Impact of local recharge on arsenic concentrations in shallow aquifers inferred from the electromagnetic conductivity of soils in Araihazar, Bangladesh

The high-degree of spatial variability of dissolved As levels in shallow aquifers of the Bengal Basin has been well documented but the underlying mechanisms remain poorly understood. We compare here As concentrations measured in groundwater pumped from 4700 wells <22 m (75 ft) deep across a 25 km2 area of Bangladesh with variations in the nature of surface soils inferred from 18,500 measurements of frequency domain electromagnetic induction. A set of 14 hand auger cores recovered from the same area indicate that a combination of grain size and the conductivity of soil water dominate the electromagnetic signal. The relationship between pairs of individual EM conductivity and dissolved As measurements within a distance of 50 m is significant but highly scattered (r2 = 0.12; n = 614). Concentrations of As tend to be lower in shallow aquifers underlying sandy soils and higher below finer-grained and high conductivity soils. Variations in EM conductivity account for nearly half the variance of the rate of increase of As concentration with depth, however, when the data are averaged over a distance of 50 m (r2 = 0.50; n = 145). The association is interpreted as an indication that groundwater recharge through permeable sandy soils prevents As concentrations from rising in shallow reducing groundwater

Chapter 14 Electrical Properties of Soils

This chapter discusses the electric and electromagnetic methods that are used to evaluate the electrical properties of soils. Electric techniques exploit the flow of a steady-state current in the subsurface, while electromagnetic methods rely on the phenomenon of electromagnetic induction and the wave character of the electromagnetic field. The electrical techniques and associated properties are: (a) spontaneous potential methods in which the formation of water resistivity is determined; (b) resistivity methods in which the apparent resistivity can be calculated using Wenner, Schlumberger, and dipole-dipole arrays; and (c) specific conductivity methods in which the soil-specific conductivity is calculated by incorporating in the analysis of soil geometric factors, such as fabric anisotropy, tortuosity, resistance to solid matrix, bulk fluid phase, and electric double layer. Various parameters that influence the measured electrical properties are also presented, such as the nature of the soil composition (particle size distribution, mineralogy), soil structure (porosity, pore size distribution, connectivity, and anisotropy), moisture content, temperature, concentration of dissolved species in the pore-solution, wet-dry cycles, age of contaminants, and mineral formation due to biodegradation. Finally, the extraction of aquifer hydraulic properties such as porosity and hydraulic conductivity, from the measured electrical properties is discussed

Application of ground-penetrating radar to determine the thickness of Pleistocene periglacial slope deposits

Wide areas of the mountainous regions of Germany have rock covered by Pleistocene periglacial slope deposits (PPSD), formed by gelifluction during the cold periods of the ice ages in non‐glaciated areas. The PPSD provide the parent material for soil development, and their physical characteristics affect several stabile soil properties. Because the PPSD play a significant ecological role, we studied the spatial distribution and properties of the PPSD in order to assess the distribution of the stabile soil properties. The high stone content of the PPSD greatly hinders augering and digging. Hence, we tested the use of ground‐penetrating radar (GPR) as a potentially time‐saving, non‐destructive method to determine the thickness of the PPSD. In several study areas of the Rhenish Massif, GPR investigations of single soil profiles and soil transects along an exposed gas‐pipeline ditch were carried out. The GPR images were compared to the actual thickness of the layers of the PPSD exposed in the profiles and the ditch. In the GPR images usually at least one distinct boundary could be identified, which occurs at the transition between the loose material and the hard rock, mostly ranging between 50 and 150 cm depth. In some cases, in which stone content changed abruptly between different layers of the PPSD, also the boundaries between these layers could be identified in the GPR image. On the other hand, in areas where remnants of the Mesozoic‐Tertiary weathering mantle are preserved, the boundary between the saprolite and the overlying basal layer of the PPSD is ambiguous or not at all visible