Isotope-based investigation on the groundwater flow and recharge mechanism in a hard-rock aquifer system: the case of Ranchi urban area, India

Groundwater recharge, flow and stable isotope attenuation in sedimentary and crystalline fractured rocks: Spatiotemporal monitoring from multi-level wells

“…The use of hydraulic responses alone, for example, may lead to the misinterpretation of hydraulic artifacts for recharge (Weeks, 2002). By coupling conservative tracers with water level measurements, however, a conceptual model can more accurately be constrained (Banks et al, 2011;Cook and Herczeg, 2000;Praamsma et al, 2009;Saha et al, 2013) Oxygen-18 and deuterium in precipitation are examples of conservative and stable tracers that have been used extensively within the field of hydrology to investigate complex systems (Banks et al, 2011;Cartwright et al, 2012;Clark and Fritz, 1997;Craig, 1961;Dansgaard, 1964;Doveri and Mussi, 2014;Ettayfi et al, 2012;Huijgevoort et al, 2016;Tweed et al, 2004;Zanini et al, 2000). The δ 18 O and δ 2 H values and temperature of snowmelt in particular can be a valuable tracer for revealing recharge and transport processes in fractured rock (Gleeson et al, 2009).…”

Determination of stable isotope characteristics and natural radioactivity in drinking waters in Sandıklı basin (Afyonkarahisar-Turkey)

“…8 Sub-modern (recharged prior to 1952) 0. Mixture of sub-modern and modern [5][6][7][8][9][10][11][12][13][14][15] Modern (<5-10 years) [15][16][17][18][19][20][21][22][23][24][25][26][27][28][29][30] Some bomb tritium present >30…”

Albitization of the granitic basement of the Guilleries and Roc de Frausa Massifs (NE Spain) in relationship to the Permian - Triassic palaeosurface

“…The negative δ 18 O values are the result of water-rock interaction reactions like precipitation of kaolinite from dissolved smectite and feldspars, and precipitation of Fe-hydroxides (Kloppmann et al, 2002). These negative δ 18 O shifting in groundwaters has been reported in the French Massif Central (Kloppmann et al, 2002), the Black Forest (Stober and Bucher, 1999b), the Alps (Barth, 2000) and the Fennoscandian and Ukrainian shields (Stober and Bucher, 1999a), the Canadian shield Fritz, 1982, 1987;Frape et al, 1984;Stober and Bucher, 1999a), the Ahaggar Massif and Dodoma area (Nkotagu, 1996;Saighi et al, 2001) in Africa, and the Ranchi area (Saha et al, 2013) in India. The systematic observation of negative δ 18 O in deep groundwater (Kloppmann et al, 2002) and the reasonable analogy between the current stable crystalline basements and the Permian-Triassic granitic basement support that the Permian-Triassic palaeogroundwater hosted in the granitoids of the Guilleries and Roc de Frausa Massifs may have presented negative δ 18 O values of the same magnitude in the range -8 to -12‰.…”