The massive socioeconomic impacts engendered by extreme floods provides a clear motivation for improved understanding of flood drivers. We use self-organizing maps, a type of artificial neural network, to perform unsupervised clustering of climate reanalysis data to identify synoptic-scale atmospheric circulation patterns associated with extreme floods across the United States. We subsequently assess the flood characteristics (e.g., frequency, spatial domain, event size, and seasonality) specific to each circulation pattern. To supplement this analysis, we have developed an interactive website with detailed information for every flood of record. We identify four primary categories of circulation patterns: tropical moisture exports, tropical cyclones, atmospheric lows or troughs, and melting snow. We find that large flood events are generally caused by tropical moisture exports (tropical cyclones) in the western and central (eastern) United States. We identify regions where extreme floods regularly occur outside the normal flood season (e.g., the Sierra Nevada Mountains due to tropical moisture exports) and regions where multiple extreme flood events can occur within a single year (e.g., the Atlantic seaboard due to tropical cyclones and atmospheric lows or troughs). These results provide the first machine-learning based near-continental scale identification of atmospheric circulation patterns associated with extreme floods with valuable insights for flood risk management.
Flooding is an ever-present socio-economic risk that is likely to increase in the future under climate change and human development1,2,3. This risk has led to a variety of studies on the natural and anthropogenic causes of floods. Enhancing the predictability of floods through improved understanding of the causal natural mechanisms of flooding requires both a watershed perspective (i.e., evaluation of the status of the catchment, such as land cover, slope, aspect, morphology, initial conditions, and the nature of precipitation inputs) and an atmospheric perspective (i.e., evaluation of synoptic-scale atmosphere circulation patterns and the predictability of precipitation inputs).
Based on studies at the watershed scale, the proximate natural causes of hydrologic floods can be classified as single-day rainfall that rapidly exceeds infiltration capacity, multi-day to week-long rainfall that exceeds soil moisture holding capacity, several-day rainfall that results in a combination of the mechanisms associated with single- and multi-day rainfall, and snowmelt or rain-on-snow4,5. Proximate flood causes are driven by ultimate causes at various spatiotemporal scales, such as (extra)tropical cyclones, sea surface temperature anomalies, and preferred ridge and trough positions6. The importance of ultimate causes in generating flood events has been substantiated by global-scale studies of the correlation between floods and well-known climate patterns such as the El Niño-Southern Oscillation7,8, continental-scale studies which identify atmospheric circulation patterns associated with floods or further investigate the correlation between climate indices and floods9,10, and the myriad of regional- to local-scale studies that establish teleconnections between floods and oceanic-atmospheric patterns11,12,13.
While the natural causes of annual floods have been well-studied and summarized for each state in the United States14; surprisingly, assessment of the natural causes of extreme (e.g., return period of at least 10 years) floods is often limited to event- and regional-scale analyses. For example, studies of this type have analyzed the June 2008 floods in Iowa15, floods in the Ohio River basin and the Southwestern United States with return period greater than 10 years16,17, and floods in southeastern Australia causing record river heights18. Given the extensive damages caused by extreme floods, it is imperative to develop a unified understanding of the natural causes of extreme floods at a near-continental scale. In particular, focusing on atmospheric circulation patterns leading to heavy rainfall, which is an important factor in nearly all except snowmelt-driven extreme floods, can be especially used to inform continental-scale modeling and forecasting efforts, including the one underway with the National Water Model19.
We use self-organizing maps (SOMs), a type of artificial neural network which performs unsupervised clustering, to identify dominant atmospheric circulation patterns (i.e., synoptic-scale ultimate causes of extreme precipitation, that we refer to as circulation patterns or simply patterns) associated with extreme floods across the United States. We assess the characteristics of floods associated with each circulation pattern, including the occurrence frequency, spatial domain, size of events, and seasonality. This evaluation of the atmospheric circulation patterns associated with extreme floods at the near-continental scale provides a first-order basis for developing an understanding of how future flood risk may change through the lens of potential changes in atmospheric circulation patterns.
Circulation patterns associated with extreme floods
The circulation patterns associated with extreme floods in the contiguous United States are grouped into three regions: West, Central and East. The West region (Fig. 1, Table 1) is represented by a 2 × 3 SOM which includes gages in hydrologic unit codes (HUCs) 14 through 18 and any gages in HUC 10 at elevation higher than 4,000 feet, for a total of 169 record floods and 1,223 peaks-over-threshold (POT) floods. The West region has a longitude-latitude domain of 20°–56°N and 150°–96°W for the atmospheric fields. Note that only five, not six, patterns are shown (see Supplemental Material for explanation). West region circulation patterns are snowmelt, Pacific trough, Pacific tropical cyclone, and northern and southern pineapple express.
The Central region (Fig. 2, Table 2) is represented by a 1 × 3 SOM which includes gages in HUCs 7 through 9 and 11 through 12, any gages in HUC 10 at elevation less than 4,000 feet, and any gages in HUC 4 west of 87°W, for a total of 316 record floods and 2,183 POT floods. The Central region has a longitude-latitude domain of 24°–50°N and 112°–86°W for the atmospheric fields. Central region circulation patterns are central winter storm, warm season Great Plains jet, and Gulf of Mexico meridional transport.
