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11 pages, 2069 KiB  
Article
Inverse Design of Reflectionless Thin-Film Multilayers with Optical Absorption Utilizing Tandem Neural Network
by Su Kalayar Swe and Heeso Noh
Photonics 2024, 11(10), 964; https://doi.org/10.3390/photonics11100964 - 14 Oct 2024
Viewed by 1152
Abstract
The traditional approach to optical design faces limitations as photonic devices grow increasingly complex, requiring advanced functionalities. Recently, machine learning algorithms have gained significant interest for extracting structural designs from customized wavelength spectra, surpassing traditional simulation methods known for their time-consuming nature and [...] Read more.
The traditional approach to optical design faces limitations as photonic devices grow increasingly complex, requiring advanced functionalities. Recently, machine learning algorithms have gained significant interest for extracting structural designs from customized wavelength spectra, surpassing traditional simulation methods known for their time-consuming nature and resource-demanding computational requirements. This study focuses on the inverse design of a reflectionless multilayer thin-film structure across a specific wavelength region, utilizing a tandem neural network (TNN) approach. The method effectively addresses the non-uniqueness problem in training inverse neural networks. Data generation via the transfer matrix method (TMM) involves simulating the optical behavior of a multilayer structure comprising alternating thin films of silicon dioxide (SiO2) and silicon (Si). This innovative design considers both reflection and absorption properties to achieve near-zero reflection. We aimed to manipulate the structure’s reflectivity by implementing low-index and high-index layers along with Si absorption layers to attain specific optical properties. Our TNN demonstrated an MSE accuracy of less than 0.0005 and a maximum loss of 0.00781 for predicting the desired spectrum range, offering advanced capabilities for forecasting arbitrary spectra. This approach provides insights into designing multilayer thin-film structures with near-zero reflection and highlights the potential for controlling absorption materials to enhance optical performance. Full article
(This article belongs to the Section Optoelectronics and Optical Materials)
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<p>Structural design of a multilayer thin-film reflector. (<b>a</b>) Schematic of a five-layer thin-film arrangement alternating between SiO<sub>2</sub> and Si materials, characterized by reflective indices of 1.46 and 3.95 + 0.027i, respectively, within the wavelength range of 600–650 nm. (<b>b</b>) Structural representation of TMM simulation with n<sub>2</sub> as a complex number, and d<sub>1</sub>, d<sub>2</sub>, d<sub>3</sub>, d<sub>4</sub>, and d<sub>5</sub> representing the thicknesses of each layer. The surrounding medium is air; hence, its refractive index is denoted as n<sub>0</sub> = 1.</p>
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<p>Architecture of the tandem neural network.</p>
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<p>Training process and result of FNN. (<b>a</b>) Tuning hyperparameters for model training and comparing training loss history. (<b>b</b>) Training and validation performance of Model 2, achieving an MSE loss of 6.8909 × 10<sup>−5</sup>. (<b>c</b>) The response of FNN prediction for the target reflectivity spectrum.</p>
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<p>Training process and result of TNN. (<b>a</b>) Tuning hyperparameters for model training and comparing training loss history. (<b>b</b>) Training and validation performance of Model 2, achieving an MSE loss of 4.9648 × 10<sup>−4</sup>. (<b>c</b>) The reflectivity spectra of the target and those obtained by TNN and TMM are represented with a green line, a red dashed line, and open circles, respectively. (<b>d</b>) Error distribution of TNN on the validation dataset.</p>
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<p>(<b>a</b>) TMM simulation of the full spectrum range of the thickness resulting from the predicted tandem neural network (52, 12, 18, 49, and 94 nm), demonstrating a significant drop in reflectivity to near zero in the wavelength range of 600–650 nm. (<b>b</b>) Modified structure designs in different wavelength regions. (<b>c</b>) Comparison of reflectivity between the randomly generated structure and after optimization using TNN.</p>
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<p>Expanded performance evaluation of FNN across the 400–700 nm wavelength range.</p>
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39 pages, 8597 KiB  
Article
Multilevel Algorithm for Large-Scale Gravity Inversion
by Shujin Cao, Peng Chen, Guangyin Lu, Yajing Mao, Dongxin Zhang, Yihuai Deng and Xinyue Chen
Symmetry 2024, 16(6), 758; https://doi.org/10.3390/sym16060758 - 17 Jun 2024
Viewed by 1460
Abstract
Surface gravity inversion attempts to recover the density contrast distribution in the 3D Earth model for geological interpretation. Since airborne gravity is characterized by large data volumes, large-scale 3D inversion exceeds the capacity of desktop computing resources, making it difficult to achieve the [...] Read more.
