Generating reliable estimates of tropical-cyclone-induced coastal hazards along the Bay of Bengal for current and future climates using synthetic tracks
- 1Deltares, Delft, 2600MH, the Netherlands
- 2Deltares USA, 8601 Georgia Ave., Silver Spring, MD 20910, USA
- 3Asian Development Bank, 6 ADB Avenue, Mandaluyong City 1550, Metro Manila, the Philippines
Correspondence: Tim Willem Bart Leijnse (email@example.com)
Deriving reliable estimates of design water levels and wave conditions resulting from tropical cyclones is a challenging problem of high relevance for, among other things, coastal and offshore engineering projects and risk assessment studies. Tropical cyclone geometry and wind speeds have been recorded for the past few decades only, thus resulting in poorly reliable estimates of the extremes, especially in regions characterized by a low number of past tropical cyclone events. In this paper, this challenge is overcome by using synthetic tropical cyclone tracks and wind fields generated by the open-source tool TCWiSE (Tropical Cyclone Wind Statistical Estimation Tool) to create thousands of realizations representative of 1000 years of tropical cyclone activity for the Bay of Bengal. Each of these realizations is used to force coupled storm surge and wave simulations by means of the processed-based Delft3D Flexible Mesh Suite. It is shown that the use of synthetic tracks provides reliable estimates of the statistics of the first-order hazard (i.e., wind speed) compared to the statistics derived for historical tropical cyclones. Based on estimated wind fields, second-order hazards (i.e., storm surge and waves) are computed that are generated by the first-order hazard of wind. The estimates of the extreme values derived for wind speed, wave height and storm surge are shown to converge within the 1000 years of simulated cyclone tracks. Comparing second-order hazard estimates based on historical and synthetic tracks shows that, for this case study, the use of historical tracks (a deterministic approach) leads to an underestimation of the mean computed storm surge of up to −30 %. Differences between the use of synthetic versus historical tracks are characterized by a large spatial variability along the Bay of Bengal, where regions with a lower probability of occurrence of tropical cyclones show the largest difference in predicted storm surge and wave heights. In addition, the use of historical tracks leads to much larger uncertainty bands in the estimation of both storm surges and wave heights, with confidence intervals being +80 % larger compared to those estimated by using synthetic tracks (probabilistic approach). Based on the same tropical cyclone realizations, the effect that changes in tropical cyclone frequency and intensity, possibly resulting from climate change, may have on modeled storm surge and wave heights was computed. As a proof of concept, an increase in tropical cyclone frequency of +25.6 % and wind intensity of +1.6 %, based on literature values and without accounting for uncertainties in future climate projection, was estimated to possibly result in an increase in storm surge and wave heights of +11 % and +9 %, respectively. This suggests that climate change could increase tropical-cyclone-induced coastal hazards more than just the actual increase in maximum wind speeds.
Tropical cyclones (TCs) are among the most destructive natural hazards worldwide. Over the last 2 centuries, it is estimated that 1.9 million people have lost their lives as a result of TCs worldwide (Shultz et al., 2005; Nicholls et al., 1995). While only about 7 % of the global TCs form in the Indian Ocean, associated damage and casualties surrounding this ocean basin are much larger than in any other region. Between 1960–2004 it is estimated that more than half a million inhabitants of Bangladesh died because of TCs (Shultz et al., 2005). The recent Cyclone Amphan (2020) showed that strong TCs still occur in the Bay of Bengal (BoB), where the direct impact has however been mitigated through early warning systems, cyclone shelters and embankments.
A challenge in several coastal engineering applications consists in the determination of reliable estimates of design water levels and wave conditions resulting from these TCs, for both present and future climate scenarios. The estimation of design values resulting from TCs is often based on a limited number of recorded historical tropical cyclones (HTCs) in a given region (for the BoB see, e.g., Chiu and Small, 2016; Dube et al., 2009). This results in a large statistical uncertainty in estimating the first-order hazards resulting from TCs (e.g., wind speeds) due to the limited number of observations at a certain location. One approach to overcome this is by using synthetic tropical cyclones (STCs) based on the statistics of the properties of observed HTCs. The Tropical Cyclone Wind Statistical Estimation Tool (TCWiSE; Nederhoff et al., 2021) can, for example, be used to generate numerous synthetic tracks. These synthetic tracks allow for the creation of a much longer-term dataset than what is otherwise available through HTC tracks only and can be used to calculate more reliable estimates of first-order hazards. Subsequently, these STCs can then be modeled using hydrodynamic and wave models to generate better estimates of second-order hazards like storm surge and wave heights that are generated by the first-order hazard of wind. Other datasets and methods to generate STCs are those of Vickery et al. (2000), Hardy et al. (2003), James and Mason (2005), Emanuel et al. (2006, 2008), Haigh et al. (2014), Nakajo et al. (2014), Lee et al. (2018), and Bloemendaal et al. (2020). Hereby, the literature so far has mainly focused on deriving STC tracks and corresponding wind and pressure fields. Some work has been done exploring the effect of using these to derive offshore extremes for storm surge and wave heights compared to considering HTCs only (e.g., Meza-Padilla et al., 2015; Appendini et al., 2017) but with focus on different regions than the BoB (e.g., Australia – Haigh et al., 2014; Mexico – Meza-Padilla et al., 2015; northern Pacific Ocean – Mori and Takemi, 2016; Mori et al., 2016; Yang et al., 2020; or the USA – Lin et al., 2012; Appendini et al., 2017; Marsooli et al., 2019) or without taking waves into account, which is found to be an important factor leading to flooding in the northern BoB (Krien et al., 2017) and arguably worldwide.
