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  • 1
    Online Resource
    Online Resource
    Berlin, Heidelberg :Springer Berlin / Heidelberg,
    Keywords: Plasma (Ionized gases). ; Electronic books.
    Description / Table of Contents: Complex plasmas differ from traditional plasmas in many ways: there are low-temperature high pressure systems containing nanometer to micrometer size particles which may be highly charged and strongly interacting. The particles may be chamically reacting or be in contact with solid surfaces, and the electrons may show quantum behaviour. These interesting properties have led to many applications of complex plasmas in technology, medicine and science.Yet complex plasmas are extremely complicated, both experimentally and theoretically, and require a variety of new approaches which go beyond standard plasma physics courses. This book fills this gap presenting an introduction to theory, experiment and computer simulation in this field. Based on tutorial lectures at a very successful recent Summer Institute, the presentation is ideally suited for graduate students, plasma physicists and experienced undergraduates.
    Type of Medium: Online Resource
    Pages: 1 online resource (450 pages)
    Edition: 1st ed.
    ISBN: 9783642105920
    Series Statement: Springer Series on Atomic, Optical, and Plasma Physics Series ; v.59
    DDC: 530.44
    Language: English
    Note: Intro -- Introduction to Complex Plasmas -- Preface -- Contents -- Contributors -- Part I Introduction -- Chapter 1 Complex Plasmas -- 1.1 Plasmas in Nature and in the Laboratory -- 1.2 Complex Plasmas -- 1.3 Low-Temperature Plasmas and Technological Applications -- 1.4 Outline of this book -- References -- Part II Classical and Quantum Plasmas -- Chapter 2 Principles of Transport in Multicomponent Plasmas -- 2.1 Introduction -- 2.1.1 Production and Destruction Mechanisms of Negative Ions -- 2.1.2 The Drift-Diffusion Approximationfor the Description of Plasma Transport -- 2.2 Ambipolar Diffusion -- 2.3 Temporal Dynamics of Negative Ion Flows in Multicomponent Plasmas -- 2.4 Afterglow in Multicomponent Plasmas and Consequent Wall Fluxes of Negative Ions -- 2.5 Steady-State Profiles of Plasmas with Negative Ions -- 2.6 The Sheath in Strongly Electronegative Gases -- 2.7 The Connection Between Plasmas with Negative Ions, Dusty Plasmas, and Ball Lightning -- References -- Chapter 3 Introduction to Quantum Plasmas -- 3.1 Introduction -- 3.2 Relevant Parameters of Quantum Plasmas -- 3.3 Different States of Quantum Plasmas -- 3.4 Occurrences of Quantum Plasmas -- 3.4.1 Astrophysical Plasmas -- 3.4.2 Dense Laboratory Plasmas -- 3.4.3 Laser Plasmas -- 3.4.4 Plasmas in Condensed Matter Systems -- 3.4.5 Highly Compressed Two-Component Plasmas: Mott Effect -- 3.4.6 Ultra-Dense Plasmas in Nuclear Matter: Quark-Gluon Plasma and the Big Bang -- 3.5 Theoretical Description of Quantum Plasmas -- 3.5.1 Basic Equations -- 3.5.2 Thermodynamics of Partially Ionized Plasmas -- 3.5.2.1 Weakly Coupled Quantum Plasmas -- 3.5.2.2 Chemically Reacting Quantum Plasma -- 3.5.3 Spin Effects in Quantum Plasmas -- 3.5.4 Bose Plasmas -- 3.5.5 Plasmas of Particles Having Fermi Statistics -- 3.5.6 Quantum Kinetic Theory. , 3.5.7 More Advanced Approach: The Method of Second Quantization -- 3.5.8 Other Approaches to Quantum Plasmas -- 3.5.8.1 Bohmian Quantum Mechanics -- 3.5.8.2 Quantum Hydrodynamics -- 3.6 Conclusions -- References -- Chapter 4 Introduction to Quantum Plasma Simulations -- 4.1 Introduction -- 4.2 Time-Dependent Schrödinger Equation -- 4.2.1 1D