the Creative Commons Attribution 4.0 License.
the Creative Commons Attribution 4.0 License.
Size, shape and orientation matter: fast and semiautomatic measurement of grain geometries from 3D point clouds
Philippe Steer
Laure Guerit
Dimitri Lague
Alain Crave
Aurélie Gourdon
The grainscale morphology and size distribution of sediments are important factors controlling the erosion efficiency, sediment transport and the aquatic ecosystem quality. In turn, characterizing the spatial evolution of grain size and shape can help understand the dynamics of erosion and sediment transport in coastal, hillslope and fluvial environments. However, the size distribution of sediments is generally assessed using insufficiently representative field measurements, and determining the grainscale shape of sediments remains a real challenge in geomorphology. Here we determine the size distribution and grainscale shape of sediments located in coastal and river environments with a new methodology based on the segmentation and geometric fitting of 3D point clouds. Point cloud segmentation of individual grains is performed using a watershed algorithm applied here to 3D point clouds. Once the grains are segmented into several subclouds, each grainscale morphology is determined by fitting a 3D geometrical model applied to each subcloud. If different geometrical models can be tested, this study focuses mostly on ellipsoids to describe the geometry of grains. G3Point is a semiautomatic approach that requires a trialanderror approach to determine the best combination of parameter values. Validation of the results is performed either by comparing the obtained size distribution to independent measurements (e.g., hand measurements) or by visually inspecting the quality of the segmented grains. The main benefits of this semiautomatic and nondestructive method are that it provides access to (1) an unbiased estimate of surface grainsize distribution on a large range of scales, from centimeters to meters; (2) a very large number of data, mostly limited by the number of grains in the point cloud data set; (3) the 3D morphology of grains, in turn allowing the development of new metrics that characterize the size and shape of grains; and (4) the in situ orientation and organization of grains. The main limit of this method is that it is only able to detect grains with a characteristic size significantly greater than the resolution of the point cloud.
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Rock particles or grains are characterized by a large range of size, from clays to large boulders, and a diverse variety of shape and angularity, from spherical or ellipsoidal to cubic or polyhedral (e.g., Blott and Pye, 2008; Domokos et al., 2014; 2020). Grains form initially by fragmentation or chemical weathering, transforming a cohesive rock mass into a granular material. The initial size or shape distributions are controlled by fragmentation, weathering processes and structure of the rock mass (e.g., fracture density and orientation, mineral size) (e.g., Molnar et al., 2007; Garzanti et al., 2008; Sklar et al., 2017; DiBiase et al., 2018; Neely and DiBiase, 2020; Verdian et al., 2021). These initial distributions then evolve due to the action of geomorphological processes, including attrition, chipping, abrasion, fragmentation, chemical weathering and transport of grains by wind, river flow, avalanches along hillslopes, and sea waves and currents (e.g., Attal and Lavé, 2006; 2009; Domokos et al., 2014; Miller et al., 2014; Várkonyi et al., 2016; NovákSzabó et al., 2018; Marc et al., 2021). Grains are also found at the surface of other planetary bodies or asteroids (Burke et al., 2021) and offer unique constraints on their surface conditions. A striking example is the use of the shape of grains to reconstruct the transport history of pebbles on Mars (Szabo et al., 2015). Moreover, the in situ orientation of grains found in deposits can also provide information on the paleoflow conditions during sediment deposition (e.g., Johansson, 1963; Rust, 1972).
The distributions of grain size, shape and orientation impact the dynamics of fluvial and sedimentary environments. At the scale of rivers, the size of the sediments strongly controls the mobility of alluvial grains and their incipient threshold of motion (e.g., Shields, 1936), the timescale required to mobilize landslidedriven sediments (e.g., Croissant et al., 2017), the rate of river bedrock incision through the toolandcover effect (Sklar and Dietrich, 2004), the width of river channels (e.g., Finnegan et al., 2007; Baynes et al., 2020), and the rate of knickpoint propagation (Cook et al., 2013). At the scale of a sedimentary basin, the size of grains influences the stratigraphy of the basin together with the chemical and mechanical properties of the sediment (e.g., Armitage et al., 2011). Grain size, shape and orientation in riverbeds are also key factors for aquatic habitats (e.g., Kondolf and Wolman, 1993; Riebe et al., 2014), for water and nutrient exchange through the hyporheic zone (e.g., Tonina and Buffington, 2009), and even for river hydraulics by impacting basal friction (e.g., Hodge et al., 2009).
Despite the ubiquitous role of grain geometry on landscape properties and dynamics, and its potential to constrain paleoconditions on Earth and other planetary bodies, robustly documenting the 3D geometry of grains and their statistical distributions in natural environments remains a challenge. Sampling the grainsize distribution of the sediments lying at the surface of a riverbed is often done by the gridbynumber method (Wolman, 1954). This method measures the diameter of a predefined number of grains, generally greater than 100. The gridbynumber method is simple to implement and is regarded as directly similar to a volumetric sampling (see Bunte and Abt, 2001; and references therein). It is therefore widely used in the field (e.g., D'Arcy et al., 2017; Guerit et al., 2014; 2018; Chen et al., 2018; RodaBodula et al., 2018; Watkins et al., 2020; Baynes et al., 2020). However, samples are often taken over a few square meters and thus lead to inherent representativeness and statistical biases associated with the operator, the grain sampling strategy, the measurements themselves and with the choice of the diameter to be measured. Collecting a data set can be extremely timeconsuming, especially when many grains have to be measured to be statistically significant (Rice and Church, 1996; Green, 2003; Eaton et al., 2019; Purinton and Bookhagen, 2021). Measurements are also partly destructive (i.e., grains are moved), which generally leads to information being lost on grain orientation and exact location.
These issues have led to the development of alternative methods based on image analysis to characterize large areas in a manageable amount of time. Objectbased and statistically based approaches have been developed to characterize grainsize distributions from pictures or 3D data. The first approach (the socalled “photo sieving”) measures each grain or a number of selected grains on a picture (e.g., Bunte and Abt, 2001). Several algorithms now exist to perform these measurements manually on an image (Roduit, 2008). Because this manual procedure can be timeconsuming, (semi)automatic procedures have been implemented to recognize grains from pictures (Butler et al., 2001; Graham et al., 2005a, b; Detert and Weitbrecht, 2012; Buscombe et al., 2013; Langhammer et al., 2017; Carbonneau et al., 2018; Purinton and Bookhagen, 2019) Machine learning approaches are being developed to support grain segmentation for images (Soloy et al., 2020). However, these methods are still timeconsuming as they require the manual labeling of a large number of grains. The second approach is based on imagetexture analyses and aims to correlate some statistical properties of images with grain sizes of the study site (Buscombe and Masselink, 2009; Buscombe et al., 2010; Rubin, 2004; Carbonneau et al., 2004). Similarly, 3D approaches empirically relating bed roughness measured on highresolution topographic data can be implemented to infer the grainsize distribution from locally calibrated relationships (e.g., Rychkov et al., 2012; Westoby et al., 2015; Woodget and Austrums, 2017; VazquezTarrio et al., 2017; Pearson et al., 2017; Groom et al., 2018; Detert et al., 2018). These approaches considerably reduce the time spent in the field, efficiently increase the sampling density and coverage, and are nondestructive. Yet, postprocessing remains timeconsuming, and these methods are inherently limited to the 2D measurement of the apparent axis of individual grains (Graham et al., 2010) or to empirical local correlations with little generalization capability and limited potential to fully explore the 3D geometry of individual grains.
The last decade has seen a steep growth in the use of highresolution 3D topographic data in Earth Sciences and geomorphology, obtained by lidar measurements and photogrammetry (e.g., Schneider et al., 2015; Westoby et al., 2012; Leduc et al., 2019). The resulting 3D point clouds offer unprecedented access to landscape heterogeneities and to landscape temporal evolution (e.g., Hodge et al., 2009; Leyland et al., 2017; Beer et al., 2017; Bernard et al., 2021). The accessibility of 3D point clouds, obtained from terrestrial, drone and airborne data, and their ability to capture object geometries robustly and accurately in 3D at various scales represent a timely opportunity to develop pointcloudbased methods for the issue of grainsize measurement. Building on this opportunity, Chen et al. (2020) recently developed a deeplearning workflow to segment grains based on structurefrommotion (SfM) data. Walicka and Pfeifer (2022) also successfully applied a DBSCAN (densitybased spatial clustering of applications with noise, see Ester et al., 1996) algorithm to segment grains.
In this paper, we develop another efficient and semiautomatic approach, entitled G3Point (standing for “Granulometry from 3D Point clouds”), to measure grain size, shape and orientation using 3D point clouds. G3Point is a purely geometric algorithm, which in turn does not rely on the a priori training of a neural network on thousands or more grains which is required in Chen et al. (2020). Indeed, the associated workflow consists of the 3D segmentation of individual grains using a type of watershed algorithm, the geometrical description of individual grains using 3D ellipsoidal models, and the description of the 3D geometry of the grain population using statistical distributions. G3Point can be characterized as a semiautomatic approach as it is based on several parameters which can be optimized by a trialanderror approach. Moreover, validation of the obtained results is performed either by comparing the obtained size distribution to independent measurements (e.g., hand measurements) or by visually inspecting the quality of the segmented grains. After describing the new method, we test it against lab and natural controlled experiments (e.g., riverbeds and beaches), considering point clouds obtained from SfM, to check its ability to robustly capture the 3D geometry and size of grains, independently constrained by hand measurements.
