Solvability and asymptotic properties for an elliptic geophysical fluid flows model in a planar exterior domain

Xinguang Zhanga,c,1 , Lishan Liu , Yonghong Wu , B. Wiwatanapataphee , Yujun Cui School of Mathematical and Informational Sciences, Yantai University, Yantai 264005, Shandong, China zxg123242@163.com School of Mathematical Sciences, Qufu Normal University, Qufu, 273165 Shandong, China mathlls@163.com Department of Mathematics and Statistics, Curtin University of Technology, Perth, WA 6845, Australia y.wu@curtin.edu.au; b.wiwatanapataphee@curtin.edu.au Department of Mathematics, Shandong University of Science and Technology, Qingdao, 266590, Shandong, China cyj720201@163.com


Introduction
We study in this paper the solvability and asymptotic properties for the following model of nonlinear Schrödinger equation from the study of the gyres of geophysical fluid flows in a planar exterior domain: where Ω = {z ∈ R 2 : |z| 1}, f : [1, ∞) × R 2 → R is continuous.
Nonlinear elliptic equations are closely related to many dynamic model arising from physics, biology, geography and applied mathematics [2,3,5,39,40,43]. In Eq. (1), when the term z · ∇v disappears, Constantin and Johnson [5] model the large gyres of geophysical fluid flows by using a shallow-water asymptotic solution of Euler's equation in spherical coordinates where the Earth's rotation velocity ω > 0 refers to in nondimensional units, the unknown function v(z, y) stands for the stream function, the oceanic vorticity is defined by the function F . In fact, the gyres are generated by the interaction between the wind stress and the effect of the Earth's rotation, thus it is not good approximation to describe largescale gyres in spherical geometry of the Earth by a β-plane [1]. Therefore, it is reasonable to consider large-scale gyres in the spherical coordinates as the shallow-water approximation. In brief, in spherical coordinates, suppose the polar angle is α ∈ [0, π) and α − π/2 is the conventional angle of latitude, if α = 0, it corresponds to the south pole. Let the azimuthal angle β ∈ [0, 2π) be the angle of longitude and Ψ be the vorticity of the underlying motion of the ocean, v(α, β) = −ω cos α + Ψ (α, β) stands for the stream function. The horizontal flow on the spherical earth will form a gyre with the azimuthal and polar velocity components v β sin −1 α, v α , respectively, and the gyre equation for Ψ on the half-line is governed by 1 sin 2 α Ψ ββ + Ψ α cot α + Ψ αα = F (Ψ − ω cos α).
From the south pole to the plane of the equator make the stereographic projection ξ = re iφ , r = cot α 2 = sin α 1 − cos α , then gyre governed equation (3) is equivalent to the semilinear elliptic equation (2). Thus for given F and ω, one can explore the semilinear Dirichlet boundary value elliptic problem in a given planar region Ω For obtaining the solvability and asymptotic properties of the gyre governed equation, by using the stereographic projection for (4), Chu [3] found that the flow of an arctic gyre, described by (3), can be equivalently formulated as the following second-order ordinary differential equation: for some constant v 0 . In fact, Eq. (5) on the half-line is also related to the second ordinary differential equation By Krasnoselskii fixed point theorem on cone compression and expansion, Zima [46] studied the existence of positive solutions for the above boundary value problem when f : (0, +∞) × [0, +∞) → [0, +∞) is continuous. In particular, by using suitable growth condition and fixed point theorem, Yin [33], Constantin [4], Ertem and Zafer [8] presented the existence and asymptotic behavior of positive solutions for an extended version of Eq. (6), respectively. For other related work, we refer reader to [17,18,35,36]. In comparison, model (2) was obtained in the case where the vertical motion of the fluid was neglected. However, in the large-scale oceanic motion, saddle points and singular points on the boundary are normally caused by a jet flowing toward or away from the coastal line or the boundary, and near the saddle points and singular points, the vertical motion of the fluid can not be neglected. Thus Eq. (1) is a general form of the geophysical fluid flows model (2) describing the gyre flow of ocean in a larger scale with the vertical motion. Motivated by the existing works, this paper focuses on the existence of radial positive solutions and its asymptotic properties at boundary for the nonlinear Schrödinger equation (1). Our work has some new features, firstly, model (1) promotes and generalizes the gyre flow model proposed by Constantin, which can describe more general gyre flow of ocean in a larger scale; secondly, some appropriate comparative conditions are introduced for overcoming the influence of perpendicular vorticity, thirdly, the asymptotical property of solution at infinity of model (1) performs as nonlinear behaviour, it is well known that the asymptotical property at boundary of nonoscillatory solutions for most equations often behaves like a linear function such as [4,43], however, the asymptotical property behaving like a nontrivial nonlinear function is also interesting and important, which here can explain the interdependency of the ocean flows in arctic gyres. On the other hand, although the study of the differential equations has a long history [6, 8-14, 16, 19-34, 37-45], the geophysical fluid flows model (2) arising from arctic gyres still presents some specific challenges.

