the Creative Commons Attribution 4.0 License.
the Creative Commons Attribution 4.0 License.
Technical note: Using long shortterm memory models to fill data gaps in hydrological monitoring networks
Huiying Ren
Erol Cromwell
Ben Kravitz
Quantifying the spatiotemporal dynamics in subsurface hydrological flows over a long time window usually employs a network of monitoring wells. However, such observations are often spatially sparse with potential temporal gaps due to poor quality or instrument failure. In this study, we explore the ability of recurrent neural networks to fill gaps in a spatially distributed timeseries dataset. We use a well network that monitors the dynamic and heterogeneous hydrologic exchanges between the Columbia River and its adjacent groundwater aquifer at the U.S. Department of Energy's Hanford site. This 10yearlong dataset contains hourly temperature, specific conductance, and groundwater table elevation measurements from 42 wells with gaps of various lengths. We employ a long shortterm memory (LSTM) model to capture the temporal variations in the observed system behaviors needed for gap filling. The performance of the LSTMbased gapfilling method was evaluated against a traditional autoregressive integrated moving average (ARIMA) method in terms of error statistics and accuracy in capturing the temporal patterns of river corridor wells with various dynamics signatures. Our study demonstrates that the ARIMA models yield better average error statistics, although they tend to have larger errors during time windows with abrupt changes or highfrequency (daily and subdaily) variations. The LSTMbased models excel in capturing both highfrequency and lowfrequency (monthly and seasonal) dynamics. However, the inclusion of highfrequency fluctuations may also lead to overly dynamic predictions in time windows that lack such fluctuations. The LSTM can take advantage of the spatial information from neighboring wells to improve the gapfilling accuracy, especially for long gaps in system states that vary at subdaily scales. While LSTM models require substantial training data and have limited extrapolation power beyond the conditions represented in the training data, they afford great flexibility to account for the spatial correlations, temporal correlations, and nonlinearity in data without a priori assumptions. Thus, LSTMs provide effective alternatives to fill in data gaps in spatially distributed timeseries observations characterized by multiple dominant frequencies of variability, which are essential for advancing our understanding of dynamic complex systems.
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Longterm hydrological monitoring using distributed well networks is of critical importance for understanding how ecosystems respond to chronic or extreme perturbations as well as for informing policies and decisions related to natural resources and environmental issues (Wett et al., 2002; Taylor and Alley, 2002; Grant and Dietrich, 2017). One of the most common methods for collecting hydrologic and chemistry data in groundwater is through wells (Güler and Thyne, 2004; Strobl and Robillard, 2008; Lin et al., 2012). However, most well data have temporal gaps due to instrument failure or poor measurement quality. These data gaps degrade the quality of the dataset and increase the uncertainty in the spatial and temporal patterns derived from the data. Gap filling is essential for developing an understanding of dynamic system behaviors and for use in creating continuous, internally consistent boundary conditions for numerical models. One outstanding challenge in gap filling is capturing nonstationarity in data.
Various statistical methods have been developed to fill gaps in spatiotemporal datasets, with the autoregressive integrated moving average (ARIMA) method being the most commonly used (Han et al., 2010; Zhang, 2003). For any given spatial location, ARIMA uses temporal autocorrelations to predict unobserved data points in a time series. Spatiotemporal autocorrelations can be considered by using multivariate ARIMA and space–time autoregressive models (Kamarianakis and Prastacos, 2003; Wikle et al., 1998; Kamarianakis and Prastacos, 2005). However, ARIMA cannot capture nonlinear trends because it assumes a linear dependence between adjacent observations (Faruk, 2010; Valenzuela et al., 2008; Ho et al., 2002). In addition, all existing space–time ARIMA models assume fixed global autoregressive and moving average terms, which fail to capture evolving dynamics in highly dynamic systems (Pfeifer and Deutrch, 1980; Griffith, 2010; Cheng et al., 2012, 2014). Spectralbased methods, such as singular spectrum analysis, the maximum entropy method, and the Lomb–Scargle periodogram, have been used to account for nonlinear trends while filling in gaps in spatiotemporal datasets (Ghil et al., 2002; Hocke and Kämpfer, 2008; Kondrashov and Ghil, 2006). These methods use a few optimal spatial or temporal modes occurring at low frequencies to predict the missing values, with the other higherfrequency components discarded as noise. This can lead to a reduced accuracy of the statistical models when fitting observations and predicting missing values (Kondrashov et al., 2010; Wang et al., 2012). Kriging and maximum likelihood estimation used in spatial and spatiotemporal gap filling often face challenges computing the covariance matrix of the data vector, as it can be quite large (Katzfuss and Cressie, 2012; Eidsvik et al., 2014). Other nonlinear methods have been explored with some success, including expectation–maximization or Bayesian probabilistic inference such as hierarchical models, Gaussian process, and Markov chain Monte Carlo. Using models that build dependencies in different stages or hierarchies most effectively captures spatial and temporal correlations (Calculli et al., 2015; Banerjee et al., 2014; Datta et al., 2016; Finley et al., 2013; Stroud et al., 2017). In general, the expectation–maximization algorithm and Bayesianbased methods are sensitive to the choice of initial values and prior distributions in parameter space (Katzfuss and Cressie, 2011, 2012). Moreover, prior distributions and their associated parameters all need to be specified in both the spatial and temporal domains, which becomes increasingly difficult in more complex systems. Empirical orthogonal function (EOF) related interpolation methods, such as least squares EOF (LSEOF), data interpolation EOF (DINEOF), and recursively subtracted EOF (REEOF), are widely used to fill in missing data such as clouds in sea surface temperature datasets or other satellitebased images with regular gridded domains (Beckers and Rixen, 2003; Beckers et al., 2006; AlveraAzcárate et al., 2016). However, EOF methods require gridded data, and this limits their use in filling data gaps in irregularly spaced monitoring networks.
