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Annali di Matematica Pura ed Applicata (1923 -)

, Volume 196, Issue 6, pp 2253–2260 | Cite as

Two-dimensionality of gravity water flows governed by the equatorial f-plane approximation

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Abstract

We show that gravity wave trains governed by the equatorial f-plane approximation propagate at the free surface of a rotational water flow of constant vorticity vector \((\Omega _1, \Omega _2, \Omega _3)\) over a flat bed only if the flow is two-dimensional. Owing to the presence of Coriolis effects, our result is also true even if the vorticity vector vanishes. This represents a striking difference when compared with the cases without geophysical effects discussed in Constantin (Europhys Lett 86:29001, 2009, Eur J Mech 30:12–16; 2011) and Martin (J Math Fluid Mech 2016. doi: 10.1007/s00021-016-0306-1), where the conclusion about the two-dimensionality of the flow was possible under the assumption of constant nonvanishing vorticity vector. Another upshot is that the only nonzero component of the vorticity that may not vanish is \(\Omega _2\), that is, the one pointing in the horizontal direction orthogonal to the direction of wave propagation.

Keywords

f-plane approximation Gravity wave trains Vorticity 

Mathematics Subject Classification

Primary 35Q31 35Q35 Secondary 35Q86 

1 Introduction

There is an increased interest nowadays in the study of geophysical water flows. These are flows whose motion is influenced by the Earth’s rotation reflected through the manifestation of the Coriolis force. The thorough understanding of geophysical flows is highly dependent upon inclusion of nonlinear aspects that considerably complicate the matter to the point of eluding exact treatment; this drawback is somehow mitigated by the discovery by Gerstner [17] who presented in 1802 the only known explicit exact solution (in Lagrangian variables) for the governing equations for periodic homogeneous two-dimensional traveling gravity water waves. Gerstner solution was extended in 1932 to a heterogeneous fluid by Dubreil-Jacotin [13]; we refer the reader to Constantin [1] and Henry [18] for modern presentations of the Gerstner wave solution.

The specific general difficulties raised by the nonlinear character of equations governing the water wave propagation are enhanced by the inclusion of the before mentioned Coriolis effects; especially the complex dynamics of flows near the equatorial Pacific presents some peculiarities like a strong stratification (evidentiated by the presence of an interface, called thermocline, separating two layers of constant density), the presence strong depth-dependent underlying currents, cf. [9], with flow reversal at a depth of about 100–200 m and a wide range of other wave propagation phenomena. The softening of these intricacies becomes possible through the employment of suitable approximations of the geophysical governing equations; one of these is the f-plane approximation which is appropriate for oceanic flows within a restricted meridional range of about \(2^{\circ }\) latitude from the Equator [9, 12, 21].

The rigorous mathematical study of geophysical water flows has resulted in the appearance of a bulk of papers commencing with the modeling of wave-current interactions in the f-plane approximation for underlying currents of constant vorticity, by Constantin [4] and with the derivation of an exact solution (in the Lagrangian framework) of the nonlinear geophysical water waves in the \(\beta \)-plane near the Equator by Constantin in [5] by a suitable and substantial modification of the Gerstner wave solution to the case of three-dimensional flows. These studies were followed by papers presenting explicit exact solutions describing flows accommodating flow reversal and allowing for underlying currents in the \(\beta \)-plane setting, cf. [7, 8, 19]. An additional aspect of centrifugal forces in the \(\beta \)-plane approximation was addressed recently by Henry in [22] where an exact and explicit solution describing equatorially trapped waves was obtained.

Circumscribed to the same vein of solution flows exhibiting a prefered direction of propagation are recent works describing oceanic flows propagating in an azimuthal direction and exhibiting a complicated vertical structure [10, 11, 25]. Such geophysical flows were also analyzed from the perspective of stability/instability properties [6, 16, 20, 23, 24].