G3Point is a Matlab program which aims at measuring the size, shape and orientation of a large number of individual grains as detected from 3D point clouds describing the topography of surfaces covered by sediments. The main functions of G3Point are described in the following and Fig. 1. Compared to 2D digital elevation models (DEMs), where elevation z is defined as a function of the horizontal coordinates (x, y), 3D point clouds can include several points located at the same horizontal position (e.g., the face above and below a grain), allowing a better description of geomorphological features such as grains. In the following, we assume that the considered point cloud is already denoised and cleaned of any geometrical feature not corresponding to pebbles. These features include trees, trunks, vegetation, the water surface, humanmade objects and patches of fine grains (i.e., smaller than the minimal detected grain size). Several efficient algorithms are available to perform the denoising task (e.g., Lague and Brodu, 2013). We also assume that the point cloud surface, over the region of interest (i.e., generally an area of a few tens of square meters, what we later refer to as the “patch scale”), is relatively planar with its normal oriented vertically upward. We provide functions to denoise and reorient the point cloud accordingly. We also assume that in most cases vertically stacked rocks cannot be individually segmented.
To illustrate the method, we apply it to a point cloud of an active alluvial riverbed, of an area of ∼40 m^{2}, acquired in 2011 with a terrestrial lidar scanner (Leica ScanStation 2) along the Otira River in New Zealand (Fig. 2) and already featured in Brodu and Lague (2012). The subset of this point cloud that we use in the following is made of ∼10^{5} points with an average point density of ∼2.410^{3} pt m^{−2} and was obtained after a single scan (Fig. 2a). Because it was acquired after a single scan and therefore misses a significant surface area for each visible grain, this point cloud is not optimal to obtain robust information on grain size. However, it represents a valuable test to check the ability of G3Point.
2.1 Initial segmentation: from a global point cloud to individual grains using a watershed algorithm
The segmentation of the point clouds into subpoint clouds representing individual grains uses a single flow algorithm based on the steepest slope criterion (O'Callaghan and Mark, 1984). This algorithm is generally used to route water and identify watersheds on 2D DEMs. It uses the steepest slope criterion to route water between neighborhood points until reaching a local topographic minimum, which corresponds to the outlet of the watershed. Each watershed is therefore described by a directed acyclic graph which associates each point of the point cloud with its outlet node through a single flow path (e.g., Schwanghart and Scherler, 2014). To perform the watershed segmentation, we use the Fastscape algorithm as it offers a fast solution to order points along the steepest water flow path (Braun and Willett, 2013). For each node i, Fastscape defines a receiver node, corresponding to the neighborhood node leading to the steepest slope (i.e., that therefore would receive water when defining a flow topology), and donor nodes, corresponding to neighborhood nodes that give water to node i. Starting from each outlet node, a stack of nodes is built by recursively adding the donor nodes to the stack until reaching nodes without donors. The list of nodes in each stack therefore defines a watershed associated with one outlet node. This algorithm, designed for regular grids, can be readily adapted to irregular grids, such as 3D point clouds, as long as the neighborhood nodes of each node are known. We use here the knearest neighbors algorithm, using 3D Euclidean distances, to identify the neighborhood nodes. The parameter k controls the “neighborhood scale”, which varies locally based on the spatial density of points (Fig. A1a). For the point cloud of the Otira River, k was taken as equal to 20 as this provides a good solution to grain segmentation. We provide some guidelines on how to choose a suitable value of k in the Supplement (Fig. S1).
To identify grains instead of watersheds, the single flow algorithm is modified by using the criterion of the steepest slope upward instead of the steepest slope downward to route water. In other words, water is routed from a point to its steepest upward neighbor, which is associated with the maximum value of $\mathrm{\Delta}z\left./{\left(\mathrm{\Delta}{x}^{\mathrm{2}}+\mathrm{\Delta}{y}^{\mathrm{2}}\right)}^{\mathrm{1}/\mathrm{2}}\right)$, with Δx, Δy and Δz the distance along x, y and z between the considered point and its knearest neighbors. Using this approach, each grain should be identified by a single watershed, with the outlet corresponding to the summit of the grain. For the Otira River, the initial segmentation identifies 772 grains (Fig. 2b), and their set of points are associated with a unique label. This segmentation approach is relatively simple to implement, and the topology of a grain can be simplified to the position of its summit (red dots in Fig. 2b). Moreover, this segmentation method is fast as it takes ∼0.1 or ∼1 s of CPU time for ∼10^{5} or ∼10^{6} points, respectively, on a laptop with 32 GB of RAM and an Intel i9 CPU of eight cores with a clock speed of 2.4 GHz. We emphasize that this algorithm is not intended to provide an accurate description of hydrological flow over a point cloud as in Rheinwalt et al. (2019) but simply to provide a fast segmentation of the point cloud. This algorithm only imposes one spatial scale: the theoretical minimum grain diameter which can be segmented, i.e., the local neighborhood scale. This scale can lead to undersegmentation of small grains, when their number of points is lower than or of the same order as the k parameter. Except for the neighborhood scale, no other scale is introduced, and the algorithm can identify grains of varying size. However, results show that this watershed segmentation approach also leads to a global oversegmentation of grains. Indeed, grains can exhibit several local maxima, due to the geometry of the grain (i.e., angularity) or to a rough surface or to potential data noise, leading to a grain being oversegmented (Fig. 2b). Oversegmentation is a classical issue for algorithms dedicated to grain segmentation in 2D (e.g., Purinton et al., 2019; Purinton and Bookhagen, 2021) or 3D.
2.2 Correcting from oversegmentation by merging grains
Correcting oversegmentation is not a trivial task due to the large range of grain sizes. Mostly because of this issue, classical clustering approaches such as hierarchical clustering or DBSCAN (e.g., Esther et al., 1996) proved ineffective to solving this issue. Moreover, approaches that use all the points in the point cloud can lead to a longer computational time, which might become prohibitive for large point clouds. Here, we develop an approach which makes use of the properties of the segmented watersheds, which associate grains (i.e., watersheds) to their unique summit points (i.e., outlets) and to their border nodes (i.e., crests). We combine three criteria (Fig. A1b) to decide if a pair of grains (ij) should be merged into a single grain.

Criterion 1: the distance d_{ij} between two summit points should be smaller than the sum of the characteristic radius of the two grains. Using a criterion based on a single scale to decide whether two grains should be merged would be problematic due to the large range of grain size. We therefore use the drainage area A at the summit node (i.e., outlet), which receives water from all the points sharing the same label, to determine a characteristic scale or grain radius ${l}_{i}={\left({A}_{i}\left(\right)open="/">\mathit{\pi}\right)}^{}\mathrm{1}/\mathrm{2}$. The criterion to merge the pair of grains (ij) together is therefore d_{ij}<C_{F}(l_{i}+l_{j}), with C_{F} a factor that we take generally to be equal to 0.5–1. These values were obtained after several trialanderror tests.

Criterion 2: grains i and j should be neighbors (i.e., at least one of the points of grain i belongs to the k neighbors of one point of grain j and vice versa).

Criterion 3: the 3D angle between the normals of the crest points of grains i and j should be small. Orientation of the normal is computed by taking the normal of the bestfitting local plane to the knearest neighbors of the considered point. For each of the crest nodes of grain i, the sum of the 3D angle between its normal and the normal of its neighbors belonging to grain j is computed. This operation is performed for every crest point of grains i and j, and then a mean 3D angle is determined. The criterion to merge the grains is that their mean 3D angle is lower than a threshold α that we take as equal to 60^{∘} for the point cloud of the Otira River. This last criterion prevents grains that are separated by a clear change in surface orientation from being merged.
A pair of grains (ij) is merged if, and only if, these three criteria are respected. Due to the low number of grains compared to the number of points in the point cloud, this step is also fast (i.e., $\sim \mathrm{0.1}\mathrm{1}$ or $\sim \mathrm{1}\mathrm{10}$ s of CPU time on a laptop for ∼10^{5} or ∼10^{6} points, respectively). The results show that many labels, suffering from oversegmentation and describing a single grain, were effectively merged by applying this test, leaving only 657 labels or grains instead of 772 (Fig. 2c). Overall, the resulting segmentation looks qualitatively good, even if some grains still suffer from oversegmentation while a limited number of labels now suffer from undersegmentation and include more than one grain. We provide some guidelines on how to choose suitable values of C_{F} and α in the Supplement (Fig. S2).
2.3 Segmentation cleaning operations
To increase the quality of the segmentation, we offer optional routines to perform several postsegmentation operations (Fig. A1c):

applying Criterion 3 only, which merges a pair of grains if the 3D angle between their normal, computed on the common border, is lower than a threshold β. The objective is mostly to merge small grains, resulting from the initial oversegmentation due to grain local maxima, with large ones.

cleaning the segmentation by removing grains with less than n_{min} points. This number of points should be greater than or equal to k, the number of nearest neighbors, and greater than or equal to 10, regarded as the strict minimum number of points required to fit an ellipsoid (i.e., number of parameters of an ellipsoid). However, larger values of n_{min} should be favored to reduce the uncertainty in the resulting ellipsoidal model.

removing flattish or overelongated grains, as they generally do not correspond to individual grains but to clusters of fine grains with a characteristic size much lower than the typical point spacing of classical point clouds or to improperly segmented grains. To detect flattish or overelongated grains, we perform a singular value decomposition (SVD) over the 3D coordinates of each of the subpoint clouds. If a grain has a minimum or an intermediate singular value divided by its maximum singular value (i.e., the axis ratio between the intermediate or minimum dimension of the 3D labeled point cloud and its maximum dimension) lower than a threshold, ∅_{flat} or 2∅_{flat}, then this grain is considered flattish or overelongated, respectively, and removed from the segmentation. Values of ∅_{flat}<0.1 were found to be suitable in this study, even if natural settings with very flat (e.g., as found for slate grains) or elongated grains should probably consider smaller values.
