the Creative Commons Attribution 4.0 License.
the Creative Commons Attribution 4.0 License.
Recession analysis revisited: impacts of climate on parameter estimation
David E. Rupp
Clément Roques
John S. Selker
Recession analysis is a classical method in hydrology to assess watersheds' hydrological properties by means of the receding limb of a hydrograph, frequently expressed as the rate of change in discharge ($\mathrm{d}Q/\mathrm{d}t$) against discharge (Q). This relationship is often assumed to take the form of a power law $\mathrm{d}Q/\mathrm{d}t=a{Q}^{b}$, where a and b are recession parameters. Recent studies have highlighted major differences in the estimation of the recession parameters depending on the method, casting doubt on our ability to properly evaluate and compare hydrological properties across watersheds based on recession analysis of $\mathrm{d}Q/\mathrm{d}t$ vs. Q. This study shows that estimation based on collective recessions as an average watershed response is strongly affected by the distributions of event interarrival time, magnitudes, and antecedent conditions, implying that the resulting recession parameters do not represent watershed properties as much as they represent the climate. The main outcome from this work highlights that proper evaluation of watershed properties is only ensured by considering independent individual recession events. While average properties can be assessed by considering the average (or median) values of a and b, their variabilities provide critical insight into the sensitivity of a watershed to the initial conditions involved prior to each recharge event.
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Accurate representations of watershedscale hydrological processes are urgent in a global and anthropogenicchange perspective. Streamflow recession analysis has been routinely used for about half a century to assess watershed properties (e.g., Brutsaert and Nieber, 1977; Kirchner, 2009; Mcmillan et al., 2014) and more recently their vulnerability to climatic and anthropogenic factors (Berghuijs et al., 2016; Brooks et al., 2015; Buttle, 2018; Fan et al., 2019). Recession analysis is commonly done by plotting the time rate of change in discharge $\mathrm{d}Q/\mathrm{d}t$ vs. discharge Q with bilogarithmic axes. Theory for an idealized single aquifer predicts a power law relationship with parameters a and b (Brutsaert and Nieber, 1977; Rupp and Selker, 2005).
However, it has long been recognized that the accuracy in the estimation of those parameters is highly sensitive to the methods used (Chen et al., 2018; Dralle et al., 2017; Roques et al., 2017; Rupp and Selker, 2006a; Santos et al., 2019; Stoelzle et al., 2013).
Two categories of parameter estimation methods are based on: (1) the aggregation of all observations in the space of $\mathrm{d}Q/\mathrm{d}t$ vs. Q, hereafter referred to as the “point cloud”, to describe the average watershed behavior and (2) the identification of individual recession events in the space of $\mathrm{d}Q/\mathrm{d}t$ vs. Q to look at the variability of a watershed's response. There is a long history of recession analysis parameter estimation using the point cloud beginning with Brutsaert and Nieber (1977), and it remains common (e.g., Buttle, 2018; Liu et al., 2016; Meriö et al., 2019; Ploum et al., 2019; SánchezMurillo et al., 2015; Stewart, 2015; Vannier et al., 2014; Yeh and Huang, 2019). In recent literature there has been a shift toward using individual recessions to estimate recession parameters (Basso et al., 2015; Karlsen et al., 2018; Roques et al., 2017), and Santos et al. (2019) go as far as to question the validity of point cloud estimation methods.
When Brutseart and Nieber (1977) first proposed their recession analysis method, aquifer recession behavior was identified by fitting a lower envelope to the point cloud, thus assuming small values of $\mathrm{d}Q/\mathrm{d}t$ for a given Q represent aquifer discharge flow, and anything larger has contributions from faster pathways such as overland flow. This lowerenvelope (LE) method of estimating recession analysis parameters was shown to be highly subject to artifacts arising from measurement noise and recording precision (Rupp and Selker, 2006a; Troch et al., 1993), and improvements to fitting a lower envelope have been proposed (Stoelzle et al., 2013; Thomas et al., 2015). An alternative fitting method wherein b was estimated as the best linear fit to the point cloud was introduced by Vogel and Kroll (1992) as the central tendency (CT). The central tendency method was adapted by Kirchner (2009) to address the undue weight of highly uncertain extreme points. Kirchner (2009) also suggested fitting a polynomial function to averages within bins of the cloud data. All of these point cloud fitting approaches fundamentally treat each computation of $\mathrm{d}Q/\mathrm{d}t$ and Q as reflecting a single average underlying curve, with deviations from a single curve effectively treated as noise. In other studies, data have been subset by season or month (e.g., Szilagyi et al., 2007; Thomas et al., 2015) to examine seasonal variations in the recession characteristics with the subsets still treated to point cloud analyses.