The effects that climate change and global warming have on TCs are subject to scientific debate. As discussed in Knutson et al. (2010), this is related to the large temporal fluctuations in TC frequency and intensity, making it difficult to derive reliable trends. Recent work has shown that, globally, a statistically significant trend towards an increase in TC intensity can be found (Kossin et al., 2020). According to Knutson et al. (2010), future projections indicate an increase towards stronger storms of 2 %–11 % by 2100 and a decrease in the globally averaged frequency of TCs by 6 %–34 %, with a large variation between models and different basins. These general findings were confirmed in the modeling study by Knutson et al. (2015). The authors assessed, by means of CMIP5 model ensembles, the possible changes in TC frequency and intensity under Representative Concentration Pathway (RCP) 4.5 for the late twenty-first century compared to the period 1982–2005. Large differences between basins were depicted in the modeling study. For the north Indian Ocean (NIO) basin, an increase in TC frequency was estimated to be equal to 25.6 % for TCs of categories 1–5. The increase was even larger for TCs of categories 4–5 (200 %, although the change is marked as not being statistically significant). An increase in intensification of TCs in the NIO during the last few decades has already been reported by several authors (Webster, 2005; Singh et al., 2001; Singh, 2007; Deo et al., 2011; Kishtawal et al., 2012). According to Knutson et al. (2015), this increase in intensity was estimated to be 1.6 % for TCs of categories 1–5. Nevertheless, the values described by different authors suggest a large scatter, making it difficult to derive statistically robust trends and conclusions. In combination with sea level rise, an increase in TC intensity will lead to significant and amplified increases in flood risk (Karim and Mimura, 2008).
In this study, TCWiSE was applied in combination with the hydrodynamic Delft3D Flexible Mesh Suite (Delft3D FM; Kernkamp et al., 2011) and the coupled wave model SWAN (Booij et al., 1999) to estimate storm surge and wave conditions along the BoB. TCWiSE was extended to be able to derive estimates for present and future scenarios, therefore accounting for the possible influence of climate change. In particular, downscaled projections of TC frequency and intensity based on Knutson et al. (2015) were used as input to the modeling study. Estimates of extreme storm surge and wave conditions were derived along the BoB (4000+ km in total) at an alongshore resolution of 5–25 km following the coastal segments of the DIVA database (Vafeidis et al., 2008). Derived estimates can be used as boundary conditions for the estimation of present and future hazards and risks resulting from TC events for the entire region and the conceptual design of suitable mitigation options, in combination with higher-resolution local models. The methodology and tool are generic and can in principle be applied to any location worldwide that is exposed to TCs.
2.1 Study area
The BoB is the northeastern part of the NIO, bounded to the southwest by Sri Lanka, to the west and northwest by India, to the north by Bangladesh, and to the east by Myanmar. Within the bay lie the Andaman and Nicobar Islands (see “ANI” in Fig. 1). The different countries and regions considered in the study are described in Table 1. Per region, one representative location is included for further analysis and shown in Fig. 1 (“Coastal cities”). The entire Bay of Bengal, in particular the northern part, is highly affected by TCs. Extreme sea levels around the bay, including maximum tidal levels and storm surge, increase towards Bangladesh as a result of the bay geometry and the shallow continental shelf (Fig. 1 and Muis et al., 2016).
Different datasets were used in order to set up the numerical modeling system, namely bathymetry, coastal segments and HTC tracks with associated maximum wind speeds.s
Deep-water bathymetry data for the BoB were derived from the GEBCO 2008 global bathymetric dataset (Becker et al., 2009); see Fig. 1. These bathymetric data were used as input for both the hydrodynamic and the wave models.
Output locations were chosen based on DIVA coastal segmentation as in Vafeidis et al. (2008), allowing a global spatial determination of similar stretches (segments) of coastline (linear coastal segments). A total of 197 output locations (1 per segment) along the entire coastline were defined, at which time series of extreme storm surge and significant wave heights were extracted as in Muis et al. (2016). Each segment has a length of approximately 5–25 km. For the wave conditions, the locations in the DIVA segments were translated into locations in deeper water to provide deep-water wave conditions and were therefore not affected by the local bathymetry. For each location, the closest point with a water depth larger than 30 m was chosen (Fig. 1).
HTC data were derived from the IBTrACS (International Best Track Archive for Climate Stewardship) database version v04r00 (Knapp et al., 2018). The IBTrACS database contains the most complete global set of HTCs available. From the IBTrACS dataset, the best-track data of the Joint Typhoon Warning Center (JTWC) for the NIO were chosen as a source, including reliable satellite-derived data (Singh, 2010) available for the period 1972–2020. The data contain TC information including the best-track coordinates and maximum wind speeds. The 1 min averaged wind speeds were converted into 10 min wind speeds using, as a correction factor, the value 0.93, following Harper et al. (2010). In total, 110 historical tracks were available for the NIO, of which 81 originated in the BoB including the recent Cyclone Amphan (2020). In the dataset, two distinct periods with TC activity can be identified, corresponding to the pre-monsoon period (May) and the post-monsoon period (November, e.g., Alam et al., 2003; Islam and Peterson, 2009). Generally, about 2–4 TCs per year are generated in the NIO, though this is not spread evenly through time as the TC generation is influenced by a number of external factors such as the El Niño–Southern Oscillation (ENSO) cycle (e.g., Singh et al., 2000; Hoarau et al., 2012). The HTC tracks were used to derive the STC tracks in TCWiSE. Figure 2a illustrates the selected HTC tracks, with different colors indicating different wind speed categories, while Fig. 2b shows the generated STC tracks based on the HTCs. Note that wind speeds on land may be less reliable as they are affected by several factors (e.g., land friction, local topography). Nevertheless, these uncertainties are not relevant for this study, which instead focuses on storm surge and waves in the ocean and coastal zone.
The methodology which was followed for generating extreme values for surge and waves for both historical and synthetic tracks is described in Fig. 3. From the IBTrACS dataset, a regional subset of HTCs are extracted for the NIO. In particular, TC characteristics (i.e., location, wind speed) describing the HTCs are extracted and used for generating the STCs with TCWiSE. The HTCs and STCs are then converted into wind and pressure fields using WES (Wind Enhancement Scheme; Deltares, 2019), which is a routine incorporated within TCWiSE. The generated wind and pressure fields are then used to force the numerical hydrodynamic and wave models Delft3D FM and SWAN. From these models, time series of storm surge and wave heights are extracted at the DIVA segments, and, per location, an extreme value analysis (EVA) is performed using the peaks-over-threshold (POT) method. The results are extreme values of storm surge and wave heights for different return periods at each location, which are used to perform regional comparisons between the obtained HTC and STC datasets.