Surface gravity inversion attempts to recover the density contrast distribution in the 3D Earth model for geological interpretation. Since airborne gravity is characterized by large data volumes, large-scale 3D inversion exceeds the capacity of desktop computing resources, making it difficult to achieve the appropriate depth/lateral resolution for geological interpretation. In addition, gravity data are finite and noisy, and their inversion is ill posed. Especially in the absence of a priori geological information, regularization must be introduced to overcome the difficulty of the non-uniqueness of the solutions to recover the most geologically plausible ones. Because the use of Haar wavelet operators has an edge-preserving property and can preserve the sensitivity matrix structure at each level of the multilevel method to obtain faster solvers, we present a multilevel algorithm for large-scale gravity inversion solved by the re-weighted regularized conjugate gradient (RRCG) algorithm to reduce the inversion computational resources and improve the depth/lateral resolution of the inversion results. The RRCG-based multilevel inversion was then applied to synthetic cases and airborne gravity data from the Quest-South project in British Columbia, Canada. Results from synthetic models and field data show that the RRCG-based multilevel inversion is suitable for obtaining density contrast distributions with appropriate horizontal and vertical resolution, especially for large-scale gravity inversions compared to Occam’s inversion. Full article
(This article belongs to the Special Issue Asymmetric and Symmetric Study on Algorithms Optimization)
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<p>A 3D interpretation model is discretized into prismatic cells (blue wireframe) with constant density.</p>
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<p>Gravitational attraction at observation point <span class="html-italic">P</span> is due to a prismatic cell <span class="html-italic">Q</span> with a constant density.</p>
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<p>Two surveys. (<b>a</b>) Generalized inversion; (<b>b</b>) equidimensional inversion [<a href="#B76-symmetry-16-00758" class="html-bibr">76</a>].</p>
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<p>Diagrammatic sketch of equivalent geometric framework in vertical view.</p>
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<p>Diagrammatic sketch of extension translational equivalent geometric framework in vertical view.</p>
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<p>The Line–Line survey scheme and the Layer–Layer survey scheme.</p>
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<p>The diagrammatic sketch of sensitivity matrix <math display="inline"><semantics> <msub> <mi>g</mi> <mrow> <mi>x</mi> <mi>x</mi> </mrow> </msub> </semantics></math> of one-layer observation points is due to single-layer prismatic cells. (<b>a</b>) <math display="inline"><semantics> <msub> <mi>G</mi> <mrow> <mi>t</mi> <mo>,</mo> <mi>n</mi> </mrow> </msub> </semantics></math>; (<b>b</b>) <math display="inline"><semantics> <msub> <mover accent="true"> <mi>G</mi> <mo>˜</mo> </mover> <mrow> <mi>q</mi> <mo>,</mo> <mi>m</mi> </mrow> </msub> </semantics></math>.</p>
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<p>Rapid algorithm’s forward results for different components (<b>a</b>) <math display="inline"><semantics> <msub> <mi>g</mi> <mrow> <mi>x</mi> <mi>x</mi> </mrow> </msub> </semantics></math>, (<b>b</b>) <math display="inline"><semantics> <msub> <mi>g</mi> <mi>x</mi> </msub> </semantics></math>, (<b>c</b>) <math display="inline"><semantics> <msub> <mi>g</mi> <mi>z</mi> </msub> </semantics></math>, (<b>d</b>) <math display="inline"><semantics> <msub> <mi>g</mi> <mrow> <mi>x</mi> <mi>y</mi> </mrow> </msub> </semantics></math>, (<b>e</b>) <math display="inline"><semantics> <msub> <mi>g</mi> <mrow> <mi>y</mi> <mi>y</mi> </mrow> </msub> </semantics></math>, (<b>f</b>) <math display="inline"><semantics> <msub> <mi>g</mi> <mi>y</mi> </msub> </semantics></math>, (<b>g</b>) <math display="inline"><semantics> <msub> <mi>g</mi> <mrow> <mi>x</mi> <mi>z</mi> </mrow> </msub> </semantics></math>, (<b>h</b>) <math display="inline"><semantics> <msub> <mi>g</mi> <mrow> <mi>y</mi> <mi>z</mi> </mrow> </msub> </semantics></math>, and (<b>i</b>) <math display="inline"><semantics> <msub> <mi>g</mi> <mrow> <mi>z</mi> <mi>z</mi> </mrow> </msub> </semantics></math>.</p>