In contrast, the variability in watershed response to individual recharge events can be depicted by fitting recession parameters to individual recession events. Several authors have observed that individual recessions had greater b values than the point cloud did (Biswal and Marani, 2010; McMillan et al., 2011, 2014; Mutzner et al., 2013; Shaw and Riha, 2012); a larger value of b indicates a time rate of decline that decreases more quickly with decreasing streamflow. Consistent with these studies, we have also observed individual recessions that have a larger b value than the point cloud fit across watersheds in the Oregon Cascades. As an example, we present in Fig. 1 recessions for Lookout Creek, Oregon, USA, using daily discharge data (m^{3} s^{−1}) from 1949 to 2016 (USGS station no. 14161500; United States Geological Survey) (Johnson and Rothacher, 2019; obtained from USGS, 2019). In the 66 years of data presented, a total of 1309 recession events are identified with an average of 19 events per year. It is clear that values of b for individual recession events tend to be larger than b for the point cloud, particularly at lower discharges. In this example, individual event selection criteria include recessions lasting longer than 5 d, starting 1 d after the peak to exclude the influence of overland flow and ending at the next precipitation event, following other studies (Biswal and Marani, 2010; Shaw and Riha, 2012). The b parameter estimated using point cloud analysis (binning average method; BA) is smaller (b=1.5) compared to the median of b values from the individual recessions (b=2.8 with 50 % of individual recessions taking values from 2.0 to 4.7; see the color bar of Fig. 1). The frequency distribution of the b parameter from the individual recessions is skewed right and roughly lognormal, which suggests that b from the point cloud does not represent an average or “master” recession behavior.
For a given discharge range in Fig. 1, there appears to be multiple individual recessions with similar values of b that are horizontally offset, implying a common b but a variable a value. The offset of individual recession events suggests that antecedent conditions may be influencing the location of the recession curves (e.g., Rupp et al., 2009), consistent with various theoretical definitions of a that include the aquifer saturated thickness at the onset of the recession as a parameter (Rupp and Selker, 2006b). Many authors have associated the pattern of shifted individual recessions with seasonality (Bart and Hope, 2014; Dralle et al., 2015; Karlsen et al., 2018; McMillan et al., 2011; Shaw and Riha, 2012; Tashie et al., 2019). Authors describe a generally sinusoidal relationship with larger a values associated with summer months (Dralle et al., 2015; Shaw and Riha, 2012) and a weaker seasonal relationship for values of b (Karlsen et al., 2018; Tashie et al., 2019). Seasonality associated with meteorological conditions may well be used as a predictor of a or b, but seasonality alone fails to address the underlying climatic conditions that control streamflow recession. Instead of describing the variability between events based on seasonality as a proxy, parameter estimation should focus on antecedent and meteorological conditions that control streamflow recession in order to form a more comprehensive physically based understanding of recession parameters (e.g., Bart and Hope, 2014; Karlsen et al., 2018).
This paper explores the source of the offset (ln(a)) and slope (b) on individual recessions. Using a time series of synthetic hydrographs with known parameters, we compare different methods for estimating the recession analysis parameters and the sensitivity to the method on the frequency and magnitude of events that make up the hydrograph. We are particularly concerned with how individual recessions collectively create the emergent point cloud and seek to describe how recession parameter estimation of the point cloud is affected by the distribution of individual recessions.
This section presents methods for (1) the definition of three synthetic hydrographs, (2) the description of recession extraction from the hydrograph, and (3) the comparisons between four fitting methods for parameter estimation applied to a discharge time series for Lookout Creek.