2.3.1 Generation of synthetic cyclone tracks
The generation of STC tracks was carried out using TCWiSE (Nederhoff et al., 2021). The tool allows the generation of synthetic tracks based on a Markov model where observed data serve as a data source to compute synthetic tracks. The main variables it keeps track of are location (latitude and longitude); time; and the statistics of maximum sustained wind speeds (vmax), forward speed (c) and heading (θ) as spatially varying PDFs (probability density functions). TC genesis is computed through randomly sampling the locations for each track from a spatially varying PDF. TC termination is estimated based on PDFs describing the probability that a TC will terminate at a certain location and with a given wind speed. These spatially varying PDFs are all constructed based on historical input data and created on a 0.1∘ grid for the entire NIO. Furthermore, the number of TCs per year and the probable period within the year of TC generation are used to provide each track with a unique time within the synthetic year.
At first, the 81 HTC tracks which have occurred in the BoB over a period of 48 years, with location and vmax, were extracted from the IBTrACS dataset (Fig. 4). After calculating the PDFs of the different variables based on the HTCs, TCWiSE was run to estimate 1000 years of synthetic tracks for both current climates (synthetic tropical cyclone current climate, STCC) and future climates (synthetic tropical cyclone future climate, STCF). The estimation of the effects of future climate on TCs was based on Knutson et al. (2015). The authors estimated that the frequency of TCs per year may increase to 25.6 % by the end of the century, for all TC categories (categories 1–5), defined as TCs with wind speeds larger than 33 m s−1, and according to an RCP 4.5 scenario. In order to avoid creating sampling differences when creating the synthetic tracks for current and future scenarios separately, the total tracks for the STCF were generated first, resulting in 2191 tracks. Then, the first 1745 tracks were selected as representative of 1000 years of TCs in the current climate (Fig. 4). The ratio between these two values () represents the 25.6 % TC frequency increase between the future and current scenario. Similarly, according to Knutson et al. (2015), the intensity (i.e., maximum wind speed) may increase by 1.6 % for the future climate. Only after generating all synthetic tracks were the wind speeds for all time steps of the STCF tracks increased by 1.6 % to represent the intensity increase for the future climate.
2.3.2 Generation of pressure and wind fields
For each HTC and STC track, time-varying and spatially varying wind and pressure fields were generated based on the parametric wind model of Holland et al. (2010) using WES. The wind–pressure relations of Holland (2008) were used to compute the maximum pressure drop and create corresponding spatially varying pressure fields. The calibrated coefficients for the NIO basin based on Nederhoff et al. (2019) were used to compute TC geometry (most probable radius of maximum winds (RMW) and radius of gale force winds (R35)). TC asymmetry between the different quadrants was defined using Schwerdt et al. (1979). Furthermore, a constant inflow angle of 22∘ based on Zhang and Uhlhorn (2012) was assumed and a wind decay after landfall was included based on Kaplan and DeMaria (1995).
2.3.3 Hydrodynamic and wave numerical models
The effects of each individual TC on storm surge and wave conditions were modeled using a coupled hydrodynamic (Delft3D FM) and wave model (SWAN), where water levels are exchanged every hour and the wave radiation stresses are communicated from SWAN to Delft3D FM as well. The resolution of the models was chosen in such a way as to keep the running time sufficiently low to be able to run the entire set of thousands of tracks and still allow sufficient accuracy to simulate realistic results. For the hydrodynamic model, the finest grid size was equal to about 3 km nearshore, extracted from the GTSM (Global Tide and Surge Model; Muis et al., 2016) grid, and forced with wind and pressure fields only from the TCs. Therefore, storm surge estimates are computed based on both wind speed and atmospheric pressure. Tidal forcing was excluded from the model to be able to intercompare the impact of different TCs directly and focus on the wind-driven and atmospheric-pressure-driven surge components only, without the timing of the actual high or low water of the tide playing a role. In reality, non-linearities between tide and surge can, depending on the tidal range, have a large effect on the estimated total water level values (Chiu and Small, 2016).
For the wave model, a constant resolution of 0.02∘ (∼ 2 km) was used to allow the simulation of the large number of tracks. This resolution is not sufficient to accurately model nearshore processes like wave shoaling and breaking. Therefore, only results in water depths deeper than 30 m were used. The wave model was run in non-stationary mode, with a time step of 10 min, and forced by wind fields from the TCs only. No background winds or wave heights were included since these are not available for the synthetic tracks and they would alter the comparison with the historical tracks. For more details regarding the setup of the numerical models, see Appendix A. Per DIVA section, the generated time series of storm surge and significant wave heights per track were combined to generate 1000-year-long time series of STCs. Additionally, a 48-year-long time series of storm surge and wave heights was also created forcing the models with the HTC winds and pressures.
2.3.4 Extreme value analysis
An EVA was carried out on the extreme storm surge and wave heights using a POT method and an exponential fit (Caires, 2016). Extreme values were derived along the entire coastline at each DIVA segment and based on the created time series, for return periods corresponding to 10, 25, 50 and 100 years. The POT thresholds were automatically selected between the 99th percentile, as the minimum threshold, and the 99.9th percentile as the maximum threshold, using the threshold stability criteria (Caires, 2016). For the HTCs, the 98th percentile was used as a minimum percentile to create stable EVA fits as the time series contained a lower number of peaks. Additionally, 95 % confidence intervals (CIs) were computed and based on the CI of a generalized Pareto distribution (GPD), by applying the relative values of the lower and upper estimates relative to the point estimates. The point estimates are determined with a plotting position , where n is the sample size, i the order and lu the Poisson rate. Hereafter, for the comparison between the HTC, STCC and STCF results, the absolute values per DIVA section were averaged into larger regions, as indicated in Table 1.
