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19 pages, 19605 KiB  
Article
Skill Validation of High-Impact Rainfall Forecasts over Vietnam Using the European Centre for Medium-Range Weather Forecasts (ECMWF) Integrated Forecasting System (IFS) and Dynamical Downscaling with the Weather Research and Forecasting Model
by Tran Anh Duc, Mai Van Khiem, Mai Khanh Hung, Dang Dinh Quan, Do Thuy Trang, Hoang Gia Nam, Lars R. Hole and Du Duc Tien
Atmosphere 2025, 16(2), 224; https://doi.org/10.3390/atmos16020224 - 16 Feb 2025
Abstract
This research evaluates the quality of high-impact rainfall forecasts across Vietnam and its sub-climate regions. The 3-day rainfall forecast products evaluated include the European Centre for Medium-Range Weather Forecasts (ECMWF) High-Resolution Integrated Forecasting System (IFS) and its downscaled outputs using the Weather Research [...] Read more.
This research evaluates the quality of high-impact rainfall forecasts across Vietnam and its sub-climate regions. The 3-day rainfall forecast products evaluated include the European Centre for Medium-Range Weather Forecasts (ECMWF) High-Resolution Integrated Forecasting System (IFS) and its downscaled outputs using the Weather Research and Forecasting (WRF) model with the Advanced Research WRF core (WRF-ARW): direct downscaling and downscaling with data assimilation. A full 5-year validation period from 2019 to 2025 was processed. The validation focused on basic rainfall thresholds and also considered the distribution of skill scores for intense events and extreme events. The validations revealed systematic errors (bias) in the models at low rainfall thresholds. The forecast skill was the lowest for northern regions, while the central regions exhibited the highest. For regions strongly affected by terrain, high-resolution downscaling with local observation data assimilation is necessary to improve the detectability of extreme events. Full article
(This article belongs to the Special Issue Precipitation Observations and Prediction (2nd Edition))
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Figure 1

Figure 1
<p>(<b>a</b>) Distribution of automatic weather stations (black dots) used for model validations and the seven sub-climate regions (R1–R7). (<b>b</b>) The 5-year average (2019–2023) of annual accumulated rainfall (unit: mm).</p>
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<p>(<b>a</b>) The observation analysis 24 h accumulated rainfall map, (<b>b</b>–<b>d</b>) 24 h accumulated rainfall and mean sea level pressure forecast on 21 July 2020, 00:00 UTC (07:00 LTC) from the Integrated Forecasting System (IFS), WRF3kmIFS, and WRF3kmIFS-DA, respectively, and more detailed plots for Vietnam only (<b>e</b>–<b>g</b>) for the IFS, WRF3kmIFS, and WRF3kmIFS-DA, respectively.</p>
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<p>The 5-year average (<b>a</b>) bias score (BIAS), (<b>b</b>) probability of detection (POD), (<b>c</b>) false alarm rate (FAR), and (<b>d</b>) threat score (TS) scores at a 24 h forecast range for the IFS, WRF3kmIFS, and WRF3kmIFS-DA model for seven sub-climate regions (R1–R7) at three thresholds (&gt;5 mm/24 h, &gt;25 mm/24 h, and &gt;50 mm/24 h).</p>
Full article ">Figure 3 Cont.
<p>The 5-year average (<b>a</b>) bias score (BIAS), (<b>b</b>) probability of detection (POD), (<b>c</b>) false alarm rate (FAR), and (<b>d</b>) threat score (TS) scores at a 24 h forecast range for the IFS, WRF3kmIFS, and WRF3kmIFS-DA model for seven sub-climate regions (R1–R7) at three thresholds (&gt;5 mm/24 h, &gt;25 mm/24 h, and &gt;50 mm/24 h).</p>
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<p>The 5-year average TS scores at 24 h, 48 h, and 72 h forecast ranges for the (<b>a</b>) IFS, (<b>b</b>) WRF3kmIFS, and (<b>c</b>) WRF3kmIFS-DA models for seven sub-climate regions (R1–R7) at three thresholds (&gt;5 mm/24 h, &gt;25 mm/24 h, and &gt;50 mm/24 h).</p>
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<p>Yearly performances of TS scores at 24 h forecast range for the (<b>a</b>) IFS, (<b>b</b>) WRF3kmIFS, and (<b>c</b>) WRF3kmIFS-DA models for seven sub-climate regions (R1–R7) at three thresholds (&gt;5 mm/24 h, &gt;25 mm/24 h, and &gt;50 mm/24 h).</p>
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<p>Yearly performances of BIAS scores at 24 h forecast range for the (<b>a</b>) IFS, (<b>b</b>) WRF3kmIFS, and (<b>c</b>) WRF3kmIFS-DA models for seven sub-climate regions (R1–R7) at three thresholds (&gt;5 mm/24 h, &gt;25 mm/24 h, and &gt;50 mm/24 h).</p>
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<p>Spatial distribution of TS scores at the threshold &gt;25 mm/24 h for the IFS (<b>first row</b>), WRF3kmIFS (<b>second row</b>), and WRF3kmIFS-DA (<b>third row</b>) at forecast ranges of 24 h (<b>left column</b>), 48 h (<b>center column</b>), and 72 h (<b>right column</b>).</p>
Full article ">Figure 7 Cont.
<p>Spatial distribution of TS scores at the threshold &gt;25 mm/24 h for the IFS (<b>first row</b>), WRF3kmIFS (<b>second row</b>), and WRF3kmIFS-DA (<b>third row</b>) at forecast ranges of 24 h (<b>left column</b>), 48 h (<b>center column</b>), and 72 h (<b>right column</b>).</p>
Full article ">Figure 8
<p>Similar to <a href="#atmosphere-16-00224-f007" class="html-fig">Figure 7</a> but for POD scores.</p>
Full article ">Figure 8 Cont.
<p>Similar to <a href="#atmosphere-16-00224-f007" class="html-fig">Figure 7</a> but for POD scores.</p>
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<p>Spatial distribution of PODs for extreme precipitation forecasts (&gt;100 mm/24 h) using the IFS (<b>first row</b>), WRF3kmIFS (<b>second row</b>), and WRF3kmIFS-DA (<b>third row</b>) models at forecast ranges of 24 h (<b>left column</b>), 48 h (<b>center column</b>), and 72 h (<b>right column</b>).</p>
Full article ">Figure 9 Cont.
<p>Spatial distribution of PODs for extreme precipitation forecasts (&gt;100 mm/24 h) using the IFS (<b>first row</b>), WRF3kmIFS (<b>second row</b>), and WRF3kmIFS-DA (<b>third row</b>) models at forecast ranges of 24 h (<b>left column</b>), 48 h (<b>center column</b>), and 72 h (<b>right column</b>).</p>
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<p>Similar to <a href="#atmosphere-16-00224-f009" class="html-fig">Figure 9</a> but for spatial distribution of Heidke skill scores.</p>
Full article ">Figure 10 Cont.
<p>Similar to <a href="#atmosphere-16-00224-f009" class="html-fig">Figure 9</a> but for spatial distribution of Heidke skill scores.</p>
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17 pages, 4531 KiB  
Article
Solar Irradiance Estimation in Tropical Regions Using Recurrent Neural Networks and WRF Models
by Fadhilah A. Suwadana, Pranda M. P. Garniwa, Dhavani A. Putera, Dita Puspita, Ahmad Gufron, Indra A. Aditya, Hyunjin Lee and Iwa Garniwa
Energies 2025, 18(4), 925; https://doi.org/10.3390/en18040925 - 14 Feb 2025
Abstract
The accurate estimation of solar radiation is crucial for optimizing solar energy deployment and advancing the global energy transition. This study pioneers the development of a hybrid model combining Recurrent Neural Networks (RNNs) and the Weather Research and Forecasting (WRF) model to estimate [...] Read more.
The accurate estimation of solar radiation is crucial for optimizing solar energy deployment and advancing the global energy transition. This study pioneers the development of a hybrid model combining Recurrent Neural Networks (RNNs) and the Weather Research and Forecasting (WRF) model to estimate solar radiation in tropical regions characterized by scarce and low-quality data. Using datasets from Sumedang and Jakarta across five locations in West Java, Indonesia, the RNN model achieved moderate accuracy, with R2 values of 0.68 and 0.53 and RMSE values of 159.87 W/m2 and 125.53 W/m2, respectively. Additional metrics, such as Mean Bias Error (MBE) and relative MBE (rMBE), highlight limitations due to input data constraints. Incorporating spatially resolved GHI data from the WRF model into the RNN framework significantly enhanced accuracy under both clear and cloudy conditions, accounting for the region’s complex topography. While the results are not yet comparable to best practices in data-rich regions, they demonstrate promising potential for advancing solar radiation modeling in tropical climates. This study establishes a critical foundation for future research on hybrid solar radiation estimation techniques in challenging environments, supporting the growth of renewable energy applications in the tropics. Full article
(This article belongs to the Special Issue Machine Learning in Renewable Energy Resource Assessment)
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<p>Sample of visible satellite images (0.64 µm) provided by GK2A satellite stationed at 36,000 km above the equator. The image is considered Level-1B fulldisk data.</p>
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<p>Result of model benchmarking with 3 different stations. (<b>A</b>) Busan station; (<b>B</b>) Gwangju station; (<b>C</b>) Gangneung station.</p>
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<p>Result of solar irradiance estimation. (<b>A</b>) Sumedang station; (<b>B</b>) Jakarta station.</p>
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<p>Kernel density visualization of solar irradiance estimation. (<b>A</b>) Sumedang station; (<b>B</b>) Jakarta station.</p>
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<p>Spatial distribution of solar irradiance in West Java, obtained from WRF. (<b>A</b>) clear sky condition; (<b>B</b>) cloudy condition.</p>
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<p>Result of solar irradiance estimation by adding WRF outputs into dataset. (<b>A</b>) Sumedang station; (<b>B</b>) Jakarta station.</p>
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<p>Overlay of solar irradiance and landform in West Java.</p>
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22 pages, 11030 KiB  
Article
Adjusting Soil Temperatures with a Physics-Informed Deep Learning Model for a High-Resolution Numerical Weather Prediction System
by Qiufan Wang, Yubao Liu, Yueqin Shi and Shaofeng Hua
Atmosphere 2025, 16(2), 207; https://doi.org/10.3390/atmos16020207 - 12 Feb 2025
Abstract
Soil temperature (ST) plays an important role in the surface heat energy balance, and an accurate description of soil temperatures is critical for numerical weather prediction; however, it is difficult to consistently measure soil temperatures. We developed a U-Net-based deep learning model to [...] Read more.