Preliminaries and lemmas
In order to establish the existence and asymptotic behavior of radial solutions for the general geophysical fluid flows model (1), we need to transform the model (1) to a more convenient form.
Next, let x = ln r, w(x) = v(r). So we have r = e x , w(x) = v(e x ) and Substituting (9) into (7), we get Remark 1. It follows from Lemma 1 that if w(x) is a positive solution of the second differential equation (7), then v(|z|) = w(ln |z|) is a radial symmetric solutions of the model (1). Thus in what follows, we only consider Eq. (7). Now we are concerned with the solvability of Eq. (7) on [0, +∞). Firstly, let us introduce the following function space: which is equipped with the usual maximum norm Lemma 2. (See [33].) X is a Banach space.
http://www.journals.vu.lt/nonlinear-analysis Lemma 3. (See [33].) Let X be defined as before and P ⊂ X. Then P is relatively compact in X if the following conditions hold: (i) The set P is uniformly bounded in X, i.e., there exists a positive constant M such that for all w ∈ P and all x > 0, |w(x)| M and |w(x) + xw (x)| M . (ii) P is equicontinuous, i.e., for any > 0, there exists δ > 0 such that for all The function from P is equiconvergent, i.e., for any given > 0, there exists a T = T ( ) > 0 such that for all y, x > T and all w ∈ P , |w(x) − w(y)| < ,

Main results
Before stating our main results, we firstly introduce the following assumptions: (A1) There exists a continuous function F : [1, +∞) × R + × R + → R + , which is nondecreasing with respect to the second and third arguments for each Proof. We start our proof by studying the equivalent form (7) of model (1). To do this, by the Lebesgue dominated convergence theorem, (A2) implies that there exists a positive constant ∈ (0, µ) such that For the above > 0, define a subset of X notice that ∈ P , then P is nonempty bounded closed convex set. Now define a nonlinear operator T : P → X by Now we divide our proof into the following four steps.
Step 1. We firstly prove that T P ⊆ P . In fact, by (10) and the monotonicity of F , for any x 0 and w ∈ P , we have which implies that (T w)(x) 2µ − for any x 0. On the other hand, by (11), one has and Substituting (13) and (11) into the following formula, we have http://www.journals.vu.lt/nonlinear-analysis which implies that (T w)(x) + x(T w) (x) 2µ − for any x 0. Thus T P ⊆ P and T : P → P is well defined.
Step 2. We show that T (P ) is relatively compact in X by verifying that T (P ) satisfies conditions of (i)-(iii) of Lemma 3. From (12) and (14) we know T (P ) is uniformly bounded, i.e., condition (i) holds. In what follows, we prove that T (P ) is equicontinuous. Let {w} n 1 is any sequence in P , by L'Hôspital rule and (10), we have Thus according to (10), (13) and (15), one gets x 0 se 2s f e s , sw n (s), w n (s) + sw n (s) ds 1 x 2 x 0 se 2s F e s , sw n (s), w n (s) + sw n (s) ds for some M > 0. From (16) and the mean value theorem one gets that for any n 1, On the other hand, it follows from (10) and (13) that Consequently, {T w n } n 1 is equicontinuous in X. Thus condition (ii) of Lemma 3 is satisfied.
Now we check condition (iii). In fact, by (12) and (14), we have and By (17) (17)- (19) imply that for any > 0, there exists M > 0 such that Thus {T w n } n 1 is equiconvergence in X. According to Lemma 3, T (P ) is relatively compact in X.
Step 3. We check that T : P → P is continuous. It follows from (A2) and the integral absolutely continuity that for any > 0, there exits some x * > 0 such that +∞ e x * s 2 F (s, 2µ ln s, 2µ) ds < 3 .
Hence (23) and (24) yield Thus T : P → P is a continuous operator. According to Schauder's fixed point theorem, T has a fixed point w µ in P , i.e., T w µ = w µ .
According to Theorem 1, the conclusion of Corollary 1 holds.
In the following, we consider the existence of positive solutions and its asymptotic properties for the following separated type geophysical fluid flows model: where f, g : [1, ∞) × R → R are continuous and Ω = {z ∈ R 2 : |z| 1}.
Proof. Let for x ∈ [1, +∞) and u, v ∈ R, and for any µ > 0, For (26), if f (t, u) ≡ 0 or g(t, v) ≡ 0, then it will reduce to the following form in a planar exterior domain: where f, g : [1, ∞) × R → R are continuous. From Theorem 2 we have the following corollaries.

Example 3.
Let Ω = {z ∈ R 2 : |z| 1}, consider the following gyres model of geophysical fluid flows: If there exists a continuous nondecreasing function F 1 : R + → R + and a constant µ > 0 such that Then the gyre flow model (2) has a radial solution v µ , which possesses the following asymptotic properties: Let By Corollary 2, the gyre flow model (31) has a radial solution v µ with the asymptotic properties (32).

Remark 3.
Normally, if the oceanic vorticity contribution disappears, i.e, F ≡ 0, then the gyre flow model (2) describes that the flow field is irrotational, Example 3 can be applied. But, for long waves in oceanic vorticity, since the averaged vorticity plays dynamically the dominant role (see [7]), the flow behaves like nonzero constant vorticity F = a when a (µ − ω)/2, we still can use Example 3 to govern the behaviour of long waves in oceanic vorticity. In addition, it is reasonable to model Coriolis vorticities [15] by Example 3 when the prime sources of vorticity in the oceans continues to increase in the form of the tidal currents.

Conclusion
In this paper, we study the solvability and asymptotic properties of a recently derived general nonlinear gyre of geophysical fluid flows model. In a general way, there are two factors (the spin vorticity 2ω cos α and the oceanic vorticity F (Ψ − ω cos α)) to influence the vorticity of geophysical flows because the earth rotates and ocean motions (for detail, see [3,5]). The spin vorticity is completely confirmed by the features of planets, however for the motion of the ocean, one may choose the suitable vorticity associated with the movement of the ocean and coupled to the earth's rotation [5] to express a special gyre. In this paper, the oceanic vorticity F is a general nonlinear function, which can be chosen properly according to the actual situation, this makes the model have more extensive application value and significance.