3.1 Verification of synthetic cyclone tracks
Time series of 1000 years of synthetic tracks for the BoB for current climate (STCC) and future climate (STCF) were generated using TCWiSE. Since the synthetic tracks were based on historical data, statistical properties for the STCC should be similar to those of the HTCs. Nederhoff et al. (2021) demonstrated this through an application of TCWiSE for the Gulf of Mexico, by comparing statistical properties for 10 000 years of synthetic tracks and those of 133 years of historical data.
Here, a similar analysis is presented for the BoB. Spatial patterns for genesis, occurrence and termination were compared qualitatively and quantitatively using the correlation parameter R based on the similarity score of Kirchhofer (1974) in Fig. B1 in the Appendix. The closer R is to 1, the more similar the spatial patterns of the HTCs and subsequently generated STCC are. The regions with the highest probability of TC genesis in the historical data were found around the Andaman and Nicobar Islands in the middle of the BoB (Fig. B1a and b). The spatial genesis patterns of the STCC appear very similar to those of the HTCs, which is confirmed by the correlation parameter R being 0.88 (–). For the probability of termination of TCs, the patterns appear similar as well (Fig. B1c and d), but the magnitudes are more spread out for the STCC, leading to a slightly lower R value of 0.82. The main regions of TCs making landfall are around eastern India, Bangladesh and northern Myanmar. The highest TC occurrence is found in the middle of the BoB (Fig. B1e and f). The yearly occurrences are quite well reproduced with an R value of 0.68. The lower correlation is due to the spatial patterns of the synthetic tracks being more smoothed out compared to that of the HTCs due to the much larger number of realizations. The maximum yearly probability of the HTCs is about 0.4 (i.e., return period of 2.5 years), indicating that a particular region in the NIO is likely to be affected by a TC on average once every 2.5 years. The spatial coverage of the probability of genesis, probability of termination and yearly probability estimation over the whole BoB, as well as the similarities in spatial patterns between the HTCs and the STCC, indicate that the STCC can be used as a basis for quantifying wave heights and storm surges along the entire coast.
A comparison between the cumulative distribution functions (CDFs) of maximum wind speeds (vmax) for HTCs and STCC, at nine locations along the BoB, is shown in Fig. 5. The functions are estimated based on TCs within a 200 km radius of each of the nine locations. Per location, the number of samples of time steps of TCs within a 200 km radius is included; this is between a factor 6 and 34 larger for the STCC compared to HTCs and includes 1000 samples or more except in the case of Mawlamyine (Myanmar). The CDFs of the other parameters (i.e., forward speed and heading) are presented in Figs. B2 and B3, respectively, of Appendix B. Additionally, a number of statistical parameters describing the differences between the two distributions are computed (i.e., absolute difference in maxima (Δmax), normalized mean absolute error (nMAE), the relative bias of the median value (bias) and the root-mean-square error (RMSE) of the whole CDF). Locations characterized by a higher HTC occurrence, such as the ones in India and Bangladesh, generally have a lower absolute bias. For locations with a lower HTC occurrence, for example Batticaloa (Sri Lanka) and Mawlamyine (Myanmar), the bias is larger and the CDFs of the HTCs indicate a less smooth distribution as a result of the lower number of tracks included. The nMAE varies between 0.01 and 0.06, according to the location, and the RMSE between 1 and 10 m s−1, with the largest discrepancies seen at Batticaloa. At Batticaloa, there are a limited number of samples for the HTCs with a clear distinction of tracks with a wind speed of either below 15 or above 25 m s−1 (Fig. 5), while for the STCC a more gradual distribution can be seen, including also realizations in between these values. Maximum wind speeds are generally higher for the STCC than for the HTCs, meaning that more extremes are captured in the STCC, with the largest differences observed at Port Blair reaching up to 25 m s−1. Smoother distributions of the parameters describing the TCs are one of the advantages of using synthetic tracks computed over a long period of 1000 years. Similar patterns are also visible for the forward speed, heading and central pressure (Figs. B2–B4). In these cases, the RMSE for the forward speed ranges between 0.4 and 1.4 m s−1 (nMAE 0.1–0.5), the RMSE for the heading ranges between 11.3 and 50.5∘ (nMAE 0–0.04) and the RMSE for the central pressure ranges between 2.3 and 16.4 hPa (nMAE 0–0.08). Here, the central pressure values were not sampled in TCWiSE directly but are derived after applying the Holland (2008) estimates of pressure based on maximum wind speed.
Based on these results it can be concluded that the first-order hazard of wind speed is well resembled by the synthetic tracks created by TCWiSE for the current climate compared to historical observations. Therefore, the computed synthetic tracks and wind speed will be used for further analysis in the paper to estimate the resulting second-order hazards (i.e., storm surge and wave height).
3.2 Convergence of synthetic results
After validation of the synthetic cyclone tracks, spatially varying wind fields were created and used as input to force coupled Delft3D FM and SWAN models to estimate storm surge and wave heights along the BoB. It is first verified how dependent the estimated variables of wind speed, wave heights and storm surge are on the number of years of synthetic data included and if or how fast the results converge. In Fig. 6 an example for Charchenga (Bangladesh) is shown. To verify the convergence, 99 000 EVAs were performed on the time series of wind speeds, wave heights and storm surge to estimate the 100-year return period value while increasing the X number of years extracted from the available 1000-year time series (i.e., X = 10, 20, 30, …, 1000 years). Hereby for every X number of years extracted, these years are selected randomly and combined into one new time series after which an EVA is computed. This is repeated 1000 times per X number of years included to obtain a stable estimate. Estimates of the 2.5th, 50th and 97.5th percentiles for a 100-year return period value were computed at each iteration. Therefore, per X years of data included, the 95 % CI spread of the estimated median value was calculated over the 1000 realizations, which is shown in Fig. 6a, c and e as green fill. The estimated median value of this spread is included as orange line. The same was calculated for the 2.5th- and 97.5th-percentile values, with their respective median values of the spread shown as gray and black lines, respectively, and with their combined total spread as gray fill. Figure 6a, c and e show that the more years of synthetic data that are included, the smaller the CIs become and the more the median values converge to a stable value. The number of years of data to be included to reach this stable value depends on the variable that is analyzed.
