3.1 The Entle and Schimbrig catchments

Our study area is located in the northern foothills of the Central Swiss Alps, between Bern and Lucerne (Fig. 2). The Entle catchment has a drainage basin of 64 km², with an elevation ranging between 680 m a.s.l. at the outlet near Entlebuch village and 1815 m on the Schimbrig summit. The study area lies at the intersection between the Swiss Plateau, i.e. the Molassic basin, and the frontal thrusts of the Alpine orogeny. The molasse unit, covering the lower reaches of the catchment, is composed of Late Oligocene conglomerate bedrock knobs, forming erosion-resistant low ridges. The intermediate part of the catchment is covered by subalpine flysch, while the higher SW–NE-oriented ridge is composed of Cretaceous carbonate rocks of the Helvetic thrust sheet (Schlunegger et al., 2016b; Fig. 2). The Entle catchment is dissected by a 7 km long central inner gorge with two tributaries, i.e. the Grosse and the Kleine Entle, that are deeply incised into a more than 100 m thick unconsolidated glacial till. The glacial till was deposited during repetitive and extensive glaciations during the Pleistocene. Lateral and terminal moraines deposited by the Entle glacier during the Last Glacial Maximum (LGM) are dissected by the Grosse and Kleine Entle rivers up to the headwaters (Fig. 2). The inner gorge contains knick zones in its longitudinal profile, and several cut terraces are visible. A ¹⁰Be-based sediment budget, which covers the last ca. 2000 years, highlighted that incision rates in the inner gorge are more than 4 times higher than in the non-incised reaches (Van den Berg et al., 2012). The study area experiences three types of mass movement processes over distinctive landscape units. Landslides categorized as earthflows mainly affect the flysch areas. This type of mass movement is very common in flysch sedimentary sequences and represents more than 30 % of all mass movements in Switzerland according to Lateltin et al. (1997). Near the summits, rock falls are common phenomena, and the sidewalls of river valleys are subject to widespread rotational and translational landslides.

Figure 2Simplified geological and geomorphological settings of the Entle River catchment (after Van den Berg et al., 2012; Schlunegger et al., 2016a). Inset: location of the study area in Switzerland. Source of the DEM: Swiss Federal Office of Topography Swisstopo (2013).

Within the Entle River catchment, an earthflow named Schimbrig has been particularly active over the last 150 years, acting as a sediment factory by excavating and mobilizing sediments because of its deep rotational structure (Clapuyt et al., 2017; Lopez-Saez et al., 2017; Savi et al., 2013; Schwab et al., 2008). It is located in the first-order Schimbrig catchment, the latter draining successively into the Rossloch River and the Kleine Entle, before entering the trunk river, i.e. the Grosse Entle. The earthflow occurs on the hillslopes of the Schimbrig ridge and is not directly connected to the Schimbrig stream, except during short episodes when superimposed debris flows occur (Schwab et al., 2008). The Schimbrig earthflow consists of a fine-grained matrix of silt and mud, with centimetric to decimetric large clasts (Clapuyt et al., 2017). The internal structure of the earthflow is complex with nested rotational units (Clapuyt et al., 2017). Field observations revealed that a major earth slide with a surface lowering of up to 12 m occurred in the summer of 1994 after a succession of heavy precipitation events, followed by debris flows until March 1995 (Schwab et al., 2008). The intensity and spatial pattern of sediment redistribution, as well as the internal structure of the earthflow have rapidly evolved at the annual and decadal scale (Clapuyt et al., 2017; Schwab et al., 2008). The Schimbrig catchment also experiences scree-slope-like erosion processes in the upper part on the Schimbrig ridge. Eroded material is stored at the foot of the slope, above river sources. Within the Schimbrig catchment, the described earthflow affects ca. 25 % of the area and is the only active process in the catchment.

3.2 Annual sediment fluxes

The annual sediment fluxes of the active part of the Schimbrig earthflow (Fig. 3) were derived from time series of very high-resolution topographic datasets from Clapuyt et al. (2017). The earthflow has a rotational structure and is the dominant source of sediment on the hillslopes. By quantitatively comparing topographic datasets, we assessed spatial patterns of surface lowering, i.e. a decrease in ground elevation, and bulging, i.e. an increase in ground elevation. The overall sediment budget of the area affected by the earthflow, i.e. the difference between surface lowering and bulging, is indicative of the change in sediment volume through time. The sediment flux is derived at the base of the hillslopes at the transition between the hillslope and fluvial domains and represents the net flux of sediment from the earthflow to the Schimbrig River. The earthflow acts as a pure sediment source on the hillslope.

