Advanced Search
Article Contents

The Dynamics of Barotropic Vortex Merging


doi: 10.1007/s00376-016-6006-1

  • The merging of multiple vortices is a fundamental process of the dynamics of Earth's atmosphere and oceans. In this study, the interaction of like-signed vortices is analytically and numerically examined in a framework of two-dimensional inviscid barotropic flows. It is shown that barotropic vortex interaction turns out to be more intricate than simple merging scenarios often assumed in previous studies. Some particular configurations exist in which the vortex merging process is never complete despite strong interaction of like-signed vortices, regardless of the strengths or distances between the vortices. While the conditions for a complete vortex merging process introduced in this study appear to be too strict for most practical applications, this study suggests that careful criteria for vortex mergers should be properly defined when simulating the interaction of vortices, because the merging may not always result in a final enhanced circulation at the end of the interaction, as usually assumed in the literature.
  • 加载中
  • Brown M. R., 1997: Experimental evidence of rapid relaxation to large-scale structures in turbulent fluids: Selective decay and maximal entropy. Journal of Plasma Physics, 57, 203- 229.10.1017/S00223778960052114520c01f-28cd-4d22-891e-3408a2b8cac580d575761c10ceb2f89d366bb22488d7http%3A%2F%2Fjournals.cambridge.org%2Fabstract_S0022377896005211refpaperuri:(1a0b78c914dbf25e21c7d7f8ca319ff8)http://journals.cambridge.org/abstract_S0022377896005211There is abundant experimental, theoretical and computational evidence that certain constrained turbulent fluid systems self-organize into large-scale structures. Examples include two-dimensional (geostrophic) fluids, guiding-centre plasmas and pure-electron plasmas, as well as two- and three-dimensional magnetofluids such as reversed-field pinches and spheromaks. The theoretical understanding of relaxation phenomena is divided into two quite different constructs: selective decay and maximal entropy. Theoretical foundations of both of these principles are largely due to Montgomery and his collaborators. In this paper, selective decay and maximal entropy theories of turbulent relaxation of fluids are reviewed and experimental evidence is presented. Experimental evidence from both 2D fluids and from 3D magnetofluids is consistent with the selective decay hypothesis. However, high-resolution computational evidence strongly suggests that formation of large-scale structures is dictated by maximal-entropy principles rather than selective decay.
    Canzani Y., 2013: Notes for analysis on manifolds via the Laplacian. Harvard University. [Available online at http://www.math.harvard.edu/\simcanzani/docs/Laplacian.pdf.]
    Cerretelli C., C. H. K. Williamson, 2003: The physical mechanism for vortex merging. J. Fluid Mech., 475, 41- 77.10.1017/S00221120020028471d23548a0980665e88d9488b3709791fhttp%3A%2F%2Fjournals.cambridge.org%2Farticle_S0022112002002847http://journals.cambridge.org/article_S0022112002002847We study the physical mechanism for merging of two co-rotating trailing vortices. We directly measure the structure of the antisymmetric vorticity field that causes the vortices to merge, and we find that the form of the antisymmetric vorticity comprises two counter-rotating vortex pairs, whose induced velocity field readily pushes the two centroids together. If one observes the streamlines in a rotating reference frame, then one finds an inner and outer recirculating region of the flow bounded by a separatrix streamline. Initially, when the vortices grow large enough, diffusion across the separatrix places vorticity into the outer recirculating region of the flow, and this leads to the generation of the antisymmetric quadrupole, causing merger. There are four distinct phases in these interactions. The first stage is diffusive, while the second (convective) stage corresponds with the motion of the vortex centroids towards each other. A diffusive third stage (a symmetrisation process) causes the final merging into one vorticity structure, which is ultimately followed by the diffusion of the merged single vortex structure. Further details are found in Cerretelli & Williamson (JFM, 2002).
    Dritschel D. G., D. W. Waugh, 1992: Quantification of the inelastic interaction of un-equal vortices in two-dimensional vortex dynamics. Physics of Fluids A: Fluid Dynamics, 4, 1737- 1744.10.1063/1.85839440eb2a2d-bac5-4b94-a2e2-3b6c94b1d5cd64c158a96c5fcfd813f9611017795fcchttp%3A%2F%2Fscitation.aip.org%2Fcontent%2Faip%2Fjournal%2Fpofa%2F4%2F8%2F10.1063%2F1.858394refpaperuri:(eb85cab19c05d9ca2c1bbab983e0a0bd)http://scitation.aip.org/content/aip/journal/pofa/4/8/10.1063/1.858394The interaction of two isolated vortices having uniform vorticity is examined in detailed contour dynamics calculations, and quantified using a diagnostic that measures the coherence of the final state. The two vortices have identical vorticity, leaving two basic parameters that determine the evolution: the radius ratio and separation distance. It is found that the term ‘‘vortex merger’’ inadequately describes the general interaction that takes place. Five regimes are found: (1) elastic interaction, (2) partial straining‐out, (3) complete straining‐out, (4) partial merger, and (5) complete merger. Regime 5 is what used to be called ‘‘merger,’’ but occurs in less than one‐quarter of the parameter space. Contrary to popular belief, inelastic vortex interactions (IVI’s) do not always lead to vortex growth. In fact, in over half of the parameter space, smaller vortices are produced. These results bring into question commonly accepted ideas about nearly inviscid two‐dimensional turbulence.
    Ferreira R. N., W. H. Schubert, 1997: Barotropic aspects of ITCZ breakdown. J. Atmos. Sci., 54, 261- 285.bd77399ff1540417e84a6a2e895346a5http%3A%2F%2Fadsabs.harvard.edu%2Fcgi-bin%2Fnph-data_query%3Fbibcode%3D1997JAtS...54..261N%26db_key%3DPHY%26link_type%3DEJOURNAL/s?wd=paperuri%3A%282d47da21436eae1946b83d4d9712fcfe%29&filter=sc_long_sign&tn=SE_xueshusource_2kduw22v&sc_vurl=http%3A%2F%2Fadsabs.harvard.edu%2Fcgi-bin%2Fnph-data_query%3Fbibcode%3D1997JAtS...54..261N%26db_key%3DPHY%26link_type%3DEJOURNAL&ie=utf-8&sc_us=18297807624181243802
    Hendricks E. A., M. T. Montgomery, and C. A. Davis, 2004: The role of "Vortical" hot towers in the formation of tropical cyclone Diana (1984). J. Atmos. Sci., 61, 1209- 1232.10.1175/1520-0469(2004)061<1209:TROVHT>2.0.CO;25f7e5331-39df-44f2-961c-dd0816114c144e1e5c476bba9fd500245fdebb582948http://www.researchgate.net/publication/253063511_The_Role_of_Vortical''_Hot_Towers_in_the_Formation_of_Tropical_Cyclone_Diana_(1984)http://www.researchgate.net/publication/253063511_The_Role_of_Vortical''_Hot_Towers_in_the_Formation_of_Tropical_Cyclone_Diana_(1984)Abstract A high-resolution (3-km horizontal grid spacing) near-cloud-resolving numerical simulation of the formation of Hurricane Diana (1984) is used to examine the contribution of deep convective processes to tropical cyclone formation. This study is focused on the 3-km horizontal grid spacing simulation because this simulation was previously found to furnish an accurate forecast of the later stages of the observed storm life cycle. The numerical simulation reveals the presence of vortical hot towers, or cores of deep cumulonimbus convection possessing strong vertical vorticity, that arise from buoyancy-induced stretching of local absolute vertical vorticity in a vorticity-rich prehurricane environment. At near-cloud-resolving scales, these vortical hot towers are the preferred mode of convection. They are demonstrated to be the most important influence to the formation of the tropical storm via a two-stage evolutionary process: (i) preconditioning of the local environment via diabatic production of multiple small-scale lower-tropospheric cyclonic potential vorticity (PV) anomalies, and (ii) multiple mergers and axisymmetrization of these low-level PV anomalies. The local warm-core formation and tangential momentum spinup are shown to be dominated by the organizational process of the diabatically generated PV anomalies; the former process being accomplished by the strong vertical vorticity in