Hilltop curvature as a proxy for erosion rate: wavelets enable rapid computation and reveal systematic underestimation
- 1Department of Geosciences, University of Arizona, Tucson, Arizona 85721, USA
- 2Department of Earth Sciences, University of Oregon, Eugene, Oregon 97403, USA
Correspondence: William T. Struble (email@example.com)
Estimation of erosion rate is an important component of landscape evolution studies, particularly in settings where transience or spatial variability in uplift or erosion generates diverse landform morphologies. While bedrock rivers are often used to constrain the timing and magnitude of changes in baselevel lowering, hilltop curvature (or convexity), CHT, provides an additional opportunity to map variations in erosion rate given that average slope angle becomes insensitive to erosion rate owing to threshold slope processes. CHT measurement techniques applied in prior studies (e.g., polynomial functions), however, tend to be computationally expensive when they rely on high-resolution topographic data such as lidar, limiting the spatial extent of hillslope geomorphic studies to small study regions. Alternative techniques such as spectral tools like continuous wavelet transforms present an opportunity to rapidly document trends in hilltop convexity across expansive areas. Here, we demonstrate how continuous wavelet transforms (CWTs) can be used to calculate the Laplacian of elevation, which we utilize to estimate erosion rate in three catchments of the Oregon Coast Range that exhibit varying slope angle, slope length, and hilltop convexity, implying differential erosion. We observe that CHT values calculated with the CWT are similar to those obtained from 2D polynomial functions. Consistent with recent studies, we find that erosion rates estimated with CHT from both CWTs and 2D polynomial functions are consistent with erosion rates constrained with cosmogenic radionuclides from stream sediments. Importantly, our CWT approach calculates curvature at least 103 times more quickly than 2D polynomials. This efficiency advantage of the CWT increases with domain size. As such, continuous wavelet transforms provide a compelling approach to rapidly quantify regional variations in erosion rate as well as lithology, structure, and hillslope sediment transport processes, which are encoded in hillslope morphology. Finally, we test the accuracy of CWT and 2D polynomial techniques by constructing a series of synthetic hillslopes generated by a theoretical nonlinear transport model that exhibit a range of erosion rates and topographic noise characteristics. Notably, we find that neither CWTs nor 2D polynomials reproduce the theoretically prescribed CHT value for hillslopes experiencing moderate to fast erosion rates, even when no topographic noise is added. Rather, CHT is systematically underestimated, producing a power law relationship between erosion rate and CHT that can be attributed to the increasing prominence of planar hillslopes that narrow the zone of hilltop convexity as erosion rate increases. As such, we recommend careful consideration of measurement length scale when applying CHT to estimate erosion rate in moderate to fast-eroding landscapes, where curvature measurement techniques may be prone to systematic underestimation.
The morphology of landscapes adjusts to conform to exogenic perturbations such as uplift and climate as well as spatial variations in lithology, geologic structure, and biology. As such, numerous studies have taken advantage of landscape morphology to estimate rates and timing of perturbations to these landscape properties. In bedrock rivers, for instance, geomorphic transport laws have been formulated to allow for linkages between landscape form and process, including from measurements such as channel steepness and χ, a metric that integrates drainage area along a channel profile (Kirby and Whipple, 2001; Perron and Royden, 2013; Royden and Perron, 2013). These tools have been effectively utilized to estimate and map spatial variations in uplift, quantify the timing and rates of landscape transience and uplift history, and predict drainage basin reorganization (e.g., Barnhart et al., 2020; Dietrich et al., 2003; Fox, 2019; Kirby and Whipple, 2001, 2012; Roberts and White, 2010; Willett et al., 2014; Wobus et al., 2006).
Similarly, hillslope geomorphic transport laws formulated for soil-mantled landscapes allow for estimation of uplift and erosion rates as well as prediction of the migration of hillcrests in response to landscape transience (Forte and Whipple, 2018; Mohren et al., 2020; Mudd, 2017; Mudd and Furbish, 2007, 2005; Roering, 2008; Roering et al., 2007, 2001, 1999). Over 100 years ago, it was proposed that hillslope form, specifically slope and curvature, may be an effective predictor of erosion rate, as hillslopes steepen and lengthen to accommodate increases in baselevel lowering (Gilbert, 1909, 1877). However, hillslopes do not continue to steepen as baselevel lowering progressively increases to faster and faster rates (e.g., Howard, 1994; Penck, 1953; Schumm, 1967; Strahler, 1950). Rather, hillslope gradients approach a threshold value as erosion rate increases, such that gradient becomes invariant and insensitive to further increases in baselevel lowering (Andrews and Bucknam, 1987; Burbank et al., 1996; DiBiase et al., 2012; Larsen and Montgomery, 2012; Montgomery, 2001; Roering et al., 1999). In such cases, sediment flux varies nonlinearly with slope due to threshold-dependent processes such as landsliding as well as granular creep (BenDror and Goren, 2018; Deshpande et al., 2021; DiBiase et al., 2012; Ferdowsi et al., 2018; Gabet, 2000; Larsen and Montgomery, 2012; Montgomery, 2001; Ouimet et al., 2009; Roering et al., 2001).
Despite the insensitivity of hillslope gradient in rapidly eroding landscapes, soil-mantled hillslopes remain an effective record of landscape transience and uplift. Specifically, hilltop curvature continues to respond to baselevel lowering when uplift and erosion rates are high, even as slope becomes insensitive to ever-increasing erosion rate (Hurst et al., 2012; Mohren et al., 2020; Roering et al., 2007). For a one-dimensional hillslope at steady state, erosion rate, E [L T−1], can be estimated as
where ρs and ρr are the density of soil and bedrock [M L−3], respectively, D is the soil transport coefficient or diffusivity [L2 T−1], and CHT is curvature at the hilltop [L−1] (Roering et al., 2007). Using this formulation, Hurst et al. (2012) demonstrated in the Sierra Nevada, California, that CHT records erosion rate in both low-relief, low-slope headwater catchments of the Feather River as well as in high-relief catchments that have already adjusted to a faster baselevel lowering rate where hillslopes approach a threshold angle. Similarly, Hurst et al. (2013) observed that hillslopes that are translating through an uplift gradient along the San Andreas Fault actively steepen and become sharper (CHT becomes more negative) as they traverse the zone of high uplift and hillslope gradients become invariant. The hillslopes then decay (i.e., slopes become gentler and curvatures become less sharp) as they reenter the region of low background uplift (Hurst et al., 2013). Similarly, Clubb et al. (2020) observed that steep channels and sharp hilltops record uplift along the Mendocino Triple Junction in northern California, and they note that the lag in hillslope response time relative to the bedrock channels records the northward migration of the Mendocino Triple Junction.
Past studies that couple geomorphic transport laws and hilltop curvature have typically relied on curvature calculated from 2D polynomial functions fit to the topographic surface (PFTs; i.e., polynomials fit to topography; e.g., Roering et al., 1999). While a variety of polynomial forms and types of curvature (i.e., tangential, planform, Laplacian, etc.) have been utilized (e.g., Minár et al., 2020; Moore et al., 1991), Hurst et al. (2012) found that six term functions were sufficient for measuring curvature to estimate erosion rate. Specifically, Hurst et al. (2012) used least squares regression to fit a surface, z, to topography such that
where curvature, or more specifically the Laplacian of elevation, ∇2z, is denoted as
To reduce the impact of topographic roughness due to stochastic sediment transport and surface perturbations such as boulders and tree throw pits as well as noise in the digital topographic data, they applied the PFT over a scale, λ (L in Hurst et al., 2012), which defines the size of the square polynomial kernel that is fit to the surface. The value of λ [L] can be obtained by analysis of the scale dependency of roughness metrics (e.g., Hurst et al., 2012; Roering et al., 2010). As elaborated in the methodology proposed by Hurst et al. (2012), the PFT is not required to pass through any digital elevation model (DEM) nodes; hence, λ can be understood as a smoothing scale, thus measuring the background CHT and removing topographic noise.
While the application of PFTs has proven useful for calculating curvature to estimate erosion rate and predict spatial and temporal variations in uplift (e.g., Clubb et al., 2020; Godard et al., 2020; Hurst et al., 2019, 2013, 2012; Mohren et al., 2020; Roering et al., 2007), PFTs are computationally cumbersome, hindering large-scale exploitation of high-resolution topographic datasets that have become increasingly available. Here, we demonstrate that 2D continuous wavelet transforms (CWTs) provide an alternative and computationally efficient approach to calculating hilltop curvature, operating at least 102 to >103 times faster than PFTs, with the relative efficiency advantage of CWTs increasing with the size of digital elevation models. We establish the similarity of the output CWT CHT values to those produced by PFTs, and we compare estimated erosion rates calculated from CHT values to erosion rates measured with cosmogenic radionuclides (CRNs) in catchments in the Oregon Coast Range. In addition, we test the relative accuracy of the CWT and PFT approaches by applying them to synthetic hillslopes with known erosion rates generated by a nonlinear transport model and superimposed topographic noise. We find that both techniques systematically underestimate CHT at moderate to high erosion rates and appear to approximate a square root relationship between CHT and erosion rate as erosion rate increases, consistent with a recent study (Gabet et al., 2021).
We selected the Oregon Coast Range (OCR) to compare CWTs and PFTs as hilltop curvature measurement techniques, as it is a region that has been extensively studied in the geomorphic literature, exhibits relatively uniform topography over intra-catchment scales while exhibiting diversity in hillslope form and erosion rate across the axis of the range, and has negligible spatial variability in climate. The OCR is an unglaciated humid landscape that parallels the Cascadia Subduction Zone and is characterized by cool, wet winters when the majority of the annual 1–2 m of precipitation falls, and warm, dry summers (PRISM Climate Group, 2016). The dominant tree populations are composed of Douglas-fir (Pseudotsuga menziesii) and western hemlock (Tsuga heterophylla) that reside on hillslopes that are soil-mantled throughout the range. Soils are thickest in colluvial hollows and unchannelized valleys (∼1–2 m), thinnest (∼0.5 m) on planar hillslopes and hilltops, and are primarily produced stochastically through tree throw and bioturbation (Dietrich and Dunne, 1978). Colluvial hollows are periodically evacuated by shallow landslides that mobilize into debris flows (Benda and Dunne, 1997; Dietrich and Dunne, 1978; Penserini et al., 2017; Stock and Dietrich, 2003). Erosion rates, measured using techniques including CRNs, 14C dating, and fluvial and colluvial sediment flux, usually cluster at approximately 0.1 mm yr−1 (Balco et al., 2013; Bierman et al., 2001; Heimsath et al., 2001; Penserini et al., 2017; Reneau and Dietrich, 1991), though these rates can temporally and spatially vary dramatically (Almond et al., 2007; Marshall et al., 2015; Sweeney et al., 2012). Average OCR erosion rates approximately correspond with uplift rates calculated from abandoned marine terraces, ranging from <0.05 to >0.4 mm yr−1 (Kelsey et al., 1996), as well as from fluvial strath terraces which range from 0.1 to 0.3 mm yr−1 (Personius, 1995), which has led to suggestions that the OCR may approximate steady state. Nonetheless, deviations from uniform erosion have been noted based on morphologic trends as well as soil properties (Almond et al., 2007; Sweeney, et al., 2012).