2.1 Synthetichydrograph methods
This paper makes use of synthetic hydrographs to explore factors that change b for individual recession events as well as the interarrival times of individual events that create the point cloud. Our synthetic hydrographs are created by defining individual recession events and stitching them together to create a long time series. Synthetic hydrographs were chosen for this study because each individual recession can be definitively identified, as the characteristics are known, which is unrealistic when considering real watersheds. Furthermore, the synthetic hydrographs can be specified to directly compare different climatic controls without the confounding variables traditionally associated with real watersheds. For these purposes, the specifications of the synthetic hydrographs were chosen to explore the effects of the magnitudes and frequency of recharge events on the recession analysis parameters from collective vs. individual recessions.
The falling limb of the hydrograph is assumed to follow a power law following Eq. (2) (Dewandel et al., 2003; Drogue, 1972; Rupp and Woods, 2008):
where Q is the discharge, Q_{0} is the initial discharge prior recession at t=0, t is the time in days since the recession started, τ is a characteristic timescale, and w is the dimensionless power law decay exponent. Equation (2) can be expressed as Eq. (1) with $a=w/\left(\mathit{\tau}{Q}_{\mathrm{0}}^{\mathrm{1}/w}\right)$ and $b=(\mathrm{1}+w)/w$.
Holding τ constant and varying the initial condition Q_{0}, results in a hysteretic relationship of $\mathrm{d}Q/\mathrm{d}t$ vs. Q, in contrast to a constant a value which produces a single nonhysteric relationship. Defining a as a function of initial conditions has both theoretical (e.g., Rupp and Selker, 2006b) and empirical (e.g., Bart and Hope, 2014) support. The constancy of τ is not well established, but we assume it is constant for the scenarios examined here. Consequentially, a constant τ results in a variable value for a that is inversely proportional to the initial discharge. An inverse relationship is consistent with theoretical expectations for nonlinear aquifers (b>1), where Q_{0} increases with increasing initial saturated thickness (see Figs. 2 and 3 in Rupp et al., 2006b). Though the particular timescale is not important to our objectives, we chose it to be 45 d. Brutsaert (2008) noted a tendency for τ to be near 45 d across a large number of basins when fitting Eq. (1) with b=1 to point cloud data. It remains to be seen whether a similarly narrow distribution of τ occurs for b not equal to 1.
A pulse recharge amount corresponding to a given Q_{0} can be calculated by integrating Eq. (2) from t=0 to t=∞. For w>1 (b<2), the recharge volume is
where D is the depth of recharge and A is the aquifer area. For w≤1 (b≥2), integrating Eq. (2) results in an infinite volume, so b>2 can only be sustained over a finite part of any recession. Values of b>2 have been derived from the physical theory for the early portion of a recession (Brutsaert and Nieber, 1977; Rupp and Selker, 2005) or can be obtained from recession curves over a finite time period while retaining physical realism by combining discharge from multiple linear (b=1) or nonlinear ($\mathrm{1}<b<\mathrm{2}$) reservoirs (e.g., McMillan et al., 2011). The effect on b of combining linear reservoirs in parallel (e.g., Clark et al., 2009; Gao et al., 2017; Harman et al., 2009) and series (e.g., Rupp et al., 2009; Wang, 2011) has received much more attention.
We compared three hypothetical time series generated with different assumptions about the distribution of the magnitudes and interarrival times of recharge events and the superposition of recession events (Table 1). The interarrival times are distributed lognormally (Cases 1 and 3) or uniformly (Case 2). Event magnitudes (as defined by Q_{0}) are either distributed lognormally (Cases 1 and 3) or have a constant magnitude (Case 2). Events are either independent of antecedent conditions (Case 1), or events are superimposed on antecedent conditions (Cases 2 and 3) (Table 1 and Fig. 2).