the hot tower cores, which effectively traps the latent heat from moist convection. In addition to the organizational process of the PV anomalies, the cyclogenesis is enhanced by the aggregate diabatic heating associated with the vortical hot towers, which produces a net influx of low-level mean angular momentum throughout the genesis. Simpler models are examined to elucidate the underlying dynamics of tropical cyclogenesis in this case study. Using the Sawyer-揈liassen balanced vortex model to diagnose the macroscale evolution, the cyclogenesis of Diana is demonstrated to proceed in approximate gradient and hydrostatic balance at many instances, where local radial and vertical accelerations are small. Using a shallow water primitive equation model, a characteristic -渕oist- (diabatic) vortex merger in the cloud-resolving numerical simulation is captured in a large part by the barotropic model. Since a moist merger results in a stronger vortex and occurs twice as fast as a dry merger, it is inferred (consistent with related work) that a net low-level convergence can accelerate and intensify the merger process in the real atmosphere. Although the findings reported herein are based on a sole case study and thus cannot yet be generalized, it is believed the results are sufficiently interesting to warrant further idealized simulations of this nature.
    Holton J. R.2004: An Introduction to Dynamic Meteorology. 4th ed., Academic Press, 535 pp.6bf55d6fdd75e2bd869f655ee8c358achttp%3A%2F%2Fwww.elsevier.com%2Fbooks%2Fan-introduction-to-dynamic-meteorology-48%2Fholton%2F978-0-12-354355-4http://www.elsevier.com/books/an-introduction-to-dynamic-meteorology-48/holton/978-0-12-354355-4This revised text presents a cogent explanation of the fundamentals of meteorology, and explains storm dynamics for weather-oriented meteorologists. It discusses climate dynamics and the implications posed for global change. The Fourth Edition features a CD-ROM with MATLAB0003 exercises and updated treatments of several key topics. Much of the material is based on a two-term course for seniors majoring in atmospheric sciences.
    Huang H. M., X.-L. Xu, 2010: Simulation on motion of particles in vortex merging process. Applied Mathematics and Mechanics, 31, 461- 470.10.1007/s10483-010-0406-xbb34a9e408917afade2a481e5267601dhttp%3A%2F%2Fwww.cnki.com.cn%2FArticle%2FCJFDTotal-YYSL201004006.htmhttp://d.wanfangdata.com.cn/Periodical_yysxhlx-e201004006.aspxIn a two-phase flow,the vortex merging influences both the flow evolution and the particle motion.With the blobs-splitting-and-merging scheme,the vortex merging is calculated by a corrected core spreading vortex method (CCSVM).The particle motion in the vortex merging process is calculated according to the particle kinetic model.The results indicate that the particle traces are spiral lines with the same rotation direction as the spinning vortex.The center of the particle group is in agreement with that of the merged vortex.The merging time is determined by the circulation and the initial ratio of the vortex radius and the vortex center distance.Under a certain initial condition,a stretched particle trail is generated,which is determined by the viscosity,the relative position between the particles and the vortex,and the asymmetrical circulation of the two merging vortices.
    Jang W., H. Y. Chun, 2015: Characteristics of binary tropical cyclones observed in the Western North Pacific for 62 years (1951-2012). Mon. Wea. Rev., 143, 1749- 1761.
    Josser C., M. Rossi, 2007: The merging of two co-rotating vortices: A numerical study. European Journal of Mechanics-B/Fluids, 26, 779- 794.10.1016/j.euromechflu.2007.02.00592f63e9cdae9085936a04122b59fea28http%3A%2F%2Fwww.sciencedirect.com%2Fscience%2Farticle%2Fpii%2FS0997754607000295http://www.sciencedirect.com/science/article/pii/S0997754607000295Not Available
    Kieu C. Q., D. L. Zhang, 2009: Genesis of tropical storm Eugene (2005) from merging vortices associated with ITCZ breakdowns. Part II: Roles of vortex merger and ambient potential vorticity. J. Atmos. Sci., 67, 1980- 1996.10.1175/2008JAS2905.18ab2edd6-5e85-4358-99ed-480bf5d355c3769f8ae85b0fd2b667c01c3c12003aa5http%3A%2F%2Fadsabs.harvard.edu%2Fabs%2F2009JAtS...66.1980Krefpaperuri:(ba340e445233dfc0d39781f73090b1ff)http://adsabs.harvard.edu/abs/2009JAtS...66.1980KNot Available
    Kuo H. C., W. H. Schubert, C. L. Tsai, and Y. F. Kuo, 2008: Vortex interactions and Barotropic aspects of concentric eyewall formation. Mon. Wea. Rev., 136, 5183- 5198.10.1175/2008MWR2378.1e8913d7dd52dec0a594585c16432bd00http%3A%2F%2Fadsabs.harvard.edu%2Fabs%2F2008MWRv..136.5183Khttp://adsabs.harvard.edu/abs/2008MWRv..136.5183KConcentric eyewall formation can be idealized as the interaction of a tropical cyclone core with nearby weaker vorticity of various spatial scales. This paper considers barotropic aspects of concentric eyewall formation from modified Rankine vortices. In this framework, the following parameters are found to be important in concentric eyewall formation: vorticity strength ratio, separation distance, companion vortex size, and core vortex skirt parameter. A vorticity skirt on the core vortex affects the filamentation dynamics in two important ways. First, the vorticity skirt lengthens the filamentation time, and therefore slows moat formation in the region just outside the radius of maximum wind. Second, at large radii, a skirted core vortex induces higher strain rates than a corresponding Rankine vortex and is thus more capable of straining out the vorticity field far from the core. Calculations suggest that concentric structures result from binary interactions when the small vortex is at least 409恪6 times as strong as the larger companion vortex. An additional requirement is that the separation distance between the edges of the two vortices be less than 609恪7 times the smaller vortex radius. Broad moats form when the initial companion vortex is small, the vorticity skirt outside the radius of maximum wind is small, and the strength ratio is large. In concentric cases, an outer vorticity ring develops when the initial companion vortex is large, the vorticity skirt outside the radius of maximum wind is small, and the strength ratio is not too large. In general, when the companion vortex is 3 times as strong as the core vortex and the separation distance is 409恪6 times the radius of the smaller vortex, a core vortex with a vorticity skirt produces concentric structures. In contrast, a Rankine vortex produces elastic interaction in this region of parameter space. Thus, a Rankine vortex of sufficient strength favors the formation of a concentric structure closer to the core vortex, while a skirted vortex of sufficient strength favors the formation of concentric structures farther from the core vortex. This may explain satellite microwave observations that suggest a wide range of radii for concentric eyewalls.
    Land er, M., G. J. Holland, 1993: On the interaction of tropical-cyclone-scale vortices. I: Observations. Quart. J. Roy. Meteor. Soc., 119, 1347- 1361.10.1002/qj.49711951406702d82b9d057c113794da41cc0329d1bhttp%3A%2F%2Fonlinelibrary.wiley.com%2Fdoi%2F10.1002%2Fqj.49711951406%2Fabstracthttp://onlinelibrary.wiley.com/doi/10.1002/qj.49711951406/abstractAbstract A detailed analysis is made of the observed behaviour in interaction, tropical-cyclone-scale vortices in the western North Pacific region. It is found that all multiple-vortex interactions can be broken down into a common model of binary interaction. The classical Fujiwhara model of converging cyclonic rotation about a centroid followed by merger is rarely followed. Capture tends to occur rapidly, within several hours, and is followed by a period of relatively stable cyclonic orbit. Cyclone merger occurs by one vortex experiencing a loss of convective organization, followed by horizontal shearing and incorporation into the outer circulation of the other vortex. However, a substantial proportion of interacting cyclones escape from the interaction, and the changeover from a stable orbiting configuration occurs rapidly. A model of binary interaction is presented. Cases where swarms of mesoscale vortices are formed in convectively active regions without tropical cyclones are also documented. These vortices have a much narrower range of influence (a few hundred kilometres) then that observed for tropical cyclones. When groups of vortices come within this range they are observed to conform to the same interaction model as observed for tropical cyclones.