Figure 3Illustration of the Schimbrig earthflow acting as a source of sediment in the river catchment. (a) Upper part with surface subsidence. (b) Toe of the earthflow with surface bulging. The location of the Schimbrig earthflow is depicted in Fig. 2.

The 3-D topographic reconstructions were computed using the structure-from-motion algorithm based on aerial photographs acquired by an unmanned aerial vehicle (Clapuyt et al., 2016). Point clouds were subsequently interpolated into digital surface models (DSMs) at a spatial resolution of 0.04 m, defined based on the density of the point clouds. The accuracy of the time series ranges between 0.20 and 0.24 m. The acquisition dates are October 2013, June 2014 and October 2015. As part of this sediment flux assessment, only the dataset of the 2014–2015 time interval was used because it covers the full spatial domain of the Schimbrig earthflow. The sediment budget was quantified from a digital elevation model of differences (DoDs) between DSMs, using the Geomorphic Change Detection software (Wheaton et al., 2010). In this paper, values are eventually reported on an annual basis instead of over the entire period of interest (as in Clapuyt et al., 2017). Detailed information about the methodology and extended results are available in Clapuyt et al. (2017). Errors reported at the annual scale were computed based on a uniform limit of detection applied to each topographic surface. Therefore, the associated error of the annual sediment fluxes should be seen as a maximum value. It is likely that spatializing the error in very high-resolution topographic measurements, i.e. accounting for the spatial variation in photogrammetric and georeferencing precisions of the reconstructions, would lead to an increase in the signal-to-noise ratio as shown by James et al. (2017).

3.3 Decadal sediment fluxes

The sediment fluxes at a decadal scale were derived from Schwab et al. (2008), who assessed sediment transport by the Schimbrig earthflow and associated slopes, i.e. the Schimbrig catchment (Fig. 4), and linked it with suspended sediment loads from a gauging station in the trunk stream, i.e. the Waldemme River. The authors based their analysis on a time series of DEMs derived from classic photogrammetry of aerial photographs acquired in 1962, 1986, 1993, and 1998. Each image of stereo-pairs was scanned with a ground resolution of 0.4 m and georeferenced using a differential GPS. Because of the scarcity of well-recognizable features through time, the associated volumetric errors of the photogrammetric workflow ranged between 2 % for the 1986–1993 time interval and 29 % for the 1962–1986 time interval. The sediment budget based on DEMs provides two metrics. The total sediment displaced corresponds to surface lowering while the total sediment exported per year, i.e. the sediment flux entering the Rossloch River, is the balance between surface lowering and bulging. The ratio between both metrics indicates the percentage of sediment mass evacuated compared to the displaced mass. For this study, we converted the average sediment fluxes that were expressed in tonnes per year into cubic metres per year, using a material density of 2.70 g cm⁻³ following a study by Gong (2005) on similar flysch units in Switzerland. A detailed methodology and results are available in the original paper of Schwab et al. (2008).