Soil temperature (ST) plays an important role in the surface heat energy balance, and an accurate description of soil temperatures is critical for numerical weather prediction; however, it is difficult to consistently measure soil temperatures. We developed a U-Net-based deep learning model to derive soil temperatures (designated as ST-U-Net) primarily based on 2 m air temperature (T2) forecasts. The model, the domain of which covers the Mt. Lushan region, was trained and tested by utilizing the high-resolution forecast archive of an operational weather research and forecasting four-dimensional data assimilation (WRF-FDDA) system. The results showed that ST-U-Net can accurately estimate soil temperatures based on T2 inputs, achieving a mean absolute error (MAE) of less than 0.8 K on the testing set of 5055 samples. The performance of ST-U-Net varied diurnally, with smaller errors at night and slightly larger errors in the daytime. Incorporating additional inputs such as land uses, terrain height, radiation flux, surface heat flux, and coded time further reduced the MAE for ST by 26.7%. By developing a boundary-layer physics-guided training strategy, the error was further reduced by 8.8%. Full article
(This article belongs to the Section Meteorology)
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<p>PRUFS nested-grid Domain 3 with 1 km grid intervals. (<b>a</b>) Terrain height; (<b>b</b>) land uses. The starred Croplands occupy 41.4% of the region, and the Evergreen Broad-leaved Forest occupies 41.3% of the region.</p>
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<p>Workflow of this study. The PRUFS data were first processed through cleansing, normalization, and partitioning, used to train the ST-U-Net, then followed by statistical evaluation and further analysis of the auxiliary information in the testing set. Additionally, a supplementary experiment was conducted, designing a training strategy based on temporal grouping and pretraining, with results compared to Exp_T2.</p>
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<p>The configuration of ST-U-Net. C, H, and W represent channels, height, and width, respectively.The blocks marked with a red star do not contain normalization and the arrows represent the last convolutional layer. Conv2d denotes a two-dimensional convolutional layer, with a kernel size of 3 × 3. InstanceNorm represents a two-dimensional instance normalization layer, while ReLU serves as the activation function. MaxPool2d and upsampling transposed convolution (TransConv) refer to two-dimensional max-pooling and upsampling layers, respectively, both employing a 2 × 2 window size. Skip connections are utilized to integrate multiscale features. The dimensions of the input data are N × 288 × 288, where N represents the number of input variables, and the dimensions of the output data are N × 288 × 288.</p>
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<p>Comparisons of verification metrics for Exp_T2, Exp_NoTER, Exp_NoLU, Exp_ALL, and Exp_NoTime (listed in <a href="#atmosphere-16-00207-t001" class="html-table">Table 1</a>) for the results on the testing set. Blue bars represent RMSE, red bars MAE, and green bars variance in MAE. PCC stands for Pearson correlation coefficient (R).</p>
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<p>Comparison of retrieved STs of Exp_T2 (<b>a</b>,<b>f</b>), Exp_NoTER (<b>b</b>,<b>g</b>)<b>,</b> Exp_ALL (<b>c</b>,<b>h</b>), and Exp_NoTime (<b>d</b>,<b>i</b>) at 14:20 p.m. (daytime, (<b>a</b>–<b>e</b>)) and 02:20 a.m. (nighttime, (<b>f</b>–<b>j</b>)) BJT with the truth (<b>e</b>,<b>j</b>) on 15 March 2024. (Blue boxes represent areas of steep slope, green boxes represent flat areas).</p>
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<p>The same as <a href="#atmosphere-16-00207-f005" class="html-fig">Figure 5</a>, but for the bias distribution of the STs retrieved by Exp_T2 (<b>a</b>,<b>e</b>), Exp_NoTER (<b>b</b>,<b>f</b>), Exp_ALL(<b>c</b>,<b>g</b>), and Exp_NoTime (<b>d</b>,<b>h</b>) at 14:20 p.m. (daytime, (<b>a</b>–<b>d</b>)) and 02:20 a.m. (nighttime, (<b>e</b>–<b>h</b>)) BJT. The domain-averaged RMSE (K) is labeled with bold black numbers at the bottom-right corner of each panel. (Blue boxes represent areas of steep slope, green boxes represent flat areas).</p>
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<p>Distribution of errors in the ST retrieval for the testing set with 5055 samples. (<b>a</b>) Exp_T2 and (<b>b</b>) Exp_Notime. The error bins of 0.15 K. The gray dotted line represents a value of 0 and there is no deviation.</p>
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<p>Density scatterplots of the STs of the PRUFS forecasts and the STs retrieved by ST-U-Net. Derived from experiments (<b>a</b>) Exp_T2 and (<b>b</b>) Exp_Notime.</p>
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<p>Diurnal evolution of MAE of STs retrieved by five experiments—Exp_T2, Exp_NoTER, Exp_NoLU, Exp_ALL, and Exp_NoTime—for the testing set. Horizontal axis represents Beijing time (BJT), orange curve is for Exp_T2, purple for Exp_NoTER, green for Exp_NoTER, blue for Exp_ALL, red for Exp_NoTime.</p>
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<p>MAE of STs retrieved in (<b>a</b>) Exp_T2, (<b>b</b>) Exp_ALL, and (<b>c</b>) Exp_NoTER. (<b>d</b>) Terrain height.</p>
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<p>A sensitivity analysis on retrieving STs by the trained Exp_ALL with artificially modified inputs. The left column is for the case with the unmodified input. The middle and right columns present the cases where T2 or the terrain data of the input are horizontally averaged, respectively. Results at 01:00 a.m. (nighttime, (<b>a</b>–<b>c</b>)) and 10:00 p.m. (daytime, (<b>d</b>–<b>f</b>)) BJT on 26 March 2024 are shown.</p>
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<p>MAE of STs retrieved in (<b>a</b>) Exp_NoLU and (<b>b</b>) Exp_ALL; (<b>c</b>) terrain height. The horizontal color bar represents the MAE scale, while the vertical color bar represents the elevation scale.</p>
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<p>Testing set mean bias of STs retrieved in (<b>a</b>) Exp_NoLU and (<b>b</b>) Exp_ALL; (<b>c</b>) land type. The horizontal color bar represents the bias scale, while detailed land use information is presented in <a href="#atmosphere-16-00207-f001" class="html-fig">Figure 1</a>.</p>
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<p>Performance of ST-U-Net trained with different sample sizes for the experiments (Exp_T2, Exp_NoTER, Exp_NoLU, Exp_ALL, Exp_NoTime) listed in <a href="#atmosphere-16-00207-t001" class="html-table">Table 1</a> on the testing set. Green line for Exp_ALL, red line for Exp_LU, gray line for Exp_T2, blue line for Exp_TER.</p>
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<p>Superimposition of disturbance areas on PRUFS model domains with 1 km horizontal resolution: (<b>a</b>) terrain height; (<b>b</b>) land uses (four main regions marked: brown for croplands, green for evergreen broad-leaved forest, yellow for grasslands, and blue for water). Red circles represent the areas that are disturbed.</p>
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<p>A point-wise sensitivity test with Exp_T2 for 16:00 on January 14, 2024: (<b>a</b>) ST retrieval with normal T2 inputs; (<b>b</b>) ST retrieval with perturbed T2 inputs; (<b>c</b>) the truth; (<b>d</b>) the difference between the ST retrievals with and without perturbed T2 inputs; and (<b>e</b>) details of bias. The black dots mark the center point of the T2 perturbations.</p>
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<p>Correlation coefficients between the MAE of the ST retrieved for each hour of day for the testing set. The red dashed line demarcates four distinct time periods. The periods are classified into two transition groups (08:00–10:00 BJT and 16:00–19:00 BJT), a daytime period (10:00–16:00 BJT), and a nighttime period (19:00 BJT to 07:00 BJT).</p>
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<p>Comparison between the errors of the STs retrieved by ST-U-Net with four time training strategies: IGT_hour (red solid line), IGT (green), PGT (purple), and DT (orange). The black dashed line shows the size of the training dataset for each hour.</p>
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21 pages, 6948 KiB  
Article
Causes and Transmission Characteristics of the Regional PM2.5 Heavy Pollution Process in the Urban Agglomerations of the Central Taihang Mountains
by Luoqi Yang, Guangjie Wang, Yegui Wang, Yongjing Ma and Xi Zhang
Atmosphere 2025, 16(2), 205; https://doi.org/10.3390/atmos16020205 - 11 Feb 2025
Abstract
The Taihang Mountains serve as a critical geographical barrier in northern China, delineating two major 2.5-micrometer particulate matter (PM2.5) pollution hotspots in the Beijing–Tianjin–Hebei region and the Fenwei Plain. This study examines the underlying mechanisms and interregional dynamic transport pathways of [...] Read more.
The Taihang Mountains serve as a critical geographical barrier in northern China, delineating two major 2.5-micrometer particulate matter (PM2.5) pollution hotspots in the Beijing–Tianjin–Hebei region and the Fenwei Plain. This study examines the underlying mechanisms and interregional dynamic transport pathways of a severe PM2.5 pollution event that occurred in the urban agglomerations of the Central Taihang Mountains (CTHM) from 8–13 December 2021. The WRF-HYSPLIT simulation was employed to analyze a broader range of potential pollution sources and transport pathways. Additionally, a new river network analysis module was developed and integrated with the Atmospheric Pollutant Transport Quantification Model (APTQM). This module is capable of identifying localized, small-scale (interplot) pollution transport processes, thereby enabling more accurate identification of potential source areas and transport routes. The findings indicate that the persistence of low temperatures, high humidity, and stagnant atmospheric conditions facilitated both the local accumulation and cross-regional transport of PM2.5. The eastern urban agglomerations, such as Shijiazhuang and Xingtai, were predominantly influenced by northwesterly air masses originating from Inner Mongolia and Shanxi, with pollution levels intensified due to topographic blocking and subsidence effects east of the Taihang Mountains. In contrast, western urban centers, including Taiyuan and Yangquan, experienced pollution primarily from short-range transport within the Fen River Basin, central Inner Mongolia, and Shaanxi, compounded by basin-induced stagnation. Three principal transport pathways were identified: (1) a northwestern pathway from Inner Mongolia to Hebei, (2) a southwestern pathway following the Fen River Basin, and (3) a southward inflow from Henan. The trajectory analysis revealed that approximately 68% of PM2.5 in eastern receptor cities was transported through topographic channels within the Taihang Transverse Valleys, whereas 43% of pollution in the western regions originated from intra-basin emissions and basin-capture circulation. Furthermore, APTQM-PM2.5 identified major pollution source regions, including Ordos and Chifeng in Inner Mongolia, as well as Taiyuan and the Fen River Basin. This study underscores the synergistic effects of basin topography, regional circulation, and anthropogenic emissions in shaping pollution distribution patterns. The findings provide a scientific basis for formulating targeted, regionally coordinated air pollution mitigation strategies in complex terrain areas. Full article
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<p>Overview of the study area. (<b>a</b>) shows the extent of the study area; (<b>b</b>,<b>c</b>) correspond to the distribution of cities in the CTHM and the elevation map; (<b>d</b>) is the distribution of the “Eight Passes of the Taihang Mountains”, where the red lines are valley transmission channels, the blue are rivers, and the black dots are neighboring cities and counties (belonging to the province).</p>
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<p>Nested regions of the WRF grid (where d01 is 27 km, d02 is 9 km, and d03 is 3 km).</p>
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<p>APTQM-PM<sub>2.5</sub> modeling step analysis. Step 1: (<b>a</b>,<b>b</b>) area gridding and boundary processing where (<b>a</b>) is the target study area and (<b>b</b>) is the gridding, where the shaded grid is the matching blocks of the study area. Step 2: (<b>c</b>,<b>d</b>) gradient analysis and airflow direction classification, where (<b>c</b>) is the air pressure gradient schematic, where the blue color is the relatively high-value cell and the red color is the relatively low-value cell, and (<b>d</b>) is the air gradient flow schematic, and the black vector arrow is the airflow direction. Step 3: (<b>e</b>,<b>f</b>) river network classification and flow intensity analysis, where (<b>e</b>) is the river network classification of the study area, direction of air flow; (<b>e</b>) shows the results of river network classification in the study area, where the yellow grid (level 1) is the outflow cell, i.e., upstream grid, and the green grid (level 2) is the inflow cell, i.e., downstream grid; and (<b>f</b>) is the schematic illustration of the flow intensity, where the yellow color is the main stream flow, and the blue color is the secondary flow.</p>
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<p>Hourly variations of PM<sub>2.5</sub> mass concentration and comparative variations of related meteorological factors in the urban agglomerations of CTHM during the period of heavy pollution. (<b>a</b>) mean surface wind speed (wspd, m/s) and temperature (temp, °C) in December 2021 for both sides of the urban agglomerations; (<b>b</b>) relationship and dynamics between visibility (vis, km) and PM<sub>2.5</sub> mass concentration (PM<sub>2.5</sub> Conc, μg); (<b>c</b>) relationship and dynamics between relative humidity (RH, %) and PM<sub>2.5</sub> mass concentration.</p>
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<p>Visualization of the Taylor coefficients between the simulated and observed meteorological fields.</p>
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<p>Backward trajectory analysis of major cities during periods of heavy pollution based on WRF-HYSPLIT. (<b>a</b>) Eastern urban agglomeration, Shijiazhuang, Hebei Province. (<b>b</b>) Eastern urban agglomeration, Handan, Hebei Province. (<b>c</b>) Eastern urban agglomeration, Xingtai, Hebei Province. (<b>d</b>) Western urban agglomeration, Taiyuan, Shanxi Province. (<b>e</b>) Western urban agglomeration, Yangquan, Shanxi Province. (<b>f</b>) Western urban agglomeration, Jinzhong, Shanxi Province.</p>
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<p>Mean geopotential height field and wind field from 9–13 December 2021, at time 0. Where (<b>a</b>) is the mean geopotential height field and wind field at 500 hpa at time 0 on the 9th, (<b>b</b>) is on 500 hpa at time 0 on the 11th, (<b>c</b>) is on 500 hpa at time 0 on the 13th; (<b>d</b>–<b>f</b>) is on 750 hpa, and the (<b>g</b>–<b>i</b>) is 850 hpa, where the gray filled areas are terrain obstructions.</p>
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<p>The longitudinal vertical circulation, mean hourly wind field, and potential pseudo-equivalent temperature (θse) variations in the study area during 9–13 December 2021, at time 0. (<b>a</b>) For 9th, (<b>b</b>) for 11th, and (<b>c</b>) for 13th (where the left side of the y-axis is labeled as the height (km), the right side is the pseudo-equivalent temperature (K) for the corresponding height, and the bottom black fill is the terrain).</p>
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<p>Average migration and regional transmission distribution per unit grid (3 km × 3 km) during heavy pollution periods. (The color-filled part of the figure shows the gradient level.)</p>
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22 pages, 18605 KiB  
Article
Essential Organizing and Evolving Atmospheric Mechanisms Affecting the East Bay Hills Fire in Oakland, California (1991)
by William Agyakwah, Yuh-Lang Lin and Michael L. Kaplan
Fire 2025, 8(2), 72; https://doi.org/10.3390/fire8020072 - 10 Feb 2025
Abstract
This study examined atmospheric mechanisms affecting the East Bay Hills Fire (1991) in Oakland, California, using the Advanced Weather Research and Forecasting (WRF) model and North American Regional Reanalysis (NARR) dataset. High-resolution WRF simulations, initially at 16 km, were downscaled to 4 km [...] Read more.