    Lansky I. M., T. M. O'Neil, and D. A. Schecter, 1997: A theory of vortex merger. Physical Review Letters, 79, 1479- 1482.01c7f760d2c3422282cbf0f7799a90a4http%3A%2F%2Fscitation.aip.org%2Fgetabs%2Fservlet%2FGetabsServlet%3Fprog%3Dnormal%26id%3DPRLTAO000079000008001479000001%26idtype%3Dcvips%26gifs%3DYes/s?wd=paperuri%3A%285be60f68cc06ab95c38f751957dbeb31%29&filter=sc_long_sign&tn=SE_xueshusource_2kduw22v&sc_vurl=http%3A%2F%2Fscitation.aip.org%2Fgetabs%2Fservlet%2FGetabsServlet%3Fprog%3Dnormal%26id%3DPRLTAO000079000008001479000001%26idtype%3Dcvips%26gifs%3DYes&ie=utf-8&sc_us=16291279055777527212
    Luo D. H., J. Cha, L. H. Zhong, and A. G. Dai, 2014: A nonlinear multiscale interaction model for atmospheric blocking: The eddy-blocking matching mechanism. Quart. J. Roy. Meteor. Soc., 140, 1785- 1808.10.1002/qj.23379a49966a-3117-4422-b21c-9cd6beceab5d69a157b05f48c4cc885cc7fd0f3211a0http%3A%2F%2Fonlinelibrary.wiley.com%2Fresolve%2Fdoi%3FDOI%3D10.1002%252Fqj.2337refpaperuri:(ef5d30768a06fa5020316496877d1504)http://onlinelibrary.wiley.com/resolve/doi?DOI=10.1002%2Fqj.2337In this article, a nonlinear multiscale interaction (NMI) model is used to propose an eddy‐blocking matching (EBM) mechanism to account for how synoptic eddies reinforce or suppress a blocking flow. It is shown that the spatial structure of the eddy vorticity forcing (EVF) arising from upstream synoptic eddies determines whether an incipient block can grow into a meandering blocking flow through its interaction with the transient synoptic eddies from the west. Under certain conditions, the EVF exhibits a low‐frequency oscillation on time‐scales of 2–3 weeks. During the EVF phase with a negative‐over‐ positive dipole structure, a blocking event can be resonantly excited through the transport of eddy energy into the incipient block by the EVF. As the EVF changes into an opposite phase, the blocking decays. The NMI model produces life cycles of blocking events that resemble observations. Moreover, it is shown that the eddy north–south straining is a response of the eddies to a dipole‐ or Ω‐type block. In our model, as in observations, two synoptic anticyclones (cyclones) can attract and merge with one another as the blocking intensifies, but only when the feedback of the blocking on the eddies is included. Thus, we attribute the eddy straining and associated vortex interaction to the feedback of the intensified blocking on synoptic eddies. The results illustrate the concomitant nature of the eddy deformation, the role of which, as a potential vorticity source for the blocking flow, becomes important only during the mature stage of a block. Our EBM mechanism suggests that an incipient block flow is amplified (or suppressed) under certain conditions by the EVF coming from the upstream of the blocking region. This also suggests that weather and climate models need to be run with a grid size below 100 km in order to simulate the matching EVF and thus atmospheric blocking.
    Montgomery M. T., J. Enagonio, 1998: Tropical cyclogenesis via convectively forced vortex Rossby waves in a three-dimensional quasigeostrophic model. J. Atmos. Sci., 55, 3176- 3207.10.1175/1520-0469(1998)055<3176:TCVCFV>2.0.CO;2fd45a550a24949f394b26b9e47fb1f9dhttp%3A%2F%2Fadsabs.harvard.edu%2Fabs%2F1998JAtS...55.3176Mhttp://adsabs.harvard.edu/abs/1998JAtS...55.3176MAbstract This work investigates the problem of tropical cyclogenesis in three dimensions. In particular, the authors examine the interaction of small-scale convective disturbances with a larger-scale vortex circulation in a nonlinear quasigeostrophic balance model. Convective forcing is parameterized by its estimated net effect on the potential vorticity (PV) field. Idealized numerical experiments show that vortex intensification proceeds by ingestion of like-sign potential vorticity anomalies into the parent vortex and expulsion of opposite-sign potential vorticity anomalies during the axisymmetrization process. For the finite-amplitude forcing considered here, the weakly nonlinear vortex Rossby wave mean-flow predictions for the magnitude and location of the spinup are in good agreement with the model results. Vortex development is analyzed using Lagrangian trajectories, Eliassen-alm flux vectors, and the Lorenz energy cycle. Using numerical estimates of the magnitude of PV injection based on previous observational and theoretical work, the authors obtain spinup to a 15 m s 1 cyclone on realistic timescales. Simulation of a midlevel vortex with peripheral convection shows that axisymmetrization results in the spinup of a surface cyclone. The axisymmetrization mechanism demonstrates the development of a warm-core vortex. The relative contribution from eddy-heat and eddy-momentum fluxes to the warm core structure of the cyclone is investigated. The vortex spinup obtained shows greater than linear dependence on the forcing amplitude, indicating the existence of a nonlinear feedback mechanism associated with the vortex Rossby waves. Building on recent work by several authors, this work further clarifies the significance of the axisymmetrization process for the problem of tropical cyclogenesis. The theory is shown to be consistent with published observations of tropical cyclogenesis. Further observational and modeling tests of the theory, specific to the dynamics examined here, are proposed.
    Nica M., 2011: Eigenvalues and Eigenfunctions of the Laplacian, The Waterloo Mathematics Review, 1, 23- 34.
    Prieto R., B. D. McNoldy, S. R. Fulton, and W. H. Schubert, 2003: A classification of binary tropical cyclone-like vortex interactions. Mon. Wea. Rev., 131, 2656- 2666.10.1175/1520-0493(2003)131<2656:ACOBTC>2.0.CO;2dd2d5f4c-d2f9-45ea-9136-c0b7a80b29d517e96bf4facbc8bf8bb4cabc164cf8b4http%3A%2F%2Fadsabs.harvard.edu%2Fabs%2F2003MWRv..131.2656Prefpaperuri:(166a20a958d21915afbe508ba483d078)http://adsabs.harvard.edu/abs/2003MWRv..131.2656PNot Available
    Rodrguez-Marroyo, R., À. Viùdez, S. Ruiz, 2011: Vortex merger in oceanic tripoles. J. Phys. Oceanogr., 41, 1239- 1251.10.1175/2011JPO4582.1c739f2c1468473fd3c3da47c634f4964http%3A%2F%2Fconnection.ebscohost.com%2Fc%2Farticles%2F62522986%2Fvortex-merger-oceanic-tripoleshttp://connection.ebscohost.com/c/articles/62522986/vortex-merger-oceanic-tripolesAbstract A new type of vortex merger is experimentally reported and numerically investigated. The merging process of two anticyclones under the influence of a cyclone (a three-vortex interaction) was observed in sea surface height (SSH) altimetry maps south of the Canary Islands. This three-vortex interaction is investigated using a process-oriented three-dimensional (3D), Boussinesq, and f -plane numerical model that explicitly conserves potential vorticity (PV) on isopycnals. The initial conditions consist of three static and inertially stable baroclinic vortices: two anticyclones and one cyclone. The vortex cores form a triangle in a configuration similar to that found south of the Canary Islands. The numerical results show, in agreement with SSH observations, that two corotating vortices, sufficiently close to each other and in presence of a third counterrotating vortex, merge, leading to a new elongated vortex, which couples with the counterrotating vortex, forming a dipole. Thus, the merging process occurred south of the Canary Islands is consistent with simplified vortex dynamics (basically PV conservation). The merging process depends on the initial PV density extrema, vertical extent, and the angle spanned by the corotating vortices. It is found that the presence of the third counterrotating vortex importantly affects the critical angle of merger and the processes of axisymmetrization and filamentation associated with the two corotating merging vortices. The torque exerted by the counterrotating vortex on the two corotating vortices delays, but does not prevent, their merger.