We pinpointed catchments in the OCR that exhibit a range of hilltop curvatures for analysis. Specifically, we focus on Hadsall Creek (43.983∘ N, 123.823∘ W), the North Fork Smith River (NFSR; 43.963∘ N, 123.811∘ W), and Bear Creek (44.181∘ N, 123.371∘ W). Hadsall Creek and the NFSR are catchments in the central OCR that share a drainage divide (Fig. 1a). Hadsall Creek is characterized by steep channels and hillslopes with evenly spaced ridges and valleys where incision is dominated by debris flows (Penserini et al., 2017; Fig. 2a). Contrastingly, the NFSR, which is erosionally isolated from baselevel by an Oligocene-age gabbroic dike that has pinned the fluvial channel, exhibits comparatively gentle channel and hillslope angles as well as longer soil residence times (Sweeney et al., 2012; Fig. 2b). CRN measurements have recorded catchment-averaged erosion rates at Hadsall Creek and the NFSR of 0.113±0.018 and 0.058±0.0054 mm yr−1, respectively (recalculated from Penserini et al., 2017; Table 1). We also utilize hillslopes within three small sub-catchments that drain to Bear Creek (Fig. 1b), a tributary to the Long Tom River on the eastern margin of the OCR in the southwestern Willamette Valley (WV). Hillslopes within Bear Creek and the western margin of the WV exhibit gentle slopes, weathered soils with long residence times >150 kyr (Almond et al., 2007), and are bounded by broad alluviated valleys (Fig. 2c). We additionally report a newly collected CRN-derived catchment-averaged erosion rate for the northern Bear Creek subcatchment that we study here (Fig. 1b).
The spatial proximity of Bear Creek, Hadsall Creek, and the NFSR makes them well-suited to compare CHT measurement techniques, as other factors that may influence morphology, such as climate and lithology, remain relatively invariant. All three catchments are within the Tyee Formation, a ∼3 km thick sequence of gently dipping Eocene turbidite deposits characterized by a sequence of sandstone and siltstone interbeds (Baldwin, 1956; Heller and Dickinson, 1985; Lovell, 1969). While variability in sandstone–siltstone ratios in the Tyee Formation results in latitudinal north–south variations in deep-seated landsliding (Roering et al., 2005), our three study sites are within sufficient proximity to each other such that lithologic variability in setting hillslope morphology should be limited. In addition, while common elsewhere in the OCR (Franczyk et al., 2019; LaHusen et al., 2020; Roering et al., 2005), the sites we have selected for analysis do not exhibit pronounced evidence of deep-seated landslides, which may bias CHT values, complicating comparison to known erosion rates from CRN analysis. As such, Hadsall Creek, the NFSR, and Bear Creek provide an ideal spectrum of hillslopes that allows for assessment of CHT measurement techniques (Fig. 2).
3.1 Curvature calculation: polynomial fit and continuous wavelet transform
We used PFTs to calculate curvature of the Hadsall and Bear Creeks and NFSR lidar DEMs as enumerated in Eqs. (2) and (3). Each DEM has a grid spacing of 0.9144 m (3 ft). The lidar for Bear Creek was collected in 2009 (average point density: 8.14 pulses m−2, ground density: 1.36 pulses m−2), and the lidar at Hadsall Creek and NFSR was collected in 2014 (average point density: 10.41 pulses m−2, ground density 0.54 pulses m−2). (See “Code and data availability” for access information to lidar data.) In order to identify and remove the topographic impact of stochastic sediment transport processes such as tree throw, we calculated PFT curvature rasters using variable kernel sizes, corresponding to a range of smoothing scales, specifically for λ=5–141 m (the diameter of the polynomial kernel requires odd dimensions). These values of λ are informed by the requirements of the CWT, which we discuss below. For the PFT, λ is the diameter of the smoothing window.
In contrast to PFTs, CWTs are computationally efficient and can provide a variety of outputs depending on the analysis and type of wavelet used (e.g., Foufoula-Georgiou and Kumar, 1994, and references therein). Here, we applied a 2D CWT using the Ricker wavelet (often known as the Mexican hat wavelet). The Ricker wavelet has been used in geomorphology to map and estimate landslide ages based on surface roughness (Booth et al., 2009; LaHusen et al., 2020), identify dominant landforms at particular wavelengths (Struble et al., 2021), and extract channel heads and drainage networks (Lashermes et al., 2007; Passalacqua et al., 2010) and other topographic spectral analyses including mapping faults and predicting lithospheric thickness (e.g., Audet, 2014; Jordan and Schott, 2005; Malamud and Turcotte, 2001). In applying the Ricker wavelet, we take advantage of a useful property of convolutions that allows for simultaneous removal of topographic noise and calculation of derivatives. Specifically,
where f is some function (topography in our case), h is a smoothing function (2D Gaussian for instance), and ∗ represents the convolution. Hence, for the case of calculating derivatives of topography, Eq. (4) implies that applying a low-pass filter to topography and then taking the derivative (left term of Eq. 4) is identical to taking the derivative of topography and smoothing the outputs (middle term), which is correspondingly equivalent to taking the derivative of the smoothing function and using that function to smooth topography (right term; Lashermes et al., 2007). The application of the Ricker wavelet to calculate land surface curvature is akin to the rightmost term in Eq. (4), albeit by taking the second derivative of the smoothing function.
The Ricker wavelet is the negative second derivative of a 2D Gaussian function [L−2], which is given as
where (u, v) and s [L] (σ in Lashermes et al., 2007) define the location and size, specifically the standard deviation, of the Gaussian function, respectively (derivative of a Gaussian, DoG, wavelets constitute a wavelet family). The Ricker wavelet, ψ [1 L−4], as the negative, second derivative of Eq. (5), then, is defined as
The generalized 2D CWT of topography, z, at location (u, v), then is given as
Equation (7), notably, is a convolution of z and ψ, expressed as
where ∗ represents the convolution. The output wavelet coefficients, C, of the Ricker wavelet from Eq. (8) provide a measure of the low-pass filtered Laplacian over the input scale of interest (Foufoula-Georgiou and Kumar, 1994; Lashermes et al., 2007) that we use to estimate curvature of extracted hilltops (CHT).
Similar to the application of PFTs to estimate erosion rate, it is necessary to select a measurement scale that effectively smooths over stochastic sediment transport perturbations and noise that is inherent to topographic datasets and DEMs and does not represent long-term morphology reflective of baselevel lowering (Hurst et al., 2012; Roering et al., 2010). Thus, it is important to utilize an appropriately scaled wavelet, s (akin to a kernel size), to generate curvature values that are appropriate to represent CHT. Several definitions for the smoothing scale of a DoG wavelet exist. Torrence and Compo (1998) define the smoothing scale, λ [L], for an mth DoG as
For the Ricker wavelet, m=2. Under the Torrence and Compo (1998) definition, λ is determined by the scale, s, at which the wavelet power spectrum applied for a particular function with a known frequency (i.e., a cosine function) attains a maximum value. Alternatively, Lashermes et al. (2007) define the Ricker wavelet smoothing scale as the inverse of the wavelet's band-pass frequency, such that
To clarify, while λ represents the physical scale at which topography is smoothed, s specifically defines the scale of the wavelet function and is related to the physical smoothing scale through Eqs. (9) and (10) and is not interchangeable with λ. While the Torrence and Compo (1998; TC98) and Lashermes et al. (2007; L07) λ definitions generate similar smoothing scales, the output Laplacian values may be sufficiently diverse to produce significantly different erosion rate estimates depending on the choice. Thus, we utilize both definitions by selecting a range of λ and solving for s using both Eqs. (9) and (10) in order to apply the CWT, which we then compare to the curvature values produced from the PFT.
We applied the CWT and PFT for λ values that correspond to the scales at which topographic noise manifests in topographic data. The CWT can only be applied for s>1, which for DEMs with a grid spacing of ∼1 m with the odd-dimensions constraint of the PFT, places a lower λ limit of 5 m. We additionally tested larger λ (up to 141 m) to isolate the consistency between the CWT and PFT. For each smoothing scale, λ, for which we calculated curvature, we solved for s in Eqs. (9) and (10) to construct the appropriately sized Ricker wavelet (Eq. 6). We then applied the CWT to the OCR lidar DEMs for smoothing scales of 5–141 m (same as PFT) and produced CHT values for the CWT and PFT methods, denoted as CHT-W and CHT-P, respectively.
3.2 Computational efficiency of curvature values
We compared the efficiency of calculating curvature with a PFT to the CWT, including both definitions of wavelet smoothing scale, λ (TC98 and L07; Eqs. 9, 10). We measured curvature for λ=5–197 m in MATLAB on a personal laptop with 16 GB of RAM (2.60 GHz CPU). To account for potential variations in calculation time that may result from variable landscape morphology, we utilized sample regions of the Hadsall Creek and Bear Creek DEMs, as they represent the high and low erosion rate end members of our test sites. Each DEM was a 513×513 single precision grid (32-bit float) with a cell size of 0.9144 m.
We also tested how DEM size affects the relative speed of the CWT and PFT algorithms. We selected a DEM of size 682×682 pixels from the Hadsall Creek catchment and measured curvature for λ=5–101 m. We then calculated curvature for the same λ on the northwest quadrant of the 682×682 pixel DEM, corresponding to a 341×341 pixel medium-sized grid. Finally, we calculated curvature for λ=5–101 m on the northwest quadrant of the medium-sized DEM, corresponding to a 171×171 pixel grid.