3.4 Millennial sediment fluxes

The geomorphic process rates at a millennial scale were assessed from catchment-averaged denudation rates derived from in situ produced cosmogenic radionuclides in fluvial sediments. In order to get a comprehensive dataset on the spatial variation in denudation rates in the Entle catchment, we collected river sand at eight locations in and around the Schimbrig catchment (Fig. 4) and combined the resulting dataset with earlier work by Van den Berg et al. (2012). The new samples were processed following the protocol described in Vanacker et al. (2007), which is similar to the one followed by Van den Berg et al. (2012). After washing and sieving samples to the 0.25–1.00 mm fraction size, grains were separated using a Frantz isodynamic magnetic separator. The remaining non-magnetic fraction was leached up to 10 times with 10 % hydrochloric acid to remove organic, calcium, and carbonate components. Then, samples were treated up to four times with 5 % hydrofluoric acid in order to dissolve anything but quartz and also to remove any meteoric ¹⁰Be left. After the leaching step, 157.8 µg of ⁹Be carrier was added to the clean quartz samples containing ca. 25 g of material. The purified quartz, i.e. ca. 10 % of the original sample weight, was subsequently dissolved in concentrated hydrofluoric acid, from which beryllium was extracted stepwise using anion–cation exchange column chemistry. Remaining precipitates were oxidized and pressed into copper targets. Finally, ¹⁰Be∕⁹Be ratios were quantified using the 500 kV Tandy facility at ETH Zurich (Christl et al., 2013). These values were normalized with the in-house standard S2007N and corrected with a blank ¹⁰Be∕⁹Be ratio of $\mathrm{4.06}\pm \mathrm{0.23}\times {\mathrm{10}}^{-\mathrm{15}}$. Catchment-wide denudation rates were then computed from the in situ produced ¹⁰Be concentrations, i.e. from this study and from earlier data published by Van den Berg et al. (2012), using the catchment-averaged denudation rates from the cosmogenic nuclide (CAIRN) method (Mudd et al., 2016). This open-source calculator uses the topography to weight the ¹⁰Be production rate and shielding. A 1 m digital terrain model (DTM) resampled to 30 m resolution was used to compute topographic shielding. Snow shielding was averaged for each catchment individually. Snow cover is estimated using an elevation-dependent mean annual snow cover database for Switzerland (Auer, 2003). Following Jonas et al. (2009), an empirical relationship is used to derive the snow water equivalent thickness (SWE; g cm⁻²).We kept the default parameters from Mudd et al. (2016) to run the CAIRN model, including the sea-level high-latitude production rate of 4.30 atoms g⁻¹ yr⁻¹ (based on Braucher et al., 2011). Long-term denudation rates obtained by the CAIRN calculator were converted into sediment fluxes (m³ yr⁻¹), by multiplying them with the catchment area.

4.1 Schimbrig earthflow sediment dynamics at the annual scale

When focusing on the active part of the Schimbrig earthflow (Fig. 4), we obtained a net mass flux of 1000±4000 m³ yr⁻¹ for the 2014–2015 period (Table 1; Clapuyt et al., 2017). Accounting for the associated error, the sediment flux is considered to be zero. The sediment budget for the 2013–2014 time interval supports this finding. In the eroding sites, the average denudation was 0.8±0.2 m yr⁻¹ and equivalent to the accumulation that was observed in the bulging areas (Table 1). For the Schimbrig earthflow, Clapuyt et al. (2017) reported a mean horizontal displacement of ca. 6.30 m yr⁻¹ in the downslope direction. The UAV-SfM-derived data suggest that the earthflow was in a dynamic equilibrium over the 2014–2015 period, with earthflow-derived material being temporarily stored on the slopes during the period of interest.

Notwithstanding the state of dynamic equilibrium, the data suggest large internal movements with a complex pattern of sediment redistribution along the slope (Clapuyt et al., 2017). A succession of areas with terrain lowering and bulging characterized the earthflow along its longitudinal axis. The earthflow was re-adjusting to a new state of equilibrium after a massive failure that occurred in 1994. The sediment redistribution on the slopes was not associated with an increased sediment export downstream. Between 2013 and 2015, the hillslope domain was disconnected from the fluvial domain.

Table 1Sediment fluxes for the 2014–2015 time interval from the Schimbrig earthflow reported on an annual basis (modified from Clapuyt et al., 2017).

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4.2 Sediment budget of the Schimbrig catchment at a decadal scale

Sediment fluxes were computed from 1962 to 1998 over the first-order catchment affected by the earthflow, down to the confluence with the Rossloch River (Table 2; Fig. 4; Schwab et al., 2008). The average sediment flux per year, evacuated from the catchment, varies over time, from 14 000±4000 m³ yr⁻¹ for the 1962–1986 period to 850±20 m³ yr⁻¹ for 1986–1993 to 24 000±4000 m³ yr⁻¹ for the 1993–1998 time interval. The data from Schwab et al. (2008) indicate that there is no clear link between the sediment fluxes exported from the Schimbrig catchment and the earthflow dynamics on the hillslopes. This is evident from the fact that the proportion of the mass evacuated from the study area to the total displaced mass varies greatly between 6 % and 89 % (Table 2).