    Simpson J., E. Ritchie, G. J. Holland , J. Halverson, and S. Stewart, 1997: Mesoscale interactions in tropical cyclone genesis. Mon. Wea. Rev., 125, 2643- 2661.4a0bbb8305845d225ad7c60c9f4255cchttp%3A%2F%2Fadsabs.harvard.edu%2Fcgi-bin%2Fnph-data_query%3Fbibcode%3D1997MWRv..125.2643S%26db_key%3DPHY%26link_type%3DABSTRACT%26high%3D545ab6db6a23402/s?wd=paperuri%3A%2853ff85988c4ef4cd5b7bf027a238077e%29&filter=sc_long_sign&tn=SE_xueshusource_2kduw22v&sc_vurl=http%3A%2F%2Fadsabs.harvard.edu%2Fcgi-bin%2Fnph-data_query%3Fbibcode%3D1997MWRv..125.2643S%26db_key%3DPHY%26link_type%3DABSTRACT%26high%3D545ab6db6a23402&ie=utf-8&sc_us=16492626511897460957
    Tallapragada V., C. Kieu, 2014: Real-Time Forecasts of Typhoon Rapid Intensification in the North Western Pacific Basin with the NCEP Operational HWRF Model. Tropical Cyclone Research and Review, 3, 63- 77.c42a59c6df6a4dde59cb2379d9a129a1http%3A%2F%2Fwww.researchgate.net%2Fpublication%2F268035291_Real-Time_Forecasts_of_Typhoon_Rapid_Intensification_in_the_North_Western_Pacific_Basin_with_the_NCEP_Operational_HWRF_Modelhttp://www.researchgate.net/publication/268035291_Real-Time_Forecasts_of_Typhoon_Rapid_Intensification_in_the_North_Western_Pacific_Basin_with_the_NCEP_Operational_HWRF_Model
    Wang C.-C., G. Magnusdottir, 2006: The ITCZ in the central and eastern Pacific on synoptic time scales. Mon. Wea. Rev., 134, 1405- 1421.3a71a909d523c94534f6573fd7767ebehttp%3A%2F%2Fadsabs.harvard.edu%2Fabs%2F2006mwrv..134.1405w/s?wd=paperuri%3A%28f50e3ef7aeea57017b83f21c59a6993f%29&filter=sc_long_sign&tn=SE_xueshusource_2kduw22v&sc_vurl=http%3A%2F%2Fadsabs.harvard.edu%2Fabs%2F2006mwrv..134.1405w&ie=utf-8&sc_us=8885453622267742853
    Yamazaki A., H. Itoh, 2013: Vortex-vortex interactions for the maintenance of blocking. Part I: The selective absorption mechanism and a case study. J. Atmos. Sci., 70, 725- 742.10.1175/JAS-D-11-0295.1152d1b90-2369-4eba-b7b5-c2831bdd708a9712426d49fb5355c978003a42cc039fhttp%3A%2F%2Fonlinelibrary.wiley.com%2Fresolve%2Freference%2FXREF%3Fid%3D10.1175%2FJAS-D-11-0295.1refpaperuri:(f93e9fc9016ed6d230b04b217797b272)http://onlinelibrary.wiley.com/resolve/reference/XREF?id=10.1175/JAS-D-11-0295.1Not Available
    Yasuda I., 1995: Geostrophic vortex merger and streamer development in the ocean with special reference to the merger of Kuroshio warm core rings. J. Phys. Oceanogr., 25, 979- 996.10.1175/1520-0485(1995)025<0979:GVMASD>2.0.CO;21a29dc9813736ef35248b36e0abf27f1http%3A%2F%2Fadsabs.harvard.edu%2Fabs%2F1995JPO....25..979Yhttp://adsabs.harvard.edu/abs/1995JPO....25..979YNot Available
    Yu Z. F., X. D. Liang, H. Yu, and J. C. L. Chan, 2010: Mesoscale vortex generation and merging process: A case study associated with a post-landfall tropical depression. Adv. Atmos. Sci.,27, 356-370, doi: 10.1007/s00376-009-8091-x.10.1007/s00376-009-8091-x4a11c1fe48fb608522002fd605b0e3a6http%3A%2F%2Fd.wanfangdata.com.cn%2FPeriodical_dqkxjz-e201002014.aspxhttp://d.wanfangdata.com.cn/Periodical_dqkxjz-e201002014.aspxAn observational analysis of satellite blackbody temperature (TBB) data and radar images suggests that the mesoscale vortex generation and merging process appeared to be essential for a tropical-depression-related heavy rain event in Shanghai, China. A numerical simulation reproduced the observed mesoscale vortex generation and merging process and the corresponding rain pattern, and then the model outputs were used to study the related dynamics through diagnosing the potential vorticity (PV) equation. The tropical depression (TD) was found to weaken first at lower levels and then at upper levels due to negative horizontal PV advection and diabatic heating effects. The meso-vortices developed gradually, also from the lower to the upper levels, as a result of positive horizontal PV advection and diabatic heating effects in the downshear left quadrant of the TD. One of these newly-generated vortices, V1, replaced the TD ultimately, while the other two, V2 and V3, merged due to the horizontal PV advection process. Together with the redevelopment of V1, the merging of V2 and V3 triggered the very heavy rain in Shanghai.
  • [1] CHEN Lianshou, LUO Zhexian, 2004: Interaction of Typhoon and Mesoscale Vortex, ADVANCES IN ATMOSPHERIC SCIENCES, 21, 515-528.  doi: 10.1007/BF02915719
    [2] Melinda S. PENG, Jiayi PENG, Tim LI, Eric HENDRICKS, 2014: Effect of Baroclinicity on Vortex Axisymmetrization. Part I: Barotropic Basic Vortex, ADVANCES IN ATMOSPHERIC SCIENCES, 31, 1256-1266.  doi: 10.1007/s00376-014-3237-x
    [3] ZHONG Wei, LU Han-Cheng, Da-Lin ZHANG, 2010: Mesoscale Barotropic Instability of Vortex Rossby Waves in Tropical Cyclones, ADVANCES IN ATMOSPHERIC SCIENCES, 27, 243-252.  doi: 10.1007/s00376-009-8183-7
    [4] ZHANG Ming, ZHAO Yanling, HUANG Hong, LIANG Danqing, 2007: The Generalized Energy Equation and Instability in the Two-layer Barotropic Vortex, ADVANCES IN ATMOSPHERIC SCIENCES, 24, 147-151.  doi: 10.1007/s00376-007-0147-1
    [5] Jiayi PENG, Melinda S. PENG, Tim LI, Eric HENDRICKS, 2014: Effect of Baroclinicity on Vortex Axisymmetrization. Part II: Baroclinic Basic Vortex, ADVANCES IN ATMOSPHERIC SCIENCES, 31, 1267-1278.  doi: 10.1007/s00376-014-3238-9
    [6] Na LI, Lingkun RAN, Shouting GAO, 2016: The Impact of Deformation on Vortex Development in a Baroclinic Moist Atmosphere, ADVANCES IN ATMOSPHERIC SCIENCES, 33, 233-246.  doi: 10.1007/s00376-015-5082-y
    [7] Tianju WANG, Zhong ZHONG, Ju WANG, 2018: Vortex Rossby Waves in Asymmetric Basic Flow of Typhoons, ADVANCES IN ATMOSPHERIC SCIENCES, 35, 531-539.  doi: 10.1007/s00376-017-7126-y
    [8] Gao Shouting, 2000: The Instability of the Vortex Sheet along the Shear Line, ADVANCES IN ATMOSPHERIC SCIENCES, 17, 525-537.  doi: 10.1007/s00376-000-0016-7
    [9] CHEN Gong, and LI Guoping, 2014: Dynamic and Numerical Study of Waves in the Tibetan Plateau Vortex, ADVANCES IN ATMOSPHERIC SCIENCES, 31, 131-138.  doi: 10.1007/s00376-013-1035-5
    [10] Shuhua YU, Wenliang GAO, Dixiang XIAO, Jun PENG, 2016: Observational Facts Regarding the Joint Activities of the Southwest Vortex and Plateau Vortex after Its Departure from the Tibetan Plateau, ADVANCES IN ATMOSPHERIC SCIENCES, 33, 34-46.  doi: 10.1007/s00376-015-5039-1
    [11] Guanshun ZHANG, Jiangyu MAO, Yimin LIU, Guoxiong WU, 2021: PV Perspective of Impacts on Downstream Extreme Rainfall Event of a Tibetan Plateau Vortex Collaborating with a Southwest China Vortex, ADVANCES IN ATMOSPHERIC SCIENCES, 38, 1835-1851.  doi: 10.1007/s00376-021-1027-9
    [12] JIANG Yongqiang, WANG Yuan, HUANG Hong, 2012: A Study on the Dynamic Mechanism of the Formation of Mesoscale Vortex in Col Field, ADVANCES IN ATMOSPHERIC SCIENCES, 29, 1215-1226.  doi: 10.1007/s00376-012-1186-9
    [13] Xiangzhou SONG†, Rui Xin HUANG, Dexing WU, Fangli QIAO, Guansuo WANG, 2019: Geostrophic Spirals Generated by the Horizontal Diffusion of Vortex Stretching in the Yellow Sea, ADVANCES IN ATMOSPHERIC SCIENCES, 36, 219-230.  doi: 10.1007/s00376-018-8091-9
    [14] Yongqiang JIANG, Yuan WANG, Chaohui CHEN, Hongrang HE, Hong HUANG, 2019: A Numerical Study of Mesoscale Vortex Formation in the Midlatitudes: The Role of Moist Processes, ADVANCES IN ATMOSPHERIC SCIENCES, 36, 65-78.  doi: 10.1007/s00376-018-7234-3
    [15] WANG Zhi, GAO Kun, 2003: Sensitivity Experiments of an Eastward-Moving Southwest Vortex to Initial Perturbations, ADVANCES IN ATMOSPHERIC SCIENCES, 20, 638-649.  doi: 10.1007/BF02915507
    [16] REN Rongcai, Ming CAI, 2006: Polar Vortex Oscillation Viewed in an Isentropic Potential Vorticity Coordinate, ADVANCES IN ATMOSPHERIC SCIENCES, 23, 884-900.  doi: 10.1007/s00376-006-0884-6
    [17] LI Lun, ZHANG Renhe, WEN Min, 2011: Diagnostic Analysis of the Evolution Mechanism for a Vortex over the Tibetan Plateau in June 2008, ADVANCES IN ATMOSPHERIC SCIENCES, 28, 797-808.  doi: 10.1007/s00376-010-0027-y
    [18] LI Lin, LI Chongyin, PAN Jing, TAN Yanke, 2012: On the Differences and Climate Impacts of Early and Late Stratospheric Polar Vortex Breakup, ADVANCES IN ATMOSPHERIC SCIENCES, 29, 1119-1128.  doi: 10.1007/s00376-012-1012-4
    [19] Shuanglin Li, 2010: A Comparison of Polar Vortex Response to Pacific and Indian Ocean Warming, ADVANCES IN ATMOSPHERIC SCIENCES, 27, 469-482.  doi: 10.1007/s00376-009-9116-1
    [20] FU Shenming, SUN Jianhua, ZHAO Sixiong, LI Wanli, 2011: The Energy Budget of a Southwest Vortex With Heavy Rainfall over South China, ADVANCES IN ATMOSPHERIC SCIENCES, 28, 709-724.  doi: 10.1007/s00376-010-0026-z