The East region (Fig. 3, Table 3) is represented by a 2 × 2 SOM which includes gages in HUCs 1 through 3, HUCs 5 and 6, and all gages in HUC 4 east of 87°W, for a total of 196 record floods and 1,467 POT floods. The East region has a longitude-latitude domain of 20°–50°N and 100°–60°W for the atmospheric fields. East region circulation patterns are cold season extratropical cyclone, east winter storm, Gulf of Mexico meridional transport, and Atlantic tropical cyclone (includes hurricanes).
For a given circulation pattern, the record and POT floods generally occur at the same time of year and in the same geographical region; additionally, for a given pattern, the percent of all record and POT floods in the region that are assigned to the pattern is very similar. For example, in the West region, 43.2% and 47% of record and POT floods, respectively, are assigned to snowmelt and occur primarily in May and June in the Rocky Mountains (Fig. 1, top row). However, POT floods do span a wider range of months and a larger geographical region than record floods.
Some circulation patterns are evident in multiple regions. For example, the seasonality and atmospheric fields associated with central and east winter storm are very similar, especially in the north (for the portion of the Central atmospheric domain which overlaps with the East domain). Another example is Gulf of Mexico meridional transport which causes extreme flooding in both the Central and East regions in a continuous geographical domain stretching from the lower Mississippi River basin into the Ohio River basin.
Interestingly, some circulation patterns have similar atmospheric signatures but are displaced in time or space. For example, in the West region, northern and southern pineapple express are both cold season tropical moisture exports from the central Pacific, but the former is steered to the north by the North Pacific High. In the Central region, winds in both warm season Great Plains jet and Gulf of Mexico meridional transport come from the Gulf of Mexico and curve to the northeast, but the primary distinguishing characteristic between the two patterns is their seasonality, with associated differences in temperature and magnitude of moisture transport, as well as steering (Gulf of Mexico meridional transport is steered further eastward). In the East region, the eastern winter storm, which is often associated with a multi-day rising limb of the flood hydrograph, may be a cold season extratropical cyclone that has dissipated and moved to the northeast.
Record and POT flood characteristics by circulation pattern
Figure 4 shows the characteristics of record and POT floods associated with each circulation pattern. Warm season Great Plains jet is the most active pattern, causing on average approximately 1.4% of all contiguous United States gages to have a POT flood in any given year. Other active patterns include snowmelt in the West region, central winter storm in the Central region, Atlantic tropical cyclone in the East region, and Gulf of Mexico meridional transport in the Central and East regions.
In the West region, the northern and southern pineapple express are the dominant circulation patterns on the coast and in the Sierra Nevada and Cascade Mountain ranges, snowmelt is the dominant pattern in the Rocky Mountains, and Pacific trough is the dominant pattern in the Southwest; Pacific tropical cyclone is never dominant. In the Central region, dominance of a single circulation pattern over a distinct spatial domain is not as evident as in the West region; however, central winter storm is generally confined to either far north or far south, while warm season Great Plains jet and Gulf of Mexico meridional transport are generally more active in the west and the east, respectively. In the East region, Gulf of Mexico meridional transport is clearly dominant in the Ohio River basin and southward; the remaining three circulation patterns impact the Atlantic seaboard but have no clear dominance over a given spatial domain.
Many record and POT floods caused by southern pineapple express occur in large events (i.e., multiple gage locations are flooded at the same time) and are primarily located in northern California and Oregon; particularly exceptional events occurred during Christmas 1964 and New Year’s 199720,21. Other patterns that cause large events include snowmelt in the Rocky Mountains, warm season Great Plains jet and Gulf of Mexico meridional transport in the Midwest, particularly in December 1982 and June 200815,22, and Atlantic tropical cyclone in the mid-Atlantic states, particularly Hurricane Agnes in June 197223.
In the West region, altered flood seasonality (i.e., the record or POT flood occurs more than 90 days away from the mean day of flood occurrence) is most prominent in the Sierra Nevada Mountains, where nearly all record and POT floods occur in winter due to the southern pineapple express, rather than in the late spring due to snowmelt. Notably, seasonality is rarely altered in the Rocky Mountains and northern central United States where floods are caused by snowmelt or central winter storm. In the Central region, both warm season Great Plains jet and Gulf of Mexico meridional transport cause altered seasonality, most prominently in the lower western Mississippi River basin. In the East region, most record and POT floods east of the Appalachian Mountains caused by Atlantic tropical cyclone have an altered seasonality, occurring in late summer rather than during spring storms.
Results outside the contiguous United States
Due to limited data availability, only a partial analysis was performed for HUCs 19 through 21 (for more details, see Supplemental Material). Alaska (HUC 19) is represented by a 2 × 2 SOM with a total of 17 record and 82 POT floods; the longitude-latitude domain is 54°–74°N and 170°–128°W for the atmospheric fields. Alaska circulation patterns are Gulf of Alaska low, snowmelt, Bering Sea jet, and Gulf of Alaska jet. Hawaii (HUC 20 without gages in Guam or American Samoa, which were not analyzed) is represented by a 2 × 2 SOM with a total of 27 record and 181 POT floods; the longitude-latitude domain is 10°–30°N and 170°–142°W for the atmospheric fields. Hawaii circulation patterns are Pacific tropical cyclone, kona low, upper trough, and cold front. Puerto Rico (HUC 21) is represented by a 1 × 2 SOM with a total of 12 record and 70 POT floods; the longitude-latitude domain is 10°–26°N and 74°–58°W for the atmospheric fields. Puerto Rico circulation patterns are Atlantic tropical cyclone and cold front.