Table 2Sediment fluxes between 1962 and 1998 (after Schwab et al., 2008).

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During the 1962–1986 period, about 89 % of the displaced mass was evacuated from the catchment, suggesting that sediment storage during this period was not significant. In contrast, during the following periods (1986–1993, 1993–1998) when the major earthflow event occurred in 1994, only up to 34 % of the mobilized earthflow material was evacuated.

4.3 CRN concentrations in the Entle catchment

The ¹⁰Be concentrations reported in this study are spatially and quantitatively consistent with earlier measurements by Norton et al. (2008) and Van den Berg et al. (2012) (Fig. 4). Overall, the ¹⁰Be concentrations (Table 3; Fig. 4; Van den Berg et al., 2012) range from $\mathrm{0.15}\pm \mathrm{0.53}\times {\mathrm{10}}^{\mathrm{3}}$ atoms g⁻¹ in the upper part of the Schimbrig earthflow (CH-ENT-3) to $\mathrm{5.28}\pm \mathrm{0.26}\times {\mathrm{10}}^{\mathrm{3}}$ atoms g⁻¹ in the upper part of the Entle catchment, i.e. the Rothbach River (E-9). As the ¹⁰Be concentrations of the earthflow-affected area are low, relatively high errors are reported for the ¹⁰Be concentrations of the earthflow-derived sediment (Table 3). The errors subsequently propagated to the denudation rates, particularly for the samples from the Schimbrig stream draining the earthflow, i.e. CH-ENT-1, CH-ENT-5, and CH-ENT-8.

Table 3¹⁰Be concentrations (atoms g⁻¹), CRN-derived denudation rates (mm kyr⁻¹) and sediment fluxes (m³ yr⁻¹) for the Schimbrig catchment and other first-order rivers, i.e. samples CH-ENT-^*, from this study and recomputed denudation rates and sediment fluxes for the Entle River catchment, i.e. samples Ent^* and E-^*, from Van den Berg et al. (2012). “dd” stands for “decimal degrees”.

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Figure 4Location of CRN samples in the Entle catchment. CRN concentrations (CRN; ×10³ atoms g⁻¹), denudation rates (DR; mm kyr⁻¹) and sediment fluxes (SF; m³ yr⁻¹) displayed are discussed in the text. Values are available in Table 3. (a) Entle River and (b) Rossloch River catchments. The Schimbrig catchment is depicted by the hatched polygon within the Rossloch catchment in panel (b). Source of the DEM: Swiss Federal Office of Topography Swisstopo (2013).

When analysing the ¹⁰Be concentrations as a function of distance along the stream, we observe a clear and steady decrease in ¹⁰Be concentrations with increasing downstream distance (and catchment area) for the catchments not affected by active mass movements (Figs. 4, 5). This decrease in CRN concentrations could, at least in part, result from an increase in erosion rates downstream, as suggested in earlier work by Korup and Schlunegger (2007) and Van den Berg et al. (2012), or from a recycling of buried glacial sediment as the river cuts through 100 m thick unconsolidated glacial deposits in the central part of the catchment (Fig. 2).

Figure 5¹⁰Be concentrations (atoms g⁻¹) along the river network of the Entle catchment. Downstream distance is computed from the river source to the outlet of the Entle catchment. Samples from the earthflow-affected Schimbrig catchment are marked with a star.

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Figure 5 illustrates the strong contrast in the downstream change in ¹⁰Be concentrations between the earthflow-affected Schimbrig and nearby catchments. Downslope of the Schimbrig earthflow, the river samples CH-ENT-1, CH-ENT-5, and CH-ENT-8 have systematically low CRN concentrations that increase downstream. The latter is likely to reflect poor sediment mixing and long sediment residence time in the alluvial domain. At the confluence with the Rossloch River, the CRN concentration of the earthflow-affected catchment equals 1.34±0.27 atoms g⁻¹ (CH-ENT-8), which is at least 2 times lower than in the neighbouring catchment, i.e. 3.53±0.28 atoms g⁻¹ (CH-ENT-9).