Get Citation+

Export:  

Share Article

Manuscript History

Manuscript received: 07 January 2016
Manuscript revised: 26 March 2016
Manuscript accepted: 25 April 2016
通讯作者: 陈斌, bchen63@163.com
  • 1. 

    沈阳化工大学材料科学与工程学院 沈阳 110142

  1. 本站搜索
  2. 百度学术搜索
  3. 万方数据库搜索
  4. CNKI搜索

The Dynamics of Barotropic Vortex Merging

  • 1. Department of Geological Sciences, Indiana University, Bloomington, Indiana 47405, USA

Abstract: The merging of multiple vortices is a fundamental process of the dynamics of Earth's atmosphere and oceans. In this study, the interaction of like-signed vortices is analytically and numerically examined in a framework of two-dimensional inviscid barotropic flows. It is shown that barotropic vortex interaction turns out to be more intricate than simple merging scenarios often assumed in previous studies. Some particular configurations exist in which the vortex merging process is never complete despite strong interaction of like-signed vortices, regardless of the strengths or distances between the vortices. While the conditions for a complete vortex merging process introduced in this study appear to be too strict for most practical applications, this study suggests that careful criteria for vortex mergers should be properly defined when simulating the interaction of vortices, because the merging may not always result in a final enhanced circulation at the end of the interaction, as usually assumed in the literature.

1. Introduction
  • The vortex merging process by which multiple vortices of the same sign interact and are eventually aggregated into a broader circulation at the end of their interaction plays an important role in studies of atmospheric and oceanic circulations. Various fluid processes have been shown to be characterized by well-defined and coherent vortex interactions ranging from minute fluid vortex eddies to large-scale circulations (e.g., Yasuda, 1995; Ferreira and Schubert, 1997; Lansky et al., 1997; Cerretelli and Williamson, 2003; Josser and Rossi, 2007; Rodríguez-Marroyo et al., 2011; Yamazaki and Itoh, 2013; Luo et al., 2014; Tallapragada and Kieu, 2014). For specific mesoscale circulations in the atmosphere, vortex mergers are often connected to swift changes in development of tropical disturbances, which have significant impacts on the formation and subsequent track and intensity changes of tropical cyclones (Lander and Holland, 1993; Simpson et al., 1997; Ferreira and Schubert, 1997; Kieu and Zhang, 2009; Yu et al., 2010; Jang and Chun, 2015). At the smaller convective scales, coalescence of deep convective towers in the atmosphere——the so-called vortical hot towers——has been recently suggested as a pathway for the upscale growth of tropical depressions during the early phase of tropical cyclogenesis ["the vortical hot towers hypothesis", e.g., (Montgomery and Enagonio, 1998) and (Hendricks et al., 2004)].

    Despite extensive numerical studies on the vortex merging process for a wide range of scales, it is nevertheless intriguing that the process of merging vortices has never been precisely defined. Specifically, it is not clear in general if the process of merging multiple vortices into a single vorticity patch can be fully complete at the end of the vortex interaction, or if the final circulation must be enhanced as a result of the vortex merger. For example, modeling studies of vortex merger by (Dritschel and Waugh, 1992), (Prieto et al., 2003) and (Kuo et al., 2008) revealed that the merger depends on the strength of each different vortex, the distance between the vortices, and the relative size of the vortices. In all cases, the full vortex merger does not appear to be realized, even for cases that belong to the complete merger category.

    In this study, the vortex merging process is investigated for a special class of 2D flows that is barotropic and inviscid, and the necessary conditions for the merger to be considered complete at the end of the merging process are examined. The approach is based essentially on the unique characteristics of the barotropic vorticity equation, which allow for rigorous analyses of the vorticity dynamics under some specific boundary conditions. While these analyses are strictly valid only for the inviscid barotropic dynamics, due to some technical constraints that may not be applicable to more general vortex merging processes, the modest aim in this study is to present an approach that could highlight the subtlety of the vortex merging and interpretation that has not been adequately addressed in previous studies.

    The rest of the paper is organized as follows. The next section introduces a definition for a complete vortex merger in the framework of the barotropic flows. Analyses of the vorticity dynamics and the evolution of the merging processes are then presented in detail under different boundary configurations. Some concluding remarks are given in the final section.

2. Barotropic dynamics
  • Although vortex merging processes in both 2D and 3D flows have been extensively demonstrated in numerous modeling studies, the fact that the merging varies strongly with different scales and dynamical systems renders it difficult to understand whether and how the merging process really occurs. Depending on the relative size and distances between vortices, a study of the vortex merging in (Dritschel and Waugh, 1992) showed that there are generally five different flow regimes at the end of the merging, which include (1) elastic interaction, (2) complete merger, (3) partial merger, (4) partial straining out, and (5) complete straining out for the 2D flows. Such a classification of merging processes was later investigated in many numerical experiments (e.g., Yasuda, 1995; Prieto et al., 2003; Kuo et al., 2008), which confirmed these regimes systematically in both the barotropic and 3D framework.

    Following the innovative contour dynamics approach presented in (Dritschel and Waugh, 1992), a quantitative criterion to classify the vortex merging process for mesoscale atmospheric flows was introduced in (Prieto et al., 2003) and (Kuo et al., 2008), which is based on the ratio of the final to the initial circulation for each participating vortex; the circulation ratio is equal to 1 for complete merger, and zero for elastic interaction. Such a definition of vortex merger based on global contour circulation has the benefit of efficiently removing filamentary structures and isolating coherent vorticity patches, but it subjectively depends on how one defines the contours around which the circulation can be computed, as mentioned in (Dritschel and Waugh, 1992). This explains why the complete merger regime in (Prieto et al., 2003) and (Kuo et al., 2008) does not really exhibit the complete merging of two vortices into a single vorticity patch at the end of the merging process, but instead displays a spread of one vortex in the form of vorticity skirts wrapping around the other vortex [e.g., Prieto et al. (2003, Fig. 2a) and Kuo et al. (2008, Fig. 9)].

    Given the lack of a rigorous definition for the vortex merging process, which is needed to better define and understand the evolution of the vortex dynamics, this subsection begins by first redefining the merging process from a barotropic flow perspective, to facilitate subsequent analyses of the vortex merger. Note a specific property that one would expect from a complete vortex merging process is that the end product of a merging process should be a stationary vortex, which would not evolve by itself or break down at all later time. This condition is necessary so that it can at least be agreed whether or not the vortex merger is complete. One could relax this condition by allowing for cases with some type of periodic oscillation instead of a stationary vortex patch at the end of the vortex merger. However, as shown in the next section, certain configurations in the barotropic framework do not even approach an equilibrium with a single vortex patch at the end of the merging, let alone oscillating around an equilibrium. The aim in this subsection is to express such a stationary merger condition more quantitatively, and use this condition to examine how and when the vortex dynamics will approach the stationary limit.