One limitation of our analysis is the temporal and spatial coverage of the streamflow data. There are limited gage locations in the Southwest northward to Montana (Fig. 4) and there is a relatively high density of gages in the Central region (not shown). Additionally, because the longest available continuous water year record was used for each gage location, the data records are not consistent across locations. A potential consequence of this is limited characterization of circulation patterns in the Southwest; thus, it is possible that Pacific tropical cyclone would be dominant if more data were available. Furthermore, the frequency of flood events caused by circulation patterns in the Central region (e.g., warm season Great Plains jet), may be unduly enhanced due to the higher sampling.
Another limitation is the finite number of circulation patterns identified by the SOMs (i.e., 12 for the contiguous United States). Thus, a pattern which occurs infrequently may not be represented by a unique cluster. For example, in the West region, a few POT summer floods in the central Sierra Nevada Mountains and the Olympic Peninsula are assigned to Pacific tropical cyclone. Similarly, in the Central region, the few summer floods associated with tropical cyclones from the Gulf of Mexico or with mesoscale convective systems are assigned to warm season Great Plains jet. And finally, in the East region, some floods associated with warm season southerly moisture transport from the Gulf of Mexico are assigned to Atlantic tropical cyclone. In all these cases, the cluster assignments likely occur because Pacific or Atlantic tropical cyclone and warm season Great Plains jet are the only warm season circulation patterns in the West, East, and Central regions, respectively. A similar limitation is that only atmospheric fields are used as input data to the SOMs, meaning that antecedent conditions (e.g., snowpack and soil moisture) are not explicitly considered. This limitation can lead to incorrect cluster assignments for snowmelt or rain-on-snow floods and floods caused by light or normal rainfall on high soil moisture conditions. For example, the Central region has no snowmelt-only pattern despite snowmelt floods occurring in the northern portion of the region.
Finally, the SOMs as currently configured do not track the movement of an atmospheric phenomenon in space and time. This limitation is exacerbated by the fact that (i) the boundaries of the West, Central and East region are, to some degree, arbitrary discontinuities imposed on a continuous geographical domain, and (ii) the date of the flood is not explicitly provided as input data, but rather is implicit in that the atmospheric fields are from two days before the record or POT flood (the temperature data also implicitly indicates cold or warm season). In consequence, there is a limit to the extent a single atmospheric phenomenon can be transposed in space but still be identified as one phenomenon by the SOM. This is likely a contributing factor to the omission of Gulf of Mexico tropical cyclones in the Central region and is likely the reason why winds in Atlantic tropical cyclone in the East region are weak, having been smeared over multiple storm centers.
Another consequence of this final limitation is that the same circulation patterns affect multiple regions (e.g., Gulf of Mexico meridional transport in the Central and East regions) and one event may be split across regions or across patterns, which would negatively bias the calculation of large events and lead to incorrect cluster assignments. For example, in the East region, four locations in relatively close geographical proximity in Georgia and Florida experienced a record flood between April 2nd and 5th in 1948 but were assigned to Gulf of Mexico meridional transport, cold season extratropical cyclone, and eastern winter storm depending on the date. The specific atmospheric fields associated with each date (not shown) clearly indicate that all four record floods were caused by one atmospheric wave. However, that atmospheric wave changed sufficiently and quickly during its eastward progression across the United States such that the SOM assigned the floods to three different patterns. This limitation is likely amplified by the choice of atmospheric data only on the date two days before the flood because in general, daily circulation patterns exhibit large variability; however, the circulation patterns associated with extreme floods tend to be more persistent than usual (e.g., a front becomes stalled over a region). One possible solution would be to use a multi-day average of the atmospheric data, recognizing that doing so would cause spatiotemporal smearing of circulation patterns, possibly obscuring extremes.
This paper presents the first near-continental scale identification of synoptic-scale atmospheric circulation patterns associated with extreme floods. Furthermore, this study demonstrates that, despite some limitations, identification of these patterns can be effectively accomplished by applying SOMs at judiciously chosen spatial scales to basic reanalysis atmospheric fields associated with extreme floods (see methods for more details). The results of this analysis provide valuable insights that can be used for improved flood risk preparation and management.
One insight is that although 12 circulation patterns were identified for the contiguous United States, the similarity in atmospheric fields implies four primary categories: tropical moisture exports (encompasses northern and southern pineapple express, warm season Great Plains jet, and Gulf of Mexico meridional transport in both the Central and East regions; accounts for a total of 411 record and 2,782 POT floods), tropical cyclones (encompasses Pacific tropical cyclone and Atlantic tropical cyclone; accounts for a total of 80 record and 488 POT floods), atmospheric lows or troughs (encompasses Pacific trough, eastern winter storm and possibly central winter storm, and cold season extratropical cyclone; accounts for a total of 117 record and 1,028 POT floods) and melting snow (snowmelt; accounts for a total of 73 record and 575 POT floods; note that during cold season tropical moisture exports or atmospheric lows, melting snow can also be an important factor in causing floods at high elevations or northern locations). This result implies that overall there are only a few distinct types of circulation patterns causing extreme floods in the contiguous United States and highlights that these types of patterns should be prioritized in efforts to assess and improve weather forecasting models.
