Hydrochemistry and Environmental Isotopes to Identify the Origin of Barapukuria Coal Mine Inflow Water, Northwestern Bangladesh

    

    

    Figure 3:  Major ion composition of groundwater, coal mine water and river
water samples plotted on a Piper diagram.
    
    

Oxygen, hydrogen and tritium isotopes

The collected groundwater sample d¹⁸O and d² compositions ranged from –5.4 to –3.4‰ (average –4.7‰) and –36 to –21‰ (average –31‰), respectively. Meanwhile, the d¹⁸O and d² compositions of collected coal mine water samples ranged from –5.0‰ to –4.4‰ (average –4.7‰) and –32 to –27‰ (average –28.9‰), respectively. Surprisingly, the average d¹⁸O (–4.7‰) composition of coal mine water was similar to the groundwater average d¹⁸O value (–4.7‰). But the river water d¹⁸O (–9.3‰) and d² (–66‰) compositions were much lighter than the average groundwater and mine water d¹⁸O and d² compositions Tritium (3H) is a natural radioactive isotope of hydrogen which is formed naturally by the dissociation of nitrogen following interaction with cosmic rays. It is also formed as a byproduct of thermonuclear testing and has a half life of 12.26 years. The widespread testing ‘above ground’ of thermonuclear devices between 1952 and 1962 drastically increased the amount of tritium in the atmosphere swamping natural background levels. The intermittent testing of such devices has also led to the introduction of periodic pulses or peaks of tritium to the atmosphere. Over land areas the removal of atmospheric tritium is principally via precipitation, which is extremely variable and dependent on the various climatic, land distance and orographic influences affecting precipitation. It is therefore apparent that tritium concentrations reaching the earth’s surface can be exceedingly variable in both time and space. Consequently, tritium levels in groundwater via both direct and indirect recharge can also be extremely variable [34]. Tritium content of analysed groundwater and coal mine water ranged from 0.1 to 4.5 TU.

Discussion

The composition of mineral salts affects the Electrical Conductivity (EC) of groundwater and EC values of groundwater increase along flow paths with increasing groundwater residence time, whether groundwater is not affected by sea water intrusion [18]. The high EC values (more than 5 times) for the coal mine water collected from the dewatering chambers indicate a good hydraulic connectivity between the most severely fractured coal seam bearing Gondwana sandstone and the overlying Dupi Tila aquifers. It also signifies that the fractured Gondwana sandstone permeability greatly increases downward and drains directly into the coal mine. Thus the long migration path of the infiltrating groundwater facilitates dissolution of mineral salts along the fractured Gondwana sandstone which may cause higher EC values and these results comply with the conclusion made by Kibria et al. [2]. The acidic to neutral groundwater pH values imply an open system unconfined aquifer all over the study area with high soil CO₂ giving rise to low pH. The alkaline pH values (>8.0) for coal mine water suggest decline in partial pressure of CO₂ (pCO₂) levels within the Gondwana aquifers and indicates lack of oxygen in the deeper Gondwana aquifers which could contribute to a more alkaline pH [35] for the inflowing coal mine water.

Circulating groundwater will acquire geothermal heating along its flow path [36] and subsurface temperature acts as a tracer for detecting the groundwater movement [37]. In present study the coal mine water average temperature (37.3 °C) is much higher (more than 10.7 °C) than the groundwater average temperature (26.7 °C). This implies that groundwater having low temperature within the Dupi Tila aquifers percolates into the deeper Gondwana aquifers attaining high temperatures within the coal seams which cause high heat flow in the coal mine [38].

Piper diagram shows that most of the samples are clustered at the central diamond (group-II) (Figure 3). The Piper diagram illustrates that the groundwater is dominantly of Na–Ca–HCO₃ and Ca–Na– HCO₃ type water, which are the initial source of water recharging into the aquifer systems. The Na–Ca–HCO₃ type groundwater observed in the study area shows slightly increase of N^a+ concentration with respect to Ca²⁺ and Mg²⁺. The increase in N^a+ exchange for Ca²⁺ and Mg²⁺ suggest softening process, which may indicate rapid recharge and/or much more water-rock interactions along the flow paths. The coal mine water samples are also rich in Na–Ca–HCO₃ and Ca–Na–HCO₃ type water and this phenomenon indicates possible connectivity between overlying Dupi Tila and underlying Gondwana aquifers causing rapid recharge into the Gondwana aquifers without changing chemical characteristics of recharging water. Besides, Ca– Mg–HCO₃ type low mineralized water observed in both groundwater and coal mine water also indicates connectivity between the shallow and deeper coal seam bearing Gondwana aquifers.