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<p>The relative error of forward results between the rapid algorithm and analytical solution [<a href="#B13-symmetry-16-00758" class="html-bibr">13</a>] for different components (<b>a</b>) <math display="inline"><semantics> <msub> <mi>g</mi> <mrow> <mi>x</mi> <mi>x</mi> </mrow> </msub> </semantics></math>, (<b>b</b>) <math display="inline"><semantics> <msub> <mi>g</mi> <mi>x</mi> </msub> </semantics></math>, (<b>c</b>) <math display="inline"><semantics> <msub> <mi>g</mi> <mi>z</mi> </msub> </semantics></math>, (<b>d</b>) <math display="inline"><semantics> <msub> <mi>g</mi> <mrow> <mi>x</mi> <mi>y</mi> </mrow> </msub> </semantics></math>, (<b>e</b>) <math display="inline"><semantics> <msub> <mi>g</mi> <mrow> <mi>y</mi> <mi>y</mi> </mrow> </msub> </semantics></math>, (<b>f</b>) <math display="inline"><semantics> <msub> <mi>g</mi> <mi>y</mi> </msub> </semantics></math>, (<b>g</b>) <math display="inline"><semantics> <msub> <mi>g</mi> <mrow> <mi>x</mi> <mi>z</mi> </mrow> </msub> </semantics></math>, (<b>h</b>) <math display="inline"><semantics> <msub> <mi>g</mi> <mrow> <mi>y</mi> <mi>z</mi> </mrow> </msub> </semantics></math>, and (<b>i</b>) <math display="inline"><semantics> <msub> <mi>g</mi> <mrow> <mi>z</mi> <mi>z</mi> </mrow> </msub> </semantics></math>. E stands for Eotvos, which is standard for characterising how sensitive different gravity gradiometers (1 Eotvos = <math display="inline"><semantics> <msup> <mn>10</mn> <mrow> <mo>−</mo> <mn>9</mn> </mrow> </msup> </semantics></math><math display="inline"><semantics> <msup> <mi>s</mi> <mrow> <mo>−</mo> <mn>2</mn> </mrow> </msup> </semantics></math>).</p>
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<p>Peak memory usage to calculate <math display="inline"><semantics> <msub> <mi>g</mi> <mi>z</mi> </msub> </semantics></math> fields with different-sized models (<math display="inline"><semantics> <mrow> <msub> <mi>N</mi> <mi>m</mi> </msub> <mo>=</mo> <msub> <mi>N</mi> <mi>G</mi> </msub> <mo>/</mo> <msub> <mi>N</mi> <mi>d</mi> </msub> </mrow> </semantics></math>, <math display="inline"><semantics> <mrow> <msub> <mi>n</mi> <mi>x</mi> </msub> <mo>≡</mo> <msub> <mi>n</mi> <mi>y</mi> </msub> <mo>=</mo> <mspace width="3.33333pt"/> </mrow> </semantics></math> sqrt<math display="inline"><semantics> <mrow> <mo>(</mo> <msub> <mi>N</mi> <mi>d</mi> </msub> <mo>)</mo> </mrow> </semantics></math>, and <math display="inline"><semantics> <mrow> <msub> <mi>N</mi> <mi>z</mi> </msub> <mo>=</mo> <msub> <mi>N</mi> <mi>m</mi> </msub> <mo>/</mo> <msub> <mi>N</mi> <mi>d</mi> </msub> </mrow> </semantics></math>).</p>
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<p>Calculation time obtained by performing <math display="inline"><semantics> <msub> <mi>g</mi> <mi>z</mi> </msub> </semantics></math> fields with different sizes of models.</p>
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<p>Gravity data. The first and second columns are noise-contaminated gravity data and residual data of the RRCG inversion, respectively. The columns from top to bottom are <math display="inline"><semantics> <mrow> <mo>Δ</mo> <mi>z</mi> </mrow> </semantics></math> = 0, 100, 200, and 300, respectively.</p>
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<p>The slices of density models. The first and second columns represent forward and inversion models, respectively. The columns from top to bottom are <math display="inline"><semantics> <mrow> <mo>Δ</mo> <mi>z</mi> </mrow> </semantics></math> = 0, 100, 200, and 300, respectively. <math display="inline"><semantics> <msub> <mi>m</mi> <mrow> <mi>m</mi> <mi>i</mi> <mi>n</mi> </mrow> </msub> </semantics></math> = 0 and <math display="inline"><semantics> <msub> <mi>m</mi> <mrow> <mi>m</mi> <mi>a</mi> <mi>x</mi> </mrow> </msub> </semantics></math> = <math display="inline"><semantics> <mrow> <mn>1.0</mn> </mrow> </semantics></math> g/<math display="inline"><semantics> <msup> <mi>cm</mi> <mn>3</mn> </msup> </semantics></math>.</p>
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<p>Inversion density slices obtained using Occam’s inversion.</p>
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<p>Inversion density slices obtained using multilevel inversion.</p>