Crank-Nicolson Method -- 4.2.1.1 Boundary Conditions -- 4.2.1.2 Absorbing Boundary Conditions -- 4.2.1.3 Initial Conditions -- 4.2.2 TDSE Solution in Basis Representation -- 4.2.2.1 Deriving a Time Evolution Scheme -- 4.2.2.2 Computation of Matrix Elements of Uij -- 4.2.3 Computational Example: Electron Scattering in a Laser Field -- 4.3 Hartree-Fock Method -- 4.3.1 Standard Approach -- 4.3.2 NEGF Approach -- 4.3.3 Example -- 4.4 Quantum Monte Carlo Methods -- 4.4.1 Metropolis Monte Carlo Method -- 4.4.2 Path-Integral Monte Carlo -- 4.5 Summary -- References -- Chapter 5 Quantum Effects in Plasma Dielectric Response: Plasmons and Shielding in Normal Systems and Graphene -- 5.1 Introduction -- 5.1.1 Background -- 5.1.2 Quantum Theory of Dielectric Response -- 5.2 Quantum Effects in Normal Solid-State Plasmas -- 5.2.1 Three-Dimensional Quantum Plasma -- 5.2.2 Dielectric Properties of Low-Dimensional Systems -- 5.2.3 Dielectric Function of a Magnetized Quantum Plasma -- 5.3 Graphene -- 5.3.1 Introduction -- 5.3.2 Graphene Hamiltonian, Green's Function,and RPA Dielectric Function -- 5.3.3 Some Physical Features of Graphene -- 5.4 Summary -- References -- Part III Strongly Coupled and Dusty Plasmas -- Chapter 6 Imaging Diagnostics in Dusty Plasmas -- 6.1 Introduction -- 6.2 Imaging 2D Systems -- 6.2.1 Imaging Particles -- 6.2.2 Image Analysis -- 6.2.2.1 Threshold Method -- 6.2.2.2 Moment Method -- 6.2.2.3 Moment Method with Gaussian Bandpass Filter -- 6.2.2.4 Least Quadratic Kernel Method -- 6.3 Imaging 3D Systems. , 6.3.1 Scanning Video Microscopy -- 6.3.2 Color Gradient Method -- 6.3.3 Stereoscopy -- 6.3.4 Digital Holography -- 6.4 Summary and Outlook -- References -- Chapter 7 Structure and Dynamics of Finite Dust Clusters -- 7.1 Introduction -- 7.2 Trapping of Dust Clouds -- 7.3 Formation of Finite Dust Clusters -- 7.4 Structural Transitions in 1D Dust Clusters -- 7.5 Structure of 2D Dust Clusters -- 7.6 Normal Mode Dynamics of Dust Clusters -- 7.7 Formation of 3D Dust Clusters -- 7.8 Structure of 3D Dust Clusters -- 7.9 Metastable Configurations of Yukawa Balls -- 7.10 Shell Transitions in Yukawa Balls -- 7.11 Dynamical Properties of Yukawa Balls -- 7.12 Summary -- References -- Chapter 8 Statistical Theory of Spherically Confined Dust Crystals -- 8.1 Introduction -- 8.2 Variational Problem of the Energy Functional -- 8.3 Ground-State Density Profile Within Mean-Field Approximation -- 8.3.1 The Coulomb Limit and Electrostatics -- 8.3.2 General Solution -- 8.3.3 Density Profile for Harmonic Confinement -- 8.3.4 Force Equilibrium Within Yukawa Electrostatics -- 8.4 Simulation Results of Spatially Confined Dust Crystals -- 8.4.1 Ground-State Simulations -- 8.4.2 Comparison of Simulation and Mean-Field Results -- 8.5 Inclusion of Correlations by Using the Local Density Approximation -- 8.5.1 LDA Without Correlations -- 8.5.2 LDA with Correlations -- 8.5.3 Comparison of Simulation and LDA Results -- 8.6 Shell Models of Spherical Dust Crystals -- 8.7 Summary and Discussion -- References -- Chapter 9 PIC-MCC Simulations of Capacitive High-Frequency Discharge Dynamics with Nanoparticles -- 9.1 Introduction -- 9.2 Combined PIC-MCC Approach for Fast Simulation of a Radio-Frequency Discharge at Low Gas Pressure -- 9.2.1 Combined PIC-MCC Approach -- 9.2.2 Description of the Algorithm -- 9.2.3 How Many Simulation Particles We Need?. , 9.2.4 Simulation Results of a CCRF-Discharge in Helium and Argon -- 9.3 Physical Model of Discharge Plasma with Movable Dust -- 9.3.1 Algorithm of Calculation -- 9.3.2 Ion Drag Force -- 9.3.3 Transition Between