3.3 Hilltop extraction
We calculated curvature at every pixel of our DEMs, but CHT requires limiting curvature values to hilltop pixels. Therefore, we extracted hilltop masks in MATLAB with the DIVIDEobj function of TopoToolbox (Scherler and Schwanghart, 2014), restricting extracted first-order divides to those with lengths exceeding 800 m (Schwanghart and Scherler, 2020). We further refined the hilltop masks by only considering locations where CHT is negative (convex) and where local hillslope gradient is less than 0.4, above which a greater proportion of hillslope sediment transport can be classified as nonlinear. We manually removed drainage divides mapped in low-relief valley bottoms and where flow routing is interrupted by roads, which are common in the OCR and introduce noisy high-magnitude curvatures. While the signature of deep-seated landslides is generally absent from our study catchments, if it appeared in the DEM that there has been a history of bedrock slope instability, we filtered hilltops proximal to mapped landslides. We also did not consider hilltops that may exhibit prominent asymmetry due to disequilibrium with neighboring drainage basins. Thus, at Hadsall Creek and NFSR, we neglected all hilltops at the main drainage divide (Fig. 1a). At the Bear Creek catchments, we similarly removed all hilltops at the main drainage divide (the northeast divide in Fig. 1b) except for those that border adjacent catchments that are likely experiencing the same baselevel imposed by Bear Creek (southwest divide in Fig. 1b). Finally, to visualize the scale-dependency of CHT and reduce potential noise in CHT measurements for full catchments obscuring curvature scaling breaks (Hurst et al., 2012; Roering et al., 2010), we selected a single representative hilltop in each catchment (Figs. 1, 2), chosen such that it approximates the average curvature for the catchment when compared to curvature measurements taken for all hilltops (Fig. 3). The selected representative hilltop spans 234 m at Hadsall Creek (average gradient 0.23), 149 m at NFSR (average gradient 0.14), and 274 m at Bear Creek (average gradient 0.11).
3.3.1 Erosion rates estimated from hilltop curvature
We applied the CWT and PFT to the Hadsall Creek, NFSR, and Bear Creek lidar DEMs and calculated curvature. We utilized the hilltop masks to extract curvature at the hilltops (CHT). In the OCR, Roering et al. (2010) observed a scaling break in curvature at 15 m, corresponding to the length scale below which pit and mound topography dominate the surface morphology. We observe similar scaling breaks in hilltop curvature for selected hilltops at λ≈15–20 m (Fig. 3), though we note that the clarity of this scaling break depends on the size of the study area and consistency, or lack thereof, of small pit and mound topography in a landscape. Thus, while the scaling break that distinguishes the effective scale at which topographic noise is filtered out may differ between the DEMs and catchments we analyze here, we find that the scaling breaks do not clearly or systematically differ from those observed by Hurst et al. (2012) and Roering et al. (2010; Fig. 3). Thus, we used a smoothing scale of λ=15 m for the PFT and CWT in each OCR catchment to estimate erosion rate as enumerated in Eq. (1). We assumed that and D=0.003 m2 yr−1, a hillslope diffusivity estimated for the OCR (Roering et al., 1999, 2007). We compared the mean and variance of these estimated erosion rates to CRN-derived erosion rates in each OCR study catchment.
3.3.2 Erosion rates from cosmogenic radionuclides
To test the efficacy of CHT as a proxy for erosion rate, we compare erosion rates estimated from CHT to those estimated from CRNs in stream sediments. We collected stream sediments from the western tributary to Bear Creek that we study here (Fig. 1b; 44.186∘ N, 123.375∘ W) to estimate erosion rate with cosmogenic 10Be (Balco et al., 2013; Heimsath et al., 2001). We used the online calculator CRONUS (Balco et al., 2008) to calculate erosion rate for the sample, which incorporates the material from the upstream drainage area and assumes steady erosion over the CRN integration timescale (Tables 3, 4). We additionally recalculate the erosion rates for Hadsall Creek and NFSR from the CRN data previously reported by Penserini et al. (2017; Tables 2, 3).
a Recalculated erosion rates from Penserini et al. (2017); see Table 3. b See Table 4.
3.4 Construction of synthetic hillslopes to test CHT measurements
We utilized synthetic hillslopes generated from a theoretical model to compare the accuracy of hilltop curvature calculated using the PFT and CWT as well as test how well these approaches can predict erosion rate. We used the functional form for a 1D hillslope experiencing nonlinear diffusion given as
where E is the erosion rate calculated using Eq. (1) [L T−1], Sc is the threshold, or critical, slope angle, and x is distance along the hillslope profile (Roering et al., 2007). We extended the hillslope profile solution perpendicular to the x axis to construct a 2D synthetic hillslope on a 201×201 m grid (Figs. 8, 9, and S2 in the Supplement). Odd hillslope dimensions ensure the existence of a hilltop pixel in the middle of the domain. We utilized the PFT and CWT, including both CWT definitions for the wavelet scale λ (Eqs. 9, 10; TC98, L07), to calculate CHT-W and CHT-P of the synthetic hillslopes for several different scenarios. Specifically, we considered various dimensionless erosion rates, E*, given by
where LH is hillslope length (Roering et al., 2007). In testing the ability of the CWT and PFT to predict hilltop curvature, we generate hillslopes with a range of E* values that can account for variations in E, CHT, LH, and Sc. For instance, low (high) E* values may correspond to low (high) E, CHT, or LH as well as high (low) Sc, or some combination thereof. We specifically tested E* values of 1, 10, 30, and 100. While is an extreme case and may only be rarely observed in natural landscapes that are eroding rapidly and also manage to maintain a soil mantle, such as badlands, E* values of 1, 10, and 30 have been readily observed in multiple landscapes. For instance, Hurst et al. (2012) observed E* values in the Sierra Nevada, California, as high as 30, but most measured hillslopes exhibited . Hurst et al. (2013) similarly observed at the Dragon's Back along the San Andreas Fault that E* ranges from 5 to 30, reflecting a strong uplift gradient. E* along coastal California has been noted as ≲10 along the Mendocino Triple Junction (Clubb et al., 2020), ≲8 further south along the Bolinas Ridge (Hurst et al., 2019), and ranging from 1–2 at Gabilan Mesa (Roering et al., 2007). Finally, in the OCR, past studies have observed that (Marshall and Roering, 2014; Roering et al., 2007).
In addition, to account for natural topographic roughness that the CWT and PFT smooth over to estimate CHT, we introduce noise to the synthetic hillslopes in the form of white (β=0), pink (), and red, or Brownian, () noise, where β is spectral slope. White noise denotes a random surface where all wavenumbers (frequencies) have equal amplitude, or spectral power. Conversely, spectral power density varies inversely () with wavenumber for pink noise such that low wavenumbers have higher intensity. Similarly, red noise exhibits higher spectral power at low wavenumbers but more dramatically than for pink noise. While hillslope spectra will vary between landscapes and likely exhibit a combination of different spectral slopes depending on the scale of analysis, red noise surfaces generally best describe topographic noise in natural landscapes while white noise surfaces are comparatively the least likely (e.g., Booth et al., 2009; García-Serrana et al., 2018; Marshall and Roering, 2014; Pelletier and Field, 2016; Perron et al., 2008). We generated each noisy surface of values normally distributed about 0 with the standard deviation ranging from −1 m (pits) to 1 m (mounds; Konowalczyk, 2021). For each type of noise, we tested how the amplitude of the noise affects calculated CHT by scaling the noise distributions (±1 m) by 0.1 %, 0.5 %, and 5 % of hillslope length (LH=100 m). In other words, we test cases where the standard deviation of the noise, σ, is , and σ=0.05LH, corresponding to 1σ values of 10 cm, 50 cm, and 5 m, respectively. While topographic noise with a distribution of amplitudes with a standard deviation of 5 m is likely unphysical for soil-mantled landscapes, this extreme case allows us to clearly test how different topographic parameters affect calculated values of E* and how well each measurement technique can filter out noise.
4.1 Computational efficiency of CWT and PFT curvature calculation
We find that the CWT is dramatically more efficient at calculating hilltop curvature than the PFT. Curvature calculation time depends on smoothing scale, λ, with large kernel sizes taking longest for both the PFT and CWT. Specifically, we compared curvature calculation times for the PFT and CWT in selected portions of the Hadsall Creek and Bear Creek catchments for λ=5–197 m. We find that for the 513×513 single precision grid, the PFT takes ∼4–4.5 s to calculate curvature at the smallest scales and ∼30 s to calculate curvature at larger scales. Measurement time does not vary greatly between the fast and slowly eroding landscape DEMs. By comparison, for λ=5–197 m, both the CWT L07 and TC98 definitions for λ calculate curvature at the smallest scales in ∼0.0039–0.004 s while at larger scales they calculate curvature in ∼2.2–2.3 s. Comparing the two techniques, we find that at the smallest smoothing scales (λ=5 m) the CWT operates >103 times faster than the PFT, while at larger scales where λ approaches 200 m, the CWT still outpaces the PFT by over an order of magnitude (Fig. 4a, b).
In addition to the CWT outpacing the PFT at a large range of λ in two landscapes exhibiting contrasting morphology, we observe that the relative speed of the CWT to the PFT increases with DEM size. Specifically, we find that for the smallest DEM for which we calculated curvature (171×171 grid), the CWT is ∼500 times faster than the PFT when λ=5 m and is ∼10 times faster than the PFT when λ=101 m (Fig. 4c). As DEM size increases, the computational advantage of the CWT increases such that for the large DEM (682×692 grid), the CWT operates >103 times faster than the PFT when λ=5 m and ∼30 times faster when λ=101 m (Fig. 4c).
