The Nesselbach catchment (51°26^′54^′′ N, 9°22^′59^′′ E) is located in the geological region of the “Westhessische Senke,” part of the Central Uplands, Germany. It directly drains into the Esse River, a tributary of the Weser. The Nesselbach has a mean discharge of 8.1 Ls-1 and a stream length of 1.8 km from its source to the monitoring station. The monitored catchment area covers 3.2 km2 and consists of 65 % agricultural area, 25 % mixed forest, and 10 % settlement/commercial areas. Some agricultural fields are equipped with drainage systems that directly discharge into the stream. The drainage system in the area could not be monitored and seemed to be self-organized by the farmers. One drainage outlet could be identified as a road drainage and was located near the point of measurement but was never observed active. There is no data on the drainage system nor are there any official maps of the drainage network. Elevation in the monitored area ranges from 173 to 306 m, as shown in Fig. 1. Soils are predominantly classified as Vertisol (90 %), with Cambisol and Leptosol found in the forested regions. The underlying bedrock comprises red Sandstone and Muschelkalk. Meteorological data were collected from a WMO-compliant weather station (Thies Clima, DL-15) near the catchment area (51°28^′2^′′ N, 9°22^′41^′′ E) from August 2020 to November 2022 (Spill et al., 2023). The area has a temperate climate, with a measured mean annual air temperature of 8.6 °C and an annual precipitation of 635 mm for the year 2021. During the monitoring period, the Nesselbach catchment experienced relatively low precipitation (635 mma-1) compared to the multi-annual mean of 792 mma-1 (DWD 2025). Precipitation was measured by a tipping bucket rain gauge.

All necessary parameters, except climate parameters, were measured at the same location (Fig. 1), where the Nesselbach crosses a road and flows through a 1 m inner diameter concrete pipe. The measurement took place between February 2021 and June 2022, the setup had to be removed until July 2022 due to institutional restrictions. In situ devices were installed at the end of the pipe together with a small weir, ensuring that all devices were always submerged. NO3- concentrations were measured in situ using a UV-VIS probe (S::can Spectro::lyzer) with a temporal resolution of 5 min and an automated cleaning procedure, utilizing compressed air. Continuous measurements were complemented by biweekly grab samples for calibration purposes (Fig. S1 in the Supplement), and additional samples taken during precipitation events. Discharge was determined by measuring water depth and velocity using an ultrasonic probe (Nivus), employing cross-correlation techniques to detect the flow velocity of particles in the water. The temporal resolution of the measurement was set to 5 min. Due to the often highly scattered discharge data, caused by low particle density in the water, smoothing of the discharge curve was performed using Spearman correlation between discharge and water depth, followed by applying a Nadaraya-Watson density estimator with a Gaussian kernel to the data. The smoothed discharge was assessed using the Nash–Sutcliffe Efficiency, a flowchart and an example is provided in Fig. S2. Stream water samples during precipitation events were collected using an automatic sampler (ISCO) with a resolution of 15 min. The automatic sampler, equipped with 24 bottles (1000 mL), was activated by a water level actuator (ISCO) at an activation threshold of approximately 5 mm precipitation equivalent. The activation and deactivation of the automated sampler also mark the beginning and endpoint of the events we use for the NCL-analysis. Events start with the incoming signal from the actuator to the sampler and end with signal termination. This approach was getting more precise over the course of the sampling campaign, while the optimal position of the actuator was approximated by trial and error. Every activation and deactivation signal was compared to the water level and precipitation measurement to minimize activation error. Due to the maximum capacity of the automated sampler of 24 bottles and frequent errors during sampling, we only considered events with at least 6 consecutive samples. Samples were analyzed in the laboratory using UV-VIS photometry for nitrate, major ions and Ptot concentrations. Stable water isotope ratios in the discharge during precipitation events were sampled at a resolution of 15 min. For the determination of the background signal biweekly grab samples and, if possible, anticipated grab samples before a precipitation event, were taken. Isotope samples in precipitation were collected using a tipping bucket coupled with a sequential precipitation gauge with a 5 mm resolution, based on the design by Fischer et al. (2019). The isotopic signal of the collected 5 mm sample was aligned to the samples from the automated discharge sampler via the timestamps of both instruments. A cavity ring-down spectrometer (Picarro L2130-i) was used to determine isotope ratios. Electrical conductivity was measured every 5 min using an in-situ probe (HOBO). Major ions were also included into the testing of the new approach. The available data covers major ions for 8 events.