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<p>Residuals between observed and predicted data obtained by (<b>a</b>) Occam’s inversion, and (<b>b</b>) multilevel inversion.</p>
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<p>Data misfit obtained by Occam’s and multilevel inversion.</p>
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<p>Example of multilevel inversion for noise-corrupted data (8%), (<b>a</b>) noise-corrupted data, (<b>b</b>) reconstructed density model, and (<b>c</b>) residual data.</p>
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<p>Data misfit obtained by multilevel inversion for noise-corrupted gravity data (8%).</p>
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<p>SEG/EAGE salt dome model (<b>a</b>) the forward model; (<b>b</b>) the forward result of <math display="inline"><semantics> <msub> <mi>g</mi> <mi>z</mi> </msub> </semantics></math>.</p>
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<p>Result of inversion of <math display="inline"><semantics> <msub> <mi>g</mi> <mi>z</mi> </msub> </semantics></math> using Occam’s inversion.</p>
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<p>Result of inversion of <math display="inline"><semantics> <msub> <mi>g</mi> <mi>z</mi> </msub> </semantics></math> using multilevel inversion.</p>
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<p>Residuals between observed and predicted data obtained by (<b>a</b>) Occam’s inversion; (<b>b</b>) multilevel inversion.</p>
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<p>Data misfit obtained by Occam’s and multilevel inversion.</p>
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<p>Survey area map. The red line corresponds to the QUEST-South geophysical survey, the light green blocks are Quaternary sedimentary strata, and the other colors are bedrock. Please see Erdmer and Cui [<a href="#B96-symmetry-16-00758" class="html-bibr">96</a>] for details.</p>
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<p>Residual gravity data provided by Sander Geophysics [<a href="#B97-symmetry-16-00758" class="html-bibr">97</a>].</p>
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<p>Inversion density distributions provided by Mira Geoscience Limited at different depths <span class="html-italic">z</span>: (<b>a</b>) 500 m, (<b>b</b>) 1300 m, (<b>c</b>) 2100 m, (<b>d</b>) 2900 m, (<b>e</b>) 3700 m, and (<b>f</b>) 4500 m [<a href="#B98-symmetry-16-00758" class="html-bibr">98</a>].</p>
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<p>Inversion density distributions using Occam’s inversion code at different depths <span class="html-italic">z</span>: (<b>a</b>) 500 m, (<b>b</b>) 1300 m, (<b>c</b>) 2100 m, (<b>d</b>) 2900 m, (<b>e</b>) 3700 m, and (<b>f</b>) 4500 m.</p>
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<p>Inversion density distributions using the multilevel inversion at different depths <span class="html-italic">z</span>: (<b>a</b>) 500 m, (<b>b</b>) 1300 m, (<b>c</b>) 2100 m, (<b>d</b>) 2900 m, (<b>e</b>) 3700 m, and (<b>f</b>) 4500 m.</p>
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<p>Residuals between observed and predicted data obtained by (<b>a</b>) Occam’s inversion; and (<b>b</b>) multilevel inversion.</p>
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<p>Data misfit obtained by Occam’s and multilevel inversion.</p>
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<p>Histogram of the recovered model (<b>a</b>) and the data residual (<b>b</b>) with corresponding mean and standard deviation (std) for Occam’s inversion.</p>
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<p>Histogram of the recovered model (<b>a</b>) and the data residual (<b>b</b>) with corresponding mean and standard deviation (std) for multilevel inversion.</p>
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13 pages, 3664 KiB  
Article
A New Stochastic Process of Prestack Inversion for Rock Property Estimation
by Long Yin, Sheng Zhang, Kun Xiang, Yongqiang Ma, Yongzhen Ji, Ke Chen and Dongyu Zheng
Appl. Sci. 2022, 12(5), 2392; https://doi.org/10.3390/app12052392 - 25 Feb 2022
Viewed by 1424
Abstract
In order to enrich the current prestack stochastic inversion theory, we propose a prestack stochastic inversion method based on adaptive particle swarm optimization combined with Markov chain Monte Carlo (MCMC). The MCMC could provide a stochastic optimization approach, and, with the APSO, have [...] Read more.
