Recently, these properties have been also determined using remote sensing data derived from Interferometric synthetic-aperture radar.
The specific storage is the amount of water that a portion of an aquifer releases from storage, per unit mass or volume of the aquifer, per unit change in hydraulic head, while remaining fully saturated.
Aquifer-test analyses provide estimates of aquifer-system storage coefficients by examining the drawdown and recovery responses of water levels in wells to applied stresses, typically induced by pumping from nearby wells.
[4] Elastic and inelastic skeletal storage coefficients can be estimated through a graphical method developed by Riley.
[5] This method involves plotting the applied stress (hydraulic head) on the y-axis against vertical strain or displacement (compaction) on the x-axis.
The inverse slopes of the dominant linear trends in these compaction-head trajectories indicate the skeletal storage coefficients.
[9] The inelastic skeletal specific storage of the sample can be determined by calculating the ratio of vertical hydraulic conductivity to the coefficient of consolidation.
Simulations of land subsidence incorporate data on aquifer-system storage and hydraulic conductivity.
Calibrating these models can lead to optimized estimates of storage coefficients and vertical hydraulic conductivity.
Specific yield can be close to effective porosity, but there are several subtle things which make this value more complicated than it seems.
Also, the value of specific yield may not be fully realized for a very long time, due to complications caused by unsaturated flow.
Problems related to unsaturated flow are simulated using the numerical solution of Richards Equation, which requires estimation of the specific yield, or the numerical solution of the Soil Moisture Velocity Equation, which does not require estimation of the specific yield.