To quantify how quickly each of the different variables converges, the relative (%) ratio between the median value of the 50th percentile (i.e., computed based on X years of data) and the same median value based on 1000 years of data (i.e., here assumed to be the “true value”) is presented as orange lines in Fig. 6b, d and f. These results show that, for all variables, the convergence is exponential. While the variables wind speed and wave height already have a relative difference of less than 5 % (dashed orange line) compared to the true value after about 380 and 350 years, respectively, for the storm surge this takes about 450 years. In the same figure, the range describing the difference in spreading of the median value (i.e., the size of the green fill in Fig. 6a, c and e) is also shown as a green line. This range indicates how “wrong” the estimated median values can be after including a certain number of years of data. After including 200 years of data, the 95 % spread of the median values is still 15 m s−1 for the wind speed, 5 m for the wave height and 0.8 m for the storm surge. This decreases more rapidly for the wave heights and more slowly for the wind speed and storm surge. The difference in convergence can be explained by the related probability distribution for each of the variables, also known as “tail dependence” in probability theory. For wind speed and storm surges, the range of possible values is generally larger (type-I tail denotes no upper limit), while this is more limited for wave heights (type-III tail is with an upper limit). This can be explained physically by the influence area of the variables wind speed and resulting storm surge that is limited to close to the landfall location of a TC. Swell waves generated by a TC can travel hundreds of kilometers and have a larger area of influence, so higher wave heights are more often reached, and the range of possible values is more limited. Since all three variables reach a relative difference of a maximum of 5 % within 450 years and a maximum difference of 2 % (dotted orange line) within using 830 years of data, we can assume that results have converged after including the full 1000 years of data, and these are further used in this analysis for comparison with the HTC data.
3.3 Evaluation of predicted storm surge and wave heights for historical versus synthetic tracks
3.3.1 Local differences based on one location
To compare the results of predicted storm surge and wave heights based on historical and synthetic tracks for the current climate, first an EVA is performed and discussed for one example location at Charchenga. Afterwards, results for all points combined are presented as general differences based on all modeled locations (Sect. 3.3.2), as well as differences between regions within the BoB (Sect. 3.3.3). In all figures, results for HTCs, STCC and STCF are shown in black, blue and red, respectively.
Focusing on the differences at one location first, Fig. 7 shows a comparison of the EVA specifically for storm surge at Charchenga. The EVA for the HTCs is based on 14 data points only, with just 4 points above a return period of 10 years. Given the length of the record equals 48 years, the maximum value of the dataset has an estimated return period of approximately 48 years. Thus, in order to obtain values for longer return periods (e.g., 100-year return period), one needs to extrapolate from the fitted GPD. For the STCC, there are 100 data points that have a return period of at least 10 years and the maximum return period in the dataset is approximately 1000 years. This leads to a much smaller 95 % CI for the STCC. In particular, the STCC has a 95 % CI of 0.95 m for a return period of 100 years versus 2.34 m for the HTCs.
For return periods lower than 5 years, the point estimates of the HTC and STCC converge. This gives further confidence in the local validity of the STCC estimates, in addition to the verification as described in Sect. 3.1 and 3.2. The estimated storm surge for the 100-year return period is underestimated when using the HTCs with respect to the use of the STCC. This underestimation is a result of a limited number of data points on which to fit the GPD (i.e., undersampling). This may lead to a different fit, as shown in Fig. 7, where the lines of the HTCs and STCC are approximately parallel but that of the STCC is shifted upwards (Fig. 7). The result is, for example, that the highest value modeled of the HTCs, with a storm surge close to 2 m, has a return period estimate close to the length of the dataset of 48 years. However, based on the STCC results, this event has a return period of only 30 years.
In the STCC the maximum modeled surge is 1.5 m higher than observed with historical events. Given that the CDFs of the maximum wind speed for HTCs and STCC are very similar and the maximum wind speed is only 4 m s−1 larger (Fig. 5), this means that more disadvantageous (but statistically plausible) trajectories in terms of landfall location, heading and forward speed are included in the synthetic dataset compared to historic events, meaning in turn that the worst event for this location may not have happened yet in recorded history. The same figure but for wave heights is shown in the appendix (Fig. B5).
3.3.2 General differences based on all locations
Besides analyzing the difference in modeled values and CIs of the EVA at a specific location (Fig. 7), such analysis was also performed for all 197 DIVA segments together, over the entire BoB. Figure 8 shows the results presented as scatterplots for different return periods for both storm surge (Fig. 8a) and wave height (Fig. 8b), where computed values based on HTCs are shown on the x axis and computed values based on STCC are shown on the y axis. The figure shows that, with an increasing return period, the root-mean-square difference (RMSD) also increases. Computed storm surges are in general slightly larger when using the STCC (increase of ∼ 5 %–10 % depending on the return period), while computed wave heights are in general larger when using the HTCs (increase of up to ∼ 5 % for larger return periods, though with more scatter). These increases for the HTCs and STCC are calculated as relative bias with respect to HTCs, though since the values based on HTCs are not the true values (i.e., the length of the historical record is too short to reliably describe the current climate), this is referred to as a trend. In Fig. 9, the same information is shown but for the 95 % CI, computed as the difference between the 97.5th- and the 2.5th-percentile estimates. The 95 % CIs are significantly smaller for the STCC compared to the HTCs with a trend between 60 % and 80 %.
3.3.3 Regional differences within the Bay of Bengal
The differences between storm surge and wave heights computed based on HTCs and STCC also vary spatially within the BoB. At locations where TCs occur more frequently, for example Chittagong in Bangladesh (Sect. 3.3.1), the STCC results generally fall within the CI of the HTCs, though using the HTC results, underestimations are still present (Fig. 10). At locations with a lower TC occurrence, for instance Batticaloa (Sri Lanka), the use of HTCs to estimate storm surge leads to much larger confidence intervals and lower values of the storm surge than those predicted based on STCC, which could be an underestimation of the potential hazard using the HTCs. Since the number of TCs making impact at these locations is very limited, TCs that could possibly hit these stretches of coast may not have occurred yet in the historical events. Therefore, using a large synthetic dataset largely reduces the confidence intervals and improves the estimation of the coastal hazards of extreme events since a larger range of possible events is covered. For wave heights, the differences between using HTCs and STCC are smaller (Fig. 11). This is because waves are in general a less local effect than storm surge with extreme waves at one location possibly being the result of a TC passing at a certain distance from a specific location, leading to more events for the HTCs. The estimated values for waves based on STCC also fall within the CI of the HTC estimates, while for storm surge this is not always the case.