The two-component hydrograph separation is based on the deuterium signal in precipitation and discharge during events (Clark and Fritz, 1997): 1Qpre=Qtδt-δrδpre-δr where Qpre equals the volume of pre-event water, Qt the discharge at a given timestep t, δt the isotope composition in the discharge at a given timestep, δpre the isotope composition of the pre-event discharge and δr the isotope composition in precipitation. Due to the sub-hourly resolution of the event samples and the nature of the stable isotopes, it is possible to separate the hydrograph with very high precision. A dual isotope plot (in Fig. S3) was drawn to identify potential influences of evaporation on the stable water isotopes signal in the precipitation, but the dataset showed no such influence. Two samples had to be excluded from the analysis because their isotopic signals in precipitation were distorted and not clearly assignable to the discharge signal. This is exemplary for the difficulties coming with stable isotope hydrograph separation, besides already occurring technological challenges and cost effectiveness (e.g. Seeger and Weiler, 2014). Due to the spatial and temporal heterogeneous nature of precipitation (Allen et al., 2019), stable isotopes are only meaningful to use if enough data is available to identify different volumes of water. In best case scenarios, time series spanning years of data are available for the stable isotope signature of the groundwater, discharge and precipitation to account for all seasonal changes and to determine the isotopic fingerprints for robust solutions of Eq. (1) (Klaus et al., 2015). But since this is seldom the case, researchers have to be careful handling isotopic data and collect as many samples as possible for creating reliable datasets. In case of this study, the exclusion of two samples was due to a leakage in the sequential rain gauge, leading to mixing and therefore dampening of the isotopic fingerprint. There were 13 events suitable for stable isotope-based hydrograph separation. These events consisted of at least 6 consecutive discharge isotope samples [15 min time increment] and successfully sampled clearly assignable precipitation samples. For a better understanding of the differences in the event dynamics, the events were clustered by k-means cluster analysis, a common and classical method (Lloyd 1982). Cluster analysis can be used to categorize the discharge functions into groups such as fast reacting curves, bi- or multi-modal functions and strength of function volatility (Bloomfield et al., 2015; Wunsch et al., 2022). K-means algorithm is based on the following assumption (Lloyd 1982): 2J=∑i=1k∑xj∈Si||xj-μi|| where J equals the target function, k equals the number of pre-identified clusters, x  equals the datapoints, μ equals the mean values of each cluster S. The k-means algorithm aims at minimizing the squared distance of the datapoints to the cluster means. After necessary normalization of the data, a Scree-plot (in Fig. S4) was drawn to visually identify the best number of clusters (Cattell 1966). The k-means algorithm was computed in R (R Core Team 2025). Cluster pairs comprised the following parameters: precipitation [mm] and event water portion [%], function mean volatility [Ls-1] and mean rate of change [Ls-1], function mean volatility [Ls-1] and area of the best power function fit of the NCL function [-].The function mean volatility and mean rate of change of the hydrographs are mathematical parameters delineated from the empirical discharge hydrograph. We calculated these parameters with the sole purpose of grouping the hydrographs by their mathematical behavior. Comparing the mean rate of change, or the abruptness of rising and falling function behavior, is the first step to sorting the hydrograph behavior. To delineate the mean rate of change of a discharge function (Fig. 2), the first derivative of each discharge function k was calculated and its values averaged to compare the rate of change between the discharge functions f(Q): 3k=ddtf(Q)

With k equal to the value of the first derivative of the discharge function at a given timestep and ddt equal to the first derivative of the discharge function f(Q) at timestep t. Combined with the calculation of the average first absolute derivative, which describes the average volatility of a function, it is possible to get a detailed insight into the dynamics of the catchment's hydrology. The average volatility of a hydrograph can be interpreted as the average length of the path the function is taking from the start of an event to the end (Fig. 2): 4kabs=ddtf(Q)

With kabs equal to the absolute derivative of f(Q).