4.2 Similarity of CHT-P and CHT-W
We utilized 2D CWTs and PFTs to calculate CHT-W and CHT-P for a range of λ in the OCR catchments of Hadsall Creek, NFSR, and Bear Creek. We find that CHT-W and CHT-P are similar when using λ values of 5–30 m. Specifically, Fig. 3 compares output CHT-W using both λ length scale definitions (Eqs. 9, 10) and CHT-P for the representative hilltop in each catchment. Mean measured CHT-W and CHT-P values differ the most at small smoothing scales, where signal-to-noise ratio (topographic noise to underlying CHT) is highest (Fig. 3a, d, g). At these small smoothing scales, the standard deviation of CHT-P is larger than that of CHT-W (Fig. 3b, e, h). Mean CHT-W values for both L07 and TC98 λ definitions are similar, as are the output standard deviations (Fig. 3). However, we observe that mean CHT-W calculated using the TC98 definition of λ is lower in magnitude than that of L07 (Fig. 3; Table 1). This is not unexpected, however, since λ, as defined by TC98 in Eq. (9), is effectively smaller than that of L07 defined in Eq. (10), for a given wavelet scale, s. Figure 5 compares the output CHT measurements from each technique by plotting CHT for individual DEM nodes for λ=15 m. If measurements from each technique are in agreement, their output CHT values should plot as a 1:1 line. Indeed, CHT-W for TC98 λ is lower than that of L07 for both the representative hilltop and all mapped hilltops, with the largest deviation occurring on the sharpest hilltops (Fig. 5c, f, i). Similarly, mean CHT-W (TC98 and L07) is lower than CHT-P, particularly for high-magnitude curvatures. Nevertheless, the output values from each definition do not vary dramatically, particularly when considering the CHT for DEM nodes corresponding to representative hilltops (Fig. 5).
We additionally plot probability density functions (PDFs) of measured CHT-W and CHT-P for each catchment (Figs. 6, S1). Notably, the shape of each PDF is similar between measurement techniques but is shifted along the x axis due to the variable definitions of λ. This shift is a further illustration of the deviation from a 1:1 relationship between each measurement technique as observed in Fig. 5. Similar to the greater deviation between calculated CHT at curvature extrema in Fig. 5, we observe greater offset between PDFs in the distribution tails, while the peaks remain similar. We observe this consistency between PDF peaks reflected in the mean CHT of the PDFs, which are similar regardless of measurement technique (Fig. 6; Tables 1, 2).
4.3 Erosion rate calculated with CHT and cosmogenic radionuclides
We utilized CHT for λ=15 m to estimate erosion rate. Erosion rates calculated from CHT-P and CHT-W for all mapped hilltops and the representative hilltop in each catchment can be found in Table 2. We observe that CHT-P and CHT-W produce expected relative pattern of erosion rate in our OCR catchments. That is, calculated erosion rate from CHT is fastest at Hadsall Creek and slowest at Bear Creek, as revealed by our cosmogenic erosion rate data (Fig. 6, Table 2). Notably, we observe that CHT-generated erosion rates (mean ± standard deviation) fall within or near the measurement uncertainty of the CRN erosion rate for both the representative hilltop and all hilltops (Table 2). For instance, CRN-measured erosion rates are 0.113±0.018 mm yr−1 at Hadsall Creek, 0.058±0.0054 mm yr−1 for the NFSR, and 0.008±0.0007 mm yr−1 at Bear Creek (Tables 3, 4). Similarly, for the case of the representative hilltop and using the TC98 λ definition, we find CHT-calculated erosion rates of 0.178±0.030 mm yr−1 at Hadsall Creek, 0.088±0.025 mm yr−1 for the NFSR, and 0.007±0.005 mm yr−1 at Bear Creek. The rates calculated with the PFT and L07 λ definition are similar, whether considering the representative hilltop or all mapped hilltops in each catchment (Table 2; Figs. 6, 7, S1). Finally, we observe linear correlation between CHT-calculated and CRN-measured erosion rates at our OCR catchments (), consistent with the relationship between CHT and E expected in Eq. (1) (Fig. 7). Furthermore, the diffusivity we infer from the slope of this relationship is 0.002±0.0004 m2 yr−1 (taking into account ), a value consistent with diffusivities measured elsewhere in the OCR (Roering et al., 1999).
4.4 Testing of CHT extraction with synthetic hillslopes
We calculated CHT-P and CHT-W for a series of synthetic hillslopes with a range of dimensionless erosion rates, E*, and topographic noise (Figs. 8, 9). We observe that the ability of the CWT and PFT to reproduce the defined curvature at particular λ depends on the dimensionless erosion rate, E*, though the type and magnitude of added noise contributes to uncertainty in appropriate λ values to be used to calculate erosion rate. We focus on synthetic hillslopes where no noise has been added (i.e., σ=0 cm) as well as where noise amplitude σ=0.5 % LH, as the magnitude of noise in this case (σ=50 cm) is a reasonable physical approximation of noise and surface roughness in natural landscapes (e.g., Marshall and Roering, 2014; Pelletier and Field, 2016; Roth et al., 2020). The cases where noise amplitude is defined by σ=0.1 % LH (σ=10 cm) and σ=5 % LH (σ=5 m) can be found in the Supplement (Figs. S5–S10).
4.4.1 Slowly eroding synthetic hillslopes,
We observe that for , both the PFT and CWT reasonably predict the model-defined CHT (and thus E) at moderate smoothing scales. Specifically, when σ=0.5 % LH, CHT-W and CHT-P converge on the defined CHT when λ≳9–11 m for white noise, λ≳15–19 m for pink noise, and λ≳13 m for red noise (Fig. 10b–d). At smaller λ, the signal-to-noise ratio is too high for noise to be adequately filtered by either the PFT or CWT. This mirrors past results in natural landscapes, where a sufficiently large smoothing scale must be selected to smooth over topographic noise and recover an accurate CHT (Hurst et al., 2012; Roering et al., 2007). Notably, when , the hillslopes are not sufficiently steep to approach Sc (Figs. 8, 9). Thus, even at the largest smoothing scales, the CWT and PFT accurately record curvature (Fig. 10a–d). In natural landscapes, however, valley bottoms will introduce positive curvatures, which will cause an increase in curvature (i.e., become less negative), at smoothing scales that approach the hillslope length, which has also been utilized to constrain an optimal smoothing scale (Hurst et al., 2012), and which we observe in OCR catchments (Fig. 3a, d, g).
We observe that the uncertainty in CHT, which we define as the standard deviation of CHT along the hilltop, is highest at the smallest smoothing scales (Figs. S3, S4). Notably, we observe for all noise types that at small smoothing scales of λ=5–∼13 m, CHT-P exhibits higher uncertainty than CHT-W. As λ increases, the uncertainty in CHT-P and CHT-W diminishes as topographic noise is progressively filtered. Because red noise includes higher spectral power at long wavelengths, we observe that the decrease in CHT uncertainty occurs at larger smoothing scales, converging towards 0 at scales of >17 m (Fig. S4).
We find that when no noise is added to the synthetic hillslopes, CHT-P and CHT-W accurately predict CHT at all scales (Fig. 10a). While there is some deviation between measured and defined CHT at larger scales, this deviation is exceptionally small (<0.5 %) and is primarily a result of edge effects that may not be fully clipped for both the CWT and PFT at the edge of the synthetic hillslope domain. Uncertainty in CHT-W and CHT-P is near 0 when no surface noise is added, with deviations again primarily due to the presence of edge effects that are not fully clipped off at the hillslope tips (Fig. S4). Finally, we observe that for a given style and amplitude of added topographic noise, the uncertainty in CHT does not vary with changes in E* (Fig. S4). We do not vary topographic noise as a function of E*, so equal uncertainty over a range of E* values indicates that variable hillslope form as defined by E* does not affect the uncertainty in CHT along the hilltop. Given the convolutional form of the CWT in Eq. (8) and the distributive property of convolutions, given as
where f is the wavelet, h is the synthetic hillslope, and k is surface noise, the standard deviation of CHT remaining constant as a function of E* is not unexpected.
4.4.2 Moderate to fast eroding synthetic hillslopes,
We observe that both the CWT and PFT produce biased CHT as E* increases. The deviation between the model-defined and measured CHT progressively grows for larger E*. Specifically, for the case of λ=15 m, when , we find that CHT-W and CHT-P are within ∼10 % of the defined CHT, with modest dependencies on the type of topographic noise (Fig. 10f, g, h). However, CHT-P and CHT-W are underestimated by >20 % for hillslopes and by 60 % for slopes when λ=15 m. This deviation occurs for hillslopes constructed with topographic noise of all types as well as the synthetic hillslopes without added noise (Fig. 10i–l). Even for small λ, we observe that CHT is systematically underestimated. For the case of , we observe that CHT-W and CHT-P deviate by 10 %–25 % for λ<15 m, with the smallest λ (∼5–7 m) exhibiting the least deviation, with CHT-P and CHT-W falling within ∼10 % of the known CHT. CHT is reasonably recovered at λ=5 m for the red noise hillslope, despite the noise dominating CHT-W and CHT-P when λ=5 m for the , 10 hillslopes. Given the added noise is constant between E* values, this accurate recovery of CHT for when λ=5 m may indicate that planar hillslopes introduce curvature values sufficiently near-zero to cancel out the positive (concave) noise. For λ>15 m, we observe that CHT is underestimated by at least 25 % for all hillslopes and >60 % for hillslopes. As λ increases, this deviation systematically grows such that when λ=35, CHT is underestimated by half for hillslopes and ∼80 % for exceptionally narrow hillslopes where (Fig. 10i–p). Importantly, we observe these major deviations for the hillslopes with no added noise as well, indicating that topographic noise is not solely responsible for biased CHT.
Application of CWTs and PFTs to measure CHT and estimate erosion rate in soil-mantled landscapes such as the OCR produces erosion rate values that are in agreement with those collected from CRNs in stream sediments, though with dramatically disparate efficiencies. Yet, we also observe that while both techniques accurately reproduce hillslope morphology in synthetic landscapes experiencing modest dimensionless erosion rates, both techniques exhibit systematic bias where dimensionless erosion rate is moderate to high, calling into question the accuracy of past estimates of erosion rate in landscapes that are experiencing moderate to rapid erosion rates. Nevertheless, CWTs are an exciting tool to be added to hillslope geomorphometric analyses, particularly as high-resolution topographic datasets continue to grow and classification of topographic roughness, particularly on the hillslope scale, continues to improve.
