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Abstract and Applied Analysis
Volume 2013 (2013), Article ID 620320, 9 pages
Stability Analysis of the Supercritical Surface Quasi-Geostrophic Equation
School of Mathematical Sciences, Anhui University, Hefei 230601, China
Received 9 June 2013; Accepted 21 August 2013
Academic Editor: Diego Córdoba
Copyright © 2013 Yan Jia et al. This is an open access article distributed under the Creative Commons Attribution License, which permits unrestricted use, distribution, and reproduction in any medium, provided the original work is properly cited.
This paper is devoted to the study of the stability issue of the supercritical dissipative surface quasi-geostrophic equation with nondecay low-regular external force. Supposing that the weak solution of the surface quasi-geostrophic equation with the force satisfies the growth condition in the critical BMO space , it is proved that every perturbed weak solution converges asymptotically to solution of the original surface quasi-geostrophic equation. The initial and external forcing perturbations are allowed to be large.
1. Introduction and Main Results
Mathematical models in fluid dynamics play an important role in theoretical and computational studies in meteorological and oceanographic sciences and petroleum industries, and so forth. In this paper, we consider a simple mathematical model of large scalar ocean and atmosphere dynamics (see Pedlosky )—the dissipative surface quasi-geostrophic equation which is first introduced by Constantin et al. : Here is a dissipative coefficient and is the Riesz potential operator defined by the fractional power of : is an unknown scalar function representing potential temperature. is the velocity field determined by where , is the 2D Riesz transform, is the initial data, and is the nondecay external force.
The surface quasi-geostrophic equation shares many features with fundamental fluid motion equations. When , it is comparable to the formation of sharp fronts between masses of hot and cold air (see Majda and Tabak ). When (1) can be looked to as a nonviscous wind driven circulation equation (see Pedlosky ). What is more, (1) with shares many similar features with three-dimensional incompressible Navier-Stokes equations . Thus is therefore referred to as the critical case, while the cases and are supercritical and subcritical, respectively.
Due to the importance in mathematics, there is much attention on the well-posedness and large time behaviors of the surface quasi-geostrophic equation. When , Constantin and Wu  proved that this equation possesses a unique and global smooth solution for a sufficiently smooth initial function. When , Kiselev et al.  showed the existence of global smooth solutions for smooth periodic initial data. At the same time, Caffarelli and Vasseur  also constructed a global smooth solution with . In the supercritical case , however, the question of the global regularity is still generally not clear although many efforts have been made on the small regular solution or regularity criteria (see [8–16]). One may also refer to some interesting results of the generalized quasi-geostrophic equations (see [17–21]).
However, it is desirable to understand the asymptotic stability issue of the supercritical dissipative surface quasi-geostrophic equation. More precisely, we consider the perturbed quasi-geostrophic equation: where and are the initial data and external forcing perturbations. The stability problem of (4) has been studied by many authors and a lot of good results have been obtained. To go directly to the main points of the present paper, in what follows we only review some former results which are closely related to our main results. First, when the surface quasi-geostrophic equations (1) has zero external force or time-decay external force, some interesting time decay results [22–25] have been obtained which essentially show the asymptotic stability for the trivial solution . For the stability issue of the nontrivial solutions, Chae and Lee  studied the asymptotic stability of critical quasi-geostrophic equation in Besov space under the small initial perturbation. The nonlinear stability and instability analysis of the subcritical quasi-geostrophic equation is recently investigated by Chen and Price . Dong and Chen  recently considered the asymptotic stability problem in the Serrin-type critical Lebesgue space () under the external force. It is natural and interesting to further investigate the asymptotic stability for the nontrivial global solutions in the larger critical spaces, especially in the margin case .
The main purpose of this study is to investigate the asymptotic stability for the global solution of the supercritical surface quasi-geostrophic equation in the critical BMO space with nondecay low-regular external force. To state our main results, we first give the definition of the weak solution of the dissipative surface quasi-geostrophic equation (1).
Definition 1. Letting , . A measurable function is said to be a global weak solution of the surface quasi-geostrophic equation (1) if the following conditions hold true. (i) for all . (ii) is continuous on in the weak topology of and as for all . (iii) For , and any test function , where denotes the inner product of the space . (iv) Energy-type inequality
Now our results read as the following.