Our intention here is to show that gravity wave trains can propagate at the free surface of a rotational water flow of constant vorticity and governed by the equatorial f-plane approximation only if the flow has a two-dimensional character. From a historical perspective, the property that the flow below a wave train does not vary in the horizontal direction perpendicular to the direction of motion was validated by previous works of Constantin and Kartashova [2] proving the two-dimensionality of constant vorticity water flows below wave trains driven by capillarity and of Constantin [3] showing the two-dimensionality of constant vorticity gravity flows below wave trains; see also the works of Wahlén [30] and Stuhlmeier [29], the latter in the case of solitary waves.

2 The governing equations

We choose a rotating framework with the origin at a point on the Earth’s surface, with the x axis pointing horizontally due East, the y-axis horizontally due North, while the z-axis is oriented upward. We will consider here regular wave trains of water waves propagating steadily in the direction of the horizontal x axis, periodic (of period L) in the variable x, and exhibiting no variation in the y direction. We will, in fact, show that the lack of the y-dependence of the free surface manifests throughout the entire flow.

The fluid domain is bounded below by the impermeable flat bed \(z=-d\) and above by the free surface \(z=\eta (x-ct)\), where the function \(\eta \) gives the wave profile and \(c>0\) is the wave speed.

If (u, v, w) denotes the velocity field, t is the time variable, P the pressure, \(\rho \) the constant density, g is the constant acceleration of gravity, and \(\omega =73\times 10^{-6}\) rad/s is the constant rotational speed of Earth round the polar axis, the governing equations in the f-plane approximation near the Equator are the Euler’s equations
$$\begin{aligned} \begin{array}{rcl} u_t+uu_x+vu_y+wu_z+2\omega w &{} = &{} -\frac{1}{\rho }P_x\\ v_t+uv_x+vv_y+wv_z &{}= &{}-\frac{1}{\rho }P_y\\ w_t+uw_x+vw_y+ww_z-2\omega u &{}=&{}-\frac{1}{\rho }P_z-g \end{array} \end{aligned}$$
(2.1)
and the equation of mass conservation
$$\begin{aligned} u_x+v_y+w_z=0. \end{aligned}$$
(2.2)
To single out the water wave problem from a vast range of hydrodynamical ones we impose the kinematic boundary conditions
$$\begin{aligned} w=(u-c)\eta _x\quad \mathrm{on}\quad z=\eta (x-ct), \end{aligned}$$
(2.3)
and
$$\begin{aligned} w=0\quad \mathrm{on}\quad z=-d, \end{aligned}$$
(2.4)
together with the dynamic boundary condition
$$\begin{aligned} P=P_{\mathrm{atm}}\quad \mathrm{on}\quad z=\eta (x-ct). \end{aligned}$$
(2.5)
To model observed phenomena, like underlying currents, it is essential to include the vorticity \(\Omega (x,y,z,t)\), obtained as the curl of the velocity field, that is,
$$\begin{aligned} \Omega =(w_{y}-v_{z},u_{z}-w_{x},v_{x}-u_{y}). \end{aligned}$$
(2.6)
The evolution of the vorticity is governed by the equation
$$\begin{aligned} \Omega _t + (\mathbf{u}\cdot \nabla )\Omega -2\omega (u_y,v_y,w_y)=(\Omega \cdot \nabla )\mathbf{u}. \end{aligned}$$
(2.7)

Remark 2.1

Throughout the paper we shall work under the assumption that \(\Omega _2+2\omega \ne 0\). This is a reasonable assumption, since \(\omega \approx 0.73\times 10^{-4}\) rad/s, while a typical value for \(\Omega _2\) in the equatorial Pacific is \(25\times 10^{-3}\,s^{-1}\), cf. [4].

After these preliminary considerations we are able to formulate the main result of the paper.

Theorem 2.2

Gravity wave trains can propagate at the free surface of a water flow over a flat bed governed by Eqs. (2.1)–(2.5) and exhibiting a constant vorticity only if the flow is two-dimensional.