Different Modes -- 9.3.4 Dust Motion Effect -- 9.4 Conclusion -- References -- Chapter 10 Molecular Dynamics Simulation of Strongly Correlated Dusty Plasmas -- 10.1 Introduction -- 10.2 Basics of Molecular Dynamics Simulation -- 10.2.1 Simulation Model of Strongly Coupled Dusty Plasmas -- 10.2.2 Equations of Motion of a One-Component Plasma -- 10.2.3 Velocity Verlet Integration Scheme -- 10.2.4 Runge-Kutta Integration Scheme -- 10.3 Equilibrium Simulations: Thermodynamic Ensembles -- 10.3.1 Velocity Scaling -- 10.3.2 Stochastic Thermostats -- 10.3.3 Nosé-Hoover Thermostat -- 10.3.4 Langevin Dynamics Simulation -- 10.3.5 Dimensionless System of Units -- 10.4 Simulation of Macroscopic Systems -- 10.4.1 Potential Truncation -- 10.4.2 Electrostatic Interactions -- 10.4.3 Finding of Neighboring Particles -- 10.4.4 Periodic Boundary Conditions -- 10.5 Input and Output Quantities -- 10.5.1 Pair Distribution Function and Static StructureFactor -- 10.5.2 Transport Properties -- 10.6 Applications I: Mesoscopic Systems in Traps -- 10.6.1 Simulated Annealing -- 10.6.2 Effect of Screening -- 10.6.3 Effect of Friction -- 10.7 Applications II: Macroscopic Systems -- 10.7.1 Simulation Results -- 10.8 Conclusion -- References -- Part IV Reactive Plasmas, Plasma-Surface Interaction, and Technological Applications -- Chapter 11 Nonthermal Reactive Plasmas -- 11.1 Introduction -- 11.2 Nonthermal Plasma Conditions -- 11.3 Plasma Kinetics and Plasma Chemical Reactions -- 11.3.1 Boltzmann Equation -- 11.3.2 Reaction Rate Coefficient -- 11.4 Plasma-Surface Interaction -- 11.4.1 Plasma Sheath -- 11.4.2 Surface on Floating Potential. , 11.4.3 High-Voltage Plasma Sheath, Radio-Frequency Plasma Sheath -- 11.5 Low-Pressure Oxygen rf-Plasma -- 11.5.1 Plasma Characterization -- 11.5.1.1 Electric Probe Measurement, Positive Ion Density -- 11.5.1.2 Microwave Interferometry, Electron Density -- 11.5.1.3 Ion Analysis at Discharge Electrodes (Positive and Negative Oxygen Ions) -- 11.5.1.4 Optical Emission Spectroscopy, rf-Phase-Resolved Optical Spectroscopy -- 11.5.1.5 Atomic Oxygen Ground-State Density -- 11.5.2 Interaction of Oxygen Plasma with Polymers -- 11.5.2.1 Fourier Transform Infrared Spectroscopy of Thin Polymer Films -- 11.5.2.2 Spectroscopic Ellipsometry of Thin Plasma-Treated Polymer Films -- 11.5.2.3 Mass Spectrometric Investigation of Reaction Products in Plasma/Gas Phase -- References -- Chapter 12 Formation and Deposition of Nanosize Particles on Surfaces -- 12.1 Introduction -- 12.2 Magnetron Discharge -- 12.3 Nucleation Processes in a Magnetron Plasma -- 12.4 Nanosize Cluster Deposition -- 12.5 Melting Temperature and Lattice Parameters of Ag Clusters -- 12.6 Rapid-Thermal Annealing (RTA) of Deposited Cluster Films -- 12.7 Evaporation of Clusters -- 12.8 Conclusions -- References -- Chapter 13 Kinetic and Diagnostic Studies of Molecular Plasmas Using Laser Absorption Techniques -- 13.1 Introduction -- 13.2 Plasma Chemistry and Reaction Kinetics -- 13.2.1 Studies of Ar/H2/N2/O2 Microwave Plasmas -- 13.2.2 On the Importance of Surface Associationto the Formation of Molecules in a Recombining N2/O2 Plasma -- 13.3 Kinetic Studies and Molecular Spectroscopy of Radicals -- 13.3.1 Line Strengths and Transition Dipole Moment of CH3 -- 13.3.1.1 The 2 Fundamental Band -- 13.3.1.2 The 2 First Hot Band -- 13.3.2 Molecular Spectroscopy of the CN Radical -- 13.4 Quantum Cascade Laser Absorption Spectroscopy for Plasma Diagnostics and Control -- 13.4.1 General Considerations. , 13.4.2 Time-Resolved Study of a Pulsed DC Discharge: NO and Gas Temperature Kinetics.