    To present the characteristics of vortex merging in an analytically tractable manner, let us start first with the inviscid barotropic equation in an f-plane (see Holton, 2004) as follows: \begin{equation} \dfrac{\partial}{\partial t}({\nabla}^2\psi)+J(\psi,{\nabla}^2\psi)=0 , (1)\end{equation} where ψ(x,y,t) is assumed to be at least a real square-integrable function over a given domain Ω R2. Equation (1) accepts a stationary solution Ψ(x,y) if \begin{equation*} J(\Psi,{\nabla}^2\Psi)=0 , \end{equation*} or equivalently \begin{equation} \dfrac{\partial\Psi}{\partial y}\dfrac{\partial({\nabla}^2\Psi)}{\partial x}=\dfrac{\partial\Psi}{\partial x}\dfrac{\partial({\nabla}^2\Psi)}{\partial y} .(2) \end{equation} A symmetry in the x and y derivatives in Eq. (2) immediately suggests that this equation will be generally satisfied if the following relationship holds: \begin{equation} {\nabla}^2\Psi=\lambda\Psi , (3)\end{equation}

    where Λ is an eigenvalue. Equation (3) is familiar and indicates that the stationary solution Ψ(x,y) is nothing but an eigenfunction of the Laplacian operator . The existence of such a stationary solution is of key importance for studying barotropic vortex evolution, because if the complete merging of multiple vortices can indeed take place, then one would expect eventually that the final state of the vortex dynamics would settle down to some "stable" configuration, which is exactly what a stationary solution is supposed to be. For most applications in the atmosphere, it suffices to assume also that the streamfunction on Ω has a compact support such that the Laplacian operator is self-adjoint (i.e., \(\langle \Delta f,g\rangle=\langle f,\Delta g\rangle\)), where f and g are two arbitrary smooth functions defined on Ω. This ensures that the eigenvalues of the Laplacian are all positive, 0<Λ123, and the corresponding eigenfunctions 123,…} form an orthogonal basis according to the Spectral Theorem (Nica, 2011).

    Figure 1.  Illustration of the eigenfunctions $\varphi_k,\lambda(\theta,\lambda)$ of the Laplacian operator with different values of $\lambda$ and $k$.

    It should be noted that, strictly speaking, the pure eigenfunctions of the Laplacian operator are not the most general stationary solution of Eq. (2). However, given the fact that the spectrum of the Laplacian eigenfunctions are complete for homogeneous boundary conditions from the Spectral Theorem, any stationary solutions with the same boundary condition will therefore have to be a superposition of the Laplacian eigenfunctions. As such, examining the characteristics of the Laplacian eigenfunctions can provide insights into general long-term behaviors of the stationary solutions of the barotropic vorticity equation [Eq. (1)].

    With well-established properties of the eigenfunctions of the Laplacian operator, it is apparent that there are an infinite number of stationary states for the barotropic vorticity equation; each corresponds to one eigenfunction of the Laplacian operator. For a circle domain Ω, an eigenfunction φk,Λ(θ,r) corresponding to an eigenvalue (Λ,k) is given by (e.g., Canzani, 2013): \begin{equation} \varphi_{k,\lambda}(\theta,r)=(a_k\cos(k\theta)+b_k\sin(k\theta))J_k(\sqrt{\lambda}r) , (4)\end{equation} where ak,bk are constants, θ is the azimuthal coordinate variable, and Jk(x) is the k-order Bessel functions defined as follows: \begin{equation} J_k(x)=\sum_{n=0}^\infty\dfrac{(-1)^n}{n!(n+k)!}\left(\dfrac{x}{2}\right)^{k+2n} . (5)\end{equation} As seen in Fig. 1, these eigenfunctions display a wide range of shapes, depending on the value of the radial eigenvalue Λ and the azimuthal eigenvalue k. For a typical vortex merging problem that is expected to settle down towards a stationary state, we note however that it is the eigenfunction with no θ-dependence, i.e., any eigenmode with k=0, that is most anticipated at the end of the vortex merger. This is because these k=0 states are the only configurations that possess a vortex concentrated at the domain center and diminishes radially outwards (assuming that one can always arrange the domain in such a way that an initial vortex distribution has its mass-weighted vorticity center located at the domain center). Any other configuration with \(k\neq 0\) would correspond to a distribution of positive vorticity centers located at different places, which are not expected for the "complete" vortex merging from the symmetry perspective.

    The above observation of the radial symmetry of the eigenfunctions thus allows us to precisely define conditions for a complete merging process. Assume one starts with an arbitrary distribution of vorticity on a domain Ω with a null boundary condition for which the streamfunction ψ(r,θ,t) can be expanded as follows: \begin{equation} \psi(r,\theta,t)=\sum_{\lambda,k}c_{k,\lambda}(t)\varphi_{k,\lambda}(\theta,r), (6)\end{equation}

    where ck,Λ are expansion coefficients. It is then clear that the evolution of the barotropic flow under the governing equation [Eq. (1)] will eventually approach a stationary axisymmetric configuration if the following conditions hold: \begin{equation} \left\{ \begin{array}{l@{\quad}l} \lim\limits_{t\to\infty}c_{k,\lambda}(t)=0 & \forall k\in N^+\\[2mm] \lim\limits_{t\to\infty}\dfrac{dc_{k,\lambda}(t)}{dt}=0 & \forall k,\lambda>0\\[3mm] \exists\lambda>0|\lim\limits_{t\to\infty}c_{0,\lambda}(t)\neq 0 \end{array} \right.. (7)\end{equation} Indeed, if these conditions are satisfied after a sufficiently long period of time, then the merging process can be claimed as complete because the flow settles down to a specific superposition of stationary axisymmetric eigenfunctions with a resulting vortex located at the center. Such a complete merger will directly support the assumption of aggregating multiple like-signed vortices, as often assumed in previous studies of vortex interaction. We should mention that the condition represented by Eq. (7) by no means dictates that the end phase of the merging process has to be exactly an eigenfunction of the Laplacian operator. The final vortex could in fact be a superposition of infinite eigenfunctions φ0,Λ(θ,Λ), provided that the superposition ensures a peak vorticity at the center to meet with the expectation of a complete vortex merger. The problem will be much less flexible for different boundary conditions or different domain topologies. Nonetheless, the existence of an orthogonal basis that corresponds to eigenfunctions of the Laplacian operator gives us a unique way to shed light onto these merging processes in some specific applications, at least from the barotropic flow perspective, to which the focus turns next.

    Figure 2.  Illustration of eigenfunctions $\varphi_m,n$ in a square domain with periodic boundary conditions for several different values of $(m,n)$.

  • In this section, the above definition of the complete vortex merger is applied to examine the vortex dynamics in a limited-area domain. The objective in this subsection is to investigate how an arbitrary distribution of vorticity at the initial time in a square domain would evolve and under what conditions the merging process can be considered complete, as defined by the complete merger conditions [i.e., Eq. (7)]. To approach the problem of modeling the vortex dynamics in as practical a way as possible, a specific square domain [0,L]× [0,L] with periodic boundary conditions is hereinafter considered, where L is a given domain size. The compact-support requirement to ensure the self-adjoint property of the Laplacian operator puts a strong constraint on the set of the eigenfunctions of Eq. (3), which are now given for each specific mode (m,n) as follows: \begin{equation} \varphi_{m,n}(x,y)=\sin\left(\dfrac{m\pi}{L}x\right)\sin\left(\dfrac{n\pi}{L}y\right) , (8)\end{equation} with \begin{equation*} \lambda_{m,n}=\dfrac{\pi^2(m^2+n^2)}{L^2}\quad \forall m,n\in N^+ . \end{equation*} Figure 2 illustrates the first few eigenfunctions φm,n(x,y). Unlike a circular disk domain that can support many axisymmetric eigenmodes toward which the barotropic flow could approach at the end of the vortex merger, the only mode that possesses the maximum vorticity at the center of the square domain is m=1,n=1. Based again on the symmetry argument, the conditions for a vortex merging process to be complete in a square domain are thus reduced to \begin{equation} \left\{ \begin{array}{l@{\quad}l} \lim\limits_{t\to\infty}c_{m,n}(t)=0 & \forall m>1,n>1\\[1mm] \lim\limits_{t\to\infty}\dfrac{dc_{m,n}(t)}{dt}=0 & \forall m,n\\[3mm] \lim\limits_{t\to\infty}c_{1,1}(t)\neq 0 \end{array} \right.. (9)\end{equation} These conditions [Eq. (9); hereinafter referred to as the complete merger condition for the square domain] are used to examine how an initial distribution of vorticity will evolve and eventually approach the stationary eigenmode (1,1) at the end of the merging process. It should be mentioned again that both sets of conditions [Eqs. (7) and (9)] are in fact "strong conditions" for a complete vortex merger. This is because some infinite superposition of coefficients cm,n may exist such that the final function could possess a radially axisymmetric distribution, mimicking a stationary end product of the vortex merging. It will be shown below, however, that the dynamics of the barotropic flows in the square domain possesses very specific characteristics, which do not admit such an arbitrary superposition of general eigenmodes.

