Floods and the Ganges-Brahmaputra-Meghna Delta
Bangladesh is a highly flood prone country, reflecting the strongly seasonal regional climate and monsoon river flows of the Ganges, Brahmaputra and Meghna Rivers, its low-lying nature and its position at the north of the Bay of Bengal. Flooding can be classified as either fluvial, tidal, fluvial-tidal or storm surge, each of which create different flood extents and associated damages. Cyclones and associated storm surges can breach embankments threatening life and livelihoods on the coast, while extreme fluvial events can cause extensive flooding of up to a quarter of the national land area. Existing management interventions, including flood warnings, cyclone shelters, and coastal embankments, mitigate flood inundation and its consequences. However, they can affect the hydro- and morphodynamics in the area influencing future flood events.
Bangladesh is a highly flood prone country, reflecting the strongly seasonal regional climate and monsoon run-off of three large rivers from the Himalayas (Brammer 1990; Hofer and Messerli 2006; Brammer 2014), heavy local precipitation during the monsoon and tropical cyclones in the Bay of Bengal (Nicholls 2006). As a result, flooding can occur for multiple reasons, posing a threat to life and damage to economic assets. Of relevance to this analysis, floods can cause damage to ecosystem services, particularly agriculture and associated livelihoods.
In coastal Bangladesh, floods are related to a number of inter-related physical processes, which can be classified according to the main driver: (i) fluvial floods, (ii) tidal floods, (iii) fluvio-tidal floods and (iv) storm surge floods. While all types of floods can cause damage and disruption, coastal Bangladesh is best known for storm surge flooding due to large historic death toll associated with some of these events most notably between 1970 and 1991 (Nicholls 2006; Alam and Dominey-Howes 2015; Lumbroso et al. 2017). Fluvial and fluvio-tidal flooding is largely dictated by the flow in the major rivers of the delta due to precipitation and run-off upstream. The study area in this research (see Chap. 4, Fig. 4.2) has a large tidal range (three to six metres) which can cause tidal flooding in unprotected (un-poldered) areas. The magnitude of storm surge flooding due to tropical cyclones is also related to the tide; landfall of a cyclone during high tide can cause more extensive storm surge flooding, while cyclone landfall at low tide may not be noticed in terms of water level. The consequences for the resident population are therefore varied.
Coastal Bangladesh has an extensive system of coastal embankments and polders built since the 1960s with the goal to reduce flooding, manage water levels and enhance agriculture. While reducing the extent and frequency of coastal flooding, these have greatly modified the flood characteristics and associated coastal morphodynamics and rates of subsidence (e.g. Auerbach et al. 2015). Moreover, there are plans for substantial upgrade to some embankments as part of the Bangladesh Delta Plan 2100 (BanDuDeltAS 2014). In this chapter, a general overview of the four types of floods defined above is provided, followed by a summary and refection on the need for further research on flooding in coastal Bangladesh. More details of the flood modelling conducted in this research are given in Chap. 16.
8.2 Fluvial Floods
Fluvial flooding extents, as percentage of the national area, from 1954 to 2014 (60 fluvial flood events in 60 years) (BWDB 2015)
Extreme flood year (flooded area >24%)
Average flood year (flooded area 20–24%)
Dry year (flooded area <20%)
No. of events
No. of events
No. of events
The Brahmaputra water level starts rising from the early monsoon (June–July) and reaches its first peak in the third week of July. It then falls and rises again and, in an average flood year, attains its second peak in the first week of August. The Ganges has a single peak of flood level occurring in the second week of September. For the Upper Meghna, the first flood peak occurs in the second or third week of May, and, in an average flood year, a second peak occurs close to the second peak of the Brahmaputra. The effect of flow from the Upper Meghna on overall flooding is small as its discharge only represents ten per cent of the combined discharges of Ganges and Brahmaputra Rivers (Islam et al. 2010). The different timing of the flood peaks of the major rivers are mainly due to variations in rainfall in the upper catchments and the travel time to reach the discharge measurement points considered. Synchronisation of the peaks across the three rivers is rare, but has occurred: the floods of 1988 and 1998 (see Fig. 8.2) being examples (Islam and Chowdhury 2002). During peak synchronisation, the second peak of the Brahmaputra is delayed or may occur as a third peak coinciding with the single peak of the Ganges. This triggers significant fluvial flooding in Bangladesh.