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  • 2
    Publication Date: 2024-04-25
    Description: 〈title xmlns:mml="http://www.w3.org/1998/Math/MathML"〉Abstract〈/title〉〈p xmlns:mml="http://www.w3.org/1998/Math/MathML" xml:lang="en"〉Dansgaard‐Oeschger (D‐O) climate variability during the last glaciation was first evidenced in ice cores and marine sediments, and is also recorded in various terrestrial paleoclimate archives in Europe. The relative synchronicity across Greenland, the North Atlantic and Europe implies a tight and fast coupling between those regions, most probably effectuated by an atmospheric transmission mechanism. In this study, we investigated the atmospheric changes during Greenland interstadial (GI) and stadial (GS) phases based on regional climate model simulations using two specific periods, GI‐10 and GS‐9 both around 40 ka, as boundary conditions. Our simulations accurately capture the changes in temperature and precipitation as reconstructed by the available proxy data. Moreover, the simulations depict an intensified and southward shifted eddy‐driven jet during the stadial period. Ultimately, this affects the near‐surface circulation toward more southwesterly and cyclonic flow in western Europe during the stadial period, explaining much of the seasonal climate variability recorded by the proxy data, including oxygen isotopes, at the considered proxy sites.〈/p〉
    Description: Plain Language Summary: The climate during the last ice age varied between colder and warmer periods on timescales ranging from hundreds to thousands of years. This variability was first detected in Greenland ice cores and marine sediment cores of the North Atlantic, as well as in continental geological records in Europe. The variation between the colder and warmer periods occur mostly simultaneously in Greenland and in Europe, which is why the atmosphere is assumed to have an important role in transferring the climate signals. We simulated two different periods of the last ice age, one colder and one warmer around 40,000 years ago, using a regional climate model. The aim was to study how the climate and atmospheric circulation changed during these two periods. We find the eddy‐driven jet over the North Atlantic intensified and shifted southward during the colder period. The jet influences the near‐surface atmospheric circulation and leads to more southwesterly and cyclonic flow in western Europe. Oxygen isotope variations observed in western European paleoclimate records may be partly explained by different, more southern moisture sources on top of changes in seasonal temperatures.〈/p〉
    Description: Key Points: 〈list list-type="bullet"〉 〈list-item〉 〈p xml:lang="en"〉Simulated temperatures agree with proxy data; precipitation is biased but GI‐10 versus GS‐9 differences are well captured〈/p〉〈/list-item〉 〈list-item〉 〈p xml:lang="en"〉The stadial winter jet stream is intensified and shifted southward, consistent with dominant southwesterly/cyclonic flow in western Europe〈/p〉〈/list-item〉 〈list-item〉 〈p xml:lang="en"〉Oxygen isotope signal changes at western European proxy sites may be explained not only by temperature but also by varying moisture sources〈/p〉〈/list-item〉 〈/list〉 〈/p〉
    Description: NRDIO
    Description: AXA Research Fund http://dx.doi.org/10.13039/501100001961
    Description: https://doi.org/10.5065/1dfh-6p97
    Keywords: ddc:551.6 ; Dansgaard‐Oeschger cycle ; regional atmospheric dynamics ; regional climate modeling ; continental paleoclimate proxy ; Europe
    Language: English
    Type: doc-type:article
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  • 3
    Publication Date: 2022-03-29
    Description: We investigate the glacial climate conditions in the southeastern Carpathian Basin (Vojvodina, Serbia) based on the reconstruction of malacological palaeotemperatures and results from a high‐resolution regional climate simulation. Land snail assemblages from eight loess profiles are used to reconstruct July temperatures during the Last Glacial Maximum (LGM). The malacological reconstructed temperatures are in good agreement with the simulated LGM July temperatures by the Weather Research and Forecast model. Both methods indicate increasing temperatures from the northwestern towards the southeastern parts of the study area. LGM aridity indices calculated based on the regional climate model data suggest more arid conditions in the southeastern parts compared with more humid conditions in the northwestern parts. However, for present‐day conditions, the moisture gradient is reversed, exhibiting more humid (arid) conditions in the southeast (northwest). An explanation for the reversed LGM aridity pattern is provided by an analysis of the prevailing wind directions over the South Banat district (Serbia). The prevailing moist northwesterly winds during summer are not able to compensate for the annual lack of moisture induced by the dry winds from the southeast that are more frequent during the LGM for the other seasons.