Proof

We start the proof by noticing that, due to the assumption of constant vorticity, the evolution equation (2.7) takes the form
$$\begin{aligned} (\Omega \cdot \nabla )\mathbf{u}+2\omega (u_y,v_y,w_y)=0. \end{aligned}$$
(2.8)
We are going to use the third equation in the system above, which can be written as
$$\begin{aligned} \Omega _1 w_x+(\Omega _2+2\omega )w_y+\Omega _3 w_z=0, \end{aligned}$$
(2.9)
to prove that \(\Omega _3=0\). We will resort to the method of proof by contradiction and assume that \(\Omega _3\ne 0\). Consequently, w is constant in the direction of the vector \((\Omega _1,\Omega _2+2\omega , \Omega _3)\), which, owing to \(\Omega _3\ne 0\), is not parallel to the flat bed \(z=-d\). We then use the kinematic condition (2.4) and argue as in [3] to conclude that \(w=0\) within the fluid domain. Moreover, \(w=0\) implies that \(u_z=\Omega _2\) and \(v_z=-\Omega _1\). The latter two relations yield the existence of two functions \(\tilde{u}=\tilde{u}(x,y,t)\) and \(\tilde{v}=\tilde{v}(x,y,t)\) such that
$$\begin{aligned} \begin{array}{c} u(x,y,z,t)=\tilde{u}(x,y,t)+\Omega _2 z,\\ v(x,y,z,t)=\tilde{v}(x,y,t)-\Omega _1 z. \end{array} \end{aligned}$$
(2.10)
The advantage of working with \(\tilde{u},\tilde{v}\) emerges as the possibility of deriving from (2.2) the existence of a function \(\psi (x,y,t)\) satisfying
$$\begin{aligned} \tilde{u}=\psi _y,\quad \tilde{v}=-\psi _x. \end{aligned}$$
(2.11)
The latter equation can be used to rewrite \(\Omega _3=v_x-u_y\) as
$$\begin{aligned} \psi _{xx}+\psi _{yy}=-\Omega _3. \end{aligned}$$
(2.12)
Moreover, the first two equations of (2.9) can be written in terms of the function \(\psi \) as
$$\begin{aligned}&\Omega _1\psi _{xy}+(\Omega _2+2\omega )\psi _{yy}+\Omega _2\Omega _3=0\nonumber \\&-\Omega _1\psi _{xx}-(\Omega _2+2\omega )\psi _{xy}-\Omega _1\Omega _3=0. \end{aligned}$$
(2.13)
Note that the system (2.13) implies that \(\Omega _1^2 +(\Omega _2+2\omega )^2>0\). Therefore, we obtain
$$\begin{aligned} \psi _{xx}= & {} \frac{-\Omega _1^2\Omega _3-2\omega (\Omega _2+2\omega )\Omega _3}{\Omega _1^2+(\Omega _2+2\omega )^2},\nonumber \\ \psi _{xy}= & {} -\frac{\Omega _1\Omega _2\Omega _3}{\Omega _1^2+(\Omega _2+2\omega )^2},\nonumber \\ \psi _{yy}= & {} -\frac{\Omega _2(\Omega _2+2\omega )\Omega _3}{\Omega _1^2+(\Omega _2+2\omega )^2}, \end{aligned}$$
(2.14)
relations from which we infer that
$$\begin{aligned} \psi (x,y,t)=D x^2+E xy+F y^2 +d(t)x +e(t)y +f(t), \end{aligned}$$
