The GRACE constellation is a pair of twin satellites that can measure changes in Earth's gravitational field. There is a precise radar rangefinder between the two satellites. When Earth's gravitational field changes slightly, it can be detected by either of the two satellites. The distance signal between the two satellites is amplified to measure the state change at the current moment relative to the previous moment (Cazenave and Chen, 2010). The short-term gravitational field changes of Earth are mainly caused by changes in factors such as terrestrial water storage, atmospheric water vapor and ocean tides. When these signals are deducted, the change in the entire terrestrial water storage can be inverted (Wahr et al., 1998). The daily GRACE data selected in this study come from daily solutions obtained using Kalman smoothing by Mayer-Gürr et al. (2018), Graz University of Technology, based on the ITSG-Grace2018 gravity field model. The ITSG-Grace2018 gravity field model, which offers unconstrained monthly and Kalman-smoothed daily solutions, is the most recent GRACE-only gravity field model computed in Graz (Mayer-Gürr et al., 2018). The time period spans from 1 April 2002 to 31 August 2016, the resolution is 1∘ and the unit is meters (m). A third-order autoregressive (AR) model was used to stabilize the daily solution. A set of spherical harmonic coefficients for the various degrees (n=2…40) was estimated. When GRACE data were not available for a specific day, daily solutions were delivered through an adjustment process (Bergmann-Wolf et al., 2015; Dill, 2008). These processed data can be obtained from the following website: https://www.tugraz.at/institute/ifg/downloads/gravity-field-models/itsg-grace2018/ (last access: 21 November 2021).

This study used Global Precipitation Measurement (GPM) data to calculate extreme precipitation. GPM is an international satellite mission launched by the National Aeronautics and Space Administration (NASA) and Japan Aerospace Exploration Agency (JAXA). It is the next-generation, high-quality global rain and snow satellite observation network after the TRMM. GPM provides an important data foundation for scientific researchers to understand the Earth's water resources and energy cycles and improve their ability to predict extreme events (Huffman et al., 2019). The resolution of these data is 0.1∘, with the unit of millimeters (mm), mainly covering the range of 60∘ S–60∘ N, and both north–south latitudes of 60–90∘ have partial coverage. This study selects the IMERG Final Run product, which uses global microwave precipitation data, infrared data, precipitation station data and other potential precipitation indicators to cross-calibrate, fuse and interpolate TRMM and GPM data at refined temporal and spatial scales. It is an officially recommended product and can be obtained from the following website: https://gpm.nasa.gov/data/directory (last access: 10 October 2021). To remain consistent with the GRACE resolution and maintain extreme precipitation signals, we take the maximum values of the precipitation covered by each 1∘ GRACE grid to further calculate the flood potential index and the number of extreme precipitation days.

The DFO dataset records large flood events from various news reports as well as governmental, instrumental and remote sensing sources. It contains the start and end times of each flood, the country where it occurred, the approximate flood extent, the cause of the flood and the degree of damage. It is a rare and useful product for studying global historical floods. This data product has been widely used in flood hazard science research (Tellman et al., 2021; Hagen et al., 2010; Winsemius et al., 2013; Idowu and Zhou, 2019). This study focuses on precipitation-induced floods. A total of 2380 flood events in the 60∘ S–60∘ N range were caused by heavy precipitation between 1 April 2002 and 31 August 2016. This product was primarily used to validate the flood data extracted in this study and can be obtained from https://floodobservatory.colorado.edu/Archives/index.html (last access: 1 October 2021).

The flood inundation extent data used in this study come from a total of 807 flood events extracted based on MODIS data by Tellman et al. (2021) in the 60∘ S–60∘ N region from 1 April 2002 to 31 August 2016. This product was produced based on atmospherically corrected Terra (MOD09GA/GQ) and Aqua (MYD09GA/GQ) MODIS images. The authors then used threshold analysis methods (including standard and Otsu-optimized threshold methods) and slope constraints (slopes greater than 5∘ were masked out) to extract inundations at a 250 m spatial resolution according to the flood events recorded by the DFO (Tellman et al., 2021). The MODIS-based floods were compared and verified for coincidence with the 30 m resolution inundation data derived from Landsat 5, 7 and 8 images, and flood map quality control analysis was also performed. This product relies on the Google Earth Engine platform (Gorelick et al., 2017), which can be obtained from the following site: https://developers.google.com/earth-engine/datasets/catalog/GLOBAL_FLOOD_DB_MODIS_EVENTS_V1 (last access: 1 October 2021). These data were further refined on the basis of DFO-recorded approximate flood extent and provided a reliable spatial inundation dataset for verification in our study.