Deep neural networks (DNNs) (Schmidhuber, 2015) are datadriven tools that, in principle, could provide a powerful way of extracting the nonlinear spatiotemporal patterns hidden in distributed timeseries data without knowing their explicit forms (Längkvist et al., 2014). They are increasingly being used in geoscience domains to extract patterns and insights from streams of geospatial data and to transform our understanding of complex systems (Reichstein et al., 2019; Shen, 2018; Sun, 2018; Sun et al., 2019; Gentine et al., 2018). The umbrella term of DNN contains numerous architecture categories which can be selected for the problem at hand. Recurrent neural networks (RNNs) are a natural choice of architecture for the analyses in this paper, which focus on filling gaps in timeseries data (Jordan, 1986). RNNs take sequences (e.g., time series) as input, and they output either the single values or sequences that follow. They are designed to use information about previous events to make predictions about future events by essentially letting the model “remember.” However, RNNs have been shown to lose memory from previously trained data for longer sequences of data, i.e., they “forget” (Hochreiter et al., 2001). The earlier information becomes exponentially less impactful for prediction as the sequence size increases. Long shortterm memory (LSTM) networks are variations of RNNs that are explicitly designed to avoid this problem by using memory cells to retain information about relevant past events (Hochreiter and Schmidhuber, 1997). RNNs and LSTMs have been successfully applied to text prediction (Graves, 2013), text translation (Wu et al., 2016), speech recognition (Graves et al., 2013), and image captioning (You et al., 2016). Recently, hydrology applications of RNNs and LSTMs have emerged. For example, Kratzert et al. (2018) used LSTMs to predict watershed runoff from meteorological observations, Zhang et al. (2018) used LSTMs for predicting sewer overflow events from rainfall intensity and sewer water level measurements, and Fang et al. (2017) used LSTMs to predict soil moisture with high fidelity.
Our study aims to evaluate the potential of using LSTM models for filling gaps in spatiotemporal timeseries data collected from a distributed network. We tested the LSTMbased gapfilling method using datasets collected to understand the interactions between a regulated river and a contaminated groundwater aquifer. We treat the gap filling as a forecasting problem, i.e., we use the historical data as input to predict the missing values in the data gaps. The future information relative to the gap is implicitly used in training the LSTM models. Framing gap filling as a predictive problem is a common practice when machine learning methods are used for filling gaps in timeseries data (see examples in Kandasamy et al., 2013; Körner et al., 2018; Chen et al., 2020; Zhao et al., 2020; Sarafanov et al., 2020; and Contractor and Roughan, 2021). The performance of the LSTMbased gapfilling method is compared with traditional timeseries approaches (i.e., ARIMA) to identify situations in which LSTM models out or underperform the ARIMA models.
A 10year (2008–2018) spatiotemporal dataset was collected from a network of groundwater wells that monitor temperature (CS547A water conductivity and temperature probe, Campbell Scientific), specific conductance (SpC) (CS547A water conductivity and temperature probe, Campbell Scientific), and water table elevation (CS451 stainlesssteel pressure transducer, Campbell Scientific) at the 300 Area of the U.S. Department of Energy Hanford site, located in southeastern Washington State. The groundwater well network was originally built to monitor the attenuation of legacy contaminants. The groundwater aquifer at the study site is composed of two distinct geologic formations: a highly permeable formation (Hanford formation, consisting of coarse gravelly sand and sandy gravel) underlain by a much less permeable formation (the Ringold Formation, consisting of silt and fine sand). The dominant hydrogeologic features of the aquifer are defined by the interface between the Hanford and Ringold formations as well as the heterogeneity within the Hanford formation (Chen et al., 2012, 2013).