To generate the time series for Cases 1 and 3, independent recessions were created using a randomnumber generator for a lognormal distribution for event peak magnitude and duration for a total of 10 years of time series data. The lognormal distributions for event magnitude and duration are chosen for the synthetic hydrographs because the distributions for Lookout Creek are skewed right and roughly lognormal (Supplement Fig. S1), which is also consistent with other skewedright precipitation distributions in previous studies (Begueria et al., 2009; Selker and Haith, 1990). Recharge events were created with lognormally distributed interarrival times (μ=2.5, σ=1) and event magnitudes (μ=1 d, σ=1) where both values are normalized by timescale and the unit hydrograph respectively, resulting in dimensionless quantities. These values of μ and σ result in event lengths with a mean of 20 d and an average of 18 events per year. This value was chosen to be comparable to the 19 events per year identified in the Lookout Creek example. The distributions of both the interarrival times and event magnitudes are skewed right, representing the high frequency of smaller events and less frequent large events. Changing μ and σ will modify the amount of variability in individual recessions and could be further explored with different distributions in future research regarding the resulting variability in b. Case 2 assumes a constant event interarrival time ($\mathit{\mu}=\mathrm{450}/\mathit{\tau}$) and magnitudes (μ=1). The mean interarrival time of 10 d is intended to be comparable with the 19 events per year identified in the Lookout Creek example.
For Case 1, the individual recessions were combined to make a time series such that each event was concatenated onto the last event disregarding the antecedent flows. For Cases 2 and 3, individual recessions were superimposed on antecedent flows, appealing to the simplest model presented by the instantaneous unit hydrograph method (Dooge, 1973). We acknowledge that the framework for the instantaneous unit hydrograph as described in Dooge (1973) does not consider nonlinear reservoirs, but we use it as a simple representation to produce variability between recessions. We discuss the implicit assumptions of this model in the Discussions and Conclusions section. From Fig. 2, the baseflow from the first event, Q_{B}, is a simple continuation of the first recession. The underlying second event, Q_{C}, is defined by the second event's initial magnitude (constant in Case 2 and randomly generated in Case 3). The resulting flow, Q_{D}, is the sum of Q_{B} and Q_{C}.
As a result, Case 1 looks specifically at a time series events where the falling limb of each event maintains the same decay constant and the effect of having no antecedent baseflow influence on streamflow. By including baseflow to Case 2 but maintaining equal interarrival times and event magnitudes, we look specifically at the effect of antecedent conditions on individual recessions and the point cloud. Case 3 combines the distribution of event interarrival times and magnitudes of Case 1 with the baseflow conditions of Case 2, best representing the variability and interarrival times of individual recession events seen in Fig. 1 for data from Lookout Creek. Each case will address how the controls on the hydrograph affect the recession analysis plot and the estimates of a and b.
2.2 Recession extraction method
Recession extraction from observed hydrographs and the associated sensitivities to different criteria have been explored by Dralle et al. (2017), including minimum recession length and the definition of the beginning and the end of the event. For Lookout Creek, we used extraction criteria similar to those of other studies (e.g., Chen and Krajewski, 2016; Dralle et al., 2017; Stoelzle et al., 2013) and applied the same criteria prior to all fitting methods presented in Sect. 2.3 to isolate differences in calculated b values due to the fitting method only. An individual recession event duration must be longer than 5 d. Rainfall data can be used to identify noninterrupted recessions, but rainfall data will not available in all cases, so we rely on the hydrograph only. The start of the recession is defined as 1 d after the discharge peak to account for the presence of overland flow. The end of the recession occurs at the minimum discharge prior to an increase in discharge greater than the error associated with instrument precision for stage height of ∼0.5 cm, which translates into errors in discharge from ∼0.01–0.1 m^{3} s^{−1}, depending on the rating curve and the discharge level (Thomas et al., 2015).
For the synthetic hydrographs used in Sect. 3.2, events of any length were included; the recession start was selected at peak discharge because overland flow was not a factor; and the end of the recession was chosen as the time immediately before the next generated discharge peak.
2.3 Parameter estimation methods
Four methods of estimating representative recession parameters were evaluated: lower envelope, central tendency, binning average (Kirchner, 2009), and the median individual recessions (MI) (Roques et al., 2017). Linear regression in bilogarithmic space was used with each method for consistency across methods.