In the example shown in Fig. 2, the segmentation was not cleaned. We provide some guidelines on how to choose suitable values of β, n_{min} and ∅_{flat} in the Supplement (Fig. S3).
2.4 Geometrical modeling: 3D ellipsoidal fitting of grains
Once the grains are segmented and labeled, the following phase consists of the 3D geometrical description of each grain, particularly their size and orientation. A strong constraint results from the fact that only an unknown fraction of the upper surface of the segmented grains (i.e., the visible part of the grain) is topographically described by the point cloud. This prevents us from directly using the point cloud to describe each grain and measure their sizes and orientations. Instead, we rely on geometrical models to represent each grain. The simplest 3D geometrical model to describe a grain is the ellipsoidal model. Two strategies are adopted to describe the geometry of a grain with an ellipsoidal model: fitting an ellipsoid or determining its ellipsoid of inertia.
Fitting an ellipsoid to a set of points in 3D is a complex problem that has received attention from different applied mathematics communities, including computer vision, pattern recognition, numerical analysis and statistics. Ellipsoids belong to the family of quadric surfaces that can be defined as
where A, B, C, F, G, H, P, Q, R and D are the parameters of the quadric surface. Defining $I=A+B+C$ and $J=\mathrm{AB}+\mathrm{BC}+\mathrm{AC}{F}^{\mathrm{2}}{G}^{\mathrm{2}}{H}^{\mathrm{2}}$, it can be shown that Eq. (1) must represent an ellipsoid when $\mathrm{4}J{I}^{\mathrm{2}}>\mathrm{0}$ (Li and Griffiths, 2004). This condition is respected when the short radius is at least half the length of the major radius of an ellipsoid. This represents a sufficient condition, but not a necessary one, and ellipsoids can be mathematically defined without respecting $\mathrm{4}J{I}^{\mathrm{2}}>\mathrm{0}$. We use an efficient and robust Matlab version (Hunyadi, 2022) of a direct leastsquare fitting method (Li and Griffiths, 2004), based on the condition that $\mathrm{4}J{I}^{\mathrm{2}}>\mathrm{0}$, to describe the geometry of the segmented grains by minimizing the square of the distance between labeled points and the ellipsoidal model. For ellipsoids fitting grains which do not satisfy this condition, the fitting method might still lead to ellipsoids or to other quadric surfaces. Grains suffering from fitting issues or leading to quadric surfaces other than an ellipsoid are filtered out, leaving 630 correctly fit ellipsoids over 657 labeled grains. The resulting ellipsoids, fitted to each labeled grain, appear qualitatively consistent with the shape, size and orientation of the labeled grains (Fig. 2d). Other ellipsoidal fitting algorithms exist, but this direct leastsquare approach was found to lead to the best solution for the data set we used. In turn, the condition $\mathrm{4}J{I}^{\mathrm{2}}>\mathrm{0}$ prevents the occurrence of flat or overelongated ellipsoids, which could otherwise represent better mathematical solutions despite being, in some cases, physically unlikely.
The second approach considered to characterize the geometry of the grains computes the inertia ellipsoids corresponding to the labeled points of the grains. This is performed first by computing the mean position of the points, second by computing the covariance matrix of the points subtracted from their mean position and third by making an SVD of the covariance matrix normalized by the number of points.
The approach based on the inertia ellipsoid can be considered simpler than the direct leastsquare fitting method and does not suffer from mathematical constraints of the direct leastsquare approach. However, as it is not a fitting method, its main drawback is that it is unable to guess the “hidden” geometry of the grains (i.e., by using the curvature of the visible part of the grain), and the obtained inertia ellipsoids will tend to be flatter than the grains. We later compare the two approaches in the Results section. We also compare the obtained ellipsoids to cuboids that are obtained by determining the minimal 3D bounding box for each grain, with at least one side oriented along the horizontal plan. More specifically, the orientation and dimensions (i.e., length, width and height) of the cuboids are compared to the orientation and dimensions of the major, intermediate and short axes of the ellipsoids.
2.5 Geometrical and statistical description of grain size, shape and orientation
Once the grains are fitted by an ellipsoid, it is straightforward to access their geometrical information. For each ellipsoid, we measure the radius (and the diameter, as classically used for grainsize distributions) of the major a, intermediate b and short c axes, the orientation (i.e., azimuth and dip) of these three axes, the volume of the ellipsoid $V=\mathrm{4}/\mathrm{3}\mathit{\pi}abc$, and the approximate surface area A of the ellipsoid using Knud Thomsen's formula $A=\mathrm{4}\mathit{\pi}{\left(\left({a}^{p}{b}^{p}+{a}^{p}{c}^{p}+{b}^{p}{c}^{p}\right)/\mathrm{3}\right)}^{\mathrm{1}/p}$. Indeed, there is no general formula for estimating A and this formula approximates the ellipsoid area with an error of less than 1.061 % when p=1.6705. We can also compute two different axis ratios, with $c/a$ the 3D axis ratio between the short and major axis and $b/a$ the 2D axis ratio (or elongation ratio) between the intermediate and the major axis. We coin this latter the 2D axis ratio as it generally corresponds to the axis ratio measured from 2D images, by contrast with the 3D axis ratio that is generally not measurable from 2D images (i.e., assuming that the short axis is oriented vertically).
For each grain, we can also compute the distance of each point of the grain, of coordinates (xyz), to its projection on the ellipsoid surface, of coordinates (x_{e}y_{e}z_{e}). The square of this distance, corresponding to the residuals in a leastsquare sense, characterizes the goodness of the fit through the coefficient of determination:
with $\overline{x},\overline{y},\overline{z}$, and the mean coordinates of the points. R^{2} provides information on the quality of the mathematical fit itself and on the consistency between the ellipsoidal model and the shape of the grain, which can deviate significantly from an ellipsoidal geometry.
The statistical description of grain geometrical properties of a grain population, such as the classical 1D grainsize distribution (GSD), is then performed based on the geometrical attributes of each individual grain of the considered population (Fig. 3). The range of measured diameters, ∼0.01 to ∼1 m, spans 2 orders of magnitude (Fig. 3a–c), and the 3D ($c/a$) and 2D ($b/a$) axis ratios unsurprisingly vary between 0 and 1 with mean values of 0.55 and 0.65, respectively (Fig. 3d–e). The range of volume of the ellipsoids spans almost 5 orders of magnitude, from 10^{−5} to 1 m^{3} (Fig. 3f). In addition to this classic description, G3Point also provides information on the 3D organization of the grains. Here, the orientation distribution of the grains along this active alluvial bed shows that there is no preferential orientation of grains due to the river flow, as they appear to follow a mostly uniform distribution of the azimuth φ (Fig. 3g), and, as testified by their dip angle θ, that most grains are lying in a subhorizontal position with $\mathrm{0}<\mathit{\theta}<\mathrm{30}$ or $\mathrm{150}<\mathit{\theta}<\mathrm{180}{}^{\circ}$ (Fig. 3h).
In addition to its robustness and efficiency, an algorithm dedicated to extract granulometric information from point clouds must be able to manage various sources of data, including SfM and lidar. In the following, we therefore test the newly developed algorithm against “ground truth” data sets of grain size, obtained in the lab or natural environments. For each data set, we compare the distribution obtained with G3Point to the grainsize distribution measured by hand. It is important to highlight that the grain sampling approach of G3Point belongs to the family of areal or areabynumber approaches. We first start by assessing the pros and cons of the different grain fitting approaches by applying them to individual grains of various shapes.
3.1 The influence of grain shape and surface cover on the resulting ellipsoid size and orientation
Two strategies are adopted to describe the geometry of a grain with an ellipsoidal model: fitting an ellipsoid by a direct leastsquare fitting approach (DLSF) or determining its ellipsoid of inertia (IE). We here test the influence of using these two strategies on the quality of the resulting geometrical models, for individual grains, considering a variable surface covered by the point cloud (Fig. 4).
Indeed, in natural environments, grains have a significant proportion of their surface that is not topographically described, as it is hidden under the grain itself, by other grains or features (e.g., vegetation, water), or due to a lack of visibility with respect to the sensor (e.g., lidar station). The tested grains consist of a spherical ball (grain 1), a lowangularity grain (grain 2), an angular grain (grain 3), and an angular, flattish and elongated grain (grain 4). The point clouds representing the surface of these four grains were obtained by SfM using Agisoft Metashape. Each grain was put on a 1 cm radius plastic plate attached to the top of a tripod and about 50 pictures were acquired all around the grain. For each of these point clouds, we generated ellipsoidal models considering only a prescribed percentage of their surface covered by the point cloud, from 10 % to 100 %. Practically, surface cover is varied by first choosing a random seed among the points of the point cloud and then sampling a number of nearest neighbors leading to the sought surface cover of the grain. Ellipsoidal modeling by DLSF and IE is then applied only to this sampled part of the total point cloud. The modeled ellipsoidal volume V_{model} and surface area A_{model} are then compared to the volume V_{true} and surface area A_{true} of the convex hull of the point cloud. The modeled diameters d_{model} of the three axes are compared to the dimensions d_{true} of the bounding box of the point cloud. Last, the 3D angle Δα, between the modeled orientation of the ellipsoid axes and axes of the “true” ellipsoid obtained by considering the entire grain, is computed. For each surface cover, 10 samples are tested, leading to 10 models obtained by the DLSF and IE approaches, allowing us to define a mean value and a standard deviation for each metric.