    Description: Helmholtz Association http://dx.doi.org/10.13039/501100009318
    Description: Past Global Changes http://dx.doi.org/10.13039/100010439
    Keywords: ddc:551.6
    Language: English
    Type: doc-type:article
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  • 4
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    COPERNICUS GESELLSCHAFT MBH
    In:  EPIC3Climate of the Past, COPERNICUS GESELLSCHAFT MBH, 17(6), pp. 2559-2576, ISSN: 1814-9324
    Publication Date: 2022-02-15
    Description: During the Last Glacial Maximum (LGM), a very cold and dry period around 26.5–19 kyr BP, permafrost was widespread across Europe. In this work, we explore the possible benefit of using regional climate model data to improve the permafrost representation in France, decipher how the atmospheric circulation affects the permafrost boundaries in the models, and test the role of ground thermal contraction cracking in wedge development during the LGM. With these aims, criteria for possible thermal contraction cracking of the ground are applied to climate model data for the first time. Our results show that the permafrost extent and ground cracking regions deviate from proxy evidence when the simulated large-scale circulation in both global and regional climate models favours prevailing westerly winds. A colder and, with regard to proxy data, more realistic version of the LGM climate is achieved given more frequent easterly winds conditions. Given the appropriate forcing, an added value of the regional climate model simulation can be achieved in representing permafrost and ground thermal contraction cracking. Furthermore, the model data provide evidence that thermal contraction cracking occurred in Europe during the LGM in a wide latitudinal band south of the probable permafrost border, in agreement with field data analysis. This enables the reconsideration of the role of sand-wedge casts to identify past permafrost regions.
    Repository Name: EPIC Alfred Wegener Institut
    Type: Article , isiRev
    Format: application/pdf
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  • 5
    Publication Date: 2023-06-07
    Repository Name: EPIC Alfred Wegener Institut
    Type: Article , peerRev
    Format: application/pdf
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  • 6
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    Unknown
    Wiley
    In:  Annals of the New York Academy of Sciences, 1436 (1). pp. 54-69.
    Publication Date: 2020-01-02
    Description: Regional climate modeling bridges the gap between the coarse resolution of current global climate models and the regional-to-local scales, where the impacts of climate change are of primary interest. Here, we present a review of the added value of the regional climate modeling approach within the scope of paleoclimate research and discuss the current major challenges and perspectives. Two time periods serve as an example: the Holocene, including the Last Millennium, and the Last Glacial Maximum. Reviewing the existing literature reveals the benefits of regional paleo climate modeling, particularly over areas with complex terrain. However, this depends largely on the variable of interest, as the added value of regional modeling arises from a more realistic representation of physical processes and climate feedbacks compared to global climate models, and this affects different climate variables in various ways. In particular, hydrological processes have been shown to be better represented in regional models, and they can deliver more realistic meteorological data to drive ice sheet and glacier modeling. Thus, regional climate models provide a clear benefit to answer fundamental paleoclimate research questions and may be key to advance a meaningful joint interpretation of climate model and proxy data.