Theorem 2. Letting , . Assume is a global weak solution of the supercritical dissipative surface quasi-geostrophic equation (1) with the nondecay low-regular external force and satisfies the critical growth condition in BMO space: Then, for any perturbations and , every weak solution of the perturbed quasi-geostrophic equation (4) converges asymptotically to solution as
Remark 3. The critical space-time mixed space (7) in Theorem 2 is scaling invariant under the scaling transformation . Moreover, according to the result of Dong and Chen , the weak solution satisfying (7) is actually regular. Furthermore, our results also show that the weak solutions of the perturbed equation (4) do not need to satisfy the energy-type inequality (6) and then they do not have to be regular.
Remark 4. On one hand, compared with the stability result by Chae and Lee , there is no any smallness restriction on the perturbation functions and in Theorem 2. That is to say, the initial and external forcing perturbations from are allowed to be large. On the other hand, our result here extends the previous result  to the margin case due to the embedding relation . Moreover, in comparison with , we require less regularity for the external force.
Remark 5. Although Theorem 2 shows that the decay property of difference between the global solution and the perturbed solution , however, it is different from the time decay issue of the zero-forced surface quasi-geostrophic equations (see [22, 23] and references therein) . The latter indeed shows the asymptotic stability of the trivial solution for the surface quasi-geostrophic equation with zero external force. However, when the surface quasi-geostrophic equation (1) has the nonzero low-regular external force , is obviously not a solution of (1), therefore, our result here essentially shows the asymptotic stability of the nonzero global solution of (1).
Remark 6. The main idea in the proof of Theorem 2 is based on some new observations due to the special structure in nonlinear term which is different from the classic Navier-Stokes equations. Additionally, in order to derive an auxiliary decay estimate in the framework of the critical BMO space, we also need to choose a suitable test function and derive some average decay properties. It is worth noting that although the study of the classic incompressible Navier-Stokes equations is beneficial to that of quasi-geostrophic equation, compared with some asymptotic stability results of three-dimensional Navier-Stokes equations (refer to [30–32]), we do not know, however, whether our result in the framework of the critical BMO space is still valid for the Navier-Stokes equations. We will focus on that problem in the future.
The remains of this paper are organized as follows. In Section 2, we will investigate the global estimates of the difference between the original surface quasi-geostrophic equation and the perturbed equation. In Section 3, we will further derive an average decay estimates of the difference. Finally, we will prove the asymptotic stability of large solution to the surface quasi-geostrophic equation (1) under the large initial perturbation in Section 4.
Let us end this section by some notations. In what follows, stands for the abstractly positive constant. with denotes the usual Lebesgue space. with is the fractional Sobolev space with the norm:
BMO is the space of the bounded mean oscillation defined by where is the average of over . In particular, BMO is the dual space of the Hardy space .
2. Global Estimate of
In this section, we will investigate the global estimates of the difference between the global solution of the original equation (1) and the weak solution of the perturbed equation (4). It is mentioned that some necessary smooth properties of the difference is required in the derivation of the global estimates below. As stated in Remark 3, the global weak solution of the original equation (1) satisfying the regular condition (6) is actually regular. However, the perturbed weak solution is not smooth, in order to derive the global estimates of the difference . We first seek a smooth function to approximate the weak solution of the perturbed quasi-geostrophic equation (4). To do so, we apply the standard Galerkin method to construct the smooth approximate solutions: Here is an orthonormal basis of .
Instead of the perturbed quasi-geostrophic equation (4), for any test function = the space spanned by satisfy where
It is worth noting that, for fixed integer , equations (13) are indeed ordinary differential equations. The theory of existence and uniqueness for such ordinary differential equations is standard. Therefore, we can prove that the approximated solutions exist globally and smoothly and are uniformly bounded in the following space:
Furthermore, it allows us to prove that the approximates smooth solutions converge to the weak solution of the perturbed quasi-geostrophic equation (4) when tends to infinity. Indeed, we only need to obtain the strong convergence of in space . To do so, for example, with the aid of Hölder and Sobolev embedding estimates, it follows that for . This implies the uniform bounds of By the compactness theorem [4, Chapter 3, Theorem 2.1], the sequence admits a subsequence denoted also by converging to the weak solution of the perturbed equation (4): from which and uniformly bounds of due to (15), we have for almost all .
