The steady-state height of water in a one-dimensional, unconfined groundwater aquifer (as shown in Figure 2) can be modeled with the nonlinear ODE di (Khen) + N = 0, (6) where x is the distance (m), K is hydraulic conductivity (m/d), h is the height of the water table (m), and N is infiltration rate (m/d). Given the domain and conditions x = 0 to 1000 m with h(0) = 10 m, h(1000) = 5 m, K = 1m/d, and N = 0.0001 m/d: (a) Solve for the water height using the shooting method (use ode45 to integrate). Ground surface Infiltration h Water table Aquifer Groundwater flow Confining bed Figure 2: An unconfined groundwater aquifer (b) Solve for the water height using the finite-difference method (Ax = 10 m). The steady-state height of water in a one-dimensional, unconfined groundwater aquifer (as shown in Figure 2) can be modeled with the nonlinear ODE di (Khen) + N = 0, (6) where x is the distance (m), K is hydraulic conductivity (m/d), h is the height of the water table (m), and N is infiltration rate (m/d). Given the domain and conditions x = 0 to 1000 m with h(0) = 10 m, h(1000) = 5 m, K = 1m/d, and N = 0.0001 m/d: (a) Solve for the water height using the shooting method (use ode45 to integrate). Ground surface Infiltration h Water table Aquifer Groundwater flow Confining bed Figure 2: An unconfined groundwater aquifer (b) Solve for the water height using the finite-difference method (Ax = 10 m)