) (<b>h</b>); warm nights (TN90p) (<b>i</b>); cool days (TX10p) (<b>j</b>); cool nights (TN10p) (<b>k</b>) and frost days (FD) (<b>l</b>).</p>
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<p>Pearson correlations between Pacific SST anomalies in the Niño 3.4 region and extreme precipitation indices: number of heavy precipitation days (R10mm) (<b>a</b>); number of very heavy precipitation days (R20mm) (<b>b</b>); number of days above 30 mm (R30mm) (<b>c</b>); max 1-day precipitation amount (Rx1day) (<b>d</b>); max 5-day precipitation amount (Rx5day) (<b>e</b>); annual total wet day precipitation (PRCPTOT) (<b>f</b>); simple daily intensity index (SDII) (<b>g</b>); precipitation on very wet days (R95p) (<b>h</b>); precipitation on extremely wet days (R99p) (<b>i</b>); consecutive wet days (CWD) (<b>j</b>); and consecutive dry days (CDD) (<b>k</b>) over the climate reference regions of the Sixth Assessment Report of the Intergovernmental Panel on Climate Change (IPCC—AR6) on South America from 1979 to 2020. Only values with statistical significance at the 5% level are presented in the maps.</p>
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<p>Pearson correlations between Atlantic SST anomalies in the Northern Atlantic Ocean (TNA) sector and extreme precipitation indices: number of heavy precipitation days (R10mm) (<b>a</b>); number of very heavy precipitation days (R20mm) (<b>b</b>); number of days above 30 mm (R30mm) (<b>c</b>); max 1-day precipitation amount (Rx1day) (<b>d</b>); max 5-day precipitation amount (Rx5day) (<b>e</b>); annual total wet day precipitation (PRCPTOT) (<b>f</b>); simple daily intensity index (SDII) (<b>g</b>); precipitation on very wet days (R95p) (<b>h</b>); precipitation on extremely wet days (R99p) (<b>i</b>); consecutive wet days (CWD) (<b>j</b>); and consecutive dry days (CDD) (<b>k</b>) over the climate reference regions of the Sixth Assessment Report of the Intergovernmental Panel on Climate Change (IPCC—AR6) on South America from 1979 to 2020. Only values with statistical significance at the 5% level are presented in the maps.</p>
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<p>Relationship between sea surface temperature (SST) anomalies in the Pacific Ocean (Niño 3.4), Northern and Southern Atlantic Ocean sectors (TNA) (TSA), and extreme climate precipitation indices: number of heavy precipitation days (R10mm) (<b>A</b>); number of very heavy precipitation days (R20mm) (<b>B</b>); number of days above 30 mm (R30mm) (<b>C</b>); max 1-day precipitation amount (Rx1day) (<b>D</b>); max 5-day precipitation amount (Rx5day) (<b>E</b>); annual total wet day precipitation (PRCPTOT) (<b>F</b>); simple daily intensity index (SDII) (<b>G</b>); precipitation on very wet days (R95p) (<b>H</b>); precipitation on extremely wet days (R99p) (<b>I</b>); consecutive wet days (CWD) (<b>J</b>); and consecutive dry days (CDD) (<b>K</b>) over South America from 1979 to 2020.</p>
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<p>Pearson correlation between sea surface temperature (SST) anomalies in the Pacific Ocean over the Nino 3.4 region and extreme climatic temperature indices: warmest day (TXx) (<b>a</b>); warmest night (TNx) (<b>b</b>); coldest day (TXn) (<b>c</b>); coldest night (TNn) (<b>d</b>); diurnal temperature Range (DTR) (<b>e</b>); warm spell duration (WSDI) (<b>f</b>); cold spell duration (CSDI) (<b>g</b>); warm days (TX90p) (<b>h</b>); warm nights (TN90p) (<b>i</b>); cool days (TX10p) (<b>j</b>); cool nights (TN10p) (<b>k</b>); and frost days (FD) (<b>l</b>) over the climate reference regions of the Sixth Assessment Report of the Intergovernmental Panel on Climate Change (IPCC—AR6) on South America from 1979 to 2020. Only values with statistical significance at the 5% level are presented in the maps.</p>
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<p>Pearson correlation coefficients between sea surface temperature (SST) anomalies in the Northern Atlantic Ocean (TNA) sector and extreme climatic temperature indices: warmest day (TXx) (<b>a</b>); warmest night (TNx) (<b>b</b>); coldest day (TXn) (<b>c</b>); coldest night (TNn) (<b>d</b>); diurnal temperature Range (DTR) (<b>e</b>); warm spell duration (WSDI) (<b>f</b>); cold spell duration (CSDI) (<b>g</b>); warm days (TX90p) (<b>h</b>); warm nights (TN90p) (<b>i</b>); cool days (TX10p) (<b>j</b>); cool nights (TN10p) (<b>k</b>); and frost days (FD) (<b>l</b>) over the climate reference regions of the Sixth Assessment Report of the Intergovernmental Panel on Climate Change (IPCC—AR6) on South America from 1979 to 2020. Only values with statistical significance at the 5% level are presented in the maps.</p>