Another insight is gained in the identification of circulation patterns which tend to cause clustering of extreme floods and the associated spatial domains where clustering occurs. Broadly, the results show that large events usually occur in the West and Central regions due to tropical moisture exports, and in the East region due to tropical cyclones. This corroborates previous statistical analysis showing that record floods across the United States are “on average more extreme than would be expected if they occurred randomly, and that they tend to form spatial clusters”24. Additionally, regions which exhibit spatial clustering of record floods generally correspond to regions where the climatological length scale of extreme precipitation is high (i.e., extreme precipitation falls over a large region)25, although the correspondence is not exact. Knowledge of which regions tend to experience spatial clustering of extreme flood events enables improved disaster preparedness and management. For example, it may be possible to reduce the likelihood of uncontrolled spill from flood control reservoirs by coordinating operations to account for one large flood event that affects a whole region. Similarly, emergency supplies and essential facilities can be strategically placed to provide adequate aid in the scenario that a whole region is affected26.
A third insight is in understanding the dominant circulation patterns and seasonality of extreme floods in a given spatial domain. In a region dominated by one pattern, there is a high likelihood that extreme floods will only occur during the time of year the pattern occurs. Notably, this is not necessarily during the regular flood season, which can present significant challenges for flood control operations designed for regular season flood events. For example, in the Sierra Nevada Mountains, southern pineapple express causes rain-on-snow floods in December through March, which is several months before the regular snowmelt-driven flood season of May through June. In 1997 in particular, when a southern pineapple express followed an already abnormally wet winter, multiple levees failed and multiple reservoirs in the San Joaquin and Sacramento River basins were at capacity, threatening major downstream flooding; of these, the Don Pedro reservoir had an uncontrolled release of water over the emergency spillway27. Yet based on historical records, the Christmas Eve 1861 event, caused by a prolonged southern pineapple express, was even larger and more devastating28. Conversely, in a region where no one circulation pattern is dominant, there is the possibility of a much wider timeframe in which extreme floods may occur and furthermore, multiple extreme flood events may occur in the same year due to different patterns. For example, the Atlantic seaboard may experience floods throughout the whole year; in particular on the Pigg River in Virginia, the record flood occurred in September 1987 due to Atlantic tropical cyclone and the second highest flood occurred earlier that year in April due to Gulf of Mexico meridional transport. These results highlight regions of the country that would benefit from flood control and disaster preparedness operations designed for both the regular flood season and an extreme flood season that may occur at a different time of year.
There are a variety of directions to extend these results. The methodology could be improved to enable tracking of atmospheric wave propagation in space and time, enabling deeper understanding of whether one atmospheric phenomenon can engender multiple flood-causing circulation patterns. This could be accomplished by incorporating lagged atmospheric fields in the SOM. This method could be applied to other continents to develop a global understanding of circulation patterns associated with extreme floods. Further investigation could also examine the implications of these results for flood risk, including: dependence (are there dependencies between different circulation patterns that may lead to multiple temporally-proximate extreme floods), attribution (how does the frequency and intensity of the circulation patterns relate to large-scale oceanic-atmospheric modes of climate variability), forecasting (how often does the occurrence of a given circulation pattern result in an extreme flood), non-stationarity and projection (has the frequency and intensity of the circulation patterns changed historically and is it projected to change under climate change), and design (how can financial instruments and infrastructure be designed and operated for flood risk mitigation given an improved knowledge of the circulation patterns associated with extreme floods).
Finally, to further inform flood management for a particular location of interest and recognizing the limitations of the results presented herein, an interactive website with detailed information for each record flood has been developed (https://kschlef.shinyapps.io/ExtremeFloods/). In addition to the reanalysis data and SOM results, data on the presence and type of extreme precipitation29, tropical cyclone tracks30, and tropical moisture exports31, as well as information from historical reports, are provided where relevant and available. This additional data enables a more nuanced perspective on the natural causes of record floods. In particular, the information from historical reports provides insight into the importance of antecedent conditions in setting up the hydrologic conditions that enable an extreme flood. This website is a valuable resource that enables further understanding of the causes and characteristics of the record flood at a location of interest.
Daily reanalysis atmospheric data was obtained from the 20th Century V2 reanalysis data32,33,34, available from 1851–2014 at 2° grid resolution. The atmospheric fields used for analysis were, at the 850 mb level, specific humidity, omega (vertical velocity in pressure units), and zonal and meridional winds, and at the 1,000 mb level, temperature. Initial analysis only included the four atmospheric fields at 850 mb. Omega was chosen to provide information about convective processes, specific humidity and winds were chosen to provide information about the advection and availability of atmospheric moisture, and 850 mb, generally the top of the planetary boundary layer, was chosen as indicative of precipitation-producing processes occurring in the lower atmosphere. However, these atmospheric fields alone were not able to appropriately distinguish between cold- and warm-season circulation patterns; adding temperature at the 1,000 mb (i.e., near surface) level solved this problem.
Daily streamflow data was obtained from United States Geological Survey gages designated as part of the Hydro-Climatic Data Network35 for the contiguous United States (i.e., HUCs 1 through 18). Data pre-processing occurred as follows: gages with basin area less than 200 square miles were excluded; for each gage, after the exclusion of any data after 2014 (due to the availability of the reanalysis data), the longest period of continuous data was cut to begin and end with the water year (October 1 through September 30); any gages with less than 30 water years of continuous data were excluded. This process resulted in a total of 681 gages with data spanning water years 1874–2014. Gages in HUCs 19 (Alaska), 20 (Hawaii, Guam and American Samoa), and 21 (Puerto Rico) were processed separately following the same procedure except the requirement of a minimum basin area of 200 square miles was relaxed due to the limited number of available gages.