The Global Runoff Data Centre is an international data center operating under the auspices of the World Meteorological Organization. It was established in 1988 to support research on global climate change and integrated water resource management. We downloaded the global mean daily discharge data from https://www.bafg.de/GRDC/EN/Home/homepage_node.html (last access: 2 November 2021), which additionally contained other attributes, like the country, longitude, latitude and river name, associated with each flood event. The unit of mean daily discharge is cubic meters per second (m3 s-1), and the stations with more than 50 % of days missing in the research time period (1 April 2002–31 August 2016) were excluded to ensure accuracy. Finally, we obtained 3408 stations from 1 April 2002 to 31 August 2016 as the validation dataset to verify the GRACE-derived flood days.

Extreme precipitation has sudden characteristics, and its signals are reflected in the high-frequency signals of GRACE (Xiong et al., 2022; Gouweleeuw et al., 2018). Seasonal and trend decomposition using loess (STL) (Robert et al., 1990) is a filtering process as well as a general and robust time series decomposition and forecasting method used to decompose time series variables into seasonal, trend and remainder components for further forecasting. This process can handle data with any type of seasonality as well as high-frequency signal data. It also allows seasonal components to vary over time and is robust to outliers. In this study, we selected this method as a high-pass filtering tool to process GRACE TWS and obtain high-frequency signals (excluding seasonal and trend components) for subsequent analyses. In this work, the STL function in the R language “stats” package was used to process all grid time series corresponding to the GRACE TWS period (1 April 2002–31 August 2016). The two main parameters, “t.window” and “s.window”, should be specified when using STL. “t.window” is the number of consecutive observations when estimating the trend cycle; it was set to a 31 d window to cover the month and separates daily data according to Gouweleeuw et al. (2018) and Xiong et al. (2022). “s.window” is the number of consecutive years when estimating each value in the seasonal component; it was set to 360, which was determined using a Fourier transform to convert to the frequency domain to obtain the frequency corresponding to the maximum amplitude.

The generalized extreme studentized deviate (GESD) test (Rosner, 1983) is a simple and effective statistical method for detecting one or more outliers in univariate data that follow an approximately normal distribution. It has been widely used in the field of hydrological anomaly detection (Saghafian et al., 2014; Clark and Zipper, 2016). The GESD test is mainly used in this study to extract possible flood days corresponding to the high-frequency signals. In this study, the method selected for extracting flood information from the high-frequency signals needed to ensure minimum impact from the random error in the high-frequency signal and maximum flood signal extraction. The method requires only that an upper bound for suspected outliers be specified and determines the number of possible outliers based on hypothesis testing (Rosner, 1983). The basic assumptions of GESD are as follows:  

there are no outliers in the dataset (H0);

Consistent with the r test statistics, the r critical values are computed as follows: 2λi=(n-i)tp,n-i-1(n-i-1+tp,n-i-12)(n-i+1);i=1,2,…,r;3p=1-α2(n-i+1). Here, tp,v is the 100p percentage point in a t distribution with v degrees of freedom, and α is the significance level. The number of final outliers is then determined by the corresponding maximum i value in Ri>λi (Rosner, 1983).

Considering that the GRACE high-frequency signal contains both random errors and useful signals, we used the GESD test to control the number of outliers so that they were not affected by subjective thresholds. In this study, the “AnomalyDetection” package (https://github.com/twitter/AnomalyDetection, last access: 2 November 2021) (Aggarwal, 2013; Chandola et al., 2009; Rosner, 1983; Vallis et al., 2014) was used to extract GRACE high-frequency signal data. This package not only includes the GESD algorithm but can also specify the direction of detected outliers. The parameter “direction” indicates whether to extract peaks or valleys, where “pos” means the extraction of peaks, and “neg” means the extraction of valleys. As we considered extreme weather events caused by heavy precipitation in this study, important information was contained in the peak. The main parameter “direction” was set to the “pos”, and the maximum possible number of abnormal days “max_anoms” was set to 0.1 to cover the maximum number of abnormal days among the global time series comprising every grid. We provide an example in Fig. S1 in the Supplement to show the process of extracting possible flood days from high-frequency signals of GRACE TWS using the GESD test method as well as the reason for missing some flood events. We have also considered the reliability of the GESD test method in Fig. S2.