(2.15)
where
$$\begin{aligned} D= & {} \frac{1}{2}\cdot \frac{-\Omega _1^2\Omega _3-2\omega (\Omega _2+2\omega )\Omega _3}{\Omega _1^2+(\Omega _2+2\omega )^2},\\ E= & {} -\frac{\Omega _1\Omega _2\Omega _3}{\Omega _1^2+(\Omega _2+2\omega )^2},\\ F= & {} -\frac{1}{2}\cdot \frac{\Omega _2(\Omega _2+2\omega )\Omega _3}{\Omega _1^2+(\Omega _2+2\omega )^2}, \end{aligned}$$
and d, e and f are functions. With the previous considerations in mind, the kinematic boundary condition (2.3) becomes
$$\begin{aligned} \left[ -c+Ex +2Fy+e(t)+\Omega _2 \eta (x-ct)\right] \eta ^{\prime }(x-ct)=0. \end{aligned}$$
(2.16)
Since \(\eta ^{\prime }\) is not identically zero and the equality in (2.16) is true for all x it follows from above that \(F=0\). Since \(\Omega _2+2\omega \ne 0\), it necessarily follows from \(F=0\) that \(\Omega _2 =0\), because we are also in the hypothesis that \(\Omega _3\ne 0\). Moreover, we also have that \(E=0\) and \(D=-\frac{1}{2}\Omega _3\). Consequently, from relation (2.16) we conclude that for all x it holds
$$\begin{aligned} (e(t)-c)\eta ^{\prime }(x-ct)=0, \end{aligned}$$
which implies that \(e(t)\equiv c\), and therefore
$$\begin{aligned}&u(x,y,z,t)\equiv c,\nonumber \\&v(x,y,z,t)=-d(t)+\Omega _3 x-\Omega _1 z,\nonumber \\&w(x,y,z,t)=0. \end{aligned}$$
(2.17)
From the third of Euler’s equations (2.1) we conclude that
$$\begin{aligned} P_z=\rho (2\omega c-g)\quad \mathrm{throughout}\quad \mathrm{the}\quad \mathrm{fluid}, \end{aligned}$$
which implies that
$$\begin{aligned} P(x,y,z,t)=\rho (2\omega c-g)z+p(x,y,t), \end{aligned}$$
(2.18)
for some function p(x, y, t). From (2.17) and the first of the Euler’s equations we obtain that \(p_x=P_x=0\), while using also the second of the Euler’s equations we get that \(p_y=P_y=\rho (d^{\prime }(t)-c\Omega _3)\). Consequently,
$$\begin{aligned} P(x,y,z,t)=\rho (d^{\prime }(t)-c\Omega _3)y+\rho (2\omega c -g)z+\tilde{f}(t), \end{aligned}$$
(2.19)
for some function \(\tilde{f}\). The dynamic boundary condition (2.5) can now be written
$$\begin{aligned} \rho (d^{\prime }(t)-c\Omega _3)y+\tilde{f}(t)=P_{atm}+\rho (g-2\omega c)\eta (x-ct),\quad \mathrm{for}\quad \mathrm{all}\quad x,y,t. \end{aligned}$$
(2.20)
We infer from above that the coefficient of y has to vanish and that \(\tilde{f}\) and \(\eta \) have to be constant functions. But \(\eta \) constant is equivalent with our flow having a flat surface, which is a contradiction.