    Type: Article , PeerReviewed
    Format: text
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  • 7
    Publication Date: 2022-01-31
    Type: Article , PeerReviewed
    Format: text
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  • 8
    Publication Date: 2021-12-15
    Description: Highlights: • Multiproxy record from S Ethiopia extends knowledge about environment and climate of past 116,000 yrs during human expansion. • Hydroclimate during Marine Isotope Stage (MIS) 5 was much more variable (frequency and amplitude) than during MIS 3 and 4. • Earth system models and model simulations of intermediate complexity emulate corresponding amplitude shifts in hydroclimate. • Environment was arid during MIS 3 and 4, but permanent lake water bodies existed as inferred from our biological proxies. Abstract: Archaeological findings, numerical human dispersal models and genome analyses suggest several time windows in the past 200 kyr (thousands of years ago) when anatomically modern humans (AMH) dispersed out of Africa into the Levant and/or Arabia. From close to the key hominin site of Omo-Kibish, we provide near continuous proxy evidence for environmental changes in lake sediment cores from the Chew Bahir basin, south Ethiopia. The data show highly variable hydroclimate conditions from 116 to 66 kyr BP with rapid shifts from very wet to extreme aridity. The wet phases coincide with the timing of the North African Humid Periods during MIS5, as defined by Nile discharge records from the eastern Mediterranean. The subsequent record at Chew Bahir suggests stable regional hydrological setting between 58 and 32 kyr (MIS4 and 3), which facilitated the development of more habitable ecosystems, albeit in generally dry climatic conditions. This shift, from more to less variable hydroclimate, may help account for the timing of later dispersal events of AMH out of Africa.
    Type: Article , PeerReviewed
    Format: text
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  • 9
    Publication Date: 2024-02-14
    Description: Geomorphic and sedimentologic data indicate that the climate of today's hyper-arid Atacama Desert (northern Chile) was more humid during the mid-Pliocene to Late Pliocene. The processes, however, leading to increased rainfall in this period are largely unknown. To uncover these processes we use both global and regional kilometre-scale model experiments for the mid-Pliocene (3.2 Ma). We found that the PMIP4–CMIP6 (Paleoclimate Modelling Intercomparison Project–Coupled Model Intercomparison Project) model CESM2 (Community Earth System Model 2) and the regional model WRF (Weather Research and Forecasting) used in our study simulate more rainfall in the Atacama Desert for the mid-Pliocene in accordance with proxy data, mainly due to stronger extreme rainfall events in winter. Case studies reveal that these extreme winter rainfall events during the mid-Pliocene are associated with strong moisture conveyor belts (MCBs) originating in the tropical eastern Pacific. For present-day conditions, in contrast, our simulations suggest that the moisture fluxes rather arise from the subtropical Pacific region and are much weaker. A clustering approach reveals systematic differences between the moisture fluxes in the present-day and mid-Pliocene climates, both in strength and origins. The two mid-Pliocene clusters representing tropical MCBs and occurring less than 1 d annually on average produce more rainfall in the hyper-arid core of the Atacama Desert south of 20∘ S than what is simulated for the entire present-day period. We thus conclude that MCBs are mainly responsible for enhanced rainfall during the mid-Pliocene. There is also a strong sea-surface temperature (SST) increase in the tropical eastern Pacific and along the Atacama coast for the mid-Pliocene. It suggests that a warmer ocean in combination with stronger mid-tropospheric troughs is beneficial for the development of MCBs leading to more extreme rainfall in a +3 ∘C warmer world like in the mid-Pliocene.
    Type: Article , PeerReviewed , info:eu-repo/semantics/article
    Format: text
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  • 10
    Publication Date: 2013-09-19
    Description: Langmuir DOI: 10.1021/la4027738
    Print ISSN: 0743-7463
    Electronic ISSN: 1520-5827
    Topics: Chemistry and Pharmacology
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