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<p>Relationship between sea surface temperature (SST) anomalies in the Pacific Ocean (Niño 3.4), Northern and Southern Atlantic Ocean sectors (TNA) (TSA), and extreme climate temperature indices: warmest day (TXx) (<b>A</b>); warmest night (TNx) (<b>B</b>); coldest day (TXn) (<b>C</b>); coldest night (TNn) (<b>D</b>); diurnal temperature Range (DTR) (<b>E</b>); warm spell duration (WSDI) (<b>F</b>); cold spell duration (CSDI) (<b>G</b>); warm days (TX90p) (<b>H</b>); warm nights (TN90p) (<b>I</b>); cool days (TX10p) (<b>J</b>); cool nights (TN10p) (<b>K</b>); and frost days (FD) (<b>L</b>) over South America from 1979 to 2020.</p>
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<p>Atmospheric circulation climatology (<b>a</b>,<b>d</b>,<b>g</b>) and observed atmospheric circulation under El Niño (<b>b</b>,<b>e</b>,<b>h</b>) and La Niña (<b>c</b>,<b>f</b>,<b>i</b>) conditions at pressure levels of 200 hPa, 500 hPa, and 850 hPa, respectively, over South America. The shaded region represents wind speed in m s<sup>−1</sup>. The climatology period is from 1981 to 2010, while the observed data refers to the mean composites of the intense El Niño events in 1982–1983, 1997–1998, and 2015–2016, and La Niña in 1988–1989, 1999–2000, and 2010–2011 in the December–January–February (DJF) quarter.</p>
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<p>Atmospheric circulation climatology (<b>a</b>,<b>d</b>,<b>g</b>) and observed atmospheric circulation under El Niño (<b>b</b>,<b>e</b>,<b>h</b>) and La Niña (<b>c</b>,<b>f</b>,<b>i</b>) conditions at pressure levels of 200 hPa, 500 hPa, and 850 hPa, respectively, over South America. The shaded region represents wind speed in m s<sup>−1</sup>. The climatology period is from 1981 to 2010, while the observed data refers to the mean composites of the intense El Niño events in 1982–1983, 1997–1998, and 2015–2016 and La Niña in 1988–1989, 1999–2000, and 2010–2011 in the June–July–August (JJA) quarter.</p>
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<p>Climatology (blue vectors) and anomaly (red vectors) of vertical wind velocity between 5 °S and 15°S during El Niño (<b>a</b>) and La Niña (<b>b</b>) events in the December-January-February (DJF) quarter. (<b>c</b>,<b>d</b>) Vertical wind speed (filled contours) and wind direction (arrows) between 5 °S and 15 °S during El Niño (<b>c</b>) and La Niña (<b>d</b>) events in the DJF quarter. (<b>e</b>,<b>f</b>) Sea surface temperature (SST) anomalies and precipitation anomalies over the continent between 5 °S and 15 °S during El Niño (<b>e</b>) and La Niña (<b>f</b>) events in the DJF quarter. (<b>g</b>,<b>h</b>) Air temperature anomalies over the continent between 5 °S and 15 °S during El Niño (<b>g</b>) and La Niña (<b>h</b>) events in the DJF quarter. Data correspond to the composite averages of El Niño (1982–1983, 1997–1998, and 2015–2016) and La Niña (1988–1989, 1999–2000, and 2010–2011) events in the DJF quarter.</p>
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<p>Climatology (blue vectors) and anomaly (red vectors) of vertical wind velocity between 5 °S and 15 °S during El Niño (<b>a</b>) and La Niña (<b>b</b>) events in the June-July-August (JJA) quarter. (<b>c</b>,<b>d</b>) Vertical wind speed (filled contours) and wind direction (vectors) between 5 °S and 15 °S during El Niño (<b>c</b>) and La Niña (<b>d</b>) events in the JJA quarter. (<b>e</b>,<b>f</b>) Sea surface temperature (SST) anomalies and precipitation anomalies over the continent between 5 °S and 15 °S during El Niño (<b>e</b>) and La Niña (<b>f</b>) events in the JJA quarter. (<b>g</b>,<b>h</b>) Air temperature anomalies over the continent between 5 °S and 15 °S during El Niño (<b>g</b>) and La Niña (<b>h</b>) events in the JJA quarter. Data correspond to the composite averages of El Niño (1982–1983, 1997–1998, and 2015–2016) and La Niña (1988–1989, 1999–2000, and 2010–2011) events in the JJA quarter.</p>
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