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 As rivers transport water and sediment across Earth's surface, they radiate elastic and acoustic waves. We use seismic and infrasound observations during a controlled flood experiment (CFE) in the Grand Canyon to show that three types of fluvial processes can be monitored from outside the channel. First, bed-load transport under conditions of evolving bed mobility is identified as the dominant seismic source between 15 and 45 Hz. Two lower-frequency seismic bands also excited by the CFE exhibited greater power increases and are consistent with source processes related to fluid rather than sediment transport. The second fluvial seismic source is inferred to be fluid tractions on the rough riverbed, which drive the maximum seismic power increase at 0.73 Hz, but do not excite infrasound. Waves at the fluid-air interface are suggested as a third source, which generates a common 6–7 Hz peak in seismic and infrasound responses to the CFE.
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 Fluvial sediment transport and incision are fundamental landscape evolution processes that are effective at timescales relevant to land-use management and geological studies. Among the limitations in monitoring and modeling these processes is the difficulty of quantifying bed-load transport and the forces exerted on the riverbed. Existing methods for monitoring bed-load transport such as direct collection [e.g., Leopold and Emmett, 1977], tracking tracer particles [e.g., Wilcock, 1997], measuring vibrations in steel plates installed beneath riverbeds [e.g., Turowski et al., 2011], and monitoring of riverbed velocities [e.g., Rennie et al., 2002] provide valuable data, but often require considerable effort to monitor a single site. Additionally, there is concern that collection may interfere with the natural state of sediment transport, and that short sampling durations with any method can yield inaccurate estimates of longer-term transport rates [Bunte and Abt, 2005]. The potential benefits of new noninvasive, long-duration, and broadly applicable methods for monitoring riverbed processes have motivated research on the seismic signal emanating from rivers.
 There is growing observational and theoretical support for the concept of remotely monitoring bed-load transport by measuring ground vibrations outside the channel [e.g., Govi et al., 1993]. Using seismic observations that were primarily acquired to study Earth structure, Burtin et al.  showed that 1–20 Hz noise levels were strongly correlated with discharge of the Trisuli River in Nepal. They further demonstrated that seismic power versus discharge exhibited seasonal hysteresis that is consistent with regional estimates of sediment transport rates [Gabet et al., 2008]. Similar hysteresis was also observed at 1–10 Hz at time scales of several days during storm events in the Cho-Shui River in Taiwan [Hsu et al., 2011]. Seismic observations of a small braided alpine stream [Burtin et al., 2011] suggest that gravel transport generates detectable seismic energy. These observations identify potential to develop methods for seismically monitoring bed-load flux, but rivers likely generate seismic energy through a diverse range of processes and their relative importance is poorly known.
 To better isolate fluvial seismic signals and link them to distinct processes, we collected data at the Colorado River during the November 2012 controlled flood experiment (CFE) in the Grand Canyon [e.g., Topping et al., 2010]. Our new seismic and infrasound observations take advantage of the predictable, large magnitude, and accurately known discharge variations. Additionally, we exploit the occurrence of a flash flood in a tributary canyon 3 months prior to the CFE, which locally increased the supply of weakly packed sediments. These circumstances in conjunction with 250 Hz seismic and infrasound sampling at only 38 m from the channel allow novel discrimination of multiple fluvial sources of seismic energy. Here we report on the characteristics of three distinct signals excited by the CFE. Based on their characteristics, we suggest that one of the signals dominantly results from bed-load transport and the other two dominantly result from fluid transport processes.
2 Field Site and Data
 The field site is in eastern Grand Canyon where the ephemeral Red Canyon tributary enters the Colorado River (see supporting information). Grand Canyon is a debris fan dominated channel with characteristic sequences of backwater pools upstream of tributary debris fans, coarse-grained debris fans, and eddies and associated sand and gravel bars downstream of debris fans [Howard and Dolan, 1981]. The Red Canyon confluence marks the beginning of Hance Rapid, which includes many 1–3 m standing water waves that span a downstream distance of about 150 m. Mean channel slope over a 1 km reach centered at Hance Rapid is 0.25%. Three months prior to the CFE, a flash flood in Red Canyon deposited poorly sorted sediment into the main channel at low discharge (<300 m3/s) relative to peak CFE discharge of ~1300 m3/s. Between the flash flood and CFE discharge never exceeded 550 m3/s, and for 60 days prior to the CFE discharge was <280 m3/s. This created a circumstance where the river's first interaction with naturally deposited sediments near the channel edge could be predictably recorded in addition to signals from elsewhere in the channel.
