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Spatiotemporal Variation of Van Der Burgh's Coefficient in a Salt Plug Estuary

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Spatiotemporal Variation of Van Der Burgh's Coefficient in a Salt Plug Estuary Hydrol. Earth Syst. Sci., 21, 4563–4572, 2017 https://doi.org/10.5194/hess-21-4563-2017 © Author(s) 2017. This work is distributed under the Creative Commons Attribution 3.0 License. Spatiotemporal variation of Van der Burgh’s coefficient in a salt plug estuary Dinesh Chandra Shaha1,2, Yang-Ki Cho2, Bong Guk Kim2, M. Rafi Afruz Sony1, Sampa Rani Kundu3, and M. Faruqul Islam4 1Department of Fisheries Management, Bangabandhu Sheikh Mujibur Rahman Agricultural University, Gazipur 1706, Bangladesh 2School of Earth and Environmental Science/Research Institute of Oceanography, Seoul National University, Seoul, Korea 3Deparment of Oceanography, Chonnam National University, Gwangju, Korea 4Hydrography Division, Mongla Port Authority, Bagherhat, Bangladesh Correspondence to: Yang-Ki Cho ([email protected]) Received: 11 February 2017 – Discussion started: 21 March 2017 Revised: 28 July 2017 – Accepted: 8 August 2017 – Published: 13 September 2017 Abstract. Salt water intrusion in estuaries is expected to be- dry season, causing the upstream intrusion of high-salinity come a serious global issue due to climate change. Van der bottom water. Our results explicitly show that K varies spa- Burgh’s coefficient, K, is a good proxy for describing the rel- tially and depends on the river discharge. This result provides ative contribution of tide-driven and gravitational (discharge- a better understanding of the distribution of hydrographic driven and density-driven) components of salt transport in properties. estuaries. However, debate continues over the use of the K value for an estuary where K should be a constant, spa- tially varying, or time-independent factor for different river discharge conditions. In this study, we determined K dur- 1 Introduction ing spring and neap tides in the dry (< 30 m−3 s−1/ and wet (> 750 m−3 s−1/ seasons in a salt plug estuary with an ex- A quantitative understanding of the characteristics of salin- ponentially varying width and depth, to examine the rela- ity distribution and transport under various environmental tive contributions of tidal versus density-driven salt trans- conditions is essential for the interpretation of the physi- port mechanisms. High-resolution salinity data were used cal, chemical, biological, and ecological status of an estuary. to determine K. Discharge-driven gravitational circulation Salt water intrusion into tropical estuaries has received sub- (K ∼ 0.8) was entirely dominant over tidal dispersion dur- stantial attention in recent years due to changes in rainfall ing spring and neap tides in the wet season, to the extent frequency and intensity levels. In addition, salt water intru- that salt transport upstream was effectively reduced, resulting sion can be aggravated by decreasing river discharges that in the estuary remaining in a relatively fresh state. In con- result from barrages being built upstream to provide water trast, K increased gradually seaward (K ∼ 0.74) and land- for drinking and irrigation (Shaha and Cho, 2016). Changes ward (K ∼ 0.74) from the salt plug area (K ∼ 0.65) during in river discharge levels alter estuarine circulation, stratifica- the dry season, similar to an inverse and positive estuary, re- tion, flushing times, salt water intrusion, as well as the trans- spectively. As a result, density-driven inverse gravitational port of biota and dissolved and particulate materials such as circulation between the salt plug and the sea facilitates in- salt, pollutants, nutrients, and organic matter (Azevedo et al., verse estuarine circulation. On the other hand, positive estu- 2010; Lee and An, 2015; Savenije, 2012; Shaha and Cho, arine circulation between the salt plug and the river arose due 2016; Valle-Levinson, 2010). Therefore, it is particularly im- to density-driven positive gravitational circulation during the portant to understand the responses of estuarine salt transport mechanisms to temporal changes in river discharge levels be- Published by Copernicus Publications on behalf of the European Geosciences Union. 4564 D. C. Shaha et al.: Spatiotemporal variation of Van der Burgh’s coefficient cause salt water intrusion may lead to shortages of drinking dry (< 30 m−3 s−1/ and wet (> 750 m−3 s−1/ seasons in a salt and irrigation water (Khan et al., 2011), decreased rice pro- plug estuary with an exponentially varying width and depth duction (Mirza, 2004), reduced freshwater fish habitat (Das- to examine the relative contributions of tidal versus gravita- gupta et al., 2014), and inadequate industrial freshwater sup- tional components of salt transport mechanisms. In addition, plies (Mirza, 1998). whether K functions in an inverse salinity gradient area of a Estuarine circulation represents the interaction among salt plug estuary has, thus far, not been examined. Therefore, contributions from gravitational circulation, tidal residual we also examined whether K can serve in an