In order to enrich the current prestack stochastic inversion theory, we propose a prestack stochastic inversion method based on adaptive particle swarm optimization combined with Markov chain Monte Carlo (MCMC). The MCMC could provide a stochastic optimization approach, and, with the APSO, have a better performance in global optimization methods. This method uses logging data to define a preprocessed model space. It also uses Bayesian statistics and Markov chains with a state transition matrix to update and evolve each generation population in the data domain, then adaptive particle swarm optimization is used to find the global optimal value in the finite model space. The method overcomes the problem of over-fitting deterministic inversion and improves the efficiency of stochastic inversion. Meanwhile, the fusion of multiple sources of information can reduce the non-uniqueness of solutions and improve the inversion accuracy. We derive the APSO algorithm in detail, give the specific workflow of prestack stochastic inversion, and verify the validity of the inversion theory through the inversion test of two-dimensional prestack data in real areas. Full article
(This article belongs to the Special Issue Integration of Methods in Applied Geophysics)
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<p>The workflow chart of APSO.</p>
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<p>The general workflow of stochastic inversion.</p>
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<p>Well placement and Vp/Vs ratio map of working area.</p>
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<p>Single channel multiple particle inversion results.</p>
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<p>The value of the objective function changes with the number of iterations.</p>
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<p>(<b>a</b>) Gas and non-gas porosity histogram, (<b>b</b>) Gas and non-gas P-impedance histogram, (<b>c</b>) Cross-plot of Porosity and impedance of gas and non-gas layer.</p>
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<p>Vp/Vs histogram among gas-layer (red), non-gas layer (green), and target layer (yellow).</p>
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<p>(<b>a</b>) Background model (<b>b</b>) P-impedance of inverted results (<b>c</b>) Poisson’s ratio of inverted results.</p>
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13 pages, 935 KiB  
Article
Energy Optimization of the Continuous-Time Perfect Control Algorithm
by Marek Krok, Paweł Majewski, Wojciech P. Hunek and Tomasz Feliks
Energies 2022, 15(4), 1555; https://doi.org/10.3390/en15041555 - 19 Feb 2022
Cited by 3 | Viewed by 1665
Abstract
In this paper, an attempt at the energy optimization of perfect control systems is performed. The perfect control law is the maximum-speed and maximum-accuracy procedure, which allows us to obtain a reference value on the plant’s output just after a time delay. Based [...] Read more.
In this paper, an attempt at the energy optimization of perfect control systems is performed. The perfect control law is the maximum-speed and maximum-accuracy procedure, which allows us to obtain a reference value on the plant’s output just after a time delay. Based on the continuous-time state-space description, the minimum-error strategy is discussed in the context of possible solutions aiming for the minimization of the control energy. The approach presented within this study is focused on the nonunique matrix inverse-originated so-called degrees of freedom being the core of perfect control scenarios. Thus, in order to obtain the desired energy-saving parameters, a genetic algorithm has been employed during the inverse model control synthesis process. Now, the innovative continuous-time procedure can be applied to a wide range of multivariable plants without any stress caused by technological limitations. Simulation examples made in the MATLAB/Simulink environment have proven the usefulness of the new method shown within the paper. In the extreme case, the energy consumption has been reduced by approximately 80% in comparison with the well-known Moore–Penrose inverse. Full article
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<p>Simulation results, case 1: (<b>left</b>) the Moore–Penrose approach; (<b>right</b>) the new energy-optimal approach; <math display="inline"><semantics> <mrow> <msub> <mi mathvariant="bold">y</mi> <mi>ref</mi> </msub> <mo>=</mo> <mn>0</mn> </mrow> </semantics></math>.</p>
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<p>Simulation results, case 2: (<b>left</b>) Moore–Penrose approach; (<b>right</b>) the new optimal energy approach; <math display="inline"><semantics> <mrow> <msub> <mi mathvariant="bold">y</mi> <mi>ref</mi> </msub> <mo>=</mo> <mn>0</mn> </mrow> </semantics></math>.</p>
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<p>Cartesian robot visualization.</p>
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<p>Simulation results, case 3: (<b>left</b>): Moore–Penrose approach; (<b>right</b>): the new optimal energy approach; <math display="inline"><semantics> <mrow> <msub> <mi mathvariant="bold">y</mi> <mi>ref</mi> </msub> <mo>=</mo> <mn>0</mn> </mrow> </semantics></math>.</p>
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23 pages, 15439 KiB  
Article
High-Resolution Cooperate Density-Integrated Inversion Method of Airborne Gravity and Its Gradient Data
by Guoqing Ma, Tong Gao, Lili Li, Taihan Wang, Runxin Niu and Xinwei Li
Remote Sens. 2021, 13(20), 4157; https://doi.org/10.3390/rs13204157 - 17 Oct 2021
Cited by 3 | Viewed by 2194
Abstract
Airborne (or satellite) gravity measurement is a commonly used remote sensing method to obtain the underground density distribution. Airborne gravity gradiometry data have a higher horizontal resolution to shallower causative sources than airborne gravity anomaly, so joint exploration of airborne gravity and its [...] Read more.