This study examined atmospheric mechanisms affecting the East Bay Hills Fire (1991) in Oakland, California, using the Advanced Weather Research and Forecasting (WRF) model and North American Regional Reanalysis (NARR) dataset. High-resolution WRF simulations, initially at 16 km, were downscaled to 4 km and 1 km for analyzing primary and secondary circulations at synoptic and meso-α/meso-β scales, respectively, before the fire. Additionally, the interaction between the synoptic-scale and mesoscale environments was examined using backward trajectories derived from NARR data. The findings reveal that a strong pressure gradient created by a ridge over the Great Basin and a trough off the Pacific coast generated favorable meso-α conditions for the hot, dry northeasterly winds, known as “Diablo winds”, which initiated the wildfire in northern California. Mountain waves, enhanced by jet stream dynamics, contributed to sinking air on the Sierra Nevada’s western slopes. The main conclusion is that jet circulation did not directly transport warm, dry air to the fire but established a vertical atmospheric structure conducive to wave amplification and breaking and downward dry air fluxes leading to the necessary warm and dry low-level air for the fire. The hot–dry–windy (HDW) fire weather index further confirmed the highly favorable fire weather conditions. Full article
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<p>Domain set up for the East Bay Hills Fire (1991) with three nested domains with grid resolutions of 16 km (d01), 4 km (d02), and 1 km (d03). On the left-hand side is the zoomed-in view of the San Francisco Bay area and the East Bay Hills Fire location.</p>
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<p>North American Regional Reanalysis (NARR) data of 500 hPa geopotential height (shaded) and wind barbs valid at (<b>a</b>) 10/19/00Z, (<b>b</b>) 10/19/12Z, (<b>c</b>) 10/20/00Z, and (<b>d</b>) 10/20/12Z. NNV indicates northern Nevada, and SFB is San Francisco Bay. The East Bay Hills Fire (1991) started on 20 October 1991, around 1753 UTC, peaked on October 20 between 1804 and 2000 UTC, and was extinguished in the morning of 21 October, around 0230 UTC.</p>
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<p>North American Regional Reanalysis (NARR) data of MSLP (shaded and contour lines; hPa) and wind barbs at (<b>a</b>) 10/19/00Z, (<b>b</b>) 10/19/12Z, (<b>c</b>) 10/20/00Z, and (<b>d</b>) 10/20/12Z. NNV indicates northern Nevada, and SFB is San Francisco Bay. The East Bay Hills Fire (1991) started on 20 October 1991, around 1753 UTC, peaked on October 20 between 1804 UTC and 2000 UTC, and was extinguished in the morning of October 21, around 0230 UTC.</p>
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<p>Observed thermodynamic diagram for Oakland International Airport valid at (<b>a</b>) 1200 UTC Oct 19 (10/19/12Z), (<b>b</b>) 10/20/00Z, (<b>c</b>) 10/20/12Z, (<b>d</b>) 10/21/00Z, (<b>e</b>) 10/21/12Z, and (<b>f</b>) 10/22/00Z. The solid lines on the left and right in each panel denote dewpoint temperature and temperature, respectively. The East Bay Hills Fire (1991) started on 20 October 1991, around 1753 UTC, peaked on October 20 between 1804 and 2000 UTC, and was extinguished in the morning of October 21, around 0230 UTC.</p>
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<p>WRF (d02) simulated wind speeds (shaded; ms<sup>−1</sup> and directions (wind barbs) at various levels during the fire event’s start time between 10/20/15Z and 10/20/18Z, peak time between 10/20/18Z and 10/20/20Z, and extinguished the next day 10/21/12Z: 250 hPa (<b>a</b>), 850 hPa (<b>b</b>), and 10 m winds above the ground (<b>c</b>) at 10/20/15Z (left panels), 10/20/18Z (middle panels), and 10/21/12Z (right panels). Note that at the fire location (denoted with a black dot), the simulated winds from the surface up to 250 hPa are predominantly northeasterly (panels <b>a</b>–<b>g</b>) and moderately strong winds at the surface (12–14 ms<sup>−1</sup>, panels <b>c</b>,<b>f</b>), which are consistent with those observed (<a href="#fire-08-00072-f004" class="html-fig">Figure 4</a>c,d) from 10/20/15Z to 10/20/18Z, creating a highly favorable environment for fire spread. The winds then turn to a south-southwesterly flow during 10/21/12Z (panels <b>h</b>,<b>i</b>), consistent with those observed (<a href="#fire-08-00072-f004" class="html-fig">Figure 4</a>e,f).</p>
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<p>WRF (d02) simulated RH (shaded; %) and directions (wind barbs) at various levels during the fire event’s start time between 10/20/15Z and 10/20/18Z, peak time between 10/20/18Z and 10/20/20Z, and extinguishing the next day 10/21/12Z: 250 hPa (<b>a</b>), 850 hPa (<b>b</b>), and 10m winds above the ground (<b>c</b>) at 10/20/15Z (left panels), 10/20/18Z (middle panels), and 10/21/12Z (right panels). Note that at the fire location (denoted with a black dot), the simulated winds from the surface up to 250 hPa are predominantly northeasterly (panels <b>a</b>–<b>g</b>). Additionally, near the fire site, the surface air was more humid (RH at 60–70%, panels <b>c</b>,<b>f</b>,<b>i</b>), but it was drier in the 850 hPa layer (RH at 10–20%, panels <b>b</b>,<b>e</b>,<b>h</b>), which indicates that the lower tropospheric air (surface to 850 hPa) advected drier air toward the ocean.</p>
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<p>WRF (d02) simulated temperature (shaded; °C) and directions (wind barbs) at various levels during the fire event’s start time between 10/20/15Z and 10/20/18Z, peak time between 10/20/18Z and 10/20/20Z, and extinguishing the next day 10/21/12Z: 250 hPa (<b>a</b>), 850 hPa (<b>b</b>), and 10 m winds above the ground (<b>c</b>) at 10/20/15Z (left panels), 10/20/18Z (middle panels), and 10/21/12Z (right panels). Note that at the fire location (denoted with a black dot), the simulated winds from the surface up to 250 hPa are predominantly northeasterly (panels <b>a</b>–<b>g</b>). Additionally, during the fire’s start time, the surface temperature rose consistently from 24 to 32 °C (75–90 °F) (panels <b>c</b>,<b>f</b>,<b>i</b>), which helped to strengthen the fire intensity, with winds shifting to a south-southwesterly flow during 10/21/12Z (panels <b>h</b>,<b>i</b>), consistent with those observed (<a href="#fire-08-00072-f004" class="html-fig">Figure 4</a>e,f).</p>
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<p>Backward trajectory analysis of air parcels from the NARR meteorological data starting from the fire location (37.86° N, 122.22° W) starting at (<b>a</b>) 1500 UTC Oct 20 (10/20/15Z), 1991, and (<b>b</b>) 10/20/18Z, 1991. They all end at 10/18/12Z, 1991. The analysis indicates that both air parcels near the East Bay Hills originated from northeast, at a level around 850 hPa, where the air was hot, dry, and windy. See text for detailed explanation.</p>
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<p>Cross-section along AB (denoted in the upper-right corner) from the WRF (d01) simulation of wind speeds (shaded; ms<sup>−1</sup>), isentropes (contour lines; K), and wind barbs from 10/20/00Z to 10/21/12Z, 1991, for every 6 or 3 h, as shown on top of each figure panel (<b>a</b>–<b>h</b>). The cross-section line passes through the jet streak’s right exit region and the fire location at 250 hPa level. This analysis indicates that downward motion associated with the jet streak at the exit region is far from the fire location (<b>a</b>–<b>h</b>). Thus, the downslope wind on the lee side of East Bay Hills did not seem to be affected by the jet streak directly.</p>
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<p>Vertical cross-section at the lee side of Sierra Nevada using the WRF (d02) simulation of (<b>a</b>) isotachs (shaded; ms<sup>−1</sup>) and isentropes (contour lines; K), (<b>b</b>) isentropes (shaded; K), and (<b>c</b>) TKE (shaded; m<sup>2</sup>s<sup>−2</sup>) and isentropes (contour lines; K) from 10/20/06Z to 10/20/18Z. CL and HJ represent critical level and hydraulic jump, respectively. Note that the three distinct stages for forming severe downslope winds, as proposed in the resonant amplification mechanism [<a href="#B13-fire-08-00072" class="html-bibr">13</a>,<a href="#B38-fire-08-00072" class="html-bibr">38</a>], and the hydraulic jump and well-mixed (dead) region, as proposed in the hydraulic jump mechanism [<a href="#B14-fire-08-00072" class="html-bibr">14</a>], can be identified in this analysis. Detailed discussions can be found in the relevant text.</p>
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<p>Cross-section along line CD (indicated in the upper-left panel) from the WRF (d02) simulation of isotachs (shaded; ms<sup>−1</sup>), isentropes (contour lines; K), and wind barbs. The red dashed lines represent the level where wind reversal occurs. The two horizontal lines are critical level heights calculated using CP84’s resonant amplification (upper) and S85’s hydraulic mechanisms (upper and lower). This analysis implies that the resonant amplification and hydraulic jump mechanisms were responsible for the severe downslope wind formation in the wildfire event in Oakland, California. The panels illustrate the fire’s ignition, escalation, and eventual extinction. The establishment of critical level (<b>a</b>) prompted the emergence of a wave breaking (<b>b</b>). The depth of the internal hydraulic jump increases (<b>c</b>), followed by the formation of intense downslope winds through resonance (panels <b>d</b>,<b>e</b>). Eventually, these winds diminished, and weaker winds are observed on the leeside of the Sierra Nevada, coinciding with the period when the fire was contained (panels <b>f</b>–<b>h</b>). Detailed discussions can be found in the text.</p>
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<p>Cross-section along line CD (denoted in <a href="#fire-08-00072-f011" class="html-fig">Figure 11</a>) from the WRF (d02) simulated temperature (shaded; °C), isentropes (contour lines; K), and wind barbs from 10/20/03Z to 10/21/03Z. Note that the high-temperature layer near the surface (<b>a</b>,<b>b</b>) at the Central Valley became relatively colder than the air above (~2 km) (<b>c</b>–<b>e</b>), due to the sinking air motion associated with the high-pressure system extending southwestwards from the Great Basin offshore decreases the depth of the marine layer. Panels (<b>f</b>–<b>h</b>) illustrate that wind speeds decreased, revealing weaker winds on the leeside of the Sierra Nevada when the fire was contained. Refer to the text for a more detailed discussion.</p>
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<p>Cross-section along line CD (denoted in <a href="#fire-08-00072-f011" class="html-fig">Figure 11</a>) from the WRF (d02) simulated RH (shaded; %), isentropes (contour lines; K), and wind barbs from 10/20/03Z to 10/21/03Z. Along with <a href="#fire-08-00072-f012" class="html-fig">Figure 12</a>, the sinking air motion associated with the high-pressure system extending southwestwards from the Great Basin offshore leads to the destruction of the marine boundary layer and then a warmer and drier air at the surface. Strong winds are seen at the lee side of the Sierra Nevada, which transports dry air over the Central Valley of California to the East Bay Hills area (Panels <b>a</b>–<b>e</b>). Panels (<b>f</b>–<b>h</b>) illustrate that wind speeds decreased, revealing weaker winds on the leeside of the Sierra Nevada when the fire was contained. See detailed discussions in the text.</p>