Because a change of hydraulic regime was suggestive in Fig. 1 between highflow ranges and lowflow ranges, recession analysis parameters were estimated for two flow ranges, early time and late time. Early time and late time describe a theoretical transition of flow regimes between highflow and lowflow ranges (Brutsaert and Nieber, 1977). To reduce the subjectivity of distinguishing between high and low flows, a breakpoint in discharge separating high from lowflow behavior was optimized to best represent the analytical solution. By separating the data into two subgroups, either smaller or larger than a defined breakpoint discharge, the bestfit line was determined for each subgroup. The location of the breakpoint is defined so the error between the observed ratio of b for the two subgroups and the theoretical ratio (b=3 for early and 1.5 for late give a ratio of 2) is minimized, theoretically defining the subgroup above the breakpoint as early time and the subgroup below the breakpoint at late time.
For each of the four estimated methods, parameters were estimated for the earlytime and latetime behavior separately. For the LE method, b was fixed to 3 and 1.5 for early and late time, respectively, following Brutsaert and Nieber (1977), and a was chosen such that 5 % of points were below the lower envelope (Brutsaert, 2008; Troch et al., 1993; Wang, 2011). It should be noted that using these values for b assumes that the groundwater discharge behaves like discharge from a single, initially saturated, and homogenous Boussinesq aquifer. An alternative method to fitting the lower envelope without a predefined value of b was introduced by Thomas et al. (2015) using quantile regression to estimate both a and b, but it was not used in this study. For the CT method, the fit included all points of $\mathrm{d}Q/\mathrm{d}t$ vs. Q as unweighted (Vogel and Kroll, 1992). For the BA method, bins spanned at least 1 % of the logarithmic range, and a line, instead of the polynomial suggested by Kirchner (2009), was fit to the binned data. We dispensed with the inversevariance bin weighting used by Kirchner (2009) to account for data noise when we applied the method to the synthetic recessions because some bins contained few points with very low variance and therefore were weighted excessively. For the MI method, parameters were estimated for individual recessions following Roques et al. (2017), and the medians of a and b were calculated. In all cases, the time derivative of $\mathrm{d}Q/\mathrm{d}t$ was computed using the exponentialtimestep (ETS) method proposed by Roques et al. (2017).
3.1 Parameter estimation for observed recessions (Lookout Creek)
In Fig. 3 we display the recession plot stacking all individual recessions resulting in the formation of the point cloud. The different fitting strategies revealed that the LE, CT, and BA methods all fit to the point cloud and result in different values of b when applied to the observed daily averaged streamflow for Lookout Creek: earlytime values of b are over 50 % larger for LE (fixed at 1.5) than CT and BA, and latetime values of b are 50 % and 25 % larger for LE than CT and BA, respectively (Fig. 3 and Table 2). The CT and BA methods are fairly consistent with each other for both early and late time, whereas the predefined theoretical b values for the LE appear to provide poorer fits to the point cloud.
More importantly, parameter estimation differs greatly whether the point cloud or individual recessions are used. The latetime b value which defines the lowflow baseflow regime is 6 times greater for MI than CT (Table 2). Using the MI method, the b value is larger than any other method for both early and late time.
3.2 Synthetichydrograph results
Based on the similar results from BA and CT methods discussed above, and the questionable practice of setting an early and latetime b a priori as we did in the LE method, hereafter we use the BA method to represent the point cloud recession parameter estimation when comparing it to the MI method using individual recessions.
The recession decay exponent w in Eq. (2) was set to 1.2; distinct values of w were not used for early and late time. This value for w results in b=1.8 for an individual synthetic recession, which is near the reported median of individual b values of 2.0 in Biswal and Marani (2010) and 2.1 in Shaw and Riha (2012) and Roques et al. (2017), though less than the median individual b of 2.8 for Lookout Creek.