The contradiction that we reached shows that \(\Omega _3=0\). In the following, we will be concerned with proving that \(\Omega _1\) also vanishes. Moreover, we will show that the pressure P and the velocity field (u, v, w) are independent of y.

Our next goal is to show that \(\Omega _1=0\) and for this purpose we assume for the sake of contradiction that \(\Omega _1\ne 0\).

We note first that from (2.8) and using that \(\Omega _3=0\) we obtain
$$\begin{aligned}&\Omega _1 u_x+(\Omega _2+2\omega )u_y=0,\nonumber \\&\Omega _1 v_x+(\Omega _2+2\omega )v_y=0,\nonumber \\&\Omega _1 w_x+(\Omega _2+2\omega )w_y=0. \end{aligned}$$
(2.21)
On the other hand, from \(0=\Omega _3=v_x-u_y\) we obtain a function \(\varphi =\varphi (x,y,z,t)\) which satisfies
$$\begin{aligned} u=\varphi _x,\quad v=\varphi _y. \end{aligned}$$
Up to addition to \(\varphi \) of a function that depends only on z and t we infer from the expressions of \(\Omega _1\) and \(\Omega _2\) that
$$\begin{aligned} w=\varphi _z-(\Omega _2 x-\Omega _1 y). \end{aligned}$$
With the help of the above expressions of u, v, w in terms of \(\varphi \) we see that the equation of mass conservation (2.2) becomes
$$\begin{aligned} \varphi _{xx}+\varphi _{yy}+\varphi _{zz}=0. \end{aligned}$$
(2.22)
The harmonicity of w emerges now as a direct consequence of differentiating (2.22) with respect to z. We are going to show now that \(w=0\) on a plane parallel to the flat bed and contained entirely in the fluid domain. To be more precise, let
$$\begin{aligned} l:=\{(x_0,y,\eta (x_0,t_0)):y\in \mathbb {R}\} \end{aligned}$$
be a trough line located at some position \(x_0\) at some moment \(t_0\). Using the kinematic condition (2.3) and the fact that \(\eta _x =0\) along l we conclude that
$$\begin{aligned} w=0\,\,\mathrm{on}\,\, \mathrm{the}\,\,\mathrm{whole}\,\,\mathrm{of}\,\, l. \end{aligned}$$
(2.23)
The third relation in (2.21) allows us to conclude that w is constant in the direction of the vector \((\Omega _1, \Omega _2+2\omega ,0)\) which, due to the assumption \(\Omega _1\ne 0\), is not collinear with l. Thus, \(w=0\) at all points of the plane containing l and spanned by l and the vector \((\Omega _1, \Omega _2+2\omega ,0)\), which is in fact the plane \(z=\eta (x_0,t)\) and which is parallel to the bed \(z=-d\) and contained entirely in the fluid domain.
Using that w is a bounded harmonic function that vanishes on \(z=-d\) and on \(z=\eta (x_0,t)\) we conclude from the Phragmen–Lindelöf maximum principle, cf. [15], that \(w=0\) in the region of the fluid domain bounded by the flat bed and the plane \(z=\eta (x_0,t)\). We can also infer from [14] that, owing to its harmonicity, w is real-analytic at any instant t. Thus, since \(w=0\) on an open set, it must vanish on the entire fluid domain. Then, as in the beginning of the proof we infer the existence of a function \(\psi (x,y,t)\) satisfying relations (2.10) and (2.11). In addition, since now \(\Omega _3=0\), we have for the function \(\psi \) the relations
$$\begin{aligned} \psi _{xx}+\psi _{yy}=0, \end{aligned}$$
(2.24)
and
$$\begin{aligned}&\Omega _1\psi _{xy}+(\Omega _2+2\omega )\psi _{yy}=0\nonumber \\&-\Omega _1\psi _{xx}-(\Omega _2+2\omega )\psi _{xy}=0. \end{aligned}$$
(2.25)
We obtain immediately from (2.24) and (2.25) that
$$\begin{aligned} \psi _{xx}=\psi _{xy}=\psi _{yy}=0 \end{aligned}$$
within the fluid domain which means that there are function d(t), e(t) and f(t) such that
$$\begin{aligned} \psi (x,y,t)=d(t)x+e(t)y+f(t) \end{aligned}$$
for all x, y, t. We rely once more on the kinematic condition (2.3) to derive the relation
$$\begin{aligned} \left[ -c+e(t)+\Omega _2\eta (x-ct)\right] \eta ^{\prime }(x-ct)=0. \end{aligned}$$
From the latter we infer first that \(\Omega _2=0\) and then, as a consequence, it follows that \(e(t)\equiv c\). We follow now the same route as in the beginning of the proof and reach that \(\eta \) has to be a constant. The latter contradiction shows that \(\Omega _1\) necessarily has to vanish.
We are going to prove now that the velocity field does not depend on the y variable. Moreover, we will prove that v is in fact a constant and the y-derivative of the pressure function vanishes. To this end note that the vorticity equation (2.8) takes the form
$$\begin{aligned} (\Omega _2+2\omega )u_y=(\Omega _2+2\omega )v_y=(\Omega _2+2\omega )w_y=0, \end{aligned}$$
(2.26)
which, due to \(\Omega _2+2\omega \ne 0\), implies \(u_y=v_y=w_y=0\). Using also \(0=\Omega _1=w_y-v_z\) and \(0=\Omega _3 =v_x-u_y\) we infer that \(v_x=v_z=0\). Thus, the second component of the velocity field depends only on t.
A consequence of the previous findings is that the second equation in (2.1) reduces to
$$\begin{aligned} v_t=-\frac{1}{\rho }P_y. \end{aligned}$$
Integrating with respect to y in the above relation we find that
$$\begin{aligned} P(x,y,z,t)=-\rho v_t y+F(x,z)+R(t), \end{aligned}$$
for some functions F and R whose variables are as indicated in the formula above. With the latter structure for P, the dynamic boundary condition (2.5) becomes
$$\begin{aligned} -\rho v_t y +F(x,\eta (x))+R(t)=P_{\mathrm{atm}}, \end{aligned}$$
for all x, y and t. But this implies that \(v_t\equiv 0\). Therefore, \(P_y\equiv 0\). We have thus proved that the flow has a two-dimensional character.\(\square \)

