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20 pages, 15268 KiB  
Article
Automatic Reading and Reporting Weather Information from Surface Fax Charts for Ships Sailing in Actual Northern Pacific and Atlantic Oceans
by Jun Jian, Yingxiang Zhang, Ke Xu and Peter J. Webster
J. Mar. Sci. Eng. 2024, 12(11), 2096; https://doi.org/10.3390/jmse12112096 - 19 Nov 2024
Abstract
This study is aimed to improve the intelligence level, efficiency, and accuracy of ship safety and security systems by contributing to the development of marine weather forecasting. The accurate and prompt recognition of weather fax charts is very important for navigation safety. This [...] Read more.
This study is aimed to improve the intelligence level, efficiency, and accuracy of ship safety and security systems by contributing to the development of marine weather forecasting. The accurate and prompt recognition of weather fax charts is very important for navigation safety. This study employed many artificial intelligent (AI) methods including a vectorization approach and target recognition algorithm to automatically detect the severe weather information from Japanese and US weather charts. This enabled the expansion of an existing auto-response marine forecasting system’s applications toward north Pacific and Atlantic Oceans, thus enhancing decision-making capabilities and response measures for sailing ships at actual sea. The OpenCV image processing method and YOLOv5s/YOLO8vn algorithm were utilized to make template matches and locate warning symbols and weather reports from surface weather charts. After these improvements, the average accuracy of the model significantly increased from 0.920 to 0.928, and the detection rate of a single image reached a maximum of 1.2 ms. Additionally, OCR technology was applied to retract texts from weather reports and highlighted the marine areas where dense fog and great wind conditions are likely to occur. Finally, the field tests confirmed that this auto and intelligent system could assist the navigator within 2–3 min and thus greatly enhance the navigation safety in specific areas in the sailing routes with minor text-based communication costs. Full article
(This article belongs to the Special Issue Ship Performance in Actual Seas)
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Figure 1

Figure 1
<p>(<b>a</b>) Weather report and warning symbols in JMA surface weather fax chart retrieved from imocwx.com.(accessed on 14 Feb 2022). (<b>b</b>) Warning symbols and wind barbs in a 48 h surface forecast chart issued by US National Weather Service at 1758 UTC on 13 February 2022.</p>
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<p>JMA (<b>a</b>) original surface fax weather chart, (<b>b</b>) averaged base chart, (<b>c</b>) after binarization, (<b>d</b>) difference between the original (<b>a</b>) and base chart (<b>c</b>), resulting in a pure weather map.</p>
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<p>Flow chart of the auto-warning system for JMA charts.</p>
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<p>YOLOv5s-CBAM(SE) network structure diagram, the parts related with CBAM(SE) are marked in gray.</p>
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<p>YOLOv8n model structure diagram.</p>
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<p>Comparison of weather briefing text recognition results.</p>
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<p>Recognition of warning symbols “hPa”, “GW”, “SW”, and “FOG[W]” from the chart <a href="#jmse-12-02096-f002" class="html-fig">Figure 2</a>d.</p>
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<p>Comparison of detection results of wind barb (interception).</p>
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<p>Comparison of detection results of wind barb (interception).</p>
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<p>Training process visualization (<b>a</b>) train-loss and (<b>b</b>) mAP values for original and improved YOLOv5s.</p>
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<p>(<b>a</b>) JMA charts with warning symbols detected, (<b>b</b>) JMA charts with warning area colored, red and yellow for wind speeds greater than 50 kts and 35–49 kts, green for visibility &lt; 0.3 nm (<b>c</b>) US charts with wind levels colored.</p>
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<p>Field tests of the auto-warning system (<b>upper</b> and <b>middle</b>) US case (<b>bottom</b>) and JMA case.</p>
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16 pages, 2628 KiB  
Article
Possible Missing Sources of Atmospheric Glyoxal Part I: Phospholipid Oxidation from Marine Algae
by Renee T. Williams, Annika Caspers-Brown, Camille M. Sultana, Christopher Lee, Jessica L. Axson, Francesca Malfatti, Yanyan Zhou, Kathryn A. Moore, Natalie Stevens, Mitchell V. Santander, Farooq Azam, Kimberly A. Prather and Robert S. Pomeroy
Metabolites 2024, 14(11), 639; https://doi.org/10.3390/metabo14110639 - 19 Nov 2024
Viewed by 123
Abstract
Background: Glyoxal has been implicated as a significant contributor to the formation of secondary organic aerosols, which play a key role in our ability to estimate the impact of aerosols on climate. Elevated concentrations of glyoxal over remote ocean waters suggests that there [...] Read more.
Background: Glyoxal has been implicated as a significant contributor to the formation of secondary organic aerosols, which play a key role in our ability to estimate the impact of aerosols on climate. Elevated concentrations of glyoxal over remote ocean waters suggests that there is an additional source, distinct from urban and forest environments, which has yet to be identified. Herein, we demonstrate that the ocean can serve as an appreciable source of glyoxal in the atmosphere due to microbiological activity. Methods and Results: Based on mass spectrometric analyses of nascent sea spray aerosols and the sea surface microlayer (SSML) of naturally occurring algal blooms, we provide evidence that during the algae death phase phospholipids become enriched in the SSML and undergo autoxidation thereby generating glyoxal as a degradation product. Conclusions: We propose that the death phase of an algal bloom could serve as an important and currently missing source of glyoxal in the atmosphere. Full article
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Figure 1
<p>Derivatization of glyoxal to quinoxaline (<b>a</b>) for the purpose of GC analysis over the course of IMPACTS (<b>b</b>), which was verified by characterization of the retention time and MS spectrum of a commercially purchased standard (<a href="#app1-metabolites-14-00639" class="html-app">Figure S3</a>).</p>
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<p>GC/MS temporal chromatograms of glyoxal transported by SSA and collected within an impinger of <span class="html-italic">o</span>-PDA where it was derivatized to quinoxaline (RT 12.1; SIC <span class="html-italic">m</span>/<span class="html-italic">z</span> 130) (<b>a</b>); and gas-phase molecules captured by an array of SPME fibers (traces are superimposed) highlighting the primary presence of unsaturated FAMEs (<b>b</b>) during the microcosm culture flask experiment. Formaldehyde was also characterized in the impinger of <span class="html-italic">o</span>-PDA where it was derivatized to benzimidazole (RT 30.1 min, SIC <span class="html-italic">m</span>/<span class="html-italic">z</span> 118) during the microcosm experiment. Labeled peaks were verified by retention time and MS spectrum using standards (<a href="#app1-metabolites-14-00639" class="html-app">Figures S3–S5</a>). (<b>c</b>) the reaction product of <span class="html-italic">o</span>-PDA and formaldehyde was detected, which implies methanol may have undergone oxidation.</p>
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<p>Proposed mechanism for the formation of marine glyoxal from the peroxidation of PUFA-containing phospholipids (<b>a</b>), which was validated by the ESI-MS/MS positive-ion mode characterization of PAPC (<b>b</b>), its oxidation product HO-PAPC (<b>c</b>), and the corresponding short-chain degradation product HOOA-PC (<b>d</b>) that were found in the foam of the SSML.</p>
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<p>ESI-HR-MS/MS positive-ion spectra of peroxidized PLPC (<b>a</b>) and PAPC (<b>b</b>); and ozonides of PLPC (<b>c</b>).</p>
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<p>Measured lipase (stearase) activity in the sea surface microlayer (SSML; top of the striped bars) and bulk (top of the solid bars) waters of the wave channel during IMPACTS.</p>
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<p>GC/MS headspace analysis of the dose-dependent UV irradiation of C18:2 FAME standard (RT 21.5 min) (<b>a</b>) and the MS of hexanal which is an oxidation product of C18:2 (<b>b</b>) collected by SPME.</p>
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18 pages, 9708 KiB  
Article
Behavior and Energy of the M2 Internal Tide in the Madagascar–Mascarene Region
by Qian Wu, Jing Meng, Xu Chen and Yulin Guo
Remote Sens. 2024, 16(22), 4299; https://doi.org/10.3390/rs16224299 - 18 Nov 2024
Viewed by 310
Abstract
Internal tides serve as essential intermediate steps in the cascading of oceanic energy, playing a crucial role in oceanic mixing. M2 internal tides are the dominant tidal constituent in many oceanic regions, significantly influencing ocean dynamics. The Madagascar–Mascarene Region has high-energy internal tides, [...] Read more.
Internal tides serve as essential intermediate steps in the cascading of oceanic energy, playing a crucial role in oceanic mixing. M2 internal tides are the dominant tidal constituent in many oceanic regions, significantly influencing ocean dynamics. The Madagascar–Mascarene Region has high-energy internal tides, but due to a lack of observational studies, their propagation remains underexplored and warrants further investigation. In this study, we used satellite altimetry data to capture the sea surface manifestation of the first-mode M2 internal tides in the region. The results show that the Mascarene Plateau plays a key role in shaping the region’s uneven internal tide distribution. The Mascarene Strait is the most intense generation area, with an east-west energy flux of 1.42 GW. Using the internal tidal energy concentration index, we decomposed the internal tidal beams, finding the primary beam oriented at 148°. These beams propagate outward for over 800 km, with a maximum distance exceeding 1000 km. Geostrophic currents intensify the northward refraction of westward-propagating internal tides in the Mascarene Basin, particularly between 15°S and 20°S. Full article
(This article belongs to the Special Issue Satellite Remote Sensing for Ocean and Coastal Environment Monitoring)
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Figure 1
<p>Bathymetric topography of the Madagascar–Mascarene Region, delineating two isobaths at 500 m and 3000 m to illustrate the underwater terrain.</p>
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<p>A diagrammatic representation of the satellite data’s temporal span, which is not detailed to the monthly level.</p>
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<p>Iterative two-dimensional plane wave fitting process diagram. (<b>a</b>) The case study location is positioned at 11.5°S, 56.5°E, with the fitting window set to a 160 km square. (<b>b</b>–<b>f</b>) represent the amplitude and direction of the 1st to 5th wave components, respectively.</p>
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<p>(<b>a</b>) Sea surface height (SSH) of the M2 internal tides in this study. (<b>b</b>) SSH of the M2 internal tides from ZHAO. (<b>c</b>) Directional wavenumber spectrums.</p>
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<p>The degree of multiwave interference <span class="html-italic">R<sub>in</sub></span>, with 0 indicating the presence of complete standing waves and 1 denoting the presence of complete progressive wave.</p>
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<p>Barotropic tidal body force <math display="inline"><semantics> <mrow> <msub> <mi>F</mi> <mrow> <mi>b</mi> <mi>o</mi> <mi>d</mi> <mi>y</mi> </mrow> </msub> </mrow> </semantics></math>, illustrating the conversion rate, with the enlargement of the black boxes (<b>A</b>–<b>C</b>).</p>
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<p>(<b>a</b>) M2 internal tide sea surface amplitude (<b>b</b>) M2 internal tide vertically integrated energy flux, where color indicates magnitude and arrows indicate direction. The energy is integrated along the green line.</p>
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<p>(<b>a</b>,<b>b</b>,<b>d</b>) The SSH of internal tides propagating in the directions of 100–170°, 0–60°, and 300–360°, with the green line representing the integral line of energy and the blue line illustrating the representative paths of tidal beams. The black line box in (<b>a</b>) is the region used to calculate the direction of the energy concentration. (<b>c</b>) Internal tidal energy concentration index, where the eastward orientation is set at 0° and rotation in a counterclockwise direction is considered positive.</p>
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<p>(<b>a</b>) The variation of the propagation direction (blue line, left <span class="html-italic">y</span>-axis) and phase (orange line, right <span class="html-italic">y</span>-axis) of beam 2, with the black arrow signifying the direction of the increasing phase. (<b>b</b>) The variation in the phase velocity of beam 2, where <span class="html-italic">C</span> indicates the observed phase velocity (gradient of the phase), <span class="html-italic">C<sub>n</sub></span> is the eigenspeed, and <span class="html-italic">C<sub>p</sub></span> is the theoretical velocity from Formula (5).</p>
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<p>(<b>a</b>–<b>c</b>) The SSH of internal tides in the 300–120°, 300–60°, and 60–120° directions, respectively. (<b>d</b>–<b>f</b>) are corresponding sea surface amplitudes for (<b>a</b>), (<b>b</b>), and (<b>c</b>), respectively, where the arrows depict the direction of energy flux and the lengths of the arrows are proportional to the magnitude of the energy flux.</p>
Full article ">Figure 11
<p>(<b>a</b>–<b>c</b>) The SSH of internal tides in the 210–60°, 300–60°, and 210–300° directions, respectively. (<b>d</b>–<b>f</b>) are corresponding sea surface amplitudes for (<b>a</b>), (<b>b</b>), and (<b>c</b>), respectively, where the arrows depict the direction of energy flux and the lengths of the arrows are proportional to the magnitude of the energy flux.</p>
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<p>(<b>a</b>) Sea surface amplitude of internal tides in the 270–210° direction (excluding waves within the 210–270°), where arrows depict the energy flux directions, and the lengths of the arrows are proportional to the energy flux magnitudes. (<b>b</b>) The topographic critical parameter, with <math display="inline"><semantics> <mi>γ</mi> </semantics></math> exceeding 1 indicating regions that are supercritical and prone to wave reflection. The arrows represent the directions of energy flux, with arrow colors distinguishing the propagation directions.</p>
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<p>(<b>a</b>) The SSH of internal tides in the 120–210° direction, where arrows indicate the energy flux directions, and the lengths of the arrows are proportional to the energy flux magnitudes. Green lines signify energy integration lines. (<b>b</b>) The SSH of internal tides in the 60–120° direction. (<b>c</b>) The SSH of internal tides in the 270–60° direction. (<b>d</b>) Internal tidal energy concentration index.</p>
Full article ">Figure 14
<p>(<b>a</b>) The SSH of internal tides in the direction of 120–210°, where the direction of the arrows indicates the direction of the geostrophic flow, and the length of the arrows indicates the magnitude of the geostrophic flow. (<b>b</b>) The propagation directions of internal tides, with blue representing the northern part and yellow lines representing the southern part. (<b>d</b>) Phase velocities. The solid line represents the theoretical phase speed, and the dashed line represents the phase speed after geostrophic current correction, with colors corresponding to those in (<b>b</b>). (<b>c</b>,<b>e</b>) Schemas of the westward internal tidal propagation directions before and after geostrophic flow correction.</p>
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10 pages, 4032 KiB  
Communication
Driving Factors and Future Trends of Wildfires in Alberta, Canada
by Maowei Bai, Qichao Yao, Zhou Wang, Di Wang, Hao Zhang, Keyan Fang and Futao Guo
Fire 2024, 7(11), 419; https://doi.org/10.3390/fire7110419 - 18 Nov 2024
Viewed by 259
Abstract
Departures from historical wildfire regimes due to climate change have significant implications for the structure and composition of forests, as well as for fire management and operations in the Alberta region of Canada. This study analyzed the relationship between climate and wildfire and [...] Read more.