5.1 CHT measurement and erosion rate estimation in natural landscapes: Oregon Coast Range
We utilized CWTs and PFTs to estimate erosion rate in a landscape that has been thoroughly studied in past geomorphology studies. Encouragingly, CHT-calculated erosion rates in Hadsall Creek, NFSR, and Bear Creek reproduce CRN-measured erosion rates from each site. We also observe, however, that some variability in measured CHT reinforces the need to use caution when selecting hilltops at which curvature will be extracted, especially in landscapes where topographic noise, including from anthropogenic sources such as roads, as well as landslides and variable lithology, may introduce inaccurate measurements of curvature. Indeed, despite careful selection of hilltops, calculated CHT exhibits a wide range of values (Figs. 5, 6, S1). Fortunately, the catchments we have sampled here exhibit few to no deep-seated landslides and are mapped entirely within the Tyee Formation, which exhibits little variability over small spatial scales. Also, while there are numerous forest and logging roads throughout the OCR, they are easily identifiable in lidar data and are limited to a small portion of hilltops. Hence, while haphazard selection of hilltops without a predefined methodology for trimming hilltops should be avoided, our observed agreement between estimated erosion rates for all selected hilltops in a catchment and representative hilltops emphasizes that mild to moderate trimming of hilltop masks is sufficient for estimating an accurate erosion rate (Table 2, Figs. 6, S2). Finally, agreement between TC98 and L07 λ definitions and CRN erosion rates suggests that either definition is reasonable for calculating CHT. However, careful and informed selection of λ when calculating erosion rate remains paramount.
5.2 Rapid calculation of CHT
We have demonstrated that CWTs calculate CHT>103 times faster than PFTs at smoothing scales of λ=5 m (for a 513×513 single precision grid). At smoothing scales often utilized to estimate CHT (∼10–30 m), the CWT operates >102 times faster (Fig. 4). Even at the largest smoothing scales we test (up to 197 m), the CWT operates ∼14–15 times faster than the PFT. Importantly, the computational advantage of the CWT increases with DEM size (Fig. 4c) such that the ∼103 computation time advantage that we observe should be considered a minimum, as most landscape analyses utilize DEMs larger than the grids we test here. While PFT computation times can often be substantially reduced by limiting curvature calculation to the hilltops, this dramatic difference in curvature calculation time opens many doors for utilizing hilltop curvature in topographic analyses of landscapes that require consideration of large spatial scales. What's more, the ability of the CWT to operate so efficiently on high-resolution lidar data does not necessitate that coarse data be used to analyze large regions, as has generally been the case for past geomorphic analyses of regional- and continental-scale bedrock rivers. Rather, the ability of the CWT to calculate hilltop curvature over large spatial scales with such speed means that the limiting factor for large landscape analyses where lidar data are available is not the operating time of the measurement technique but rather the ability of existing systems to store vast quantities of high-resolution topographic data and curvature-related products! In addition to CHT measurement, the rapidity of the CWT will allow for large-scale analyses of other types of curvature and landscape characteristics well-suited to spectral analyses including mapping landslides (Booth et al., 2009; LaHusen et al., 2020), quantifying surface roughness (Doane et al., 2019; Roth et al., 2020), and mapping landforms (Black et al., 2017; Clubb et al., 2014; Passalacqua et al., 2010; Perron et al., 2008; Struble et al., 2021).
5.3 CHT underestimated in moderate to fast-eroding landscapes
We find that both the CWT and PFT are unable to reproduce accurate CHT at moderate to fast dimensionless erosion rates. Disagreement between measured and defined CHT for a given E* can be conceptualized primarily as a biasing of curvature measurement as hilltops progressively narrow and steepen in response to faster erosion rates. Specifically, since we utilize a nonlinear diffusion framework to construct the synthetic hillslopes (Eq. 11), planar side slopes begin to develop and advance towards the hilltop as the hillslope gradient approaches the critical slope angle, Sc, at moderate to fast E*. The formation of planar hillslopes means, by definition, that curvature does not accurately reflect CHT along the entire hillslope length, as would be the case for a slowly eroding broad hillslope with constant curvature (i.e., linear diffusion). The synthetic hillslope, while also constructed with Eq. (11), can be approximated as experiencing linear diffusion, as slopes are not sufficiently steep to approach Sc and develop planarity. In this case, even as λ increases, CHT-W and CHT-P accurately recover the actual CHT. We observe that at these slow erosion rates (–10), the main obstacle to recovering an accurate CHT is topographic noise (Fig. 10a–h). As we have applied here, and has been previously demonstrated (Hurst et al., 2012; Roering et al., 2007), careful selection of a λ sufficiently large to remove such noise, but not so large such that concave valley bottoms introduce positive curvatures, still allows for accurate calculation of CHT, particularly for . By contrast, in cases where E* is sufficiently high to develop planar side slopes, once λ reaches a sufficiently high value to remove topographic noise, the CWT and PFT kernels have become sufficiently large to incorporate planar slopes into the curvature measurements, thus underpredicting the actual value of CHT. In these cases, topographic noise is a secondary impediment to accurate CHT measurement, preventing utilization of a sufficiently small λ that avoids planar hillslopes. Furthermore, if E* is sufficiently large, planar side slopes may appear close enough to the hilltop to disqualify almost any smoothing scale, which is clear from our synthetic hillslopes with no added noise (Fig. 10e, i, m). Importantly, even for , planar slopes begin to bias CHT (Fig. 10e).
The grid resolution of digital topographic data has been recognized to affect measurements of topographic curvature and hillslope sediment flux (e.g., Ganti et al., 2012; Grieve et al., 2016b). However, the deviation between known and measured CHT we note here is intrinsic to the form of hillslopes that are described by the nonlinear diffusion model. As E* increases and the hilltop undergoes a concomitant increase in CHT, a smaller λ is ideally required to avoid the planar side slopes and accurately calculate CHT. Unfortunately, however, λ can only be decreased so much before topographic noise and stochastic and disturbance-driven processes begin to overwhelm the calculated curvature values (Hurst et al., 2012, 2013; Roering et al., 2007; Figs. 3, 10). As such, increasing the resolution of topographic data, while desirable for characterizing hillslope sediment transport processes, will not by itself alleviate the systematic deviation between measured and model-specified CHT, as such high-resolution data will also be recording the stochastic signals that deviate from the underlying hillslope form (Roth et al., 2020). However, improved characterization of the distribution of roughness and microtopography in landscapes and how they may vary with erosion rate may provide a remedy for estimating erosion rate from topography and defining a better-informed λ, particularly in landscapes where hilltops are conspicuously sharp and where topographic resolution continues to improve.
Importantly, we stress that neither CWTs nor PFTs are, at this time, capable of accurately estimating hilltop curvature at moderate to high E*, even when λ is small (Fig. 10). We observe that the CWT and PFT systematically underpredict CHT when (Fig. 10m–p). However, we acknowledge that E* values of 100 are perhaps unreasonably high for most natural landscapes, with perhaps a few notable exceptions (e.g., Taiwan, Himalaya, New Zealand). More so, soil production limits (e.g., DiBiase et al., 2012; Heimsath et al., 1997; Montgomery, 2007; Neely et al., 2019) imply that these settings may exhibit processes that are not well represented with the soil creep model employed here. Regardless, the CWT and PFT clearly underpredict CHT when and exhibit underpredicted CHT when , even in the most ideal case when synthetic hillslopes have no added noise. Similar values of E* have been recorded in numerous natural landscapes (Clubb et al., 2020; Grieve et al., 2016a; Hurst et al., 2019, 2013, 2012; Marshall and Roering, 2014; Roering et al., 2007). Finally, the addition of topographic noise to our hillslopes serves to increase uncertainty in measurement of CHT (Figs. 10, S4, S7, S10) but does not result in systematic over- or underestimation.
5.4 Does hilltop curvature vary linearly with erosion rate?
The systematic underestimation of CHT that we observe here has important implications for interpreting erosion rates and hillslope surface processes in natural soil-mantled landscapes that are not eroding slowly. Specifically, our results here urge caution when applying hilltop curvature measurement techniques to natural soil-mantled landscapes eroding at moderate to rapid rates and where hilltops are correspondingly sharp. While CHT has been found to generally agree with independently calculated erosion rates following Eq. (1), the measurement artifact we have observed here calls into question the accuracy of calculated erosion rates from CHT in natural landscapes in past studies. Recent observations put forward by Gabet et al. (2021) show that hilltop curvature varies with the square root of erosion rate, which implies a square root relationship between hillslope diffusivity, D, and erosion rate, representing a deviation from the long-held view that CHT varies linearly with erosion rate (Eq. 1). Here we use a synthetic hillslope simulation to explore whether these findings may be influenced by a systematic bias in the estimation of CHT due to the formation of planar side slopes proximal to hilltops as described above (Fig. 10). Specifically, we followed the methodology laid out by Gabet et al. (2021) and reproduced a CHT–E relationship from synthetic hillslopes with no added noise. While Gabet et al. (2021) constructed synthetic hillslope profiles to account for the effect of grid spacing on calculated CHT, we additionally consider the role of smoothing scale, λ, on estimation of CHT. In order to facilitate comparison, we initially selected λ=14 m, the same scale that Gabet et al. (2021) applied at each of their field sites, to calculate CHT. We constructed a series of synthetic hillslopes described by Eq. (11) for –100, which corresponds to erosion rates of ∼0.01–1 mm yr−1 (for D=0.003 m2 yr−1). To constrain how hillslope diffusivity modulates the erosion rate at which CHT is underestimated, we also tested a range of diffusivities, spanning D=0.001–0.005 m2 yr−1 (assuming ). We used the CWT to calculate curvature; a PFT could be used as well, which would be consistent with the Gabet et al. (2021) methodology. However, as we have demonstrated, CHT-P and CHT-W are similar for both natural hillslopes and synthetic hillslopes with no added noise (Figs. 3, 10).