For the two low angular grains (grains 1 and 2), metrics obtained with DLSF or IE are consistent with the true geometry of the grain even for relatively low surface cover, down to 20 %–30 %. DLSF gives significantly better results than IE, in particular for a surface cover between 20 % and 80 %, which likely represents a common range for most labeled grains. Thanks to grain curvature, the DLSF fitting algorithm also converges towards value for V, A and d which are close to the true values. For the orientation, both approaches are unable to converge towards the true one for the spherical grain (i.e., grain 1), which is not surprising as the orientation of a sphere is not defined. For grain 2, both approaches converge slowly towards the true orientation for a surface cover greater than 50 %–75 %.
For the angular grain (grain 3), the DLSF and IE approaches give similar results. The dimensions are well captured for a surface cover greater than 60 %–70 %. The orientation, in particular of the c axis, converges more rapidly than for lowangularity or spherical grains. For the angular, elongated and flattish grain (grain 4), the IE approach gives better results than the DLSF for the length of the c axis and the volume, while other metrics are relatively similar. Indeed, the algorithm of the DLSF imposes some constraints on the minimum size of the c axis compared to the a axis, which makes it unable to properly capture the 3D dimensions of flattish grains.
These results show that the dimensions of spherical or lowangularity grains are well captured by the IE and DLSF approaches, with this latter giving good results even for a surface cover lower than 50 %, while their orientation is poorly captured for a surface cover lower than ∼75 %. On the other hand, grains that clearly depart from the spherical model, in particular due to their high angularity, need a greater surface cover, around 60 %–70 %, to be properly captured for their dimensions by ellipsoidal models, while their orientations converge more rapidly towards their true value. Flattish grains are better modeled by the IE approach, as the DLSF leads to a large value of the c axis. Last, we note that the orientation of the c axis is generally better captured than the one of the a and b axis, which suggests that the azimuthal orientation of grains is less well resolved than their inclination (assuming that the c axis of grains is subvertical).
3.2 Lab experiment: the test of the pebbles on a flat surface
Here, we apply G3Point to a lab experiment, consisting of 39 black pebbles, bought in a hardware store, lying in a horizontal position over a planar surface of 0.5×0.5 m (Fig. 5a). This lab experiment was photographed using a Nikon D3500 in a 4000×6000 pixel format with about 50 pictures, taken with different angles, to generate a 3D point cloud by SfM. Data were processed with Agisoft Metashape and the resulting point cloud, made of $\sim \mathrm{2}\times {\mathrm{10}}^{\mathrm{5}}$ points, has a native point density of ∼1 point per mm^{−1}. To segment grains, and only grains, the planar surface is removed from the point cloud by removing all the points below a threshold elevation over the vertical coordinate. G3Point is then applied to this point cloud using the couple of parameters k=100 and C_{F}=0.8, after a trialanderror series of tests. Indeed, the 39 pebbles are perfectly detected and labeled as individual grains. Each grain is then described by a cuboid (Fig. 5b) and ellipsoidal models using the direct leastsquare fitting method (DLSF) (Fig. 5c), as previously done, and the inertia ellipsoid (IE) approach (Fig. 5d). We force the vertical dimension of the cuboids to start at the elevation of the planar surface for their lower face, to correctly capture the height of the grains. As the grains are lying flat, the length and the width of the cuboids correspond to the long and intermediate axes of the grains, respectively. The major a, intermediate b and short c axes of the modeled ellipsoids are then compared to the true diameters of the pebbles, which are assumed to be characterized by the length, width and height of the cuboids, respectively. We emphasize here that most of the pebbles used for this test are strongly elongated ($b/a\sim \mathrm{0.5}$) and flat ($c/a\sim \mathrm{0.25}$), which can represent real challenges for most ellipsoidal fitting algorithms. This test should therefore be regarded as an endmember scenario, testing the ability of the approach to properly describe the geometry of grains using ellipsoidal models.
Despite this, the obtained diameters for the a, b and c axes are roughly consistent between the three approaches (Fig. 5e), even if the diameters obtained with the DLSF and IE approaches are systematically higher or lower, respectively, than the cuboid dimensions. The ratios between the ellipsoid diameters and the cuboid lengths for the a and b axis range between 0.8 and 1 for the IE and between 0.8 and 2 for the DLSF (see Fig. S4 in the Supplement). For the c axis, the consistency is less good and the ratio range between 0.4–0.9 and 1.1–9 for the IE and DLSF approaches, respectively. These results reflect the pros and cons of each approach: the DLSF approach leads to larger than expected ellipsoids, due to the geometrical constraint of the fitting algorithm for the c axis, while the IE approach leads to smaller than expected ellipsoids, as only the upper face of the grains is accounted for. This is well illustrated by the difference in the resulting 3D ($c/a$) and 2D ($b/a$) axis ratio. If the 2D axis ratio is relatively consistent between the three approaches (Fig. 5f), the 3D axis ratio of the DLSF ellipsoids (0.4–0.65) is significantly higher than the one of the cuboids (0.1–0.4), except for one grain. By contrast, the 3D axis ratio of the IE ellipsoids is always lower than the one of the cuboids. These discrepancies also lead to a larger or lower volume and area for the DLSF or IE ellipsoids, respectively, compared to the cuboid volume and area (Fig. 5g). We note that the consistency of the DLSF ellipsoids with the cuboids is greatly improved when increasing the 3D axis ratio (i.e., when considering more spherical grains), which limits the role of the geometrical constrain on the quality of the fit ellipsoid. Last, the horizontal orientation of the DLSF or IE ellipsoids, given by the azimuthal angle of the a axis, is relatively consistent with the orientation of the cuboids (Fig. 5g).
Despite a good firstorder accuracy of the considered ellipsoidal models to represent the 3D dimensions of grains, none of these approaches is deemed systematically suitable by itself. The consistency of the ellipsoidal models with the true geometry of the grains depends on the considered geometrical model, on the surface coverage of the grain by the point cloud and on the shape of the grain itself (Fig. 4). In the following, instead of relying on a single ellipsoidal model, we rather assess the geometry and dimensions of grains by using both the DLSF and IE ellipsoidal models. Indeed, considering the size (or size distribution) obtained with the DLSF and IE ellipsoidal models offers an upper and lower bound on the true size (or size distribution) of the grain (or grain population). We also provide a mean size (or size distribution) obtained with these two ellipsoidal models to offer an approximate solution to the true size of the grain (or grain population).
3.3 Field experiments with SfM 3D point clouds
The second experiment consists of pebbles from three natural field sites in France: the beach of Pointe du Château Renard (Brittany) with coarse and angular grains at Site 1 and smaller rounded grains at Site 2 (Fig. 6a–b) and the Hérault River near SaintAndrédeMajencoules (Cévennes) with rounded, fluvially transported pebbles (Fig. 6c). At each site, we sampled the grainsize distribution by the Wolman gridbynumber method (Wolman, 1954). At Site 1 of Pointe du Château Renard, we defined a grid of about 2.5×3 m with nodes every 0.3 m, we measured the three axes of each grain lying under a node, and a total of 76 grains were measured. At Site 2, we stretched two parallel decameters and two operators walked along these lines, picked the two grains lying under each of their hands (random selection) about every meter and measured the three axes of the grains. In total, 529 grains were measured. For the Hérault River, we defined a grid of 2.5×13 m with nodes every 0.4 m and we measured the intermediate axis of 197 grains. The others diameters were not measured due to time constraints. Measurements were performed with a calliper and rounded toward the nearest millimeter or with a decameter and rounded toward the nearest 5 mm, for small or large grains, respectively. Only grains larger than 4 mm were measured.
In addition to operator errors, related to the measurement itself and to the choice of the diameter to measure, the resulting distribution is associated with uncertainties related to the size of the sample. We used a bootstrap approach with replacement to evaluate the confidence interval of each distribution (Rice and Church, 1996; Bunte and Abt, 2001; Green, 2003). For each sample, we randomly sampled 10 000 replicates of the distribution, and the scatter defines the confidence interval. The pebbles at Site 1 of the beach of Pointe du Château Renard have a median a axis of 170±48 mm, a median b axis of 110±40 mm and a median c axis of 60±20 mm (Fig. 6a, Table S1 in the Supplement). At Site 2, the pebbles have a median a axis of 117±15 mm, a median b axis of 80±9 mm and a median c axis of 50±6 mm (Fig. 6b, Table S1). The fluvial pebbles along the Hérault River are smaller, with a median b axis of 75±18 mm (Fig. 6c, Table S1).
At Château Renard, we used a Nikon D3500 in a 4000×6000 pixel format, and for the Hérault River, we used a Nikon D7500 in a 4176×2784 pixel format. At each site, we took about 100 pictures covering a few square meters to build a 3D point cloud by SfM. Data were processed with Agisoft Metashape and the resulting point clouds have a native point density of ∼1 point per mm^{−1}. We subsampled the point clouds with CloudCompare to ∼ one point per 2 to 3 mm to reduce calculation duration. G3Point is then applied to the resulting point clouds with parameters defined after a trialanderror series of tests so that the segmentation of the grains is visually satisfying (Table 1, Fig. 6).