Clusters of separated discharge functions are finally compared by a number of corresponding variables likely influencing event discharge dynamics: total precipitation [mm], antecedent precipitation index of the preceding 14 d before an event (API14 [mm]) and precipitation intensity [mmh-1]. Following Köhler and Linsley (1951), API14 is inversely calculated by the weighted sum of daily precipitation 14 d before the referred event: 5API14=∑i=1mri×Pi

With recession coefficient r [–] being 0.9 for Germany as proposed by Schröter et al. (2015), P equals precipitation [mm], m equals time span (14 d). API is considered as proxy for the pre-event wetness conditions in a catchment and therefore impacts runoff generation during events (Blanchard et al., 1981).

Event water and total discharge were analyzed for their relative contributions to NO3-, Ptot and Major Ions (Ca2+, Mg2+, K+, Cl-, Na+, SO42-) loads. Loads in the Event water and total discharge were compared against a bisector line, which represents a perfect constant behavior of cumulative discharge and load (Obermann et al., 2009). Functions above this line indicate a strong influence of rising concentrations on the loads (flushing), while curves below the bisector indicate lower concentrations relative to the discharge (dilution) (Obermann et al., 2009). This method can be used to determine which factor of the load equation dominates the system during an event. The complete formulation of the function can be found in Bertrand-Krajewski et al. (1998). The functions of the events were fitted to a power law function for better visualization and interpretation (Bertrand-Krajewski et al., 1998). The fitting procedure for the load/discharge power law relationship is derived from Bertrand-Krajewski et al. (1998) and follows a simple power function fit: 6F(x)=Xb where X equals the series of normalized discharge samples and b an exponential factor. The optimal value for b can be found by minimizing the root mean square error (RMSE): 7RMSE=∑i=1nyi-y^i2n where y equals the observed and y^ (in our case y^=F(xi)) the predicted value. RMSE can express values between 0 and infinity, with 0 indicating a perfect fit. Figure 3 visualizes the algorithm as conducted for our analysis.

The values of the exponential factor b show the behavior of power functions fitted to total load functions (Bertrand-Krajewski et al., 1997). A b value of 1 indicates a steady function aligned with the bisector (constant load and discharge), while values greater than 1 suggest functions below the bisector (dilution) and values less than 1 indicate functions above it (flushing). Because the calculation of cumulative loads is by definition a steadily and monotonously rising process, it allows for a straightforward normalization of the parameter space. Normalizing the parameter space to [0,1] allows us to constrain the power function to pass through the fixed points of (0,0) and (1,1), which forces all transformed curves to remain in the positive/positive quadrant of the Cartesian coordinate system. Under these circumstances, negative curves would be hyperbolic, or even outside of the defined parameter space and would be regarded as measurement errors. On the other side, a b value of 1 indicates a steady function aligned with the bisector (constant load and discharge), while values greater than 1 suggest functions below the bisector (dilution) and values less than 1 indicate functions above it (flushing). Approaching 0 or infinity reflects increasingly divergent behaviors. Separating event water from total discharge yields two distinct NCL functions per component, revealing significant behavioral differences through b values. To complement the exponent analysis with a more interpretable metric of flow component disparities, we calculated areas under the curve using the antiderivative of Eq. (6): 8F(x)→∫01Xbdx→1b+1×Xb+1

An area of 0.5 indicates constant export behavior. Values > 0.5 imply flushing, and < 0.5 indicate dilution. Areas with very small deviation from 0.5 can be regarded as expressions of quasi-constant curves. Thus, areas under the curve (< 0.5) represent stronger dilution during events and areas > 0.5 indicate flushing. This calculation was performed separately for total and event water discharge.

Correlations between nutrients in separated discharge and total discharge were calculated using Spearman correlation, differences between distributions were quantified using Kolmogorov–Smirnov test (KS test) and t-test (p < 0.05 each). For deeper insights, we compared the behavior of NO3- and Ptot during events.

Most discharge events were characterized by total precipitation between 6 and 14 mm, and durations between 15 and 23 h (Table 1). However, events number 7 and 13 stand out with a duration of 30 h and, respectively a total precipitation of 18.9 mm.