Most fluvial flow adjacent to the study area occurs through the Lower Meghna estuary (MoWR 2005; Haque et al. 2016). This can cause inundation directly through the Lower Meghna, or via the estuarine networks that ultimately drains the combined flows of the three major rivers (Fig. 8.1). The drainage rate of fluvial flood water is largely dependent on sea levels. An elevated sea level due to either spring tides or a sustained monsoon may slow drainage prolonging flood duration, as happened during the 1998 flood (Haque et al. 2002). Over the longer term, subsidence and sea-level rise will increase mean sea levels (see Chaps. 14 and 16), influencing the fluvial flooding pattern in the coastal region.
There are few channels to take fluvial flow from the upper part of the country into the study area (Fig. 8.1), and most of these channels are restricted due to sedimentation. This limits flow and hence fluvial flooding. In addition, when polder embankments are considered (see Fig. 8.1 (lower)), only a small part of the study area is susceptible to fluvial flooding as they significantly determine flood extents. The maximum, minimum and average polder heights in the study region are 5.75, 4.50 and 4.79 m, respectively. Areas within the embankments are generally therefore not flooded during average fluvial events by overtopping (because flood water levels rarely exceed the embankment height), but there are incidents when areas within the embankments are flooded due to polder breaching (because embankments are not strong enough to resist the thrust of the fluvial flood). During extreme fluvial events (e.g. floods of 1998), both overtopping and breaching of polders happens.
8.3 Tidal Floods
Tides along the Bangladesh coast are semi-diurnal. The 18.6-year lunar nodal cycle has no influence along the Bangladesh coast, but the 4.4-year lunar perigean cycle modulates the tide by 4 cm (Sumaiya 2017). Tidal range is greatest along the Noakhali coast, immediately east of the Lower Meghna estuary (see Fig. 8.1), and declines to the east and west (Ahmed and Louters 1997). The mean tidal range at Hiron Point near the Sundarbans (west coast) is around 3 m, increases up to 6 m near Sandwip (west coast) and then decreases to 3.6 m further east (Cox’s Bazar). Tides propagate up to 100 km inland along coastal Bangladesh’s estuaries (Choudhury and Haque 1990). Coastal flooding due to tides is more pronounced in the central and eastern parts of the coast compared to west coast, reflecting the tidal range.
The construction of polders since the 1960s has eliminated significant tidal flooding in these areas. However, the polders also significantly reduce the area available for sediment deposition. The entire sediment load coming from the catchments of GBM basins drains into the Bay of Bengal through the different estuaries of the coastal region (see Chap. 15). Sedimentation of the river bed has reduced the capacity of the channels (Haque et al. 2016). At high tide, water levels can easily overtop the estuary bank and flood any unprotected land. During extreme fluvial flood conditions, high tides can cause overtopping and/or breaching of the polders. Once overtopped, the flood water inside the polder is unable to drain due to the difference in land elevation caused by confined sedimentation. This creates water logging inside the polder with negative implications for agriculture and other land uses. However, water logging inside polders also happens due to flooding from internal canals (without polder overtopping and/or breaching) and drainage congestion due to unplanned road networks and confined sedimentation.
Monsoon winds need to be considered when assessing tidal flooding in coastal regions. Along the Bangladesh coast, south-westerly and south-easterly winds during the monsoon season (June–October) are termed the monsoon wind. If they exceed 10 m/s, this raises the sea surface at the coast by 0.45 m in the west to 1.65 m in the east (Sumaiya 2017). This slows the fall of the tide and prolongs high water levels (Haque et al. 2002). Hence a combination of the highest astronomical tides and strong sustained monsoon winds give the highest potential for severe tidal flooding (Sumaiya 2017).
8.4 Fluvio-Tidal Floods
Figure 8.1 indicates the main channels controlling fluvial flow. During the monsoon, there are large freshwater flows along the Lower Meghna. These enter the study area along three spill channels and then flow south along the Tetulia channel, which is situated to the west of Lower Meghna. The other potential channels from the Meghna into the study area are the Gorai and Arial Khan, but currently these have limited conveyance restricting freshwater flow. The coastal area does not therefore receive any significant fluvial flow during the monsoon except adjacent to the Lower Meghna. Hence, tidal fluctuation plays a dominant role in determining the pattern of flooding across coastal Bangladesh. Due to the dynamic interaction between the fluvial flow and tides, and considering the flood versus ebb dominance of the estuaries (see Choudhury and Haque 1990), the landward part of coastal Bangladesh is characterised by fluvial flood, the middle part is characterised by fluvio-tidal floods and the seaward part is characterised by tidal flood. The exception is around the Lower Meghna estuary. Here flooding is always fluvially dominated by the large Meghna flow as it dominates tidal action during the monsoon.