We observe that erosion rate and CHT do not vary linearly as expected from Eq. (1) for all erosion rates (Fig. 11). While the relationship between erosion rate and measured hilltop curvature (we plot the absolute value, , to allow visualization of positive values) is linear as expected from Eq. (1) for slow erosion rates of 0.01–0.08 mm yr−1 (for the case of D=0.003 m2 yr−1), the measured and actual synthetic values of begin to clearly diverge for erosion rates >0.08 mm yr−1 (Fig. 11a), though some deviation exists at erosion rates as low as ∼0.03 mm yr−1 (Fig. 11b; blue squares). This deviation occurs at even slower erosion rates for D=0.001 m2 yr−1, specifically at erosion rates of ∼0.02–0.03 mm yr−1 (Fig. 11a). As this deviation increases with erosion rate (and E*), it approximates a square root relationship between erosion rate and hilltop curvature. Importantly, the erosion rate at which this deviation occurs is heavily dependent on smoothing scale and diffusivity. For the range of tested diffusivities (D=0.001–0.005 m2 yr−1) and for λ=14 m and λ=20 m, we plotted the ratio of measured CHT to the actual CHT (Fig. 11b). We find that for smaller D, the deviation between measured and model-defined CHT occurs at slower erosion rates, while λ dictates the magnitude of deviation (Fig. 11b). For instance, for D=0.001 m2 yr−1 and λ=14 m, we find that CHT is underestimated by >10 % for erosion rates ≳0.04 mm yr−1, and when λ=20 m, CHT is underestimated by >15 % for that same erosion rate of 0.04 mm yr−1. Thus, while the erosion rates at which we observe significant deviation between measured and model-defined CHT tend to be higher than those found in many soil-mantled landscapes (for D=0.003 m2 yr−1 and λ=14 m) (Montgomery, 2007), including those tested by Gabet et al. (2021), the strong dependency of this deviation on diffusivity and smoothing scale warrants caution in interpretations of nonlinear relationships between hilltop curvature and erosion rate. Furthermore, without a priori knowledge of the diffusivity, determination of the magnitude of CHT underestimation is challenging to ascertain from topographic data alone (Fig. 11b). Importantly, the underestimation in CHT we note here is independent of topographic noise and surface roughness. Incorporation of such roughness will introduce additional uncertainties. We encourage future work to investigate climatic and other factors that dictate hillslope diffusivity and the potential coupling between diffusivity and erosion rate (e.g., Richardson et al., 2019), although care must be taken to ensure that observed relationships do not result from measurement artifacts that deviate from the true underlying hillslope form.
Current hilltop curvature measurement techniques do not have a well-defined capability to filter topographic noise that is inherent to all landscapes and topographic datasets while maintaining an unbiased value of CHT at high values of E* where nearly planar (i.e., negligible curvature) side slopes become increasingly proximal to hilltops. Essentially, the zone of hilltop convexity becomes exceedingly narrow (and thus difficult to estimate) as E* increases. As such, estimates of erosion rates using Eq.(1) should be considered minimum erosion rates, particularly in landscapes with conspicuously sharp hilltops (Fig. 10). These results strongly motivate future investigation of the structure of topographic noise in landscapes due to underlying processes such as tree throw and other sources of bioturbation, as well as noise inherent to digital topographic data. Improved understanding of the structure of topographic surface roughness may facilitate future accurate morphologic estimates of erosion rate in moderate- to fast-eroding landscapes.
We utilized 2D continuous wavelet transforms to calculate hilltop curvature in three catchments in the Oregon Coast Range that exhibit a diversity of hillslopes. We found that the measured hilltop curvature values are comparable to those calculated from fitting 2D polynomial functions to topography to calculate curvature, a method that has been commonly applied elsewhere. Both techniques produce estimates of erosion rate that are consistent with those independently constrained from cosmogenic radionuclides in stream sediments. Specifically, we find that erosion rate calculated with the CWT is mm yr−1 in Hadsall Creek, 0.1±0.05 mm yr−1 in the North Fork Smith River, and 0.01±0.008 mm yr−1 in three small catchments that drain to Bear Creek. We further find that the 2D continuous wavelet transform operates 102 to >103 times faster than the 2D polynomial when applied at smoothing scales that are commonly used for calculating hilltop curvature (∼5–30 m). We additionally find that the computational advantage of the 2D continuous wavelet transform increases as digital elevation models become larger. This dramatic disparity in operation time opens numerous doors for widespread topographic analysis as high-resolution topographic data become increasingly available.
We additionally test the accuracy of both the wavelet transform and polynomial by constructing synthetic hillslopes following a nonlinear diffusive hillslope geomorphic transport law. Synthetic hillslopes were constructed with and without added surface noise of various types (white, pink, red/Brownian) and exhibited various forms corresponding to a range of dimensionless erosion rates. We find that both the wavelet transform and polynomial are able to reproduce hilltop curvature for slow dimensionless erosion rates (–10). However, we also observe that both techniques produce underestimated values of CHT when , as planar hillslopes begin to systematically bias the calculated curvature at the hilltop. While this is in part due to the required smoothing of topography to remove added noise, which in natural landscapes is due to stochastic transport processes as well as noise inherent in digital topographic data, we also find that curvature is underestimated on synthetic hillslopes where there is no added noise. At moderate to high dimensionless erosion rates (–100), we find that hilltop curvature is systematically underestimated as hillslopes become progressively narrower near the hilltop. This systematic deviation from the defined and measured hilltop curvature has key implications for predicting erosion rates in soil-mantled landscapes. In landscapes eroding at moderate to rapid rates, erosion rates calculated with hilltop curvature should be considered a minimum. Finally, we demonstrate that underestimation of synthetic hilltop curvature at moderate to fast erosion rates results in apparent power law and square root relationships between erosion rate and hilltop curvature. This previously observed relationship from natural hillslopes has led to suggestions that hillslope diffusivity may also vary as the square root of erosion rate. Our results here, however, demonstrate that this may be a measurement artifact introduced by planar hillslopes biasing hilltop curvature measurements as hilltops progressively narrow and steepen, not simply due to poor data resolution. Future hillslope geomorphic work must more clearly characterize the roughness of soil-mantled hillslopes and develop methods that smooth and remove topographic noise while maintaining an unbiased hilltop curvature measurement, if hilltop curvature is to be applied in rapidly eroding landscapes.
We utilized TopoToolbox (https://topotoolbox.wordpress.com/download, last access: 14 September 2021, Schwanghart and Scherler, 2014, https://doi.org/10.5194/esurf-8-245-2020) code in this paper, which is freely available. We additionally used wavelet codes from the Automated Landslide Mapping toolkit (ALMtools) by Adam Booth (http://web.pdx.edu/~boothad/tools.html, last access: 14 September 2021; Booth et al., 2009, https://doi.org/10.1016/j.geomorph.2009.02.027). Additional MATLAB scripts, including for synthetic hillslope construction, are available at https://github.com/wtstruble (last access: 14 September 2021, Struble, 2021). All utilized lidar DEMs are publicly available from the Oregon Department of Geology and Mineral Industries (https://www.oregongeology.org/lidar/, last access: 14 September 2021, Oregon Lidar Consortium and Oregon Department of Geology and Mineral Industries, 2021).
The supplement related to this article is available online at: https://doi.org/10.5194/esurf-9-1279-2021-supplement.
WTS and JJR conceived of and designed the study. WTS developed the study and completed the analysis. WTS prepared the manuscript with contributions from JJR.
The contact author has declared that neither they nor their co-author have any competing interests.
Publisher’s note: Copernicus Publications remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
Thank you to Brooke Hunter, Danica Roth, Fiona Clubb, and Odin Marc for helpful discussions. Tyler Doane, an anonymous reviewer, and associate editor Simon Mudd provided insightful reviews that improved the quality of the manuscript. We are particularly grateful to Adam Booth, who provided several helpful and enlightening conversations about wavelets. 10Be data were processed at Lawrence Livermore National Laboratory.
This paper was edited by Simon Mudd and reviewed by Tyler Doane and one anonymous referee.
Almond, P., Roering, J., and Hales, T. C.: Using soil residence time to delineate spatial and temporal patterns of transient landscape response, J. Geophys. Res., 112, F03S17, https://doi.org/10.1029/2006JF000568, 2007.
Andrews, D. J. and Bucknam, R. C.: Fitting degradation of shoreline scarps by a nonlinear diffusion model, J. Geophys. Res., 92, 12857–12867, https://doi.org/10.1029/JB092iB12p12857, 1987.
Audet, P.: Toward mapping the effective elastic thickness of planetary lithospheres from a spherical wavelet analysis of gravity and topography, Phys. Earth Planet. In., 226, 48–82, https://doi.org/10.1016/j.pepi.2013.09.011, 2014.
Balco, G., Stone, J. O., Lifton, N. A., and Dunai, T. J.: A complete and easily accessible means of calculating surface exposure ages or erosion rates from 10Be and 26Al measurements, Quat. Geochronol., 3, 174–195, https://doi.org/10.1016/j.quageo.2007.12.001, 2008.
Balco, G., Finnegan, N., Gendaszek, A., Stone, J. O., and Thompson, N.: Erosional response to northward-propagating crustal thickening in the coastal ranges of the US Pacific Northwest. Am. J. Sci., 313, 790–806, 2013.
Baldwin, E. M.: Geologic map of the lower Siuslaw River area, Oregon, Oil and Gas Investigations 186, scale , United States Geological Survey, Washington, D. C., https://doi.org/10.3133/om186, 1956.
Barnhart, K. R., Tucker, G. E., Doty, S. G., Shobe, C. M., Glade, R. C., Rossi, M. W., and Hill, M. C.: Inverting Topography for Landscape Evolution Model Process Representation: 1. Conceptualization and Sensitivity Analysis, J. Geophys. Res.-Earth, 125, e2018JF004961, https://doi.org/10.1029/2018JF004961, 2020.
Benda, L. and Dunne, T.: Stochastic forcing of sediment supply to channel networks from landsliding and debris flow, Water Resour. Res., 33, 2849–2863, https://doi.org/10.1029/97WR02388, 1997.
BenDror, E. and Goren, L.: Controls Over Sediment Flux Along Soil-Mantled Hillslopes: Insights from Granular Dynamics Simulations, J. Geophys. Res.-Earth, 123, 924–944, https://doi.org/10.1002/2017JF004351, 2018.
Bierman, P., Clapp, E., Nichols, K., Gillespie, A., and Caffee, M. W.: Using cosmogenic nuclide measurements in sediments to understand background rates of erosion and sediment transport, in: Landscape Erosion and Evolution Modeling, Springer, Boston, MA, 89–115, 2001.
Black, B. A., Perron, J. T., Hemingway, D., Bailey, E., Nimmo, F., and Zebker, H.: Global drainage patterns and the origins of topographic relief on Earth, Mars, and Titan, Science, 356, 727–731, https://doi.org/10.1126/science.aag0171, 2017.