The intrusion of river water into the adjacent groundwater aquifer causes two water bodies with distinct geochemistry to mix and stimulates biogeochemical reactions at the interface. The river water has lower SpC (0.1–0.12 m cm^{−1}) than the groundwater (averaging ∼ 0.4 m cm^{−1}). Groundwater has a nearly constant temperature (16–17 ^{∘}C) as opposed to the seasonal variations in the river temperature (3–22 ^{∘}C). The highly heterogeneous coarsetextured aquifer (Zachara et al., 2013) interacts with dynamic river stages to create complex river intrusion and retreat pathways and dynamics. The time series of multiyear SpC and temperature observations at the selected wells show these complicated processes of river water intrusion into our study site (Fig. 1). Wells near the river shoreline (e.g., wells 11, 110A, 22, and 23) tend to be strongly affected by river water intrusion in spring and summer. As such, the dynamic patterns of SpC and temperature correspond well to river stage fluctuations, specifically that SpC decreases and temperature increases with increasing river stage. Fluctuations in SpC in well 22 appear to be stronger and at higher frequency than in other wells, likely indicating its higher connectivity with the river. For wells further inland (e.g., well 115), temperatures consistently remain within the groundwater temperature range, and SpC has three noticeable dips (dropping from 0.5 to 0.4 mS cm^{−1}). The SpC dips coincide with the high river stages in the years 2011, 2012, and 2017, which featured higher peak river stages than other years that enabled river water to intrude further into the groundwater aquifer. In wells located an intermediate distance from the river, such as well 25, the intrusion of river water is evident in most years. It is absent in lowflow years, such as 2009 and 2015, during which both SpC and temperature remain nearly unchanged.
Earlier studies have demonstrated that physical heterogeneity contributes to the different response behaviors of different locations while the river stage dynamics lead to multifrequency dynamics in those responses. Natural climatic forcing drives seasonal and annual variations (Amaranto et al., 2019, 2018), whereas the operations of upstream hydroelectric dams to meet human societal needs primarily induce the higherfrequency (i.e., daily and subdaily) fluctuations (Song et al., 2018). Our system is representative of many damregulated gravelbed rivers across the world, where anthropogenic dam operations have significantly altered the hydrologic exchanges between river water and groundwater as well as the associated thermal and biogeochemical processes (Song et al., 2018; Shuai et al., 2019; Zachara et al., 2020). Note that the multifrequency variations in data characterize the dynamic features of data, which could exist in both shortterm and longterm timeseries data as a result of shortterm or longterm monitoring efforts.
To understand the multifrequency variations in the river water and groundwater mixing in each well at the study site, we perform spectral analysis on multiyear SpC observations at each selected well using a discrete wavelet transform (DWT). The DWT is widely used for time–frequency analysis of time series and relies on a “mother wavelet”, which is chosen to be the Morlet wavelet (Grossmann and Morlet, 1984) to deal with the timevarying frequency and amplitude in this site's timeseries data (Stockwell et al., 1996; Grinsted et al., 2004). We illustrate the wavelet power spectrum (WPS) in log scale and its normalized global power spectrum (average WPS over the time domain) for the multiyear SpC time series in the first two columns of Fig. 2. Data gaps are shown as blank regions in Fig. 2; examples include early 2009 at well 11, the beginning of 2011 at well 110A, and the later part of 2012 at well 22. The WPS amplitude represents the relative importance of variation at a given frequency compared to the variations at other frequencies across the spectrum. At wells 11, 110A, 23, 25, and 22, the strongest intensities of the SpC signals appear at halfyearly and yearly frequencies; however, well 115 has a different pattern, with most of its high intensities below the 256 h frequency. The averaged WPS further shows the behavior contrast: wells 11, 110A, 23, and 25 have a dominant frequency at half a year; well 22 has multiple dominant frequencies at daily, monthly, and seasonal scales; and well 115 has similar intensities at the halfyearly and hourly scales. Using this information to inform our approach, we hypothesize that gap filling at well 22 could be more challenging due to the mixture of dynamics signatures.