The deeper the groundwater moves, the more enriched it becomes in Na as more dissolution and cation-exchange takes place [39]. In present study, the Na concentration of groundwater samples ranged from 6.50–23.01 mg/L with an average of 14.86 mg/L. The low Na concentration in collected groundwater suggest a relatively short residence time (greater transmissivity) from the Dupi Tila aquifer. The coal mine water Na concentration ranged from 21.88– 65.62 mg/L with an average of 36.21 mg/L. The relatively high Na concentration of coal mine water indicates that this water is derived from groundwater moving slowly through the shallow Dupi Tila aquifer and reacts with Na-rich minerals through dissolution. Finally, a preferred conduit and enhance comminution of rock fragments along the fractured Gondwana rocks promote Na dissolution giving rise to high Na concentrations in coal mine water.

The average Ca²⁺ and Mg²⁺ concentrations of groundwater samples were 14.45 mg/L and 5.22 mg/L, respectively. Meanwhile, coal mine water average Ca²⁺ and Mg²⁺ concentrations were 22.38 mg/L and 4.98 mg/L, respectively. It is obvious that coal mine water average Ca concentration is nearly 1.6 times higher than that of groundwater average Ca²⁺ concentration. But the average Mg²⁺ concentration of coal mine water is to some extent lower than that of groundwater average Mg concentration. It indicates that surface water draining towards and into the coal mine does not undergo sufficient base exchange reactions and thus Ca²⁺ and Mg²⁺ are not enough adsorbed onto clays within the sediments in exchange for N^a+ [40]. Thus the interstitial release of Na from the overlying Gondwana sediments occurs as water flows down through the fractured Gondwana sediments with insignificant cation exchange as a function of relatively short distance that the water has travelled [41] as well as short residence time. It is evident that the resultant water that ends up on the coal seam horizon is slightly enriched in Ca²⁺ and less enriched in Mg²⁺, and it indicates calcite dissolution along the flow path rather than dolomite dissolution.

In groundwater, the cations Ca²⁺ and Mg²⁺ often come from carbonate minerals such as calcite and dolomite. Most of the major cations released in groundwater from carbonate minerals dissolution enhanced by respired CO₂ from oxic and anoxic organic matter degradation [42]. Reactions that specifically produce CO₂ through oxidation of organic matter are generalized by:

CH₂O (organicmatter) + O₂→ H₂O + CO₂ (1)

This reaction is then followed by

CaMg(CO₃)₂ + CO₂ + H₂O → Mg²⁺ + 2HCO₃ ^- +CaCO₃ (2)

CaCO₃ +CO₂ + H₂O → Ca²⁺ + 2HCO₃ ^- (3)

resulting in the high Ca²⁺, Mg²⁺ and HCO₃ - concentrations found in groundwater. There is also CO₂ in rain water which can facilitate carbonate mineral dissolution [43]. So that there would be straight positive correlation between Ca²⁺ and HCO₃ ^–, and Mg²⁺ and HCO₃ ^–. A bi-variant plot (Figure 4) of Ca²⁺ versus HCO₃ ^– shows strong positive correlation (r²=0.60) for groundwater, whereas Mg²⁺ versus HCO₃ ^– shows weak correlation (r²=0.15) for mine water (Figure 5). This indicates that groundwater in Dupi Tila aquifer moves slowly downward through the Gondwana aquifer with minor dissolution of calcite and latter have a low C^a+ concentration due to relatively short residence times within the aquifer systems.

Figure 4: Bivariate plot of Ca versus HCO₃.

    

    

    Figure 4:  Bivariate plot of Ca versus HCO3.
    