Thanks to the regular solution , we then derive from (19) that for almost all , which implies by Fatou Lemma that for almost all .
Denoting by the difference between solution of original equation (1) and approximated smooth solution of the (13), with the direct computation due to the smoothness of , it is easy to examine satisfying where the divergence free property of the velocity is used. In order to deal with the nonlinear term of the right hand side of (22), we require the following important lemma.
Lemma 7 (Marchand ). Assume that , () is the Riesz transform, then there exists a constant such that is valid. Here is the Hardy space.
Thus we have the following crucial estimates for the nonlinear term of (23): where we have also used the fact that BMO is the dual space of the Hardy space .
With the aid of the Hölder inequality and the Young inequality, one shows that for the external force term
Plugging the above inequalities into (22) and taking the Gronwall inequality into consideration, we derive the global estimate of : Passing the limit in the above inequality and applying (21), we have for the constant independent of .
3. Average Decay of
In this section, we are devoted to investigating the average decay of the difference which will play an important role in the proof of Theorem 2.
It is worth noting that Kozono  and Zhou  have investigated the average decay properties of the classic Navier-Stokes equation. For the surface quasi-geostrophic equation considered here, however, the fractional dissipative operators are nonlocal singular integral operators. the new difficulty on the uniformly estimates of will rise if we directly follow the similar argument of the classic Navier-Stokes equations [30, 32].
Fortunately, we can avoid those additional difficulties with the aid of the theory of the analytic semigroup (see Pazy ). Since the Laplacian operator in whole space generates a bounded analytic semigroup in each (), thus the fractional power can be redefined with the aid of the spectral decomposition: where is a family of projection operators and is the spectral of the Laplacian operator . Namely, the analytic semigroup generated by the nonlocal singular integral operators is also defined in a satisfactory form: Furthermore, we may derive the embedding relation in a natural form where Parseval equality is used in the last two equalities.
Now we carry out to study the average decay of the difference . Firstly, according to the definitions of the weak solutions in Definition 1, we choose a special test function as where is the standard mollifier function with and . Thus satisfies the following weak formation for .
We now give the estimates of (33) by passing the limit . More precisely, we will prove the following lemma.
Lemma 8. Under the same condition in Theorem 2, we have the following uniform estimates of the difference :
then one shows that for (34)
and then letting , we have
Furthermore, employing the Parseval equality and the Hölder inequality, we obtain that for Integrating in time from to yields Together with (37) we derive the desired average decay of the difference between the global solution of the original quasi-geostrophic equation (1) and the weak solution of the perturbed quasi-geostrophic equation (4):
Now it remains to prove Lemma 8.
Proof of Lemma 8. For convenience, the three terms of the left hand side of (33) are denoted by , , and , respectively. For , we have
Applying the Fubini theorem, it is not difficult to obtain and similarly thus we have for
For we have which implies .
Hence, combining the above inequalities, one derives the estimates of :
For , employing integrating by parts gives
For , applying the Hölder inequality and the Gagliardo-Nirenberg inequality and (27) gives where we have used the following estimates:
Similarly, for , it follows that
Plugging the estimates of () into (47) yields
In order to estimate , thanks to together with the Hölder inequality and the Young inequality gives that
Inserting (46), (51), and (53) into (33), we obtain which completes the proof of Lemma 8.
4. Proof of Theorem 2
With the aid of the global estimates and average decay of the difference between the original surface quasi-geostrophic equation (1) and the perturbed surface quasi-geostrophic equation, the proof of stability is straight forward.
The integration of (28) with respect to on the interval gives From the average decay property of in Section 3, the first term of the right hand side of the above inequality tends to zero as . For the second term of the right hand side, we have according to the regular condition on in Theorem 2, the second term also tends to zero as . Hence, we derive the following stability property: which completes the proof of Theorem 2.
The authors would like to express their sincere thanks to Professor D. Córdoba for the valuable comments and suggestions. This work is partially supported by the NNSF of China (11271019) and the NSF of Anhui Province (11040606M02), and is also financed by the 211 Project of Anhui University (KJTD002B, KJJQ005).
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