5.1 Sediment fluxes at the millennial scale

Any variation in sediment mixing capacity or delivery from shielded or reworked sediment to the river channel may dilute or increase the concentration in ¹⁰Be in river sediments and lead to over- or underestimation of the catchment-averaged denudation rates and sediment fluxes. Therefore, the geomorphological context of the Entle catchment potentially has three caveats when using ¹⁰Be concentrations measured in fluvial sediments to draw conclusions about the propagation of sediment pulses throughout the landscape. First, the admixture of buried glacial sediments due to the incision of the Entle River in a 100 m thick layer of these deposits might lead to dilution of the ¹⁰Be signal in the lower reaches. However, in glacial deposits of nearby sites (Trub River catchment, about 15 km to the west of our study site), Norton et al. (2008) reported ¹⁰Be concentrations of glacial deposits reaching $\mathrm{0.76}\pm \mathrm{0.13}\times {\mathrm{10}}^{\mathrm{4}}$ atoms g⁻¹ at 8.5 m depth, and $\mathrm{3.58}\pm \mathrm{0.33}\times {\mathrm{10}}^{\mathrm{4}}$ atoms g⁻¹ at 1.5 m depth. As these values are about 15 % to 50 % higher than the catchment-wide CRN concentrations of nearby rivers, the incorporation of buried glacial material in the inner gorge is not the principal cause of the low ¹⁰Be concentrations that decrease systematically along the Entle River. Second, along with its small size, the presence of an active earthflow in the Schimbrig catchment might violate the assumption of steady-state denudation and sufficient sediment mixing, which are commonly assumed when converting ¹⁰Be concentrations of river sediment into catchment-averaged ¹⁰Be-derived denudation rates (e.g. Savi et al., 2014; Tofelde et al., 2018). We acknowledge that the dilution of ¹⁰Be concentrations in river sediment due to stochastic inputs from landslides might lead to an overestimation of CRN-derived denudation rates (Niemi et al., 2005; Yanites et al., 2009). Therefore, CRN-derived denudation rates and subsequent sediment fluxes presented hereunder will be taken as first-order or maximum estimates of the actual values (Puchol et al., 2014). Third, given that sediment production and delivery to the river network is typically stochastic in Alpine environments, the ¹⁰Be concentrations in river sediment might be highly variable in space and time as shown by Dingle et al. (2018) and West et al. (2014). Figure 5 illustrates the systematic variation in ¹⁰Be concentrations in the Entle River basin, and the strong coherence between our dataset and previously published data by Norton et al. (2008) and Van den Berg et al. (2012). As such, the effect of the stochastic input of earthflow-derived sediment is likely to be buffered at the scale of the Schimbrig and Rossloch catchments.

Ignoring samples from the earthflow-affected catchment, the long-term denudation rates correlate positively with downstream distance (Table 3; Figs. 4, 6), with values ranging from 160±30 mm kyr⁻¹ (E-9) to 340±70 mm kyr⁻¹ (Ent3-1). Characterized by a low variability, these values are akin to ¹⁰Be-derived denudation rates measured in similar Alpine tectonic settings (e.g. Norton et al., 2008). The increase in denudation rates with downstream distance along the Entle River is triggered by the ongoing relief rejuvenation and incision of the inner gorge after the LGM (Van den Berg et al., 2012). The data also indicate that the river network effectively evacuates sediments supplied to the river channel. Accounting for the drainage area at each sampling location, the long-term sediment fluxes (Table 3; Figs. 4, 7) show the same positive correlation with downstream distance. The sediment fluxes range from 600±100 m³ yr⁻¹ in upper first-order catchments (CH-ENT-6 and E-10) to 20 000±4000 mm kyr⁻¹ at the outlet of the Grosse Entle River (E-7a). This increase of 2 orders of magnitude in sediment fluxes downstream corroborates the efficient evacuation of sediment in the inner gorge.

Figure 6CRN-derived denudation rates (mm kyr⁻¹) in the Entle catchment against (a) downstream distance and (b) drainage area. Downstream distance is computed from the river source to the outlet of the Entle catchment. Samples from the earthflow-affected Schimbrig catchment are marked with a star. The grey lines connect the points that are hydrologically connected and part of the same fluvial system (Schimbrig, Rossloch, Kleine Entle, and Grosse Entle rivers). Denudation rate values on the y axis are shown on a logarithmic scale.

