Hydrogeology of the Bay of Bengal Coast of India with Special Emphasis on Saline Water Intrusion

 

A. K. Bhattacharya, S. Basak, P. Maity,
L.K. Paira, Sankar Sarkar, S.C. Maji

Department of Applied Mechanics, Bengal Engineering and Science
University, Shibpur, Howrah, India.

ABSTRACT

The geological composition and the rate at which freshwater is being exploited from the aquifers greatly control the intrusion of saline water into the coastal aquifers. The phenomenon is common in the extensive coastal sedimentary deposits and delta of major rivers of the east coast of West Bengal. Extensive work on saline water intrusion and geological formations have been carried out on the Indian coast and several other places. These have guided in making theoretical and practical assumptions that were used for studying and analyzing the data collected from boreholes in the area. The east coast of India was divided into five geological regions from which three hydrogeochemical provinces were created. Methods of controlling saline water intrusion and managing groundwater exploitation in the coastal areas were suggested. The paper equally suggested further studies and research work that can lead to sustainable exploitation/use and management of groundwater resources in coastal areas.

INTRODUCTION

The geological formations of coastal areas are composed of deposits usually laid down under fluviate, lascustrine and marine environments. These deposits normally grade into one another and usually vary widely in lateral extent and thickness. In some faulted regions the bedrock outcrops along the seashore with hardly any sedimentary cover. In deltaic areas of major river valleys, the coastal plains may extend to hundred of kilometers with sedimentary strata of great thickness that spanned considerable part of geological time scale. The stratification of these deposits reveals that grain sizes may vary widely depending on the environment under which they were laid. The coarsest materials are usually derived from the fluviate environment while the finest materials are usually deposited beyond the neritic zone in the deep seas. Deltaic deposits occurring in the outfall regions of river systems are of particular interest because they hold some of the highly productive aquifers and form significant part of coastal sedimentary. The total areas that can receive deposit of a delta have been estimated to be about 5000000 km2 (Twenhofel, 1961). Some large deltas such as Ganges-Brahamaputra, Nile and Huang Ho have areas exceeding 100000 km2. These deltas were formed from materials deposited both sub-aerially and sub-aqueously; and have grain sizes that widely range from materials coarser than gravel to clay. The grain sizes depend on several factors such as maturity of the streams, distance to source rocks and rock types in the catchment area. Coarse deposits of gravel and pebbles are commonly found where youthful streams that flowed over rocky catchments constitute the coastal drainage. Generally, materials of the size of gravel and above are confined to the basal or lower part of the sedimentary cycle. Relatively coarse sediments are found in beaches, bars and open bays while the finer sediments are concentrated in active tributaries such as in marshes, stagnant bays and abandoned channels. Plastic clay and peat are important lithologic members in some coastal deposits (Todd, 1959). In the deposits laid sub-aqueously, the grained ones may be abrupt due to a sudden reduction in the velocity of stream flow near the coasts. Grain size distribution of the sediments deposited on the continental shelf is more uniform parallel to the coast. The deposits are coarsest near the shore followed by silty materials in the inner marine shelf and clay in the outer marine shelf. The sediments in the coastal areas are wedge-shaped, the thickness increasing seaward from the shore, conforming to the topography of the basement on which the deposits are laid. These deposits may acquire an initial seaward dip conforming to the slope of the continental shelf and the stratification according to the variation in the texture of the materials brought in from the streams. The dip may be accentuated due to differential compaction/consolidation of the sediments. Coastal aquifers generally have a complex sequence because of history of sea level rise and fall. Huge piles of sediments that accumulated in coastal regions have formed part of outfall areas of geosynclines, which are characterized by subsiding floors. Deposits accumulated in this way may attain a thickness of several thousand meters as sedimentation keeps pace with consolidation. Porosity, specific yield and permeability of coastal sediments are similar to those of materials have similar textures in other types of deposits.