We used the probable flood days extracted by the flood potential index (FPI) to supplement the inability of GRACE to detect flood events with high-frequency signals. The FPI mainly considers rainfall-induced floods and has been widely used to evaluate flood events (Gupta and Dhanya, 2020; Molodtsova et al., 2016; Reager et al., 2014). Its basic assumption is that the regional water storage capacity can be approximated by the maximum value of historical TWS time series. The water storage capacity at the current time can be calculated by subtracting the TWS at the previous time from the maximum value of TWS time series. The proposal of this method was based on monthly data, but this does not affect its application to GRACE daily data. The application of the FPI was undertaken as follows.

The water storage capacity of the current day can be expressed as the temporal difference between the maximum time series value and the previous day's value; the formula is expressed as follows: 4TWSDEFt=TWSMAX-TWS(t-1), where TWSDEFt represents the maximum allowable relative water storage change on the current day, TWSMAX represents the maximum value over the entire time series and TWS(t-1) represents the TWS value of the current day relative to the previous day. A low storage deficit and high precipitation result in a high probability of flooding, i.e., the occurrence of floods should be based on the mismatch between the extreme precipitation level and the increase in water storage, as follows: 5Ft=Pdayt-TWSDEF(t), where Pdayt represents the daily precipitation, and Ft represents whether the current precipitation matches the water storage capacity. When Ft>0, flooding may occur. This study uses the FPI to supplement possible flood days in the case that the daily GRACE TWS data have lost useful high-frequency signals due to the interpolation process. In Fig. S3, we have provided an example in which the FPI was able to supplement some flood events not identified by GRACE high-frequency signals.

The flood extraction mainly went through a preselection stage and a final selection stage. We first used GRACE high-frequency signal data combined with the GESD method and FPI to preselect the possible flood days pixel by pixel. Next, we further used the number of extreme precipitation days to constrain and obtain the final flood days. This study focuses on flood events caused by heavy precipitation. Considering that floods are caused not only by single-day precipitation but also by cumulative precipitation, we calculated the extreme precipitation days based on the 1 d precipitation, 3 d cumulative precipitation and 5 d cumulative precipitation. Regarding extreme precipitation, the most commonly used metric is the percentiles of the precipitation time series data, including the nth quantiles of the entire time series data; alternatively, the nth quantile of wet days (daily precipitation > 1  mm) can be considered (Myhre et al., 2019; Pendergrass, 2018; Shi et al., 2021). In order to present the calculation process more clearly, we randomly selected a spatial grid for detailed processing. Figure S4 shows the intermediate process of flood day extraction. This process was carried out as follows:

The high-frequency signal of the TWS was extracted using the STL method.

To verify the reliability of the extracted results, this paper used the global discharge data products released by GRDC and the statistics-based automated flood event extraction (FloodR) method to extract possible flood events. FloodR is a statistics-based flood event separation method proposed by Fischer et al. (2021). It can automatically separate flood events using a univariate daily discharge time series, and it includes additional tool for manually checking and correcting the separation results quickly, allowing expert knowledge to be easily incorporated. Considering that the fluctuation in daily discharge data is smoother than that in hourly discharge data, FloodR used the moving-window variance to overcome the lower dynamic characteristics of daily discharge. Its basic rules include three points: (1) a flood event is an event that temporarily exceeds the normal discharge, and the start and end of each flood event can be defined; (2) a flood event can be characterized by significantly increased dynamics of discharge; (3) the sum of the increasing discharges is similar to the sum of the recession of the flood event (Fischer et al., 2021). FloodR can also automatically handle missing data and perform flood separation in segments according to the missing data before finally merging them. In this paper, the “eventsep” function in the FloodR package was used and the parameters were set to default (according to the practice of Fischer et al., 2021), while the “NA_mode” parameter was based on whether there were missing values in the discharge time series. The results extracted by FloodR include information like the start and end times of each flood, the flood peak date, and the flood baseflow, thereby providing an important data foundation for verifying the time series comparison ability of this study.