As the system dynamics are driven by the river stage, we perform magnitudesquared wavelet coherence analysis via the Morlet wavelet to reveal the dynamic correlations between the SpC and river stage time series (Grinsted et al., 2004; Vacha and Barunik, 2012). Wavelet coherence in the time–frequency domain is plotted in the third column in Fig. 2, and the average coherence is plotted in the fourth column; red points indicate statistically significant values at the 95th percent confidence interval. A larger coherence at a given frequency indicates a stronger correlation at that frequency between the SpC at a well and the river stage. We consider these two variables to be highly correlated when the coherence is larger than 0.7 (shown using colors ranging from green to red in the “Coherence” plots). We found that such high correlations exist at multiple frequencies, from subdaily to daily to yearly, at all wells close to the river (e.g., 11, 110A, 22, and 23). Wells farther from the river (e.g., 115 and 25) have higher correlation regimes shifted towards longer periods at semiannual and annual frequencies and are less persistent in time.
As can be seen in Fig. 2, many of the wells have long data gaps which have unknown effects on our ability to estimate dynamics from the wavelet spectra. As such, gap filling is needed to infer observations and guide our modeling of the underlying system. Figure 3 provides a summary of gap lengths for the overall network of monitoring wells. The majority of the gap lengths of the three monitored variables are less than 50 h. Therefore, our investigations explore the ability of different methods to fill gaps of 1, 6, 12, 24, 48, and 72 h lengths to capture the multifrequency fluctuations using hourly data input.
In this section, we describe two methods that we implemented to fill gaps of various lengths in SpC measurements at selected wells: an LSTM model and the traditional ARIMA model. We focused our analyses on filling gaps in SpC due to its importance in revealing river water and groundwater mixing. The same set of analyses can be performed on water level and temperature. An input with M time steps (input window length) is provided to both the LSTM and ARIMA models for predicting the next time step immediately following the input window. For gaps larger than 1 h, the gapfilling models are applied to fill in one missing value at a time. The entire gap is filled by sliding the input window forward hour by hour and treating the gapfilled values of the previous missing hours as observed values.
The input window may contain multiple variables relevant to the prediction from a single well or multiple wells. After experimenting with different sets of input variables (SpC only; SpC and water level; and SpC, water level, and temperature), we found that including SpC and water level measurements in the input window yielded the most robust performance. Therefore, we used historic water level (m) and SpC (m cm^{−1}) observations to fill gaps in the SpC time series of a single well. Using measurements from multiple wells as input allows the models to account for both the temporal and spatial correlations in the data, which impacts gapfilling performance. Wells were selected based on adequate data availability and distance from the target well. Assuming the observations from W (W≥1) wells are used to fill in data gaps, the input size of the model is then M × 2 W.
3.1 LSTM models for gap filling
We designed an LSTM architecture, shown in Fig. 4, to train models of an input size of M time steps and an output size of one time step. The LSTM model contains a single LSTM layer followed by an output dense layer. Figures S1 and S2 in the Supplement show the detailed structure of the LSTM layer.
^{a} The parameter was used to select the best LSTM model configurations and hyperparameters. ^{b} The parameter was used to evaluate the performance of LSTM vs. ARIMA.
Training data for the LSTM models were created by finding data segments of M + 1 h with no missing values, i.e., no gaps in the data, for both water level and SpC measurements over a specified monitoring window. The well data were then preprocessed by normalizing all measurements to zero mean and unit variance for each variable, as SpC is on a scale of 10^{−1}, and water level is on a scale of 10^{2}. Validation datasets were used to select the best model hyperparameters and optimal input window size M (Sect. 3.1.1) for gap filling at each well. Another independent testing period was selected at each well, depending on data availability, to compare the gapfilling performance using the LSTM and ARIMA methods. The complete set of alternatives that we considered for each LSTM model configuration is shown in Table 1. We used the Adam optimizer (Kingma and Ba, 2014) for training and the meansquared error as the loss function. The models were trained for 50 iterations (i.e., epochs) over the training data.
To evaluate the accuracy of the trained LSTM models in filling SpC data gaps during the validation and testing processes, we assumed that synthetic gaps of various lengths (e.g., 1, 6, 12, 24, 48, and 72 h, referred to as gap scenarios hereafter) exist in the validation or testing dataset of a well. We assume that only the SpC measurements are missing, whereas the water level measurements are available. An LSTM model configured with an input of M is then given M hours of data from the time series preceding the occurrence of a gap (assuming no missing values in these M hours) to fill in hour by hour. The accuracy of the gapfilling model is evaluated by calculating the mean absolute percentage error (MAPE; %) between the filled in (i.e., predicted) and observed SpC values:
where n is the total number of synthetic missing data points during the evaluation period.