The quality of water in the phreatic aquifer changes from fresh within the limits of freshwater tides to brackish in the upper reaches of estuaries to saline in the lower reaches. The saline zone in the phreatic aquifer is likely to be wider in plains with tidal influx deep into the interior than in plains in which the tidal influx is narrow. Changes in the estuarine river courses may render groundwater in the phreatic aquifer saline in extensive areas. In general, salinity in the aquifer may be several hundred meters or more in the water head. The absence of artesian aquifers with distant sources of recharge does contribute to the salinity of coastal aquifers (Todd, 1960). Deeper confined aquifers overlain and underlain by relatively impermeable layers outcropping in elevated areas beyond the tidal reach are likely to contain freshwater far down dip beneath the sea. Aquifers that outcrop in low altitude within the tidal reach are less likely to contain freshwater far down-dip because of lower hydraulic head resulting in less opportunity for flushing of salt as well as the possibility of the outcrop areas having been submerged by saline water in the past. Examples of freshwater layers of considerable thickness (greater than 100 m) are deltaic plain of Song Liao, Changjians and Huang ho rivers in China (Shuqin, 1985) and, Bhagirathi and Muhanadi-Brahmani rivers (Dutt, 1977). In the Gulf coastal plain of South West Louisiana, confined aquifers have been tapped by offshore wells yielding freshwater (Jones, et al., 1966).

THEORY OF SALINE-FRESHWATER INTERFACE

The boundary between salt and fresh water is termed the saline freshwater interface. Ghyben–Herzberg gave a relationship that, under conditions of static equilibrium between saline and fresh water in a phreatic aquifer having hydraulic connection with the sea level is expressed as:

(1)

from which

(2)

For gf = 1 and gs = 1.025, Zs = 40 Zw
where gs = Density of saline water
          gf = Density of fresh water
          Zs = Depth of the Interface below sea level
          Zw = Elevation of the Phreatic level above sea level
          g = Acceleration due to gravity

REVIEW OF LITERATURE

Some investigations on the interrelation of two miscible fluids in porous media have already been conducted both theoretically and under field conditions. Amongst important theoretical works the earliest analyses were carried out independently by two scientists; Ghyben (1988) and Herzberg (1901) both assuming simple hydrostatic condition in a homogenous unconfined coastal aquifer. The correlation developed underestimated the depth of saline-freshwater interface. Hubbert (1940) did a more realistic analysis for steady outflow into sea. With Hubbert’s suggested methodology, the exact position of the interface could be estimated with a fair degree of accuracy by graphical flownet construction. But this analysis assumes a sharp interface boundary, whereas in reality, there exist a diffused mixing zone. Henry (1960) presented a mathematical solution for steady-state flow considering dispersion. Pinder and Cooper (1970) provided a numerical solution for calculating the transient position of saline waterfront in a confined aquifer. Lee and Chang (1974) carried out finite element analysis of the same. Wicks and Herman (1995) performed a modeling study to address the effect of a single, high permeable zones at disperse aquifer of coastal aquifer. The geological profile of fresh water and saline water interrelations at Far Rockway, Nassau county, Long Island have been studied by Perlmutter & Geraghty (1963). Cooper et al (1964) studied the basic properties of the transient zone of Biscayne aquifer near Miami, Florida. Schmorak and Merado (1969) investigated the upconing of underlying saline water due to well pumping. Todd & Meyer (1971) studied the effect of annual variation in pumping rate on the upconing of underlying saline water in Honolulu, Hawaii. Smart et al (1988) studied calcite dissolution in freshwater-saltwater interface. Wallis et al (1992) mainly studied the reduction in the thickness of freshwater lens due to presence of buried high conductivity layer at Bahamas. Burnet et al (2001) conducted a comparative field study on direct discharge of freshwater from coastal aquifers into the sea. Taniguchi et al (2002) performed extensive field study with data compilation on submarine groundwater discharge (SGD) at South America, Africa and part of Asia. Bhattacharya (2002) carried out investigation on the cause and effects of saline water intrusion into the coastal aquifer of West Bengal. Sharma et al (2002) developed a three-dimensional model study to investigate the saltwater intrusion in coastal aquifers in regions of high permeability. Amer et al (1988) developed a finite element model (FEM) to investigate the Nubian aquifer system in Egypt.

Geological regions of the East Coast of India

Some regions underlain by rock types of different ages, origin and mineral compositions are characterized by a general similarity in the mode of occurrence of groundwater. These regions may be grouped into a groundwater province by ignoring the subtle difference in the hydrologic and hydraulic properties of various lithologic types. Also, from a practical perspective, the methods of exploration, assessment, development and management of groundwater resources are in most cases, common to the various rock types within a groundwater province. Taylor (1959) grouped the various stratigraphic units of India into eight water provinces, from which five fall in East coast of India.