We use the goodness of flood separation (GFS) to evaluate the performance of the FloodR method. This indicator explicitly minimizes the number of small runoff events and maximizes the number of flood events with high discharge. This indicator can be used to address the lack of a consistent and true data foundation for the evaluation of the goodness of flood separation (Fischer et al., 2021). 6GFS=QQ>THupper;FloodQQ>THupper-maxQQ<THlower;FloodQQ<THlower-Tollower,0, where QQ>THupper;Flood is the number of flood days with discharge above the threshold of THupper, QQ>THupper is the number of days above the threshold of THupper, QQ<THlower;Flood is the number of flood days with discharge below the threshold of THlower and QQ<THlower is the number of days below the threshold of THlower. The upper threshold THupper, lower threshold THlower and tolerance threshold Tollower are set as the 95th quantile of discharge, the 50th quantile of discharge and 1 % of the discharge days below the lower threshold, respectively, according to the suggestion of Fischer et al. (2021).

In order to better compare the relationship between flood events (observed from DFO, MODIS and discharge) and flood days (derived from GRACE), we referred to the probability of detection (POD) index proposed by Yang et al. (2021) and made it more appropriate for our study. 7POD=floodGRACE-based/(floodobserved+floodmiss), where floodGRACE-based denotes flood events identified by GRACE, and floodobserved denotes DFO-recorded flood events, MODIS-derived flood events or discharge-derived flood events. If each flood event with a 3 or 5 d buffer could cover the GRACE-based flood days, we consider it a floodGRACE-based event.

This study considers GRACE-based flood days obtained under the constraint of the 95th percentile of the entire time series dataset. Figure 2 shows the global cumulative flood days and flood events from 1 April 2002 to 31 August 2016, and Fig. 3 shows the histograms of flood days and flood events corresponding to Fig. 2. Although the number of flood days extracted above cannot accurately reflect how many flood events occurred, we can simplify the results such that a number of consecutive detected flood days or the interval between 2 consecutive flood days, no more than 3 d or 5 d can be considered a flood event. The principle involves roughly calculating the spatial distribution of global flood event occurrences. Consistency was found between the global spatial distributions of flood events and flood days. We found that 99.8 % of the grids around the world experienced fewer than 400 flood days except in Southeast Asian countries and countries at the junction of North and South America, which experienced more than 400 flood days from 1 April 2002 to 31 August 2016. In addition, the areas with the most flood days and events were mainly located in the tropics. Island countries, western Africa, India, the Himalayas, southern China, etc. were also prone to floods. From the perspective of the divided flood events, the number of grid cells with fewer than 100 events accounted for 96.15 % (Fig. 2b), 97.11 % (Fig. 2c) and 97.52 % (Fig. 2d) of all grids.

We also calculated the average flood days in the same month in each year from 2002 to 2016 to identify seasonal characteristics. As shown in Fig. 4, the global flood distribution reflected obvious seasonal characteristics, and differences between the Northern and Southern hemispheres are clear. More flood days were identified in the Northern Hemisphere in summer (approximately June–September), while flood days in the Southern Hemisphere were concentrated from December to March.

We also analyzed the distribution of flood days in the mountain glacier regions. We used global glacier outline data from the Randolph Glacier Inventory (RGI). This dataset can be used to estimate glacier volumes, rates of elevation change at regional and global scales, and the response of the cryosphere to climate forcing. The dataset is updated annually in shapefile format. In this paper, we used it to locate global glaciers (RGI Consortium, 2017).

In the range of 60∘ S–60∘ N, there are 10 glacial regions and 163 flood events recorded based on the DFO database (Fig. 5). A total of 142 flood events were identified, and 21 flood events were not detected, resulting in a POD of 0.87. The capacity of flood detection is close to the global POD (0.81). The results showed that GRACE also has good potential with respect to identifying precipitation-induced floods in glacial regions. Of these 21 flood events, 4 flood events could not be identified due to missing months in GRACE data. Eight flood events had a maximum daily precipitation of less than 40 mm according to the DFO-recorded time period and spatial location (minimum of 8.44 mm and maximum of 36.56 mm), and GRACE could not identify the weaker signal. The remaining nine flood events could not be identified due to GRACE itself failing to identify flood conditions.