From the daily streamflow data, the record flood, the water year timeseries of annual maximum daily streamflow (AMS), and peaks-over-threshold (POT) floods were calculated for each gage. The record flood was defined to occur on the date associated with the maximum value of daily streamflow. The POT floods, of which the record floods are a subset, were defined to occur on the date associated with a local maxima value of daily streamflow over a threshold value. The threshold was set to the 10-year flood, determined by fitting a log-Pearson type III distribution to the AMS timeseries. Additionally, the POT floods were constrained to be at least eight days apart, to avoid double-counting an event. Due to the procedure used for data pre-processing, it is possible that the identified record flood is not the same as the known flood of record for a given location.
Training and validation of clustering algorithm
Self-organizing maps (SOMs) were used to perform unsupervised clustering of the circulation patterns associated with floods. A SOM is an artificial neural network which uses a decaying neighborhood function and learning rate parameter to identify a one- or two-dimensional lattice of explanatory codes to which each individual data point is assigned36. The dimensions of the lattice determine the total number of codes as well as the number of neighbors for each code; here, a 2 × 3 SOM indicates a lattice of two columns and three rows, with a total of six codes. SOMs were chosen over supervised manual clustering, which has been used for precipitation extremes29, because of reduced subjectivity and the ability to perform validation and easily extend to other datasets besides that used for training; similarly, SOMs were chosen over other clustering algorithms such as k-means or principal component analysis because they allow increased flexibility in cluster characteristics, they imply a topographical continuity between codes as imposed by the neighborhood function (although this can impose constraints on the number of codes), and they allow inclusion of multiple distinct input variables37. Additionally, SOMs have been previously used for clustering atmospheric circulation patterns associated with temperature and precipitation extremes: examples include Alaska38, the northwestern United States39, and central Italy40.
The input data to the SOM are the five reanalysis fields over a longitude-latitude domain for the date two days prior to each record or POT flood. As in previous similar studies, data in each grid cell was normalized (e.g., subtract the mean and divide by the standard deviation over all flood dates) and weighted by the square root of the cosine of latitude39. Only record floods were used to develop the SOMs; POT floods were subsequently assigned to existing clusters. Each code from the fitted SOMs represents a distinct pattern associated with the floods placed in that code’s cluster. The observed similarities between record and POT floods (discussed in results), provides further confidence in the SOMs in addition to the validation procedures (described below).
The key choices in developing the SOMs included (i) choice of region, specified by the flood locations and the longitude-latitude domain for the reanalysis data, (ii) choice of floods to use for initialization, and (iii) choice of map topography, specified by the number of codes and the dimensions of the rectangular lattice. A variety of different SOM configurations were assessed based on physical interpretability and robustness under cross-validation (described below and in further detail in Supplemental Material); the best SOMs were retained for further analysis.
Physical interpretability was assessed based on a three factors: (i) how well months of flood occurrence were partitioned (e.g., October floods should not be clustered with January floods), (ii) whether the code was a recognizable atmospheric pattern appropriate to the associated months (e.g., a code with wind fields that clearly show a hurricane pattern should be associated with floods which occur in late summer), and (iii) whether floods for which the atmospheric circulation pattern is known a priori, based on literature or historic reports or characteristics of the flood or streamflow timeseries, were correctly clustered (e.g., floods caused by a hurricane should be clustered together and should not be clustered with floods caused by a winter storm). This analysis, which was iterative and made use of the additional information now available for each record flood on the website, also informed the pattern name given to each of the SOM codes.
Cross-validation for a given SOM configuration was performed by first fitting the SOM to the full data to create an original cluster assignment. Subsequently, 100 trials were performed in which, excepting the floods used for initialization, 90% of the floods were used as training data to fit a new SOM; the new SOM was then used to predict the cluster assignments of the remaining 10% of validation floods. Robustness under cross-validation was assessed using the adjusted rand index (ARI) and a metric of flood reassignment. The ARI measures the degree of overlap between two different sets of clusters; an ARI of zero indicates no overlap while an ARI of one indicates complete overlap. For each of the 100 trials, an ARI was calculated between (i) the clusters of the original data and the training data and (ii) the clusters of the original data and the training and validation data combined. Flood reassignment was calculated as the percent of floods for which the cross-validation cluster assignment was different than the original cluster assignment in at least 10% of the 100 trials. High ARIs and low flood reassignment indicated a robust SOM configuration.
Calculation of flood characteristics
The prominence of circulation patterns in different regions of the United States was determined by finding which pattern caused the most POT floods in each 1° grid cell. For each pattern, a percent flood occurrence was calculated for each year by dividing the number of floods associated with that pattern by the number of all operational gages across all patterns; this accounts for the different number of operational gages each year. The frequency of flood occurrence was calculated as the mean of the percent flood occurrence across all years.
Flood events (i.e., the same circulation pattern is associated with flooding at the same time at multiple gage locations) were identified by grouping the floods associated with a given pattern by the date of occurrence, such that no more than two days separate each consecutive flood within an event. Event size was defined to be the number of floods associated with each event. Large events were defined to have an event size at least as large as the 99th percentile of event size calculated from all events across all patterns; this does not account for the different number of operational gages each year.
