understood. Unconfined aquifer tests were known to experience slower drawdown than confined tests, due to water supplied by dewatering the zone near the water table, which is related to the formation specific yield (porosity less residual water). @muskat1934transient and [@hurst1934unsteady] derived solutions to confined transient radial flow problems for finite domains, but attributed transient storage solely to fluid compressibility. @jacob1940 derived the diffusion equation for groundwater flow in compressible elastic confined aquifers, using mass conservation and Darcy’s law, without recourse to analogy with heat conduction. @terzaghi1923 developed a one-dimensional consolidation theory which only considered the compressibility of the soil (in his case a clay), unknown at the time to most hydrologists [@batu1998aquifer]. @meinzer1928 studied regional drawdown in North Dakota, proposing the modern storage mechanism related to both aquifer compaction and the compressiblity of water. @jacob1940 formally showed $S_s=\rho_w g(\beta_p + n\beta_w)$, where $\rho_w$ and $\beta_w$ are fluid density \[M/L$^3$\] and compressibility \[LT$^2$/M\], $n$ is dimensionless porosity, and $\beta_p$ is formation bulk compressibility. The axis-symmetric diffusion equation in radial coordinates is $$\label{diffusion}
  \frac{\partial ^2 s}{\partial r^2}+\frac{1}{r}\frac{\partial
    s}{\partial r}=
  \frac{1}{\alpha_s}\frac{\partial s}{\partial t}.$$

When deriving analytical expressions, the governing equation is commonly made dimensionless to simplify presentation of results. For flow to a 