    

Close

Figure 5: Bivariate plot of Mg versus HCO₃.

    

    

    Figure 5:  Bivariate plot of Mg versus HCO3.
    
    

Close

The average SO₄ ^2- concentration of coal mine water is nearly six times higher than the groundwater SO₄ ^2- concentration. The elevated concentration of SO₄ ^2- in mine water can be attributed to the oxidation of sulphate minerals within the coal mine [44]. Meanwhile, the elevated sulphate concentrations in coal mine water samples indicate that the coal seam has a high acid-generating potential [41]. Nevertheless, the alkaline pH level of the coal mine water suggests that the coal seam also has sufficient base potential to neutralise the generated acid within the mine.

In Bengal delta aquifers, the sources of HCO₃ ^– would probably include root respiration (soil zone CO₂), microbial degradation of organic matter and carbonate dissolution [45]. In present study, the groundwater average bicarbonate concentration is more than two times higher than that of the coal mine water bicarbonate concentration having low pH (average <6.75). The relatively high concentrations (average 148 mg/L) of HCO₃ ^– in the shallow unconfined Dupi Tila aquifer groundwater may be caused by CO₂ dissolution of local meteoric water [46] and carbonate dissolution rather than microbial degradation of organic matter. The soil zone in the study area may contain elevated CO₂ pressure produced by decay of organic matter and root respiration, which in turn combines with rainwater to form bicarbonate following the reactions CO₂ + H₂O → H₂CO₃ and H₂CO₃ → H+ + HCO₃ ^– [47]. Bicarbonate may also be derived from the dissolution of calcite (Figure 4) rather than dolomite (Figure 5) following the equation (i). According to Kinniburgh and Smedley [48], Dupi Tila aquifers were thoroughly oxidized during its geological evolution causing a decrease in organic matter concentration in the aquifers. In addition, Ueno [49] found that bacteria may be consumed organic matters more easily from younger Holocene sediments than that of older Pleistocene Dupi Tila sediments. As per the above mentioned statements, it is obvious that the presence of insignificant concentrations of organic matter in Dupi Tila aquifer sediments may not be responsible for releasing higher concentration of HCO₃ ^– in groundwater released by the microbial degradation of organic matter. The low HCO₃ ^– concentrations of coal mine water compared to groundwater, are attributed to a lack of CO₂ present (confined aquifer), resulting slow loss of HCO₃ ^– [50] and this explains lower HCO₃ ^– concentration in mine water. It indicates that mine waters are recharged by the overlying shallower Dupi Tila aquifer.

In general, chloride is a conservative component, and evaporation and mixing are considered as the main factors controlling its concentration in groundwater. Solubility of N^a+ compounds is high, so N^a+ remains dissolved in water in a very wide range of concentration [51]. Most of the groundwater and coal mine water samples also plot above the 1:1 equiline (Figure 6). Plot of Na versus Cl shows an excess of Na to Cl, particularly for all coal mine water samples and also for most of the groundwater samples. The excess of sodium both in groundwater and coal mine water suggests that N^a+ originates from weathering of silicate minerals from the aquifer system due to rapid inflow of groundwater into deeper Gondwana aquifer facilitated by the mining activities.

Figure 6: Bivariate plot of Na versus Cl.

    

    

    Figure 6:  Bivariate plot of Na versus Cl.
    
    

