A morphologic proxy for debris flow erosion with application to the earthquake deformation cycle, Cascadia Subduction Zone, USA

Penserini, B.; Roering, Joshua J.; Streig, Ashley R.

doi:10.1016/j.geomorph.2017.01.018

Cited by 32 publications

(55 citation statements)

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“…Coseismic deformation can also locally overcome interseismic deformation when splay faults focus the former in a narrower domain as in Sumatra (Philibosian et al., 2014; Sieh et al., 2008) or in South‐Central Chile (Bookhagen et al., 2006). The respective spatial distributions of co‐ and interseismic deformation may also differ on large scale (Penserini et al., 2017). Fast (coseismic) or slow (interseismic) deformation can be discriminated with the characteristic signatures they may leave in the geological record under specific conditions.…”

Section: Discussionmentioning

confidence: 99%

Co‐location of the Downdip End of Seismic Coupling and the Continental Shelf Break

et al. 2021

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The area of a subduction interface that is, frictionally coupled between earthquakes controls the size of megathrust ruptures (Aki, 1967; Mai & Beroza, 2000). Strain accumulation from partial coupling of the plate interface (Lay & Schwartz, 2004; Wang & Dixon, 2004) produces interseismic deformation at the surface, which can be inverted to determine the extent of the fully, or strongly, coupled region on the fault, following the widely used back slip model (Savage, 1983). This procedure has been used for decades to produce maps of coupling over subduction zones (e.g.,

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Section: Discussionmentioning

confidence: 99%

Co‐location of the Downdip End of Seismic Coupling and the Continental Shelf Break

et al. 2021

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“…Although it is widely accepted that river channels are more sensitive to changes in erosion or rock uplift rate than hillslopes (Ouimet et al, 2009), several recent studies suggest that hillslope morphology encodes information about tectonics that could be useful in elucidating the character of enigmatic faults, if sufficiently high‐resolution topographic data are available (Hilley et al, 2010; Milodowski et al, 2015; Roering, 2008). Penserini et al (2017) show that with adequate resolution, the topography of debris flow valley networks can scale with erosion or rock uplift rate in Cascadia. Hurst et al (2012) demonstrate that although the relationships are complex (see Heimsath et al, 2012), hillslope curvature and roughness can yield information about the timing and spatial distribution of erosion rates, and by proxy rock uplift rates, in growing or decaying landscapes.…”

Section: The Problem Of Enigmatic Seismogenic Faults: Where Are They Located and What Is Their Geometry And Rate Of Activity?mentioning

confidence: 99%

Seismic Hazard Analyses From Geologic and Geomorphic Data: Current and Future Challenges

et al. 2020

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The loss of life and economic consequences caused by several recent earthquakes demonstrate the importance of developing seismically safe building codes. The quantification of seismic hazard, which describes the likelihood of earthquake-induced ground shaking at a site for a specific time period, is a key component of a building code, as it helps ensure that structures are designed to withstand the ground shaking caused by a potential earthquake. Geologic or geomorphic data represent important inputs to the most common seismic hazard model (probabilistic seismic hazard analyses, or PSHAs), as they can characterize the magnitudes, locations, and types of earthquakes that occur over long intervals (thousands of years). However, several recent earthquakes and a growing body of work challenge many of our previous assumptions about the characteristics of active faults and their rupture behavior, and these complexities can be challenging to accurately represent in PSHA. Here, we discuss several of the outstanding challenges surrounding geologic and geomorphic data sets frequently used in PSHA. The topics we discuss include how to utilize paleoseismic records in fault slip rate estimates, understanding and modeling earthquake recurrence and fault complexity, the development and use of fault-scaling relationships, and characterizing enigmatic faults using topography. Making headway in these areas will likely require advancements in our understanding of the fundamental science behind processes such as fault triggering, complex rupture, earthquake clustering, and fault scaling. Progress in these topics will be important if we wish to accurately capture earthquake behavior in a variety of settings using PSHA in the future. Plain Language Summary Growing infrastructure and increasing population have caused significant loss of life due to recent large earthquakes, with the 2008 M w 7.9 Wenchuan and 2005 M w 7.6 Kashmir earthquakes each causing greater than 50,000 deaths. These earthquakes highlight the need for the development of building codes designed to withstand the strong ground shaking caused by earthquakes, as reinforced infrastructure is one of the most important factors for preventing fatalities due to ground shaking from earthquakes. Identifying the seismic hazard of a region, or the likelihood of ground shaking at a site due to potential earthquakes over time, is a key ingredient for informing a defensible building code. Here, we focus on current and future advances in how data from the fields of geology and geomorphology contribute to the most widely used type of seismic hazard model. These geologic data represent vital components to seismic hazard models, as they can provide information about the location and types of earthquakes that can occur over long, thousands of years, time periods, that cannot be obtained using other methods. We discuss some of the most pressing scientific issues about these data that are important for the development of seismic hazard models and defensible building codes.

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“…Debris flow processes operating in the upper reaches of valley networks can result in steep, planar valley long profiles, with a non-power law relationship between valley slope and drainage area[45]. Furthermore, recent studies have suggested that increased erosion rates are correlated with longer sections of the channel being dominated by debris flows[46,47], which would reduce the overall apparent concavity of the channel network[28].Numerous debris flows have been mapped in the area, with high concentrations of debris flows in the headwaters beginning at catchment 30 and above (approximately 18 km along the landform measured from Point Reyes Station) [48].A reduction in concavity with uplift could also be the result of spatial gradients in uplift within individual catchments[49], but would require uplift rates to be highest near the catchment outlet in order to result in concavity values lower than typically expected (θ = 0.4−0.6,[1]). Nevertheless, a relationship between channel concavity and uplift has not previously been demonstrated from field data, and future studies should seek to verify whether such a relationship exists in other landscapes.…”

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confidence: 99%

Detection of channel-hillslope coupling along a tectonic gradient

Hurst

Grieve

Clubb

et al. 2019

Earth and Planetary Science Letters

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Landscape morphology reflects the spatial and temporal history of erosion. Erosion in turn embodies the competition between tectonic and climatic processes. Quantitative analysis of topography can therefore reveal the driving tectonic conditions that have influenced landscape development, when combined with theoretical understanding of erosion processes. Recent developments in the automated analysis of high-resolution (< 10 m) topographic data mean that integrated analysis of hillslope and channel topographic metrics can provide understanding of the transient response of landscapes to changing boundary conditions. We perform high-resolution topographic analysis of hillslopes and channels in small (< 3 km 2) catchments spanning an inferred uplift gradient along the Bolinas Ridge, California, USA, revealing tight coupling between channel steepness and hillslope metrics thought to be proxies for erosion rates. We find that the concavity of channel longitudinal profiles varies inversely with uplift rates, although drainage density increases with uplift rates. Both of these

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A morphologic proxy for debris flow erosion with application to the earthquake deformation cycle, Cascadia Subduction Zone, USA

Cited by 32 publications

References 93 publications

Co‐location of the Downdip End of Seismic Coupling and the Continental Shelf Break

Co‐location of the Downdip End of Seismic Coupling and the Continental Shelf Break

Seismic Hazard Analyses From Geologic and Geomorphic Data: Current and Future Challenges

Detection of channel-hillslope coupling along a tectonic gradient

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