A large number of grains are detected (428, 1077 and 678 for Château Renard Site 1, Site 2 and the Hérault River, respectively, Table 1). Yet, to compare the distributions obtained by G3Point to the distributions obtained by Wolman counts in the field, we must perform virtual Wolman samplings on the fitted grains. We apply a virtual grid to the 3D point cloud and automatically extract the three axes of the grains lying under the nodes, with grid spacing defined as half the maximum b axis (this roughly corresponds to the D90). Because we can easily resample the point cloud, we repeat this operation 25 times and define the grainsize distribution as the average of these 25 samples, for each fitting method. The DLSF and IE distributions are used as the confidence interval of the average distribution (see Method section). We now have 77, 332 and 183 grains for Château Renard Site 1, Site 2 and the Hérault River, respectively (Table 1). The confidence intervals of the a and b axis are up to ±14 %, but we observe intervals close to ±50 % for the c axis due to the assumptions made by the fitting methods for the c axis (Table S1, and see the Method section for details).
To better compare the two approaches, we compare the key percentiles (10th, 16th, 25th, 50th, 75th, 84th, 90th) of the grainsize distributions obtained by manual counts and by virtual Wolman on the segmented point cloud (Fig. 7). For each diameter at each study site, points align along a 1:1 line in a quantile–quantile diagram, indicating that the average distributions obtained with G3Point are similar to the ones obtained by manual counts (Fig. 7). In particular, the 50th percentiles (i.e., the D50s of the distributions) fall very close on the 1:1 line of the Q–Q plots, implying that G3Point leads to similar median diameters for any grain axis. As observed with the previous examples, the DLSF and the IE approaches perform similarly well on the a and b axis but they tend to overestimate and underestimate the c axis, respectively (Fig. S5). Other diameters are within uncertainties but must be considered with more care (Fig. 7, Table S1). In fact, at Site 1, G3Point tends to underestimates the smallest percentiles of the distributions and to overestimate the coarsest ones (Fig. 7a–c). Yet, this discrepancy is limited and always within the error bars of manual counts. For example, for the a axis, the D90 measured on the field is 304±135 mm, while it is 334±46 mm with G3Point (overestimation by ∼10 %, Fig. 7a). We observe the opposite trend at Site 2 and for the Hérault River, with an overestimation of the smallest percentiles and an overestimation of the coarsest ones (Fig. 7d–f). Here again, this trend is quite limited as, for example, the D10 of the b axis at Site 2 is 38±6 mm from manual counts and 43±3 mm with G3Point (overestimation of ∼13 %). The algorithm is unable to recover small grains because they are described by a limited number of points. As a consequence, the worst performance of G3Point is observed for the small percentiles of the c axis. For example, at Site 2, the D10 of the c axis is overestimated by ∼35 % (Fig. 7f, Table S1).
This second experiment based on natural grains thus confirms that G3Point is efficient at recovering Wolmanlike grainsize distributions for pebble and cobble populations in different environments and for various grain angularity, with a limited temporal cost in the field and in the lab.
4.1 Practical considerations for using G3Point
As already demonstrated, G3Point is designed to perform semiautomatic 3D granulometric measurements on point clouds over surface area 1: 100 m^{2} (hereinafter referred to the patch scale) with a typical point density of $\sim \mathrm{0.1}\mathrm{1}$ cm per point and a total number of points around 10^{6}. The point density should be high enough so that each grain is described by at least several dozen points. This scale enables us (1) to perform efficient and fast measurements (i.e., several seconds), (2) to visually check the quality of the resulting segmentation of the grains, and (3), if needed, to compare the resulting grainsize distribution with the one obtained with manual counting. We therefore suggest using G3Point mostly for patchscale studies. In terms of computational time, there is a tradeoff between the total surface area and point density. G3Point can also perform grain size, shape and orientation analysis over larger study areas (>100 m^{2}). In this case, the best practice consists either (1) in decreasing point density and in turn losing the ability to detect smaller grains or (2) in segmenting the initial point cloud into several subpoint clouds, at the patchscale and with the initial point density, which can then be successively processed by G3Point. We generally recommend validating the results against some field measurements (e.g., grainsize distribution obtained by a Wolman count), at least on some parts of the studied area. When no classical grainsize data are available, we recommend carefully checking the results of the grain segmentation phase and testing its sensitivity to the different parameters of G3Point. For instance, this could be the case for the measurement of grain size and shape on other planetary bodies (Szabo et al., 2015; Lauretta et al., 2019; Burke et al., 2021) or in inaccessible and remote areas. The outcomes of G3Point are tightly linked to the choice of the local neighborhood scale through the parameter k. This parameter should therefore be taken as small as possible to enable the segmentation of small grains but not too small to prevent the oversegmentation of large grains due to local topographic minima associated with surface roughness or noise. Suitable values of k are generally determined by a trialanderror series of tests (Fig. S1).
4.2 SfM or lidarderived point clouds?
As demonstrated in this paper, G3Point can be applied to point clouds obtained with a terrestrial lidar or by SfM. Point clouds obtained with terrestrial lidar data provide better accuracy than SfM but can be associated with varying point density, while the ones obtained by SfM provide uniform point density but can lead to some inaccuracies. In particular, point clouds obtained with SfM were observed to generate smooth or inaccurate topographic transitions between grains, as these correspond to “shadow” areas difficult to capture with pictures. This might be related to the quality of the photos (lighting, blurring, resolution), as with any SfM study. These smooth transitions are not too problematic for G3Point, as it is based on the steepest slope, but they prevent efficiently using a criterion based on topographic curvature to segment grains or to correct the segmentation obtained with G3Point. In that case, we recommend removing points located at local topographic minima to ease segmentation (this is an option provide by G3point). For lidar data, the issue of spatially varying point density can lead to a nonoptimal set of parameters, in particular k, the number of nearest neighbors considered, over the entire surface of the considered point cloud. In this case, we recommend working on subpoint clouds of rather homogeneous spatial point density. The use of point clouds obtained with only one station does not represent an issue for the watershed segmentation of G3Point (Fig. 2), even if it limits the number of data points per grain and their spatial distribution along the surface of the grains, which is not optimal for shape fitting algorithms.
4.3 Comparison of G3Point with previous methods
In terms of total working time, using G3Point over a surface area of about 1–100 m^{2} captured by SfM involves collecting field pictures (∼5–10 min), processing the pictures by SfM to obtain a point cloud (10 min to several hours) and running G3Point several times to find a good parametrization (∼10 min). Interestingly, G3Point itself is not the limiting factor, as field data acquisition (i.e., pictures or lidar data) and data processing (i.e., SfM) appear to be more timeconsuming. The total working time is roughly equivalent to a typical manual pebble count, which takes about 60 min to measure the three axes of 100 grains. However, data sampling for G3Point is not destructive; it can be done by a single operator, and G3Point will result in the measurement of a much larger number of grains for the same sample extension (>10^{2} grains) including their size, location and orientation in 3D. It offers a real benefit in terms of representativeness and opens new avenues to quantitatively characterize populations of grains (e.g., not only their size distribution), based on the geometry on their upper surface. Moreover, because point cloud data acquisition in the field is fast, large areas or multiple locations along a fluvial system can be documented in a limited amount of time. In addition, pictures for SfM can be acquired with drones so that remote locations or very coarsegrained environments can be safely characterized. Together with the large number of grains being considered, G3Point represents a real improvement in terms of spatial representativeness with respect to Wolman or photographic approaches which are usually limited to a few square meters and a few hundreds of grains (Bunte and Abt, 2001). Last, while most methods based on 3D data use texture or any other morphological index to estimate the grain sizes (VazquezTarrio et al., 2017; Woodget et al., 2018; Chardon et al., 2020), G3Point works directly on the grains and does not require a calibration phase. Once again, this limits bias and time spent in the field and allows remote areas to be characterized. G3Point shares some common objectives with the automatic method developed by Walicka and Pfeifer (2022), which directly segments grains from 3D point clouds. It uses a random forest algorithm to classify grains and then a DBSCAN algorithm to segment each grain individually. Compared to Chen et al. (2020), who developed a deep learning approach to segment grains based on 3D point clouds, G3Point does not rely on the a priori training of a neural network on thousands or more grains, which can be highly timeconsuming. Yet, G3Point could represent a good alternative to train deep learning algorithms, as it can provide thousands of grains in a few minutes that otherwise take weeks of work when manually labeled.
4.4 In situ results on the granulometric conversion factors
Because G3Point samples virtually all the grains at the surface, it belongs to the family of areal or areabynumber grain sampling approaches. To compare this distribution to the Wolman field counts, it must be converted to a gridbynumber distribution, which is considered equivalent to a volumetric grainsize distribution. Conversion factors have been proposed to convert grainsize data acquired with one approach to another one, based on geometrical arguments (Kellerhals and Bray, 1971; Church et al., 1987; Diplas and Fripp, 1992). For example, converting an areabynumber (or areal) distribution to a gridbynumber (or volumetric; e.g., Wolman) distribution requires multiplying the frequency of all the particle classes by the factor D^{2}. However, this exponent of 2 is theoretically valid only for spherical sediments with the same density and without porosity. The use of such a conversion factor thus requires a calibration phase and should, in any case, only be regarded as an approximate conversion method (Bunte and Abt, 2001).