 The CFE hydrograph shows a factor of 5 increase in discharge over 1 day followed by sustained peak discharge of about 1300 m3/s for 1 day and a more gradual 3 day decline back to the pre-CFE discharge (Figure 1). Peak CFE discharge is modest compared to the ~3500 m3/s discharge of 10 year recurrence interval floods prior to dam installation [Topping et al., 2010]. Peak stage increase above the pre-CFE level was typically 2–3 m near Hance Rapid and estimated by measuring the vertical distance between the post-CFE river surface and the highest vegetation disturbed by the CFE. Pre-CFE discharge is in the lower half of the 200–300 m3/s range that is necessary to prevent sand accumulation in the Grand Canyon [Topping et al., 2000], so pre-CFE transport of grains larger than sand is probably negligible. The nearest stream gages are located 27 km upstream and 16 km downstream of Hance Rapid and have a 15 min sampling period (www.gcmrc.gov). During the CFE, the largest tributary input downstream of Glen Canyon Dam was <6 m3/s and no rainfall occurred. We linearly interpolate the upstream and downstream gage data to estimate the local discharge time series.
 Seismic and infrasound instruments were located 38 m from the channel edge at minimum discharge and about 32 m from the channel edge at peak CFE discharge. Three-component ground velocity was measured by an L-22 seismometer with a corner frequency of 2 Hz and flat response to >>100 Hz. Air pressure was measured by an infrasonic microphone with a corner frequency of 0.05 Hz and flat response to >>100 Hz [Marcillo et al., 2012]. A 24-bit digitizer and a sampling rate of 250 Hz were used for both the seismic and infrasound recording. After deconvolution of the instrument response functions and application of an anti-aliasing filter, both types of data are reliable across the 0.3–100 Hz range presented here.
3 Spectral Analysis
 We focus on the river's response to the CFE in the frequency domain. Spectrograms were constructed using the multitaper method [Thomson, 1982] to estimate power spectral density in 2 min nonoverlapping windows. To minimize influence from spurious transients in the riverside environment, we examine the median spectrum across seven 2 min windows at a time. Vertical and mean horizontal spectra are analyzed. The mean of the two horizontal components is used because source processes of interest are distributed at uncertain locations in the river channel. To examine the spectral response to changes in discharge, we calculated the median spectra during times of minimal discharge (200–240 m3/s) prior to the CFE and subtract them from the raw spectrograms to yield residual spectrograms (Figure 1; see supporting information).
4 Seismic and Infrasonic Response to the CFE
 Residual ground velocity power increased with discharge in multiple frequency bands during the CFE (Figure 1). The lowest frequency band excited by the CFE is 0.5–2 Hz, with a maximum increase of 17 dB at 0.73 Hz. A second local maximum of 14 dB increase occurs at 6.25 Hz. Frequencies from about 10–45 Hz show bursts of elevated power during near the end of the CFE's rising limb. However, power between about 15–45 Hz returns to near pre-CFE levels during the descending limb while discharge is still about 1000 m3/s. Thus, two peaks in the residual seismic spectrum remain prominent throughout the duration of the CFE, while frequencies between about 15–45 Hz are strongly excited during the rising limb but not the descending limb.
 Residual infrasound power also increases with discharge and has a maximum between 6 and 7 Hz that is maintained during the rising and descending limbs. Additional peaks in the infrasound spectrogram appear as horizontal bands at <10 Hz that have a quasi-diurnal recurrence, vary in duration from 2 to 12 h, and are not correlated with variations in discharge. These features are attributed to wind because it is a common source of ≤10 Hz infrasound noise [e.g., Hedlin and Raspet, 2003], and we observed one of these episodes during fieldwork on a windy day.
 The distinct seismic bands excited by the CFE show contrasting temporal variations (Figure 2). Hysteresis between seismic power and discharge is clearly exhibited by the 15–45 Hz band, but is relatively subtle or absent in the two lower-frequency bands. If this frequency band is extended to as low as 10 Hz or as high as 60 Hz, observation of hysteresis and its magnitude remains similar. In addition to the clockwise pattern of hysteresis, the 15–45 Hz band has three episodes with 4–5 dB power increases for durations of about 30–70 min during the latter half of the CFE's rising limb. Between these episodes, power remains 1.5–3 dB higher than at the same discharge during the descending limb. The final high-power episode is truncated at the time of the transition from the rising limb to constant peak discharge, when seismic power drops by 9 dB (Figure 2c). Episodic seismic power increases and hysteresis are small or absent in the two lower-frequency bands (Figure 2). The lowest frequency band excited by the CFE, 0.5–2 Hz, shows smoothly increasing power with discharge, steady power during the plateau at peak discharge, and the rising and descending limbs are consistent within 1 dB. The 2–15 Hz band also shows steady power during the plateau at peak discharge, but weak counter-clockwise hysteresis between 375–1050 m3/s. At these intermediate discharge levels, power during the descending limb is greater by about 1 dB. The 2–15 Hz band also shows power increases at the times of the episodic bursts of 15–45 Hz power, although they are relatively subtle indicating that the source of these bursts overlaps the boundary at 15 Hz.