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The earthflow-affected catchments show a different pattern that deviates from the overall trend of increasing denudation rates with distance downstream and catchment area. In the first-order Schimbrig catchment, long-term denudation rates correlate negatively with downstream distance (Table 3; Figs. 4, 6). The denudation rates of the earthflow-affected first-order catchment are up to 1 order of magnitude higher than the rest of the Entle catchment, with values ranging between 300±100 mm kyr⁻¹ in the intermediate part (CH-ENT-5) and 5000±1000 mm kyr⁻¹ (CH-ENT-3) in the upper part of the Schimbrig catchment. The variability in denudation rates along the river is very high, with a 1 order of magnitude difference between minimum and maximum values, and it is spatially highly variable. For example, the denudation rate in CH-ENT-5 is lower than the sites directly up- and downstream of this sampling location, reflecting the stochastic character of the sediment delivery from the earthflow. The decrease in denudation rates with catchment area suggests that material initially displaced by the earthflow is not directly evacuated to the river network but remains on the slopes, hence accumulating ¹⁰Be atoms in the colluvial domain. Given that the catchment area of the first-order earthflow-affected catchments is small, the absolute sediment fluxes are low with values ranging between 120±40 and 900±200 m³ yr⁻¹. These long-term sediment fluxes computed for the Rossloch catchment, i.e. including the Schimbrig area, are 1 to 2 orders of magnitude lower than values computed in other parts of the Entle catchment (Figs. 4, 7).

Figure 7CRN-derived sediment fluxes (m³ yr⁻¹) along the river network of the Entle catchment. Downstream distance is computed from the river source to the outlet of the Entle catchment. Samples from the earthflow-affected Schimbrig catchment are marked with a star. Black square markers represent the sediment flux computed by Schwab et al. (2008) for the period 1962–1998. Grey lines present the downstream sequence of denudation rates along the Schimbrig, Rossloch, Kleine Entle, and Grosse Entle rivers. Sediment flux values on the y axis are shown on a logarithmic scale.

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The impact of landsliding on the long-term sediment dynamics can be evaluated by comparing the denudation rates of the two intersecting catchments at the confluence with the Rossloch River. At the outlet of the Schimbrig catchment, the denudation rate, i.e. 600±200 mm kyr⁻¹ (CH-ENT-8), is at least 2 times higher than in the neighbouring catchment, i.e. 210±50 mm kyr⁻¹ (CH-ENT-9). The difference in denudation rates between the two headwater catchments illustrates that the sediment dynamics of both catchments were probably very different over the last thousands of years as a function of the stochastic input of sediment from landslides (Fig. 1). When accounting for their catchment area, the sediment fluxes are very similar though with values of respectively 290±80 m³ yr⁻¹ (CH-ENT-8) and 230±50 m³ yr⁻¹ (CH-ENT-9).

Figure 8Conceptual representation of the sediment fluxes over different timescales at the outlet of a first-order river catchment. (a) Periods of high hillslope activity due to a landslide sediment pulse, resulting in intermittent hillslope–channel connections and in sediment export to the river network at the annual scale. (b) Periods of low hillslope activity both at the annual and decadal scales, due to poor sediment availability on slopes.

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5.2 Temporal upscaling: the stochastic nature of landsliding