With our new approach, we work on 3D point clouds covering large areas, and a large number of grains can be identified. Therefore, instead of converting from an areabynumber to a gridbynumber distribution, we can apply a virtual grid over the point cloud and perform a Wolman count on the fitted grains. To account for the spatial variability of the grains, we repeat this operation 25 times to define an uncertainty envelope and use the average distribution as the grainsize distribution of the sample. For our field examples, we observe that the geometrical conversion is always coarser than the virtual Wolman distribution, yet within uncertainties (Figs. 8, S6, S7, S8). The only exception is for the c axis of the grains with the IE fit. Because this fit leads to very flat ellipsoids, the geometrical conversion factor largely overestimates the size of the grains (Figs. S6, S7, S8). In agreement with previous work (Graham et al., 2010), this suggests that the geometrical factors are a correct approximation that tend to maximize the size of the grains, so that Wolman counts should be favored when possible. We emphasize that the field examples presented above were acquired in order to test our approach and the extent of the point clouds are thus similar to the extent of the Wolman counts performed in the field. Therefore, we sampled approximately the same number of grains in the field and virtually (Table 1). Yet, G3Point is designed to operate on larger point clouds so that a few hundreds of grains will be sampled with the virtual Wolman sampling, allowing for an even more accurate description of the grainsize distribution from point clouds.
4.5 Opportunities to explore and measure uncharted metrics: grain 3D orientation
Here, we briefly present some results on the orientation of grains that we obtain with G3Point. The idea is not to dedicate a detailed study of this metric but to illustrate the ability of G3Point to automatically measure it with no additional efforts. This represents a real benefit of G3Point as most field or picture measurements of grain orientation are either cumbersome or approximate (e.g., using qualitative classification), with the exception of the azimuth angle that can be accessed with approaches based on 2D pictures (e.g., Purinton and Bookhagen, 2019).
The azimuth and dip angles of a grain may give some information about the flow that transported and deposited a population of grains. G3Point offers a very simple way to access the orientation of a large population of grains as the azimuth and dip angles can easily be determined from the fit ellipsoids (Fig. 3). On average, the two fitting methods are efficient at recovering orientation, but they do not lead to the exact same results (Fig. 5g). Therefore, if grain orientation is a key element of a study, preliminary tests may be useful to determine the bestfitting approach in terms of orientation (which may depend for example on the geometry of studied grains). Here, we show the results of both approaches to illustrate their similarity and differences. Azimuth is given with respect to the y axis defined as parallel to the main water flow. At Site 1, the grains show no preferential azimuth (Fig. 9a), and most grains rest flat on the beach, with a dip angle smaller than to 30^{∘} or larger than 150^{∘} (Fig. 9b). However, 40 % to 50 % of the grains exhibit a dip angle between 30 and 150^{∘}. We propose that their orientation results from their fall from the nearby cliffs rather than from transport by the sea. At Site 2, a slightly preferential orientation can be inferred from the DLSF fit, with more grains showing an angle with the main flow than grains aligned with the flow (Fig. 9c). Here again, most grains rest flat and 30 %–40 % of them exhibit a dip angle comprised between 30 and 150^{∘} (Fig. 9d). We propose that this is due to a stronger control of the sea on this site with respect to Site 1. Along the Hérault River, grains tend to orient themselves perpendicular to the main flow (Fig. 9e) and to rest flat, with 27 %–38 % of them with a dip angle comprised between 30 and 150^{∘} (Fig. 9f).
The G3Point algorithm presented here makes progress on the issue of grain segmentation and shape analysis from 3D point cloud data. G3Point represents a methodological alternative to previous granulometric approaches, including hand measurements or 2D image analysis. Its main advantages are (1) its computational efficiency and speed that rely on the use of a stateoftheart watershed algorithm (e.g., Braun and Willett, 2013) to segment grains, (2) its scalefree approach which enables the segmentation of grains with a large range of sizes above the neighborhood scale (i.e., typically a few centimeters), (3) its 3D nature which enables the calculation of metrics (e.g., sphericity, orientation) which are seldom obtained in the field, and (4) its ability to perform a large number of measurements, which favors a good representativeness of the results.
The G3Point algorithm was able to properly describe the size and orientation of grains in a lab experiment. It was also qualitatively successful compared to hand measurements (e.g., Wolman count) in segmenting and quantitatively capturing the size distribution of hundreds to thousands of grains in fluvial and coastal environments. The modeling of grain geometry was performed using ellipsoidal models obtained either with a direct leastsquare fitting approach or by taking the inertia ellipsoid. Both ellipsoid models accurately infer the major and intermediate axes, but the inertia ellipsoids and the direct leastsquare ellipsoids tend to underestimate or overestimate the minor axis, respectively. This in turn impacts the ability of G3Point to infer the volume and surface area of grains. For the minor axis, the mean value of the inertia and direct leastsquare ellipsoids provides estimates that are consistent with hand measurements. Other geometrical models were tested, including bounding boxes. We acknowledge that future work could focus on providing better geometrical models or a better fitting approach to describe the geometry of grains. Alternatively, future efforts could investigate the surface geometry of segmented grains by G3Point, without relying on fitted geometrical models (e.g., ellipsoidal model) but by exploring the topology of the segmented point clouds. An inherent limit remains that, in natural environments, only a fraction of the grain surface is visible and can be topographically described using lidar or SfM.
Fascinating and firstorder issues remain for understanding the shape and size of grains and interpreting them in terms of abrasion and fragmentation processes (Domokos et al., 2014, 2015, 2020; NovákSzabó et al., 2018). This is pivotal for better exploiting the unique geological archives contained in the size, shape and orientation of grains found in natural systems on Earth and other planetary bodies (e.g., Szabo et al., 2015). G3Point, by filling a methodological gap, could foster the development of a more systematic characterization of grain shape in natural environments and lead to a better understanding of the physics of geomorphological processes and of their past dynamics.
A MATLAB version of the algorithm can be accessed through a GitHub and/or a Zenodo repository: https://github.com/philippesteer/G3Point/ (last access: 18 March 2022) and https://doi.org/10.5281/zenodo.6368501 (Steer, 2022).
The data that support the findings of this study are available from the corresponding authors, Philippe Steer and Laure Guerit, upon reasonable request.
The supplement related to this article is available online at: https://doi.org/10.5194/esurf1012112022supplement.
PS and LG wrote the paper. PS initiated this study, developed the numerical algorithm, performed the initial tests and provided funding. LG performed the analysis and tested the algorithm in natural environments. PS, LG, DL, AC and AG acquired field data, motivated the study and contributed to the writing of the paper. All authors checked and revised the text and the figures of the paper and contributed to the ideas developed in this study.
The contact author has declared that none of the authors has any competing interests.
Publisher’s note: Copernicus Publications remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
We thank Thomas Croissant, Edwin Baynes, Benjamin Bruneau, Benjamin Guillaume, Lucas Pelascini and Romy David for their help acquiring data. We thank Edwin Baynes for proofreading the paper. We are grateful to Rebecca Hodge, Benjamin Purinton and an anonymous reviewer for their constructive comments and their work on this paper.
This research has been supported by the H2020 European Research Council (grant agreement no. 803721). We also acknowledge support by Université Rennes 1 and CNRS.
This paper was edited by Rebecca Hodge and reviewed by Benjamin Purinton and one anonymous referee.
Armitage, J. J., Duller, R. A., Whittaker, A. C., and Allen, P. A.: Transformation of tectonic and climatic signals from source to sedimentary archive, Nat. Geosci., 4, 231–235, 2011.
Attal, M. and Lavé, J.: Changes of bedload characteristics along the marsyandi river (central nepal): Implications for understanding hillslope sediment supply, sediment load evolution along fluvial networks, and denudation in active orogenic belts, Geol. Soc. Am. Spec. Pap., 398, 143–171, 2006.
Attal, M. and Lavé, J.: Pebble abrasion during fluvial transport: Experimental results and implications for the evolution of the sediment load along rivers, J. Geophys. Res.Earth Surf., 114, F04023, https://doi.org/10.1029/2009JF001328, 2009.
Baynes, E. R., Lague, D., Steer, P., Bonnet, S., and Illien, L.: Sediment fluxdriven channel geometry adjustment of bedrock and mixed gravel–bedrock rivers, Earth Surf. Proc. Land., 45, 3714–3731, 2020.
Beer, A. R., Turowski, J. M., and Kirchner, J. W.: Spatial patterns of erosion in a bedrock gorge, J. Geophys. Res.Earth Surf., 122, 191–214, 2017.
Bernard, T. G., Lague, D., and Steer, P.: Beyond 2D landslide inventories and their rollover: synoptic 3D inventories and volume from repeat lidar data, Earth Surf. Dynam., 9, 1013–1044, https://doi.org/10.5194/esurf910132021, 2021.
Blott, S. J. and Pye, K.: Particle shape: a review and new methods of characterization and classification, Sedimentology, 55, 31–63, 2008.
Braun, J. and Willett, S. D.: A very efficient O(n), implicit and parallel method to solve the stream power equation governing fluvial incision and landscape evolution, Geomorphology, 180, 170–179, 2013.
Brodu, N. and Lague, D.: 3D terrestrial lidar data classification of complex natural scenes using a multiscale dimensionality criterion: Applications in geomorphology, ISPRS J. Photogramm., 68, 121–134, 2012.
Bunte, K. and Abt, S. R.: Sampling surface and subsurface particlesize distributions in wadable graveland cobblebed streams for analyses in sediment transport, hydraulics, and streambed monitoring, US Department of Agriculture, Forest Service, Rocky Mountain Research Station, https://doi.org/10.2737/RMRSGTR74, 2001.
Burke, K. N., DellaGiustina, D. N., Bennett, C. A., Walsh, K. J., Pajola, M., Bierhaus, E. B., Nolan, M. C., Boynton, W. V., Brodbeck, J. I., Connolly, H. C., Jr., Prasanna Deshapriya, J. D., Dworkin, J. P., Elder, C. M., Golish, D. R., Hoover, R. H., Jawin, E. R., McCoy, T. J., Michel, P., Molaro, J. L., Nolau, J. O., Padilla, J., Rizk, B., Robbins, S. J., Sahr, E. M., Smith, P. H., Stewart, S. J., Susorney, H. C. M., Enos, H. L., and Lauretta, D. S.: Particle sizefrequency distributions of the OSIRISREx candidate sample sites on asteroid (101955) Bennu, Remote Sens., 13, 1315, https://doi.org/10.3390/rs13071315, 2021.