8.5 Storm Surge Floods
The coastal region of Bangladesh is well known for storm surge flooding with major events going back several centuries or more (Alam and Dominey-Howes 2015); it dominates the global death toll due to storm surges over the last century (Nicholls 2006). The primary cause of storm surge flooding is the landfall of tropical cyclones—the magnitude, location and extent of flooding depend largely on cyclone intensity, its landfall location and time of landfall relative to the tide. The event has two inter-related components. One is the high wind speed of the cyclone leading to storm surge, and the other is the resulting land inundation from the sea and rivers/estuaries. Note that an intense cyclone does not always result in significant flood event. For example, in May 1997, a cyclone with wind speeds of 275 km/hr made landfall near the Noakhali-Chittagong coastline. This is the highest wind speed ever recorded in Bangladesh, and the landfall location is one of the most vulnerable locations for cyclone landfall. However, landfall occurred during low tide, and there was no inundation and only 155 people died. In 1991, when a cyclone with wind speeds 50 km/hr lower (225 km/hr) made landfall almost at the same location as the 1997 cyclone, there were about 138,000 deaths (Ali 1999; Dube et al. 2004); one of the most devastating cyclones in terms of human consequences in Bangladesh’s history. The variable that distinguished these two cyclones was landfall timing. The 1997 cyclone occurred at low tide, while the 1991 cyclone occurred at high tide, generating extreme water levels exceeding 8 m in a few places. For the Bangladesh coast, when a cyclone makes landfall during high tide, it has more potential for generating extensive storm surge flooding and associated damage.
Since 1991, major efforts have been made to mitigate these surge events (Lumbroso et al. 2017). These include flood forecasts and warning systems and the construction of robust surge shelters where the resident population can take refuge during these events. As a result fatalities have been greatly reduced by two orders of magnitude during recent major cyclones (e.g. Cyclone Sidr in 2007) compared to earlier events .
As coastal Bangladesh is the drainage route of the fluvial flows of the Ganges-Brahmaputra-Meghna River systems, the nature of fluvial floods in the region depends on the flooding patterns from these major rivers. The tidal range is large (between 3 and 6 m) and increases from west to east. Due to high tides, the unprotected land along the coast (outside the polders) is regularly flooded at high tide. Extreme astronomical tides combined with strong monsoons intensify the flooding situation; historical data shows that sea levels generated by tropical cyclones making landfall at high tide have the most impact on flood extents and associated damage. Polders a nd coastal embankments have stopped most fluvial and tidal floods in coastal Bangladesh. In the case of surges, forecasts, warnings and shelters have collectively great reduced fatalities during cyclones.
This chapter has focussed on describing the sources of flooding in coastal Bangladesh individually. As indicated in this chapter, it is increasingly recognised that floods occur due to multiple causes—so-called compound flooding (Leonard et al. 2014). Generally, it may therefore be more beneficial to consider flooding for Bangladesh in a more systemic manner: considering all sources, pathways, receptors and consequences. This allows analysis of the changing flood system, as illustrated for the United Kingdom by Evans et al. (2004a, b), to support national policy. Some examples of compound events have been shown here in terms of fluvial, tidal and surge events interacting. In the future, it would be useful to use this type of approach to analyse sources of coastal flooding in Bangladesh. The effects of polders on tides, morphodynamics and land elevation (subsidence) also deserve more attention .
- Ahmed, S., and T. Louters. 1997. Residual flow volume and sediment transport patterns in the Lower Meghna Estuary during pre-monsoon and post-monsoon: An analysis of available LRP data collected during 1986–1994. Meghna Estuary study technical note. Dhaka: Bangladesh Water Development Board (BWDB).Google Scholar
- Auerbach, L.W., S.L. Goodbred, D.R. Mondal, C.A. Wilson, K.R. Ahmed, K. Roy, M.S. Steckler, C. Small, J.M. Gilligan, and B.A. Ackerly. 2015. Flood risk of natural and embanked landscapes on the Ganges-Brahmaputra tidal delta plain. Nature Climate Change 5 (2): 153–157. https://doi.org/10.1038/nclimate2472.CrossRefGoogle Scholar
- BanDuDeltAS. 2014. Inception report. Bangladesh delta plan 2100 formulation project. Dhaka: General Economics Division (GED), Planning Commission, Government of the People’s Republic of Bangladesh.Google Scholar
- BWDB. 2015. Annual flood report 2015. Dhaka: Bangladesh Water Development Board (BWDB). http://www.ffwc.gov.bd/index.php/reports/annual-flood-reports. Accessed 9 May 2016.
