Figure 1: Definition sketch for the initial value
problem.

The nonlinear evolution of a wave over a sloping beach is
theoretically and numerically challenging due to the moving boundary
singularity. Yet, it is important to have a good estimate of the
shoreline velocity and associated runuprundown motion, since they
are crucial for the planning of coastal flooding and of coastal
structures. As explained in the previous section, Synolakis (1987)
solved this problem as a boundary value problem considering
canonical bathymetry. Kânoglu (2004) solved nonlinear
evolution of any given wave form over a sloping beach as an initial
value problem (Fig. 1). It is proposed that any
initial waveform can first be represented in the transform space
using the linearized form of the CarrierGreenspan transformation
for the spatial variable, then the nonlinear evolutions of these
initial waveforms can be directly evaluated. Later, Kânoglu
and Synolakis (2006) solved the similar problem considering a more
general initial condition, i.e., initial wave with velocity.
Kânoglu (2004) considers NSW equations () with
slightly different nondimensionalization than (), i.e.,
using the reference length as a scaling parameter,
the dimensionless variables are introduced as

(1) 
Using the original CarrierGreenspan transformationwithout coefficient in () and ()it is
possible to reduce the NSW equations to the following single
secondorder linear equation the same as ():

(2) 
using the Riemann invariants of the hyperbolic system (Carrier and
Greenspan, 1958). The CarrierGreenspan transformation not only
reduces the nonlinear shallow waterwave equations into a
secondorder linear equation, but also fixes the instantaneous
shoreline to in the
space as
explained previously. Furthermore, a bounded solution at the
shoreline combined with a given initial condition in terms of a wave
profile at in the space,
implies the following solution in the transform space,

(3) 
where
. Further, given the initial waveform
, the
evolution of the watersurface elevation is now given by
where, again,
Since it is important for coastal planning, simple expressions for
shoreline runuprundown motion and velocity are useful. Considering
the shoreline corresponds to in the space, (4) reduces to the following equation for the
runuprundown motion:
Here and represent shoreline velocity and
motion, respectively. The singularity of the
at the shoreline () is removed with the
consideration of the
The difficulty of deriving an initial condition in the space is overcome by simply using the linearized form of
the hodograph transformation for a spatial variable in the
definition of initial condition. It is proposed that any initial
waveform can first be represented in the transform space using the
linearized form of the CarrierGreenspan transformation for the
spatial variable (() without coefficient),
then the nonlinear evolutions of these initial waveforms can be
directly evaluated. Once an initial value problem is specified in
the space as , the linearized hodograph
transformation
is used directly to
define the initial waveform in the space,
. Thus
is found,
and
follows directly through a simple
integration, as in (4). Then it becomes possible to
investigate any realistic initial waveform such as Gaussian and
Nwave shapes employed in Carrier et al. (2003) and the
isosceles and general Nwaves defined by Tadepalli and Synolakis
(1994). Again, solution in the physical space can be found using the
NewtonRaphson algorithm proposed by Synolakis (1987) and later
used by Kânoglu (2004), as presented in (A24a, b).
The shoreline runuprundown motion and velocity are presented for
one of the initial profiles given by Carrier et al. (2003):

(6) 
The following initial profile can be obtained in the transform space
after using the linearized form of the transformation for the
spatial variable:

(7) 
which leads to the definition of the initial condition
:
Figure 2a compares the initial waveforms defined
in the physical space as in (6) with the one resulting
from the approximation of it, i.e., (calculated through
(4)). The linearized form of the spatial variable in the
definition of the initial waveforms gives satisfactory comparison.
Figures 2b and 2c present the
shoreline runuprundown motion and velocity, respectively,
calculated from equation (5) using the corresponding
parts. It should be added that the solution presented here cannot be
evaluated when the Jacobian of the transformation,
, breaks down. Even though
the transformation might become singular at certain points, the
solution can still be obtained at other points, since local
integration can be performed without prior knowledge of the
dependent variables, unlike in numerical methods. This feature is
discussed in detail in Synolakis (1987) and Carrier et al. (2003), and is not explained further in here.
Figure 2: (a) The leadingdepression initial waveform (6)
presented by Carrier et al. (2003) with = 0.006, = 0.4444, = 4.1209, = 0.018, = 4.0, and = 1.6384 (solid line) compared with the one resulting from
approximation (evaluated through (4)) (dots), (b)
shoreline wave height, and (c) shoreline
velocity.

References:
Carrier, G.F., T.T. Wu, and H. Yeh (2003): Tsunami runup and
drawdown on a sloping beach. J. Fluid Mech., 475, 7999.
Kânoglu, U. (2004): Nonlinear evolution and runuprundown
of long waves over a sloping beach. J. Fluid Mech., 513,
363372.
Kânoglu, U., and C. Synolakis (2006): Initial value problem
solution of nonlinear shallow waterwave equations. Phys.
Rev. Lett., 97, 148501148504.