 To isolate the part of the spectrum that shows the greatest power variations despite nearly constant discharge, we compare the median spectrum during the last 200 min of the rising limb to the median spectrum during the plateau at peak discharge (Figure 3). Discharge during these two time segments differs by only 5%. Power during the rising limb segment is greater than during the plateau segment from about 10–60 Hz with greatest difference between 15–45 Hz (Figure 3c). A similar difference is observed for the horizontal spectra. The two lower-frequency maxima are nearly constant for the rising and plateau time periods. Additionally, the lower frequency peaks are stronger in the vertical compared to the horizontal spectrum, with a difference of up to 4.5 dB in the lowest band.
4.1 Fluvial Sources of Seismic Energy
 Based on the contrasting characteristics of the different frequency bands excited by the CFE, we interpret that distinct fluvial processes are responsible. Specifically, we suggest that the following three source processes can be distinguished by combined seismic and infrasound monitoring at this site: bed-load transport, fluid tractions exerted on the rough riverbed, and fluid-air interactions such as breaking waves.
4.2 The Seismic Signal of Bed-Load Transport
 We consider the 15–45 Hz power variations to be dominantly driven by bed-load transport, although a contribution from bed-load likely extends to somewhat higher and lower frequencies (Figure 3c). This attribution is suggested by strong clockwise hysteresis, including 1–9 dB power differences for equivalent discharge and three episodes with 4–5 dB power increases for about 30–70 min during smoothly rising discharge. These temporal fluctuations in power are inconsistent with generation by smoothly varying fluid discharge. In contrast, bed-load transport has long observed to be temporally heterogeneous [e.g., Leopold and Emmett, 1977], including episodic pulses of increased flux [e.g., Reid et al., 1985] and both clockwise and counter-clockwise hysteresis in bed-load transport versus discharge [e.g., Hsu et al., 2011]. Recent flood simulations in a flume with heterogeneous grain sizes consistently exhibited clockwise hysteresis of bed-load flux versus discharge for a variety of hydrograph shapes [Mao, 2012].
 Power in the 15–45 Hz band began to increase consistently when discharge rose above about 550 m3/s, which is the maximum discharge that occurred between the flash flood and the CFE. Thus, the first interaction between the main channel flow and poorly packed sediments from Red Canyon is likely the dominant bed-load transport activity at the study site. Reworking of the flash flood deposits by the main channel flow during the CFE's rising limb may have resulted in tighter packing and preferential transport of fine grains [e.g., Mao et al., 2011] or changes in the friction angle without changing the surface grain-size distribution [e.g., Kirchner et al., 1990]. Either could increase the critical shear stress, such that steady peak discharge resulted in lower bed-load transport rates and 15–45 Hz seismic power than during the latter half of the rising limb. Post-CFE observations found that a sediment bar composed of gravel and larger clasts remained at the mouth of Red Canyon, supporting that variation in critical shear stress rather than exhaustion of sediment caused the 9 dB drop in seismic power at the end of the rising limb.
 A simple estimate of relative variations in bed-load flux can be made following the assumptions of Tsai et al. . They noted that variations in vertical seismic power scale linearly with bed-load mass flux if transport occurs by saltation of spherical grains on a flat elastic riverbed, and the spatial distribution of saltating grains remains constant. In this model, the episodes with 4–5 dB power increases would correspond to transient increases in bed-load flux by a factor of 2.5–3.2, and the 9 dB drop in power at the end of the rising limb would correspond to an abrupt eightfold decrease in bed-load flux. However, assumptions of the Tsai et al.  model such as vertical saltation, spherical grains and a flat bed, and a constant spatial distribution of bed-load transport may not be accurate, so the estimates above are highly uncertain.
 Isolation of the seismic power spectrum dominated by bed-load transport (Figure 3c) allows comparison with the vertical spectrum predicted by the Tsai et al.  model. Source-receiver distance is the primary control on the frequency content in the model. With an attenuation factor or Q of 8 and distance of 35 m from the river, the model is consistent with the ~30 Hz peak we observe. The requirement of a Q of 8 to match the spectral peak is plausible, but perhaps too high as Q = 9 was found at <150 m depth in highly weathered granite [Aster and Shearer, 1991], and our sensor was deployed on alluvium. It is also possible that grain-size distribution affects the seismic power spectrum more strongly than predicted by Tsai et al. . Experimental results from vertically dropping rocks show decreasing frequency with increasing grain size, and also a broader frequency response for rolling rather than vertical impacts [Huang et al., 2007].