Close

Gaillardet et al. [51] stated that the Na-normalized ratios for Ca²⁺ and Mg²⁺ might have been related to each other. Accordingly, in the plot of the molar ratios of Ca/Na versus Mg/Na are shown in a log–log space in (Figure 7). Recharging water infiltrating into the Dupi Tila aquifer shows low Ca/Na and Mg/Na rations (Figure 7), and the end member having lower Na normalized ratios is that of water draining silicates. The molar Ca/Na ratio of average crustal continental rocks is close to 0.6 [52], and due to the higher solubility of Na relative to Ca, lower Ca/Na molar ratios are expected in groundwater, which are related to weathering of silicates. In (Figure 7), the observed groundwater and coal mine water with low Ca/Na molar ratios are being influenced by silicate weathering rather than carbonate dissolution [18]. Meanwhile, Stallard and Edmond [53,54] state that the molar ratio (N^a+ + K⁺)/Cl^- 1 indicates silicate (feldspar and mica) weathering. In present study, it is observed that most of the groundwater (except sample B5 and B12) and all coal mine water samples show molar ratios (N^a+ + K⁺)/Cl^– >1 (data not shown), which indicates silicate weathering. From the above discussions, it is obvious that rainfall infiltrates into the shallow Dupi Tila aquifers through the ground and hydrogeochemical reactions take place for the formation of Ca-Mg-HCO₃ type water. The development of roadways within the coal mine creating voids facilitate rapid entrance of water into the coal mine through the overlying Dupi Tila and Gondwana aquifers. The initial Ca–Mg–HCO₃ type water tends to change into Na-Ca- HCO₃ type water due to preferentially silicate weathering, which helps to add N^a+ within the solution in increase with the length of the flow path and thus the coal mine water tends to be Na–Ca–HCO₃ type water due to silicate weathering giving rise to excess N^a+ with high pH.

Figure 7: Molar ratio bivariate plot of Na-normalized Ca and Mg.

    

    

    Figure 7:  Molar ratio bivariate plot of Na-normalized Ca and Mg.
    
    

Close

The Local Meteoric Water Line (LMWL) proposed by Majumder et al. [12] runs closely parallel to the GMWL (Figure 8). The entire groundwater, mine water and river water data set plotted along and/or close to the LMWL and GMWL, producing a regression line defined by d² = 7.4d¹⁸O + 4.4 (line not shown in Figure 8) with a regression coefficient (R2) of 0.94 that suggests a meteoric origin [55,56] with insignificant localized evaporation effect. The alignment of isotopic composition close to the GMWL and LMWL demonstrates a precipitation origin of groundwater in the studied area [57]. Except sample B2, all the groundwater and mine water d¹⁸O values show narrow range (–5.4‰ to –4‰) along the LMWL (Figure 8), which suggests that these waters have mixed sufficiently to homogenize variations in the isotopic composition of recharge water. The average d¹⁸O value (–4.7‰) for the groundwater is similar to the mine water average d¹⁸O value (–4.7‰), which indicates that the groundwater percolates in to the underlying coal seam bearing Gondwana aquifers without changing infiltrating groundwater d¹⁸O values. The groundwater sample B2 with slightly enriched d¹⁸O value (–3.4‰) indicates minor evaporation effect prior to infiltration. The river water B20 d¹⁸O value (–9.3‰) is highly depleted and the extremely negative value reveals the high content of glacier and snowmelt water, which is typical for a high-altitude river. Meanwhile, the river water d¹⁸O value (-9.3‰) of the study area is similar to the d¹⁸O value for Tista river water [18], which also reflects that the substantial amounts of monsoon rainfall in the Himalayan region as well as snow melt water [58] may give rise to the depleted d¹⁸O value for the river water. The highly depleted isotopic signatures of the observed river water reveals that the aquifers in the study area may not be recharged by the river water and thus the groundwater has a local origin of recharge (i.e., rainfalls).

Figure 8: d-plot for d¹⁸O and d²H compositions of the groundwater, coal mine water, and river water

    

    

    Figure 1:  d-plot for d18O and d2H compositions of the groundwater, coal mine
water, and river water
    
    

Close

Except groundwater sample B1, all the analysed water sample 3H content was less than 0.7 TU. The low tritium content of shallow groundwater and coal mine water indicate relatively large travel times in the overlying Madhupur clay zone (several years to tens of years) which may control the recharge pattern of study area, resulting in the loss of tritium by radioactive decay before reaching the aquifer. As a consequence, the groundwater and mine water with a tritium value <1 TU may be considered “old” water recharged prior to 1952 while higher values that is the B1 well water would represent “new” water being wholly or partially recharged since 1952 [59].