To visualize these regional differences, the estimated regionally averaged values for storm surge and wave heights along the BoB based on the STCC are presented in Figs. 12a and 13a, respectively, as well as summarized in Table 2. The regions with higher values for storm surge and wave heights are also the regions with a higher TC occurrence. Furthermore, the presence of a wide shallow continental shelf such as in front of Bangladesh contributes to further amplifying the storm surge as a result of a larger wind-driven setup. Therefore, the highest storm surge can be found there. Over the entire BoB, the average storm surge due to TCs is estimated to be 1.2 m for a 100-year return period event. For waves (Fig. 13a) there is less regional variability because wave impact due to TCs is a less local event than storm surge, though still some differences are visible. The largest wave heights are again found in front of the coast of Bangladesh. The averaged deep-water significant wave height over the entire BoB is 9.5 m for a 100-year return period.
The relative differences in estimated storm surge and wave heights computed as HTCs compared to STCC are shown in Figs. 12b and 13b, respectively. The largest differences are observed for the storm surge, in particular in the southern part of the BoB, with differences of more than 50 %. The storm surge is relatively small here and can be both relatively large/small for storm surge derived based on STCC compared to those derived based on HTCs (see also Table 2). In the northern part of the BoB (i.e., Bangladesh) differences are relatively small (less than 20 %); however the difference in magnitude is much larger (see also Table 2). Storm surge estimated based on STCC is here consistently larger than that derived based on HTCs for all return periods.
For the wave heights the differences are in general smaller. In the south of the BoB (Sri Lanka, Andaman and Nicobar Islands), the use of HTCs leads to an underestimation of the predicted wave height with respect to the use of STCC for larger return periods, while along the main continent a contrasting behavior can be seen, although with relatively minor differences (see also Table 2).
Comparing the sizes of the CI per region as a percentage of the computed absolute value based on STCC (of Figs. 12a and 13a), the size of the CI for storm surge is much smaller based on the STCC (Fig. 12c) as opposed to based on the HTCs (Fig. 12d). The maximum size for the STCC is 35 % compared to the computed 100-year return period value, while for the HTCs the CI can be just as large as the computed value or higher (>100 %). The same holds for the wave height (Fig. 13c), which with 25 % for the STCC is much smaller than the 80 % based on HTCs (Fig. 13d).
3.4 Effects of a changed future climate on storm surge and wave heights
The effect that a future climate with changes in cyclone wind speed (intensity) and frequency, possibly resulting from climate change, could have on resulting storm surge and wave heights was investigated using synthetic tracks (STCF, Sect. 2.3.1). Using the projected TC frequency and intensity changes in Knutson et al. (2015) for the NIO under RCP 4.5 for 2100, it was quantified how changes in the first-order hazard (wind speed) could result in changes in the second-order hazards (storm surge and waves). In particular, it was estimated that, as a result of a TC frequency increase of 25.6 % and an increase in maximum wind speed of 1.6 %, there could be a relative increase in predicted storm surge of 11 % and 6 % for return periods of 10 and 100 years, respectively, and an increase of 9 % and 6 % for the wave height (see Figs. 10 and 11 and Table 2). Therefore, the increase in storm surge and wave height could be larger than the increase in TC intensity only but lower than the increase in TC frequency as a result of a combined effect resulting from an increase in TC intensity and frequency. If only the TC intensity increase were relevant, one would expect an increase in second-order hazards of 2.56 % since storm surge and wave heights are in the limit proportional to the wind speed squared. Besides, the CIs remain approximately the same as for the STCC case due to the already large number of samples for that scenario (see Fig. B7 in Appendix B).
3.5 Summary of the results
To summarize the results, the values of Figs. 12 and 13 are combined into Table 2, which also includes the results estimated based on STCF. The values are presented for return periods of 10 and 100 years, as averaged values both over the entire BoB and per region. Included are the CI values (2.5th, 97.5th percentiles), indicating that the CIs are significantly smaller based on synthetic tracks.
For clarity, discussion points have been grouped under three main topics, namely the generation of synthetic cyclone tracks, numerical modeling of storm surge and waves, and effects of a changed future climate on tropical cyclones.
4.1 Generation of synthetic tropical cyclone tracks
As shown by the reduction in the CI in the GPD fit (see, e.g., Fig. 10), the uncertainty in modeling TC-induced second-order hazards (i.e., storm surge and wave heights) is greatly reduced by using synthetic tracks. However, this is a reduction in the uncertainty in the fitting parameters and thus estimates of return values and periods. Uncertainties regarding the wind parametrization and the correct representation of the climate in the underlying dataset of the TCs persist. The former source of modeling uncertainties can be quantified by comparison with locally observed data. The latter, however, is a known unknown. TCWiSE is constrained to reproduce the statistics of the historical record. This means that the tool will not be able to (fully) reproduce physically credible and statistically unlikely tracks that are not recorded in observations. Additionally, in regions of rare TC occurrence, the lack of multiple tracks in historical records as a basis of the climate representation creates an unknown in terms of how accurately the generated STC tracks represent the “real climate” here. They will resemble the observed historical data with more realizations, where the historical data could in themselves be biased within the limited time span of the observations compared to the real climate. This cannot be verified but means that, in these regions, the results should be handled with care. However, for determining design criteria it is very common to use datasets of this (limited) time span.