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<p>Maximum HDW (shaded) using WRF (d02) simulated data from 10/20/15Z to 10/21/12Z. The black dot indicates the fire location (122.22 W, 37.86 N). Note that the highest HDW occurred at the fire location (black shaded circle) on 10/20/15Z (<b>a</b>), which set the pace for a favorable wildfire that started around 10/20/1740Z (<b>b</b>). This high–HDW created favorable conditions for the wildfire, which ignited around 10:40 PDT (1740 UTC) on 20 October 1991. The elevated HDW indicates how the fire spread and affected Berkeley and surrounding areas. Subsequently, HDW gradually decreased at the fire location until 17:00 PDT on 20 October (10/21/00Z) (<b>c</b>,<b>d</b>). At 20:00 PDT on the same day (10/21/03Z) (<b>e</b>), the HDW increased again, likely due to daytime heating. Following this, the HDW diminished once more, coinciding with the time the fire was contained (<b>f</b>–<b>h</b>).</p>
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<p>Time series of the HDW using WRF (d02) simulated data at the fire location (122.22 W, 37.86 N) from 10/20/15Z to 10/21/12Z. Along with <a href="#fire-08-00072-f014" class="html-fig">Figure 14</a>, the high HDW set the pace for favorable wildfire conditions, which started around 10/20/1740Z, 1991. At 10/21/03Z, the HDW increased again due to daytime heating. Later, the HDW reduced until the end of the simulation period.</p>
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<p>Vertical cross-section from the WRF (d03) simulation of isotachs (shaded; ms<sup>−1</sup>), isentropes (contour lines; K), and wind barbs from 10/20/15Z to 10/21/06Z. The cross-section is along line CD (denoted in <a href="#fire-08-00072-f011" class="html-fig">Figure 11</a>). The establishment of critical level prompted the emergence of a wave breaking. The depth of the internal hydraulic jump increases followed by the formation of intense downslope winds through resonance (panels <b>a</b>,<b>b</b>). Eventually, these winds diminished, and weaker winds are observed on the leeside of the Sierra Nevada, coinciding with the period when the fire was contained (panels <b>c</b>–<b>f</b>).</p>
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<p>Vertical cross-section from the WRF (d03) simulation of temperature (shaded; °C), isentropes (contour lines; K), and wind barbs from 10/20/15Z to 10/21/06Z. The cross-section is along line CD (denoted in <a href="#fire-08-00072-f011" class="html-fig">Figure 11</a>). Note that at the Central Valley temperatures became relatively colder than the air above (~2 km) (<b>a</b>,<b>b</b>), due to the sinking air motion associated with the high-pressure system extending southwestwards from the Great Basin offshore decreases the depth of the marine layer. Panels (<b>c</b>–<b>f</b>) illustrate that wind speeds decreased, revealing weaker winds on the leeside of the Sierra Nevada when the fire was contained.</p>
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<p>Vertical cross-section from the WRF (d03) simulation of RH (shaded; %), isentropes (contour lines; K), and wind barbs from 10/20/15Z to 10/21/06Z. The cross-section is along line CD (denoted in <a href="#fire-08-00072-f011" class="html-fig">Figure 11</a>). Strong winds are seen at the lee side of the Sierra Nevada, which transports dry air over the Central Valley of California to the East Bay Hills area (Panels <b>a,b</b>). Panels (<b>c</b>–<b>f</b>) illustrate that wind speeds decreased, revealing weaker winds on the leeside of the Sierra Nevada when the fire was contained.</p>
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22 pages, 9741 KiB  
Article
Assessing Green Strategies for Urban Cooling in the Development of Nusantara Capital City, Indonesia
by Radyan Putra Pradana, Vinayak Bhanage, Faiz Rohman Fajary, Wahidullah Hussainzada, Mochamad Riam Badriana, Han Soo Lee, Tetsu Kubota, Hideyo Nimiya and I Dewa Gede Arya Putra
Climate 2025, 13(2), 30; https://doi.org/10.3390/cli13020030 - 31 Jan 2025
Abstract
The relocation of Indonesia’s capital to Nusantara in East Kalimantan has raised concerns about microclimatic impacts resulting from proposed land use and land cover (LULC) changes. This study explored strategies to mitigate these impacts by using dynamical downscaling with the Weather Research and [...] Read more.
The relocation of Indonesia’s capital to Nusantara in East Kalimantan has raised concerns about microclimatic impacts resulting from proposed land use and land cover (LULC) changes. This study explored strategies to mitigate these impacts by using dynamical downscaling with the Weather Research and Forecasting model integrated with the urban canopy model (WRF-UCM). Numerical experiments at a 1 km spatial resolution were used to evaluate the impacts of green and mitigation strategies on the proposed master plan. In this process, five scenarios were analyzed, incorporating varying proportions of blue–green spaces and modifications to building walls and roof albedos. Among them, scenario 5, with 65% blue–green spaces, exhibited the highest cooling potential, reducing average urban surface temperatures by approximately 2 °C. In contrast, scenario 4, which allocated equal shares of built-up areas and mixed forests (50% each), achieved a more modest reduction of approximately 1 °C. The adoption of nature-based solutions and sustainable urban planning in Nusantara underscores the feasibility of climate-resilient urban development. This framework could inspire other cities worldwide, showcasing how urban growth can align with environmental sustainability. Full article
(This article belongs to the Special Issue Applications of Smart Technologies in Climate Risk and Adaptation)
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Figure 1

Figure 1
<p>Study area map representing (<b>a</b>) Indonesia and the domains for the Weather Research and Forecast (WRF) model and the location of the Nusantara capital city and (<b>b</b>) the location of the government center core area (KIPP), the main area of Nusantara (KIKN), and the entire area, including the Nusantara capital city future development plan (IKN) and the actual land use and land cover (LULC) classes across the Nusantara region.</p>
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<p>Variations in the LULC data for the KIKN area used for the WRF numerical simulations: (<b>a</b>) scenario 1 (before development); (<b>b</b>) scenario 2, representing the baseline (50% greenery and 50% urban); (<b>c</b>) scenario 3 (50% grasslands and 50% urban); (<b>d</b>) scenario 4 (50% mixed forest and 50% urban); (<b>e</b>) scenario 5 (65% greenery and 35% urban); (<b>f</b>) scenario 6 (35% greenery and 65% urban).</p>
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<p>Spatial distributions of LULC (left column) and category-wise surface air temperature probability distributions (right column) at 01:00 and 16:00 local time for the Nusantara area domain for different scenarios: scenario 1 (<b>a</b>,<b>b</b>), scenario 2 (<b>c</b>,<b>d</b>), scenario 3 (<b>e</b>,<b>f</b>), scenario 4 (<b>g</b>,<b>h</b>), scenario 5 (<b>i</b>,<b>j</b>), and scenario 6 (<b>k</b>,<b>l</b>). The dashed lines indicate the north–south (NS) and east–west (EW) cross-sections used in <a href="#climate-13-00030-f004" class="html-fig">Figure 4</a>.</p>
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<p>Differences in surface air temperature (Temp) and wind speed (WS) at 01:00 and 16:00 local time at the east–west (EW) and north–south (NS) cross-sections before (scenario 1) and after (scenarios 2–6) Nusantara city development; Temp and WS differences (<b>a</b>) between scenario 1 and scenario 2, (<b>b</b>) between scenario 1 and scenario 3, (<b>c</b>) between scenario 1 and scenario 4, (<b>d</b>) between scenario 1 and scenario 5, and (<b>e</b>) between scenario 1 and scenario 6. <a href="#climate-13-00030-f003" class="html-fig">Figure 3</a> shows the locations of the EW and NS cross-sections. The mitigation measures were incorporated into scenarios 2–6 by adjusting the albedo values to 0.8 for roofs and 0.7 for walls. (For references to color blocks in this figure legend, please see <a href="#climate-13-00030-f003" class="html-fig">Figure 3</a>).</p>
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<p>Comparisons of the simulated surface air temperature (Temp) and wind speed (WS) from scenario 2 at 01:00 and 16:00 local time along (<b>A</b>) EW1, (<b>B</b>) EW2, (<b>C</b>) NS1, and (<b>D</b>) NS2 cross-sections and (<b>E</b>) the LULC pattern of scenario 2 with the locations of the cross-sections.</p>
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<p>Comparison of the average hourly surface air temperature over computational domain 3 for various scenarios (<b>a</b>) with water bodies, (<b>b</b>) without water bodies, and (<b>c</b>) the difference in air temperature between (<b>b</b>) and (<b>a</b>).</p>
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<p>(<b>a</b>) Observed monthly variations in rainfall and surface air temperature in the study area from Jan 2016–Dec 2020, and (<b>b</b>) the highest average surface air temperature occurred on 21 October 2020 during the five-year period, as indicated by the red circle.</p>
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<p>Paired comparison of simulated surface air temperature with wind speed before and after Nusantara city development: scenario 2 (<b>a</b>,<b>b</b>), scenario 3 (<b>c</b>,<b>d</b>), scenario 4 (<b>e</b>,<b>f</b>), scenario 5 (<b>g</b>,<b>h</b>), and scenario 6 (<b>i</b>,<b>j</b>). (For references to color blocks in this figure legend, please see <a href="#climate-13-00030-f003" class="html-fig">Figure 3</a>).</p>
Full article ">Figure A2 Cont.
<p>Paired comparison of simulated surface air temperature with wind speed before and after Nusantara city development: scenario 2 (<b>a</b>,<b>b</b>), scenario 3 (<b>c</b>,<b>d</b>), scenario 4 (<b>e</b>,<b>f</b>), scenario 5 (<b>g</b>,<b>h</b>), and scenario 6 (<b>i</b>,<b>j</b>). (For references to color blocks in this figure legend, please see <a href="#climate-13-00030-f003" class="html-fig">Figure 3</a>).</p>
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<p>Spatial wind patterns at 01:00 and 16:00 local time on 21 October 2020. (For references to color blocks in this figure legend, please see <a href="#climate-13-00030-f003" class="html-fig">Figure 3</a>).</p>
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28 pages, 10473 KiB  
Article
Urbanization Effect on Local Summer Climate in Arid Region City of Urumqi: A Numerical Case Study
by Aerzuna Abulimiti, Yongqiang Liu, Qing He, Ali Mamtimin, Junqiang Yao, Yong Zeng and Abuduwaili Abulikemu
Remote Sens. 2025, 17(3), 476; https://doi.org/10.3390/rs17030476 - 30 Jan 2025
Abstract
The urbanization effect (UE) on local or regional climate is a prominent research topic in the research field of urban climates. However, there is little research on the UE of Urumqi, a typical arid region city, concerning various climatic factors and their spatio–temporal [...] Read more.