Remark 2.3

Note that, due to the assumption \(\Omega _2+2\omega \ne 0\)– reasonable in the setting of equatorial waves—we can dispense of the constant nonzero vorticity requirement made in [2] in the context of capillary wave trains, in [3] for the case of gravity wave trains and in [26] regarding capillary-gravity water waves.

Notes

Acknowledgements

Open access funding provided by University of Vienna. We are thankful to the anonymous referee for many useful suggestions that considerably improved the exposition.

References

  1. 1.
    Constantin, A.: On the deep water wave motion. J. Phys. A 34, 1405–1417 (2001)CrossRefMATHMathSciNetGoogle Scholar
  2. 2.
    Constantin, A., Kartashova, E.: Effect of non-zero constant vorticity on the nonlinear resonances of capillary water waves. Europhys. Lett. 86, 29001 (2009)CrossRefGoogle Scholar
  3. 3.
    Constantin, A.: Two-dimensionality of gravity water flows of constant non-zero vorticity beneath a surface wave train. Eur. J. Mech. B Fluids 30, 12–16 (2011)CrossRefMATHMathSciNetGoogle Scholar
  4. 4.
    Constantin, A.: On the modelling of equatorial waves. Geophys. Res. Lett. 39, L05602 (2012)CrossRefGoogle Scholar
  5. 5.
    Constantin, A.: An exact solution for equatorially trapped waves. J. Geophys. Res. Oceans 117, C05029 (2012)CrossRefGoogle Scholar
  6. 6.
    Constantin, A., Germain, P.: Instability of some equatorially trapped waves. J. Geophys. Res. Oceans 118, 2802–2810 (2013)CrossRefGoogle Scholar
  7. 7.
    Constantin, A.: Some three-dimensional nonlinear equatorial flows. J. Phys. Oceanogr. 43(1), 165–175 (2013)CrossRefGoogle Scholar
  8. 8.
    Constantin, A.: Some nonlinear, equatorially trapped, nonhydrostatic internal geophysical waves. J. Phys. Oceanogr. 44(2), 781–789 (2014)CrossRefGoogle Scholar
  9. 9.
    Constantin, A., Johnson, R.S.: The dynamics of waves interacting with the equatorial undercurrent. Geophys. Astrophys. Fluid Dyn. 109(4), 311–358 (2015)CrossRefMathSciNetGoogle Scholar
  10. 10.
    Constantin, A., Johnson, R.S.: An exact, steady, purely azimuthal equatorial flow with a free surface. J. Phys. Oceanogr. 46(6), 1935–1945 (2016)CrossRefGoogle Scholar
  11. 11.
    Constantin, A., Johnson, R.S.: An exact, steady, purely azimuthal flow as a model for the Antarctic circumpolar current. J. Phys. Oceanogr. 46(12), 3585–3594 (2016). doi: 10.1175/JPO-D-16-0121.1 CrossRefGoogle Scholar
  12. 12.
    Cushman-Roisin, B., Beckers, J.-M.: Introduction to Geophyiscal Fluid Dynamics: Physical and Numerical Aspects. Academic Press, Waltham (2011)MATHGoogle Scholar
  13. 13.
    Dubreil-Jacotin, M.-L.: Sur les ondes de type permanent dans les liquides hétérogène. Atti Accad. Naz. Lincei, Mem. Cl. Sci. Fis. Mat. Nat. 15, 814–819 (1932)MATHGoogle Scholar
  14. 14.
    Evans, L.C.: Partial Differential Equations. American Mathematical Society, Providence (1998)MATHGoogle Scholar
  15. 15.