Also, the STCs have been generated using TCWiSE only once and used for both current and future climate conditions. When rerunning TCWiSE multiple times the generated tracks will be different (though with the same statistics). The effect of this difference in sampling has not been investigated. Additionally, using the HTC data, only one method to generate STC tracks was used although many more methods exist besides TCWiSE, e.g., Vickery et al. (2000), Hardy et al. (2003), James and Mason (2005), Emanuel et al. (2006), Haigh et al. (2014), Nakajo et al. (2014), Lee et al. (2018), and Bloemendaal et al. (2020). Furthermore, looking at physics-based methods rather than historical track-based methods (e.g., Emanuel et al., 2008; Mori et al., 2019) could also lead to different results, though it is expected that the main patterns and general conclusions will remain the same.
4.2 Numerical modeling of waves and storm surge
The currently used numerical models still have a relatively coarse resolution near the shore (> 2 km) and therefore are not capable of representing nearshore bathymetric features and their effects on nearshore wave conditions (e.g., wave shoaling, refraction, breaking) or very local wind-induced setup changes to storm surge. The use of a higher-resolution model would not be computationally feasible when run in combination with thousands of tracks and for a large domain such as the BoB. For this reason, the estimated wave conditions were extracted at a water depth larger than 30 m, under the assumption that waves would not be affected by bathymetric features at this depth. The extraction depth was not changed for storm surge since this larger-scale process generally is less sensitive to the exact extraction depth, which is however an assumption in the model setup.
As the scope of the paper lies in the comparison between hazards estimated by using historical and synthetic tracks and how the use of synthetic tracks can reduce the confidence intervals around the estimation of these hazards, the difference between simulated storm surge and wave heights on the one hand and observed values on the other was not quantified. Combined with the limitations of the model resolution nearshore, presented results should be considered indicative results and not as values to be used directly in detailed design.
Only storm surge induced by wind and by the inverse barometric effect is considered for modeling extreme water levels since tides are not included. This is justified by the purpose of the paper (i.e., comparison between hazards induced by historical and synthetic tracks) and makes the comparison easier. Nevertheless, tidal effects would be important for the simulation of the total extreme water levels (see, e.g., Chiu and Small, 2016). Additionally, river runoff due to extreme precipitation events could also increase local extreme water levels.
4.3 Effects of changes in future climate on tropical cyclones
The current approach of incorporating climate-change-induced effects via only including the change in TC intensity and frequency is still heuristic and limited in terms of physical representation. Potential effects like changes in sea surface temperature that result in changes in the statistics used of locations of TC generation and termination, forward speed, and heading have not yet been incorporated. Also, changes to the central pressure of TCs are not forced directly but only through the relation to the intensity increase in wind speed. Moreover, a multi-model ensemble of different climate models feeding into the model train could result in more robust findings. The cyclone frequency increase used in this study based on Knutson et al. (2015) is of a similar order of magnitude to that of, e.g., Sugi et al. (2017), which for the NOI describes a 21 % frequency increase for category 3–5 TCs, and also to similar trends described in other literature (e.g., Walsh et al., 2016). However, uncertainty remains as at the same time, for low-wind-speed categories, Sugi et al. (2017) found a reduction in cyclone frequency. In general, for specific regions/countries within the BoB the exact effects of climate change on TCs are still the subject of debate in the literature, as for instance seen in the spread of the model results in Knutson et al. (2020). Furthermore, in Knutson et al. (2015), different cyclone frequency increases are mentioned for different wind speed categories, not all of which are statistically significant. The 200 % frequency increase for categories 4–5 mentioned in Knutson et al. (2015) would lead to even stronger increases in derived values of storm surge and wave height, but the likelihood of such an increase is uncertain and marked as statistically insignificant (Knutson et al., 2015). Also, so far, historical data do not seem to suggest any clear local trends. These predictions will also keep on being extended and improved, for example to investigate more extreme relative changes (e.g., Knutson et al., 2020; Walsh et al., 2019). For instance, Knutson et al. (2020) indicate, after comparing results from different studies, a small decrease in the median frequency change for the NIO for categories 0–5 combined and a small frequency increase for the more intense categories 4–5. For the intensity increase, the median increase is about 5 % (Knutson et al., 2020). A large spread in projections remains, indicating that the results in this study following Knutson et al. (2015) alone should be interpreted as a proof of concept on the possible effects of climate change, based on one of many possible and different future scenarios.
In this study, estimates of extreme storm surge and significant wave heights induced by tropical cyclones were derived along the Bay of Bengal, based on both historical (deterministic method) and synthetic tracks (probabilistic method). Synthetic tropical cyclones tracks were generated by means of TCWiSE for a period of 1000 years using the statistics of historical tropical cyclones as a basis but including a much larger number of realizations (i.e., 81 historical tracks versus 1745 synthetic tracks). It is shown that the statistics of the first-order hazard of wind speed are well reproduced by the synthetic tracks. Consequently, created wind fields were used to simulate the second-order hazards, namely storm surge and wave heights, based on the coupled process-based models Delft3D FM and SWAN. The study shows that, for the Bay of Bengal, about 400 years of synthetic results is required to reach convergence with results for wind speed, wave heights and storm surges, with slight differences between the different variables. Since this is within 1000 years, the synthetic tracks produce reliable estimates to compare to the results based on historical tracks.
An extreme value analysis performed over the computed storm surge and wave heights showed that, for the Bay of Bengal, the 95 % confidence intervals using the synthetic tracks are 70 %–80 % smaller than the confidence intervals estimated based on historical tracks. The use of the deterministic method leads to an underestimation ranging between −31 % and −13 % for the estimated storm surge with return periods of 10 and 100 years and an under-/overestimation of between −2 % and +6 % for the wave heights for the same intervals. The use of synthetic tracks allows us to more robustly sample the full parameter space describing the tropical cyclones and to more accurately capture modeled extreme values, representing events with both more disadvantageous and more advantageous trajectories which could statistically be plausible but may not have happened yet historically. Hereby, regional differences occur where regions in the south of the Bay of Bengal (e.g., Sri Lanka), which generally have a lower probability/number of historical cyclone events, show the largest underestimation of extreme waves computed based on the deterministic method compared to the probabilistic method. For extreme storm surge there is more variability from region to region, indicating that in regions with a higher tropical cyclone probability, using a deterministic method could also lead to an under- or overestimation of predicted values. The probabilistic method of deriving tropical-cyclone-induced coastal hazards using synthetic tracks of TCWiSE can thereby improve the derivation of local design values anywhere in the world where tropical cyclone hazards exist.