In addition to MAPE, the models are evaluated using the Nash–Sutcliffe model efficiency coefficient (NSE) (Nash and Sutcliffe, 1970) and the Kling–Gupta efficiency (KGE) (Gupta et al., 2009) metric. NSE is a metric used to assess the predictive skills and accuracy of hydrological models. Values range from −∞ to 1, where 1 indicates a perfect model fit, 0 indicates that the model has the same predictive power as the observational mean, and a value less than 0 indicates that the model is a worse predictor than the observational mean. The NSE of the SpC predictions is calculated using the following equation:
where n is the total number of synthetic missing data points during the evaluation period, P_{t} and O_{t} are the respective predicted and observed SpC values at time t, and μ(O) is the mean observed SpC value.
The KGE is another goodnessoffit metric used to evaluate hydrological models by combining the three components of the NSE model errors (i.e., correlation, bias, and ratio of variances or coefficients of variation) in a more balanced way. It has the same range of values as the NSE, where 1 indicates a perfect model fit. The KGE is calculated on a model's SpC predictions using the following equations:
Here, cov is the covariance, σ is the standard deviation, and μ is the arithmetic mean.
In addition to the LSTM models trained for the singlewell setup, we also trained multiwell LSTM models that used observations from wells 11, 110A, and 116A to fill in data gaps for well 11. We explored the same set of configuration parameters in the multiwell LSTM models as shown in Table 1 for the singlewell models. We then compared the gapfilling performance of the multiwell LSTM with the singlewell LSTM model for well 11. The multiwell models were not explored for other wells due to the lack of closeproximity neighboring wells.
Optimizing LSTM model configuration
We used a gridsearch approach to explore different LSTM model hyperparameter configurations to find the best model for a given gap length at each well. This involved iterating over all combinations of the input time window size (M), the number of units (U) in the LSTM layer, and the learning rate (L) listed in Table 1 for each well. We chose the optimal LSTM configuration using model performance on the validation dataset (see Table 1) based on the MAPE defined in Eq. (1). The combinations that yielded the lowest SpC MAPEs were selected as the best configuration for a given gap length at each well. These configurations are shown in Table S1 in the Supplement. The best model configurations were then used to evaluate the LSTMbased gapfilling method against the ARIMAbased method (Sect. 3.2) using relative errors (similar to MAPE by setting n=1 in Eq. (1) and removing the absolute value operation) calculated for each data point in the testing period (Table 1). These varied among the wells due to the availability of continuous data required for testing.
3.2 ARIMA models for gap filling
ARIMA is one of the most general model classes for extrapolating time series to produce forecasts. We used it as a baseline to compare and assess the LSTM gapfilling method. ARIMA can be applied to nonstationary timeseries data using a combination of differencing, autoregressive, and moving average components. A nonseasonal ARIMA$(p,d,q)$ model is given by
where ϕs and θs are polynomials of orders p and q, respectively, each containing no roots inside the unit circle; e represents error terms; ${Y}_{.}^{d}$ is Y_{.} differenced d times; and c is a constant. Note that only nonseasonal terms $(p,d,q)$ are included in Eq. (2). Seasonal structure can be added with parameters $(P,D,Q{)}_{m}$ to the base ARIMA model to convert it to ARIMA$(p,d,q)(P,D,Q{)}_{m}$, with a periodic component containing m periods. c≠0 implies a polynomial of order d+D in the forecast function. The detailed mathematical equations for the seasonal ARIMA model are provided in the Supplement.
The main task in ARIMAbased forecasting is to select appropriate model orders, i.e., the values of $p,q,d,P,Q$, and D. If d and D are known, we can select the orders $p,q,P$, and Q via an information criterion such as the Akaike information criterion (AIC):
where k=1 if c≠0 and is 0 otherwise, and L is the likelihood of the model fitted to the differenced data. The ARIMA models were built using the “auto.arima” function from the “forecast” R package (Hyndman and Khandakar, 2007), which applies the Hyndman–Khandakar algorithm (Hyndman and Khandakar, 2008) that minimizes the AIC to obtain the bestfit parameters of the ARIMA model.
Similar to the LSTMbased gap filling, we explored various input window sizes, from 24 to 504 h in increments of 24 h, for the ARIMA model at each well to identify the optimal input windows within the search range. An optimal input window size is chosen for each gap length of each well using the same MAPE metric (i.e., Eq. 1) on the validation dataset.
4.1 Performance of singlewell LSTM models
We selected the best combination of LSTM units (U) and learning rate (L) for each input time window (M) under each gap length at each well using the MAPE metric. The validation MAPEs of those selected models were summarized in box plots under different groupings, examples of which are shown in Fig. 5. Each MAPE box plot was drawn from a group of models with one parameter (corresponding to each x axis) fixed at a given value while the other parameters cycle through their possible combinations.
