## Abstract

River channels are among the most common landscape features on Earth. An essential characteristic of channels is sinuosity: their tendency to take a circuitous path, which is quantified as along-stream length divided by straight-line length. River sinuosity is interpreted as a characteristic that either forms randomly at channel inception or develops over time as meander bends migrate. Studies tend to assume the latter and thus have used river sinuosity as a proxy for both modern and ancient environmental factors including climate, tectonics, vegetation, and geologic structure. But no quantitative criterion for planform expression has distinguished between random, initial sinuosity and that developed by ordered growth through channel migration. This ambiguity calls into question the utility of river sinuosity for understanding Earth's history. We propose a quantitative framework to reconcile these competing explanations for river sinuosity. Using a coupled analysis of modeled and natural channels, we show that while a majority of observed sinuosity is consistent with randomness and limited channel migration, rivers with sinuosity ≥1.5 likely formed their geometry through sustained, ordered growth due to channel migration. This criterion frames a null hypothesis for river sinuosity that can be applied to evaluate the significance of environmental interpretations in landscapes shaped by rivers. The quantitative link between sinuosity and channel migration further informs strategies for preservation and restoration of riparian habitat and guides predictions of fluvial deposits in the rock record and in remotely sensed environments from the seafloor to planetary surfaces.

## INTRODUCTION

Single-thread channels abound on planetary surfaces with varied fluids and substrates (Komatsu and Baker, 1996; Karlstrom et al., 2013; Allen and Pavelsky, 2018; Fig. 1). All natural channels, including rivers, invariably deviate from straight-line paths, with typical sinuosity values (ratio of along-channel to straight-line distance) up to ∼3 (Leopold and Wolman, 1957; Howard and Hemberger, 1991). Sinuosity is the most widely used statistic to describe river planform geometry and has been interpreted as a proxy for environmental processes including climate (Stark et al., 2010), the stabilizing effects of vegetation and fine sediment (Braudrick et al., 2009; Davies and Gibling, 2010; Lapôtre et al., 2019), tectonics, geologic structure, and lithology (Harden, 1990; Johnson and Finnegan, 2015).

However, to provide a window into past landscape conditions, sinuosity must respond to those conditions over time. Some rivers show abundant evidence for sinuosity evolution as recorded by direct observations or geologic markers like cutoffs (Fig. 1A), scroll bars, terraces, and eroded valley margins (Hooke, 2013). Yet many rivers lack these indicators of channel migration (Fig. 1B), suggesting that river sinuosity may, to some degree, form randomly at channel inception in response to intrinsic irregularities of topography (Mueller, 1968). Extreme examples of channelization also demonstrate extrinsic controls on sinuosity such as crevasses that steer supraglacial meanders (Fig. 1C) and sinuous volcanic channels that show little evidence of migration (Fig. 1D). Ambiguity in the origin of sinuosity calls into question its utility for interpreting environmental history. For example, a classic debate regarding bedrock-bound meanders centers on whether high sinuosity due to channel migration is a relic of previous alluvial states (Winslow, 1893). We consider a broader question: for any channel, under what conditions is sinuosity a diagnostic of channel migration? We propose that the magnitude of sinuosity can distinguish whether the channel form is consistent with randomness or has instead developed mainly through ordered growth by channel migration.

For single-thread rivers, theoretical models describe two end-member scenarios for the origin of sinuosity, which we define as random models and migration models, respectively. Random models treat the path of the centerline (the line equidistant between each of the river banks) as a random walk (Langbein and Leopold, 1966). In contrast, migration models explain sinuosity development by explicitly considering hydrodynamic effects that erode and construct river banks and grow meander bends (Camporeale et al., 2007). Neither class of models fully captures river forms. Geometric analyses show that compared to natural channels, centerlines made by pure random walks change direction too quickly and form tangled loops rather than alternating bends (Ferguson, 1976); channel-migration models generate bends, but they are overly regular and sinuous (Howard and Hemberger, 1991). Therefore, to better mimic the geometry of natural channels, a model requires spatial memory at relatively small length scales but irregularity at larger scales.

Many natural time series, such as climatological data, can likewise be described by a combination of inertia and randomness. A first-order autoregressive process (AR-1) is recognized as the simplest possible model—and the default expectation—for any geophysical process that is both dependent on previous states and subject to random disturbances (Roe, 2009). Ferguson (1976) showed that compared to an AR-1 model, a second-order autoregressive model (AR-2) tempers high-frequency variations while still allowing overall bend shapes to vary. That means the AR-2 model represents the simplest model for sinuosity that yields shapes comparable to natural channels. The AR-2 model is strictly geometric and is therefore sufficiently generic to describe channels whose formation processes may differ in detail. For natural channels that lack indicators of channel migration, we propose that spatially correlated randomness as expressed by the AR-2 model represents the null hypothesis for river sinuosity and can be used to test the significance of environmental interpretations.