Airborne (or satellite) gravity measurement is a commonly used remote sensing method to obtain the underground density distribution. Airborne gravity gradiometry data have a higher horizontal resolution to shallower causative sources than airborne gravity anomaly, so joint exploration of airborne gravity and its gradient data can simultaneously obtain the anomaly feature of sources with different depths. The most commonly used joint inversion method of gravity and its gradient data is the data combined method, which is to combine all the components into a data matrix as mutual constraints to reduce ambiguity and non-uniqueness. In order to obtain higher resolution results, we proposed a cooperate density-integrated inversion method of airborne gravity and its gradient data, which firstly carried out the joint inversion using cross-gradient constraints to obtain two density structures, and then fused two recovered models into a result through Fourier transform; finally, data combined joint inversion of airborne gravity, and gradient data were reperformed to achieve high-resolution density result using fused density results as a reference model. Compared to the data combined joint inversion method, the proposed cooperate density-integrated inversion method can obtain higher resolution and more accurate density distribution of shallow and deep bodies meanwhile. We also applied it to real data in the mining area of western Liaoning Province, China. The results showed that the depth of the skarn-type iron mine in the region is about 900–1300 m and gives a more specific distribution compared to the geological results, which provided reliable data for the next exploration plan. Full article
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<p>Flowchart of the cooperate density-integrated inversion method.</p>
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<p>Information of models in different depth. (<b>a</b>) Density models with 1000 kg/m<sup>3</sup>. (<b>b</b>) Airborne gravity anomaly at 100 m altitude. (<b>c</b>) Vertical gradient anomaly of airborne gravity data at 100 m altitude.</p>
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<p>Model tests of two prisms in different depths. (<b>a</b>) Density slice (y = 10 km) by Tikhonov regularized method of airborne gravity data. (<b>b</b>) Density slice (y = 10 km) by Tikhonov regularized method of airborne gravity gradient data. (<b>c</b>) Density slice (y = 10 km) by data combined joint inversion method of airborne gravity and its gradient data. (<b>d</b>) 3D density distribution (larger than 350 kg/m<sup>3</sup>) by data combined joint inversion method of airborne gravity and its gradient data. (<b>e</b>) Density slice (y = 10 km) by structure constrained joint inversion method of airborne gravity data. (<b>f</b>) Density slice (y = 10 km) by structure constrained joint inversion method of airborne gravity gradient data. (<b>g</b>) Density slice (y = 10 km) by cooperate density-integrated inversion method. (<b>h</b>) 3D density distribution (larger than 350 kg/m<sup>3</sup>) by the cooperate density-integrated inversion method.</p>
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<p>Model tests of two prisms in different depths. (<b>a</b>) Density slice (y = 10 km) by Tikhonov regularized method of airborne gravity data. (<b>b</b>) Density slice (y = 10 km) by Tikhonov regularized method of airborne gravity gradient data. (<b>c</b>) Density slice (y = 10 km) by data combined joint inversion method of airborne gravity and its gradient data. (<b>d</b>) 3D density distribution (larger than 350 kg/m<sup>3</sup>) by data combined joint inversion method of airborne gravity and its gradient data. (<b>e</b>) Density slice (y = 10 km) by structure constrained joint inversion method of airborne gravity data. (<b>f</b>) Density slice (y = 10 km) by structure constrained joint inversion method of airborne gravity gradient data. (<b>g</b>) Density slice (y = 10 km) by cooperate density-integrated inversion method. (<b>h</b>) 3D density distribution (larger than 350 kg/m<sup>3</sup>) by the cooperate density-integrated inversion method.</p>
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<p>Information of models in different depths with 5% Gaussian noise. (<b>a</b>) Airborne gravity anomaly at 100 m altitude. (<b>b</b>) Vertical gradient anomaly of airborne gravity at 100 m altitude.</p>
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<p>Model tests of two prisms in different depths containing noise. (<b>a</b>) Density slice (y = 10 km) by data combined joint inversion method of airborne gravity and its gradient data. (<b>b</b>) 3D density distribution (larger than 350 kg/m<sup>3</sup>) by data combined joint inversion method of airborne gravity and its gradient data. (<b>c</b>) Density slice (y = 10 km) by the cooperate density-integrated inversion method. (<b>d</b>) 3D density distribution (larger than 350 kg/m<sup>3</sup>) by the cooperate density-integrated inversion method.</p>
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<p>Information of models in the same depth. (<b>a</b>) Density models with 1 kg/m<sup>3</sup>. (<b>b</b>) Airborne gravity anomaly at 100 m altitude. (<b>c</b>) Vertical gradient anomaly of airborne gravity data at 100 m altitude.</p>