We further selected the GRACE grid covering the glacial regions and analyzed the characteristics of the extracted flood days. Figure 6 shows the 10 detailed glacial regions and the corresponding selected GRACE grids that covered the main glacial areas. Figure 7 shows the results of the extracted flood days related to the grid of each region. In general, the number of flood days in the glacial regions was relatively small, and flood days were mostly concentrated within 50 d from 1 April 2002 to 31 August 2016, whereas the glaciers in the South Island of New Zealand and the glacial regions in the east of southern Asia exceeded 100 d. The areas of the South Island of New Zealand where mountain glaciers are located experience a hyper-maritime climate, and the west coast of the South Island receives the most precipitation (annual precipitation > 12 m) (Anderson et al., 2010). Glacial regions in eastern South Asia are mainly located in the Himalayas, where normal climatic fluctuations become rather quick in the Himalayan sectors due to topography and the southwest Indian Ocean monsoon. Cloud bursts, high winds, snowstorms, etc. can also cause quick floods (Nandargi and Dhar, 2011).

Figure 8 shows the spatial distribution of 2380 precipitation-type floods recorded by the global DFO from 60∘ S to 60∘ N. Judging by the floods recorded by the DFO, floods have occurred in most parts of the world except in the Sahara Desert, the Great Victoria Desert and the northern part of North America.

In this study, the temporal length of the DFO database was compared with GRACE-based flood data throughout the 1 April 2002–31 August 2016 period. According to the database attributes, flood events caused by heavy precipitation were extracted as the validation dataset for this study. Given that the temporal and spatial DFO recording characteristics are approximate and considering the effect of advanced or delayed times on short-duration records, the start and end times of the DFO records were extended forward and backwards by 3 or 5 d, respectively, when being compared with the flood day results. Similarly, when the extent of the DFO polygon was less than 3∘, we appropriately built a buffer (3∘) to compensate for the positioning errors. We then detected every event in the DFO record to determine whether flood days could be identified based on its temporal and spatial coverage.

Figure 9 shows the distribution of the number of flood events recorded by DFO on 1∘ spatial grids (the same as the GRACE spatial resolution). It also shows that the eastern part of North America, the northern part of South America, the central and southern parts of Africa, western Europe, northern India and southern China are all areas with high-frequency flood events. Except for the archipelagic countries in Southeast Asia, the entire spatial distribution is consistent with our results.

We compared the 2380 precipitation-type flood events recorded by the DFO one by one with the real flood extent extracted by Tellman et al. (2021) based on remote sensing images. Figure 10 shows part of the flood event comparison results derived based on GRACE, MODIS and DFO data. The dark blue polygons show the approximate flood ranges delineated by the DFO, red pixels are the flood inundation areas extracted based on MODIS data, and light blue regions show the flood days (≥ 1 d) extracted using GRACE TWS and extreme precipitation data during the period recorded by the DFO. MODIS-based inundation extents were calculated according to the DFO time period as well as the union of DFO polygons and HydroSHEDS Basins Level 4 data (Tellman et al., 2021; Lehner et al., 2008; Lehner and Grill, 2013). We also used the DFO-recorded time series as a reference to filter flood days in each grid cell and obtained the spatial flood distributions in specific areas. The flood extents recorded by DFO are rough, and time durations are sometimes long (much more than 1 month); this causes large uncertainties in the spatial distribution and duration. Although the MODIS resolution (1 km) is higher than that of GRACE TWS (1∘, ∼ 100 km), only a limited amount of flooding can be identified by remote sensing images due to the influence of bad weather. The GRACE-based flood days that we provided were only able to indicate the presence of flood events under the ∼ 100 km grid coverage, and specific detailed flood extents require further identification using high-resolution satellite remote sensing images. Therefore, we note some differences among the spatial patterns of floods recorded by DFO, MODIS and GRACE. This study focuses on whether the flood events recorded by the DFO can be detected by GRACE; as long as the number of flood days (≥ 1 d) extracted by GRACE could be found at the time and in the space specified by DFO, the effectiveness of the method could be demonstrated. Considering the results of 2380 events, 463 flood events were not detected, resulting in a detection rate of 81 %. Among the undetected events, 85 events went undetected due to low precipitation (not the cases of extreme precipitation), and 69 events went undetected due to a lack of GRACE data in certain months, resulting in the inability to obtain effective high-frequency signals. Among the remaining 309 undetected floods, the omission of 184 floods may have occurred due to the fact that the maximum daily precipitation was less than 50 mm, causing GRACE to fail to identify a flood signal. The other 125 undetected flood events may have been caused by GRACE itself failing to identify flood conditions. To view the spatial distributions of precipitation-type floods and the corresponding situation obtained from flood inundation data extracted from GRACE and MODIS, the reader is referred to the following Zenodo repository: 10.5281/zenodo.6831105 (Zhang et al., 2022a).

