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• W2336729659 abstract "Berghan Spring is located in the southern part of Iran, northwest of Shiraz. The catchment area of the spring consists of the southern flank of the Gar Anticline, which is made up of the karstic calcareous Sarvak Formation. There are no sinkholes or other karst landforms in the catchment area. Because of the existence of several faults, the aquifer has been brecciated and may have caused karstification to occur in most of the pores and fissures. The specific conductance, pH and water temperature were measured once every twenty days for a period of 32 months and water samples were analyzed for major anions and cations. Flow rate was measured daily during the recession, and once every three weeks during the rest of the study period. Using the WATEQF computer model, the partial pressure of carbon dioxide and the saturation index of calcite and dolomite also were estimated. Three distinct periods, the first recession, the second recession, and precipitation, were observed in the hydrograph of Berghan Spring. No considerable differences were observed between the first and second recession coefficients. Base flow constitutes 71.5%, 100% and 66.2% of total flow in the first recession period, the second recession period and the precipitation period, respectively. The variation of specific conductance, calcium and bicarbonate concentrations and calcite saturation indices are not significant during the study period, implying that aquifer characteristics control the chemical behavior of the spring. The morphology and geology of the Berghan Spring catchment area, and data from hydrographs and chemographs, show that the hydrologic system is dominantly diffuse flow. Evidence for this is shown by autogenic recharge, a brecciated aquifer, and small values and slight differences in hydrograph recession coefficients. In addition, specific conductance, calcium and bicarbonate concentrations, and water temperature did not show significant variations during the study period suggesting a diffuse flow aquifer. Studies have been conducted during the last three decades on the variations of physical and chemical properties of springs in order to understand the hydrogeological behavior of karst aquifers. Such studies generally began with the work of Garrels and Christ (1965) in which underground flow in carbonate rocks was divided into open and closed systems. In an open system, there is no limit on the amount of carbon dioxide available for the dissolution of calcium carbonate, whereas in a closed system, once the available carbon dioxide is used up, the dissolution of limestone terminates. Zotl (1960), and Smith and Mead (1962) used the time variations of chemical parameters to identify hydrogeological characteristics of karstic aquifers. White and Schmidt (1966) and White (1969) divided the flow in karstic aquifers into conduit and diffuse systems, based on spring behavior. Shuster and White (1971) made the same division based on time variations of temperature, specific conductance, and calcium, magnesium, and bicarbonate concentration. Newson (1972) and Ternan (1972) confirmed this division. Jacobson and Langmuir (1974), in their studies in Pennsylvania, divided karst flow systems into conduit, diffuse-conduit, and diffuse. In a diffuse system, laminar flow occurs through interconnected fissures smaller than one centimeter. In this type of system springs are generally numerous and have small discharges. Diffuse flow is relatively uniform through the aquifer and there is small variation of physical and chemical properties in the springs. A diffuse system is mostly fed directly from carbonate rocks and the soil covering these rocks. The coefficient of variation of total hardness in diffuse flow is less than 5% and few karst geomorphological features are present in the catchment area of these springs. Turbulent flow occurs in conduits ranging from one centimeter to more than one meter and the groundwater generally discharges through one large spring. Specific conductance and other physical and chemical properties are non-uniform in conduit systems. Conduit systems are fed through sinkholes and solutional joints in bare rocks. The coefficient of variation of total dissolved solids ranges from 10 to 24%. Bakalowicz (1977) suggested that the structure of a karst aquifer cannot be defined from the coefficient of variation of chemical variables, as was suggested by Shuster and White (1971). Atkinson (1977) also noted that the very small range in calcium carbonate concentration in resurgences from the Mendip Hills, England, would suggest that they are diffuse flow springs according to Shuster and White’s criteria, yet are known to be fed largely by conduit flow. He concluded that flow in carbonate aquifers is a combination of diffuse and conduit systems and divided them into “quick” flow and “slow percolation” flow according to velocity. Scanlon and Thrailkill (1987), using the suggested criteria by previous workers, carried out a comprehensive study of conduit and diffuse regimes in the Inner Bluegrass of central Kentucky. Their results were not consistent with those of previous workers and indicated that spring water chemistry could not be related to the physical characteristics of karst aquifers in this area. Raeisi et al. (1993) attempted to determine the Sheshpeer" @default.
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• W2336729659 title "HYDROCHEMOGRAPHS OF BERGHAN KARST SPRING AS INDICATORS OF AQUIFER CHARACTERISTICS" @default.
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