Circular statistics41 were used to (i) calculate the mean day of flood occurrence and the seasonality index from the AMS timeseries and (ii) calculate the difference between the day of the record or POT flood and the mean day of flood occurrence. A flood was considered seasonally altered if it occurred more than 90 days before or after the mean day of flood occurrence.
Processed data and code are available on Hydroshare (Katherine Schlef, Extreme Floods Code and Data); original data are available from cited sources.
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Arnell, N. W. & Gosling, S. N. The impacts of climate change on river flood risk at the global scale. Clim. Change 134, 387–401, https://doi.org/10.1007/s10584-014-1084-5 (2016).
Winsemius, H. C. et al. Global drivers of future river flood risk. Nat. Clim. Chang 6, 381–385, https://doi.org/10.1038/NCLIMATE2893 (2016).
Dottori, F. et al. Increased human and economic losses from river flooding with anthropogenic warming. Nat. Clim. Chang. 8, 781–786, https://doi.org/10.1038/s41558-018-0257-z (2018).
Merz, R. & Blöschl, G. A process typology of regional floods. Water Resour. Res. 39, 1340, https://doi.org/10.1029/2002WR001952 (2003).
Berghuijs, W. R., Woods, R. A., Hutton, C. J. & Sivapalan, M. Dominant flood generating mechanisms across the United States. Geophys. Res. Lett. 43, 4382–4390, https://doi.org/10.1002/2016GL068070 (2016).
Hirschboeck, K. Flood hydroclimatology. Flood Geomorphol, 27–49 (1988).
Lee, D., Ward, P. & Block, P. Attribution of Large-Scale Climate Patterns to Seasonal Peak-Flow and Prospects for Prediction Globally. Water Resour. Res. 54, 916–938, https://doi.org/10.1002/2017WR021205 (2018).
Ward, P. J., Eisner, S., Flörke, M., Dettinger, M. D. & Kummu, M. Annual flood sensitivities to El Niño-Southern Oscillation at the global scale. Hydrol. Earth Syst. Sci. 18, 47–66, https://doi.org/10.5194/hess-18-47-2014 (2014).
Jacobeit, J., Glaser, R., Luterbacher, J. & Wanner, H. Links between flood events in central Europe since AD 1500 and large-scale atmospheric circulation modes. Geophys. Res. Lett. 30, 1172, https://doi.org/10.1029/2002GL016433 (2003).
Liu, J., Zhang, Y., Yang, Y., Gu, X. & Xiao, M. Investigating Relationships Between Australian Flooding and Large-Scale Climate Indices and Possible Mechanism. J. Geophys. Res. Atmos. 123, 8708–8723, https://doi.org/10.1029/2017JD028197 (2018).
Bracken, C., Holman, K. D., Rajagopalan, B. & Moradkhani, H. A Bayesian Hierarchical Approach to Multivariate Nonstationary Hydrologic Frequency Analysis. Water Resour. Res. 54, 243–255, https://doi.org/10.1002/2017WR020403 (2018).
Nayak, M. A. & Villarini, G. A long-term perspective of the hydroclimatological impacts of atmospheric rivers over the central United States. Water Resour. Res. 53, 1144–1166, https://doi.org/10.1002/2016WR019033 (2017).
Schlef, K. E., François, B., Robertson, A. W. & Brown, C. A General Methodology for Climate-Informed Approaches to Long-Term Flood Projection - Illustrated with the Ohio River Basin. Water Resour. Res. 54, https://doi.org/10.1029/2018WR023209 (2018).
Perry, C. A., Aldridge, B. N. & Ross, H. C. Summary of Significant Floods in the United States, Puerto Rico, and the Virgin Islands, 1970 through 1989, https://doi.org/10.3133/wsp2502 (USGS Water-Supply Paper 2502, 2001).
Smith, J. A., Baeck, M. L., Villarini, G., Wright, D. B. & Krajewski, W. Extreme Flood Response: The June 2008 Flooding in Iowa. J. Hydrometeorol. 14, 1810–1825, https://doi.org/10.1175/JHM-D-12-0191.1 (2013).
Nakamura, J., Lall, U., Kushnir, Y., Robertson, A. W. & Seager, R. Dynamical Structure of Extreme Floods in the U.S. Midwest and the United Kingdom. J. Hydrometeorol. 14, 485–504, https://doi.org/10.1175/JHM-D-12-059.1 (2013).
Ely, L. L., Enzel, Y. & Cayan, D. R. Anomalous North Pacific Atmospheric Circulation and Large Winter Floods in the Southwestern United States. J. Clim. 7, 977–987 (1994).
Callaghan, J. & Power, S. Major coastal flooding in southeastern Australia 1860–2012, associated deaths and weather systems. Aust. Meteorol. Oceanogr. J 64, 183–213, https://doi.org/10.22499/2.6403.002 (2014).
Office of Water Prediction. The National Water Model. Available at, http://water.noaa.gov/about/nwm. (Accessed: 1st March 2019).
Harmon, J. G. Floods in Northern California , January 1997. (USGS Fact Sheet FS-073-99, 1999).