    To this end, recall first that the completeness of the orthogonal eigenfunctions [Eq. (8)] over the square domain allows us to expand an arbitrary streamfunction ψ(x,y,t) as follows: \begin{equation} \psi(x,y,t)=\sum_{m=1,n=1}^\infty c_{m,n}(t)\varphi_{m,n}(x,y) . (10)\end{equation} Substituting the solution of Eq. (10) into Eq. (1), we have \endmulticols

    \begin{eqnarray} \sum_{m,n}\lambda_{m,n}\dfrac{dc_{m,n}}{dt}\varphi_{m,n}&=&\sum_{m,n}\sum_{k,l}\dfrac{\pi^2}{L^2}nkc_{m,n}c_{k,l}\lambda_{k,l} \sin\left(\dfrac{m\pi x}{L}\right)\cos\left(\dfrac{n\pi y}{L}\right)\cos\left(\dfrac{k\pi x}{L}\right)\sin\left(\dfrac{l\pi y}{L}\right)-\nonumber\\ &&\sum_{k,l}\sum_{m,n}\dfrac{\pi^2}{L^2}nkc_{k,l}c_{m,n}\lambda_{m,n}\cos\left(\dfrac{k\pi x}{L}\right)\sin\left(\dfrac{l\pi y}{L}\right)\sin\left(\dfrac{m\pi x}{L}\right)\cos\left(\dfrac{n\pi y}{L}\right) , (11)\end{eqnarray}

    where the dummy integer indices (m,n) and (k,l) have been interchanged in the second term on the right-hand side of Eq. (11) to facilitate later grouping. Multiply both sides of Eq. (11) by an eigenfunction φM,N that corresponds to a specific mode (M,N) and integrate both sides with respect to x and y over the entire domain with a note that \begin{eqnarray} &&\int_0^\pi\sin(mx)\cos(kx)\sin(Mx)dx\nonumber\\ &=&\int_0^\pi\dfrac{1}{4}(-\cos[(k-m-M)x]+\cos[(k+m-M)x]+\nonumber\\ &&\cos[(k-m+M)x]-\cos[(k+m+M)x])\nonumber\\ &=&\dfrac{\pi}{4}(\delta_{M,k+m}+\delta_{M,m-k}-\delta_{M,k-m}) , (12)\end{eqnarray} and \begin{equation} \int_0^L\sin\left(\dfrac{m\pi x}{L}\right)\sin\left(\dfrac{M\pi x}{L}\right)dx=\dfrac{L}{2}\delta_{M,m} , (13)\end{equation} where δm,n is the delta Kronecker symbol, we arrive at a governing equation for each eigenmode (M,N) after some rearrangement as follows: \begin{eqnarray} \dfrac{dc_{M,N}}{dt}&=&\dfrac{\pi^2}{2L^2\lambda_{M,N}}\sum_{m,n}\sum_{k,l}nk(\lambda_{k,l}-\lambda_{m,n})c_{m,n}c_{k,l}(\delta_{M,k+m}+\nonumber\\ &&\delta_{M,m-k}-\delta_{M,k-m})\times(\delta_{N,n+l}+\delta_{N,l-n}-\delta_{N,n-l}) .(14) \end{eqnarray} It can be seen from Eq. (14) that if one starts with any specific eigenfunction (K,L), then \(dc_m,n/dt=0,\forall m,n>0\), and the flow will stay at the same initial mode (K,L) at all times, as expected for stationary solutions. Note also that the evolution of each mode (M,N) is strongly coupled to other modes via the double summation over (m,n) and (k,l) on the right-hand side of Eq. (14). As such, the vortex dynamics is inherently nonlinear.

    A couple of remarks can be immediately obtained from Eq. (14). First, the symmetry of the (m,n) and (n,m) modes in Eq. (14) suggests that an initial distribution of vorticity composed of exactly two eigenmodes (K,L) and (L,K), where K,L are any two integer numbers, will not evolve with time. This is because the forcing term on the right-hand side of Eq. (14) will be reduced to only terms of the form ∼(δK,LL,K), or ∼(δK,LK,L), which are all canceled out because of Λm,nn,m, and so \(dc_M,N/dt=0,\forall M,N\). While this property depends crucially on the square topology of the domain, it highlights a subtle characteristic of the multiple vortex interaction. Imagine one starts with a vorticity distribution consisting of two specific amplitude modes c9,10=1 and c10,9=1, which resembles a set of small-scale like-signed vorticity centers as shown in Fig. 3. The gross overall picture of multiple like-signed vorticity centers may provide one with some intuitive feeling that these like-signed vortices may soon interact, merge, and grow upscale. As seen above, such a vortex merger could not, however, take place; the entire vorticity distribution simply stays the same without any evolution or interaction at all.

    Of further importance is an observation about the delta Kronecker symbols on the right-hand side of Eq. (14) for which the subscripts are always combinations of either k m or l n. This property dictates that if one starts with an initial vorticity distribution containing either purely even modes (i.e., both k and m are even) or purely odd modes (i.e., both k and m are odd) in one specific direction (either x or y), then the subsequent evolution will involve either entirely even modes or odd modes in that direction only. This is a direct consequence of the selective Kronecker delta for which the odd superscripts M or N can never be equal to the combination of purely even or odd subscripts m,k or n,l, which are always even numbers. For example, if the initial vorticity distribution is given by several even modes along the x direction consisting of (m=2,n-1),(m=4,n=5), and (m=6,n=7), the flow will then quickly spread out over all other even eigenstates along the x direction, as can be seen from Eq. (14), whereas all of the odd eigenstates along the x direction will never appear. In particular, this shows that the most important eigenstate expected for the complete merger condition (m=1,n=1) will never be satisfied (i.e., \(\lim_{t\to\infty} c_1,1\neq 0\) cannot occur) despite the strong interaction of vortices. As such, the complete merger condition [Eq. (9)] is not ensured, and the vortex merging process will never end up in a single vortex patch at the center as one would expect from the complete vortex merging process.

    Figure 3.  Distribution of nondimensionalized streamfunction (shaded), which is composed of exactly two eigenmodes, $(9,10)$ and $(10,9)$, with amplitudes $c_9,10=-1$ and $c_10,9=-1$.

    As an illustration of the above particular selective property of the Kronecker operator, Fig. 4 shows the evolution of the streamfunction and the corresponding horizontal wind components u=-∂ψ/∂ y and v=∂ψ/∂ x, obtained from a numerical integration of Eq. (14). Here, the numerical experiment is carried out for a square domain [0,1000\; km]× [0,1000\; km] on an f-plane located at 30°N, with homogeneous boundary conditions and an initial condition consisting of three eigenmodes of c10,10=1,c12,12=1, and c14,14=1, where the amplitudes are scaled by a factor L2f. A spectrum truncation of 30 normal modes is applied in both the x and y directions, and the integration time-step is fixed at 120 s.