The mean event precipitation sum was 14.6 mm, and the mean event water portion was 41 %, ranging from 8 % to 85 %. API14 had a maximum of 35 mm in July 2021 and its minimum in June 2021 with 1.6 mm with a mean value of 14.2 mm. Total measured discharge is lowest in January 2022 (260 m3) and highest in February 2022 (7129 m3), with a mean value of 2837 m3. K-means cluster analysis was performed on the percentage of event water and precipitation sum (Fig. 4a).

K-means cluster analysis identified 3 clusters for this combination. The first cluster (blue) comprises 5 events and has its centroid at 14 mm precipitation and 25 % event water. The cluster ranges from low event water portions (< 10 %) to moderate portions (25 %–35 %), not exceeding the value of 50 % mean event water during any event. The second cluster (green) comprises 4 events with the centroid at 5 mm precipitation and 45 % event water. Event water ranges from 35 % up to 55 %. The centroid of the third cluster (red) is located at 14 mm precipitation and 55 % event water. The cluster is formed by 4 datapoints and ranges from moderate to high event water fraction (77 %). While the majority of datapoints are found in the region between > 35 % and < 50 % event water (8 datapoints), all clusters contain data further away from their centroids. The blue cluster covers events with moderate to high precipitation and low to moderate event water fractions, the green cluster covers events with comparatively low precipitation and moderate fractions of event water. The red cluster shows moderate to high precipitation and moderate to high event water fractions, therefore showing expected hydrological behavior. The behavior of the green and blue cluster and especially of event 5 and 12 was not expected, since high precipitation usually leads to higher event water portions and vice versa. Some explanation why event 5 shows very high event discharge at only 6.5 mm precipitation might be due to a road drainage that is close to the point of measurement. Another technical explanation can be found in the activation threshold of the water level actuator, which might have led to late activation during short events and therefore shifting the sampling window to the discharge peak, creating high event water means. The explanation for the difference between the blue and the red cluster, might be found in the pre-event wetness of the catchment, which can activating additional flow paths for the event water or enabling significant surface runoff (Duncan et al., 2017). Figure 5 supports this assumption by showing that the red cluster shows greater values of API14, compared to the blue cluster, while precipitation intensity and event duration show less difference.

API14 also serves as an explanation for the difference between the blue and the red cluster for mean rate of change, even if precipitation intensity is similar, the higher pre-event wetness enables a greater dynamic in the discharge behavior. But neither API14 nor precipitation intensity can explain the high rate of change of the green cluster, which is accompanied by high volatility A high rate of change can be attributed to the abruptness of changes in the discharge function, while high volatility, as defined in this study, describes situations in which discharge peaks are concentrated within a short fraction of the overall event duration.

Therefore, short but abrupt events with a single peak can express such high values, especially if a road drainage could be involved. The observations suggest that the Nesselbach catchment is, at least for the monitored timespan, a system with fast reacting discharge dynamics sensitive to pre-event wetness (API14). To sufficiently explain the observed differences in the behavior of separated event water functions, a second analysis was conducted by clustering the mean rate of change (Eq. 3) and volatility of the separated discharge functions (Eq. 4) (Fig. 4b). Three clusters were identified by the k-means clustering. The blue cluster contains events (6 in total) with moderate volatility and high rate of change, indicating overall low function dynamics. The second cluster (green), which consists of 3 events, shows low function volatility at moderate rate of change in discharge. The third cluster (red) consists of 4 events and shows a high rate of change and moderate to high volatility. On an interpretational level, the red cluster contains events that exhibit fast rising discharge and multiple amplitudes or waves. In contrast, the blue cluster consists of events that show only one amplitude and a quick and steady rise or recession in discharge. Most events fall into the blue cluster that shows a steady rise or recession in discharge with one or more amplitudes. The statistical interpretation of the dataset is limited due to the small sample size of 13 events and the different length of each event. Groups of functions, corresponding to the results of the k-means cluster analysis are depicted in Fig. S5. This behavior of differing function dynamics may be attributed to multiple factors like the precipitation sum, land cover, climatic parameters like temperature and pre-event wetness and the soil type and geology of the catchment (Outram et al., 2016; Peter et al., 2020). It is not uncommon for small catchments to exhibit fast reacting discharge behavior (e.g. Alexander et al., 2007; Birkel et al., 2011), but it is necessary to classify the events individually for any monitored catchment to get deeper insights into the nutrient export dynamics. In general, event discharge in the Nesselbach catchment is not only governed by precipitation sum but by a variety of parameters. This is especially true for event discharge with greater dynamic behavior, as can be seen in Fig. 6.