We further selected some flood events using news reports and social media (like Twitter and Weibo) to verify if there were some flood events that could not be identified by the DFO but could be identified by GRACE-based flood days. Figure 11 presents nine flood events not recorded by the DFO, including floods that occurred in different time periods and areas, such as the eastern US, northern and southern South America, Mozambique in Africa, France, India, China, Malaysia, Indonesia and Australia. The red boxes indicate the approximate location of the reported flood events. The blue areas were the GRACE-based flood days corresponding to the duration and approximate location of flood events recorded by social media or news reports. We found that GRACE-based flood days could identify these missing flood events well, which also proved the effectiveness of using GRACE to identify large-scale flood events. Our data can be used as a good supplement to DFO data.

We also compared GRACE-based flood days with discharge data to assess our detection ability. We used the FloodR method of Fischer et al. (2021) to extract possible flood events from 3408 GRDC discharge data to serve as a basic reference standard when verifying the accuracy of the results extracted in this study. We focused on extreme precipitation-induced flood events and similarly constrained the results derived from the discharge data with extreme precipitation data. To ensure accuracy, we first selected the floods extracted from discharge stations with a GFS greater than 0.5 for comparison. Due to the fact that discharge reflects the amount of water integrated over its entire contributing basin and contributing time (Yang et al., 2019), we combined the flood events obtained from each discharge station in time series to describe the flood events in the 261 watersheds (HydroSHEDS Basins Level 4; Lehner and Grill, 2013; Lehner et al., 2008). Flood events in the same watershed were merged according to whether there was an intersection in the time series. The accuracy index used for comparison in this study was the probability of detection (POD) (Yang et al., 2021), i.e., whether each flood event in the river basin contained the GRACE-based flood days. Although flood events derived from discharge cannot guarantee that the surrounding land will experience flooding, they provide us with a reference to support the reliability of the time series verification process.

Figure 12 shows the global distribution of discharge locations and the GFS. The data distributions in North America, South America, Europe and southeastern Australia were relatively dense, whereas data were seriously missing in central, northern and eastern Asia. The areas with a higher GFS were located in the eastern US and central Europe, and the stations recorded in these areas were relatively complete. The discharge stations with a GFS above 0.5 accounted for 73.49 % of stations. Figure 13 shows the flood events in the Level 4 river basins. We find that most flood events reflected by the discharge data were located in the eastern and western US, central South America, eastern Europe and New Zealand.

The POD calculation results are shown in Fig. 14: the darker the color, the higher the corresponding flood detection accuracy. We found that the overall accuracy performed well; the detection accuracies obtained for the central and eastern parts of the US, western South America, southern Africa and around Australia were relatively high. Figure 15 shows the histogram of 261 watersheds of Level 4 basins; the percentage of river basins with POD values greater than or equal to 0.5 is 62 %. This finding shows that our extracted flood days also reflected relatively high accuracies in comparison with flood events at river basins.

In the Table 1, we list the flood detection performance compared with DFO, MODIS and discharge, respectively. GRACE was able to detect 81 % of flood events recorded by DFO and 87 % of flood events recorded by MODIS. If we summed all flood events from the 261 river basins, GRACE-based flood days could identify 53 % flood events derived from discharges. The percentage of river basins with POD values greater than or equal to 0.5 was 62 %.

The uncertainty analysis performed in this study mainly focused on the selection of the extreme precipitation threshold. The most common method for determining the extreme precipitation threshold is to use the quantile of the analyzed time series, considering either the quantile of the entire time series (QETS) data or the quantile of wet days with daily precipitation greater than 1 mm (QWDTS). This study compared the different PODs which were obtained by setting different quantile threshold scenarios when comparing with the DFO database. We selected the 90th, 95th and 99th quantiles for the two methods described above. Figure 16 shows that the selection of different thresholds in the two extreme-precipitation scenarios influenced the flood extraction accuracy of the POD, with contributions ranging from 72.4 % to 81.4 %. This shows that the selected thresholds can affect the detection rate of approximately 9 % (roughly 214) of the flood events. We also provide the six products derived based on these two constraints for further analysis and use by researchers.