Departures from historical wildfire regimes due to climate change have significant implications for the structure and composition of forests, as well as for fire management and operations in the Alberta region of Canada. This study analyzed the relationship between climate and wildfire and used a random forest algorithm to predict future wildfire frequencies in Alberta, Canada. Key factors driving wildfires were identified as vapor pressure deficit (VPD), sea surface temperature (SST), maximum temperature (Tmax), and the self-calibrated Palmer drought severity index (scPDSI). Projections indicate an increase in wildfire frequencies from 918 per year during 1970–1999 to 1151 per year during 2040–2069 under a moderate greenhouse gas (GHG) emission scenario (RCP 4.5) and to 1258 per year under a high GHG emission scenario (RCP 8.5). By 2070–2099, wildfire frequencies are projected to increase to 1199 per year under RCP 4.5 and to 1555 per year under RCP 8.5. The peak number of wildfires is expected to shift from May to July. These findings suggest that projected GHG emissions will substantially increase wildfire danger in Alberta by 2099, posing increasing challenges for fire suppression efforts. Full article
(This article belongs to the Special Issue Effects of Climate Change on Fire Danger)
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Figure 1
<p>Spatial and temporal distribution characteristics of wildfires in the Alberta region, Canada. (<b>a</b>) spatial distribution of wildfires; (<b>b</b>) monthly distribution of wildfire numbers from 1961 to 2021; (<b>c</b>) time series of annual wildfire numbers from 1961 to 2021.</p>
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<p>Main predictors of wildfires in the Alberta region, Canada. The figure shows the random forest mean predictor importance (the percentage of increase in the mean variance error (MSE)) of meteorological variables on wildfires. The cross-validated R<sup>2</sup> and significance of random forest models are shown. Significance levels: ** <span class="html-italic">p</span> &lt; 0.01; * <span class="html-italic">p</span> &lt; 0.05; n.s., non-significant (<span class="html-italic">p</span> &gt; 0.05).</p>
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<p>Sensitivity of wildfire occurrences to meteorological variables. Accumulated local effect (ALE) plots show the relationship between wildfire risk and the top four key drivers. The x-axes represent the independent covariates, and the y-axes represent the size of the mean effect each covariate has on wildfire occurrences. Variables are ranked in order of their relative importance in random forest models from high to low (<b>a</b>–<b>d</b>).</p>
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<p>Seasonal variations in the earth system model (ESM) ensemble mean number of wildfires. Monthly wildfire numbers for the end of the 20th century (1970–1999) and the middle (2040–2069) and end (2070–2099) of the 21st century in the Alberta area are shown. Wildfire number simulations for the moderate (RCP4.5) and high (RCP8.5) emission climate change scenarios are compared here. Meaning of boxplot elements: central line: median, box limits: upper and lower quartiles, upper whisker: min (max (x), Q3 + 1.5 × IQR), lower whisker: max (min (x), Q1 − 1.5 × IQR), black dots: outliers.</p>
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<p>Earth system model (ESM) ensemble-mean changes in simulated VPD (<b>a</b>,<b>b</b>), SST (<b>c</b>,<b>d</b>), Tmax (<b>e</b>,<b>f</b>), and scPDSI (<b>g</b>,<b>h</b>) by the middle (<b>a</b>,<b>c</b>,<b>e</b>,<b>g</b>, 2040–2069) and end (<b>b</b>,<b>d</b>,<b>f</b>,<b>h</b>, 2070–2099) of the 21st century compared with the historical period (1970–1999) for the RCP4.5 and RCP8.5 scenarios. Meaning of boxplot elements: central line: median, box limits: upper and lower quartiles, upper whisker: min (max (x), Q3 + 1.5 × IQR), lower whisker: max (min (x), Q1 − 1.5 × IQR), black dots: outliers.</p>
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<p>Earth system model (ESM) ensemble means the simulated annual number of wildfires. Both the historical (grey, 1961–2020) and future (blue/tan, 2021–2099, blue: moderate emission scenario, RCP4.5, tan: high emission scenario, RCP8.5) variations of these variables are shown. Shaded areas represent ±1 standard deviation. A low-pass filter was applied to remove the highest 20% frequencies to reduce noise in the time series.</p>
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<p>Earth system model (ESM) ensemble mean changes in simulated VPD (<b>a</b>), SST (<b>b</b>), Tmax (<b>c</b>), and scPDSI (<b>d</b>). Both the historical (grey, 1961–2020) and future (blue/tan, 2021–2099, blue: moderate emission scenario, RCP4.5, tan: high emission scenario, RCP8.5) variations of these variables are shown. Shaded areas represent ±1 standard deviation.</p>
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17 pages, 4597 KiB  
Article
Preparation, Structural Characterization, and Hypoglycemic Activity of Dietary Fiber from Sea Buckthorn Pomace
by Qi Xiao, Liting Yang, Jingjing Guo, Xiyu Zhang, Yu Huang and Qun Fu
Foods 2024, 13(22), 3665; https://doi.org/10.3390/foods13223665 - 18 Nov 2024
Viewed by 362
Abstract
Sea buckthorn pomace is often discarded as a by-product during the sea buckthorn processing stage. Consequently, its richness in dietary fiber is usually overlooked. In this study, soluble dietary fiber (SDF) and insoluble dietary fiber (IDF) were extracted from sea buckthorn pomace using [...] Read more.
Sea buckthorn pomace is often discarded as a by-product during the sea buckthorn processing stage. Consequently, its richness in dietary fiber is usually overlooked. In this study, soluble dietary fiber (SDF) and insoluble dietary fiber (IDF) were extracted from sea buckthorn pomace using ultrasound combined with the enzyme method. The optimal values of the independent variable were determined by a combinatorial design and a response surface optimization test with SDF/IDF as the dependent variable, prepared as follows: 5% enzyme addition, ultrasonic power of 380 W, enzymatic time of 30 min, and alcoholic precipitation liquid ratio of 4:1. Under these conditions, the SDF/IDF ratio was 17.07%. The structural characterization and hypoglycemic activity of the two dietary fibers were then compared. The results show that two dietary fibers have respective structures and functional groups of fibers. SDF was less crystalline than IDF, and its structure was looser. Furthermore, the hypoglycemic activity of SDF was significantly better than IDF’s (p < 0.05). The glucose adsorption capacity of SDF was 1.08–1.12 times higher than that of IDF. SDF inhibited α-amylase and α-glucosidase by 1.76 and 4.71 times more than IDF, respectively. These findings provide a reference for improving the utilization of sea buckthorn processing by-products. Full article
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Graphical abstract

Graphical abstract
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<p>Process for DF extraction from sea buckthorn pomace.</p>
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<p>Effect of ultrasonic coupled enzyme process combination sequence on SDF/IDF ratio. SDF and IDF represent the soluble dietary fiber and insoluble dietary fiber, respectively. Different lowercase letters indicate that there are significant differences between the treatments according to the mean separation test (<span class="html-italic">p</span> &lt; 0.05).</p>
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<p>Response surface plots of factor interaction.</p>
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<p>Structural characterization of different DFs. (<b>A</b>,<b>B</b>) TGA curves, (<b>C</b>) FT-IR, (<b>D</b>) X-ray diffraction and (<b>E</b>) SEM.</p>
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<p>Glucose adsorption capacity of different DFs from sea buckthorn pomace. Different letters indicate that there are significant differences (<span class="html-italic">p</span> &lt; 0.05).</p>
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<p>Effect of DFs from sea buckthorn pomace on glucose-lowering enzyme activity. (<b>A</b>) Inhibitory effects of DFs and acarbose on <span class="html-italic">α</span>-amylase, (<b>B</b>) Inhibitory effects of DFs and acarbose on <span class="html-italic">α</span>-glucosidase.</p>
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<p>Inhibition reversibility of glucose-lowering enzyme by DFs from sea buckthorn pomace. (<b>A</b>) IDF—<span class="html-italic">α</span>-amylase, (<b>B</b>) SDF—<span class="html-italic">α</span>-amylase, (<b>C</b>) IDF—<span class="html-italic">α</span>-glucosidase, (<b>D</b>) SDF—<span class="html-italic">α</span>-glucosidase.</p>
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<p>Lineweaver–Burk curve of sea buckthorn pomace DF on glucose-lowering enzyme. (<b>A</b>) IDF—<span class="html-italic">α</span>-amylase, (<b>B</b>) SDF—<span class="html-italic">α</span>-amylase, (<b>C</b>) IDF—<span class="html-italic">α</span>-glucosidase, (<b>D</b>) SDF—<span class="html-italic">α</span>-glucosidase.</p>
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19 pages, 11449 KiB  
Article
Near-Inertial Oscillations Induced by Winter Monsoon Onset in the Southwest Taiwan Strait
by Xiaolin Peng, Li Wang, Xiongbin Wu and Weihua Ai
Remote Sens. 2024, 16(22), 4284; https://doi.org/10.3390/rs16224284 - 17 Nov 2024
Viewed by 173
Abstract
The near-inertial motion in ocean surface currents directly reflects the energy transported by wind towards the surface layer, playing an important role in climate regulation and energy balance. Previous studies have mainly focused on near inertial oscillations (NIOs) induced by tropical cyclones in [...] Read more.