While the green cluster (lowest volatility and lowest mean rate of change) is a good example for discharge behavior primarily governed by the incoming precipitation signal. It exhibits the widest range for the parameters API14, mean precipitation intensity and event duration (Fig. 6) but shows the lowest range of precipitation levels. Events with high volatility and high mean rate of change can only be found in the red and blue clusters. Which show a much broader range of precipitation levels. The red cluster also comprises the highest maximum precipitation intensity and event water fraction values, while the blue cluster has the highest mean of API14 and also higher event water fraction compared to the green cluster. The low mean values of the red cluster for the API14 is due to the presence of event 5 in the cluster which has to be labeled as an outlier. For the observed time span, fast rising and changing discharge events are more common in the Nesselbach catchment than slowly rising events with a single amplitude (see Fig. S5) A partial explanation for this observation might be the seasonal compaction of agricultural topsoil, which reduces infiltration capacity and enables infiltration-excess overland flow (Kirkby, 2014; Peñuela et al., 2016; Stewart et al., 2019). Unfortunately, there are not enough events to test the assumption robustly, and it is based on the observation of agricultural activity in the catchment. While the occurrence of respective datapoints in May and November support the assumption, the datapoints in the month of June are contradictory. Because the temporal distribution of precipitation during the sampling period was unusual, with only just one event big enough to sample in autumn of 2021 and frequent precipitation in summer, the observed pattern is likely biased by the overweight of summer and spring events. General behavior of the catchment cannot be inferred from the available data. Combined with the spatial heterogeneity of the catchment, this results in waves of event discharge and therefore a high mean rate of change.., A moderate to high amount of precipitation triggers volatile events if pre-event wetness or maximum precipitation intensity is high.. This second cluster analysis confirms the findings of the first by highlighting that the Nesselbach catchment shows highly dynamic discharge during periods of high to moderate API (red cluster), high maximum precipitation intensity and moderate to high precipitation levels. Still, compared to a neighboring catchment with more urban infrastructure, the discharge response of the Nesselbach is moderate (Spill et al., 2023).

The NCL plots of Ptot and NO3- in the total discharge differ visually from each other (Fig. 7a and c). NO3- shows a narrower distribution of fitted curves that are more aligned with the bisector, indicating constant behavior (Winter et al., 2022). Because the main bulk of NO3- is entering the stream steadily mainly through groundwater, it was expected to show constant export behavior in many cases. Ptot loads are expressing a wider range of curve distribution, indicating a higher rate of dynamic behavior, with a small overweight on flushing. A difference in the pattern of nutrient mobilization was expected and follows the literature (Frazar et al., 2019; Ebeling et al., 2021; Spill et al., 2024). The range of values for the area under the curve of the total discharge power functions is 0.33 to 0.57 for NO3- loads and 0.38 to 0.62 for Ptot loads. It can be observed that there are more events with functions below the bisector for NO3- loads (6) than for Ptot loads (4) (Fig. 7a and c).

Applying the NCL analysis to the separated discharge dataset changes the outcome and reveals a different distribution of NCL functions (Fig. 7b and d). While the relationship between total discharge and NO3- load is mostly constant, with little deviation from the bisector (Fig. 7a), the NCL functions for the separated discharge show higher distances from the bisector (Fig. 7b), both visual and in more than doubling their range of values for the area under the curve (0.12 to 0.72). These increases in the parameter range in the event water fraction of discharge show a tendency for NO3- loads to express dilution or flushing behavior that is not observable or way less pronounced in the total discharge. This does not mean that the whole event can be classified as a flushing or dilution event, but that the transport processes differ between portions of discharge. A constant NO3- load in the total discharge can appear as a dilution or flushing behavior if the NCL curve is using the event water fraction of the same event (Fig. 7). While some events show hardly any alteration, other events are way more sensitive to the observed effect (Fig. 7a and b; Table S1).