Booth, A. M., Roering, J. J., and Perron, J. T.: Automated landslide mapping using spectral analysis and high-resolution topographic data: Puget Sound lowlands, Washington, and Portland Hills, Oregon, Geomorphology, 109, 132–147, https://doi.org/10.1016/j.geomorph.2009.02.027, 2009 (available at: http://web.pdx.edu/~boothad/tools.html, last access: 14 September 2021).
Burbank, D. W., Leland, J., Fielding, E., Anderson, R. S., Brozovic, N., Reid, M. R., and Duncan, C.: Bedrock incision, rock uplift and threshold hillslopes in the northwestern Himalayas, Nature, 379, 505–510, https://doi.org/10.1038/379505a0, 1996.
Clubb, F. J., Mudd, S. M., Milodowski, D. T., Hurst, M. D., and Slater, L. J.: Objective extraction of channel heads from high-resolution topographic data, Water Resour. Res., 50, 4283–4304, https://doi.org/10.1002/2013WR015167, 2014.
Clubb, F. J., Mudd, S. M., Hurst, M. D., and Grieve, S. W. D.: Differences in channel and hillslope geometry record a migrating uplift wave at the Mendocino triple junction, California, USA, Geology, 48, 184–188, https://doi.org/10.1130/G46939.1, 2020.
Deshpande, N., Furbish, D., Arratia, P., and Jerolmack, D.: The perpetual fragility of creeping hillslopes, Nat. Commun., 12, 3909, https://doi.org/10.31223/OSF.IO/QC9JH, 2021.
DiBiase, R. A., Heimsath, A. M., and Whipple, K. X.: Hillslope response to tectonic forcing in threshold landscapes, Earth Surf. Proc. Land., 37, 855–865, https://doi.org/10.1002/esp.3205, 2012.
Dietrich, W. E. and Dunne, T.: Sediment budget for a small catchment in mountainous terrain, Z. Geomorphol. N.F., 29, 191–206, 1978.
Dietrich, W. E., Bellugi, D. G., Sklar, L. S., Stock, J. D., Heimsath, A. M., and Roering, J. J.: Geomorphic transport laws for predicting landscape form and dynamics, in: Geophysical Monograph Series, edited by: Wilcock, P. R. and Iverson, R. M., American Geophysical Union, Washington, D.C., 103–132, 2003.
Doane, T. H., Roth, D. L., Roering, J. J., and Furbish, D. J.: Compression and Decay of Hillslope Topographic Variance in Fourier Wavenumber Domain, J. Geophys. Res.-Earth, 124, 60–79, https://doi.org/10.1029/2018JF004724, 2019.
Ferdowsi, B., Ortiz, C. P., and Jerolmack, D. J.: Glassy dynamics of landscape evolution, P. Natl. Acad. Sci. USA, 115, 4827–4832, https://doi.org/10.1073/pnas.1715250115, 2018.
Forte, A. M. and Whipple, K. X.: Criteria and tools for determining drainage divide stability, Earth Planet. Sc. Lett., 493, 102–117, https://doi.org/10.1016/j.epsl.2018.04.026, 2018.
Foufoula-Georgiou, E. and Kumar, P.: Wavelet Analysis in Geophysics, in: Wavelet Analysis and Its Applications, Academic Press, New York, 1–43, https://doi.org/10.1016/B978-0-08-052087-2.50007-4, 1994.
Fox, M.: A linear inverse method to reconstruct paleo-topography, Geomorphology, 337, 151–164, https://doi.org/10.1016/j.geomorph.2019.03.034, 2019.
Franczyk, J. J., Burns, W. J., and Calhoun, N. C.: Statewide Landslide Information Database for Oregon Release-4.0, SLIDO 4.0, Digital Data Series. Oregon Department of Geology and Mineral Industries, Portland, OR, 2019.
Gabet, E. J.: Gopher bioturbation: Field evidence for non-linear hillslope diffusion, Earth Surf. Proc. Land., 25, 1419–1428, https://doi.org/10.1002/1096-9837(200012)25:13<1419::AID-ESP148>3.0.CO;2-1, 2000.
Gabet, E. J., Mudd, S. M., Wood, R. W., Grieve, S. W. D., Binnie, S. A., and Dunai, T. J.: Hilltop Curvature Increases with the Square Root of Erosion Rate, J. Geophys. Res.-Earth, 126, e2020JF005858, https://doi.org/10.1029/2020JF005858, 2021.
Ganti, V., Passalacqua, P., and Foufoula-Georgiou, E.: A sub-grid scale closure for nonlinear hillslope sediment transport models, J. Geophys. Res., 117, F02012, https://doi.org/10.1029/2011JF002181, 2012.
García-Serrana, M., Gulliver, J. S., and Nieber, J. L.: Description of soil micro-topography and fractional wetted area under runoff using fractal dimensions: Soil micro-topography, fractional wetted area, and fractal dimensions, Earth Surf. Proc. Land., 43, 2685–2697, https://doi.org/10.1002/esp.4424, 2018.
Gilbert, G. K.: Report on the Geology of the Henry Mountains, US Government Printing Office, Washington, D.C., 1–152, 1877.
Gilbert, G. K.: The Convexity of Hilltops, J. Geol., 17, 344–350, https://doi.org/10.1086/621620, 1909.
Godard, V., Hippolyte, J.-C., Cushing, E., Espurt, N., Fleury, J., Bellier, O., Ollivier, V., and the ASTER Team: Hillslope denudation and morphologic response to a rock uplift gradient, Earth Surf. Dynam., 8, 221–243, https://doi.org/10.5194/esurf-8-221-2020, 2020.
Grieve, S. W. D., Mudd, S. M., Hurst, M. D., and Milodowski, D. T.: A nondimensional framework for exploring the relief structure of landscapes, Earth Surf. Dynam., 4, 309–325, https://doi.org/10.5194/esurf-4-309-2016, 2016a.
Grieve, S. W. D., Mudd, S. M., Milodowski, D. T., Clubb, F. J., and Furbish, D. J.: How does grid-resolution modulate the topographic expression of geomorphic processes?, Earth Surf. Dynam., 4, 627–653, https://doi.org/10.5194/esurf-4-627-2016, 2016b.
Heimsath, A. M., Dietrich, W. E., Kunihiko, N., and Finkel, R. C.: The soil production function and landscape equilibrium, Nature, 388, 358–361, 1997.
Heimsath, A. M., Dietrich, W. E., Nishiizumi, K., and Finkel, R. C.: Stochastic processes of soil production and transport: erosion rates, topographic variation and cosmogenic nuclides in the Oregon Coast Range, Earth Surf. Proc. Land., 26, 531–552, https://doi.org/10.1002/esp.209, 2001
Heller, P. L. and Dickinson, W. R.: Submarine Ramp Facies Model for Delta-Fed, Sand-Rich Turbidite Systems. AAPG Bulletin, 69, 960–976, https://doi.org/10.1306/AD462B37-16F7-11D7-8645000102C1865D, 1985
Howard, A. D.: A detachment-limited model of drainage basin evolution, Water Resour. Res., 30, 2261–2285, 1994.
Hurst, M. D., Mudd, S. M., Walcott, R., Attal, M., and Yoo, K.: Using hilltop curvature to derive the spatial distribution of erosion rates, J. Geophys. Res., 117, F02017, https://doi.org/10.1029/2011JF002057, 2012.
Hurst, M. D., Mudd, S. M., Attal, M., and Hilley, G.: Hillslopes Record the Growth and Decay of Landscapes, Science, 341, 868–871, https://doi.org/10.1126/science.1241791, 2013.
Hurst, M. D., Grieve, S. W. D., Clubb, F. J., and Mudd, S. M.: Detection of channel-hillslope coupling along a tectonic gradient, Earth Planet. Sc. Lett., 522, 30–39, https://doi.org/10.1016/j.epsl.2019.06.018, 2019.
Jordan, G. and Schott, B.: Application of wavelet analysis to the study of spatial pattern of morphotectonic lineaments in digital terrain models. A case study, Remote Sens. Environ., 94, 31–38, https://doi.org/10.1016/j.rse.2004.08.013, 2005.
Kelsey, H. M., Ticknor, R. L., Bockheim, J. G., and Mitchell, E.: Quaternary upper plate deformation in coastal Oregon, Geol. Soc. Am. Bull., 108, 843–860, 1996.
Kirby, E. and Whipple, K.: Quantifying differential rock-uplift rates via stream profile analysis, Geology, 29, 415–418, 2001.
Kirby, E. and Whipple, K. X.: Expression of active tectonics in erosional landscapes, J. Struct. Geol., 44, 54–75, https://doi.org/10.1016/j.jsg.2012.07.009, 2012.
Konowalczyk, M.: randnd, GitHub [code], available at: https://github.com/MarcinKonowalczyk/randnd/, last access: 14 September 2021.
LaHusen, S. R., Duvall, A. R., Booth, A. M., Grant, A., Mishkin, B. A., Montgomery, D. R., Struble, W., Roering, J. J., and Wartman, J.: Rainfall triggers more deep-seated landslides than Cascadia earthquakes in the Oregon Coast Range, USA, Science Advances, 6, eaba6790, https://doi.org/10.1126/sciadv.aba6790, 2020.
Larsen, I. J. and Montgomery, D. R.: Landslide erosion coupled to tectonics and river incision, Nat. Geosci., 5, 468–473, https://doi.org/10.1038/ngeo1479, 2012.
Lashermes, B., Foufoula-Georgiou, E., and Dietrich, W. E.: Channel network extraction from high resolution topography using wavelets, Geophys. Res. Lett., 34, L23S04, https://doi.org/10.1029/2007GL031140, 2007.
Lovell, J. P. B.: Tyee Formation: Undeformed Turbidites and their Lateral Equivalents: Mineralogy and Paleogeography, Geol. Soc. Am. Bull., 80, 9–22, https://doi.org/10.1130/0016-7606(1969)80[9:TFUTAT]2.0.CO;2, 1969.
Malamud, B. D. and Turcotte, D. L.: Wavelet analyses of Mars polar topography, J. Geophys. Res., 106, 17497–17504, https://doi.org/10.1029/2000JE001333, 2001.
Marshall, J. A. and Roering, J. J.: Diagenetic variation in the Oregon Coast Range: Implications for rock strength, soil production, hillslope form, and landscape evolution, J. Geophys. Res.-Earth, 119, 1395–1417, https://doi.org/10.1002/2013JF003004, 2014.