Characterized by a relatively gentle Alpine topography, the millennial geomorphic activity of the study area is moderate in intensity. In comparison, the average CRN-derived denudation rate is 270±140 mm kyr⁻¹ in similar surrounding areas, i.e. in the Alpine foreland, but increases to 900±300 mm kyr⁻¹ in the high crystalline Alps (Wittmann et al., 2007). Dendrogeomorphological data confirmed that the Entle River catchment has been affected by an active earthflow at least over the past 150 years (Lopez-Saez et al., 2017; Savi et al., 2013). Given the extent of its active part, i.e. ca. 0.5 km², the Schimbrig earthflow is a larger-than-average landslide (Stark and Hovius, 2001). Therefore, according to the magnitude–frequency distribution of landslides (e.g. Hovius et al., 1997), this type of phenomenon is generally relatively infrequent, i.e. between 10⁻² and 10⁻³ events km⁻² yr⁻¹. The mean annual horizontal displacements (Fig. 1a) that we measured within the earthflow, i.e. ca. 6.30 m yr⁻¹ for the period 2014–2015, are relatively high in comparison with decimetric displacements reported in the western Slovakian Carpathians (Prokešová et al., 2014), submetric (< 2 m yr⁻¹) displacements reported for the Eel earthflow in California (Mackey et al., 2009), and metric to decametric displacements for the Super-Sauze landslide in southern French Alps (Niethammer et al., 2012). The toe of the earthflow experienced a downslope movement of ca. 55 m between June 2014 and October 2015 (Fig. 1b, Clapuyt et al., 2017). Despite the important internal reorganization of the Schimbrig earthflow, its net sediment budget is roughly in equilibrium: sediment transfer from the colluvial to the fluvial domain (Fig. 1c) is minimal over the period 2013–2015. The sediment mobilized by the earthflow is buffered in the colluvial domain, due to the decoupling of the hillslope–channel system (Fig. 1d) over the annual timescale. In contrast to the limited annual sediment flux (period 2013–2015) of the Schimbrig catchment, its decadal sediment flux (period 1962–1998) equals 13 000±2000 m³ yr⁻¹ (Table 2; Fig. 7). The decadal sediment flux is 2 orders of magnitude higher than the sediment fluxes computed at the millennial timescale over the same spatial extent, i.e. 290±80 m³ yr⁻¹ (CH-ENT-8). We note here that the potential overestimation of ¹⁰Be-derived denudation rates due to the addition of ¹⁰Be-poor material from the earthflow (discussed in Sect. 5.1) does not affect our interpretation.

The sediment fluxes measured over different timescales reveal the episodic character of sediment production, delivery, and transport out of first-order Alpine catchments, such as the Schimbrig and Rossloch catchments (Fig. 1). Landslides such as the Schimbrig earthflow generate sediment (Fig. 1a) that is temporarily stored in the colluvial domain (Fig. 1b) and continues to accumulate ¹⁰Be nuclides during storage. During short phases when hillslope and channel systems are coupled, the colluvial deposits are evacuated out of the first-order sediment stores. The discrepancy between decadal and millennial sediment fluxes illustrates that these phases of hillslope–channel geomorphic coupling are short-lived and intermittent and interrupt long periods of largely uncoupled colluvial and fluvial geomorphic systems (Fig. 8). During most of the time, the first-order catchments are transport-limited, and sediment dynamics in the headwaters are uncoupled from the fluvial systems.

5.3 Spatial upscaling: the importance of landsliding for sediment budgets

Episodic landslides, such as the Schimbrig earthflow, have the potential to mobilize large quantities of sediment at annual or decadal timescales. The average sediment flux at the decadal scale (1962–1998) out of the Schimbrig catchment, i.e. 13 000±2000 m³ yr⁻¹ (Table 2; Fig. 7), represents about 65 % of the average sediment flux out of the Entle catchment at the millennial scale, i.e. 20 000±4000 m³ yr⁻¹ (E-7a; Table 3; Fig. 7). This illustrates that landslide-affected catchments can act as principal point sources of sediment, as a sub-catchment covering 1 % of the area can provide 65 % of the total sediment flux. The higher-order river network, i.e. the Kleine and Grosse Entle rivers, attenuates decadal sediment pulses through the sediment cascade, during which subsequent erosion and deposition occur over centennial timescales. The propagation of the sediment pulses (from, e.g., landslides) across the channel network is largely controlled by the hillslope–channel geomorphic coupling and the transport capacity of the fluvial systems. The latter act as non-linear filters that smooth out spikes produced by episodic landslide disturbances as also suggested by Jerolmack and Paola (2010). In this sense, we can consider the episodic supply of sediment from landslides during intermittent phases of hillslope–channel coupling as noise that is averaged out when considering sediment fluxes at longer timescales and larger spatial scales. As our data show, one single disturbance (such as an earthflow) does not necessarily have an impact on the long-term sediment budget of first-order catchments. Rather, it is the cumulated effect of multiple landslides, which are intermittently connected to the channel network at the decadal scale, along with sediment transport, that may regulate sediment fluxes at the regional spatial scale over the millennial timescale.