A similar but less pronounced pattern is also observed for Ptot loads. Visually detectable differences in the distribution of curves for Ptot loads are backed by an increase in area range from 0.38–0.62 to 0.27–0.77. The Spearman correlation coefficient (ρ) for the area under the curve values of the event water fraction of NO3- and Ptot loads is significant (p < 0.05) and positive (ρ: 0.64), indicating a robust correlation of both parameters and a mutual reaction to the precipitation signal. Figure 8 summarizes this analysis by showing the ranges of calculated areas under the curve for the fitted NCL functions of the separated fractions for NO3- and Ptot (coefficient of variation: 0.38 and 0.21, respectively) compared to the total discharge (coefficient of variation: 0.13; 0.14). An overview of the changes in area for every nutrient and event can be found in the Supplement (Table S1).

The changes in the distribution of NCL functions when using separated discharge instead of the total discharge, especially for NO3- loads, were not apparent, because the total discharge signal masked stronger dilution or flushing tendencies. This shows the potential of the proposed method for contributing to better understanding nutrient export processes in headwater catchments. From the literature we get an ambivalent description of Ptot and NO3- behavior if compared to discharge. Frazar et al. (2019) and Kincaid et al. (2020) found that NO3- concentrations are decreasing while Ptot concentrations increase due to greater mobilization by fast overland flow in rural catchments. Ebeling et al. (2021) showed, in contrast, enrichment patterns for NO3- in over 700 catchments in Germany for long term timeseries. And Winter et al. (2024) showed that long-term export patterns of NO3- may diverge from event export patterns but show similar tendencies for flushing or dilution. But to our best knowledge there are no other studies that try to differentiate between the export patterns of Ptot and NO3- in the event water fraction and the total discharge. Those signals of flushing and dilution in the event water were dampened in the NCL functions of total discharge and would have remained undetected without hydrograph separation. To answer the question under which conditions those sudden changes occur, a cluster analysis for the volatility of the separated discharge function of event water and the value of the area under the curve for each nutrient was conducted (Fig. 9).

NO3- load (Fig. 9a) shows three clusters, with the red cluster clearly showing dilution tendency at moderate volatility, the green cluster showing mostly constant behavior and flushing tendency at moderate volatility, and a blue cluster expressing high volatility at constant behavior. The pattern of clustering is quite similar for Ptot load (Fig. 9b) but with different events and a less pronounced dilution behavior. Ptot loads in the event water express flushing tendency more often. Overall, the range of areas under the curve is smaller for Ptot but volatility patterns are quite similar to nitrate. The comparison of the cluster analysis shows that the volatility of event discharge is in some way a governing factor for the expressed behavior of nutrient export dynamics. Flushing and dilution tendencies can be found both during high volatile and low volatile events, while constant export behavior is centered at moderate and even highly volatile discharges. An explanation for this observation can be found in the mechanics of flushing and dilution: both need a strong signal of precipitation intensity to initialize the effects. Flushing needs an overweight of the cumulative solute load in the beginning of the event and vice versa for dilution patterns. Moreover, highly volatile event discharge is rarely capable of mobilizing enough NO3- to initialize the phenomenon of first flush. Despite flushing tendencies, a NCL curve clearly showing a first-flush, could not be observed in this dataset. A first-flush would occur if a maximum distance of 0.2 between a function and the bisector could have been observed (Lee et al., 2002) A steady supply of event water at the beginning of an event, transporting the NO3- in soil water and overland flow, is needed (Obermann et al., 2009). The same is true for dilution effects: during events, a steady supply of fresh precipitation water, mostly free of nutrients, can dilute the nutrient background signal stemming from diffuse or even point sources (Ebeling et al.,2021). NCL functions aligned to the bisector on the other hand, are not dominated by one of the effects. Due to the more evenly distributed event water discharge and nutrient concentration, they reflect neither the fast mobilization and enrichment of the discharge with nutrients nor a significant dilution. The reasons for the occurrence of flushing or dilution events are therefore not only attributed to the hydrological functioning of this catchment, but also to the capacity of nutrient storage or seasonally varying effects like pre-event wetness, land use and soil conductivity (Schwientek et al., 2013; Duncan et al., 2015; Winter et al., 2024). This is of great interest, because it was not expected to see such dynamic changes in the NO3- load patterns between portions of discharge during precipitation events by using a method originally developed to compare long term solute export behavior. Event water is partly composed of surface runoff, which is often associated with lower NO3- loads (Outram et al., 2016; Frazar et al., 2019). These observations contradict the expected behavior of stronger differences between NO3- and Ptot loads (Kincaid et al., 2020). The method reveals previously concealed dynamics of nutrient export in this specific catchment. By focusing on the nutrient signal of the event water fraction, it adds an additional dimension to the NCL-method, enabling it to compare different nutrient export processes during the same event. Unexpected nutrient export patterns in the event water might be attributed to catchment properties like the catchments drainage system, unknown point sources, or its legacy storage (mean NO3- concentration in discharge:68 mgL-1) (Blaen et al., 2017; Ehrhardt et al., 2019; Spill et al., 2023).