The b values and the offset of individual recessions resulting from Eq. (1) are both functions of w. A larger b value indicates a more stable baseflow discharge (a slower decline rate for given discharge). For a given value of b and τ, a varies inversely with ${Q}_{\mathrm{0}}^{\mathrm{1}/(b\mathrm{1})}$. Decreasing w results in larger values of b while also increasing the offset between individual recessions, resulting in a larger range of a values and a more scattered point cloud. In contrast, as w approaches infinity, the offset is minimized as b goes to 1, representing an exponential fallinglimb recession in time (Rupp and Woods, 2008). In this special case, all of the individual recessions overlap with constant a (i.e., there is no offset among individual recessions lines). While b=1 is interpreted as a linear reservoir according to traditional theory and is a convenience often assumed, this result suggests that a condition where b=1 and a is a constant is not consistent with the existence of a point cloud, except to the degree at which observation error introduces noise into the recession hydrograph or other pathways (e.g., overland flow) contribute to the flow in the stream. In summary, the more linear the response is (the closer b is to 1), the smaller the offset is, whereas the more nonlinear the response (the larger the b) is, the greater the offset and thus the more different the parameter estimations between the point cloud and individual recession methods will be. The three following cases using synthetic hydrographs are intended to highlight the offset of the individual recession curves.
3.2.1 Case 1
Recession analysis of a hydrograph with lognormally distributed event interarrival times and peak discharge with a constant fallinglimb decay constant (no baseflow represented) results in individual recession events with the same b, horizontally shifted based on the initial discharge (Fig. 4). In this case, the peak flow of the event is the only source of variability in the recession parameter a. The variable event magnitudes result in individual events located over a range of ln(Q) values, whereas if the same flow magnitude was preserved for each event, each individual recession would plot on top of one another creating a single line without a point cloud. The variable event interarrival times change the duration of an event, with longer events occurring over a greater range on the y axis. In this simple hydrograph, parallel individual recessions are present, and all have b=1.8, as expected. The value of b is estimated at 1.3 considering the point cloud, which appears to be significantly less than imposed individual b value of 1.8. This underestimation results from the offset between individual recessions based on the range of initial discharges.
To examine the sensitivity of parameter estimation to recession extraction criteria, we evaluated how choosing the start of the recession (i.e., the time elapsed since peak discharge) affects the value of a when using the point cloud method. Whether we chose 0, 1, or 2 d following peak discharge, a from the point cloud a was 0.17 (–), and b was 1.3 (–).
3.2.2 Case 2
The superposition of recession events accounts for the effects of antecedent baseflow. The superposition changes the effective w of the falling limb of the hydrograph as the event recession is added to the antecedent events, resulting in a variable b value across the individual recessions (Fig. 5). The median b value represented is 3.25 with a range of 2.56 to 3.41 (quantile range represented in the color bar of Fig. 5). The point cloud b of 2.35 falls outside of the range of b values for individual recessions. Superposition results in a larger b value than what would arise from nonsuperposition. Steeper recessions (higher b value) are associated with events with higher baseflow contribution given the same addition of flow. By including antecedentflow conditions, neither a nor b is preserved between individual recessions.
3.2.3 Case 3
A hydrograph more representative of realcase conditions includes variable interarrival times and event magnitudes from Case 1 and baseflow antecedent conditions from Case 2 (Fig. 6a). These complexities result in a recession plot where the individual recessions represent the variability in watershed response represented by the hydrograph (Fig. 6b), where a and b are different between individual recessions. As with Cases 1 and 2, the median individual b value (3.3) is greater than the point cloud b value (2.0). The minimum individual b value is 1.9 with a maximum of 8.5, while the point cloud b is near the low end of the range of individual b values (see the color bar of Fig. 6). The similarity of features of Figs. 6b and 1 are noteworthy. Though many of the observed recessions in Fig. 1 are slightly curvilinear (in the log–log space), the synthetic recessions are power laws; in both cases there is a tendency for recessions with lower initial discharges to have higher values of b, yet still many instances of recessions have similar initial discharges but different values of b.