As shown in Fig. 5a, model performance deteriorates as the gap length increases, indicating that the LSTMbased method tends to lose ground truth information from its input to inform prediction. In comparing MAPEs across the various input window sizes shown in Fig. 5b, we observe that models with all input windows have comparable MAPE summary statistics, with larger input windows (> 96 h) leading to slightly smaller MAPE quartiles. The larger input windows also yield fewer outliers on the larger MAPE end, indicating that the memory units in the LSTM layers are capturing important daily to weekly signatures for some wells (which is evident in the WPS plots in Fig. 2 for all wells except for well 115).
The performance of singlewell LSTM models varied among the wells, as shown in Fig. 5c. The LSTM models for well 115 lead performance with the smallest MAPEs, whereas the model of well 22 yields the worst performance. The LSTM models for wells 11,110A, 23, and 25 performed comparably overall, with slightly more large MAPE outliers for well 23.
4.2 Singlewell LSTM and ARIMA comparisons
The singlewell LSTM gapfilling approach was compared to the ARIMA approach using the relative errors calculated for each data point assumed to be missing in the testing data by setting n=1 in Eq. (1) for MAPE. Relative errors were used to show the overestimations or underestimations of both approaches. Their respective best model configurations, determined on the validation dataset (i.e., data from year 2011), were used to compare the two approaches. Figure 6 illustrates the optimal input windows for the LSTM and ARIMA methods. We observe that the LSTM models require much less input information than the ARIMA method under all gap lengths for all of the wells.
Figure 7 shows the box plots of relative errors under different gap lengths for all testing wells. As expected, the relative errors increase as the gap length increases for both approaches. The ARIMA models tend to perform better than the LSTM models in terms of interquartile range. However, the ARIMA models produce more outliers of large positive or negative relative errors than the LSTM models in general and particularly for larger gap lengths (48 and 72 h). For well 115, the relative errors of both approaches are small for all gap lengths. Both approaches appear to have larger error outliers at well 23.
For each well, we performed a T test to calculate the T score and p value between the relative errors of the two models to determine the significance in the performance difference of the models. As seen in Table 2, each well has a high T score and a p value significantly less than 0.05. Thus, the differences between their relative errors are significant and meaningful.
In addition to the relative errors, we calculated the MAPE, rootmeansquared error (RMSE), NSE, and KGE for the best LSTM and ARIMA model for each gap length. Table 2 compares the performance of the LSTM and ARIMA models filling in gap lengths of 24 h. The results for all gap lengths are given in the Supplement (Table S2).
The LSTM and ARIMA models yielded comparable average metrics at all wells for the 24 h gap length, as can be seen in Table 2. The NSE and KGE resulting from both models are close to 1 for all of the wells with negligible differences between the two models. The difference in the MAPE and RMSE is also small, with more notable differences for wells 22 and 23, where the ARIMA models resulted in lower MAPE and RMSE values.
In addition to the error statistics, it is also important to examine how well a gapfilling method captures the desired dynamics patterns in the gapfilled time series. Therefore, the SpC time series reproduced by the gapfilling methods during the testing period (2016 for wells 11, 110A, 22, 23; 2017 for well 115; 2008 for well 25) with 24 h synthetic gaps are evaluated against the real time series. The model configurations are the same as those used in the error statistics comparison (Fig. 6). A gap length of 24 h is the selected example, as we consider it a reasonably challenging case to fill the gaps in timeseries data exhibiting significant nonstationarity, such as the SpC data at well 23. Moreover, the relative performance of the two approaches is similar at other gap lengths with varying error magnitudes.
As shown in the first column of Fig. 8, both approaches capture the general dynamic patterns in the data fairly well. For more detail, the time series of relative errors for both methods are provided in Fig. S3. The ARIMA approach (blue lines in column 1) missed some abrupt changes that occur over a short time window (i.e., at higher frequency), leading to more error spikes in all wells. This is consistent with the relative error outliers in Fig. 7 and is an indication that the ARIMA models lack mechanisms to represent such highfrequency changes. The LSTM approach (red lines in column 1) is able to better capture such dynamics in all of the wells. However, the inclusion of the highfrequency fluctuations may also lead to overly dynamic predictions in time windows dominated by lowerfrequency fluctuations. This contributed to less desirable relative errors distributed between the first and third quartiles in some wells (i.e., wells 11, 23, 22, and 115), as shown in Fig. S4. The errors are likely caused by the variability in dynamics signatures among the training, validation, and testing periods, as well as the selection of the training loss functions and validation metric that balance between the occurrence of small and large errors to achieve optimal solutions.