The near-inertial motion in ocean surface currents directly reflects the energy transported by wind towards the surface layer, playing an important role in climate regulation and energy balance. Previous studies have mainly focused on near inertial oscillations (NIOs) induced by tropical cyclones in the Taiwan Strait, with few reports on near inertial oscillations induced by monsoon onset. Using high-frequency radar observations, we detected an amplification of NIOs induced by the winter monsoon onset. While not as strong as NIOs induced by tropical cyclones, the near-inertial current (NIC) induced by winter monsoon onset in the Taiwan Strait has peak speeds reaching up to 5.2 cm/s and explaining up to 0.7% of non-tidal variance. This study presents observational results of NIOs during three monsoon onset events, and analyzes the impact of winds and temperature changes on NIOs. Temporal and spectral analysis reveals that the monsoon onset is the primary driver behind the formation of NIOs. Results indicate that near-inertial kinetic energy is relatively lower in shallower waters, such as the Taiwan Bank, compared to deeper regions. Furthermore, by integrating the air and sea surface temperature from reanalysis products, we have examined the abrupt changes in sea surface temperature (SST) before and after monsoon onset and their correlation with NIOs. The findings suggest that temperature falling favors the intensification of NICs during monsoon onset, and a lack of significant SST changes precludes the triggering of notable NICs. These insights enhance our understanding of the mechanisms driving NIOs and their roles in seawater mixing. Full article
(This article belongs to the Special Issue Remote Sensing of High Winds and High Seas)
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Figure 1

Figure 1
<p>(<b>a</b>) Map of the southwestern Taiwan Strait and HF radar coverage areas. (<b>b</b>) The bathymetry of research region. One can see the Dongshan and Longhai radar stations marked as red points, and one mooring site of the Buoy marked as a black five-pointed star. The surface currents at Points A, B, C, and D were investigated in the following results. The longitudes of points A, B, and C are all 118.6°E, with latitudes of 23.8°N, 23°N, and 22.5°N, respectively. Point D is situated at 118°E, 23°N. The water depths are 51, 11, 49, and 20 m, respectively.</p>
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<p>(<b>a</b>) The transmitting antenna. (<b>b</b>) The receiving array. (<b>c</b>) Wind rose during experiment period. Comparison between wind velocities from buoy and CCMP in (<b>d</b>) east direction and (<b>e</b>) north direction.</p>
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<p>Data in the figure are from point A in <a href="#remotesensing-16-04284-f001" class="html-fig">Figure 1</a>. (<b>a</b>) The comparison between winds at 10 m above sea surface along the strait and the residual currents along the strait (where negative values indicate winds and residual currents toward the SW). (<b>b</b>) The temperatures at altitudes of 1500 m and 750 m above sea level, as well as the sea surface temperatures.</p>
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<p>(<b>a</b>) Clockwise and (<b>b</b>) counterclockwise rotary spectral estimates of the surface currents measured at point A. Blue and red curves represent before and after monsoon onset.</p>
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<p>The first panel (<b>a</b>) shows the SST (blue line) and wind velocity magnitude (magenta line) at point A. The second and third panels (<b>b</b>,<b>c</b>) are the NICs output by radar observations and the Slab mode at along–and cros–strait directions, as well as the winds. (<b>d</b>) shows NIKE, the magnitude of wind vorticity and wind arrows. The lowest panels (<b>e</b>,<b>f</b>) are progressive vector diagrams for all experiment periods, and each day from 15 to 25 February. The red cross means the start.</p>
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<p>(<b>a</b>) Mean NIKE and (<b>b</b>) its ratio to total current kinetic energy during the whole experimental.</p>
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<p>(<b>a</b>) Mean NIKE and (<b>b</b>) its ratio to detided current kinetic energy during onset 1.</p>
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<p>(<b>a</b>) Mean NIKE and (<b>b</b>) its ratio to detided current kinetic energy during onset 2.</p>
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<p>(<b>a</b>) Mean NIKE and (<b>b</b>) its ratio to detided current kinetic energy during onset 3.</p>
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<p>The spatial distribution of wind variation during three onset events ((<b>a</b>): Onset1, (<b>b</b>): Onset2, (<b>c</b>): Onset3). The periods are from 17–19 February, from 28 February to 2 March, and from 12–14 March.</p>
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<p>The spatial distribution of Mean <math display="inline"><semantics> <mi mathvariant="normal">Π</mi> </semantics></math>.</p>
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<p>The spatial distribution of E during the three onset periods ((<b>a</b>): Onset1, (<b>b</b>): Onset2, (<b>c</b>): Onset3).</p>
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<p>The spatial distribution of the amplitude values of E during the three onset periods ((<b>a</b>): Onset1, (<b>b</b>): Onset2, (<b>c</b>): Onset3).</p>
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<p>(<b>a</b>) The vertical temperature profiles of grid points at black solid line passing through point A. (<b>b</b>–<b>k</b>) The distribution of daily SST from 14–23 February, temperature data are from GLORYS12V1.</p>
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<p>The ratio of the sum of the power spectra in the near-inertial frequency band before and after the monsoon onset ((<b>a</b>): Onset1, (<b>b</b>): Onset2, (<b>c</b>): Onset3).</p>
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<p>The distribution of phase of the near inertial currents from 14 to 26 February at an interval of 31 h. (<b>a</b>–<b>j</b>): Phase patterns from 12:00 on 14 February to 03:00 26 February.</p>
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<p>Zonal and meridional near inertial currents from 19–23 February at an interval of 31 h. (<b>a</b>–<b>d</b>): Zonal NIC patterns from 16:00 on 19 February to 13:00 on 23 February. (<b>e</b>–<b>h</b>): Meridional NIC patterns from 16:00 on 19 February to 13:00 on 23 February.</p>
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21 pages, 5869 KiB  
Article
Impacts of Typhoons on the Evolution of Surface Anticyclonic Eddies into Subsurface Anticyclonic Eddies in the Northwestern Subtropical Pacific Ocean
by Shangzhan Cai, Jindian Xu, Weibo Wang, Chunsheng Jing, Kai Li, Junpeng Zhang and Fangfang Kuang
Remote Sens. 2024, 16(22), 4282; https://doi.org/10.3390/rs16224282 - 17 Nov 2024
Viewed by 259
Abstract
In this study, we investigated the impacts of typhoons on the transformation of anticyclonic eddies (AEs) into subsurface anticyclonic eddies (SAEs) in the northwestern subtropical Pacific Ocean (NWSP) based on an ocean reanalysis product and multiple satellite observations. Results suggest that while the [...] Read more.
In this study, we investigated the impacts of typhoons on the transformation of anticyclonic eddies (AEs) into subsurface anticyclonic eddies (SAEs) in the northwestern subtropical Pacific Ocean (NWSP) based on an ocean reanalysis product and multiple satellite observations. Results suggest that while the heavy precipitation and strong positive wind stress curl (WSC) induced by the passage of typhoons may be two main driving factors that transformed shallow mixed layer depth (MLD) AEs (i.e., those shallower than 50 m at the eddy core) into SAEs, the latter played a greater role in such transformation. In addition, shallow MLD AEs with a less depressed isopycnal structure near the eddy center before the passage of typhoons were more likely to be transformed into SAEs under the impacts of typhoons. The likely timing of such transformation may be within 9 days after the passage of typhoons. For deep MLD AEs (i.e., those deeper than 80 m at the eddy core), the impacts of typhoons may be much less prominent below the mixed layer. Based on a diagnostic analysis of the vertical potential vorticity (PV) flux at the surface, we examined the mechanism and dynamic processes involved in the transformation of deep MLD AEs into SAEs under the impacts of typhoons. Results show that while typhoons played a positive role in maintaining low PV within deep MLD AEs, which was favorable for further transformation into SAEs, the diabatic process associated with the net air–sea heat flux was the crucial favorable condition for the transformation of deep MLD AEs into SAEs. Full article
(This article belongs to the Special Issue Recent Advances on Oceanic Mesoscale Eddies II)
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Graphical abstract

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<p>Tracks of typhoons (black dotted lines), tracks of the AEs (green lines) and edges of the AEs (red lines) at T = 0 for (<b>a</b>) typhoon Levi (1997) and AE1, (<b>b</b>) typhoon Chan-hom (2003) and AE2, (<b>c</b>) typhoon Lekima (2007) and AE3. Tracks of typhoons (black dotted lines) and center locations (red dots) of the (<b>d</b>) strong SAEs and (<b>e</b>) strong AEs at T = 0. The blue triangles in (<b>a</b>–<b>c</b>) indicate the center locations of typhoons at T = 0. T = 0 means the day when the typhoons passed over the AEs. The edge of an AE is defined as the outermost closed SLA contour associated with the AE.</p>
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<p>Maps of (<b>a</b>,<b>e</b>,<b>i</b>) SLA (cm) and vertical distributions of (<b>b</b>,<b>f</b>,<b>j</b>) temperature (°C), (<b>c</b>,<b>g</b>,<b>k</b>) salinity, (<b>d</b>,<b>h</b>,<b>l</b>) potential density (kg/m<sup>3</sup>, contours) and PV (10<sup>−10</sup> m<sup>−1</sup>s<sup>−1</sup>, shading) along the transect crossing the AE1 center indicated by black lines in (<b>a</b>,<b>e</b>,<b>i</b>) before, during and after typhoon Levi (1997). The green lines in (<b>a</b>,<b>e</b>,<b>i</b>) represent the outermost closed SLA contour associated with AE1. The cyan line and black triangle in (<b>e</b>) indicate the track of typhoon Levi (1997) and its center location at 29 May 1997 12:00. The red lines denote the MLD along the transect.</p>
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<p>Maps of (<b>a</b>–<b>c</b>) precipitation (mm/d), (<b>d</b>–<b>f</b>) sea surface salinity, (<b>g</b>–<b>i</b>) wind (vectors, m/s) and wind stress curl (shading, N/m<sup>3</sup>) before, during and after typhoon Levi (1997). The blue lines represent the outermost closed SLA contour associated with AE1.</p>
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<p>Time–depth plots of (<b>a</b>) temperature (°C), (<b>b</b>) salinity, (<b>c</b>) potential density (kg/m<sup>3</sup>, contours), PV (10<sup>−10</sup> m<sup>−1</sup>s<sup>−1</sup>, shading), (<b>d</b>) variations of 0–60 m (red line) and 60–200 m (blue line) averaged PV at the core of AE1 along the eddy track during its lifespan. Variations of (<b>e</b>) precipitation (mm/d), wind stress (N/m<sup>2</sup>), (<b>f</b>) wind stress curl (N/m<sup>3</sup>) and Ekman pumping velocity (m/s) averaged within the extent of AE1 along the eddy track during its life span. The cyan lines denote the MLD. The black triangles indicate the day when typhoon Levi (1997) passed over AE1.</p>
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<p>Potential density anomaly fields (kg/m<sup>3</sup>) of composite strong SAEs and strong AEs before (T = −7, (<b>a</b>–<b>f</b>,<b>m</b>–<b>r</b>)) and after (T = 7, (<b>g</b>–<b>l</b>,<b>s</b>–<b>x</b>)) the passage of typhoons in the NWSP at 5 m, 34 m, 56 m, 156 m, 266 m and 454 m. The <span class="html-italic">x</span> and <span class="html-italic">y</span> axes are normalized by eddy radius R.</p>
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<p>Vertical distributions of potential density anomalies (kg/m<sup>3</sup>) along the zonal transect crossing the eddy center of the composite (<b>a</b>,<b>b</b>) strong SAEs and (<b>c</b>,<b>d</b>) strong AEs at T = −7 and T = 7. Time–depth plots of PV anomalies (10<sup>−10</sup> m<sup>−1</sup>s<sup>−1</sup>) of composite (<b>e</b>) strong SAEs and (<b>f</b>) strong AEs at the eddy core along its track between T = −15 and T = 15. (<b>g</b>) Variation of 60–200 m averaged PV anomalies (10<sup>−10</sup> m<sup>−1</sup>s<sup>−1</sup>) of composite strong SAEs (red line) and strong AEs (blue line) at the eddy core along its track between T = −15 and T = 15. The <span class="html-italic">x</span> axes in (<b>a</b>–<b>d</b>) are normalized by eddy radius R.</p>