Ganges-Brahamaputra Alluvial Province

The province, encompassing an area of about 850,000 km2 comprises the vast plain of the Ganges and Brahmaputra rivers underlain by late tertiary and quartenary alluvium that has been deposited in a secondary environment. The thickness of the sediments increases from north to south, the basement surface of hard rocks under the alluvium sloping at an average angle of 10 to 30 (Krishna 1968).

At some places, the thickness of alluvium exceeds 100 m. This vast and thick alluvium fills constitutes the most potential and productive groundwater reservoir in India. In the deltaic tract from the top zones, down to depth of 15m to 76m, is predominantly clayey and underlain by clay interbedded with sand and gravel.

Precambrian Sedimentary Province

The province comprises of structural basins that contain limestone, shale, sand stone, quartzite and local conglomerates, principally belonging to the Cuddapah, Kurnool and Vindhyan system of late Precambrian to early Paleozoic age. The thickness of sediments is 3000 m in the Cuddapah basin. They dip at low angles of 20 to 100. Limestone, dolomite and calcareous shale have been karstified to varying degrees as evidenced by caves (Borra and Betamcherla in Andhra Pradesh). Springs mark the landscape of limestone in the Cuddapah basin.

Cenozonic Sedimentary Province

The province comprises some narrow coastal plains on the Coromandel coast and a belt of strong rocks in Eastern India. It is underlain by a sequence of semi-consolidated conglomerates, sandstone, shale and lignite ranging in age from late cretaceous to late tertiary. Locally and exceptionally, sandstone horizons are so hard that they require blasting (Gowrisankaram et al 1980). In the Coromandel coast, the seaward-dipping strata contain several artesian aquifers down to a depth of 400 m or more. In the Neyveli area (Coromandel coast) the cuddalore sand stone form the aquifers of friable, loosely cemented, porous and permeable well-sorted coarse sand stones that are laterally extensive and fairly uniform in thickness. Dense, plastic clay and shale form effective confining layers of the flowing-well areas for which individual aquifers are different. In the Krishna-Godavari inter-stream area in Andhra Pradesh and Caurvery-Paleru inter stream area in Tamil Nadu, wells of 150 m to 300 m depth tapping artesian aquifers are in free-flowing, with the discharge rates of some exceeding 100 m3/h. Tubewells commonly yield 50 m3/h to 200 m3/h.

Precambrian Crystalline Province

Plutonic, igneous and metamorphic rocks of Archaean and Algorkian systems, consisting chiefly of granite, quartzite, schist etc; extends from Kanyakumari to Calcutta. Locally, deep circulation of groundwater is indicated as instanced by striking a solution cavity at depth 290 m in a borehole drilled through charnockite in the Ponnani basin in Tamil Nadu. Groundwater development is largely through large diameter dug wells, which have discharge generally in the range of 20 m3/day to 200 m3/day. Well drilling and blasting to obtain enhanced supplies sometimes revitalize dug wells. In recent years borewells are being constructed in increasing numbers especially for public water supplies in the basin. The yields of these borewells are generally less than 25 m3/h but exceptional yields of over 90 m3/h have been recorded. Generally groundwater in this province contains less than 1000 ppm of dissolved solids but locally it may be brackish or saline. High concentration of fluoride has been reported to occur in localized areas in this province, especially in Audhra Pradesh and Tamil Nadu.

Cenozonic Fault Basins

The three discrete fault basins included in the province are; the Narmada, the Purna and the Tapti valleys, all of which contain extensive quaternary valley-fill deposits consisting of lenses of sand and gravel intercalated with silt and clay. The fill ranges in thickness from about 50 m to 150 m. Sand and gravel lenses form aquifers that sustain tubewells of 25 m3/h to 150 m3/h capacity. Groundwater in the Narmada and Tapti valleys contain 100 ppm to 500 ppm of dissolved solids but in parts of the Purna valley the groundwater is extensively saline.

Hydrogeochemical Provinces in East Coast of India

The basic similarities in chemical composition have been used to divide the groundwater in east cost of India into broad hydrogeochemical provinces of zones. The zoning was also influenced by hydrogeologic and climatic situations that have bearing on the variations in the nature and concentration of dissolved solids in the groundwater. Such classification enables visualization of geochemical characteristics of groundwater from the regions and useful in assessing the quality rating of groundwater for various uses. Handa (1964) divided the groundwater in sedimentary rocks in East Coast of India into three broad hydrogeochemical zones.