Buscombe, D.: Transferable wavelet method for grainsize distribution from images of sediment surfaces and thin sections, and other natural granular patterns, Sedimentology, 60, 1709–1732, 2013.
Buscombe, D. and Masselink, G.: Grainsize information from the statistical properties of digital images of sediment, Sedimentology, 56, 421–438, 2009.
Buscombe, D., Rubin, D. M., and Warrick, J. A.: A universal approximation of grain size from images of noncohesive sediment, J. Geophys. Res.Earth Surf., 115, F02015, https://doi.org/10.1029/2009JF001477, 2010.
Butler, J., Lande, S., and Chandler, J., Automated extraction of grainsize data from gravel surfaces using digital image processing, J. Hydraul. Res., 39, p. 519–529, https://doi.org/10.1080/00221686.2001.9628276, 2001.
Carbonneau, P. E., Lane, S. N., and Bergeron, N. E.: Catchmentscale mapping of surface grain size in gravel bed rivers using airborne digital imagery, Water resources research, 40, W07202, https://doi.org/10.1029/2003WR002759, 2004.
Carbonneau, P. E., BIzzi, S., and Marchetti, G.: Robotic photosieving from lowcost multirotor sUAS: a proofofconcept, Earth Surf. Proc. Land., 43, 1160–1166, 2018.
Chardon, V., Schmitt, L., Piégay, H., and Lague, D.: Use of terrestrial photosieving and airborne topographic LiDAR to assess bed grain size in large rivers: a study on the Rhine River, Earth Surf. Proc. Land., 45, 2314–2330, 2020.
Chen, C., Guerit, L., Foreman, B. Z., HassenruckGudipati, H. J., Adatte, T., Honegger, L., Perret, M., Sluijs, A., and Castelltort, S.: Estimating regional flood discharge during PalaeoceneEocene global warming, Sci. Rep., 8, 1–8, 2018.
Chen, Z., Scott, T. R., Bearman, S., Anand, H., Keating, D., Scott, C., Arrowsmith, J. R., and Das, J.: Geomorphological analysis using unpiloted aircraft systems, structure from motion, and deep learning. In 2020 IEEE/RSJ International Conference on Intelligent Robots and Systems (IROS), Las Vegas, NV, USA, 24 October 2020–24 January 2021, 1276–1283 pp., https://doi.org/10.1109/IROS45743.2020.9341354, 2020.
Church, M. A., McLean, D. G., and Wolcott, J. F.: River Bed Gravels: Sampling and Analysis, in: Sediments transport in Gravel Bed Rivers, 43–88, John Wiley and Sons, New York, USA, 1987.
Cook, K. L., Turowski, J. M., and Hovius, N.: A demonstration of the importance of bedload transport for fluvial bedrock erosion and knickpoint propagation, Earth Surf. Proc. Land., 38, 683–695, 2013.
Croissant, T., Lague, D., Steer, P., and Davy, P.: Rapid postseismic landslide evacuation boosted by dynamic river width, Nat. Geosci., 10, 680–684, 2017.
D'Arcy, M., Whittaker, A. C., and RodaBoluda, D. C.: Measuring alluvial fan sensitivity to past climate changes using a selfsimilarity approach to grainsize fining, Death Valley, California, USA, Sedimentology, 64, 388–424, 2017.
Detert, M. and Weitbrecht, V.: Automatic object detection to analyze the geometry of gravel grains – a free standalone tool, In River flow, Taylor and Francis Group London, UK, 595–600 pp., ISBN 9780415621298, 2012.
Detert, M., Kadinski, L., and Weitbrecht, V.: On the way to airborne gravelometry based on 3D spatial data derived from images, Int. J. Sediment Res., 33, 84–92, 2018.
DiBiase, R. A., Rossi, M. W., and Neely, A. B.: Fracture density and grain size controls on the relief structure of bedrock landscapes, Geology, 46, 399–402, 2018.
Diplas, P. and Fripp, J. B.: Properties of various sediment sampling procedures, J. Hydraul. Eng., 118, 955–970, 1992.
Domokos, G., Jerolmack, D. J., Sipos, A. Á., and Török, Á.: How river rocks round: resolving the shapesize paradox, 2–4 August 1996, Portland, Oregon, PloS One, 9, e88657, 2014.
Domokos, G., Kun, F., Sipos, A. A., and Szabó, T.: Universality of fragment shapes, Sci. Rep., 5, 1–6, 2015.
Domokos, G., Jerolmack, D. J., Kun, F., and Török, J.: Plato's cube and the natural geometry of fragmentation, P. Natl. Acad. Sci., 117, 18178–18185, 2020.
Eaton, B. C., Moore, R. D., and MacKenzie, L. G.: Percentilebased grain size distribution analysis tools (GSDtools) – estimating confidence limits and hypothesis tests for comparing two samples, Earth Surf. Dynam., 7, 789–806, https://doi.org/10.5194/esurf77892019, 2019.
Ester, M., Kriegel, H. P., Sander, J., and Xu, X.: A densitybased algorithm for discovering clusters in large spatial databases with noise, in: Proceedings of the 2nd International Conference on Knowledge Discovery and Data mining, 226–231, 1996.
Finnegan, N. J., Sklar, L. S., and Fuller, T. K.: Interplay of sediment supply, river incision, and channel morphology revealed by the transient evolution of an experimental bedrock channel, J. Geophys. Res.Earth Surf., 112, F03S11, https://doi.org/10.1029/2006JF000569, 2007.
Garzanti, E., Andò, S., and Vezzoli, G.: Settling equivalence of detrital minerals and grainsize dependence of sediment composition, Earth Planet. Sci. Lett., 273, 138–151, 2008.
Graham, D. J., Rice, S. P., and Reid, I.: A transferable method for the automated grain sizing of river gravels, Water Resour. Res., 41, W07020, https://doi.org/10.1029/2004WR003868, 2005.
Graham, D. J., Reid, I., and Rice, S. P.: Automated sizing of coarsegrained sediments: imageprocessing procedures, Math. Geol., 37, 1–28, 2005.
Graham, D. J., Rollet, A. J., Piégay, H., and Rice, S. P.: Maximizing the accuracy of imagebased surface sediment sampling techniques, Water Resour. Res., 46, W02508, https://doi.org/10.1029/2008WR006940, 2010.
Green, J. C.: The precision of sampling grainsize percentiles using the Wolman method, Earth Surf. Proc. Land., 28, 979–991, 2003.
Groom, J., Bertin, S., and Friedrich, H.: Evaluation of DEM size and grid spacing for fluvial patchscale roughness parameterisation, Geomorphology, 320, 98–110, 2018.
Guerit, L., Barrier, L., Narteau, C., Métivier, F., Liu, Y., Lajeunesse, E., Gayer, E., Meunier, P., Malverti, L., and Ye, B.: The Grainsize Patchiness of Braided GravelBed Streams – example of the Urumqi River (northeast Tian Shan, China), Adv. Geosci., 37, 27–39, https://doi.org/10.5194/adgeo37272014, 2014.
Guerit, L., Barrier, L., Liu, Y., Narteau, C., Lajeunesse, E., Gayer, E., and Métivier, F.: Uniform grainsize distribution in the active layer of a shallow, gravelbedded, braided river (the Urumqi River, China) and implications for paleohydrology, Earth Surf. Dynam., 6, 1011–1021, https://doi.org/10.5194/esurf610112018, 2018.
Hodge, R., Brasington, J., and Richards, K.: Analysing laserscanned digital terrain models of gravel bed surfaces: linking morphology to sediment transport processes and hydraulics, Sedimentology, 56, 2024–2043, 2009.
Hunyadi, L.: Fitting quadratic curves and surfaces, MATLAB Central File Exchange, https://www.mathworks.com/matlabcentral/fileexchange/45356fittingquadraticcurvesandsurfaces, last access: 10 February 2022.
Johansson, C. E.: Orientation of pebbles in running water, A laboratory study, Geografiska Annaler, 45, 85–112, 1963.
Kellerhals, R. and Bray, D. I.: Sampling procedures for coarse fluvial sediments, J. Hydr. Eng. Div., 97, 1165–1180, 1971.
Kondolf, G. M., and Wolman, M. G.: The sizes of salmonid spawning gravels, Water Resour. Res., 29, 2275–2285, 1993.
Lague, D., Brodu, N., and Leroux, J.: Accurate 3D comparison of complex topography with terrestrial laser scanner: Application to the Rangitikei canyon (NZ), ISPRS J. Photogramm., 82, 10–26, 2013.
Langhammer, J., Lendzioch, T., Mirijovky, and Hartvich, F.: UAVbased Optical Granulometry as Tool for Detecting Chnages in Strctures of Flood Depositions, Remote Sens., 9, 240, https://doi.org/10.3390/rs9030240, 2017.