Waananen, A. O., Harris, D. D. & Williams, R. C. Floods of December 1964 and January 1965 in the Far Western States: Part 1. Description, https://doi.org/10.3133/wsp1866A (USGS Water-Supply Paper 1866-A, 1971).
Sauer, V. B. & Fulford, J. M. Floods of December 1982 and January 1983 in Central and Southern Mississippi River Basin, https://doi.org/10.3133/ofr83213 (USGS Open-File Report 83–213, 1983).
Disaster Survey Team. Final Report of the Disaster Survey Team on the Events of Agnes. (NOAA Natural Disaster Survey Report 73-1, 1973).
Douglas, E. M. & Vogel, R. M. Probabilistic Behavior of Floods of Record in the United States. J. Hydrol. Eng. 11, 482–488, https://doi.org/10.1061/(ASCE)1084-0699(2006)11:5(482) (2006).
Touma, D., Michalak, A. M., Swain, D. L. & Diffenbaugh, N. S. Characterizing the Spatial Scales of Extreme Daily Precipitation in the United States. J. Clim. 31, 8023–8037, https://doi.org/10.1175/JCLI-D-18-0019.1 (2018).
Shang, H., Yan, J. & Zhang, X. El Niño – Southern Oscillation influence on winter maximum daily precipitation in California in a spatial model. Water Resour. Res. 47, W11507, https://doi.org/10.1029/2011WR010415 (2011).
Fridirici, R. & Shelton, M. L. Natural and Human Factors in Recent Central Valley Floods. Yearb. Assoc. Pacific Coast Geogr. 62, 53–69 (2000).
Dettinger, M. D. & Ingram, B. L. The Coming Megafloods. Sci. Am. 308, 64–71 (2013).
Kunkel, K. E. et al. Meteorological Causes of the Secular Variations in Observed Extreme Precipitation Events for the Conterminous United States. J. Hydrometeorol. 13, 1131–1141, https://doi.org/10.1175/JHM-D-11-0108.1 (2012).
Landsea, C. W. & Franklin, J. L. Atlantic Hurricane Database Uncertainty and Presentation of a New Database Format. Mon. Weather Rev. 141, 3576–3592, https://doi.org/10.1175/MWR-D-12-00254.1 (2013).
Knippertz, P. & Wernli, H. A lagrangian climatology of tropical moisture exports to the northern hemispheric extratropics. J. Clim. 23, 987–1003, https://doi.org/10.1175/2009JCLI333 (2010).
Compo, G. P. et al. The Twentieth Century Reanalysis Project. Q. J. R. Meteorol. Soc. 137, 1–28, https://doi.org/10.1002/qj.776 (2011).
Compo, G. P., Whitaker, J. S. & Sardeshmukh, P. D. Feasibility of a 100-year reanalysis using only surface pressure data. Bull. Am. Meteorol. Soc. 87, 175–190, https://doi.org/10.1175/BAMS-87-2-175 (2006).
Whitaker, J. S., Compo, G. P., Wei, X. & Hamill, T. M. Reanalysis before radiosondes using ensemble data assimilation. Mon. Weather Rev. 132, 2983–2991, https://doi.org/10.1175/1520-0493(2004)132<1190:RWRUED>2.0.CO;2 (2004).
Landwehr, J. M. & Slack, J. R. Hydro-Climatic Data Network: A U.S. Geological Survey streamflow data set for the United States for the study of climate variations, 1874–1988. (USGS Open-File Report 92-129, 1992).
Haykin, S. Neural Networks and Learning Machines. (Prentice Hall, 2009).
Reusch, D. B., Alley, R. B. & Hewitson, B. C. Relative Performance of Self-Organizing Maps and Principal Component Analysis in Pattern Extraction from Synthetic Climatological Data. Polar Geogr 29, 188–212, https://doi.org/10.1080/789610199 (2005).
Cassano, J. J., Cassano, E. N., Seefeldt, M. W., Gutowski, W. J. Jr. & Glisan, J. M. Synoptic conditions during wintertime temperature extremes in Alaska. J. Geophys. Res. Atmos. 121, 3241–3262, https://doi.org/10.1002/2015JD024404 (2016).
Loikith, P. C., Lintner, B. R. & Sweeney, A. Characterizing large-scale meteorological patterns and associated temperature and precipitation extremes over the northwestern United States using self-organizing maps. J. Clim. 30, 2829–2847, https://doi.org/10.1175/JCLI-D-16-0670.1 (2017).
Conticello, F., Cioffi, F., Merz, B. & Lall, U. An event synchronization method to link heavy rainfall events and large-scale atmospheric circulation features. Int. J. Climatol. 38, 1421–1437, https://doi.org/10.1002/joc.5255 (2018).
Villarini, G. On the seasonality of flooding across the continental United States. Adv. Water Resour. 87, 80–91, https://doi.org/10.1016/j.advwatres.2015.11.009 (2016).
Boner, F. C. & Stermitz, F. Floods of June 1964 in Northwestern Montana. (USGS Water-Supply Paper 1840-B, 1967).
Paulsen, C. G. Floods of May-June 1948 in Columbia River Basin, https://doi.org/10.3133/wsp1080 (USGS Water-Supply Paper 1080, 1949).
Rivera, E. R., Dominguez, F. & Castro, C. L. Atmospheric Rivers and Cool Season Extreme Precipitation Events in the Verde River Basin of Arizona. J. Hydrometeorol. 15, 813–829, https://doi.org/10.1175/JHM-D-12-0189.1 (2014).