inverse salinity circulation, and circulation driven by tidally asymmetric ver- gradient of such a salt plug estuary. tical mixing. In turn, gravitational circulation is driven by The Pasur River estuary (PRE) is the longest (> 164 km) river discharge and density gradients (Valle-Levinson, 2011). estuary in the southwestern part of the Ganges–Brahmaputra Gravitational circulation tends to be dominant in many es- Delta in Bangladesh. Salt water intrusion in the PRE has re- tuaries and can be classified according to the morphol- ceived substantial attention in recent years due to increases in ogy or origin of the basin, its water balance, or the com- the magnitude and frequency of salt water intrusion upstream petition between tidal forcing and river discharge (Valle- as a result of climate change – from which there is a predicted Levinson, 2011). Van der Burgh’s coefficient, K, is one pa- sea-level rise of 30 cm by the year 2050 (Intergovernmen- rameter used to describe the relative weights of both tidal and tal Panel on Climate Change (IPCC), 2007) – and decreases density-driven horizontal salt transport mechanisms in estu- in river discharge levels resulting from an upstream barrage aries (Savenije, 2005; Shaha and Cho, 2011; Van der Burgh, (Shaha and Cho, 2016). Most previous studies focused pri- 1972). Tidal mixing and density-driven mixing vary along marily on analyzing the relationship between discharge and the axis of an estuary according to the tidal influence and salinity in the PRE (Mirza, 1998, 2004; Rahman et al., 2000; the volume of river discharge. Tide-driven mixing usually Uddin and Haque, 2010). A few studies of the hydrology of dominates downstream; a combination of tidal and gravita- mangrove ecosystems (Wahid et al., 2007), fish biodiversity tional components influences the central regimes, and grav- (Gain et al., 2008, 2015), surface-water quality (Rahman et itational mixing tends to dominate upstream (Shaha et al., al., 2013), and nutrient distributions (Rahaman et al., 2014) 2010). Therefore, a constant K value for an estuary, as sug- have been conducted in the PRE. Recently, a new type of gested in earlier work (Gisen, 2015; Savenije, 1993, 2005; salt plug formation was discovered in the multi-channel PRE. Zhang and Savenije, 2017), can not accurately represent the This was found to have been caused by decreasing river dis- nature of salt transport in estuaries for high and low river dis- charge levels resulting from an upstream barrage (Shaha and charge conditions. Shaha and Cho (2011), who suggested a Cho, 2016). However, earlier work typically omitted details modified equation to account for the exponential variation in of the salt transport mechanisms in the PRE, and these de- estuarine widths, examined the spatial variability of K along tails are necessary for a complete understanding of the hy- the axis of a small, narrow estuary with a large salinity gra- drodynamics and causes of salt water intrusion upstream. dient of 1.4 psu km−1. In the narrow Sumjin estuary, both Therefore, in this study, we applied the equation suggested the large spatial salinity gradient and exponentially varying by Shaha and Cho (2011) to determine K during spring and width are responsible for spatial variation of K and salinity neap tides in the dry and wet seasons. We sought to deter- distribution (Shaha and Cho, 2011). mine the variations in salt transport mechanisms in the PRE Nonetheless, debate continues as to whether K should be considering its exponentially varying width and depth, and to a constant (Savenije, 2005) or spatially varying (Shaha and assess the influence of river discharge levels on K. Cho, 2011) value for estuaries, and/or whether it can serve as a time-independent factor for varying river discharges (Gisen, 2015) and depends on geometries (Gisen, 2015). K is 2 Material and methods assumed to be a time-independent parameter, with every es- tuary having its own characteristic K value (Savenije, 1986, 2.1 Study area 1993, 2005). In their test of a small, narrow estuary, Shaha and Cho (2011) found that K values not only vary owing There are three distinct seasons in Bangladesh: a dry sum- to different salt transport mechanisms, but also depend on mer from March to June; a rainy monsoon season from July river discharge levels. In contrast, Gisen (2015) assumed K to October; and a dry winter from November to February to be independent of the river discharge level, finding in- (Rashid, 1991). River discharge is strongly seasonal. During stead that it depends on topography. Conversely, Zhang and the wet season (monsoon), approximately 80 to 90 % of the Savenije (2017) suggested a constant K value if the depth annual rainfall occurs. Maximum discharge occurs between is constant along the estuary; however, the depth typically July and October (wet season). In contrast, river discharge is varies. For instance, earlier research showed that the depth negligible from November to June (dry season). varied in 15 out of 18 estuaries and was constant in only The Pasur River is the most commercially important river 3 (Zhang and Savenije, 2017).
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