- Choudhury, J.U., and A. Haque. 1990. Permissible water withdrawal based upon prediction of salt-water intrusion in the Meghna delta. The hydrological basis for water resources management proceedings of the Beijing symposium. Publication no. 197. Wallingford: International Association of Hydrological Sciences (IAHS).Google Scholar
- Dube, S.K., P. Chittibabu, P.C. Sinha, A.D. Rao, and T.S. Murty. 2004. Numerical modelling of storm surge in the head Bay of Bengal using location specific model. Natural Hazards 31 (2): 437–453. https://doi.org/10.1023/B:NHAZ.0000023361.94609.4a.CrossRefGoogle Scholar
- Evans, E.P., R.M. Ashley, J. Hall, E. Penning-Rowsell, A. Saul, P. Sayers, C. Thorne, and A. Watkinson. 2004a. Foresight; future flooding. Scientific summary, volume I: Future risks and their drivers. London: Office of Science and Technology.Google Scholar
- Evans, E.P., R.M. Ashley, J. Hall, E. Penning-Rowsell, P. Sayers, C. Thorne, and W. Watkinson. 2004b. Foresight; future flooding. Scientific summary, volume II: Managing future risks. London: Office of Science and Technology.Google Scholar
- Haque, A., M. Salehin, and J.U. Chowdhury. 2002. Effects of coastal phenomena on the 1998 flood. In Engineering concerns of flood: A 1998 perspective, ed. M.A. Ali, S.M. Seraj, and S. Ahmad. Dhaka: Directorate of Advisory, Extension and Research Services, Bangladesh University of Engineering and Technology.Google Scholar
- Hofer, T., and B. Messerli. 2006. Floods in Bangladesh: History, dynamics and rethinking the role of the Himalayas. Paris: United Nations University Press. http://archive.unu.edu/unupress/sample-chapters/floods_in_Bangladesh_web.pdf. Accessed 09 Aug 2017.
- Islam, A.K.M.S., and J.U. Chowdhury. 2002. Hydrologic characteristics of the 1998 flood in major rivers. In Engineering concerns of flood: A 1998 perspective, ed. M.A. Ali, S.M. Seraj, and S. Ahmad. Dhaka: Directorate of Advisory, Extension and Research Services, Bangladesh University of Engineering and Technology.Google Scholar
- Leonard, M., S. Westra, A. Phatak, M. Lambert, B. van den Hurk, K. McInnes, J. Risbey, S. Schuster, D. Jakob, and M. Stafford-Smith. 2014. A compound event framework for understanding extreme impacts. Wiley Interdisciplinary Reviews: Climate Change 5 (1): 113–128. https://doi.org/10.1002/wcc.252.Google Scholar
- Lumbroso, D.M., N.R. Suckall, R.J. Nicholls, and K.D. White. 2017. Enhancing resilience to coastal flooding from severe storms in the USA: International lessons. Natural Hazards and Earth Systems Sciences 17: 1357–1373. https://doi.org/10.5194/nhess-17-1-2017.
- MoWR. 2005. Coastal zone policy. Dhaka: Ministry of Water Resources (MoWR), Government of the People’s Republic of Bangladesh. http://lib.pmo.gov.bd/legalms/pdf/Costal-Zone-Policy-2005.pdf. Accessed 20 Apr 2017.
- Nicholls, R.J. 2006. Storm surges in coastal areas. Natural disaster hotspots: Case studies. In Disaster risk management 6, ed. M. Arnold, R.S. Chen, U. Deichmann, M. Dilley, A.L. Lerner-Lam, R.E. Pullen, and Z. Trohanis, 79–108. Washington, DC: World Bank.Google Scholar
- Sumaiya. 2017. Impacts of dynamic interaction between astronomical tides and monsoon wind on coastal flooding in Bangladesh. M.Sc thesis, Institute of Water and Flood Management (IWFM), Bangladesh University of Engineering and Technology (BUET), Dhaka.Google Scholar
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