Lauretta, D. S., DellaGiustina, D. N., Bennett, C. A., Golish, D. R., Becker, K. J., BalramKnutson, S. S., Barnouin, O. S., Becker, T. L., Bottke, W. F., Boynton, W. V., Campins, H., Clark, B. E., Connolly Jr, H. C., Drouet d’Aubigny, C. Y., Dworkin, J. P., Emery, J. P., Enos, H. L., Hamilton, V. E., Hergenrother, C. W., Howell, E. S., Izawa, M. R. M., Kaplan, H. H., Nolan, M. C., Rizk, B., Roper, H. L., Scheeres, D. J., Smith, P. H. , Walsh, K. J., Wolner, C. W. V., and The OSIRISREx Team: The unexpected surface of asteroid (101955) Bennu, Nature, 568, 55–60, 2019.
Leduc, P., Peirce, S., and Ashmore, P.: Short communication: Challenges and applications of structurefrommotion photogrammetry in a physical model of a braided river, Earth Surf. Dynam., 7, 97–106, https://doi.org/10.5194/esurf7972019, 2019.
Leyland, J., Hackney, C. R., Darby, S. E., Parsons, D. R., Best, J. L., Nicholas, A. P., Aalto, R., and Lague, D.: Extreme flooddriven fluvial bank erosion and sediment loads: direct process measurements using integrated Mobile Laser Scanning (MLS) and hydroacoustic techniques, Earth Surf. Proc. Land., 42, 334–346, 2017.
Li, Q. and Griffiths, J. G.: Least squares ellipsoid specific fitting, Geometric Modeling and Processing, Proceedings, 335–340 pp., https://doi.org/10.1109/GMAP.2004.1290055, 2004.
Marc, O., Turowski, J. M., and Meunier, P.: Controls on the grain size distribution of landslides in Taiwan: the influence of drop height, scar depth and bedrock strength, Earth Surf. Dynam., 9, 995–1011, https://doi.org/10.5194/esurf99952021, 2021.
Miller, K. L., Szabó, T., Jerolmack, D. J., and Domokos, G.: Quantifying the significance of abrasion and selective transport for downstream fluvial grain size evolution, J. Geophys. Res.Earth Surf., 119, 2412–2429, 2014.
Molnar, P., Anderson, R. S., and Anderson, S. P.: Tectonics, fracturing of rock, and erosion, J. Geophys. Res.Earth Surf., 112, F03014, https://doi.org/10.1029/2005JF000433, 2007.
Neely, A. B. and DiBiase, R. A.: Drainage area, bedrock fracture spacing, and weathering controls on landscapescale patterns in surface sediment grain size, J. Geophys. Res.Earth Surf., 125, e2020JF005560, https://doi.org/10.1029/2020JF005560, 2020.
NovákSzabó, T., Sipos, A. Á., Shaw, S., Bertoni, D., Pozzebon, A., Grottoli, E., Sarti, G., Ciavola, P., Domokos, G., and Jerolmack, D. J.: Universal characteristics of particle shape evolution by bedload chipping, Sci. Adv., 4, eaao4946, https://doi.org/10.1126/sciadv.aao4946, 2018.
O'Callaghan, J. F., and Mark, D. M.: The extraction of drainage networks from digital elevation data, Computer Vision, Graphics, And Image Processing, 28, 323–344, 1984.
Pearson, E., Smith, M. W., Klaar, M. J., and Brown, L. E.: Can high resolution 3D topographic surveys provide reliable grain size estimates in gravel bed rivers?, Geomorphology, 293, 143–155, 2017.
Purinton, B. and Bookhagen, B.: Introducing PebbleCounts: a grainsizing tool for photo surveys of dynamic gravelbed rivers, Earth Surf. Dynam., 7, 859–877, https://doi.org/10.5194/esurf78592019, 2019.
Purinton, B. and Bookhagen, B.: Tracking downstream variability in large grainsize distributions in the southcentral Andes, J. Geophys. Res.Earth Surf., 126, e2021JF006260, https://doi.org/10.1029/2021JF006260, 2021.
Rheinwalt, A., Goswami, B., and Bookhagen, B.: A networkbased flow accumulation algorithm for point clouds: FacetFlow Networks (FFNs), J. Geophys. Res.Earth Surf., 124, 2013–2033, 2019.
Rice, S. and Church, M.: Sampling surficial fluvial gravels; the precision of size distribution percentile sediments, J. Sediment. Res., 66, 654–665, 1996.
Riebe, C. S., Sklar, L. S., Overstreet, B. T., and Wooster, J. K.: Optimal reproduction in salmon spawning substrates linked to grain size and fish length, Water Resour. Res., 50, 898–918, 2014.
RodaBoluda, D. C., D'Arcy, M., McDonald, J., and Whittaker, A. C.: Lithological controls on hillslope sediment supply: insights from landslide activity and grain size distributions, Earth Surf. Proc. Land., 43, 956–977, 2018.
Roduit, N.: JMicroVision: Image analysis toolbox for measuring and quantifying components of highdefinition images, ver. 1, 2002–2007, 2008.
Rubin, D. M.: A simple autocorrelation algorithm for determining grain size from digital images of sediment, J. Sediment. Res., 74, 160–165, 2004.
Rust, B. R.: Structure and process in a braided river, Sedimentology, 18, 221–245, 1972.
Rychkov, I., Brasington, J., and Vericat, D.: Computational and methodological aspects of terrestrial surface analysis based on point clouds, Computers and Geosciences, 42, 64–70, 2012.
Schneider, J. M., Rickenmann, D., Turowski, J. M., Bunte, K., and Kirchner, J. W.: Applicability of bed load transport models for mixedsize sediments in steep streams considering macroroughness, Water Resour. Res., 51, 5260–5283, 2015.
Schwanghart, W. and Scherler, D.: Short Communication: TopoToolbox 2 – MATLABbased software for topographic analysis and modeling in Earth surface sciences, Earth Surf. Dynam., 2, 1–7, https://doi.org/10.5194/esurf212014, 2014.
Shields, A.: Anwendung der Aehnlichkeitsmechanik und der Turbulenzforschung auf die Geschiebebewegung, PhD Thesis Technical University Berlin, Germany, 1936.
Sklar, L. S. and Dietrich, W. E.: A mechanistic model for river incision into bedrock by saltating bed load, Water Resour. Res., 40, W06301, https://doi.org/10.1029/2003WR002496, 2004.
Sklar, L. S., Riebe, C. S., Marshall, J. A., Genetti, J., Leclere, S., Lukens, C. L., and Merces, V.: The problem of predicting the size distribution of sediment supplied by hillslopes to rivers, Geomorphology, 277, 31–49, 2017.
Soloy, A., Turki, I., Fournier, M., Costa, S., Peuziat, B., and Lecoq, N.: A deep learningbased method for quantifying and mapping the grain size on pebble beaches, Remote Sens., 12, 3659, https://doi.org/10.3390/rs12213659, 2020.
Steer, P.: philippesteer/G3Point: G3Point v1.0 (v1.0), Zenodo [code], https://doi.org/10.5281/zenodo.6368501, 2022.
Szabó, T., Domokos, G., Grotzinger, J. P., and Jerolmack, D. J.: Reconstructing the transport history of pebbles on Mars, Nat. Commun., 6, 1–7, 2015.
Tonina, D. and Buffington, J. M.: Hyporheic exchange in mountain rivers I: Mechanics and environmental effects, Geography Compass, 3, 1063–1086, 2009.
Várkonyi, P. L., Laity, J. E., and Domokos, G.: Quantitative modeling of facet development in ventifacts by sand abrasion, Aeol. Res., 20, 25–33, 2016.
VázquezTarrío, D., Borgniet, L., Liébault, F., and Recking, A.: Using UAS optical imagery and SfM photogrammetry to characterize the surface grain size of gravel bars in a braided river (Vénéon River, French Alps), Geomorphology, 285, 94–105, 2017.
Verdian, J. P., Sklar, L. S., Riebe, C. S., and Moore, J. R.: Sediment size on talus slopes correlates with fracture spacing on bedrock cliffs: implications for predicting initial sediment size distributions on hillslopes, Earth Surf. Dynam., 9, 1073–1090, https://doi.org/10.5194/esurf910732021, 2021.
Walicka, A. and Pfeifer, N.: Automatic Segmentation of Individual Grains From a Terrestrial Laser Scanning Point Cloud of a Mountain River Bed, IEEE J. Sel. Top. Appl., 15, 1389–1410, 2022.
Watkins, S. E., Whittaker, A. C., Bell, R. E., Brooke, S. A., Ganti, V., Gawthorpe, R. L., McNeill, L. C., and Nixon, C. W.: Straight from the source's mouth: Controls on fieldconstrained sediment export across the entire active Corinth Rift, central Greece, Basin Research, 32, 1600–1625, 2020.
Westoby, M. J., Brasington, J., Glasser, N. F., Hambrey, M. J., & Reynolds, J. M.: “StructurefromMotion” photogrammetry: A lowcost, effective tool for geoscience applications, Geomorphology, 179, 300–314, 2012.
Westoby, M. J., Dunning, S. A., Woodward, J., Hein, A. S., Marrero, S. M., Winter, K., and Sugden, D. E.: Sedimentological characterization of Antarctic moraines using UAVs and StructurefromMotion photogrammetry, J. Glaciol., 61, 1088–1102, 2015.
Wolman, M. G.: A method of sampling coarse riverbed material, EOS, Transactions American Geophysical Union, 35, 951–956, 1954.
Woodget, A. S. and Austrums, R.: Subaerial gravel size measurement using topographic data derived from a UAVSfM approach, Earth Surf. Proc. Land., 42, 1434–1443, 2017.
Woodget, A. S., Fyffe, C., and Carbonneau, P. E.: From manned to unmanned aircraft: Adapting airborne particle size mapping methodologies to the characteristics of sUAS and SfM, Earth Surf. Proc. Land., 43, 857–870, 2018.