 In theory, the dominant elastic wave type generated by a vertical force at the riverbed would be Rayleigh waves [e.g., Tsai et al., 2012], such that mean power of the two horizontal components would be less than the vertical power. At the site near Hance Rapid, we find approximately equal power in the vertical and horizontal spectra in the inferred bed-load transport frequency band (Figure 3c). This suggests that factors such as bed roughness and rolling or sliding mechanisms are probably important, as they would enhance the generation of horizontally polarized Love waves.
4.3 Two Seismic Sources From Fluid Processes
 At the study site, bed-load transport is not the dominant source of seismic power during the CFE. Two lower-frequency seismic bands exhibit greater power increases than in the 15–45 Hz band we infer to be dominated by bed-load transport. Power in both the 0.5–2 Hz and 2–15 Hz bands varies more smoothly with discharge and remains steady during peak discharge. A major difference between these two signal bands is that the lower band, which contains the greatest seismic power increase, is not excited in the infrasound spectrum and the higher seismic band closely corresponds with the maximal infrasound response to the CFE.
 We attribute the increased power in the 0.5–2 Hz band primarily to turbulent fluid flow that exerts pressure on the riverbed, which is probably enhanced by flow over boulders. In Grand Canyon rapids, such as Hance Rapid, the riverbed is generally covered by boulders and talus that were only partially mobilized by pre-dam floods greater than ~3000 m3/s [Howard and Dolan, 1981] so a continuously active layer of bed sediments is unlikely. Smooth power variations with discharge and lack of hysteresis are consistent with a fluid flow source. Lack of an infrasound response in this frequency band further suggests a source process limited to the fluid-solid interface. The 0.73 Hz maximum is 4.5 dB stronger in the vertical than horizontal spectrum indicating that vertical tractions dominate over shear tractions at the source (Figure 3). We suggest that fluid flow over the rough riverbed in Hance Rapid is the source of dominantly vertical tractions whose magnitude varies smoothly with discharge.
 Power in the 2–15 Hz band is primarily attributed to fluid-air interactions in Hance Rapid. There appears to be overlap between this signal and the bed-load signal between about 6–15 Hz, but steady power near the 6.25 Hz peak throughout the time of near-maximal discharge suggests that fluid transport creates the majority of the seismic power below ~15 Hz (Figure 3). Coincidence of the local maxima of residual seismic and infrasound power is the basis for our interpretation that fluid-air interactions are the dominant source. Seismic power in the 2–15 Hz band exhibits counter-clockwise hysteresis restricted to discharge values of 375–1000 m3/s and with ~1 dB greater power on the descending limb. If waves at the fluid-air interface are primarily responsible for power in this band, the difference at intermediate discharge levels could represent a modest change in the water wave pattern owing to bed-load movement during peak discharge.
 We have shown that the seismic response to the CFE is peaked in three distinct frequency bands that exhibit contrasting temporal evolutions during the CFE. Sources related to fluid transport are identified by their lack of sporadic power fluctuations and subtle or absent hysteresis. Sources of this type comprise the majority of the seismic power increase during the CFE and produce maxima in two different seismic bands. The lower band is absent in the infrasound spectrum and is consequently attributed to fluid tractions on the riverbed, while the higher band coincides with the maximal infrasound response and is attributed to waves at the fluid-air surface. Similar to prior studies, a bed-load contribution is indentified by clockwise hysteresis between seismic power and discharge. In addition, we detect transient increases in bed-load transport rate during the rising limb and use differential spectra between the end of the rising limb and plateau at peak discharge to isolate the spectrum of the bed-load signal. Nearly equal power of the bed-load signal in the vertical and mean horizontal spectra indicates that Love and Rayleigh waves should be considered in methods to seismically monitor bed-load flux.
 We thank M. Hahn and R. Newton from the National Park Service, and J. Schmidt, C. Fritzinger, N. Voichick, and R. Tusso from the Grand Canyon Monitoring and Research Center for making it possible to use this exceptional science opportunity. The IRIS PASSCAL Instrument Center, and particularly P. Miller and G. Slad are thanked for instrument and data handling support. E. Aster assisted with fieldwork. Mike Lamb provided informal feedback. Two anonymous reviewers helped improve the manuscript. B.S. acknowledges Caltech for time to conduct fieldwork and support for this research from the University of New Mexico.
 The Editor thanks two anonymous reviewers for their assistance in evaluating this paper.