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<p>Model tests of two prisms in the same depths. (<b>a</b>) Density slice (y = 10 km) by data combined joint inversion method of airborne gravity and its gradient data. (<b>b</b>) 3D density distribution (larger than 370 kg/m<sup>3</sup>) by data combined joint inversion method of airborne gravity and its gradient data. (<b>c</b>) Density slice (y = 10 km) by the cooperate density-integrated inversion method. (<b>d</b>) 3D density distribution (larger than 370 kg/m<sup>3</sup>) by the cooperate density-integrated inversion method.</p>
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<p>Information of complex models. (<b>a</b>) Density models with 1000 kg/m<sup>3</sup>. (<b>b</b>) Airborne gravity anomaly at 100 m altitude. (<b>c</b>) Vertical gradient anomaly of airborne gravity at 100 m altitude.</p>
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<p>Complex model tests of three prisms. (<b>a</b>) Density slice (x = 10 km) by data combined joint inversion method of airborne gravity and its gradient data. (<b>b</b>) Density slice (x = 10 km) by cooperate density-integrated inversion method. (<b>c</b>) Density slice (y = 10 km) by data combined joint inversion method of airborne gravity and its gradient data. (<b>d</b>) Density slice (y = 10 km) by the cooperate density-integrated inversion method. (<b>e</b>) 3D density distribution (larger than 370 kg/m<sup>3</sup>) by data combined joint inversion method of airborne gravity and its gradient data. (<b>f</b>) 3D density distribution (larger than 370 kg/m<sup>3</sup>) by the cooperate density-integrated inversion method of airborne gravity and its gradient data.</p>
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<p>Complex model tests with different altitudes. (<b>a</b>) Airborne gravity anomaly at 150 m altitude. (<b>b</b>) Vertical gradient anomaly of airborne gravity at 150 m altitude. (<b>c</b>) Density slice (y = 10 km) by cooperate density-integrated inversion method at 150 m altitude. (<b>d</b>) 3D density distribution (larger than 370 kg/m<sup>3</sup>). (<b>e</b>) Airborne gravity anomaly at 200 m altitude. (<b>f</b>) Vertical gradient anomaly of airborne gravity at 200 m altitude. (<b>g</b>) Density slice (y = 10 km) by cooperate density-integrated inversion method at 200 m altitude. (<b>h</b>) 3D density distribution (larger than 370 kg/m<sup>3</sup>).</p>
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<p>Complex model tests using airborne gravity and calculated vertical gradient data. (<b>a</b>) Calculated airborne gravity gradient data. (<b>b</b>) Density slice (y = 10 km) by cooperate density-integrated inversion method. (<b>c</b>) 3D density distribution (larger than 370 kg/m<sup>3</sup>) by cooperate density-integrated inversion method.</p>
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<p>Complex model tests using airborne gravity and calculated vertical gradient data. (<b>a</b>) Calculated airborne gravity gradient data. (<b>b</b>) Density slice (y = 10 km) by cooperate density-integrated inversion method. (<b>c</b>) 3D density distribution (larger than 370 kg/m<sup>3</sup>) by cooperate density-integrated inversion method.</p>
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<p>Real data. (<b>a</b>) Geological map of Liaoning western area. (<b>b</b>) Real airborne gravity anomaly of Liaoning western area. (<b>c</b>) Calculated airborne gravity vertical gradient anomaly of Liaoning western area. (<b>d</b>) Drilling data information.</p>
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<p>Real data. (<b>a</b>) Geological map of Liaoning western area. (<b>b</b>) Real airborne gravity anomaly of Liaoning western area. (<b>c</b>) Calculated airborne gravity vertical gradient anomaly of Liaoning western area. (<b>d</b>) Drilling data information.</p>
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<p>Density inversion result of real data. (<b>a</b>) The vertical slices and the 3D density results with the value larger than 0.2 kg/m<sup>3</sup> computed by data combined joint inversion method. (<b>b</b>) The horizontal slices of 3D density results computed by the data combined joint inversion method. (<b>c</b>) The vertical slices and the 3D density results with a value larger than 0.2 kg/m<sup>3</sup> computed by the proposed cooperative density inversion method. (<b>d</b>) The horizontal slices of 3D density results computed by the proposed cooperative density inversion method.</p>
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<p>Distribution of density inversion results. (<b>a</b>) The modified location of iron mines by data combined joint inversion method. (<b>b</b>) The modified location of iron mines by the proposed cooperative density inversion method.</p>
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10 pages, 436 KiB  
Article
Continuous-Time Perfect Control Algorithm—A State Feedback Approach
by Marek Krok, Wojciech P. Hunek and Paweł Majewski
Appl. Sci. 2021, 11(16), 7466; https://doi.org/10.3390/app11167466 - 14 Aug 2021
Cited by 1 | Viewed by 1583
Abstract
In this paper, a new approach to the continuous-time perfect control algorithm is given. Focusing on the output derivative, it is shown that the discussed control law can effectively be implemented in terms of state-feedback scenarios. Moreover, the application of nonunique matrix inverses [...] Read more.