Reid, J. K. Summary of Floods in the United States During 1969, 10.3313.wsp2030 (USGS Water-Supply Paper 2030, 1975).
Aldridge, B. N. & Hales, T. A. Floods of November 1978 to March 1979 in Arizona and west-central New Mexico, https://doi.org/10.3133/wsp2241 (USGS Water-Supply Paper 2241, 1984).
Higgins, R. W., Yao, Y. & Wang, X. L. Influence of the North American Monsoon System on the U.S. Summer Precipitation Regime. J. Clim. 10, 2600–2622 (1997).
Adams, D. K. & Comrie, A. C. The North American Monsoon. Bull. Am. Meteorol. Soc. 78, 2197–2213 (1997).
Saarinen, T. F., Baker, V. R., Durrenberger, R. & Maddock, T. Tucson, Arizona, flood of October 1983. (National Academies Press, 1984).
National Weather Service. Hurricane Joanne. Available at, https://www.wrh.noaa.gov/twc/tropical/joanne_1972.htm (2018).
Rutz, J. J., Steenburgh, W. J. & Ralph, F. M. The Inland Penetration of Atmospheric Rivers over Western North America: A Lagrangian Analysis. Mon. Weather Rev. 143, 1924–1944, https://doi.org/10.1175/MWR-D-14-00288.1 (2015).
Hubbard, L. L. Floods of November 1990 in Western Washington, https://doi.org/10.3133/ofr93631 (USGS Open-File Report 93–631, 1994).
Colle, B. A. & Mass, C. F. The 5–9 February 1996 flooding event over the Pacific Northwest: sensitivity studies and evaluation of the MM5 precipitation forecasts. Mon. Weather Rev. 128, 593–617 (2000).
Hammond, S. E. & Harmon, J. G. Publications Document Floods of January 1997 in California and Nevada. (USGS Fact Sheet FS-093-98, 1998).
Isard, S. A., Angel, J. R. & VanDyke, G. T. Zones of Origin for Great Lakes Cyclones in North America, 1899–1996. Mon. Weather Rev. 128, 474–485 (2000).
Reitan, C. H. Frequencies of Cyclones and Cyclogenesis for North America, 1951–1970. Mon. Weather Rev. 102, 861–868 (1974).
Westerman, D. A., Merriman, K. R., De Lanois, J. L. & Berenbrock, C. Analysis and Inundation Mapping of the April – May 2011 Flood at Selected Locations in Northern and Eastern Arkansas and Southern Missouri, https://doi.org/10.3133/sir20135148 (USGS Scientific Investigations Report 2013–5148, 2013).
Lavers, D. A. & Villarini, G. Atmospheric rivers and flooding over the central United States. J. Clim. 26, 7829–7836, https://doi.org/10.1175/JCLI-D-13-00212.1 (2013).
Bell, G. D. & Janowiak, J. E. Atmospheric Circulation Associated with the Midwest Floods of 1993. Bull. Am. Meteorol. Soc. 76, 681–695 (1995).
Steinschneider, S. & Lall, U. Spatiotemporal structure of precipitation related to tropical moisture exports over the eastern United States and its relation to climate teleconnections. J. Hydrometeorol. 17, 897–913, https://doi.org/10.1175/JHM-D-15-0120.1 (2016).
Lu, M. & Lall, U. Tropical Moisture Exports, Extreme Precipitation and Floods in Northeastern US. Earth Science Research 6, 91–111, https://doi.org/10.5539/esr.v6n2p91 (2017).
Smith, J. A., Villarini, G. & Baeck, M. L. Mixture Distributions and the Hydroclimatology of Extreme Rainfall and Flooding in the Eastern United States. J. Hydrometeorol. 12, 294–309, https://doi.org/10.1175/2010JHM1242.1 (2011).
Grover, N. C. The Floods of March 1936: Part 1. New England Rivers, https://doi.org/10.3133/wsp798 (USGS Water-Supply Paper 798, 1937).
Miller, A. J. Flood Hydrology and Geomorphic Effectiveness in the Central Appalachians. Earth Surf. Process. Landforms 15, 119–134 (1990).
Frankenfield, H. C. Rivers and Floods. Mon. Weather Rev. 54, 111–118 (1929).
Smith, J. A. & Baeck, M. L. ‘Prophetic vision, vivid imagination’: The 1927 Mississippi River flood. Water Resour. Res. 51, 9964–9994, https://doi.org/10.1002/2015WR017927 (2015).
Glatfelter, D. R. & Chin, E. H. Floods of March 1982 in Indiana, Ohio, Michigan, and Illinois. (USGS Professional Paper 1467, 1988).
Villarini, G., Goska, R., Smith, J. A. & Vecchi, G. A. North atlantic tropical cyclones and U.S. flooding. Bull. Am. Meteorol. Soc. 95, 1381–1388, https://doi.org/10.1175/BAMS-D-13-00060.1 (2014).
Suro, T. P., Roland, M. A. & Kiah, R. G. Flooding in the Northeastern United States, 2011, https://doi.org/10.3133/pp1821 (USGS Professional Paper 1821, 2015).
This research is based on work supported by the Science and Technology Directorate of the U.S. Department of Homeland Security for the Flood Apex Program as a supplement to National Science Foundation agreement: NSF EAR-13386086.