Received 28 December 2015; accepted 26 January 2016; published 29 January 2016
Descriptions of unusually high waves appearing on the sea surface for a short time (freak, rogue or killer waves) have been considered as a part of marine folklore for a long time. A number of instrumental registrations have appeared recently making the community to pay more attention to this problem and to reconsider known observations of freak waves whose existences are now universally recognized  - . Furthermore, images on the extent of damage caused by these monsters of the ocean are available. However, the physics of processes responsible for the formation (or origin) and propagation of these phenomena as well as their prediction is not completely understood. Contrary to developed country researchers’ opinion, physics of spectacular phenomenon like rogue waves is not easily obtainable by the only use of advance data provided by high technology equipment like: Powerful Computers; sophisticated WIS (Weather Information Systems); Wind’s Profilers; Radar Drones; Lidar Drones; Satellites; etc. Indeed, rogue waves are a combination of multi-spectral processes that occur under the thermodynamic and dynamic accuracy conditions. Mathematical models  - offer more tremendous opportunities for understanding of the systems whose physics is, at the present level of our knowledge, difficult to obtain. To allow a better understanding of the behavior of rogue waves triggered by winds in terms of their origin and spatiotemporal evolution, that is, their motion and also in terms of mechanical transformations that these systems may suffer in their dealings with other systems, the standard nonlinear Schrödinger equation of off balance systems is implemented in the specific case of waves driven by wind and gravity forces. A mathematical model based on Navier-Stokes and Euler Lagrange equations coupled with assumptions derived from the literature on the nature of the training locations (or birth places) of rogue waves is developed to enhance the wind and gravity force effects on the behavior of surface waves. Given the complexity of the process to be studied, it seemed necessary for us to make a use of modulational instability theories such as the standard NLSE in order to better understand the contribution of wind and water viscosity to modulations of driven waves’ amplitudes (or phases): modulations which sometimes can accidentally trigger unpredictable rogue waves.
2. Navier-Stokes and Euler Lagrange Equations
The general fluid continuity equation is given by:
This leads to the continuity equation for an incompressible fluid
The kinematic boundary conditions
, at and (3)
where is the unit vector normal to the boundary surfaces and is the sea surface elevation. Hence:
Equation of motion in natural coordinates
According to (5): solutions of the equation of motion depends mainly on pressure P (closely related to the prevailing winder over the ocean); gravity g and water viscosity (n). Only mathematical models (theories) that incorporate best these different parameters will next be considered.
3. Weakly Nonlinear Approach: The Nonlinear Schrödinger Equation
Under the effects of wind and gravity, the wave moves through successive deformations of its surface (Figure 1). This situation is perfectly described by the Nonlinear Schrödinger Equation (NLSE) which can be obtained from the fully nonlinear potential theory by using the multi-scale method  -  . The Taylor developing-series allows the NLSE to be expanded around a small wave steepness ε. Thereafter, the equation obtained is a third order in ε approximation of the system formed by equations 1 to 4. To investigate both damping and amplification effects on the Benjamin-Feir instability, we have use the forced and damped nonlinear Schrödinger equation (fdNLSE),
Herein, represents the wind effect, is the group velocity of the carrier wave and ν, ρ, ρair, g, u∗, and k are well-known parameters  -  . Equation (6) describes the spatial and temporal evolution of the envelope of the surface elevation, for weakly nonlinear and dispersive gravity waves on deep water when dissipation (due to viscosity), and amplification (due to wind), are considered. If considering the right hand side of this equation, it can be rewritten as
The stability of the envelope depends on the sign of K. For values of K ˂ 0, solutions are found to be stable, while for values of K ≥ 0, solutions are unstable. Physically, they interpreted this result in terms of frequency of the carrier wave ω0 and friction velocity u∗ of the wind over the waves. We plotted (Figure 2 & Figure 3) the critical curve separating stable envelopes from unstable envelopes. Namely, they showed that for a given friction velocity u∗, only carrier wave of frequency ω0 which satisfies the following condition are unstable to modulational perturbations
Figure 1. Driven wave’s velocity profile  .
Figure 2. Growth rate versus of the wave number of the perturbation k for positive values of K (A0 = 0.2 and θ = 35).
Figure 3. Growth rate versus of the wave number of the perturbation k for negative values of K (A0 = 0.2 and θ = 35).
We can transform this Equation (8) to have a standard nonlinear Schrödinger equation in 3D.
And then introduce an oblique coordinates (S) associated with the direction of the spatial modulation
Substuting Equation (10) and (9) in (8) we obtain:
K values are very small and this make possible to do Taylor expansion in first order of and obtain (12)
Moving from the NLS equation to the standard NLS become possible if is a linear
function in T. We can therefore consider the following new variable:
As said before, wave trains are unstable to small perturbation of other wave travelling in the same direction  . The standard stability analysis consist in linearizing around the monochromatic wave solution of the nonlinear Schrödinger equation
Here K and Ω referring respectively to the perturbation wave number and frequency of the perturbation amplitude. Substituting this equation in Equation (8) we obtain the growth rate of instability:
It is well known that one of the main effects of Modulational instability, which refers to the growth of certain modulation sideband of nonlinear plane waves propagating in a dispersive medium as deep water is a result of the interplay between nonlinearity, gravity and dispersion effects. In this case of forced/damped regime in deep water, instability is significantly influenced by K (Figures 4-9). It is seen that the growth rate increases (or decreases)
Figure 4. η = η(S) at: −100 ≤ t ≤ 100.
Figure 5. η = η(x, y) at: t = 0; ηmax = 1.8.
Figure 6. η = η(x, y) at: t = 10; ηmax = 2.0.
Figure 7. η = η(x, y) at: t = 25; ηmax = 4.0.
Figure 8. η = η(x, y) at: t = 35;.
Figure 9. η = η(x, y) at: t = 50;.
with the increasing (decreasing) values of forcing/damping coefficient K. It is evident to say that wind effect destabilize the wave train in deep water in two dimensional directions however the dissipation stabilize the wave train.
The upsurges of abnormally large waves on the sea surface are due to complex physical mechanisms. In this paper, we discuss the modulational instability scenario of a single freak wave formation in 3D (i.e., time-space scales). One of the important properties of an unstable wave packet is the growth rate. Small amplitude modulation theory for the NLS equation predicts a number of interesting features about the nonlinear propagation of initially small amplitude sine wave modulations. One of the most important is shown in Figures 5-7 where carrier-wave’s amplitude increases with respect to t (e.g., when comparing: to or. A later time after, the carrier wave’s amplitude modulation escapes from our prediction (we observe the upsurge of amplitude’s modulational instability. e.g., amplitude of the carrier wave at t = 35 (Figure 8) becomes lesser than amplitude of the same carrier wave at t = 50 (Figure 9) where 03 complete summits are observed). According to pertinent results obtained in this paper, wind alone cannot easily generate rogue waves; effect of winds combined with other physical mechanisms (e.g., viscosity and gravity force) may provide a fuller explanation of upsurge of freak wave phenomena. As wind blows over the ocean, its momentum is transferred to water molecules located at the surface of the sea. When strong winds (e.g., winds triggered by cyclones) blow in the opposing direction of the ocean current, its intensity might be strong enough to randomly generate rogue waves. Viscosity and gravity force contributions to the behavior of wind’s carrier waves are well described by our adopted weakly nonlinear approach and the related NLSE (Nonlinear Schrödinger Equation).
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