Conclusion

The hydrochemical and isotopic data of collected groundwater, mine water, and river water show distinct evidence of the origin of Barapukuria coal mine inflow water. EC, pH, Temperature, solute concentrations (N^a+, Cl^–, Ca²⁺, Mg²⁺, SO₄ ^2–, and HCO₃ ^–), stable isotope ratios (hydrogen and oxygen), and 3H concentrations were used successfully to identify the origin of Barapukuria coal mine inflow water. The long migration path of the infiltrating groundwater facilitates dissolution of mineral salts along the fractured Gondwana sandstone which may cause higher EC values and the coal mine water high EC values indicate a good hydraulic connectivity between the most fractured coal seam bearing Gondwana aquifer and the overlying Dupi Tila aquifers. The acidic to neutral groundwater pH values imply an open system unconfined aquifer all over the study area. But the alkaline pH values for coal mine inflow water suggest decline in partial pressure of CO₂ levels within the Gondwana aquifers and indicates lack of oxygen in the deeper Gondwana aquifers which could contribute to a more alkaline pH for the inflowing coal mine water. Besides, the coal mine water higher temperature than that of groundwater temperature implies that low temperature Dupi Tila aquifer water percolates into the deeper Gondwana aquifers attaining high temperatures within the coal seams which cause high heat flow in the coal mine. Both groundwater and coal mine inflow water are dominantly of Na–Ca–HCO₃ and Ca–Na–HCO₃ type water and this phenomenon indicates potential connectivity between overlying Dupi Tila and underlying coal seam bearing Gondwana aquifers causing rapid inflow into the coal mine tunnel without changing chemical characteristics of recharging water. Besides, low mineralized Ca–Mg–HCO₃ type water observed in both groundwater and coal mine inflow water also indicates infiltration of shallow groundwater into the deeper coal seam bearing Gondwana aquifers, which helps to increase inflow of mine water.

The relatively high Na concentration of coal mine water indicates that the mine water is recharged from overlying shallow groundwater aquifers moving slowly downward through the Gondwana aquifers promoting dilution of Na-rich minerals. Meanwhile, slightly higher Ca²⁺ concentration of coal mine water indicates insufficient base exchange reactions of surface water inflowing into the coal mine and thus Ca²⁺ does not adsorbed enough onto clays within the sediments in exchange for Na, and the insignificant cation exchange implies relatively short travel path of recharging water as well as short residence time. Strong positive correlation between Ca²⁺ and HCO₃ ^– indicates that the groundwater in Dupi Tila aquifer moves downward through the Gondwana aquifer with minor dissolution of calcite giving rise to low C^a+ concentration due to relatively short residence times of the inflowing mine water within the aquifer systems. Compared to observed groundwater, relatively low HCO₃ ^– concentrations of coal mine water attributes lack of CO₂ present (confined aquifer) resulting loss of HCO₃ ^– and it indicates that the coal mine inflow waters are mainly recharged by the overlying shallower Dupi Tila aquifer.

The clustering of groundwater, mine water and river water samples close to the LMWL indicates a common origin for aforesaid water samples, and provides compelling evidence that the observed groundwater and mine water are derived from local rainfalls with insignificant localized evaporation effect. Besides, the similarity between the average d¹⁸O composition of groundwater and the mine water indicates that the groundwater percolates in to the underlying coal seam bearing Gondwana aquifers without changing infiltrating groundwater d¹⁸O compositions. The low tritium content of shallow groundwater and coal mine water indicates relatively large travel times in the overlying Madhupur clay zone. The groundwater and mine water with a tritium value <1 TU could be considered as old water recharged prior to 1952. Finally, it can be concluded that the origin of Barapukuria coal mine inflow water is from the Dupi Tila aquifer recharged by local rainfalls which have been recharged within the aquifers prior to 1952.

Acknowledgement

The first author would like to acknowledge the Ministry of Education, Culture, Sports Science and Technology (MEXT), Japan for providing funds for Doctor of Science research during 2005 to 2008. The authors are thankful to the Barapukuria Coal Mine authority for their support during mine water sampling.