The urbanization effect (UE) on local or regional climate is a prominent research topic in the research field of urban climates. However, there is little research on the UE of Urumqi, a typical arid region city, concerning various climatic factors and their spatio–temporal characteristics. This study quantitatively investigates the UE of Urumqi on multiple climatic factors in summer based on a decade-long period of WRF–UCM (Weather Research and Forecasting model coupled with the Urban Canopy Model) simulation data. The findings reveal that the UE of Urumqi has resulted in a reduction in the diurnal temperature range (DTR) within the urban area by causing an increase in night-time minimum temperatures, with the maximum decrease reaching −2.5 °C. Additionally, the UE has also led to a decrease in the water vapor mixing ratio (WVMR) and relative humidity (RH) at 2 m, with the maximum reductions being 0.45 g kg−1 and −6.5%, respectively. Furthermore, the UE of Urumqi has led to an increase in planetary boundary layer height (PBLH), with a more pronounced effect in the central part of the city than in its surroundings, reaching a maximum increase of over 750 m at 19:00 Local Solar Time (LST, i.e., UTC + 6). The UE has also resulted in an increase in precipitation in the northern part of the city by up to 7.5 mm while inhibiting precipitation in the southern part by more than 6 mm. Moreover, the UE of Urumqi has enhanced precipitation both upstream and downstream of the city, with a maximum increase of 7.9 mm. The UE of Urumqi has also suppressed precipitation during summer mornings while enhancing it in summer afternoons. The UE has exerted certain influences on the aforementioned climatic factors, with the UE varying across different directions for each factor. Except for precipitation and PBLH, the UE on the remaining factors exhibit a greater magnitude in the northern region compared to the southern region of Urumqi. Full article
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Figure 1
<p>(<b>a</b>) Geographical locations and terrain altitude (colorful shading, units: m) of the study area; the boundary of the major urban and built-up area of Urumqi is indicated by the closed irregular area with a thick blue solid line, and the gray solid lines indicate the administrative boundaries of Urumqi and its districts. The location of the study area is also indicated by the small red box from a broader perspective in the little globe in the upper left corner of this panel. (<b>b</b>) Terrain altitude (colorful shading, units: m) from an enlarged scope of the study area, showing the locations of the 51 weather stations (pointed out by black dots) selected in this present study to verify the results of the numerical simulation. Further, the small red target symbol with a cross and dot in the central area indicates the location of the central point of the urban area. The red square areas indicate the immediate areas in various orientations around the central point of the urban and build-up area, i.e., NW (northwestern), N (northern), NE (northeastern), W (western), C (central), E (eastern), S (southern), and SE (southeastern) areas, respectively. The outline of the urban area is indicated by the closed irregular area with a thick blue solid line.</p>
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<p>The technical flow chart regarding the data, methods, and results of this study.</p>
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<p>(<b>a</b>) The land surface (land use) categories (colorful shading) obtained from the CLCD dataset of the urban (control) experiment of the WRF–UCM simulation. Here, (<b>b</b>) is the same as (<b>a</b>) but for the non-urban (sensitivity) experiment of the simulation in which the urban areas are substituted by grasslands. The dashed line boxes indicate the area of the plane figure showing spatial distribution of the climatic factors which will be shown in the following.</p>
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<p>Scatter plots with linear regression fitting lines and regression equations and Pearson’s correlation coefficient (r), as well as the root mean square error (RMSE) depicted at the top of each panel, indicating the corresponding simulation results (monthly average value at the 51 meteorological stations shown in <a href="#remotesensing-17-00476-f001" class="html-fig">Figure 1</a>b) with corresponding observational data in July (2012–2021). Here, (<b>a</b>), (<b>b</b>), and (<b>c</b>) indicate the Tmax, Tmin, and precipitation, respectively.</p>
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<p>(<b>a</b>–<b>c</b>) Spatial distribution of the averaged diurnal temperature range (DTR) (colorful shading, unit: °C) in summer from 2012 to 2021 in Urumqi in the urban and non-urban experiments and UE (i.e., values of urban–non-urban) on the Tmean, respectively. The closed irregular area with a thick blue solid line represent the outline of the urban area, and the thinner black lines show the boundaries of districts in Urumqi. The black square areas show the immediate areas in the various orientations of the urban central point of Urumqi, which are also depicted in <a href="#remotesensing-17-00476-f001" class="html-fig">Figure 1</a>b. (<b>d</b>) The average values of the averaged Tmean in summer over the eight immediate areas (calculated over the urban area) in the various orientations of the urban central point. The capital letters on the horizontal axis indicate the eight square areas illustrated in <a href="#remotesensing-17-00476-f001" class="html-fig">Figure 1</a>b, and ALL denotes the average value of all of the urban areas (i.e., the mean value of all eight square areas).</p>
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<p>Here, (<b>a</b>–<b>c</b>) are the same as in <a href="#remotesensing-17-00476-f005" class="html-fig">Figure 5</a>a–c, but for the spatial distribution of the averaged Tmax (colorful shading, unit: °C) in summer from 2012 to 2021 in Urumqi in the urban and non-urban experiments and UE (i.e., values of urban–non-urban) on the Tmax, respectively. Here, (<b>d</b>) is the same as in <a href="#remotesensing-17-00476-f005" class="html-fig">Figure 5</a>d, but for the average values of the averaged Tmax in summer over the nine areas.</p>
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<p>Here, (<b>a</b>–<b>c</b>) are the same as in <a href="#remotesensing-17-00476-f005" class="html-fig">Figure 5</a>a–c but for the spatial distribution of the averaged Tmin (colorful shading, unit: °C) in summer from 2012 to 2021 in Urumqi in the urban and non-urban experiment and UE (i.e., values of urban–non-urban) on the Tmin, respectively. Here, (<b>d</b>) is the same as in <a href="#remotesensing-17-00476-f005" class="html-fig">Figure 5</a>d, but for the average values of the averaged Tmin in summer over the nine areas.</p>
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<p>Here, (<b>a</b>–<b>c</b>) are the same as in <a href="#remotesensing-17-00476-f005" class="html-fig">Figure 5</a>a–c, but for the spatial distribution of the averaged WVMR (colorful shading, unit: g kg<b><sup>−</sup></b><sup>1</sup>) at 2 m in summer from 2012 to 2021 in Urumqi in the urban and non-urban experiments and UE (i.e., values of urban–non-urban) on the WVMR at 2 m, respectively. Here, (<b>d</b>) is the same as in <a href="#remotesensing-17-00476-f005" class="html-fig">Figure 5</a>d, but for the average values of the averaged WVMR at 2 m in summer over the nine areas.</p>
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<p>(<b>a</b>–<b>c</b>) Diurnal variation features of the averaged water vapor mixing ratio (WVMR, unit: g kg<b><sup>−</sup></b><sup>1</sup>) at 2 m in summer from 2012 to 2021 in different square areas in various orientations of the urban central point of Urumqi in the urban and non-urban experiment and UE (i.e., values of urban–non-urban) on the WVMR at 2 m, respectively. The capital letters indicate the corresponding values of WVMR at 2 m calculated in these eight square areas shown in <a href="#remotesensing-17-00476-f001" class="html-fig">Figure 1</a>b, and ALL shows the averaged value of all urban areas.</p>
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<p>Here, (<b>a</b>–<b>c</b>) are the same as in <a href="#remotesensing-17-00476-f005" class="html-fig">Figure 5</a>a–c, but for the spatial distribution of the averaged RH (colorful shading, unit: %) at 2 m in summer from 2012 to 2021 in Urumqi in the urban and non-urban experiment and UE (i.e., values of urban–non-urban) on the RH at 2 m, respectively. Here, (<b>d</b>) is the same as in <a href="#remotesensing-17-00476-f005" class="html-fig">Figure 5</a>d, but for the average values of the averaged RH at 2 m in summer over the nine areas.</p>
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<p>Here, (<b>a</b>–<b>c</b>) is the same as in <a href="#remotesensing-17-00476-f009" class="html-fig">Figure 9</a>a–c but for the averaged RH (unit: %) at 2 m in summer from 2012 to 2021 in different square areas in various orientations of the urban central point of Urumqi in the urban and non-urban experiment and UE (i.e., values of urban–non-urban) on the RH at 2 m, respectively.</p>
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<p>Here, (<b>a</b>–<b>c</b>) are the same as in <a href="#remotesensing-17-00476-f005" class="html-fig">Figure 5</a>a–c, but for the spatial distribution of the averaged PBLH (colorful shading, unit: m) in summer from 2012 to 2021 in the urban and non-urban experiment and UE (i.e., values of urban–non-urban) on the PBLH, respectively. Here, (<b>d</b>) is the same as in <a href="#remotesensing-17-00476-f005" class="html-fig">Figure 5</a>d, but for the average values of the averaged PBLH in summer over the nine areas.</p>
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<p>Here, (<b>a</b>–<b>c</b>) is the same as in <a href="#remotesensing-17-00476-f009" class="html-fig">Figure 9</a>a–c, but for the averaged planetary boundary layer height (PBLH, unit: m) in summer from 2012 to 2021 in different square areas in the various orientations of the central point of urban area in the urban and non-urban experiment and UE (i.e., values of urban–non-urban) on the PBLH, respectively.</p>
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<p>Here, (<b>a</b>–<b>c</b>) are the same as in <a href="#remotesensing-17-00476-f005" class="html-fig">Figure 5</a>a–c, but for the spatial distribution of the average precipitation (colorful shading, unit: mm) in summer from 2012 to 2021 in the urban and non-urban experiment and UE (i.e., values of urban–non-urban) on the precipitation, respectively. Here, (<b>d</b>) is the same as in <a href="#remotesensing-17-00476-f005" class="html-fig">Figure 5</a>d, but for the average values of the average precipitation in summer over the nine areas. The two rectangular areas, delineated by red solid lines and black dashed lines, indicate the northern and eastern suburbs of Urumqi, respectively, where the UE has increased the precipitation.</p>
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<p>Here, (<b>a</b>–<b>c</b>) are the same as in <a href="#remotesensing-17-00476-f005" class="html-fig">Figure 5</a>a–c, but for the spatial distribution of the average precipitation (colorful shading, unit: mm) in summer from 2012 to 2021 in the urban and non-urban experiment and UE (i.e., values of urban–non-urban) on the precipitation, respectively. Here, (<b>d</b>) is the same as in <a href="#remotesensing-17-00476-f005" class="html-fig">Figure 5</a>d, but for the average values of the average precipitation in summer over the nine areas. The two rectangular areas, delineated by red solid lines and black dashed lines, indicate the northern and eastern suburbs of Urumqi, respectively, where the UE has increased the precipitation.</p>
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<p>Here, (<b>a</b>–<b>c</b>) is the same as in <a href="#remotesensing-17-00476-f009" class="html-fig">Figure 9</a>a–c, but for the averaged precipitation (unit: mm) in summer from 2012 to 2021 in various square areas in various orientations of the urban central point of Urumqi in the urban and non-urban experiment and UE (i.e., values of urban–non-urban) on the precipitation, respectively.</p>
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<p>Here, (<b>a</b>–<b>c</b>) is the same as in <a href="#remotesensing-17-00476-f009" class="html-fig">Figure 9</a>a–c, but for the averaged precipitation (unit: mm) in summer from 2012 to 2021 in various square areas in various orientations of the urban central point of Urumqi in the urban and non-urban experiment and UE (i.e., values of urban–non-urban) on the precipitation, respectively.</p>
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11 pages, 233 KiB  
Article
Heart Failure and Worsening Renal Function: Prevalence, Risk Factors, and Impact on Hospital Readmissions in an Urban Minority Population
by Asmaa AlShammari, Mariel Magdits, Rosemarie Majdalani, Sriraman Devarajan, Anna Hughes, Lily McCann, Natalia Ionescu and Farbod Raiszadeh
J. Clin. Med. 2025, 14(3), 877; https://doi.org/10.3390/jcm14030877 - 28 Jan 2025
Abstract
Background and Objectives: Heart failure (HF) often leads to worsening renal function (WRF), negatively impacting patient outcomes. This study aims to examine the incidence of WRF in HF patients, identify its risk factors, and assess its effect on readmissions. Materials and Methods [...] Read more.