In the 42 years since Brutsaert and Nieber (1977) proposed their recession analysis, it has provided a seemingly simple analytical method for estimating basinscale hydrologic properties. However, recent studies have highlighted the sensitivity to estimation methods on the recession parameter values and to the resulting interpretation of average watershed behavior. This paper explores the effect of the distribution (in time and in magnitude) of individual recessions on parameter estimation and compares that to the parameter estimation from collective recessions (i.e., the point cloud). The four estimation methods considered were the lower envelope, central tendency, binning, and individual recession method. Because of the poorer apparent fit and problems pointed out from previous studies when using the lower envelope and central tendency methods, we chose to use the binning method to compare with results from the individual recessions method for a set of synthetic case studies.
We hypothesize that the climate controls the distribution of individual recessions in bilogarithmic plots of $\mathrm{d}Q/\mathrm{d}t$ vs. Q. This distribution can be related to the variability in recession analysis parameters. Using the three synthetic case studies, we examine the effects of event interarrival time, magnitude, and antecedent conditions on the distribution of individual recession events that comprise the pattern of collective recessions.
We conclude that recession analysis performed on collective recessions does not capture average watershed behavior, regardless of the fitting method. The point cloud is an artifact of the variability of the individual recessions, including the event interarrival times and distribution of magnitudes. Individual recessions with the same b but different a values can be produced by varying the initial discharges (Case 1); variability of b for individual recessions can be produced by superimposing events on antecedentflow conditions (Case 2); and different recession event lengths with different b values can be produced by including variable event interarrival times and magnitudes (Case 3).
For Case 1, the recession analysis parameter a is equal to $w/\left(\mathit{\tau}{Q}_{\mathrm{0}}^{\mathrm{1}/w}\right)$, and thus the intercept of the individual recession curves will scale with Q_{0}. The result is a collection of individual recession curves that are horizontally offset based on the initial discharge, producing a smaller b value for the point cloud compared to the individual recessions. Case 1 illustrates that the slope of individual recession events can be greater than the bestfit line through the point cloud, consistent with previous studies (Biswal and Marani, 2010; Mutzner et al., 2013; Shaw and Riha, 2012). However, the point cloud in Case 1 is generated by a collection of multiple individual recessions, all with the same slope, and does not have the variability in b values presented in these previous studies and shown for Lookout Creek in Fig. 1. Cases 2 and 3 use superposition of antecedentflow events that consequentially changes the individual b values, providing a possible explanation for the variability in b values for individual recessions. For Case 2, the superposition of events takes account of antecedent conditions which results in a distribution of individual b values despite the decay exponent w being fixed. For Case 3, the horizontal offset of individual recessions from Case 1 and the effects of antecedent conditions from Case 2 result in the recessions with variable individual b values that are horizontally offset to create a pattern similar to that observed in a real watershed.
While the mean b for individual recessions in Case 1 is a direct consequence of the value of w used in Eq. (2), this is not true when the discharge from each application of Eq. (2), which we call an event, is superimposed on the antecedent flow, as in Cases 2 and 3. This superposition of events results in a range of individual recession b as often observed in the literature (Basso et al., 2015; Biswal and Marani, 2010; Mcmillan et al., 2014; Mutzner et al., 2013; Shaw and Riha, 2012); thus it appears that the straightforward superposition of events can recreate the watershed behavior. However, there is a key underlying assumption of this superposition that is inconsistent with a real watershed. To help describe this inconsistency, we can compare two distinctly different conceptual models of watersheds. The first, and very frequently used, model is a single bucket with an outlet near the bottom. The bucket contains a porous medium whose properties may vary with depth to create a variety of nonlinear outflows. Each new recharge event adds to the preexisting storage of water in the bucket. The second model is the one used for Cases 2 and 3: each new event adds water to a new and independent bucket, and the outflows from all buckets are aggregated. Both conceptual models have components that are patently unrealistic when applied to natural watersheds, but, remarkably, the latter model produces a distribution of recession events in the space of $\mathrm{d}Q/\mathrm{d}t$ vs. Q that is more like what is observed in the Lookout Creek basin and others (Mutzner et al., 2013; Shaw and Riha, 2012). This finding reveals key information about the subsurface plumbing system of the basin and its dynamics that could be explored with models with a higher degree of realism. We acknowledge that there are other ways to create watershed memory that would also generate variability in apparent recession parameters and would be worthwhile to consider. For example, following previous works that have shown that multiple linear reservoirs can generate power law recessions (Clark et al., 2009; Harman et al., 2009), one could explore combinations of parallel linear reservoirs with varying sizes and recession constants under timevarying recharge. However, based on the results of Harman et al. (2009) using periodic recharge events, it is not clear that this would lead to a distribution of recession curves of varying b values like what is seen in Fig. 1. A similar, albeit more complicated, exercise could also be done with combinations of parallel nonlinear reservoirs with distinct recession parameters.