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<p>Maps of (<b>a</b>,<b>e</b>,<b>i</b>) SLA (cm) and vertical distributions of (<b>b</b>,<b>f</b>,<b>j</b>) temperature (°C), (<b>c</b>,<b>g</b>,<b>k</b>) salinity, (<b>d</b>,<b>h</b>,<b>l</b>) potential density (kg/m<sup>3</sup>, contours) and PV (10<sup>−10</sup> m<sup>−1</sup>s<sup>−1</sup>, shading) along the transect crossing the AE2 center indicated by black lines in (<b>a</b>,<b>e</b>,<b>i</b>) before, during and after typhoon Chan-hom (2003). The green lines in (<b>a</b>,<b>e</b>,<b>i</b>) represent the outermost closed SLA contour associated with AE2. The cyan line and black triangle in (<b>e</b>) indicate the track of typhoon Chan-hom (2003) and its center location at 00:00 on 25 May 2003. The red lines denote the MLD along the transect.</p>
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<p>(<b>a</b>) Time–depth plots of potential density (kg/m<sup>3</sup>, contours) and PV (10<sup>−10</sup> m<sup>−1</sup>s<sup>−1</sup>, shading) at the core of AE2 along the eddy track during its lifespan. Variations of (<b>b</b>) PV flux components (kg m<sup>−3</sup>s<sup>−2</sup>), (<b>c</b>) net surface heat flux (Q<sub>net</sub>, W/m<sup>2</sup>, positive downward) and sea surface temperature (SST, °C) averaged within the extent of AE2 along the eddy track during its life span. The red line in (<b>a</b>) denotes the MLD. The black triangles indicate the day when typhoon Chan-hom (2003) passed over AE2.</p>
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<p>Maps of (<b>a</b>,<b>e</b>,<b>i</b>) sea surface temperature (SST, °C), (<b>b</b>,<b>f</b>,<b>j</b>) net surface heat flux (Q<sub>net</sub>, W/m<sup>2</sup>, positive downward), PV flux associated with (<b>c</b>,<b>g</b>,<b>k</b>) diabatic processes (<math display="inline"><semantics> <mrow> <msubsup> <mrow> <mi mathvariant="normal">J</mi> </mrow> <mrow> <mi mathvariant="normal">z</mi> </mrow> <mrow> <mi mathvariant="normal">D</mi> </mrow> </msubsup> </mrow> </semantics></math>, kg m<sup>−3</sup>s<sup>−2</sup>, positive downward) and (<b>d</b>,<b>h</b>,<b>l</b>) frictional forces (<math display="inline"><semantics> <mrow> <msubsup> <mrow> <mi mathvariant="normal">J</mi> </mrow> <mrow> <mi mathvariant="normal">z</mi> </mrow> <mrow> <mi mathvariant="normal">F</mi> </mrow> </msubsup> </mrow> </semantics></math>, kg m<sup>−3</sup>s<sup>−2</sup>, positive downward) before, during and after typhoon Chan-hom (2003). The green lines represent the outermost closed SLA contour associated with AE2.</p>
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<p>Variations of (<b>a</b>) PV flux components (kg m<sup>−3</sup>s<sup>−2</sup>), (<b>b</b>) net surface heat flux (Q<sub>net</sub>, W/m<sup>2</sup>, positive downward), (<b>c</b>) net fresh water (evaporation minus precipitation, mm/d, positive downward) and (<b>d</b>) wind stress curl (WSC, N/m<sup>3</sup>) averaged within the extent of AE2 along the eddy track during May–July 2003. (<b>e</b>) Variation of PV (m<sup>−1</sup>s<sup>−1</sup>) averaged within the mixed layer at the core of AE2 along its track during May–July 2003. The black triangles indicate the day when typhoon Chan-hom (2003) passed over AE2.</p>
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<p>Variations of (<b>a</b>) precipitation (mm/d), (<b>b</b>) wind stress (N/m<sup>2</sup>), (<b>c</b>) wind stress curl (N/m<sup>3</sup>) and (<b>d</b>) Ekman pumping velocity (m/s) averaged within the eddy extent along the track of composite strong SAEs (red lines) and strong AEs (blue lines) between T = −15 and T = 15.</p>
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<p>Maps of (<b>a</b>–<b>c</b>) SLA (cm) and vertical distributions of (<b>d</b>–<b>f</b>) potential density (kg/m<sup>3</sup>, contours) and PV (10<sup>−10</sup> m<sup>−1</sup>s<sup>−1</sup>, shading) along the transect crossing the AE3 center indicated by black lines in (<b>a</b>–<b>c</b>) before, during and after typhoon Lekima (2007). The green lines in (<b>a</b>–<b>c</b>) represent the outermost closed SLA contour associated with AE3. The cyan line and magenta triangle in (<b>b</b>) indicate the track of typhoon Lekima (2007) and its center location at 18:00 on 28 September 2007. The red lines denote the MLD along the transect.</p>
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<p>(<b>a</b>) Time–depth plots of potential density (kg/m<sup>3</sup>, contours) and PV (10<sup>−10</sup> m<sup>−1</sup>s<sup>−1</sup>, shading), (<b>b</b>) variation of PV (m<sup>−1</sup>s<sup>−1</sup>) averaged within the mixed layer at the core of AE3 along the eddy track during its lifespan. Variations of (<b>c</b>) PV flux components (kg m<sup>−3</sup>s<sup>−2</sup>), (<b>d</b>) net surface heat flux (Q<sub>net</sub>, W/m<sup>2</sup>, positive downward) and sea surface temperature (SST, °C) averaged within the extent of AE3 along the eddy track during its lifespan. The red line in (<b>a</b>) denotes the MLD. The black triangles indicate the day when typhoon Lekima (2007) passed over AE3.</p>
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20 pages, 9833 KiB  
Article
Reconstruction of Hourly Gap-Free Sea Surface Skin Temperature from Multi-Sensors
by Qianguang Tu, Zengzhou Hao, Dong Liu, Bangyi Tao, Liangliang Shi and Yunwei Yan
Remote Sens. 2024, 16(22), 4268; https://doi.org/10.3390/rs16224268 - 15 Nov 2024
Viewed by 282
Abstract
The sea surface skin temperature (SSTskin) is of critical importance with regard to air–sea interactions and marine carbon circulation. At present, no single remote sensor is capable of providing a gap-free SSTskin. The use of data fusion techniques is [...] Read more.
The sea surface skin temperature (SSTskin) is of critical importance with regard to air–sea interactions and marine carbon circulation. At present, no single remote sensor is capable of providing a gap-free SSTskin. The use of data fusion techniques is therefore essential for the purpose of filling these gaps. The extant fusion methodologies frequently fail to account for the influence of depth disparities and the diurnal variability of sea surface temperatures (SSTs) retrieved from multi-sensors. We have developed a novel approach that integrates depth and diurnal corrections and employs advanced data fusion techniques to generate hourly gap-free SST datasets. The General Ocean Turbulence Model (GOTM) is employed to model the diurnal variability of the SST profile, incorporating depth and diurnal corrections. Subsequently, the corrected SSTs at the same observed time and depth are blended using the Markov method and the remaining data gaps are filled with optimal interpolation. The overall precision of the hourly gap-free SSTskin generated demonstrates a mean bias of −0.14 °C and a root mean square error of 0.57 °C, which is comparable to the precision of satellite observations. The hourly gap-free SSTskin is vital for improving our comprehension of air–sea interactions and monitoring critical oceanographic processes with high-frequency variability. Full article
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Graphical abstract

Graphical abstract
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<p>The overall flowchart of multi-sensors fusion for SST<sub>skin</sub>.</p>
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<p>The DV of SST<sub>skin</sub> modeled by GOTM on 8 May 2007.</p>
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<p>Histogram of the difference between MTSAT-observed DV and GOTM DV on 8 May 2007.</p>
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<p>GOTM of the SST at 2 p.m. on 8 May 2007. (<b>a</b>) The SST profile at 122°E and 35.25°N; (<b>b</b>) the difference in the spatial distributions between SST<sub>skin</sub> and SST<sub>subskin</sub>.</p>
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<p>(<b>a</b>) The original hourly MTSAT SST on 8 May 2007. (<b>b</b>) The diurnal variation-corrected (normalized) hourly MTSAT SST on 8 May 2007.</p>
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<p>(<b>a</b>) The original hourly MTSAT SST on 8 May 2007. (<b>b</b>) The diurnal variation-corrected (normalized) hourly MTSAT SST on 8 May 2007.</p>
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<p>(<b>a</b>) Number of sensors available on 8 May 2007; (<b>b</b>) the fusion SST at 10:30 a.m. using Markov estimation.</p>
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<p>Covariance structure function of the East China Sea estimated from MTSAT in 2007. The spatial covariance functions at (<b>a</b>) zonal and (<b>b</b>) meridional directions for the SST variations. Temporal correlation with time lags computed using hourly SST (<b>c</b>). Red line is the fitting function. Vertical bars represent ±1 standard deviation.</p>
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<p>The hourly gap-free SST<sub>skin</sub> on 8 May 2007.</p>
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<p>The diurnal variation of SST<sub>skin</sub> at 124°E and 28°N on 8 May 2007.</p>
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<p>(<b>a</b>) Scatter plot between in situ SST<sub>skin</sub> and fusion SST<sub>skin</sub>. (<b>b</b>) The hourly mean bias and standard deviation during 2007.</p>
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11 pages, 606 KiB  
Article
An Ecologically Consistent Model of Growth for Hard-Bodied Marine Organisms
by Cian Warby, Frederic Dias, Franck Schoefs and Vikram Pakrashi
J. Mar. Sci. Eng. 2024, 12(11), 2067; https://doi.org/10.3390/jmse12112067 - 15 Nov 2024
Viewed by 349
Abstract
There are several factors to account for marine growth including but not limited to temperature, salinity, chlorophyll-a content, existing species in the environment and predating. This paper proposes a model of biological growth for hard species on marine structures, which can be compatible [...] Read more.
There are several factors to account for marine growth including but not limited to temperature, salinity, chlorophyll-a content, existing species in the environment and predating. This paper proposes a model of biological growth for hard species on marine structures, which can be compatible with site-specific and realistic ecology while also being able to translate the results for analyses linked to lifetime hydrodynamic or structural effects via commercial software or computing. The model preserves fundamentals of ecological aspects rather than using heuristics or random sampling to data fitting on sparsely collected information. The coefficients used in the proposed model align to the real world, with location-specific values, and can be adapted to new information. The growth model is demonstrated for Mythulis Edulis (blue mussel) colonisation to assess the lifetime hydrodynamic effects for the West Coast of Ireland and the Gulf of Guinea. The model can be extended to any hard growth approach. Full article
(This article belongs to the Section Ocean Engineering)
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Figure 1
<p>Examples of growth coefficient <math display="inline"><semantics> <mo>Φ</mo> </semantics></math> versus temperature <span class="html-italic">T</span>. Note how location-specific temperature-dependent growth functions are required and despite the similarity in the shape growth curves, temperature and species have different relationships in different locations of the world based on their tolerances.</p>
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<p>Examples of the vertical distribution of chlorophyll-a.</p>
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<p>An example of the vertical distribution of temperature (Ireland).</p>
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<p>Chlorophyll-a surface concentration for a one-year period. Satellite data can be used to adapt such values for any location for the proposed model.</p>
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<p>Sea surface temperature for a one-year period. Based on specific locations, they can vary significantly, impacting the growth patterns and related effects.</p>
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<p>Values of the thickness and growth coefficient as a function of depth at the end of the five-year period.</p>
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<p>Thickness of growth near the surface with time. Note how the proposed model responds to favourable ecological environments corresponding to seasons and also reflects where there is an absence of distinct seasons.</p>
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34 pages, 41034 KiB  
Article
The Dynamics of Air Pollution in the Southwestern Part of the Caspian Sea Basin (Based on the Analysis of Sentinel-5 Satellite Data Utilizing the Google Earth Engine Cloud-Computing Platform)
by Vladimir Tabunshchik, Aleksandra Nikiforova, Nastasia Lineva, Polina Drygval, Roman Gorbunov, Tatiana Gorbunova, Ibragim Kerimov, Cam Nhung Pham, Nikolai Bratanov and Mariia Kiseleva
Atmosphere 2024, 15(11), 1371; https://doi.org/10.3390/atmos15111371 - 14 Nov 2024
Viewed by 295
Abstract
The Caspian region represents a complex and unique system of terrestrial, coastal, and aquatic environments, marked by an exceptional landscape and biological diversity. This diversity, however, is increasingly threatened by substantial anthropogenic pressures. One notable impact of this human influence is the rising [...] Read more.
