It is the soil’s hydraulic conductivity after the effect of fluid viscosity and density are removed. It is calculated as hydraulic conductivity (K) multiplied by the fluid viscosity divided by fluid density and the gravitational constant.

Hydraulic conductivity is a property of the soil, whether it is the (highly varying) hydraulic conductivity in the unsaturated zone or the saturated hydraulic conductivity in the saturated zone. The infiltration rate is the inflow into the soil, where the water movement in the vadose zone is the flow inside the soil.

The hydraulic conductivity K can be calculated through the analytical solution of equation (9): A = −C′Q2/4π2K2H02, where H0 is the hydraulic head in the pumping well (equal to 1.96); C′ is the slope factor of the linear relationship between self-potential and drawdown data in Figure 12 (until 0.4 m) and represents the …

Hydraulic conductivity is the ease with which water moves through porous spaces and fractures in soil or rock. It is subject to a hydraulic gradient and affected by saturation level and permeability of the material. Hydraulic conductivity is generally determined either through one of two approaches.

It’s critical to understanding the complete water balance and is also used for estimating groundwater recharge through the vadose zone. Hydrologists need hydraulic conductivity values for modeling, and researchers use it to determine soil health or to predict how water will flow through soil at different field sites.

Hydraulic conductivity is the rate of flow under a unit hydraulic gradient through a unit cross-sectional area of aquifer (opening A). Transmissivity is the rate of flow under a unit hydraulic gradient through a unit width of aquifer of thickness m (opening B).

The hydraulic head is measured by determination of the vertical position of the water table in a well relative to a reference surface. Darcy’s law says that the discharge rate q is proportional to the gradient in hydrauolic head and the hydraulic conductivity (q = Q/A = -K*dh/dl).

Magnetic permeability is represented as μ (it is pronounced as mu) and can be expressed as μ = B/H, where, B is the magnetic flux density which is a measure of the actual magnetic field within a material and is considered as a concentration of magnetic field lines or magnetic flux per unit cross-sectional area.

Flux density is simply the total flux divided by the cross sectional area of the part through which it flows – B = Φ / Ae teslas. Thus 1 weber per square metre = 1 tesla. Flux density is related to field strength via the permeability. B = μ × H.

Magnetic permeability μ (Greek mu) is thus defined as μ = B/H. Magnetic flux density B is a measure of the actual magnetic field within a material considered as a concentration of magnetic field lines, or flux, per unit cross-sectional area.

1. n. [Geology] The measurement of the permeability, or ability to flow or transmit fluids through a rock, conducted when a single fluid, or phase, is present in the rock. The symbol most commonly used for permeability is k, which is measured in units of darcies or millidarcies.

The ratio of the magnetic flux density, B, to the magnetic field strength, H, at a point in a material medium, given by the relation μabs = B/H. See also incremental magnetic permeability, magnetic field strength, magnetic flux, magnetic flux density, magnetic permeability, relative magnetic permeability.

The relative saturations of the fluids as well as the nature of the reservoir affect the effective permeability. In contrast, absolute permeability is the measurement of the permeability conducted when a single fluid or phase is present in the rock.