## MODELING AND ANALYSIS OF CHANNEL PLANFORMS

^{1}). The AR-2 model, a discrete approximation of a differential equation (Ferguson, 1976), is where θ is the azimuth of the channel centerline,

*i*is the index of the centerline node,

*b*

_{1}and

*b*

_{2}are coefficients, and ϵ is a random series of direction disturbances drawn independently from a normal distribution with a mean of zero and variance of σ

^{2}.

For a global data set of natural channels, we calculated sinuosity and fit AR-2 model parameters to constrain their ranges (Fig. S1 in the Supplemental Material). We then used a suite of model runs to estimate the magnitude of sinuosity (*S*) that can be explained with Equation 1 using a systematic parameter sweep for *b*_{1}, *b*_{2}, and σ. For each parameter combination, we analyzed 100 replicates with different disturbance series (ϵ) to statistically characterize model randomness (Figs. S2 and S3). Because in some model runs the channel crossed itself, we treated each self-intersection as a cutoff loop and removed it to maintain a simplified, continuous centerline. For each set of replicates, we calculated the mean and standard deviation of sinuosity of the simplified centerlines and the average length of the original centerlines bound in self-intersecting loops.

## RESULTS

The suite of model runs shows that both sinuosity and the degree of self-intersection vary systematically with *b*_{1}, *b*_{2}, and σ (Fig. 2A). Higher values of *b*_{1} and σ increase sinuosity, with mean values typically <1.5. The inherent randomness in the model causes sinuosity to vary across the replicate simulations (Fig. 2B). For a fraction of the replicates, *S* is >1.5, particularly where self-intersection is common or σ 0.3 (Fig. 2C); the latter rarely occurs in nature (Fig. S1). These model results imply that randomly generated sinuosity rarely exceeds 1.5 for channels that are both geometrically realistic and have not migrated. We hypothesize that a channel typically only reaches *S* > 1.5 by migrating.

*t**) is used to track the cumulative channel migration, where

*t*is dimensioned time,

*E*

_{L}is maximum lateral erosion rate, and

*w*

_{c}is channel width. In this scenario, the channel begins with a low sinuosity caused by randomness (

*S*= 1.1 at

*t** = 0; Fig. 3A). Subsequent channel migration causes increased sinuosity by elongating half-meanders between curvature inflections (Fig. 3B; Howard and Hemberger, 1991). Importantly, AR-2 randomness cannot generate half-meanders of comparable length because the sense of curvature reverses over shorter distances along-stream. This behavior ultimately limits the range of sinuosity that randomness can generate absent extrinsic factors.

The migration model further shows that bends in initially random channels with different sinuosity follow offset trajectories for sinuosity growth through channel migration (Fig. 3C). These cases arrive, at different dimensionless times, at a critical sinuosity that suggests channel migration (*S*_{c} = 1.5). As expected, the dimensionless time to reach the critical sinuosity (*t*_{c}***) generally decreases with increasing initial sinuosity (Fig. 3D). Moreover, *t*_{c}* is <15 in all cases, which suggests an upper bound on the amount of channel migration that must occur before the centerline conclusively reflects channel migration. In other words, the initial, random sinuosity of the channel is overwritten over a finite time interval.

For a global data set of river planforms, sinuosity mostly varies from 1 to 2.5 (Fig. 4A). We fit the AR-2 model to each observed planform to find the corresponding distribution of sinuosity values predicted by the model. For model cases with no self-intersection in the original centerline, the probability of the random sinuosity exceeding the observed sinuosity (*S*_{obs}) is significant for *S*_{obs} < 1.2 but declines sharply with increasing *S*_{obs} (Fig. 4B). If cases with self-intersection in the original centerline are considered, the random model accounts for a greater range of *S*_{obs} but is unlikely to account for *S*_{obs} > 2 (Fig. 4C). A separate data set of channels with documented migration (Fig. 4D) shows that migration favors higher sinuosity values, including *S* > 1.5 for all cases in the Andean foreland with especially high migration rates (>10% *w*_{c} per year; Sylvester et al., 2019). Substituting *t*_{c}* = 15 and these observed migration rates in Equation 2, for the Andean foreland rivers we estimate that the time scale to critical sinuosity (*S*_{c} = 1.5)—the clear distinction from randomness in the planform—is *t*_{c} ≈ 150 years.