The Caspian region represents a complex and unique system of terrestrial, coastal, and aquatic environments, marked by an exceptional landscape and biological diversity. This diversity, however, is increasingly threatened by substantial anthropogenic pressures. One notable impact of this human influence is the rising concentration of pollutants atypical for the atmosphere. Advances in science and technology now make it possible to detect certain atmospheric pollutants using remote Earth observation techniques, specifically through data from the Sentinel-5 satellite, which provides continuous insights into atmospheric contamination. This article investigates the dynamics of atmospheric pollution in the southwestern part of the Caspian Sea basin using Sentinel-5P satellite data and the cloud-computing capabilities of the Google Earth Engine (GEE) platform. The study encompasses an analysis of concentrations of seven key pollutants: nitrogen dioxide (NO2), formaldehyde (HCHO), carbon monoxide (CO), ozone (O3), sulfur dioxide (SO2), methane (CH4), and the Aerosol Index (AI). Spatial and temporal variations in pollution fields were examined for the Caspian region and the basins of the seven rivers (key areas) flowing into the Caspian Sea: Sunzha, Sulak, Ulluchay, Karachay, Atachay, Haraz, and Gorgan. The research methodology is based on the use of data from the Sentinel-5 satellite, SRTM DEM data on absolute elevations, surface temperature data, and population density data. Data processing is performed using the Google Earth Engine cloud-computing platform and the ArcGIS software suite. The main aim of this study is to evaluate the spatiotemporal variability of pollutant concentration fields in these regions from 2018 to 2023 and to identify the primary factors influencing pollution distribution. The study’s findings reveal that the Heraz and Gorgan River basins have the highest concentrations of nitrogen dioxide and Aerosol Index levels, marking these basins as the most vulnerable to atmospheric pollution among those assessed. Additionally, the Gorgan basin exhibited elevated carbon monoxide levels, while the highest ozone concentrations were detected in the Sunzha basin. Our temporal analysis demonstrated a substantial influence of the COVID-19 pandemic on pollutant dispersion patterns. Our correlation analysis identified absolute elevation as a key factor affecting pollutant distribution, particularly for carbon monoxide, ozone, and aerosol indices. Population density showed the strongest correlation with nitrogen dioxide distribution. Other pollutants exhibited more complex distribution patterns, influenced by diverse mechanisms associated with local emission sources and atmospheric dynamics. Full article
(This article belongs to the Special Issue Study of Air Pollution Based on Remote Sensing (2nd Edition))
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<p>Geographic location of the study area.</p>
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<p>Overall methodology for air pollution assessment and the evaluation of its relationship with geographical factors.</p>
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<p>Distribution of Aerosol Index: (<b>a</b>) 2018, (<b>b</b>) 2019, (<b>c</b>) 2020, (<b>d</b>) 2021, (<b>e</b>) 2022, and (<b>f</b>) 2023.</p>
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<p>Distribution of Aerosol Index: (<b>a</b>) 2018, (<b>b</b>) 2019, (<b>c</b>) 2020, (<b>d</b>) 2021, (<b>e</b>) 2022, and (<b>f</b>) 2023.</p>
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<p>Distribution of nitrogen dioxide concentrations: (<b>a</b>) 2018, (<b>b</b>) 2019, (<b>c</b>) 2020, (<b>d</b>) 2021, (<b>e</b>) 2022, and (<b>f</b>) 2023.</p>
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<p>Distribution of ozone concentrations: (<b>a</b>) 2018, (<b>b</b>) 2019, (<b>c</b>) 2020, (<b>d</b>) 2021, (<b>e</b>) 2022, and (<b>f</b>) 2023.</p>
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<p>Distribution of ozone concentrations: (<b>a</b>) 2018, (<b>b</b>) 2019, (<b>c</b>) 2020, (<b>d</b>) 2021, (<b>e</b>) 2022, and (<b>f</b>) 2023.</p>
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<p>Distribution of carbon monoxide concentrations: (<b>a</b>) 2018, (<b>b</b>) 2019, (<b>c</b>) 2020, (<b>d</b>) 2021, (<b>e</b>) 2022, and (<b>f</b>) 2023.</p>
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<p>Distribution of carbon monoxide concentrations: (<b>a</b>) 2018, (<b>b</b>) 2019, (<b>c</b>) 2020, (<b>d</b>) 2021, (<b>e</b>) 2022, and (<b>f</b>) 2023.</p>
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<p>Distribution of formaldehyde concentrations: (<b>a</b>) 2018, (<b>b</b>) 2019, (<b>c</b>) 2020, (<b>d</b>) 2021, (<b>e</b>) 2022, and (<b>f</b>) 2023.</p>
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<p>Distribution of sulfur dioxide concentrations: (<b>a</b>) 2018, (<b>b</b>) 2019, (<b>c</b>) 2020, (<b>d</b>) 2021, (<b>e</b>) 2022, and (<b>f</b>) 2023.</p>
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<p>Distribution of methane concentrations: (<b>a</b>) 2018, (<b>b</b>) 2019, (<b>c</b>) 2020, (<b>d</b>) 2021, (<b>e</b>) 2022, and (<b>f</b>) 2023.</p>
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<p>Distribution of methane concentrations: (<b>a</b>) 2018, (<b>b</b>) 2019, (<b>c</b>) 2020, (<b>d</b>) 2021, (<b>e</b>) 2022, and (<b>f</b>) 2023.</p>
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<p>Intra-annual dynamics of average Aerosol Index concentrations in the river basins of Sunzha, Sulak, Ulluchay, Karachay, Atachay, Haraz, and Gorgan.</p>
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<p>Intra-annual dynamics of average carbon monoxide concentrations in the river basins of Sunzha, Sulak, Ulluchay, Karachay, Atachay, Haraz, and Gorgan.</p>
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<p>Intra-annual dynamics of average formaldehyde concentrations in the river basins of Sunzha, Sulak, Ulluchay, Karachay, Atachay, Haraz, and Gorgan.</p>
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<p>Intra-annual dynamics of average carbon ozone concentrations in the river basins of Sunzha, Sulak, Ulluchay, Karachay, Atachay, Haraz, and Gorgan.</p>
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<p>Intra-annual dynamics of average nitrogen dioxide concentrations in the river basins of Sunzha, Sulak, Ulluchay, Karachay, Atachay, Haraz, and Gorgan.</p>
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<p>Intra-annual dynamics of average sulfur dioxide concentrations in the river basins of Sunzha, Sulak, Ulluchay, Karachay, Atachay, Haraz, and Gorgan.</p>
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<p>Correlation diagrams between pollution indicators and geographic factors in the Caspian region: (<b>a</b>) 2019, (<b>b</b>) 2020, (<b>c</b>) 2021, and (<b>d</b>) 2022.</p>
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<p>Correlation diagrams between pollution indicators and geographic factors in the Sunzha River basin: (<b>a</b>) 2019, (<b>b</b>) 2020, (<b>c</b>) 2021, and (<b>d</b>) 2022.</p>
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<p>Correlation diagrams between pollution indicators and geographic factors in the Sulak River basin: (<b>a</b>) 2019, (<b>b</b>) 2020, (<b>c</b>) 2021, and (<b>d</b>) 2022.</p>
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<p>Correlation diagrams between pollution indicators and geographic factors in the Ulluchay River basin: (<b>a</b>) 2019, (<b>b</b>) 2020, (<b>c</b>) 2021, and (<b>d</b>) 2022.</p>
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<p>Correlation diagrams between pollution indicators and geographic factors in the Karachay River basin: (<b>a</b>) 2019, (<b>b</b>) 2020, (<b>c</b>) 2021, and (<b>d</b>) 2022.</p>
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<p>Correlation diagrams between pollution indicators and geographic factors in the Atachay River basin: (<b>a</b>) 2019, (<b>b</b>) 2020, (<b>c</b>) 2021, and (<b>d</b>) 2022.</p>
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<p>Correlation diagrams between pollution indicators and geographic factors in the Haraz River basin: (<b>a</b>) 2019, (<b>b</b>) 2020, (<b>c</b>) 2021, and (<b>d</b>) 2022.</p>
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<p>Correlation diagrams between pollution indicators and geographic factors in the Gorgan River basin: (<b>a</b>) 2019, (<b>b</b>) 2020, (<b>c</b>) 2021, and (<b>d</b>) 2022.</p>
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<p>Average Aerosol Index values from 2018 to 2023 in the basins of small and medium rivers of the Caspian Sea.</p>
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<p>Average nitrogen dioxide concentrations from 2018 to 2023 in the basins of small- and medium-sized rivers of the Caspian Sea.</p>
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<p>Average tropospheric ozone concentrations from 2018 to 2023 in the basins of small- and medium-sized rivers of the Caspian Sea.</p>
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<p>Average carbon monoxide concentrations in the basins of small- and medium-sized rivers in the Caspian Sea from 2018 to 2023.</p>
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<p>Average formaldehyde concentrations from 2018 to 2023 in the basins of small- and medium-sized rivers in the Caspian Sea region.</p>
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<p>Average sulfur dioxide concentrations in the basins of small- and medium-sized rivers in the Caspian Sea from 2018 to 2023.</p>
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20 pages, 19918 KiB  
Article
Anatomical-Foliar Diversity of Agave salmiana subsp. salmiana (Asparagaceae) in Three Populations of the Teotihuacán Region (Mexico)
by Estela Sandoval-Zapotitla, Lorena E. Chávez-Güitrón, Florencia del C. Salinas-Pérez, Ulises Rosas and Alejandro Vallejo-Zamora
Plants 2024, 13(22), 3195; https://doi.org/10.3390/plants13223195 - 14 Nov 2024
Viewed by 340
Abstract
Agave salmiana Otto ex Salm-Dyck is an endemic Mexican plant distributed from 1230 to 2460 m above sea level, native to the arid zones of central and southern Mexico. It is a traditionally used species, with morphotypes ranging from wild to cultivated, with [...] Read more.