    Fraenkel, L.E.: An Introduction to Maximum Principles and Symmetry in Elliptic Problems. Cambridge University Press, Cambridge (2000)CrossRefMATHGoogle Scholar
  16. 16.
    Genoud, F., Henry, D.: Instability of equatorial water waves with an underlying current. J. Math. Fluid Mech. 16(4), 661–667 (2014)CrossRefMATHMathSciNetGoogle Scholar
  17. 17.
    Gerstner, F.: Theorie der Wellen samt einer daraus abgeleiteten Theorie der Deichprofile. Ann. Phys. 2, 412–445 (1809)CrossRefGoogle Scholar
  18. 18.
    Henry, D.: On gerstner’s water wave. J. Nonlinear Math. Phys. 15(suppl. 2), 87–95 (2008)CrossRefMATHMathSciNetGoogle Scholar
  19. 19.
    Henry, D.: An exact solution for equatorial geophysical water waves with an underlying current. Eur. J. Mech. B Fluids 38, 18–21 (2013)CrossRefMATHMathSciNetGoogle Scholar
  20. 20.
    Henry, D., Hsu, H.-C.: Instability of internal equatorial water waves. J. Differ. Equ. 258(4), 1015–1024 (2015)CrossRefMATHMathSciNetGoogle Scholar
  21. 21.
    Henry, D.: Exact equatorial water waves in the \(f\)-plane. Nonlinear Anal. Real World Appl. 28, 284–289 (2016)CrossRefMATHMathSciNetGoogle Scholar
  22. 22.
    Henry, D.: Equatorially trapped nonlinear water waves in a \(\beta \)-plane approximation with centripetal forces. J. Fluid Mech. 804, R1 (2016). doi: 10.1017/jfm.2016.544 CrossRefMATHMathSciNetGoogle Scholar
  23. 23.
    Ionescu-Kruse, D.: Instability of equatorially trapped waves in stratified water. Ann. Mat. Pura Appl. (4) 195(2), 585–599 (2016)CrossRefMATHMathSciNetGoogle Scholar
  24. 24.
    Ionescu-Kruse, D., Martin, C. I.: Local stability for an exact steady purely azimuthal equatorial flow, to appear in J. Math. Fluid Mech. doi: 10.1007/s00021-016-0311-4
  25. 25.
    Hsu, H.-C., Martin, C.I.: Free-surface capillary-gravity azimuthal equatorial flows. Nonlinear Anal. 144, 1–9 (2016)CrossRefMATHMathSciNetGoogle Scholar
  26. 26.
    Martin, C.I.: Resonant interactions of capillary-gravity water waves. J. Math. Fluid Mech. (2016). doi: 10.1007/s00021-016-0306-1
  27. 27.
    Matioc, A.-V.: An exact solution for geophysical equatorial edge waves over a sloping beach. J. Phys. A 45(36), 365501, 10 (2012)CrossRefMATHMathSciNetGoogle Scholar
  28. 28.
    Matioc, A.-V.: Exact geophysical waves in stratified fluids. Appl. Anal. 92(11), 2254–2261 (2013)CrossRefMATHMathSciNetGoogle Scholar
  29. 29.
    Stuhlmeier, R.: On constant vorticity flows beneath two-dimensional surface solitary waves. J. Nonlinear Math. Phys 19(suppl. 1), 1240004 (2012)MATHMathSciNetGoogle Scholar
  30. 30.
    Wahlén, E.: Non-existence of three-dimensional travelling water waves with constant non-zero vorticity. J. Fluid Mech. 746, R2 (2014)CrossRefGoogle Scholar

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Authors and Affiliations

  1. 1.Faculty of MathematicsUniversity of ViennaViennaAustria

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