## DISCUSSION AND CONCLUSIONS

We used a null-hypothesis test to estimate the role of spatially correlated randomness in river channel sinuosity (*S*) and show that a random model typically produces *S* < 1.5 (Fig. 2A). The low probability of exceeding this critical value (*S*_{c} = 1.5; Fig. 2C) indicates that for channels with *S* > *S*_{c}, the null hypothesis can be rejected, and that non-random, ordered channel migration is a necessary condition for the sinuosity observed. The converse (*S* < *S*_{c})—not rejecting the null hypothesis—does not imply that randomness fully explains the observed sinuosity. Migrating channels with *S* < *S*_{c} are relatively common (Fig. 4D); relatively low sinuosity in migrating channels could result from slow channel migration and/or limited evolution time (Equation 2) or extrinsic constraints. Thus, although the sinuosity criterion cannot rule out migration if *S* < *S*_{c}, the metric does identify cases in which channel migration is definitive (*S* > *S*_{c}).

A quantitative signature of migration in river sinuosity lends this common characteristic further significance for interpreting landscape history. Sinuosity in natural channels reflects neither pure randomness nor universal channel migration but rather exists on a continuum between the two. To borrow from Shakespeare's *Twelfth Night*, some channels are born sinuous (Fig. 1D); some achieve further sinuosity, through channel migration (Fig. 1A); and some have sinuosity thrust upon them, by faulting, valley shape, or other non-random topographic control (Fig. 1C). Random, initial sinuosity is embellished to a degree determined by the rate and duration of channel migration (Fig. 3C). Spatial correlation should be considered for initial planform geometry in numerical models of channel migration, as this geometry and its persistence through time (Fig. 3D) are more realistic than the uncorrelated, ephemeral noise that is most often used (e.g., Frascati and Lanzoni, 2010). At quasi-steady-state, such channel-migration models can develop sinuosity (*S* > 3.5) that exceeds typical observations (Fig. 4A; Howard, 1996; Frascati and Lanzoni, 2010). Therefore, in the absence of evidence indicating channel migration, spatially correlated randomness should represent the null hypothesis for sinuosity.

In rivers characterized by channel migration and non-local avulsions, a given channel may express the two regimes of the randomness-order continuum both in space and over time (Valenza et al., 2020). When a river avulses to create a diversion across its own floodplain, it may reoccupy relict channels and/or cut new ones. An avulsing channel may therefore simultaneously form new reaches guided by random landscape disturbances and also inherit the bends of an antecedent, migrating channel. As the planform of the avulsion channel evolves with bend migration, indicators of its randomness are overwritten.

Our findings can inform interpretations of environmental forcing from the sinuosity of natural channels. For example, Stark et al. (2010) interpreted climate forcing from a spatial trend in sinuosity for mixed bedrock-alluvial rivers with reported sinuosity *S* < 1.5, which is the critical value that we identify. Our analysis suggests that using sinuosity as a proxy for the degree of channel migration should be done with caution for rivers with sinuosity below the critical value; future analyses could account for the role of random sinuosity as a null hypothesis. Our results suggest that river sinuosity could, however, be used to infer alluvial sediment deposited by channel migration in a channel belt many times wider than the river itself (Jobe et al., 2016). This approach could inform predictions for stratigraphic architecture in cases where channel belts are not directly observable as in some seismic images of marine sediments (Pirmez and Imran, 2003) and on planetary surfaces (Burr et al., 2013). Finally, these results may apply to optimizing river restoration projects, which are commonly designed to match idealized meandering forms (Kondolf, 2006). Our analysis shows that for cases where migration by the original channel exhibited minimal migration, restored channels should have low sinuosity (*S <* 1.5). Meanwhile, natural, rapidly migrating channels drive forest disturbance and primary succession that may contribute to biodiversity (Salo et al., 1986). These observations suggest that high-sinuosity (*S* >>2) river corridors, which are likely dominated by migration and relatively rare (Figs. 4A and Fig. 4D), should be prioritized for conservation.

^{1}Supplemental Material. Additional methods. Please visit https://doi.org/10.1130/GEOL.S.15152385 to access the supplemental material, and contact editing@geosociety.org with any questions.

## ACKNOWLEDGMENTS

We thank Samuel Johnstone and an anonymous reviewer for helpful comments, and Roman DiBiase, Douglas Edmonds, and Chris Paola for discussions. The U.S. National Science Foundation (grants EAR-1823530 and EAR-1246761), the British Society for Geomorphology, and Los Alamos National Laboratory (LDRD-20170668PRD1) supported this work. Data and code from this study are available at the University of Virginia's (USA) data repository LibraData (https://doi.org/10.18130/V3/TRTTIS) and at Github (https://github.com/alimaye/AR2-sinuosity), respectively.