    One notices in Fig. 4 that, clearly, despite strong evolution of the vortex patches with time, there is no global merger of like-signed vortices. In fact, the initial condition consisting of the above selected even modes results in a complete cancellation of the wave amplitudes at the center of the domain, such that there is no way for the vorticity centers to aggregate at the center of the domain; all vortex merging can only take place locally, away from the domain center, and the complete merger with a single vortex patch at the domain center never occurs. While the merging of the vorticity cannot be aggregated toward the center of the domain, note that multiple vortex mergers could take place elsewhere, which is seen by the development of several major patches of vorticity in four quadrants shown in Figs. 4c-e. Such self-organization of small-scale vortices is consistent with the concept of "vortex relaxation" into large-scale structures due to minimization (or maximization) of potential intrinsic invariants of the barotropic fluid such as enstrophy, energy, or helicity (e.g., Brown, 1997). However, the type of larger-scale vorticity patches shown in Figs. 4b and c does not grow upscale indefinitely, but instead breaks down subsequently, as seen in Fig. 4f. The processes of vortex merging and breaking down take place around 2000 time-steps. One can in principle increase the degree of vortex interaction by either using a larger wave amplitude to increase the vortex strength, or selecting higher wavenumbers to reduce the distances between like-signed vortices. Nevertheless, a complete vortex merger with relaxation towards a single stationary vortex at the domain center could not take place due to the selective mode of the barotropic dynamics. Of course, the vortex merging process seen in Fig. 4 is particularly inherent to the inviscid barotropic model, and it will change entirely if diffusion forcings or higher dimensions are introduced. However, this barotropic merging process could demonstrate the intricate dynamics that a simple merging scenario for like-signed vortices may not always apply.

    Figure 4.  Snapshots of the nondimensionalized streamfunction $\psi$ (shaded) and the corresponding horizontal wind components $(u,v)$ (vectors) on an $f$-plane located at 30$^\circ$N, which are valid at $t=0$ h, $t\approx6.5$ h, $t\approx13$ h, $t\approx19.5$ h and $t\approx 27$ h, which correspond to 0, 200, 400, 600, 800 and 1000 time-steps into the integration, using Eq. (14).

    It is worth emphasizing that, unlike the superposition of two symmetric states, which leads to stationary dynamics due to the topology of the square domain shown in Fig. 3, the evolution of either purely even or odd eigenstates illustrated in Fig. 4 is a general property of the governing equation [Eq. (14)] related to the completeness of the eigenfunctions φm,n. In fact, this selective property of the Kronecker symbols has an even stronger implication, as it essentially eliminates any possibility of superimposing arbitrary eigenfunctions φm,n to obtain a stationary Gaussian-like state for the complete vortex merger. To the best of the author's knowledge, no superposition of purely even or odd sinusoidal modes along the x or y direction has been known that could produce a Gaussian-like profile for vorticity at the domain center to mimic the complete merger expectation. From this perspective, the unique selective property of Eq. (14) suggests that simple intuition regarding the merging of like-signed vortices should be taken with caution, as it may not be applicable.

    Except for the above special characteristics of Eq. (14) that result in either strictly stationary states or interaction among eigenmodes in some selective way, an arbitrary vorticity arrangement will overall be distributed across the whole spectrum of eigenfunctions quickly with time, and it seems to have no stationary end state as one would expect for the complete merger. For the sake of discussion, consider an arbitrary initial field ψ(x,y,0) that consists of only three eigenstates of (m=1,n=1),(m=1,n=2) and (m=2,n=1) (i.e., \(c_1,1(0)\neq0,c_1,2\neq0\), and \(c_2,1(0)\neq 0\)), which roughly correspond to a vortex at the center of the domain surrounded by two lumps of vorticity along its x and y direction. The purpose is to see if the superposition of these three eigenstates in this example could eventually become a single stationary mode of (m=1,n=1) that represents a resulting merged vortex. More general distribution of ψ(x,y,0) can be similarly examined along the same line of argument. Given such an initial condition, Eq. (14) gives us a sequence of spectral evolution shown in Table 1. As seen in Table 1, the strong nonlinear coupling of all eigenstates in Eq. (14) leads to rapid expansion of the flow over many other eigenstates after just a few time steps. If one continues the integration of Eq. (14) further in time, the entire eigenfunctions spectrum would be occupied quickly, and there appears to be no simple setup to guarantee that the complete merger condition [Eq. (9)] could be ensured in general.

    It is of interest to mention that the rapid distribution of barotropic flow over the whole eigenfunction spectrum can also be applied for the β-plane vorticity equation due to the orthogonality of the eigenfunctions φm,n. As discussed in (Yasuda, 1995), the β-effects will, however, complicate the vortex merging process by creating asymmetry of the vortex merging along the south-north direction, and the vortex merger becomes even less complete. In particular, (Prieto et al., 2003) showed that inclusion of the β-effect can significantly slow down the mutual rotation between two vortices, as the Coriolis forcing is weaker at higher latitudes, thus lengthening the merging process. These details are hard to formulate from the analytical perspective, because the stationary states may not exist for the β-plane dynamics. However, the completeness of the eigenfunctions φm,n still at least allows for the expansion [Eq. (10)], and therefore the spread of the eigenfunction spectrum as seen for the f-plane dynamics can still be valid. This continuous spread over the whole eigenfunction spectrum appears to explain the formation of vorticity skirts wrapping around the other vortex instead of a single enhanced circulation seen at the end of the complete vortex merger case, as presented in (Prieto et al., 2003) and (Kuo et al., 2008).

    It should be noted that the spread of the eigenmodes over the spectrum of the Laplacian eigenfunctions does not sufficiently imply that the vortex merging will never take place for all configurations. It is still possible that, as time goes on, the flow may evolve in such a way that \(c_m,n\to \in,\forall m,n\neq 1\), where is an arbitrarily small number, such that, practically, one may no longer be able to notice any other modes except for the dominant mode of (m=1,n=1) from a numerical viewpoint. For these situations, it is reasonable to state that these higher wavenumber modes diminish to a point that the merging is considered to be practically complete. While such an argument could be applied from the numerical standpoint, apparently it requires one to define carefully how small a perturbation would be so that it can be numerically neglected. To the best of the author's knowledge, there is no known configuration at present that could strictly ensure the complete merger conditions [Eq. (9)] for the barotropic dynamics as given by Eq. (1), and so it is more likely that the complete vortex merging processes may never occur in the sense of the complete merger condition [Eq. (9)].

3. Concluding remarks
  • This study analyzes the 2D vortex dynamics governed by the inviscid barotropic vorticity equation. By noting that the Jacobian operator in the vorticity equation of the form J(ψ,∇2ψ) accepts a set of stationary solutions that are inherently eigenfunctions of the Laplacian operator, it is found that the vortex evolution can be decomposed into a set of spectral components that evolve according to a system of highly nonlinear constraints. Given the specific shapes and characteristics of the eigenfunctions of the Laplacian operator with a prescribed boundary, it is shown that sufficient conditions exist for the vortex merging process to be considered strictly complete.

    Examination of the vortex dynamics for a square domain with periodic boundary conditions shows that, unlike the common expectation of merging of like-signed vortices, the complete merger is not guaranteed for an arbitrary initial distribution of vorticity. In fact, it is demonstrated that there are certain initial combinations of vorticity that the complete vortex merger condition can never be satisfied. Specifically, the superposition of eigenmodes that are purely even or odd in either the x or y direction will lead to an evolution that contains only even modes in either the x or y direction at all times, regardless of how close and strong like-signed vortices are. In a more extreme case with two symmetric sinusoidal modes, the dynamics is even strictly stationary, and no vortex merging would take place. Analyses of the more general cases also suggests that an arbitrary vorticity distribution at the initial time would quickly spread out over the whole spectrum of the eigenfunctions of the Laplacian operator, and there is no guarantee that modes with higher wavenumbers would diminish in time such that the flow would settle in a final state with a single vortex patch at the center of interaction.

    It is important to note that the results obtained in this study are very specific for inviscid barotropic fluid, and by no means encompass the full range of vortex interactions. In particular, the strict definition of the complete vortex merger, as given by either the condition for a circular domain [Eq. (7)] or a square domain [Eq. (9)], is too strong such that no configuration may exist for the complete vortex merger to occur. In practice, it is possible that the vortex dynamics in a 3D space or inclusion of viscosity may allow for a complete merger and subsequent upscale growth of the resulting vortex (Kieu and Zhang, 2009; Huang and Xu, 2010; Luo et al., 2014). However, the barotropic model in this study suffices to demonstrate that an intuitive notion of merging of like-signed vortices, which is often assumed in studies of multiple vortex interaction, is highly intricate and should be taken with caution, as the vortex merger may not lead to an eventually enhanced circulation as one would expect.

Reference

Catalog

    /

    DownLoad:  Full-Size Img  PowerPoint
    Return
    Return