To evaluate the robustness of the proposed method, it was also applied to major ion concentrations sampled in the same catchment (Fig. 10). Major ions are suitable for testing the method independently of seasonal nutrient patterns and hydrological conditions.

While the differences between major ion loads are not as strong as between NO3- and Ptot loads, differences between event water and total discharge are also prevalent in the distributions of power functions fitted to the ion data. The distributions differ significantly when tested with KS test (p < 0.05). Potassium loads express the biggest difference between total discharge and event water, and magnesium loads express the smallest. Calcium, magnesium, and sulphate loads shift from near-constant or slight dilution tendencies in the total discharge to mild flushing behavior in the event water. The range of calculated areas drastically increases for all ion species (Fig. 10), indicating overall more volatile dynamics of discharge and mobilization of ions in the event water, which is supported by the strong increase in the coefficient of variation for each ion species (Table 2).

The more pronounced flushing tendencies in the event water fraction were unexpected, given the generally conservative behavior of these solutes under typical flow conditions (Shanley et al., 2011; Moatar et al., 2017). This observation in the monitored catchment can possibly be linked to an influence of either a frequent overland flow or temporary activation of the catchments drainage system. Spearman correlation analysis (p < 0.05) reveals strong positive relationships between the concentrations of most ion species in discharge. These correlations are likely governed by shared hydrological drivers rather than direct chemical dependencies between ions. As discharge rises, all major ion species are mobilized throughout the duration of an event.

Like all data-driven empirical analyses, this method needs a robust sample size from which to draw. 13 events over multiple parameters, as presented in this study, are sufficient to satisfy rigorous statistical thresholds. However, the more data is available, the more robust the method becomes. At first glance, it appears difficult to interpret the comparison between the total discharge and the event water by using baseline descriptive methods like arithmetic mean, median or standard deviation, because they might show no significant changes. However, statistical methods like calculating the range of values and coefficient of variation show a clear difference, which indicates a more complex nature of the observed export dynamics. Using the range of values seems to be the easiest way to highlight differences, but it lacks interpretational power, which could be enhanced by applying a KS test. As an inherited limitation from the NCL function analysis, this method does not allow for interpretation of the influence of event duration and the thresholds for identifying flushing and dilution behavior remain somewhat arbitrary (Bertrand-Krajewski et al., 1998; Hathaway et al., 2012). Therefore, the method requires a broader framework of supporting parameters and complementary statistical analysis like cluster analysis to gain interpretive power. This method is not a stand-alone tool, and it is not suited to quantify the governing processes of the catchment's nutrient export. Rather, it serves to detect whether changing patterns in the catchment's transport processes occur during events. Additionally, we recommend increasing the cleaning interval of the Spectrolyzer, both automated cleaning with pressure and manual cleaning to ensure less instrument failure. Since we used an hourly cleaning with compressed air in this setup, we recommend going down to 30 min, to minimize the influence of sediments covering the optical slit. For the manual cleaning we did a 1 week cleaning interval with brushes and hydrochloric acid (2 %) to remove any biofilm. Recommendations for catchments with a higher biological turnover or water treatment plants influencing the discharge see Spill et al. (2024). Finally, the method would profit from a higher temporal and spatial resolution of tracers in discharge and precipitation within in the catchment, like for example achieved by Freyberg et al., 2018.