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raypaths
Improving parsimonious refraction interferometry through U-Net-based correction of first-arrival traveltimes
Preliminary Implications of Viscoelastic Ray Theory for Anelastic Seismic Tomography Models
Numerical simulation and interpretation of sonic arrival times in high-angle wells using the eikonal equation
Correct Off‐Site Determination of Seismic Sensor Orientation from Combined Analyses of Earthquake and Microseism Records
Generalized internal multiple prediction for low relief structures
Variability of response spectra of single-path ground-motion record pairs
Simultaneous waveform inversion of seismic-while-drilling data for P-wave velocity, density, and source parameters
Converted PS-wave imaging based on offset vector tiles
Evaluation of Station Timing Errors from Demeaned Arrival Time Delays
Low-rank-based residual statics estimation and correction
Common-transmission gather for direct seismic attenuation indication
A phase transition in the O’Doherty-Anstey model
Evaluation of the P-wave seismogram approach to estimate V S 30 in California
Average Q P and Q S estimation in marine sediments using a dense receiver array
Rapid Near‐Field Attenuation of Ground Motion from Shallow Induced Earthquakes, Case Study: Preston New Road, United Kingdom
A ray perturbation method for the acoustic attenuating transversely isotropic eikonal equation
Seismic Tomographic Modeling of the Crust and Upper Mantle beneath Israel and the Middle East: Improved Resolution through Optimized Model Parameterization
Teleseismic tomography: Equation one is wrong
ABSTRACT Seismic tomography methods that use waves originating outside the volume being studied are subject to bias caused by unknown structure outside this volume. The bias is of the same mathematical order and similar magnitude as the local-structure effects being studied; failure to account for it can significantly corrupt derived structural models. This bias can be eliminated by adding to the inverse problem three unknown parameters specifying the direction and time for each incident wave, a procedure analogous to solving for event locations in local-earthquake and whole-mantle tomography. The forward problem is particularly simple: The first-order change in the arrival time at an observation point resulting from a perturbation to the incident-wave direction and time equals the change in the time of the perturbed incident wave at the point where the unperturbed ray entered the study volume. This consequence of Fermat’s principle apparently has not previously been recognized. Published teleseismic tomography models probably contain significant artifacts and need to be recomputed using the more complete theory.