Simulations were carried out both for current climate conditions and assuming changes in the frequency and intensity of tropical cyclones, representing a future climate including possible effects of climate change. Literature values were used to describe possible changes in tropical cyclone frequency and intensity by the year 2100, and what this could imply in terms of changes in storm surge and wave heights was modeled. By assuming a possible increase in tropical cyclone frequency of +25.6 % and tropical cyclone intensity of +1.6 %, results show that this could result in an increase in the second-order hazard storm surge ranging between +11 % and +6 % for return periods of 10 and 100 years, respectively, and +9 % and +6 % for the wave heights. Thus, the combination of an increase in tropical cyclone frequency and intensity could result in a much larger increase in second-order hazards (storm surges and wave heights) than the actual increase in tropical cyclone intensity only (first-order hazard wind speed), albeit lower than the increase in tropical cyclone frequency. However, the exact quantification of the effects of climate change on future tropical cyclones is still subject to debate, and these differences are still smaller than the governing confidence intervals or differences in results when using a deterministic approach. Presented results regarding the future climate hazards therefore only provide a first insight into the possible changes and should be interpreted as a proof of concept.
Since for local studies the approach followed of modeling thousands of synthetic tropical cyclones is (probably) not feasible considering that the (relatively coarse) numerical models of this study had a running time of about an hour per tropical cyclone, future work should focus on defining and reducing the number of synthetic tropical cyclone tracks needed or using faster methods to derive storm surge and wave height values (e.g., van Ormondt et al., 2021).
Code revision 66 of TCWiSE has been used, which is the same as described in Nederhoff et al. (2021). The open-source tool is available at the following link: https://www.deltares.nl/en/software/tcwise/ (last access: 31 May 2022).
Settings used are as follows.
basinid = `NI'
dx = 0.1
source = `usa'
window_KDE = 300
window_dx = 15
nyears = 1000
exclude_land_map_KDE = 1
methodlandv_KDE = 2
deleteclosezeros_KDE = [1 1 0]
merge_frac = 0.5
dt = 3
coupled_allowed = [0 0]
decoupled_allowed = [1 1]
latitude_allowed = [0 0 0]
additional_landeffect = 1
coefficientdecay = 0.0155
termination_method = 1
stochastic_radii = [0 0]
wind_conversion_factor = 0.93
cutoff_windspeed = 0
cutoff_sst = 0
A2 Delft3D Flexible Mesh Suite
The version of Delft3D FM used in this study is 22.214.171.124394. The Delft3D FM model is based on the grid of the GTSM (Muis et al., 2016), with the coarsest resolution of 25 km on the ocean and the finest resolution along the coast of about 3 km.
The applied wind drag coefficient does not linearly increase with wind speed. As described by Vatvani et al. (2012) the drag coefficient first increases linearly up to a wind speed of 25 m s−1 (with Cd,max = 0.005) and then it decreases linearly again up to a wind speed of 50 m s−1 (with Cd = 0.0025). For even higher wind speeds the drag coefficient remains constant at this last value.
The version of SWAN used in this study is 40.91AB. For the SWAN model a rectilinear grid with a resolution of 0.2∘ was used (∼ 2 km). The model was run in non-stationary mode with a time step of 10 min. At the southern boundary at the open ocean no information was applied, and therefore all waves were generated internally as a result of the forced cyclones. No background wind is included either for non-tropical cyclone conditions. A drag coefficient limiter was used with maximum value Cd,cap = 0.002 (–) as can be interpreted from Zijlema et al. (2012) to limit the wave growth for very high wind speeds. For the whitecapping the formula of van der Westhuysen et al. (2007) was used. The bottom friction was set to a constant bottom friction coefficient χ = 0.038 m2 s−3 as advised in Zijlema et al. (2012).
Water levels and flow velocities were coupled with the wave model and updated every 30 min. The directional grid covers the full circle (360∘), allowing for waves to travel to and from all directions. The number of directional bins was 36, which results in a directional resolution of 10∘. The spectral grid covers a frequency range from 0.033 to 0.5 Hz, allowing for wave periods from 2 to 33.3 s. The number of frequency bins is 30.
The ORCA toolbox to derive the POT GPD is not open source but is available through https://www.deltares.nl/en/software/orca/ (Deltares, 2022a). TCWiSE is available through https://www.deltares.nl/en/software/tcwise/ (Deltares, 2022b). The Delft3D Flexible Mesh Suite is available through https://www.deltares.nl/en/software/delft3d-flexible-mesh-suite/ (Deltares, 2022c).
The IBTrACS dataset for HTC tracks is publicly available from https://www.ncdc.noaa.gov/ibtracs/ (Knapp et al., 2018). The calculated values of storm surge and wave heights along the Bay of Bengal of the STCC used in Figs. 11a and 12a are freely available as a dataset from Zenodo: https://doi.org/10.5281/zenodo.6420739 (Leijnse et al., 2022).
All authors have read and agreed to the published version of the paper. Conceptualization, methodology and writing – review and editing were by all authors; software and resources were contributed by TWBL and KN; formal analysis was by TWBL and SC; investigation, data curation and visualization were by TWBL ; writing – original draft preparation was by TWBL and AG; funding acquisition was by AG.
The contact author has declared that neither they nor their co-authors have any competing interests.
The views expressed in this article do not reflect the views of the Asian Development Bank (ADB).
Publisher's note: Copernicus Publications remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
This article is part of the special issue “Coastal hazards and hydro-meteorological extremes”. It is not associated with a conference.
We acknowledge Deltares' internal research programs, which have provided funding to carry out the study and write the paper. Furthermore, we would like to thank Björn Röbke for helping in improving Fig. 1.
This research has been supported by Deltares' internal research programs (“Planning for Disaster Risk Reduction and Resilience”, “Seas and Coastal Zones” and “Natural Hazards”).
This paper was edited by Piero Lionello and reviewed by Christian Mario Appendini Albrechtsen and one anonymous referee.
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