Agave salmiana Otto ex Salm-Dyck is an endemic Mexican plant distributed from 1230 to 2460 m above sea level, native to the arid zones of central and southern Mexico. It is a traditionally used species, with morphotypes ranging from wild to cultivated, with an ample cultural and management history. The species is important because it generates employment, and its products are used for self-consumption and are marketed as raw materials; however, little is known about its leaf anatomical description or studies that report the variation in its characters in terms of its level of management and its altitudinal gradient. To address this, we collected leaf samples from three localities of the Teotihuacan region in the State of Mexico (Mexico) and obtained anatomical leaf sections; with these, we also obtained thirty-eight parameters to quantitatively describe leaf anatomy. Thus, in this study, the general anatomical description of the leaf of Agave salmiana subsp. salmiana is presented. Unique leaf characters and others shared with the species of the genus were identified for the leaf of A. salmiana subsp. salmiana. In addition, significant variation was observed when comparing the three sampled localities (78.95%). From the analysis of anatomical characters, abaxial outer periclinal wall length, length of adaxial palisade parenchyma cells, fiber length, surface area of abaxial epidermal cells, width of abaxial palisade parenchyma cells, and total length of parenchyma in adaxial palisade were found to distinguish individuals from the three localities analyzed and the differences are related to management and altitude gradients. Full article
(This article belongs to the Section Plant Structural Biology)
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Figure 1

Figure 1
<p>Cross-section of the leaf of <span class="html-italic">Agave salmiana</span> subsp. <span class="html-italic">salmiana</span>. (<b>A</b>) Adaxial epidermis with smooth thick cuticle, a single layer of oblong cells with greatly thickened outer periclinal walls (asterisk). Stomata with guard cells sunken (arrow), but at the level of the rest of the epidermal cells, with prominent external cuticular ridges (double arrow). Elongated substomatal chamber (arrowhead). (<b>B</b>) Abaxial epidermis, broad substomatal chamber (arrowhead), and styloid in palisade parenchyma (arrows). (<b>C</b>) Margin with reserve and palisade parenchyma, and vascular bundles in a central position. Abaxial left side, adaxial right side<b>.</b> (<b>D</b>) Small vascular bundles with sclerenchyma sheath outside the phloem and parenchyma sheath around the bundles (arrow). (<b>E</b>) Margin. Vascular bundles surrounded by a sclerenchyma sheath. Parenchyma with styloid (arrow). (<b>F</b>) Middle vein. Major vascular bundles, sclerenchyma sheath in xylem (X) and phloem (Pb), and parenchyma sheath around the vascular bundle (arrow).</p>
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<p>Variable characters among the three locations of <span class="html-italic">Agave salmiana</span> subsp. <span class="html-italic">salmiana</span>. Front view: surface area of the adaxial epidermal cells (<b>A</b>–<b>C</b> black circle); length of the abaxial guard cells (<b>D</b>–<b>F</b>). Letters with a green frame = Tecámac, red = San Martín de las Pirámides, and blue = Teotihuacán.</p>
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<p>Cross-section: adaxial cuticle width (<b>A</b>–<b>D</b>); adaxial outer periclinal wall length (<b>E</b>–<b>G</b> yellow bar); cross-sectional area of the adaxial epidermal cells (<b>E</b>–<b>G</b> black circle); abaxial outer periclinal wall length (<b>H</b>–<b>J</b> yellow bar); abaxial outer periclinal wall width (<b>H</b>–<b>J</b> orange bar); and wide abaxial palisade parenchyma cells (<b>H</b>–<b>J</b> black bar). Letters with a green frame = Tecámac, red = San Martín de las Pirámides, and blue = Teotihuacán.</p>
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<p>Cross-section: total length of the adaxial palisade parenchyma (<b>A</b>–<b>C</b> black bars); total length of the abaxial palisade parenchyma (<b>D</b>–<b>F</b> black bars). Letters with a green frame = Tecámac, red = San Martín de las Pirámides, and blue = Teotihuacán.</p>
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<p>(<b>A</b>) Graph of linear discriminant analysis (100% model precision). (<b>B</b>) Boxplot for the eight characters with the highest values; the first four characters correspond to the first discriminant (LD1) and the last four to the second discriminant (LD2). Green boxplot = Tecámac, red = San Martín de las Pirámides, and blue = Teotihuacán. Unequal letters indicate different groups in Tukey’s test (<span class="html-italic">p</span> &lt; 0.05).</p>
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18 pages, 8260 KiB  
Article
Role of the Europe–China Pattern Teleconnection in the Interdecadal Autumn Dry–Wet Fluctuations in Central China
by Linwei Jiang, Wenhao Gao, Kexu Zhu, Jianqiu Zheng and Baohua Ren
Atmosphere 2024, 15(11), 1363; https://doi.org/10.3390/atmos15111363 - 13 Nov 2024
Viewed by 225
Abstract
Based on statistical analyses of long-term reanalysis data, we have investigated the interdecadal variations of autumn precipitation in central China (APC-d) and the associated atmospheric teleconnection. It reveals that the increased autumn rainfall in central China during the last decade is a portion [...] Read more.
Based on statistical analyses of long-term reanalysis data, we have investigated the interdecadal variations of autumn precipitation in central China (APC-d) and the associated atmospheric teleconnection. It reveals that the increased autumn rainfall in central China during the last decade is a portion of the APC-d, which exhibits a high correlation coefficient of 0.7 with the interdecadal variations of the Europe–China pattern (EC-d pattern) teleconnection. The EC-d pattern teleconnection presents in a “+-+” structure over Eurasia, putting central China into the periphery of a quasi-barotropic anticyclonic high-pressure anomaly. Driven by positive vorticity advection and the inflow of warmer and moist air from the south, central China experiences enhanced ascending motion and abundant water vapor supply, resulting in increased rainfall. Further analysis suggests that the EC-d pattern originates from the exit of the North Atlantic jet and propagates eastward. It is captured by the Asian westerly jet stream and proceeds towards East Asia through the wave–mean flow interaction. The wave train acquires effective potential energy from the mean flow by the baroclinic energy conversion and simultaneously obtains kinetic energy from the basic westerly jet zones across the North Atlantic and the East Asian coasts. The interdecadal variation of the mid-latitude North Atlantic sea surface temperature (MAT-d) exhibits a significant negative relationship with EC-d, serving as a modulating factor for the EC-d pattern teleconnection. Experiments with CMIP6 models predict that the interdecadal variations in APC-d, EC-d, and MAT-d will maintain stable high correlations for the rest of the 21st century. These findings may contribute to forecasting the interdecadal autumn dry–wet conditions in central China. Full article
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Figure 1
<p>(<b>a</b>) Climatological autumn precipitation in 1901–2020 [unit: mm/mon]; (<b>b</b>) time series of normalized year-to-year [gray bars] and the interdecadal components [green line] of the autumn precipitation in central China (APC-d index); (<b>c</b>) regression map of precipitation [contours, dotted areas are significant at <span class="html-italic">p</span> &lt; 0.05; unit: mm/mon] on the APC-d index; and (<b>d</b>) same as <a href="#atmosphere-15-01363-f001" class="html-fig">Figure 1</a>c, but for the results in the Global Precipitation Climatology Centre (GPCC) dataset for the same period. The black boxes denote central China (27–37° N, 102–114° E).</p>
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<p>Regression of the interdecadal components on the APC-d index in autumn during 1905–2011, including (<b>a</b>) zonal wind at 200 hPa [shadings; dotted areas are significant at <span class="html-italic">p</span> &lt; 0.05; unit: m/s], (<b>b</b>) geopotential height at 500 hPa [shadings; dotted areas are significant at <span class="html-italic">p</span> &lt; 0.05; unit: gpm], (<b>c</b>) wind field at 700 hPa [arrows; blue areas are significant at <span class="html-italic">p</span> &lt; 0.05; unit: m/s], and (<b>d</b>) pressure–longitude cross-section of omega averaged between 27° and 37° N [only shadings significant at <span class="html-italic">p</span> &lt; 0.05 are shown; unit: Pa/s]. The black boxes denote the boundaries of central China (27–37° N, 102–114° E), and lines denote 102° E and 114°, respectively.</p>
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<p>Regression of the interdecadal components on the APC-d index in autumn during 1905–2011, including the meridional wind [only shadings significant at <span class="html-italic">p</span> &lt; 0.05 are shown; unit: m/s] and the geopotential height [contours; interval: 2.5 gpm; solid lines: positive; dashed lines: negative] at 200 hPa. The black box denotes the boundaries of central China (27–37° N, 102°–114° E).</p>
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<p>Spatial pattern of EOF2 in (<b>a</b>) original meridional wind and (<b>b</b>) interdecadal meridional wind at 200 hPa in 20°–60° N, 0°–150° E in autumn during 1905–2011. (<b>c</b>) Time series of year-to-year [the EC-index; gray bars], the 9 yr-moved [black line] PC2 of EOF2 in original V200. (<b>d</b>) Time series of PC2 of EOF2 in interdecadal V200 [the EC-d index; red line] and the interdecadal autumn precipitation in central China [APC-d index; green line]. (<b>e</b>) Same as <a href="#atmosphere-15-01363-f003" class="html-fig">Figure 3</a>, but for the results with regard to the EC-d index.</p>
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<p>(<b>a</b>–<b>d</b>) is same as <a href="#atmosphere-15-01363-f002" class="html-fig">Figure 2</a>a–d but for the results with regard to the EC-d index.</p>
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<p>Regression of the interdecadal components on the EC-d index in autumn during 1905–2011, including (<b>a</b>) water vapor flux [arrows; only arrows significant at <span class="html-italic">p</span> &lt; 0.05 are shown; unit: 10<sup>−2</sup> kg/(m·s)] and its divergence [shadings; dotted areas are significant at <span class="html-italic">p</span> &lt; 0.05; unit: 10<sup>−6</sup> kg/(m<sup>2</sup>·s)] integrated from 1000 hPa to 300 hPa; (<b>b</b>) pressure-longitude cross-section between 27° and 37° N of the horizontal vorticity advection [shadings; dotted areas are significant at <span class="html-italic">p</span> &lt; 0.05, unit: 10<sup>−12</sup> Pa/s<sup>2</sup>]; and (<b>c</b>) pressure-longitude cross-section between 27° and 37° N of the horizontal temperature advection [shadings; dotted areas are significant at <span class="html-italic">p</span> &lt; 0.05, unit: 10<sup>−7</sup> degK/s]. The black box denotes the boundaries of central China (27–37° N, 102–114° E). The black lines denote 102° E and 114° E, respectively.</p>
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<p>Regression of the interdecadal components on the EC-d index in autumn during 1905–2011, including (<b>a</b>) vorticity source S’ [shadings; unit: 10<sup>−11</sup> s<sup>−2</sup>] with wind anomalies at 200 hPa [purple arrows; only arrows significant at <span class="html-italic">p</span> &lt; 0.05 are shown; unit:20 m/s] and (<b>b</b>) plumb wave activity flux [purple arrows; only arrows significant at <span class="html-italic">p</span> &lt; 0.05 are shown; unit: 1.5 m<sup>2</sup>/s<sup>2</sup>] and its divergence [shadings; unit: m/s<sup>2</sup>] at 200 hPa. The red lines denote the basic westerly flow [U &gt; 20 m/s; interval: 5 m/s]. The black box denotes the boundaries of central China (27–37° N, 102–114° E).</p>
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<p>(<b>a</b>) CK (conversion of kinetic energy) and (<b>b</b>) CP (conversion of potential energy) of the EC-d pattern teleconnection integrated from 1000 hPa to 10 hPa [shadings; unit: m<sup>2</sup>/s<sup>3</sup>]. The red lines denote the basic westerly flow (U &gt; 20 m/s) [interval: 5]. The black box denotes the boundaries of central China (27–37° N, 102–114° E).</p>
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<p>Regression of the interdecadal components of sea surface temperature (SST) [shadings; unit: degC] on (<b>a</b>) the EC-d index and (<b>b</b>) the AMO index in autumn during 1905–2011. (<b>c</b>) The time series of the MAT-d index [blue line] and the EC-d index [red line]. The black box denotes mid-latitude North Atlantic (30–60° N, 55–25° W).</p>
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<p>Regression of the interdecadal components on the negative MAT-d index in autumn during 1905–2011, including (<b>a</b>) SST [shadings; only shadings significant at <span class="html-italic">p</span> &lt; 0.05 are shown; unit: degC] and (<b>b</b>) wind field 700 hPa [arrows; blue areas are significant at <span class="html-italic">p</span> &lt; 0.05; unit: m/s]. (<b>c</b>) Vorticity source S’ [shadings; unit: 10<sup>−10</sup> s<sup>−2</sup>] at 200 hPa of the negative MAT-d. (<b>d</b>) Same as <a href="#atmosphere-15-01363-f003" class="html-fig">Figure 3</a>, but for the results with regard to the MAT-d index. The black box denotes mid-latitude North Atlantic (30–60° N, 55–25° W).</p>
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<p>The time series of the APC-d index [green bars], the EC-d index [red line], and the MAT index [blue line] during autumn in 2020–2090.</p>
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26 pages, 9635 KiB  
Article
A Raster-Based Multi-Objective Spatial Optimization Framework for Offshore Wind Farm Site-Prospecting
by Loukas Katikas, Themistoklis Kontos, Panayiotis Dimitriadis and Marinos Kavouras
ISPRS Int. J. Geo-Inf. 2024, 13(11), 409; https://doi.org/10.3390/ijgi13110409 - 13 Nov 2024
Viewed by 480
Abstract
Siting an offshore wind project is considered a complex planning problem with multiple interrelated objectives and constraints. Hence, compactness and contiguity are indispensable properties in spatial modeling for Renewable Energy Sources (RES) planning processes. The proposed methodology demonstrates the development of a raster-based [...] Read more.