An additional important simplifying assumption of this study is the use of a constant timescale τ for each individual event. Previous studies that have examined timescales across basins by setting b=1 and estimating τ from the point cloud (Brutsaert, 2008; Lyon et al., 2015). However, given the questionable of the validity of the point cloud estimation methods, additional studies of the variability of the timescale among individual recession events and across the basin should be done.
We show how the point cloud pattern does not arise from watershed properties alone. The consequence is that parameters estimated from the point cloud do not represent watershed properties. In all three synthetichydrograph representations, the median individual recession b is significantly greater than b from the point cloud. Additionally, it is possible for the point cloud b to be smaller than the minimum individual recession b indicating the point cloud fit represents a behavior outside the range of watershed responses represented by individual recession events. In contrast to the point cloud, individual recession analysis provides insights into the average and variability of watershed responses which is highly dependent on the memory effect of the watershed. The variability in individual responses gives insight into watershed complexities including heterogeneity in topography, geology, and climate. Watersheds may present large variability in geology and so hydrogeological conditions such as unconfined or confined aquifers, interbasin groundwater flows, high spatial hydraulic conductivity variability, depthdependent hydraulic conductivity, or largescale discontinuities. As a result, there are still opportunities to further characterize the variability in watershed responses and the associated variability in individual b values to improve streamflow prediction using recession analysis.
A strength of the criticalzone community is the ability to create a global analysis by comparing across studies (Brooks et al., 2015; Fan et al., 2019). However, a lack of consensus for a standard method for recession analysis procedures exists and thus inhibits recession analysis studies from being widely compared. If streamflow analysis is to be included in a global analysis, results need to be comparable across scales and observatories. There is a need for a common method employed to compare the average and variability in watershed responses. Because estimated parameters may differ greatly by estimation method, misinterpretation of hydrological properties and incorrect predictions within the critical zone are possible. When using the point cloud in particular, a smaller recession parameter b at a late time could be, and has been, interpreted to imply greater basin vulnerability to drought (e.g., Berghuijs et al., 2016, 2014; Yeh and Huang, 2019). However, a more stable baseflow is implied by the distribution of b from the individual recessions and its median b value, which can be much larger than what is estimated from the point cloud. We suggest that the use of collective recession analysis should be avoided in favor of individual recession analysis as the standard to describe the average and variability in watershed response. The methods employed for recession analysis certainly require more attention. Correct methods are critical to understand the underlying hydrology and thus the interpretation of a watershed's vulnerability to climate change.
The streamflow record for Lookout Creek is freely available from the USGS website (https://waterdata.usgs.gov/nwis/uv?site_no=14161500; USGS, 2019). The source code for the exponentialtimestep method is available by request (Roques et al., 2017). Randomly generated lognormal event magnitudes and interarrival times presented in this paper for Cases 1 and 3 are available at: https://doi.org/10.4211/hs.e3c159631acd470cbeef5fa1abe0142e (Jachens, 2020). Respective codes can be obtained from the corresponding author.
The supplement related to this article is available online at: https://doi.org/10.5194/hess2411592020supplement.
ERJ, DER, and JSS were involved in conceptualization. ERJ and CR developed the methodology and performed the analysis. ERJ prepared the paper with contributions from all coauthors.
The authors declare that they have no conflict of interest.
This work was supported by the National Science Foundation awards to the Center for Transformative Environmental Monitoring Programs (nos. 1551483 and 1440506).
This paper was edited by Daniel Viviroli and reviewed by Michael Stoelzle and one anonymous referee.
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