Background and Objectives: Heart failure (HF) often leads to worsening renal function (WRF), negatively impacting patient outcomes. This study aims to examine the incidence of WRF in HF patients, identify its risk factors, and assess its effect on readmissions. Materials and Methods: This retrospective analysis included 297 HF patients admitted to Harlem Hospital Center between January 2019 and December 2021. WRF incidence and its association with risk factors, hospital stays, and readmissions were analyzed. Data on age, type 2 diabetes, chronic kidney disease, high-dose furosemide use, and biomarkers (ProBNP, troponin T, creatinine) were collected. A risk-scoring system was developed to identify patients at higher risk for WRF. Results: WRF occurred in 27% of patients, with a significant correlation to longer hospital stays and lower cardiology follow-up adherence. Risk factors for WRF included older age, type 2 diabetes, chronic kidney disease, high-dose furosemide, and elevated ProBNP, troponin T, and creatinine levels. The risk scoring system revealed that patients scoring 6 or higher were four times more likely to develop WRF. Interestingly, WRF did not increase 30-day readmission rates. Conclusions: This study highlights the high incidence of WRF among HF patients, its impact on hospital stays and follow-up adherence, and the utility of a risk-scoring system to identify vulnerable patients. The findings offer valuable insights into improving care in minority-serving hospitals and provide a foundation for future research on WRF in HF patients. Full article
(This article belongs to the Section Cardiovascular Medicine)
28 pages, 17836 KiB  
Article
Study on the Fire Spread Characteristics of High-Rise Building Facades Under Strong Wind Conditions Based on the Combination of WRF and CFD
by Shi Yang, Yanfeng Li, Zhihe Su and Junmei Li
Appl. Sci. 2025, 15(3), 1327; https://doi.org/10.3390/app15031327 - 27 Jan 2025
Abstract
The spread of fires on the facades of high-rise buildings is highly influenced by atmospheric wind conditions, particularly in strong wind environments. A strong wind environment refers to the situation where the wind speed reaches level 6 or above, or the wind speed [...] Read more.
The spread of fires on the facades of high-rise buildings is highly influenced by atmospheric wind conditions, particularly in strong wind environments. A strong wind environment refers to the situation where the wind speed reaches level 6 or above, or the wind speed is between 10.8 m/s and 13.8 m/s. We conducted an in-depth study of the characteristics of flame spread on the facades of high-rise buildings under strong wind conditions. A nested coupling method based on WRF (Weather Research and Forecasting) and CFD (computational fluid dynamics) software (Ansys Fluent 2021) was used. The mesoscale meteorological simulation software WRF was utilized to obtain regional airflow variation data within a radius of 2 km around the high-rise building. Subsequently, these data were coupled with the CFD software (Ansys Fluent 2021) to simulate and obtain realistic wind field data within a 400 m range around the building. Finally, these realistic wind field data were used for FDS (Fire Dynamics Simulator) fire simulations and model experiments to accurately replicate building fire scenarios under strong wind conditions. The results indicate that using grid nesting for boundary condition division would help to improve the accuracy of fire spread characteristics on the facades of high-rise buildings under strong wind conditions. For a high-rise building, both headwinds and tailwinds promote vertical and horizontal flame spread, with a more significant impact on vertical flame spread speed. Side winds enhance horizontal flame spread but inhibit vertical flame spread. These findings provide a reference for the effective design of fire protection systems for the facades of high-rise buildings. Full article
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<p>Fire scenario at the Changsha telecom building.</p>
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<p>Schematic diagram of the building model.</p>
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<p>Schematic of multi-scale nesting.</p>
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<p>Schematic of nesting simulation process.</p>
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<p>WRF regional grid division map.</p>
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<p>WRF plane measurement point map.</p>
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<p>CFD three-dimensional schematic diagram.</p>
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<p>CFD grid diagram.</p>
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<p>FDS building model.</p>
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<p>Grid division diagram.</p>
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<p>Schematic diagram of wind speed extraction plane.</p>
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<p>Schematic diagram of wind direction.</p>
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<p>Three-dimensional diagram of boundary wind speed extraction.</p>
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<p>Temperature variation map above the middle of the building on the ignition surface at 100 s under different grid sizes.</p>
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<p>Comparison of flame spread velocity between model experiment and numerical simulation.</p>
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<p>Comparison of flame spread velocity between model experiment and numerical simulation.</p>
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<p>Comparison of flame spread velocity between model experiment and numerical simulation.</p>
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<p>Wind speed variation with height diagram. (<b>a</b>) At 16:00 on 5 September. (<b>b</b>) At 8:00 on 6 September. (<b>c</b>) At 20:00 on 6 September.</p>
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<p>Schematic diagram of flame propagation of the fire wall under Working Condition 1-1.</p>
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<p>Schematic diagram of flame propagation under Working Condition 1-2.</p>
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<p>Schematic diagram of flame propagation under Working Condition 1-2.</p>
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<p>Schematic diagram of flame propagation under Working Condition 2-1.</p>
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<p>Schematic diagram of flame propagation of the fire wall under Working Condition 2-2.</p>
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<p>Schematic diagram of flame propagation under Working Condition 3-1.</p>
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<p>Schematic diagram of flame propagation of the fire wall under Working Condition 3-2.</p>
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<p>Schematic diagram of flame propagation of the fire wall under Working Condition 3-2.</p>
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<p>Fire spread on the left wall under Working Condition 3-2.</p>
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<p>Flame spread velocity under Working Condition 1-1.</p>
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<p>Flame spread velocity under Working Condition 1-2.</p>
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<p>Flame spread velocity under Working Condition 2-1.</p>
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<p>Flame spread velocity under Working Condition 2-2.</p>
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<p>Flame spread velocity under Working Condition 3-1.</p>
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<p>Flame spread velocity under Working Condition 3-2.</p>
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<p>Temperature changes in fired wall under Working Condition 1-1.</p>
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<p>Temperature changes in fired wall under Working Condition 1-1.</p>
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<p>Temperature changes in fired wall under Working Condition 1-2.</p>
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<p>Temperature changes in fired wall under Working Condition 2-1.</p>
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<p>Temperature changes in fired wall under Working Condition 2-2.</p>
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<p>Temperature changes in fired wall under Working Condition 3-1.</p>
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<p>Temperature changes in fired wall under Working Condition 3-2.</p>
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<p>Temperature changes in fired wall under Working Condition 3-2.</p>
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22 pages, 14231 KiB  
Article
Quantitative Simulation and Planning for the Heat Island Mitigation Effect in Sponge City Planning: A Case Study of Chengdu, China
by Qingjuan Yang, Ziqi Lin and Qiaozi Li
Land 2025, 14(2), 264; https://doi.org/10.3390/land14020264 - 26 Jan 2025
Abstract
The implementation of sponge cities in China modifies the hydrological conditions of the underlying surface, effectively alleviating the urban heat island effect. However, in planning and construction, heat island mitigation targets are difficult to quantify and lack quantitative design and evaluation methods. To [...] Read more.
The implementation of sponge cities in China modifies the hydrological conditions of the underlying surface, effectively alleviating the urban heat island effect. However, in planning and construction, heat island mitigation targets are difficult to quantify and lack quantitative design and evaluation methods. To address this issue, two planning schemes were proposed based on sponge city management and control indicators. The WRF-UCM model was used to conduct numerical simulations of the current conditions (case 1) and the sponge city planning schemes (cases 2 and 3), analyzing the impact of sponge city initiatives on the mitigation of the heat island effect. The results indicated that by changing the structure of the underlying surface and increasing the water content of the underlying surface, the sponge city affects the urban energy distribution process and regional horizontal advection pattern. This not only reduces heat accumulation within the urban area but also suppresses regional convection during high-temperature periods, thereby mitigating the urban heat island effect. Moreover, different schemes following the same sponge city design requirements have varying impacts on urban microclimate elements and heat island distributions. Notably, a higher subsurface water content yields a more pronounced inhibition of the heat island effect. Finally, a sponge city planning method with the consideration of heat island mitigation was proposed, facilitating pre-simulation optimization and decision-making in sponge city planning. Full article
(This article belongs to the Special Issue Land Use Planning, Sustainability and Disaster Risk Reduction)
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<p>Simulation nested domain setup and study area location map.</p>
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<p>Classification of urban underlying surface and building information in the study area based on sponge city control zoning.</p>
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<p>Comparison validation of air temperature 2 m above ground level between on-site measurements and WRF-UCM simulation results.</p>
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<p>Comparison of microclimate factors in each case: (<b>a</b>) air temperature at 2 m above the ground (T2); (<b>b</b>) air specific humidity at 2 m above the ground (Q2); (<b>c</b>) wind speed at 10 m above the ground (UV10).</p>
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<p>Comparison of air temperature 2 m above the ground for case 1, case 2, and case 3 at 08:00 and 17:00 local time on 5 July 2015. Case 1 was the base case, or the current situation of land use in Chengdu; case 2 was a sponge city planning and design scheme with a green roof rate of 0.6; case 3 was a sponge city planning and design scheme with a green roof ratio of 0.8.</p>
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<p>Location of urban center sampling points and suburban sampling points.</p>
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<p>Comparison of heat island intensity in each case.</p>
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<p>Comparison of air temperature 2 m above the ground (T2) in different management and control zones for (<b>a</b>) case 1; (<b>b</b>) case 2; and (<b>c</b>) case 3.</p>
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<p>Comparison of average energy elements of case 1, case 2, and case 3 in different regions on 5 July 2015: (<b>a</b>) net radiation (R<sub>n</sub>); (<b>b</b>) latent heat flux (LE); (<b>c</b>) sensible heat flux (H); (<b>d</b>) surface heat flux (G<sub>0</sub>).</p>
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<p>Comparison of the air temperature 2 m above the ground and the wind direction 10 m above the ground for case 1, case 2, and case 3 at 24:00.</p>
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<p>Sponge city planning method based on the heat island mitigation target.</p>
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22 pages, 12425 KiB  
Article
Sea Clutter Suppression Method Based on Ocean Dynamics Using the WRF Model
by Guigeng Li, Zhaoqiang Wei, Yujie Chen, Xiaoxia Meng and Hao Zhang
J. Mar. Sci. Eng. 2025, 13(2), 224; https://doi.org/10.3390/jmse13020224 - 25 Jan 2025
Viewed by 140
Abstract
Sea clutter introduces a significant amount of non-target reflections in the echo signals received by radar, complicating target detection and identification. To address the challenge of existing filter parameters being unable to adapt in real-time to the characteristics of sea clutter, this paper [...] Read more.