In this paper, a new approach to the continuous-time perfect control algorithm is given. Focusing on the output derivative, it is shown that the discussed control law can effectively be implemented in terms of state-feedback scenarios. Moreover, the application of nonunique matrix inverses is also taken into consideration during the perfect control design process. Simulation examples given within this work allow us to showcase the main properties obtained for continuous-time perfect control closed-loop plants. Full article
(This article belongs to the Special Issue New Trends in Automation Control Systems and Their Applications)
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Figure 1

Figure 1
<p>Perfect control plots: <span class="html-italic">T</span>-inverse, case <math display="inline"><semantics> <mrow> <mo>Δ</mo> <mi>t</mi> <mo>=</mo> <mn>0.1</mn> </mrow> </semantics></math> s.</p>
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<p>Perfect control plots: <span class="html-italic">T</span>-inverse, case <math display="inline"><semantics> <mrow> <mo>Δ</mo> <mi>t</mi> <mo>=</mo> <mn>0.2</mn> </mrow> </semantics></math> s.</p>
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<p>Perfect control plots: <math display="inline"><semantics> <mi>σ</mi> </semantics></math>-inverse, case <math display="inline"><semantics> <mrow> <mo>Δ</mo> <mi>t</mi> <mo>=</mo> <mn>0.2</mn> </mrow> </semantics></math> s.</p>
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13 pages, 347 KiB  
Article
Switching Perfect Control Algorithm
by Marek Krok, Wojciech P. Hunek and Tomasz Feliks
Symmetry 2020, 12(5), 816; https://doi.org/10.3390/sym12050816 - 15 May 2020
Cited by 6 | Viewed by 2151
Abstract
The application of the switching control framework to the perfect control algorithm is presented in this paper. Employing the nonunique matrix inverses, the different closed-loop properties are obtained and further enhanced with possible switching methodology implementation. Simulation examples performed in the MATLAB/Simulink environment [...] Read more.
The application of the switching control framework to the perfect control algorithm is presented in this paper. Employing the nonunique matrix inverses, the different closed-loop properties are obtained and further enhanced with possible switching methodology implementation. Simulation examples performed in the MATLAB/Simulink environment clearly show that the new framework can lead to benefits in terms of the control energy, speed, and robustness of the perfect control law. The possibility of transferring the new obtained results to the symmetrical nonlinear plants seems to be immediate. Full article
(This article belongs to the Special Issue Symmetry in Dynamic Systems)
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Graphical abstract

Graphical abstract
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<p>Runs of perfect control, case: T-inverse.</p>
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<p>Runs of perfect control, case: switching inverses, <math display="inline"><semantics> <mrow> <mi>T</mi> <mo>→</mo> <mi>σ</mi> </mrow> </semantics></math>.</p>
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<p>Runs of perfect control, case: switching inverses, <math display="inline"><semantics> <mrow> <mi>σ</mi> <mo>→</mo> <mi>T</mi> </mrow> </semantics></math>.</p>
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<p>Runs of perfect control, case: switching inverses, <math display="inline"><semantics> <mrow> <mi>σ</mi> <mo>→</mo> <mi>T</mi> </mrow> </semantics></math>.</p>
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<p>Runs of perfect control, case: switching inverses, <math display="inline"><semantics> <mrow> <mi>σ</mi> <mo>→</mo> <mi>T</mi> </mrow> </semantics></math>.</p>
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<p>Scheme of the MATLAB/Simulink control implementation.</p>
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<p>Scheme of the MATLAB/Simulink switching mechanism implementation.</p>
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