Siting an offshore wind project is considered a complex planning problem with multiple interrelated objectives and constraints. Hence, compactness and contiguity are indispensable properties in spatial modeling for Renewable Energy Sources (RES) planning processes. The proposed methodology demonstrates the development of a raster-based spatial optimization model for future Offshore Wind Farm (OWF) multi-objective site-prospecting in terms of the simulated Annual Energy Production (AEP), Wind Power Variability (WPV) and the Depth Profile (DP) towards an integer mathematical programming approach. Geographic Information Systems (GIS), statistical modeling, and spatial optimization techniques are fused as a unified framework that allows exploring rigorously and systematically multiple alternatives for OWF planning. The stochastic generation scheme uses a Generalized Hurst-Kolmogorov (GHK) process embedded in a Symmetric-Moving-Average (SMA) model, which is used for the simulation of a wind process, as extracted from the UERRA (MESCAN-SURFEX) reanalysis data. The generated AEP and WPV, along with the bathymetry raster surfaces, are then transferred into the multi-objective spatial optimization algorithm via the Gurobi optimizer. Using a weighted spatial optimization approach, considering and guaranteeing compactness and continuity of the optimal solutions, the final optimal areas (clusters) are extracted for the North and Central Aegean Sea. The optimal OWF clusters, show increased AEP and minimum WPV, particularly across offshore areas from the North-East Aegean (around Lemnos Island) to the Central Aegean Sea (Cyclades Islands). All areas have a Hurst parameter in the range of 0.55–0.63, indicating greater long-term positive autocorrelation in specific areas of the North Aegean Sea. Full article
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Graphical abstract

Graphical abstract
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<p>Overview of the methodology discretizing all processing and modeling steps, including (1) offshore wind resource assessment and stochastic simulation and (2) the multiple factors spatial optimization for OWFs site-prospecting.</p>
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<p>Study area spatial extent and the bathymetric profile (in m).</p>
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<p>UERRA (MESCAN-SURFEX) reanalysis statistical properties—10 m for: (<b>a</b>) Mean (m/s), (<b>b</b>) Standard Deviation (m/s), (<b>c</b>) Skewness and, (<b>d</b>) Kurtosis.</p>
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<p>(<b>Left</b>) Raster array image, as extracted from the input data spatial extent and mask, with decision variable <span class="html-italic">Ci,j</span> and (<b>Right</b>) Customized final raster array with decision variable <span class="html-italic">Xi,j</span> (binary) that calculates all available neighbors participating in compactness calculation (number of free edges of the cluster perimeter). Modified from [<a href="#B60-ijgi-13-00409" class="html-bibr">60</a>].</p>
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<p>Calculation of compactness based on the minimization of the total cluster perimeter (<b>left</b>), and the various levels of fragmentation observed during the optimization process (<b>A</b>–<b>F</b>, <b>right</b>) (modified by Reference [<a href="#B60-ijgi-13-00409" class="html-bibr">60</a>]).</p>
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<p>Contiguity check using the BFS algorithm for each Gurobi optimizer solution (modified by Reference [<a href="#B42-ijgi-13-00409" class="html-bibr">42</a>]).</p>
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<p>(<b>a</b>) PBF shape parameter <span class="html-italic">c</span>, (<b>b</b>) PBF shape parameter <span class="html-italic">a</span> and (<b>c</b>) PBF scale parameter <span class="html-italic">b</span>.</p>
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<p>(<b>a</b>) Hurst coefficient (<span class="html-italic">H</span>), (<b>b</b>) Slope (<span class="html-italic">q</span>) for the study area, and (<b>c</b>) climacograms for different areas (pixels) between UERRA and SMA-GHK long-term simulated power output variance using Equation (1) (modified by Reference [<a href="#B42-ijgi-13-00409" class="html-bibr">42</a>]).</p>
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<p>Exemplary optimization results for 8 (<b>a</b>–<b>c</b>) and 32 cells (<b>d</b>–<b>f</b>) under varying compactness weights (modified by Reference [<a href="#B42-ijgi-13-00409" class="html-bibr">42</a>]).</p>
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<p>(<b>a</b>) Estimated AEP (<b>b</b>) WPV and Final OWF areas for (<b>c</b>) Scenario 1 (Fixed-bottom foundations) (<b>d</b>) Scenario 2 (Floating foundations) (<b>e</b>) Scenario 3 (No restrictions) (modified by Reference [<a href="#B42-ijgi-13-00409" class="html-bibr">42</a>]).</p>
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<p>Coefficient of Variation (CV) for the Central and North Aegean Sea, as extracted from UERRA dataset (historical wind speed time series spanning 38 years).</p>
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29 pages, 17765 KiB  
Article
Trends of Climate Extremes and Their Relationships with Tropical Ocean Temperatures in South America
by Luiz Octávio Fabrício dos Santos, Nadja Gomes Machado, Carlos Alexandre Santos Querino and Marcelo Sacardi Biudes
Earth 2024, 5(4), 844-872; https://doi.org/10.3390/earth5040043 - 11 Nov 2024
Viewed by 347
Abstract
South America has experienced significant changes in climate patterns over recent decades, particularly in terms of precipitation and temperature extremes. This study analyzes trends in climate extremes from 1979 to 2020 across South America, focusing on their relationships with sea surface temperature (SST) [...] Read more.
South America has experienced significant changes in climate patterns over recent decades, particularly in terms of precipitation and temperature extremes. This study analyzes trends in climate extremes from 1979 to 2020 across South America, focusing on their relationships with sea surface temperature (SST) anomalies in the Pacific and Atlantic Oceans. The analysis uses precipitation and temperature indices, such as the number of heavy rainfall days (R10mm, R20mm, R30mm), total annual precipitation (PRCPTOT), hottest day (TXx), and heatwave duration (WSDI), to assess changes over time. The results show a widespread decline in total annual precipitation across the continent, although some regions, particularly in the northeast and southeast, experienced an increase in the intensity and frequency of extreme precipitation events. Extreme temperatures have also risen consistently across South America, with an increase in both the frequency and duration of heat extremes, indicating an ongoing warming trend. The study also highlights the significant role of SST anomalies in both the Pacific and Atlantic Oceans in driving these climate extremes. Strong correlations were found between Pacific SST anomalies (Niño 3.4 region) and extreme precipitation events in the northern and southern regions of South America. Similarly, Atlantic SST anomalies, especially in the Northern Atlantic (TNA), exhibited notable impacts on temperature extremes, particularly heatwaves. These findings underscore the complex interactions between SST anomalies and climate variability in South America, providing crucial insights into the dynamics of climate extremes in the region. Understanding these relationships is essential for developing effective adaptation and mitigation strategies in response to the increasing frequency and intensity of climate extremes. Full article
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Figure 1
<p>Climate normal for precipitation and air temperature and location of the climate reference regions from the Sixth Assessment Report of the Intergovernmental Panel on Climate Change (IPCC AR6) for South America from 1979 to 2020.</p>
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<p>Location of the ENSO (Niño 1 + 2, Niño 3, Niño 3.4, and Niño 4) and Atlantic Dipole (TNA and TSA) regions in the equatorial Pacific and tropical Atlantic, respectively.</p>
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<p>Spatial distribution of trends from 1979 to 2020: number of heavy precipitation days (R10mm) (<b>a</b>); number of very heavy precipitation days (R20mm) (<b>b</b>); number of days above 30 mm (R30mm) (<b>c</b>); max 1-day precipitation amount (Rx1day) (<b>d</b>); max 5-day precipitation amount (Rx5day) (<b>e</b>); annual total wet day precipitation (PRCPTOT) (<b>f</b>); simple daily intensity index (SDII) (<b>g</b>); precipitation on very wet days (R95p) (<b>h</b>); precipitation on extremely wet days (R99p) (<b>i</b>); consecutive wet days (CWD) (<b>j</b>); and consecutive dry days (CDD) (<b>k</b>) over the climate reference regions of the Sixth Assessment Report of the Intergovernmental Panel on Climate Change (IPCC—AR6) on South America. Only values with statistical significance at the 5% level are presented in the maps.</p>
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<p>Spatial distribution of trends from 1979 to 2020: warmest day (TXx) (<b>a</b>); warmest night (TNx) (<b>b</b>); coldest day (TXn) (<b>c</b>); coldest night (TNn) (<b>d</b>); diurnal temperature Range (DTR) (<b>e</b>); warm spell duration (WSDI) (<b>f</b>); cold spell duration (CSDI) (<b>g</b>); warm days (TX90p) (<b>h</b>); warm nights (TN90p) (<b>i</b>); cool days (TX10p) (<b>j</b>); cool nights (TN10p) (<b>k</b>); and frost days (FD) (<b>l</b>) over the climate reference regions of the Sixth Assessment Report of the Intergovernmental Panel on Climate Change (IPCC—AR6) on South America. Only values with statistical significance at the 5% level are presented in the maps.</p>
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<p>Probability density function (PDF) of the annual frequency of the following extreme precipitation indices over South America from 1979 to 2020: number of heavy precipitation days (R10mm) (<b>a</b>); number of very heavy precipitation days (R20mm) (<b>b</b>); number of days with precipitation above 50 mm (R50mm) (<b>c</b>); maximum 1-day precipitation amount (Rx1day) (<b>d</b>); maximum 5-day precipitation amount (Rx5day) (<b>e</b>); annual total wet-day precipitation (PRCPTOT) (<b>f</b>); simple daily intensity index (SDII) (<b>g</b>); precipitation on very wet days (R95p) (<b>h</b>); precipitation on extremely wet days (R99p) (<b>i</b>); consecutive wet days (CWD) (<b>j</b>); consecutive dry days (CDD) (<b>k</b>).</p>
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<p>Probability density function (PDF) of the annual frequency of the following extreme temperature indices over South America from 1979 to 2020: warmest day (TXx) (<b>a</b>); warmest night (TNx) (<b>b</b>); coldest day (TXn) (<b>c</b>); coldest night (TNn) (<b>d</b>); diurnal temperature range (DTR) (<b>e</b>); warm spell duration (WSDI) (<b>f</b>); cold spell duration (CSDI) (<b>g</b>); warm days (TX90p) (<b>h</b>); warm nights (TN90p) (<b>i</b>); cool days (TX10p) (<b>j</b>); cool nights (TN10p) (<b>k</b>) and frost days (FD) (<b>l</b>).</p>
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<p>Pearson correlations between Pacific SST anomalies in the Niño 3.4 region and extreme precipitation indices: number of heavy precipitation days (R10mm) (<b>a</b>); number of very heavy precipitation days (R20mm) (<b>b</b>); number of days above 30 mm (R30mm) (<b>c</b>); max 1-day precipitation amount (Rx1day) (<b>d</b>); max 5-day precipitation amount (Rx5day) (<b>e</b>); annual total wet day precipitation (PRCPTOT) (<b>f</b>); simple daily intensity index (SDII) (<b>g</b>); precipitation on very wet days (R95p) (<b>h</b>); precipitation on extremely wet days (R99p) (<b>i</b>); consecutive wet days (CWD) (<b>j</b>); and consecutive dry days (CDD) (<b>k</b>) over the climate reference regions of the Sixth Assessment Report of the Intergovernmental Panel on Climate Change (IPCC—AR6) on South America from 1979 to 2020. Only values with statistical significance at the 5% level are presented in the maps.</p>
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<p>Pearson correlations between Atlantic SST anomalies in the Northern Atlantic Ocean (TNA) sector and extreme precipitation indices: number of heavy precipitation days (R10mm) (<b>a</b>); number of very heavy precipitation days (R20mm) (<b>b</b>); number of days above 30 mm (R30mm) (<b>c</b>); max 1-day precipitation amount (Rx1day) (<b>d</b>); max 5-day precipitation amount (Rx5day) (<b>e</b>); annual total wet day precipitation (PRCPTOT) (<b>f</b>); simple daily intensity index (SDII) (<b>g</b>); precipitation on very wet days (R95p) (<b>h</b>); precipitation on extremely wet days (R99p) (<b>i</b>); consecutive wet days (CWD) (<b>j</b>); and consecutive dry days (CDD) (<b>k</b>) over the climate reference regions of the Sixth Assessment Report of the Intergovernmental Panel on Climate Change (IPCC—AR6) on South America from 1979 to 2020. Only values with statistical significance at the 5% level are presented in the maps.</p>