To further investigate the dependence of the relative performance of the two gapfilling methods on the inherent dynamics in each time series, spectral analyses for the testing SpC datasets were performed using the same wavelet decomposition method for the multiyear analyses (shown earlier in Fig. 2). As shown in Fig. 8, the time windows of high relative errors are found to approximately colocate with the time when the highfrequency (daily and subdaily) signals gain more power. The differences between the LSTM and ARIMA models tend to be amplified during those time windows. Wells 11, 110A, and 22 share similar seasonal patterns in WPS, with the highest intensity bin above 1024 h across February to July. Their average WPSs all show peaks around daily and subdaily frequencies. Well 23 has its greatest energy between 16 and 256 h from January to July. Well 25 has low variability intensities at daily and subdaily frequencies with lowfrequency variations (monthly and seasonal) dominating the January to March time frame. For well 115, one of its strongest intensities is above 2048 h across the entire year, and the other strong intensities are narrow bands between 16 and 256 h. In general, both LSTM and ARIMA are effective at capturing lowfrequency variability (monthly and seasonal). Although LSTM is more effective at capturing highfrequency (daily and subdaily) fluctuations and nonlinearities in the datasets, it may also lead to overly dynamic predictions in time windows with no considerable highfrequency fluctuations. However, the errors during these time windows are small and can be improved by smoothing if such fluctuations are undesirable.
There is also a significant difference in the computational cost for the LSTM and ARIMA methods. ARIMA requires very few computational resources: the auto.arima function in R requires approximately 40 s to fit and validate a model for each prediction segment on a personal computer with a 3.00 GHz CPU. Conversely, training and validating a single LSTM model takes approximately 20–30 min on GPUs based on dual NVIDIA P100 12GB PCIe cards.
4.3 Performance of multiwell models
We evaluated the predictive ability of multiwell models using both approaches for filling gaps of various lengths in the SpC data at well 11 by comparing their performance against their singlewell counterparts. Well 11 was chosen because of the data availability for nearby wells (wells 110A and 116A). Similar to the singlewell ARIMA and LSTM model for well 11, the multiwell models also predict the SpC measurement using water level and SpC from three wells. We adopted the same LSTM architecture from the singlewell LSTM model and trained the same set of alternatives considering input window sizes, LSTM units, and learning rates for various gap lengths as listed in Table 1. The same training and validation periods were adopted to select the optimal combination of M, U, and L. The optimal combinations are shown in Table S3. For the multiwell ARIMA models, we included additional variables as regression terms when building and fitting models using the auto.arima function. The optimal input window sizes of ARIMA are 216, 240, 288, 288, 288, and 192 h for gap lengths of 1, 6, 12, 24, 48, and 72 h, respectively. These are smaller than the optimal window sizes of the singlewell models.
The box plots of relative errors yielded from the singlewell and multiwell models using both approaches are provided in Fig. 9 for comparison. Additionally, we include performance metrics for comparing the single and multiwell models in Table 3. Additional spatial information seems to exacerbate the relative errors of the ARIMA models, except in large gaps (e.g., 72 h). The LSTM approach, on the contrary, benefits from the information carried by the neighboring wells when filling in the larger gaps, whereas the performance for small gaps remains unchanged. The aggregated performance metrics in Table 3 show slightly improved metrics for multiwell ARIMA models for gaps smaller than 24 h compared with the singlewell models, while the turning point in relative performance is at 12 h for the LSTM models. The deteriorated performance metrics of the multiwell LSTM models at the larger gap lengths are consistent with the larger interquartile ranges, as shown in the box plots of relative errors in Fig. 9. However, the multiwell LSTM and ARIMA models can reduce the occurrence of large relative errors for larger gaps and provide more robust gap filling under those circumstances.
These comparisons show that, although the information from a single well may be sufficient to fill in gaps smaller than a day, including spatial information from neighboring wells in the LSTM and ARIMA models could potentially increase the chance of successes in filling data gaps under more challenging circumstances, such as capturing more complex dynamic patterns with longer data gaps. While the aggregated metrics provide an overall assessment of model performance, examining the distribution of relative errors could provide complementary information on large error spikes while selecting optimal model configurations.
In this study, we implemented an LSTMbased gapfilling method to account for spatiotemporal correlations in monitoring data. We extensively evaluated the method on its ability to fill data gaps in the groundwater SpC measurements that are often used to indicate groundwater and river water interactions along river corridors. We took advantage of a 10year, spatially distributed, multivariable timeseries dataset collected by a groundwater monitoring well network and optimized an LSTM architecture for filling SpC data gaps. A primary advantage of using LSTM is its ability to incorporate spatiotemporal correlations and nonlinearity in model states without a priori assuming an explicit form of correlations or nonlinear functions in advancing system states. We compared the performance of a singlewell LSTMbased gapfilling method with a traditional gapfilling method, ARIMA, to evaluate how well an LSTM model can capture multifrequency dynamics. We also trained LSTM and ARIMA models that take input from multiple wells to predict responses at one well. The multiwell models were compared with singlewell models to identify and assess improvements in gapfilling performance from including additional spatial correlation from neighboring wells.