Sea clutter introduces a significant amount of non-target reflections in the echo signals received by radar, complicating target detection and identification. To address the challenge of existing filter parameters being unable to adapt in real-time to the characteristics of sea clutter, this paper integrates ocean numerical models into the sea clutter spectrum estimation. By adjusting filter parameters based on the spectral characteristics of sea clutter, the accurate suppression of sea clutter is achieved. In this paper, the Weather Research and Forecasting (WRF) model is employed to simulate the ocean dynamic parameters within the radar detection area. Hydrological data are utilized to calibrate the parameterization scheme of the WRF model. Based on the simulated ocean dynamic parameters, empirical formulas are used to calculate the sea clutter spectrum. The filter coefficients are updated in real-time using the sea clutter spectral parameters, enabling precise suppression of sea clutter. The suppression algorithm is validated using X-band radar-measured sea clutter data, demonstrating an improvement factor of 17.22 after sea clutter suppression. Full article
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<p>Block diagram of sea clutter suppression based on ocean dynamics.</p>
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<p>Schematic of the X-band radar. (<b>a</b>) The placement of the X-band radar. (<b>b</b>) Actual photograph of the X-band radar.</p>
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<p>Range–pulse distribution of the X-band radar data.</p>
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<p>Schematic of the IPIX radar. (<b>a</b>) The placement of the IPIX radar. (<b>b</b>) Actual photograph of the IPIX radar.</p>
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<p>Range–pulse distribution under different polarization modes. (<b>a</b>) HH polarization. (<b>b</b>) VV polarization.</p>
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<p>Doppler spectrum of IPIX measured sea clutter data.</p>
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<p>Time–Doppler diagram of sea clutter.</p>
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<p>Taylor diagram of the parameterization results for different mp_physics schemes.</p>
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<p>Simulation of WRF model grid over the X-band radar detection area. The red upward triangle indicates the radar installation location.</p>
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<p>The WRF model grid over the IPIX radar detection area. The red upward triangle indicates the radar installation location.</p>
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<p>Comparison of ocean dynamic parameters obtained from WRF simulations with measured data.</p>
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<p>Measured power spectrum of pure clutter signal.</p>
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<p>Magnitude and phase responses of the FIR filter.</p>
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<p>Wavelet and EMD reconstruction suppression algorithm. (<b>a</b>) Wavelet transform-weighted reconstruction. (<b>b</b>) EMD reconstruction.</p>
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<p>Power spectrum before and after sea clutter suppression.</p>
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<p>Range–Doppler diagrams of radar before and after sea clutter suppression.</p>
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<p>Correspondence between improvement factor and target signal frequency.</p>
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20 pages, 33607 KiB  
Article
Unprecedented Flooding in the Marche Region (Italy): Analyzing the 15 September 2022 Event and Its Unique Meteorological Conditions
by Nazario Tartaglione
Meteorology 2025, 4(1), 3; https://doi.org/10.3390/meteorology4010003 - 23 Jan 2025
Viewed by 303
Abstract
On 15 September 2022, a flood affected the Marche region, an Italian region that faces the Adriatic Sea. Unlike previous floods that affected the same area, no typical weather system, such as cyclones or synoptic fronts, caused the recorded extreme precipitation. In fact, [...] Read more.
On 15 September 2022, a flood affected the Marche region, an Italian region that faces the Adriatic Sea. Unlike previous floods that affected the same area, no typical weather system, such as cyclones or synoptic fronts, caused the recorded extreme precipitation. In fact, the synoptic situation was characterized by a zonal flow, which normally does not cause intense precipitation over that area. The aim of this study was to understand which ingredients led to extraordinary precipitation in the region. ERA5 and the Weather Research Forecast (WRF) model were used to describe the synoptic situation and to reproduce rainfall. While limited area models with a horizontal resolution of a few km failed to forecast the precipitation, as confirmed by a WRF simulation with a horizontal resolution of 3 km, reducing the horizontal grid spacing to about 500 m improved the rain’s reproducibility. Together with a zonal flow that interested most of Italy, an atmospheric river starting in the eastern Mediterranean Sea transported moisture over the region. The interaction between the zonal flow and orography resulted in frontogenesis in the Apennine Lee. This process deformed the thermal structures in the area and created conditions of convective instability, transforming the moisture into copious rainfall. Moreover, ERA5 and the time series of observed rainfall from 1959 to 2022 were used to explore whether similar events, in terms of geopotential height configuration and rainfall, occurred in the past. Three metrics were employed to compare the event’s 700 hPa geopotential height pattern with all the other patterns, and the result was that the event was unique in the sense that a zonal flow, like that observed during the event of 15 September 2022, had never produced such an amount of precipitation in the time range considered, while all the events with the highest rainfall were usually associated with cyclonic structures. Full article
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<p>Topographic map of the region affected by the flood of 15 September 2022 with locality names underlined, while the names of the rivers are not. <a href="#meteorology-04-00003-f0A1" class="html-fig">Figure A1</a> shows the location of the Marche region in Europe.</p>
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<p>The isohyet map for rainfall recorded on 15 September 2022 using Marche rain gauges.</p>
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<p>The ERA5 specific humidity (g/kg) at 850 hPa (shaded) and the geopotential height (dam) at 500 hPa (dotted lines) and 700 hPa (solid lines) at 12 UTC on 15 September 2022.</p>
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<p>The mean sea level pressure (contour), ERA5 wind at 500 hPa and 700 hPa, and wind shear at 12 UTC on 15 September 2022.</p>
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<p>The ERA5 temperature at 500 hPa (shaded) and 700 hPa (contour) at 12 UTC on 15 September 2022.</p>
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<p>Frontogenesis (k (100 km)<sup>−1</sup> (3 h)<sup>−1</sup>); equivalent potential temperature (K) at 700 hPa at 12 (<b>a</b>), 15 (<b>b</b>), and 18 (<b>c</b>) UTC on 15 September 2022.</p>
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<p>Accumulated rainfall over 24 h on 15 September 2022, from the WRF simulation at a 3 km × 3 km grid resolution. The gray lines denote the administrative boundaries. The locations of Cantiano and Senigallia are also shown.</p>
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<p>Accumulated rainfall over 24 h on 15 September 2022, from the WRF simulation at a 0.55 km × 0.55 km grid resolution. The gray lines denote the administrative boundaries. The locations of Cantiano and Senigallia are also shown. The cross-sectional analysis took place on the black line.</p>
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<p>Equivalent potential temperature (K) and simulated reflectivity at 13 (<b>a</b>), 15 (<b>b</b>), and 17 (<b>c</b>) UTC as simulated by WRF having a 0.55 km horizontal resolution. The cross section was taken along the black line in <a href="#meteorology-04-00003-f008" class="html-fig">Figure 8</a>. The red and blue vertical lines are the locations of Cantiano and Senigallia, respectively.</p>
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<p>ERA5 700 hPa geopotential height (contours, in dam) and specific humidity at 850 hPa (shading, in g/kg) of the events that resemble the event that occurred on 15 September 2022, using the metrics M1, M2, and M3 (see text). The bottom row displays the events that exhibit similarities based on the metrics M1 and M2. The event that took place on 23 May 2021 bears the greatest resemblance to the reference event.</p>
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<p>The ERA5 700 hPa geopotential height (contours, in dam) and specific humidity at 850 hPa (shading, in g/kg) that contributed to precipitation exceeding 95 mm at the Cantiano station. On 15 September 2022, the station recorded 419 mm of rainfall. All the other events are arranged chronologically.</p>
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<p>Topography of the European region and toponyms used in the article. The red line delimits Italy, the gray line delimits the Marche region, and the black line indicates the Line of the Apennines.</p>
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<p>WRF domains, with green and orange boxes used in WRF having 9 km × 9 km and 3 km × 3 km horizontal resolutions; black, blue, and red are for the very high-resolution (8.8, 2.2, and 0.55 km horizontal resolutions) WRF and domain used for searching events similar to the one that occurred on 15 September 2022 in ERA5 data (pink box).</p>
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19 pages, 4625 KiB  
Article
Impacts of Physical Parameterization Schemes on Typhoon Doksuri (2023) Forecasting from the Perspective of Wind–Wave Coupling
by Lihua Li, Bo Peng, Weiwen Wang, Ming Chang and Xuemei Wang
J. Mar. Sci. Eng. 2025, 13(2), 195; https://doi.org/10.3390/jmse13020195 - 21 Jan 2025
Viewed by 451
Abstract
Tropical cyclones (TCs) form over warm ocean surfaces and are driven by complex air–sea interactions, posing significant challenges to their forecasting. Accurate parameterization of physical processes is crucial for enhancing the precision of TC predictions. In this study, we employed the Weather Research [...] Read more.
Tropical cyclones (TCs) form over warm ocean surfaces and are driven by complex air–sea interactions, posing significant challenges to their forecasting. Accurate parameterization of physical processes is crucial for enhancing the precision of TC predictions. In this study, we employed the Weather Research and Forecasting model coupled with the Simulating Waves Nearshore (WRF-SWAN) model to forecast Typhoon Doksuri (2023), which exhibited a secondary intensification process in the South China Sea (SCS). We also investigated its sensitivity to various atmospheric physical parameterization schemes (PPS). The findings indicate that improvements in microphysical and cumulus convection parameterizations have significantly enhanced the prediction accuracy of Typhoon Doksuri’s trajectory and intensity. The simulation of sea surface heat flux is primarily influenced by the microphysical scheme, while the cumulus convection scheme substantially affects the representation of the typhoon core’s size and shape. Variations in the wind field induce differences in wave height, potentially reaching up to 2–3 m at any given moment. This study provides valuable insights into the effective selection of physical parameterizations for improving typhoon forecasts. Full article
(This article belongs to the Section Ocean and Global Climate)
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<p>Nested regions for WRF and SWAN. (<b>a</b>) WRF_d01 refers to the outermost domain, WRF_d02 and SWAN domain are indicated by the red box, and the innermost region represents the WRF_d03 (moving nest). (<b>b</b>) SWAN’s regional grid resolution is set at 186 × 129, and the Lambert projection is consistent with WRF. (<b>c</b>) Bathymetric field input to SWAN.</p>
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<p>Track of Doksuri with every 3 or 6 h from 26 July 2023 0000 UTC to 28 July 2023 0600 UTC. The best track from CMA is represented by black, the colors for other experiment groups are shown in the legend. The dots represent the center location of TC. Parts of dates for CMA are indicated by arrows and fonts.</p>
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<p>MSLP and MWS time series of Doksuri every 3 or 6 h from 26 July 2023 0000 UTC to 28 July 2023 0600 UTC. The results from CMA are represented by black; the colors for other experiment groups are shown in the legend.</p>
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<p>Wind field in 10 m of Doksuri for each group at 0000 UTC on 27 July. Colored areas indicate sea level pressure, and wind plumes indicate wind speed and direction, the tail of wind plumes indicates the direction of the wind’s source, the horizontal short line represents a wind speed of 2 m/s, the long line represents a wind speed of 4 m/s, and the flag represents a wind speed of 20 m/s.</p>
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<p>The average latent heat flux of Doksuri for each group between 0000 UTC on 27 July and 0000 UTC on 28 July. The value displayed in the lower right-hand corner represents the maximum value of average latent heat flux.</p>
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<p>The average sensible heat flux of TC Doksuri for each group between 0000 UTC on 27 July and 0000 UTC on 28 July. The value displayed in the lower right-hand corner represents the maximum value of average sensible heat flux.</p>
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<p>The wind fields in 10 m of CTL_coupling and C2_coupling at 0000 UTC on 27 July, 1200 UTC on 27 July, and 0000 UTC on 28 July. Colored areas indicate wind speed values distribution, and wind plumes indicate wind speed and direction, the tail of wind plumes indicates the direction of the wind’s source, the horizontal short line represents a wind speed of 2 m/s, the long line represents a wind speed of 4 m/s, and the flag represents a wind speed of 20 m/s.</p>
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<p>The difference in wind speed field (left column) and wind direction field (right column) between C2_coupling and CTL_coupling at 0000 UTC on 27 July, 1200 UTC on 27 July, and 0000 UTC on 28 July.</p>
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<p>Comparison of the sea surface wave height field for CTL_coupling and C2_coupling at 0000 UTC on 27 July, 1200 UTC on 27 July, and 0000 UTC on 28 July. The third column represents the difference between C2_coupling and CTL_couping.</p>
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18 pages, 8177 KiB  
Technical Note
The Weather On-Demand Framework
by Ólafur Rögnvaldsson, Karolina Stanislawska and João A. Hackerott
Atmosphere 2025, 16(1), 91; https://doi.org/10.3390/atmos16010091 - 15 Jan 2025
Viewed by 832
Abstract
This paper describes the Weather On-Demand (WOD) forecasting framework which is a software stack used to run operational and on-demand weather forecasts. The WOD framework is a distributed system for the following: (1) running the Weather Research and Forecast (WRF) model for data [...] Read more.
