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power law
Variability in the Natural Frequencies of a Nine‐Story Concrete Building from Seconds to Decades
Crustal Strain Rates in the Western United States and Their Relationship with Earthquake Rates
Specific surface area: A reliable predictor of creep and stress relaxation in gas shales
Assessment of the Initial, Promising, and Predicted Geologic and Recoverable Oil Resources of the West Siberian Petroleum Province and Their Structure
Low-rank representation of omnidirectional subsurface extended image volumes
Channel Profile Response to Abrupt Increases in Mountain Uplift Rates: Implications for Late Miocene to Pliocene Acceleration of Intracontinental Extension in the Northern Qinling Range-Weihe Graben, Central China
Basement reservoir plumbing: fracture aperture, length and topology analysis of the Lewisian Complex, NW Scotland
Fault zone architecture and its scaling laws: where does the damage zone start and stop?
Abstract Damage zones of different fault types are investigated in siliciclastics (Utah, USA), carbonates (Majella Mountain, Italy) and metamorphic rocks (western Norway). The study was conducted taking measurements of deformation features such as fractures and deformation bands on multiple 1D scanlines along fault walls. The resulting datasets are used to plot the frequency distribution of deformation features and to constrain the geometrical width of the damage zone for the studied faults. The damage-zone width of a single fault is constrained by identifying the changes in the slope of cumulative plots made on the frequency data. The cumulative plot further shows high deformation frequency by a steep slope (inner damage zone) and less deformation as a gentle slope (outer damage zone). Statistical distributions of displacement and damage-zone width and their relationship are improved, and show two-slope power-law distributions with a break point at c. 100 m displacement. Bleached sandstones in the studied siliciclastic rocks of Utah are associated with a higher frequency of deformation bands and a wider damage zone compared to the unbleached zone of similar lithology. Fault damage zones in the carbonate rocks of Majella are often host to open fractures (karst), demonstrating that they can also be conductive to fluid flow.
Spatio-temporal network modelling and analysis of global strong earthquakes (M w ≥ 6.0)
Near-salt stress-induced seismic velocity changes and seismic anisotropy and their impacts on salt imaging: A case study in the Kuqa depression, Tarim Basin, China
Temporal variations in rockfall and rock-wall retreat rates in a deglaciated valley over the past 11 k.y.
Experimental quantification of bedrock abrasion under oscillatory flow
Pore structure and fractal characteristics of Ordovician Majiagou carbonate reservoirs in Ordos Basin, China
Multiscale fracture length analysis in carbonate reservoir units, Kurdistan, NE Iraq
Influence of fracture nucleation and propagation rates on fracture geometry: insights from geomechanical modelling
SPLASH: semi-empirical prediction of landslide-generated displacement wave run-up heights
Abstract Displacement waves (or tsunamis) generated by sub-aerial landslides cause damage along shorelines over long distances, making run-up assessment a crucial component of landslide risk analysis. Although site-specific modelling provides important insight into the behaviour of potential waves, more general approaches using limited input parameters are necessary for preliminary assessments. We use a catalogue of landslide-generated displacement waves to develop semi-empirical relationships linking displacement wave run-up ( R in metres) to distance from landslide impact ( x in kilometres) and to landslide volume ( V in millions of cubic metres). For individual events, run-up decreases with distance according to power laws. Consideration of ten events demonstrates that run-up increases with landslide volume, also according to a power law. Combining these relationships gives the SPLASH equation: R = a V b x c , with best-fitted parameters a = 18.093, b = 0.57110 and c = −0.74189. The 95% prediction interval between the calculated and measured run-up values is 2.58, meaning that 5% of the measured run-up heights exceed the predicted value by a factor of 2.58 or more. This relatively large error is explained by local amplifications of wave height and run-up. Comparisons with other displacement wave models show that the SPLASH equation is a valuable tool for the first-stage preliminary hazard and risk assessment for unstable rock slopes above water bodies.