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<p>Relationship between sea surface temperature (SST) anomalies in the Pacific Ocean (Niño 3.4), Northern and Southern Atlantic Ocean sectors (TNA) (TSA), and extreme climate precipitation indices: number of heavy precipitation days (R10mm) (<b>A</b>); number of very heavy precipitation days (R20mm) (<b>B</b>); number of days above 30 mm (R30mm) (<b>C</b>); max 1-day precipitation amount (Rx1day) (<b>D</b>); max 5-day precipitation amount (Rx5day) (<b>E</b>); annual total wet day precipitation (PRCPTOT) (<b>F</b>); simple daily intensity index (SDII) (<b>G</b>); precipitation on very wet days (R95p) (<b>H</b>); precipitation on extremely wet days (R99p) (<b>I</b>); consecutive wet days (CWD) (<b>J</b>); and consecutive dry days (CDD) (<b>K</b>) over South America from 1979 to 2020.</p>
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<p>Pearson correlation between sea surface temperature (SST) anomalies in the Pacific Ocean over the Nino 3.4 region and extreme climatic temperature indices: warmest day (TXx) (<b>a</b>); warmest night (TNx) (<b>b</b>); coldest day (TXn) (<b>c</b>); coldest night (TNn) (<b>d</b>); diurnal temperature Range (DTR) (<b>e</b>); warm spell duration (WSDI) (<b>f</b>); cold spell duration (CSDI) (<b>g</b>); warm days (TX90p) (<b>h</b>); warm nights (TN90p) (<b>i</b>); cool days (TX10p) (<b>j</b>); cool nights (TN10p) (<b>k</b>); and frost days (FD) (<b>l</b>) over the climate reference regions of the Sixth Assessment Report of the Intergovernmental Panel on Climate Change (IPCC—AR6) on South America from 1979 to 2020. Only values with statistical significance at the 5% level are presented in the maps.</p>
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<p>Pearson correlation coefficients between sea surface temperature (SST) anomalies in the Northern Atlantic Ocean (TNA) sector and extreme climatic temperature indices: warmest day (TXx) (<b>a</b>); warmest night (TNx) (<b>b</b>); coldest day (TXn) (<b>c</b>); coldest night (TNn) (<b>d</b>); diurnal temperature Range (DTR) (<b>e</b>); warm spell duration (WSDI) (<b>f</b>); cold spell duration (CSDI) (<b>g</b>); warm days (TX90p) (<b>h</b>); warm nights (TN90p) (<b>i</b>); cool days (TX10p) (<b>j</b>); cool nights (TN10p) (<b>k</b>); and frost days (FD) (<b>l</b>) over the climate reference regions of the Sixth Assessment Report of the Intergovernmental Panel on Climate Change (IPCC—AR6) on South America from 1979 to 2020. Only values with statistical significance at the 5% level are presented in the maps.</p>
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<p>Relationship between sea surface temperature (SST) anomalies in the Pacific Ocean (Niño 3.4), Northern and Southern Atlantic Ocean sectors (TNA) (TSA), and extreme climate temperature indices: warmest day (TXx) (<b>A</b>); warmest night (TNx) (<b>B</b>); coldest day (TXn) (<b>C</b>); coldest night (TNn) (<b>D</b>); diurnal temperature Range (DTR) (<b>E</b>); warm spell duration (WSDI) (<b>F</b>); cold spell duration (CSDI) (<b>G</b>); warm days (TX90p) (<b>H</b>); warm nights (TN90p) (<b>I</b>); cool days (TX10p) (<b>J</b>); cool nights (TN10p) (<b>K</b>); and frost days (FD) (<b>L</b>) over South America from 1979 to 2020.</p>
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<p>Atmospheric circulation climatology (<b>a</b>,<b>d</b>,<b>g</b>) and observed atmospheric circulation under El Niño (<b>b</b>,<b>e</b>,<b>h</b>) and La Niña (<b>c</b>,<b>f</b>,<b>i</b>) conditions at pressure levels of 200 hPa, 500 hPa, and 850 hPa, respectively, over South America. The shaded region represents wind speed in m s<sup>−1</sup>. The climatology period is from 1981 to 2010, while the observed data refers to the mean composites of the intense El Niño events in 1982–1983, 1997–1998, and 2015–2016, and La Niña in 1988–1989, 1999–2000, and 2010–2011 in the December–January–February (DJF) quarter.</p>
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<p>Atmospheric circulation climatology (<b>a</b>,<b>d</b>,<b>g</b>) and observed atmospheric circulation under El Niño (<b>b</b>,<b>e</b>,<b>h</b>) and La Niña (<b>c</b>,<b>f</b>,<b>i</b>) conditions at pressure levels of 200 hPa, 500 hPa, and 850 hPa, respectively, over South America. The shaded region represents wind speed in m s<sup>−1</sup>. The climatology period is from 1981 to 2010, while the observed data refers to the mean composites of the intense El Niño events in 1982–1983, 1997–1998, and 2015–2016 and La Niña in 1988–1989, 1999–2000, and 2010–2011 in the June–July–August (JJA) quarter.</p>
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<p>Climatology (blue vectors) and anomaly (red vectors) of vertical wind velocity between 5 °S and 15°S during El Niño (<b>a</b>) and La Niña (<b>b</b>) events in the December-January-February (DJF) quarter. (<b>c</b>,<b>d</b>) Vertical wind speed (filled contours) and wind direction (arrows) between 5 °S and 15 °S during El Niño (<b>c</b>) and La Niña (<b>d</b>) events in the DJF quarter. (<b>e</b>,<b>f</b>) Sea surface temperature (SST) anomalies and precipitation anomalies over the continent between 5 °S and 15 °S during El Niño (<b>e</b>) and La Niña (<b>f</b>) events in the DJF quarter. (<b>g</b>,<b>h</b>) Air temperature anomalies over the continent between 5 °S and 15 °S during El Niño (<b>g</b>) and La Niña (<b>h</b>) events in the DJF quarter. Data correspond to the composite averages of El Niño (1982–1983, 1997–1998, and 2015–2016) and La Niña (1988–1989, 1999–2000, and 2010–2011) events in the DJF quarter.</p>
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<p>Climatology (blue vectors) and anomaly (red vectors) of vertical wind velocity between 5 °S and 15 °S during El Niño (<b>a</b>) and La Niña (<b>b</b>) events in the June-July-August (JJA) quarter. (<b>c</b>,<b>d</b>) Vertical wind speed (filled contours) and wind direction (vectors) between 5 °S and 15 °S during El Niño (<b>c</b>) and La Niña (<b>d</b>) events in the JJA quarter. (<b>e</b>,<b>f</b>) Sea surface temperature (SST) anomalies and precipitation anomalies over the continent between 5 °S and 15 °S during El Niño (<b>e</b>) and La Niña (<b>f</b>) events in the JJA quarter. (<b>g</b>,<b>h</b>) Air temperature anomalies over the continent between 5 °S and 15 °S during El Niño (<b>g</b>) and La Niña (<b>h</b>) events in the JJA quarter. Data correspond to the composite averages of El Niño (1982–1983, 1997–1998, and 2015–2016) and La Niña (1988–1989, 1999–2000, and 2010–2011) events in the JJA quarter.</p>
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20 pages, 5211 KiB  
Article
Spatial Distribution and Decadal Variability of 129I and 236U in the Western Mediterranean Sea
by Maria Leimbacher, Lorenza Raimondi, Maxi Castrillejo, Christof Vockenhuber, Habacuc Pérez-Tribouillier, Katrin Schroeder, Toste Tanhua and Núria Casacuberta
J. Mar. Sci. Eng. 2024, 12(11), 2039; https://doi.org/10.3390/jmse12112039 - 11 Nov 2024
Viewed by 454
Abstract
This study investigates the spatial and temporal distribution of the artificial radionuclides 129I and 236U in the Western Mediterranean Sea, focusing on their connection to radionuclide sources and circulation dynamics. Taking advantage of unprecedented precision of accelerator mass spectrometry, both tracers [...] Read more.
This study investigates the spatial and temporal distribution of the artificial radionuclides 129I and 236U in the Western Mediterranean Sea, focusing on their connection to radionuclide sources and circulation dynamics. Taking advantage of unprecedented precision of accelerator mass spectrometry, both tracers were firstly investigated in 2013. Here, we examine tracer observations obtained along four stations (re-)visited during the TAlPro2022 expedition in May 2022. Distributions of both 129I and 236U were related to water masses and clearly linked to local circulation patterns: a tracer-poor surface Atlantic inflow, a thining of the tracer minimum at intermediate depths, and a higher tracer signal in Western Mediterranean Deep Waters due to dense water formation in the Algero-Provençal basin. The comparison to 2013 tracer data indicated recent deep ventilation of the Tyrrhenian Sea, the mixing of deep waters and enhanced stratification in intermediate waters in the Algero-Provençal basin due to a temperature and salinity increase between 2013 and 2022. We estimate an overall 129I increase of 20% at all depths between 0 and 500m with respect to 2013, which is not accompanied by 236U. This suggests either the lateral transport of 129I from the Eastern Mediterranean Sea, or an additional source of this tracer. The inventories of 129I calculated for each water mass at the four stations point to the deposition of airborne releases from the nuclear reprocessing plants (La Hague and Sellafield) on the surface Mediterranean waters as the more likely explanation for the 129I increase. This work demonstrates the great potential of including measurements of anthropogenic radionuclides as tracers of ocean circulation. However, a refinement of the anthropogenic inputs is necessary to improve their use in understanding ventilation changes in the Mediterranean Sea. Full article
(This article belongs to the Special Issue Environmental Radioactivity and Its Applications in Marine Areas)
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Figure 1

Figure 1
<p>Map of the Mediterranean Sea with locations of nuclear reprocessing plants (black dots), and arrows of surface (red) and deep (blue) circulation pathways. Locations of deep (dark blue circles) and intermediate water (light blue circles) formation are also shown here. SF = Sellafield; LH = La Hague; MC = Marcoule.</p>
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<p>Map of the Mediterranean Sea with locations of the stations sampled for <sup>129</sup>I and <sup>236</sup>U in 2013 as part of the GA04S-MedSeA2013 expedition (white circles); and in 2022 during the TAlPro2022 cruise (black circles). The four stations discussed in this work were sampled during both expeditions and are marked as red stars (with name of stations reported; DYF = DYFAMED).</p>
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<p>Vertical profiles of <sup>129</sup>I (<b>a</b>) and <sup>236</sup>U (<b>b</b>) concentrations in 2022 along the four repeated stations. Vertical lines represent values of global fallout of each tracer.</p>
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<p><math display="inline"><semantics> <mi>θ</mi> </semantics></math>-S Diagram for the four stations of the study. Lines represent isopycnals, colours show concentrations of <sup>129</sup>I (<b>a</b>) and <sup>236</sup>U (<b>b</b>). Circles identify data within different water masses (AW = (Mediterranean) Atlantic Water; LIW Levantine Intermediate Water; WIW = Western Intermediate Water; WMDW = Western Mediterranean Deep Water). Samples in the top left side of the panel, not included in any circle, represent surface waters of Atlantic origin.</p>
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<p>Depth profiles of <sup>236</sup>U (orange) and <sup>129</sup>I (purple) concentrations along four stations (panel <b>a</b>–<b>d</b>) in the Western Mediterranean Sea in 2013 and 2022 (and 2001 for DYFAMED). Note that dashed lines represent profiles shape when analytical outliers were removed.</p>
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<p>Column inventories of <sup>129</sup>I and <sup>236</sup>U along the four stations (panel <b>a</b>–<b>d</b>) in the WMED. The different colors of the stacked bar chart represent inventories in different water masses in the WMED for years 2013 and 2022 (when data available), and for 2001 for <sup>236</sup>U in DYFAMED. For the purpose of the figure, we used the following definitions: surface = 0–25 m; AW = 25–100 m; LIW = 100–500 m; deep water = 500 m-bottom. Note that, in 2013, <sup>236</sup>U at station 14 was only available below 1000 m so for comparison we reported inventories below this depth for 2022 as well (brown columns). The inventories uncertainty are 5% for <sup>129</sup>I and 3% for <sup>236</sup>U.</p>
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<p>Comparison of Salinity (red), Temperature (blue) and Dissolved Oxygen (black) data from 2013 and 2022 along four stations in the Western Mediterranean Sea.</p>
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