References

1. Islam MR, Hayashi D. Geology and coal bed methane resource potential of the Gondwana Barapukuria Coal Basin, Dinajpur, Bangladesh. Intl J Coal Geol. 2008; 75: 127-143.
2. Kibria MG, Quamruzzaman C, Woobaid Ullah ASM, Kabir AKMF. Effect of longwall mining on groundwater for underground coal extraction in Barapukuria, Bangladesh. J Mines, Metals & Fuels IP / DG / M-MA / F/. 2012; 18.5.12: 60-66.
3. Howladar MF, Deb PK, Muzemder ATMSH, Miah MI. An Assessment of the Underground Roadway Water Quality for Irrigation Use around the Barapukuria Coal Mining Industry, Dinajpur, Bangladesh. International Conference on Mechanical, Industrial and Energy Engineering. 2014.
4. Halim MA, Majumder RK, Zaman MN, Hossain S, Rasul MG, Sasaki K. Mobility and impact of trace metals in Barapukuria coal mining area, Northwest Bangladesh. Arab J Geosci. 2013; 6: 4593-4605.
5. Halim MA, Majumder RK, Zaman MN. Paddy soil heavy metal contamination and uptake in rice plants from the adjacent area of Barapukuria coal mine, northwest Bangladesh. Arab J Geosci. 2014; 8: 3391-3401.
6. Parizi HS, Samani N. Environmental Isotope Investigation of Groundwater in the Sarcheshmeh Copper Mine Area, Iran. Mine Water Environ. 2014; 33: 97-109.
7. Fantong WY, Satake H, Aka FT, Ayonghe SN, Asai K, Mandal AK, Ako AA. Hydrochemical and isotopic evidence of recharge apparent age and flow direction of groundwater in the Mayo Tsanaga River Basin Cameroon: bearings on contamination. Environ Earth Sci. 2010; 60: 107-120.
8. Matter JM, Waber HN, Loew S, Matter A. Recharge areas and geochemical evolution of groundwater in an alluvial aquifer system in the Sultanate of Oman. Hydrogeol J. 2005; 14:203-224.
9. Morton KL, Mekerk FA. A phased approach to mine dewatering. Mine Water Environ. 1993; 12: 27-33.
10. Girard P, Hillaire-Marcel C, Oga MS. Determining the recharge mode of sahelian aquifers using water isotopes. J Hydrol. 1997; 197:189-202.
11. Geirnaert W, Groenand M, Van der Sommen J. Isotope studies as a final stage in groundwater investigations on the African shield. In: Challenges in African hydrology and water resources. IAHS publication, Harare. 1984; 144: 141-153.
12. Majumder RK, Halim MA, Saha BB, Ikawa R, Nakamura T, Kagabu M, Shimada J. Groundwater flow system in Bengal Delta, Bangladesh revealed by environmental isotopes. Environ Earth Sci. 2011; 64: 1343-1352.
13. Fritz P, Hennings CS, Suzuki O, Salari E. Isotope hydrology in northern Chile. In: International Atomic Energy Agency (ed) Isotope hydrology. Vienna, Austria. 1979; 525-544.
14. Das BK, Kakar YP, Moser H, Stichler W. Deuterium and oxygen-18 studies in groundwater of the Dehli area. India J Hydrol. 1988; 98: 133-146.
15. Leontiadias IL, Payne BR, Christodoulou T. Isotope hydrology of the Aghios Nikolaos area of Crete, Greece. J Hydrol. 1988; 98: 121-132.
16. Fontes JC. Environmental isotopes in groundwater hydrology. Fritz P, Fontes JC, editors. In: Handbook of environmental isotope geochemistry. Elsevier, Amsterdam. 1980; 75-140.
17. Gat JR. The isotopes of hydrogen and oxygen in precipitation. Fritz P, Fontes JC, editors. In: Handbook of environmental isotope geochemistry. Elsevier, New York. 1980.
18. Majumder RK. Groundwater flow systems of Bengal Delta, Bangladesh, revealed by environmental isotopes and hydrochemistry (unpublished D.Sc. Thesis, Kumamoto University, Japan). 2008.
19. Dassi L, Zouari K, Seiler KP, Faye S, Kamel S. Flow exchange between the deep and shallow groundwaters in the Sbeitla synclinal basin (Tunisia): an isotopic approach. Environ Geol. 2004; 47: 501-511.
