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22 nd Salt Water Intrusion Meeting: Salt Water Intrusion in Aquifers: Challenges and PerspectivesFigure 2. Temporal evolution of heads in 3 control points. S.130 piezometer and S.40 piezometer at thedischarge zone, and R.1 well at the recharge zone. Time gaps are defined between R.1 and S.130 registers.Monthly accumulated River discharge is represented in vertical bars.The temporal evolution in both sectors follows a similar path, where the peaks detectedcorrespond to maximum and minimum of the aquifer recharge in this time interval. Comparingregistered heads in S.130 piezometer with R.1 well is observed a time gap regarding the rechargezone of about 30 days and 0.3 m of head oscillation. This gap is not detected in S.40, where theobserved variations are simultaneous with oscillations in R.1, but in this case, S.40 shows a lowerpiezometric level oscillation, with maximum of 0.6 m versus 1.5 m in R.1. The significantdifference in S.130 versus S.40 is mainly due to the different hydraulic potential that existsbetween them.The difference in hydraulic potential between them allows discern different groundwater flowpaths at the discharge zone. There are superficial flow lines where the variations of heads aresimultaneous with the variations in the recharge zone, up to 40 m deep at least. There are alsodeeper groundwater flow lines, with the same variations that we observed in the rechargezone, but with softer oscillation and time gap of about one month.3. CONCLUSIONSHeads in the discharge zone showed the same peaks that the recharge zone althoughthese oscillations are considerably softer and less immediate in the discharge zoneregarding the recharge zone These variations are related with changes of the aquiferrecharge, like modifications in the Guadalfeo River discharge.. However, comparing heads atboth sectors significant differences were observed. In heads measured at S.40, a directcorrelation is detected, without time gap regarding the recharge zone. In the deeperpiezometer (S.130) a similar trend was observed but with a time gap of 30 days. Thesedifferences indicate the existence of different scale flows in the aquifer, with different flow rateand residence time. The superficial groundwater flow (up to 40 m deep) is faster and with lowerresidence time and the variations are simultaneous with the recharge zone changes. The deepergroundwater flow (from 140 m onwards) is slower and with longer residence time.AcknowledgementsThis study was performed by funding from CGL2008-05016 funded by the Ministerio deCiencia e Innovación, the research group of the Junta de Andalucía RNM-369 andPostdoctoral Mobility Program Helps of the Ministerio de Educación.REFERENCESCalvache, M.L., Rubio J.C., López-Chicano M., González-Ramón A., Ibáñez S., Martín-Rosales W., Soler R., Díaz-Losada E. and Peinado-Parra T. (2003). Estado actual delacuífero costero Motril-Salobreña previo a la puesta en funcionamiento de la presa deRules (Granada, España); In: Simposio Internacional sobre Tecnología de la intrusión de agua demar en acuíferos costeros. IGME, Madrid, 77-8.238
22 nd Salt Water Intrusion Meeting: Salt Water Intrusion in Aquifers: Challenges and PerspectivesCalvache, M.L., Ibáñez, P., Duque, C., López-Chicano, M., Martín-Rosales, W., González-Ramón, A. and Rubio, J.C. (2009). Numerical modelling of the potential effects of a dam on acoastal aquifer in SE Spain. Hydrological Processes, 23, 1268-1281.Duque, C. (2009). Influencia antrópica sobre la hidrogeología del acuífero Motril-Salobreña.PhD thesis, University of Granada. 296 p.Duque, C., Calvache M.L., Pedrera A., Martín-Rosales W. and López-Chicano M. (2008).Combined time domain electromagnetic soundings and gravimetry to determine marineintrusion in a detrital coastal aquifer (Southern Spain). Journal of Hydrology, 349, 536-547.Duque, C., Calvache, M. L., López-Chicano, M., Pedrera, A. and Galindo-Zaldívar, J. (2011).Establecimiento preliminar de la posición de la interfase agua dulce-agua salada en elsector de la desembocadura del río Guadalfeo (acuífero Motril-Salobreña) mediantetécnicas geofísicas y registros de salinidad. Geogaceta, 50-1, pp. 75-78.Glover, R.E. (1959). The pattern of fresh-water flow in a coastal aquifer. Journal ofGeophysical Research, 64 (4), pp. 457-459.Hubbert, M. King, (1940). The theory of ground-water motion. Journal of Geology, 48(8), (PART 1), pp. 785-944.Kohout, F. A. (1964). The flow of fresh water and salt water in the Biscayne aquifer ofthe Miami area, Florida; In: Sea Water in Coastal Aquifers. U.S. Geological Survey Water-Supply Paper 1613-C, p. 12-32.López-Geta J. A., Gómez-Gómez J.D., (2007). La Intrusión Marina y su Incidencia enlos Acuíferos Españoles; In: Enseñanza de las Ciencias de la Tierra, (153) 266-273 I.S.S.N.:1132-9157.Martín Rosales, W., Duque, C., López-Chicano, M., Calvache, M. L., González-Ramón,A. and Rubio-Campos, J.C. (2008). Modificaciones recientes del régimen hidrológico en El ríoGuadalfeo (Granada); In: López-Geta, J.A., Rubio, J.C. y Martín-Machuca, M. (Eds.), VIISimposio del Agua en Andalucía. IGME, pp. 149-158.239
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SWIM22 - 22 nd Salt Water Intrusion
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Local Supporting Organizing TeamMar
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Peter StuyfzandKiwa Water Research,
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PrefaceWelcome to the 22 nd Salt Wa
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SUMMARYKeynote Lectures pg 13Coasta
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Groundwater hypersalinization in a
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Hydrostratigraphic Study of Itaipua
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Keynote Lectures
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Effects of sea levelrise and climat
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Hans Sulzbacher 1 ; Helga Wiederhol
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Resistivity [Ωm]0.1 1 10 100 10000
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2. METHODS Figure 1a.
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4. DISCUSSION AND CONCLUSIONSREFERE
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METHODS 51
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DISCUSSION AND CONCLUSIONS
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STUDY OF THE SALTWATER-FRESHWATER I
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Hydrogeochemical and isotopicmethod
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Figure 1 Location map of study area
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Therefore, it was clarified that th
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GROUNDWATER HYPERSALINIZATION IN A
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3. RESULTS AND DISCUSSIONS
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GROUNDWATER ARTIFICIAL RECHARGE IN
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