This paper describes the Weather On-Demand (WOD) forecasting framework which is a software stack used to run operational and on-demand weather forecasts. The WOD framework is a distributed system for the following: (1) running the Weather Research and Forecast (WRF) model for data assimilation and forecasts by triggering either scheduled or on-demand jobs; (2) gathering upstream weather forecasts and observations from a wide variety of sources; (3) reducing output data file sizes for permanent storage; (4) making results available through Application Programming Interfaces (APIs); (5) making data files available to custom post-processors. Much effort is put into starting processing as soon as the required data become available, and in parallel where possible. In addition to being able to create short- to medium-range weather forecasts for any location on the globe, users are granted access to a plethora of both global and regional weather forecasts and observations, as well as seasonal outlooks from the National Oceanic and Atmospheric Administration (NOAA) in the USA through WOD integrated-APIs. All this information can be integrated with third-party software solutions via WOD APIs. The software is maintained in the Git distributed version control system and can be installed on suitable hardware, bringing the full flexibility and power of the WRF modelling system to the user in a matter of hours. Full article
(This article belongs to the Section Atmospheric Techniques, Instruments, and Modeling)
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Figure 1
<p>Diagram of essential components of the WOD system and their interconnections. See text for further details.</p>
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<p>Volcanic cloud (<b>top panel</b>) emanating from the Mt. Fagradalsfjall eruption, SW Iceland, on 30 May 2021 (photo courtesy of Kristján Sævald) and a dispersion forecast (<b>bottom panel</b>) of SO<sub>2</sub> at 500 m AGL, valid at the time of the photoshoot, created by the WOD system. The red star shows the approximate location from where the photo was taken.</p>
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<p>Example of how the location of observation sides in Iceland, from a wide range of providers, can be presented within the WOD framework. Screenshot taken from <a href="https://obs.belgingur.is" target="_blank">https://obs.belgingur.is</a> on 11 July 2024.</p>
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<p>Comparison between observations (<b>left</b>) of 24 h rainfall [mm/day] over South America on 19 January 2023 estimated by the MERGE system of the Brazilian Centre for Weather Forecast and Climatic Studies (CPTEC in Portuguese), the results of a one-day-ahead WOD system with data assimilation (<b>centre</b>), and the same results without data assimilation (<b>right</b>). Areas limit the main hydro basins used for hydropower in Brazil, and numbers show the average precipitation over each basin. Numbers in red are precipitation significantly below daily average, while blues are significantly above daily average. Red circles highlight the regions where precipitation has the greatest impact on the Brazilian electric sector and where we identified the most significant improvements using the data assimilation system.</p>
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<p>Example of a power production forecast where WOD model output has been post-processed using a novel machine learning software that takes observed winds and power production, among other factors, into account.</p>
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<p>Example of a typical landing page for the graphical user interface (GUI) of the WOD API.</p>
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<p>Step two in running an on-demand forecast; click the encircled <tt>/meta/job</tt> button.</p>
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<p>The user now types in the latitude and longitude of the centre point of the outermost domain, in addition to the specific, pre-defined model configuration and forecast duration. In the encircled example shown here, the name of the job_type is <tt>small.9</tt>.</p>
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<p>The final step to set up an operational forecast is to set the unique identification number of the prototype forecast as the “Job” the schedule should be based on. In addition, the user should define the forecast duration and choose a (preferably) sensible name for the new schedule. More fine-tuning can be conducted by modifying individual entries linked to the schedule in the WOD database.</p>
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<p>The landing page (<b>top panel</b>) of the Verif web service offers the user the choice of a set of observed and modelled variables as well as plot options (<b>lower panel, left</b>); data range options (<b>lower panel, middle</b>); and the option of customizing which observation locations are to be investigated (<b>lower panel, right</b>).</p>
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<p>The Verif web service offers six types of graphs. These are scatter plots (<b>top left</b>), Taylor diagrams (<b>top centre</b>), quantile–quantile plots (<b>top right</b>), and maps showing mean absolute error (<b>bottom left</b>), bias (<b>bottom centre</b>), and root-mean-square error (<b>bottom right</b>).</p>
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21 pages, 10261 KiB  
Article
Super Typhoons Simulation: A Comparison of WRF and Empirical Parameterized Models for High Wind Speeds
by Haihua Fu, Yan Wang, Yanshuang Xie, Chenghan Luo, Shaoping Shang, Zhigang He and Guomei Wei
Appl. Sci. 2025, 15(2), 776; https://doi.org/10.3390/app15020776 - 14 Jan 2025
Viewed by 435
Abstract
As extreme forms of tropical cyclones (TCs), typhoons pose significant threats to both human society and the natural environment. To better understand and predict their behavior, scientists have relied on numerical simulations. Current typhoon modeling primarily falls into two categories: (1) complex simulations [...] Read more.
As extreme forms of tropical cyclones (TCs), typhoons pose significant threats to both human society and the natural environment. To better understand and predict their behavior, scientists have relied on numerical simulations. Current typhoon modeling primarily falls into two categories: (1) complex simulations based on fluid dynamics and thermodynamics, and (2) empirical parameterized models. Most comparative studies on these models have focused on wind speed below 50 m/s, with fewer studies addressing high wind speed (above 50 m/s). In this study, we design and compare four different simulation approaches to model two super typhoons: Typhoon Surigae (2102) and Typhoon Nepartak (1601). These approaches include: (1) The Weather Research and Forecasting (WRF) model simulation driven by NCEP Final Operational Global Analysis data (FNL), (2) WRF simulation driven by the fifth generation of the European Centre for Medium-Range Weather Forecasts (ECMWF) reanalysis data (ERA5), (3) the empirical parameterized Holland model, and (4) the empirical parameterized Jelesnianski model. The simulated wind fields were compared with the measured wind data from The Soil Moisture Active Passive (SMAP) platform, and the resulting wind fields were then used as inputs for the Simulating WAves Nearshore (SWAN) model to simulate typhoon-induced waves. Our findings are as follows: (1) for high wind speeds, the performance of the empirical models surpasses that of the WRF simulations; (2) using more accurate driving wind data improves the WRF model’s performance in simulating typhoon wind speeds, and WRF simulations excel in representing wind fields in the outer regions of the typhoon; (3) careful adjustment of the maximum wind speed radius parameter is essential for improving the accuracy of the empirical models. Full article
(This article belongs to the Section Marine Science and Engineering)
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<p>Workflow Diagram for WRF Model Simulation.</p>
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<p>Typhoon tracks and intensity information recorded by the CMA dataset.</p>
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<p>Simulation domain in the WRF model. The red lines show the d01 area, the blue lines show the d02 area, the solid line represents the simulation domain for Typhoon Surigae, and the dashed line represents the simulation domain for Typhoon Nepartak.</p>
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<p>SWAN simulation domains. The red line shows the SWAN area of typhoon Surigae, and the blue line shows the SWAN area of typhoon Nepartak.</p>
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<p>Wind field for Typhoon Surigae at 09:00 on 17 April 2021. (<b>a</b>) shows the simulation driven by FNL data using WRF, (<b>b</b>) shows the simulation driven by ERA5 data using WRF, (<b>c</b>) shows the simulation using the Holland empirical parameter typhoon model, (<b>d</b>) shows the simulation using the Jelesnianski empirical parameter typhoon model, and (<b>e</b>) shows the SMAP data.</p>
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<p>Wind field for Typhoon Surigae at 21:00 on 17 April 2021. (<b>a</b>) shows the simulation driven by FNL data using WRF, (<b>b</b>) shows the simulation driven by ERA5 data using WRF, (<b>c</b>) shows the simulation using the Holland empirical parameter typhoon model, (<b>d</b>) shows the simulation using the Jelesnianski empirical parameter typhoon model, and (<b>e</b>) shows the SMAP data.</p>
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<p>Wind field simulation results for Typhoon Nepartak at 09:00 on 4 July 2016. (<b>a</b>) shows the simulation driven by FNL data using WRF, (<b>b</b>) shows the simulation driven by ERA5 data using WRF, (<b>c</b>) shows the simulation using the Holland empirical parameter typhoon model, (<b>d</b>) shows the simulation using the Jelesnianski empirical parameter typhoon model, and (<b>e</b>) shows the SMAP data.</p>
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<p>Wind field simulation results for Typhoon Nepartak at 22:00 on 6 July 2016. (<b>a</b>) shows the simulation driven by FNL data using WRF, (<b>b</b>) shows the simulation driven by ERA5 data using WRF, (<b>c</b>) shows the simulation using the Holland empirical parameter typhoon model, (<b>d</b>) shows the simulation using the Jelesnianski empirical parameter typhoon model, and (<b>e</b>) shows the SMAP data.</p>
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<p>Comparison of Typhoon Surigae Center Path. (<b>a</b>) shows the Typhoon Surigae. (<b>b</b>) shows the Typhoon Nepartak. The red line represents CMA recorded data, the green line indicates the WRF simulation driven by ERA5, and the blue line represents the WRF simulation driven by FNL.</p>
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<p>Comparison of Typhoon Surigae Intensity Simulations. (<b>a</b>) shows the comparison of extreme wind speeds, (<b>b</b>) shows the minimum surface pressure. The black line represents the WRF simulation driven by FNL, the blue line represents the WRF simulation driven by ERA5, the green line corresponds to the empirical parameterized typhoon model Holland, the yellow line corresponds to the empirical parameterized typhoon model Jelesnianski, the purple dots represent the maximum wind speed data recorded by CMA, and the red triangles represent the maximum wind speed data from SMAP.</p>
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<p>Comparison of Typhoon Nepartak Intensity Simulations. (<b>a</b>) shows the comparison of extreme wind speeds, (<b>b</b>) shows the minimum surface pressure. The black line represents the WRF simulation driven by FNL, the blue line represents the WRF simulation driven by ERA5, the green line corresponds to the empirical parameterized typhoon model Holland, the yellow line corresponds to the empirical parameterized typhoon model Jelesnianski, the purple dots represent the maximum wind speed data recorded by CMA, and the red triangles represent the maximum wind speed data from SMAP.</p>
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<p>Comparison of Significant Wave Height Simulations in Typhoon Surigae. (<b>a</b>) shows the WRF simulation driven by FNL, (<b>b</b>) shows the WRF simulation driven by ERA5, (<b>c</b>) shows the empirical parameterized typhoon model Holland, and (<b>d</b>) shows the empirical parameterized typhoon model Jelesnianski.</p>
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<p>The location of the reference point near the coast, and the time series of significant wave height at this point for Typhoon Surigae, the red point is the location of the reference point, the red line represents the FNL-driven WRF simulation, the blue line represents the ERA5-driven WRF simulation, the green line corresponds to the Holland case, and the yellow line corresponds to the Jelesnianski case.</p>
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<p>Comparison of Significant Wave Height Simulations in Typhoon Nepartak. (<b>a</b>) shows the WRF simulation driven by FNL, (<b>b</b>) shows the WRF simulation driven by ERA5, (<b>c</b>) shows the empirical parameterized typhoon model Holland, and (<b>d</b>) shows the empirical parameterized typhoon model Jelesnianski.</p>
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<p>The location of the reference point near the coast, and the time series of significant wave height at this point for Typhoon Nepartak, the red point is the location of the reference point, the red line represents the FNL-driven WRF simulation, the blue line represents the ERA5-driven WRF simulation, the green line corresponds to the Holland case, and the yellow line corresponds to the Jelesnianski case.</p>
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