20. Rahman A. Geology of Madhyapara Area, Dinajpur District, Bangladesh. Rec. Geol. Surv. Bengal. 1987; 5.
21. Khan FH. Geology of Bangladesh, University Press Limited, Dhaka, Bangladesh. 1991.
22. Wardell A. Techno-economic feasibility study, Barapukuria coal project, Dinajpur District, Bangladesh. 1991; 1.
23. Bakr AM, Rahman QMA, Islam MM. Barapukuria coal deposit, Parbatipur Upazilla, Dinajpur District. Records of the Geological Survey of Bangladesh. 1986; 2: 35.
24. Uddin MN, Islam S. Gondwana basins and their coal resources in Bangladesh (Abst.). First South Asia Geol Congr Pakistan. 1992; 30.
25. CMC. Preliminary Geology and Exploration Report of Barapukuria Coal Mine, Bangladesh. 1994.
26. Majumder RK, Halim MA, Shimada J, Saha BB, Zahid A, Hasan MQ, et al. Hydrochemistry and isotopic studies to identify Ganges River and riverbank groundwater interaction, southern Bangladesh. Arab J Geosci. 2013; 6: 4585-4591.
27. Halim MA, Majumder RK, Rasul G, Hirosiro Y, Sasaki K, Shimada J, Jinno K. Geochemical Evaluation of Arsenic and Manganese in Shallow Groundwater and Core Sediment in Singair Upazila, Central Bangladesh. Arab J Sci Engin. 2014; 39: 5585-5601.
28. Coplen TB. New guidelines for reporting stable hydrogen, carbon, and oxygen isotope-ratio data. Geoch et Cosmoch Acta. 1996; 60: 3359-3360.
29. Craig H. Isotopic Variations in Meteoric Waters. Science. 1961; 133: 1702-1703.
30. Solomon DK, Cook PG. ³H and ³He. In: Cook P, Herczeg AL (eds). Environmental tracers in subsurface hydrology. Kluwer Academic, Boston. 1999; 397-424.
31. Yokoyama T. A temperature analysis of groundwater flow system in the upper part of the Ashigara plain, Tracers in Hydrology (Proc of the Yokohama Symp, July 1993). IAHS. 1993; 215.
32. Piper AM. A graphic procedure in geochemical interpretation of water analysis, American Geophysics Union. Transactions. 1944; 25: 914-923.
33. Soulsby C, Chen M, Ferrier RC, Helliwell C, Jenkins A, Harriman R. Hydrogeochemistry of shallow groundwater in an upland Scottish catchment. Hydrol Proce. 1998; 12: 1111–1127.
34. Aston TRC. Technical Note Tritium Dating of Water Inflows at the Donkin-Morien Project, Nova Scotia. Intl J of Mine Water. 1985; 4: 41-52.
35. Appelo CAJ, Postma D. Geochemistry, groundwater and pollution, 2^nd edition. AA Balkema, Rotterdam, 2005.
36. James ER, Manga M, Rose TP, Hudson GB. The use of temperature and the isotopes of O, H, C, and noble gases to determine the pattern and spatial extent of groundwater flow. J Hydrol. 2000; 237: 100-112.
37. Taniguchi M. Evaluation of vertical groundwater fluxes and thermal properties of aquifers based on transient temperature-depth profiles. Water Res. 1993; 29: 2021-2026.
38. Kabir SM. Subsurface temperature and geothermal gradient in Bangladesh. Dhaka University, Department of Geology, MS thesis (unpubl). 2008.
39. Vermeulen PD, Burger M, Wyk Avan, Lukas E. Using Environmental Isotopes in a Coal Mine and a Gold Mine to Determine Groundwater Interaction. Mine Water Environ. 2014; 33: 15-23.
40. Eby GN. Principles of environmental geochemistry. Thomson Brooks/Cole, Pacific Grove. 2004.
41. Hodgson FDI, Krantz RM. Investigation into the groundwater quality deterioration in the Olifants River catchment above the Loskop dam with specialised investigation into the Witbank dam sub-catchment. Inst for Groundwater Studies, Univ of the Free State, Bloemfontein. 1995.
