Abstract

ABSTRACT Thirty groundwater samples were collected from wells tapping Samalut fractured carbonate aquifer in the Eastern Desert fringes of the Nile Valley in Minia. The results show a wide variation of groundwater salinity and the graphical presentation of major ion concentrations reflecting variable sources and complex mixing. The inverse evolution modelling shows that the dedolomitization, dissolution of calcite, ion exchange, pyrite and gypsum dissolution are the main mineral–solution interactions controlling the groundwater chemical evolution along flow paths. This study provides evidence on the occurrence of recharge of Samalut aquifer from both the Nile and local floods.

Highlights

  • Egypt lies in east Sahara which is the driest part on the planet

  • The concentrations of Ca+2, Mg+2, Na+, K+, SO−2, Cl−, PO4−3 and NO3− were estimated using a Thermo Scientific Ion Chromatograph (IC), model Dionex, ICS-1100. These analyses were conducted at Laboratories of the Desert Research Centre (DRC) in Cairo, Egypt, according to the methods adopted by the US

  • If the recharge occurs from the current Nile, it must mix with another water of isotopic signature similar to that of the rainwater at Alexandria

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Summary

Introduction

Egypt lies in east Sahara which is the driest part on the planet. Life in Egypt depends mainly on Nile water running from the Ethiopian and central African plateaus. 30°43ʹ15”E and 31°30ʹE and Lat. 27°42ʹ7”N and 28°41ʹ30”N (Figure 1) This area is a part of the western rims of AlMa’aza Plateau being bounded from the west by the Nile floodplain. A flash flood of 18.5 mm3/day intensity occurred in November 1994 (EGSMA 1994 and Ashmawy 2002). Based on groundwater levels and salinity distribution, many previous studies show that Samalut aquifer is recharged from the local rainfall, the Nile Irrigation System and the percolation of excess irrigation water The stable isotopes show that the recharge of the Samalut aquifer from the Nile occurred only in the flood season before the construction of the High Dam and ceased after it (Figure 1)

Methodology
Hydrogeologic setting
Water table conditions
Mineralogical associations
Impact of groundwater temperature on its salinity
Depth to water and groundwater temperature
Groundwater flow direction and relation to the Nile
Groundwater salinity distribution
Water level–Salinity relationship
Major ion recharge indicators
Inverse hydrogeochemical modelling
Sources of recharge
Halite dissolution
Conclusions
Disclosure Statement
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