In general, both LSTM and ARIMA methods were highly accurate in filling smaller data gaps (i.e., 1 and 6 h). They were reasonably effective at filling in medium gaps between 12 and 48 h, while more work is needed for gaps larger than 48 h. Both models captured the longterm trends in data (i.e., lowfrequency variations at monthly or seasonal timescales). The ARIMA method was found to have difficulty capturing abrupt changes and is, thus, more suitable for time series with less dynamic behavior. Compared with the ARIMA models, the LSTM models excel in dealing with highfrequency dynamics (daily and subdaily) and nonlinearities, although they require more training data and computational resources. As a side effect of including highfrequency (daily and subdaily) fluctuations in the model, the LSTM approach may produce overly dynamic predictions in time windows that lack dynamics. As with any deep learning method, the availability of sufficient training data that cover a wide range of conditions is critical for the success of LSTM methods. Extrapolating the LSTM models to conditions beyond those in the training data remains a major challenge.
Wavelet analysis could provide useful insights into the dynamic signatures of the data and changes in the composition of their important frequencies over time, which can serve as a basis for selecting an appropriate gapfilling method. For example, the ARIMA method would work well if the dynamics are dominated by seasonal cycles, while more sophisticated approaches like LSTMbased methods could work better if there is evidence of weekly, daily, and subdaily fluctuations. Depending on the mixture of high and lowfrequency variability inherent in the time series, different LSTM architecture and configurations can be explored and evaluated through hyperparameter searches with respect to LSTM layers, dense layers, and activation functions to achieve better performance in capturing complex dynamics. The optimal LSTM model configuration and achievable performance would vary case by case.
We also demonstrated that incorporating spatial information from neighboring stations in LSTM models could contribute to performance improvements under challenging scenarios with dynamic system behaviors and longer data gaps of up to 2 d. However, other alternatives need to be explored for gaps beyond 2 d. Bidirectional and convolutional LSTMs are two promising methods to leverage information from the future time window and spatially distributed networks, respectively. While we introduced a new method that can be broadly applied to fill in gaps in an irregularly spaced network for monitoring groundwater and surface water interactions, the transferability of this method to other monitoring systems could be more extensively evaluated by community participation. When applying LSTM or other DNNbased methods for gap filling, it is important to rigorously evaluate the model performance by asking the following questions:

What is the dynamics signature of the data to be filled?

How is gapfilling performance impacted by the length of gaps?

How does the amount of training data impact the model performance?

How does the choice of the input time window impact gapfilling performance?

How much value can measurements at neighboring add to the performance improvement?
Better capturing spatiotemporal dynamics in system states is essential for generating the most valuable insights to advance our understanding of dynamic complex systems.
The well observations dataset is available from https://sbrsfa.velo.pnnl.gov/datasets/?UUID=14febd8105b647fbbe52439c4382decd (SBRSFA, 2022).
The supplement related to this article is available online at: https://doi.org/10.5194/hess2617272022supplement.
HR and EC developed scripts and performed the analyses; the abovementioned authors contributed equally to the paper. BK contributed to the interpretation of the results. XC conceived and designed the study. All authors contributed to writing the paper.
The contact author has declared that neither they nor their coauthors have any competing interests.
Publisher's note: Copernicus Publications remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
This research was supported by the U.S. Department of Energy (DOE), Office of Biological and Environmental Research (BER), as part of the BER Environmental System Science (ESS) program. A portion of the methodology development was supported by the Laboratory Directed Research and Development Program at Pacific Northwest National Laboratory, a multiprogram national laboratory operated by Battelle for the DOE under contract no. DEAC0576RL01830. This research was performed using PNNL Institutional Computing at Pacific Northwest National Laboratory. This research was also supported in part by the Indiana University Environmental Resilience Institute and the “Prepared for Environmental Change” grand challenge initiative. This paper describes objective technical results and analysis. Any subjective views or opinions that might be expressed in the paper do not necessarily represent the views of the U.S. Department of Energy or the United States Government.
This research has been supported by the U.S. Department of Energy, Biological and Environmental Research (grant no. PNNL SBR SFA).
This paper was edited by Dimitri Solomatine and reviewed by three anonymous referees.
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