Bicarbonate zone

It includes generally, the primary and partially softened waters that are characterized by a high percentage of bicarbonate ions generally exceeding 90% of the total anions present. The chloride and sulphate concentrations do not exceed 0.5 mg/l. the ratio of alkaline earths to sodium shows wide variations but is generally above 3, while the ratio of calcium to magnesium generally exceeds 2.

The electrical conductivity (EC) of groundwater does not normally exceed 750 micromhos/cm. The province covers the Terai-Bhaber belt as well as all the contiguous zones stretching along the Himalayan foothills and the adjoining alluvial tract. High rainfall (100 mm to 4000 mm) permeable strata and steep slopes favor flushing of salt from the soil profile. The groundwater in the eastern part of West Bengal and eastern part of Orissa falls in this category.

Bicarbonate-Chloride zone

In this province, although the bicarbonate is dominant, the chloride and sodium ions become significant. The ratio of alkaline earth to sodium falls below 1. The EC shows an increase of up to 1500 micromhos/cm and the ratio of sulphate to chloride falls steeply to values as low as 0.I. This province extends through the southern part of the axial belt of the Indo-Gangetic alluvium and coastal Cenozoic provinces. The moderate rainfall (1000 mm – 2000 mm) and low terrain slope facilitate accumulation of salt in groundwater in the province.

Chloride Zone

The dominance of chloride ions with concentrations generally exceeding 50% of the total anions; the exceedance of sodium ions over alkaline earth metal ions; and EC of over 1500 micromhos/cm are some of the characteristics of the groundwater in this province. The groundwater can be divided into two broad sub-provinces depending on the proportion (or concentration) of the sulphate present in it. The groundwater in some parts of the Coromandel falls in this category.

Management of Coastal Aquifers

Saltwater intrusion into a fresh water aquifer occurs when pumping of wells lower the groundwater levels enough to cause salt water to move towards the well by reversal of hydraulic gradients or decrease in fresh water heads. Because of close association of freshwater with saline water in coastal regions, groundwater should be exploited in such a way that upconing of saline water, seawater intrusion and leakage of saline water from near surface sources to aquifers below are prevented. Seawater intrusion can be halted or prevented by maintenance of groundwater levels well above the sea level. This can be accomplished by reducing groundwater extractions modifying the pumping patterns and also by augmenting the natural replenishment by artificial recharge of local or imported water supplies. Another approach to control seawater intrusion is to form a subsurface dam by construction of a cut-off wall of sheet pile, concrete or puddled clay. An impervious zone can be created to prevent movement of groundwater in the aquifer through injection of cement grout, emulsified asphalt, bentonite, silica gel or calcium acrylate. A series of spreading grounds or injection wells or a combination of both could be utilized along the coast as dictated by the geological conditions encountered to create a groundwater mound or ridge. A line of pumping wells properly spaced along the coast can lead to formation of a pumping trough. In this case, these wells would produce a mixture of saline and freshwater resulting in waste of considerable quantities of freshwater. The pumping costs involved and the waste of usable waters are major factors to be considered in evaluating the practicability of protecting groundwater on the basis of maintaining pumping trough. For prevention and control of seawater intrusion Todd (1959) listed several measures that include:

In locations downstream from heavily irrigated areas, the water may be too saline for satisfactory crop production. The removal of salts from saline water is exceedingly expensive especially if the water is to be used for irrigating crops. A possible solution is to dilute saline water with freshwater or waters of lower concentration so that the resulting water after mixing is suitable for use.

CONCLUSION

The review of geological conditions and hydrogeochemistry of groundwater in the region have provided limited information; it has also opened up an opportunity to carry out extensive research on saline water intrusion in aquifers of this region. There is need to improve on existing knowledge that was based on simplified assumption through expanded fieldwork, laboratory work, and research. More information is required to show the pattern of variation of salinity concentration along and across the shoreline; as well as with depth. When all these information/data are available, it will be possible to use modern techniques to prepare, design or generate decision support systems that would be useful for planning, exploitation and monitoring for sustainable management of groundwater resources in coastal regions of India.

ACKNOWLEDGEMENTS

The authors thank the All India Council for Technical Education for providing financial support to this research through the project titled ‘Saline water intrusion into coastal aquifers with special emphasis on east coast of India.’ The project was awarded through the AICTE’s letter no. 8022/RID/NPROJ/RPS-82-4 dated 22/3/2004. The authors are grateful to Dr. Karl Hofius and Dr. William Burnett for constructive comments regarding the paper.

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