42. Halim MA, Majumder RK, Nessa SA, Hiroshiro Y, Uddin MJ, Shimada J, et al. Hydrogeochemistry and arsenic contamination of groundwater in the Ganges Delta Plain, Bangladesh. J Hazard Mater. 2009; 164: 1335-1345.
43. Halim MA, Majumder RK, Nessa SA, Hiroshiro Y, Sasaki K, Saha BB, et al. Evaluation of processes controlling the geochemical constituents in deep groundwater in Bangladesh: Spatial variability on arsenic and boron enrichment. J Hazard Mater. 2010, 180: 50-62.
44. Vermeulen PD, Usher BH. Sulphate generation in South Africa underground and opencast collieries. Environ Geol. 2006; 49: 552-569.
45. Mukherjee A, Fryar AE. Deeper groundwater chemistry and geochemical modeling of the arsenic affected western Bengal basin, West Bengal, India. Appl. Geochem. 2008; 23: 863-894.
46. Mapoma HWT, Xie X, Pi K, Liua Y, Zhua Y. Understanding arsenic mobilization using reactive transport modeling of groundwater hydrochemistry in the Datong basin study plot, China. Environ. Sci. Processes Impacts. 2016; 18: 371.
47. Drever JI. The geochemistry of natural waters. Prentice Hall, Englewood Cliffs. 1988.
48. Kinniburgh DG, Smedley PL. Arsenic Contamination of Groundwater in Bangladesh, vol. 2. Technical Report WC/00/19, British Geological Survey. 2001; 267.
49. Ueno N. Social scientific village research at Samta. In: Abstract of the 5^th Forum on Arsenic Contamination of Groundwater in Asia, Yokohama. 2000; 27-36.
50. Freeze RA, Cherry JA. Groundwater. Prentice-Hall, Englewood Cliffs. 1979; 604.
51. Gaillardet J, Dupre B, Louvat P, Allegre CJ. Global silicate weathering and CO consumption rates deduced 2 from the chemistry of large rivers. Chem Geol. 1998; 159: 3-30.
52. Taylor SR, McLennan SM. The Continental Crust: its Composition and Evolution. Blackwell, London. 1985; 321.
53. Stallard RF, Edmond JM. Geochemistry of the Amazon 2. The influence of geology and the weathering environment on the dissolved load. J Geophy Res. 1983; 88: 9671-9688.
54. Stallard RF, Edmond JM. Geochemistry of the Amazon 3. Weathering chemistry and limits to dissolved inputs. J Geophy Res. 1987; 92: 8293-8302.
55. Monjerezi M, Vogt RD, Aagaard P, Gebru AG, Saka JD. Using 87Sr/86Sr, d¹⁸O and d²H isotopes along with major chemical composition to assess groundwater salinization in lower Shire valley, Malawi. Appl Geochem. 2011; 26: 2201-2214.
56. Mapoma HWT, Xie X, Zhang L. Redox control on trace element geochemistry and provenance of groundwater in fractured basement of Blantyre, Malawi. J Afr Earth Sci. 2014; 100: 335-345.
57. Mapoma HWT, Xie X, Zhu Y, Liu Y, Sitolo-Banda GC. Trace element geochemical evolution and groundwater origin in North Rukuru–Songwe alluvial aquifer of northern Malawi. Environ Earth Sci. 2016; 75: 877.
58. Lambs L, Balakrishna K, Brunet F, Probst JL. Oxygen and hydrogen isotopic composition of major Indian rivers: a first global assessment. Hydrol Proce. 2005; 19: 3345-3355.
59. Cowie R, Williams MW, Wireman M, Runkel RL. Use of Natural and Applied Tracers to Guide Targeted Remediation Efforts in an Acid Mine Drainage System, Colorado Rockies, USA. Water. 2014; 6: 745-777.

Download PDF

Citation: Majumder RK and Shimada J. Hydrochemistry and Environmental Isotopes to Identify the Origin of Barapukuria Coal Mine Inflow Water, Northwestern Bangladesh. Austin J Hydrol. 2016; 3(1): 1019. ISSN : 2380-0763

Home

Journal Scope

Online First

Current Issue

Editorial Board

Instruction for Authors

Submit Your Article

Contact Us