Marshall, J. A., Roering, J. J., Bartlein, P. J., Gavin, D. G., Granger, D. E., Rempel, A. W., Praskievicz, S. J., and Hales, T. C.: Frost for the trees: Did climate increase erosion in unglaciated landscapes during the late Pleistocene?, Science Advances, 1, e1500715, https://doi.org/10.1126/sciadv.1500715, 2015.
Minár, J., Evans, I. S., and Jenčo, M.: A comprehensive system of definitions of land surface (topographic) curvatures, with implications for their application in geoscience modelling and prediction, Earth-Sci. Rev., 211, 103414, https://doi.org/10.1016/j.earscirev.2020.103414, 2020.
Mohren, J., Binnie, S. A., Ritter, B., and Dunai, T. J.: Development of a steep erosional gradient over a short distance in the hyperarid core of the Atacama Desert, northern Chile, Global Planet. Change, 184, 103068, https://doi.org/10.1016/j.gloplacha.2019.103068, 2020.
Montgomery, D. R.: Slope distributions, threshold hillslopes, and steady-state topography, Am. J. Sci., 301, 432–454, 2001.
Montgomery, D. R.: Soil erosion and agricultural sustainability, P. Natl. Acad. Sci. USA, 104, 13268–13272, https://doi.org/10.1073/pnas.0611508104, 2007.
Moore, I. D., Grayson, R. B., and Ladson, A. R.: Digital terrain modelling: A review of hydrological, geomorphological, and biological applications, Hydrol. Process., 5, 3–30, https://doi.org/10.1002/hyp.3360050103, 1991.
Mudd, S. M.: Detection of transience in eroding landscapes: Detection of Transience in Eroding Landscapes, Earth Surf. Proc. Land., 42, 24–41, https://doi.org/10.1002/esp.3923, 2017.
Mudd, S. M. and Furbish, D. J.: Lateral migration of hillcrests in response to channel incision in soil-mantled landscapes, J. Geophys. Res., 110, F04026, https://doi.org/10.1029/2005JF000313, 2005.
Mudd, S. M. and Furbish, D. J.: Responses of soil-mantled hillslopes to transient channel incision rates, J. Geophys. Res., 112, F03S18, https://doi.org/10.1029/2006JF000516, 2007.
Neely, A. B., DiBiase, R. A., Corbett, L. B., Bierman, P. R., and Caffee, M. W.: Bedrock fracture density controls on hillslope erodibility in steep, rocky landscapes with patchy soil cover, southern California, USA, Earth Planet. Sc. Lett., 522, 186–197, https://doi.org/10.1016/j.epsl.2019.06.011, 2019.
Oregon Lidar Consortium and Oregon Department of Geology and Mineral Industries: available at: https://www.oregongeology.org/lidar/, last access: 14 September 2021.
Ouimet, W. B., Whipple, K. X., and Granger, D. E.: Beyond threshold hillslopes: Channel adjustment to base-level fall in tectonically active mountain ranges, Geology, 37, 579–582, https://doi.org/10.1130/G30013A.1, 2009.
Passalacqua, P., Do Trung, T., Foufoula-Georgiou, E., Sapiro, G., and Dietrich, W. E.: A geometric framework for channel network extraction from lidar: Nonlinear diffusion and geodesic paths, J. Geophys. Res., 115, F01002, https://doi.org/10.1029/2009JF001254, 2010.
Pelletier, J. D. and Field, J. P.: Predicting the roughness length of turbulent flows over landscapes with multi-scale microtopography, Earth Surf. Dynam., 4, 391–405, https://doi.org/10.5194/esurf-4-391-2016, 2016.
Penck, W.: Morphological Analysis of Landforms, Macmillan, Indianapolis, Indiana, 1953.
Penserini, B. D., Roering, J. J., and Streig, A.: A morphologic proxy for debris flow erosion with application to the earthquake deformation cycle, Cascadia Subduction Zone, USA, Geomorphology, 282, 150–161, https://doi.org/10.1016/j.geomorph.2017.01.018, 2017.
Perron, J. T. and Royden, L.: An integral approach to bedrock river profile analysis, Earth Surf. Proc. Land., 38, 570–576, https://doi.org/10.1002/esp.3302, 2013.
Perron, J. T., Kirchner, J. W., and Dietrich, W. E.: Spectral signatures of characteristic spatial scales and nonfractal structure in landscapes, J. Geophys. Res., 113, F04003, https://doi.org/10.1029/2007JF000866, 2008.
Personius, S. F.: Late Quaternary stream incision and uplift in the forearc of the Cascadia subduction zone, western Oregon, J. Geophys. Res.-Sol. Ea., 100, 20193–20210, https://doi.org/10.1029/95JB01684, 1995.
PRISM Climate Group: PRISM Climate Group: Oregon State University, Corvallis, OR, USA, available at: https://prism.oregonstate.edu (last access: 14 September 2021), 2016.
Reneau, S. L. and Dietrich, W. E.: Erosion rates in the southern Oregon Coast Range: Evidence for an equilibrium between hillslope erosion and sediment yield, Earth Surf. Proc. Land., 16, 307–322, https://doi.org/10.1002/esp.3290160405, 1991.
Richardson, P. W., Perron, J. T., and Schurr, N. D.: Influences of climate and life on hillslope sediment transport, Geology, 47, 423–426, https://doi.org/10.1130/G45305.1, 2019.
Roberts, G. G. and White, N.: Estimating uplift rate histories from river profiles using African examples, J. Geophys. Res., 115, B02406, https://doi.org/10.1029/2009JB006692, 2010.
Roering, J. J.: How well can hillslope evolution models “explain” topography? Simulating soil transport and production with high-resolution topographic data, Geol. Soc. Am. Bull., 120, 1248–1262, https://doi.org/10.1130/B26283.1, 2008.
Roering, J. J., Kirchner, J. W., and Dietrich, W. E.: Evidence for nonlinear, diffusive sediment transport on hillslopes and implications for landscape morphology, Water Resour. Res., 35, 853–870, https://doi.org/10.1029/1998WR900090, 1999.
Roering, J. J., Kirchner, J. W., and Dietrich, W. E.: Hillslope evolution by nonlinear, slope-dependent transport: Steady state morphology and equilibrium adjustment timescales, J. Geophys. Res., 106, 16499–16513, https://doi.org/10.1139/t01-031, 2001.
Roering, J. J., Kirchner, J. W., and Dietrich, W. E.: Characterizing structural and lithologic controls on deep-seated landsliding: Implications for topographic relief and landscape evolution in the Oregon Coast Range, USA, Geol. Soc. Am. Bull., 117, 654–668, https://doi.org/10.1130/B25567.1, 2005.
Roering, J. J., Perron, J. T., and Kirchner, J. W.: Functional relationships between denudation and hillslope form and relief, Earth Planet. Sc. Lett., 264, 245–258, https://doi.org/10.1016/j.epsl.2007.09.035, 2007.
Roering, J. J., Marshall, J., Booth, A. M., Mort, M., and Jin, Q.: Evidence for biotic controls on topography and soil production, Earth Planet. Sc. Lett., 298, 183–190, https://doi.org/10.1016/j.epsl.2010.07.040, 2010.
Roth, D. L., Doane, T. H., Roering, J. J., Furbish, D. J., and Zettler-Mann, A.: Particle motion on burned and vegetated hillslopes, P. Natl. Acad. Sci. USA, 117, 25335–25343, https://doi.org/10.1073/pnas.1922495117, 2020.
Royden, L. and Perron, J. T.: Solutions of the stream power equation and application to the evolution of river longitudinal profiles, J. Geophys. Res.-Earth, 118, 497–518, https://doi.org/10.1002/jgrf.20031, 2013.
Scherler, D. and Schwanghart, W.: Drainage divide networks – Part 1: Identification and ordering in digital elevation models, Earth Surf. Dynam., 8, 245–259, https://doi.org/10.5194/esurf-8-245-2020, 2020.
Schumm, S. A.: Rates of Surficial Rock Creep on Hillslopes in Western Colorado, Science, 155, 560–562, https://doi.org/10.1126/science.155.3762.560, 1967.
Schwanghart, W. and Scherler, D.: Short Communication: TopoToolbox 2 – MATLAB-based software for topographic analysis and modeling in Earth surface sciences, Earth Surf. Dynam., 2, 1–7, https://doi.org/10.5194/esurf-2-1-2014, 2014 (available at: https://topotoolbox.wordpress.com/download, last access: 14 September 2021).
Stock, J. and Dietrich, W. E.: Valley incision by debris flows: Evidence of a topographic signature, Water Resour. Res., 39, 1089, https://doi.org/10.1029/2001WR001057, 2003.
Strahler, A. N.: Equilibrium theory of erosional slopes approached by frequency distribution analysis; Part 1, Am. J. Sci., 248, 673–696, https://doi.org/10.2475/ajs.248.10.673, 1950.
Struble, W. T.: HilltopCurvature, GitHub [code], available at: https://github.com/wtstruble, last access: 14 September 2021.
Struble, W. T., Roering, J. J., Dorsey, R. J., and Bendick, R.: Characteristic Scales of Drainage Reorganization in Cascadia, Geophys. Res. Lett., 48, e2020GL091413, https://doi.org/10.1029/2020GL091413, 2021.
Sweeney, K. E., Roering, J. J., Almond, P., and Reckling, T.: How steady are steady-state landscapes? Using visible–near-infrared soil spectroscopy to quantify erosional variability, Geology, 40, 807–810, https://doi.org/10.1130/G33167.1, 2012.
Torrence, C. and Compo, G. P.: A Practical Guide to Wavelet Analysis, B. Am. Meteorol. Soc., 79, 61–78, 1998.
Willett, S. D., McCoy, S. W., Perron, J. T., Goren, L., and Chen, C.-Y.: Dynamic Reorganization of River Basins, Science, 343, 1248765–1248765, https://doi.org/10.1126/science.1248765, 2014.
Wobus, C., Whipple, K. X., Kirby, E., Snyder, N., Johnson, J., Spyropolou, K., Crosby, B., and Sheehan, D.: Tectonics from topography: Procedures, promise, and pitfalls, in: Special Paper 398: Tectonics, Climate, and Landscape Evolution, Geological Society of America, 55–74, https://doi.org/10.1130/2006.2398(04), 2006.